Stratno | Stratigraphic Name | Category | Contents | Last update 
37738|Accident Subgroup|Name source|Accident Creek, passing through latitude 18deg05'S longitude 138deg20'E, is an east-flowing tributary of the Gregory River in northwestern LAWN HILL, Queensland.|16-MAY-23
37738|Accident Subgroup|Unit history|Incorporates all of the South Nicholson Group mapped in Queensland (LAWN HILL and WESTMORELAND), ie the Constance Sandstone, Mullera Formation and Tidna Sandstone (Carter and Zimmerman 1960; Carter et al 1961), in the southeastern quarter of CALVERT HILLS (Ahmad and Wygralak 1989), and in the eastern third of MOUNT DRUMMOND (Smith and Roberts 1963). It also includes all of the Mittiebah Sandstone, Constance Sandstone and Mullera Formation mapped in the western two-thirds of MOUNT DRUMMOND (as revised by Rawlings et al in prep. on the second edition of the geological map). Small areas of Mittiebah Sandstone on northern Ranken, eastern Brunette Downs and southwestern Calvert Hills sheet areas are also included.|16-MAY-23
37738|Accident Subgroup|Constituents|From base to top: Constance Sandstone and its members, Mittiebah Sandstone, Mullera Formation and its members, Tidna Sandstone.|16-MAY-23
37738|Accident Subgroup|Geomorphic expression|Resistant ridge-forming basal part (sandstone-dominated units) and alternating ridge and recessive upper part (siltstone and shale dominated unit with sandstone and ironstone interbeds).|16-MAY-23
37738|Accident Subgroup|Type section locality|A complete section in an area of relatively high dips, and therefore geographically compact, is located south of Elizabeth Creek, from the Constance Range escarpment in the east, westwards for 8 km, to the core of a syncline. It runs from the base of the Constance Sandstone, at Latitude 18deg14'41"S Longitude 138deg23'28"E (224125E 7980770N), southwest for 1.7 km to the top of the Constance Sandstone, at Latitude 18deg14'57"S Longitude 138deg22'37"E (222623E 7980270N), then west for 6.4 km to the youngest beds in the Tidna Sandstone in the centre of the syncline, at Latitude 18deg14'57"S Longitude 138deg18'56" (216123E 7980170N).|16-MAY-23
37738|Accident Subgroup|Extent|Outcrops in the following 1:250 000 sheet areas: throughout MOUNT DRUMMOND, southeastern quarter of CALVERT HILLS, northeastern BRUNETTE DOWNS, northwestern RANKEN (all in the Northern Territory); and southwestern WESTMORELAND and western LAWN HILL (Queensland). Total area of outcrop and known shallow subcrop approaches 16 000 sq km.|16-MAY-23
37738|Accident Subgroup|Thickness range|From a minimum of ~400 m in southeastern MOUNT DRUMMOND, up to 3350 m in the Constance Range region in western LAWN HILL.|16-MAY-23
37738|Accident Subgroup|Lithology|A succession of sandstone, siltstone, shale and minor conglomerate and sedimentary ironstone.|16-MAY-23
37738|Accident Subgroup|Depositional environment|Mainly shallow marine, ranging to deeper water, including storm-dominated shelf, and shoreface environments; possibly minor fluvial.|16-MAY-23
37738|Accident Subgroup|Relationships and boundaries|Disconformably overlies Wild Cow Subgroup in the west and unconformably overlies McNamara and Fickling Groups in the east. In the Bauhinia Dome, it unconformably overlies Caulfield beds. Unconformably overlain by Neoproterozoic Bukalara Sandstone in northwestern MOUNT DRUMMOND, and by the Georgina Basin succession in southern MOUNT DRUMMOND and western LAWN HILL.|16-MAY-23
37738|Accident Subgroup|Age reasons|Isotopic dating is currently unavailable for any part of the South Nicholson Group and its age is therefore internally unconstrained. The maximum age of 1595+/-6 Ma is that of the Lawn Hill Formation at the top of the underlying McNamara Group (Page and Sweet 1998). There are no minimum age constraints imposed by overlying units, apart from the late Neoproterozoic to Phanerozoic Georgina Basin. The interpreted age range of the Accident Subgroup of 1500 to 1400 Ma is based on correlation with the Roper Group of the southern McArthur Basin, which combined, make up the Roper superbasin (Jackson et al 1999, Abbott et al 2001). Ages of 1492±4 and 1493±4 Ma for tuffaceous material from the lower Roper Group (Jackson et al 1999) provides the most reliable estimate for the age of that Group, and hence for the South Nicholson Group, including the Accident Subgroup.|16-MAY-23
37738|Accident Subgroup|Correlations|Middle to upper Roper (Jackson et al 1999) and Renner Groups (Hussey et al 2001).|16-MAY-23
37738|Accident Subgroup|Defn author|Ian Sweet, May 2006|16-MAY-23
37738|Accident Subgroup|Comments|This package of rocks has been accorded subgroup status because a disconformity has been recognised within the South Nicholson Group. The lower and upper parts (both now subgroups) also have distinct facies patterns and depocentres. Although the Mittiebah Sandstone is remote from the main outcrop belt, which is in Queensland and eastern parts of the NT, it is included in the Subgroup on the basis of its firm correlation with the Constance Sandstone, the basal formation of the Subgroup.|16-MAY-23
37738|Accident Subgroup|References|ABBOTT S.T., Sweet I.P., Plumb K.A., Young D.N., Cutovinos A., Ferenczi P.A., Brakel A. and Pietsch B.A., 2001. Roper region: Urapunga and Roper River special, Northern Territory (Second Edition); 1:250 000 Geological Map Series, sheets SD53-10,11. Northern Territory Geological Survey-Australian Geological Survey Organisation (NGMA), Map and Explanatory Notes.  **AHMAD M. and Wygralak A.S., 1989. Calvert Hills, Northern Territory (First Edition); 1:250 000 Metallogenic Map Series, sheet SE53-8. Northern Territory Geological Survey, Map and Explanatory Notes.  **CARTER E.K., Brooks J.H. and Walker K.R., 1961. The Precambrian mineral belt of northwestern Queensland. Bureau of Mineral Resources, Bulletin, 51.  **CARTER E.K. and Zimmerman D.O., 1960. Constance Range iron deposits, northwestern Queensland. Bureau of Mineral Resources, Record, 1960/75.  **HUSSEY K.J., Beier P.R., Crispe A.J., Donnellan N. and Kruse P.D. 2001. Helen Springs, Northern Territory (Second Edition); 1:250 000 geological series, sheet SE53-10.  **JACKSON M.J., Sweet I.P., Page R.W. and Bradshaw B.E., 1999. The South Nicholson and Roper Groups: evidence for the early Proterozoic Roper Superbasin. In: Bradshaw B.E. and Scott D.L. (Eds.), Integrated basin analysis of the Isa Superbasin using seismic, well-log and geopotential data: an evaluation of the economic potential of the northern Lawn Hill Platform. Australian Geological Survey Organisation, Record 1999/19 (unpaginated).  **PAGE R.W. and Sweet I.P., 1998. Geochronology of basin phases in the western Mount Isa Inlier, and correlation with the McArthur Basin. Australian Journal of Earth Sciences, 45, 2; 219-232.  **SMITH J.W. and Roberts H.G., 1963. Mount Drummond, N.T. (First Edition); 1:250,000 geological series, sheet SE53-12. Bureau of Mineral Resources, Geology and Geophysics, Map and Explanatory Notes.|16-MAY-23
37738|Accident Subgroup|Parent|South Nicholson Group.|16-MAY-23
26290|Adler Hill Basalt|Name source|Adler Hill (GR 426152, Bartle Frere 1:100 000 Sheet area, 8063) 11 km southeast of Mareeba, Queensland.|16-MAY-23
26290|Adler Hill Basalt|Unit history|Previously included in the Atherton Basalt by Best (1960) and de Keyser (1964).|16-MAY-23
26290|Adler Hill Basalt|Type section locality|The eastern edge of Adler Hill is the designated type locality. There vesicular and massive basalt are exposed.|16-MAY-23
26290|Adler Hill Basalt|Extent|Adler Hill double volcanic cone, its flanks, and a few basaltic lava flows which flowed down the valley of an unnamed tributary of Emerald Creek, covering about 4 km2.|16-MAY-23
26290|Adler Hill Basalt|Lithology|The basalt is dark grey, fine grained and porphyritic with phenocrysts of olivine and subordinate augit. The extent of weathering makes it difficult to accurately determine the number of flows.|16-MAY-23
26290|Adler Hill Basalt|Relationships and boundaries|The Adler Hill Basalt is considered to represent some of the volcanic activity in the Atherton Volcanic Province. Basaltic lavas and ejecta were erupted from the composite double cone at Adler Hill and unconformably overlie basement rocks comprising metasediments of the Hodgkinson Formation, and the Mareeba Granite.|16-MAY-23
26290|Adler Hill Basalt|Age reasons|Believed to be Pliocene to Pleistocene, based on ages obtained from other volcanoes in the Atherton area.|16-MAY-23
26290|Adler Hill Basalt|References|60/078; 63/079;B084; 82/22416|16-MAY-23
27685|Agate Downs Siltstone|Name source|Named after Agate Down outstation, GR 388382, in SE of Malbon 1:100 000 Sheet area.|16-MAY-23
27685|Agate Downs Siltstone|Unit history|Termed Agate Downs Siltstone Member of the Staveley Formation by Carter & others (1961), but not shown on any published map.|16-MAY-23
27685|Agate Downs Siltstone|Type section locality|From GR 378324 to 388324, a point 5 km WNW of the Tin Top mine, Malbon 1:100 000 sheet area. This is the part of the type section for the Staveley Formation of Carter & others (1961) which comprises the former Agate Downs Siltstone Member now Agate Downs Siltstone formation. Ridge-forming brown and grey siltstone, fine-grained sandstone and fine quartzite and less resistant phyllite are exposed here.|16-MAY-23
27685|Agate Downs Siltstone|Extent|The unit crops out as a linear N-trending belt 25 km long and up to 2.5 km wide, extending from GR 398189 in NE part of Mount Merlin 1:100 000 sheet area to GR 413420 in SE part of Malbon 1:100 000 sheet area, Duchess 1:250 000 sheet area.|16-MAY-23
27685|Agate Downs Siltstone|Thickness range|Maximum probably about 1000 m.|16-MAY-23
27685|Agate Downs Siltstone|Lithology|Consists of siliceous, ferruginous, and less commonly calcareous siltstone and fine-grained sandstone; quartzite, phyllite, and minor slate and breccia.|16-MAY-23
27685|Agate Downs Siltstone|Relationships and boundaries|The unit overlies Staveley Formation, apparently conformably.|16-MAY-23
27685|Agate Downs Siltstone|Age reasons|Proterozoic|16-MAY-23
27685|Agate Downs Siltstone|Comments|Cross-bedding and ripple marks indicate that the unit is preserved as a complex isoclinal syncline, and that it overlies the Staveley Formation rather than forming the lower part of this formation, as stated by Carter and others (1961). For this reason, and because it has a distinctive mappable lithology, the Agate Downs Siltstone is upgraded to formation status.|16-MAY-23
27685|Agate Downs Siltstone|References|B051|16-MAY-23
39010|Alice Creek beds|Name source|The name is derived from Alice Creek a tributary of Lockyer Creek.|16-MAY-23
39010|Alice Creek beds|Unit history|Geological mapping in the area of outcrop of this unit was undertaken as part of the production of the Ipswich and Brisbane 1:250 000 map sheets (Cranfield & others, 1976).  The rocks in this area were considered to form part of the Permian Cressbrook Creek Group however the discovery of Leptophloem in mapping by students of USQ in the early 1970s confirmed a Late Devonian to Early Carboniferous age for the upper part of this unit.  Conodonts of Mid to Lower Devonian age (Dr. B. Fordham, personal communication 1998) have been recovered from bodies of reworked limestone in the lower part of the unit .|16-MAY-23
39010|Alice Creek beds|Geomorphic expression|The unit is characterised by a subdued topography below resistant outcrop of Woogaroo Subgroup.  The unit forms the bed of Alice Creek and hill slopes to the east of Alice Creek.|16-MAY-23
39010|Alice Creek beds|Type section locality|The type section is designated along Alice Creek from AMG 417400 6962900 to 416500 6962000.  Rock types in the type section comprise predominantly volcanolithic pebble conglomerate and arenite, and minor siltstone.  Small limestone outcrops occur in the vicinity of AMG 417400 6963300 and AMG 417100 6963600.  The grid references are based on the AGD66 datum.|16-MAY-23
39010|Alice Creek beds|Extent|The unit is exposed along Alice Creek north of Helidon.  The area of outcrop is about 2 km2 and is limited to the bed of the Alice Creek and hill slopes to the east of the creek.|16-MAY-23
39010|Alice Creek beds|Thickness range|The Alice Creek Beds have an exposed thickness of about 1000m.  It is not known what effect structural thickening has had on the true thickness of the unit.|16-MAY-23
39010|Alice Creek beds|Lithology|Rock types from Alice Creek comprise volcanolithic conglomerate, lithic arenite and minor interbedded chert, silicified siltstone and mudstone. Small limestone outcrops occur in the lower part of the unit. The conglomerate contains pebbles of andesitic to rhyolitic volcanic fragments with minor chert in a feldspathic sandy matrix (Ross, 1986).  Chert is generally dark grey to dark green in colour and forms massive blocky jointed outcrops.  Indurated mudstone forms thin interbeds in the otherwise massive chert.  The andesitic volcanics are dark grey to black in colour and comprise minute plagioclase laths in a fine-grained aphanitic groundmass.  The arenite is fine grained and volcaniclastic.  Thin section studies indicate radiolarians are present in siltstones (Ross, 1986).  Smith (1974) collected an example of Leptophloem australe (McCoy) from a slate at AMG 416500 6961900 (U.S.Q. collection No. F462). The limestone bodies are possibly allochthonous.  The larger body, at AMG 417400 6963300, occurs as discontinuous outcrop over about 100m and contains contains crinoid ossicles and Thamnopora sp in rounded clasts up to 30mm (Ross, 1986).  The limestone body at AMG 417100 6963600 is smaller and has a prominent schistosity trending east west, dipping to the south (Ross, 1986).  The grid references are based on the AGD66 datum.|16-MAY-23
39010|Alice Creek beds|Depositional environment|The Alice Creek Beds are interpreted as being deposited in a marine environment, close to a continental margin with an active volcanic arc, i.e a forearc environment.  PROVENANCE:  At least some of the sediment was supplied from Early to Mid Devonian limestone reefs and was considered by Ross (1986) to be locally derived due to the sparry nature of the matrix adjacent to the limestone pebbles.  The conglomerate and sandstone consist of volcanic fragments and minor chert in a feldspathic sandy matrix (Ross, 1986), indicating a general volcanic provenance.  Thin section studies indicate radiolarians are present in siltstones (Ross 1986) suggesting a marine environment.|16-MAY-23
39010|Alice Creek beds|Relationships and boundaries|The Woogaroo Sub-Group unconformably overlies the unit.  The Mount Cross Igneous Complex and unnamed Permian to Triassic granitoids intrude and are faulted against the unit.|16-MAY-23
39010|Alice Creek beds|Age reasons|Smith (1974) identified Leptophloeum australe (McCoy) from Alice Creek, 2.5 km south-south-west of Mount Cross. This indicates that the rocks in this part of Alice Creek area are of Late Devonian to Early Carboniferous age.  Conodont faunas identified by Fordham (personal communication) indicate an Early to Mid Devonian (Late Emsian to Early Eifelian) age for the limestones at the base of the sequence.  Crinoid ossicles and Thamnopora were identified in rounded clasts from one of the limestone bodies (Ross, 1986).  These limestones are possibly allochtonous.  Thin section studies indicate radiolarians are present in siltstones (Ross 1986).  A Late Devonian to Early Carboniferous age has been assigned to the unit, but the lower part of the unit may be of Early to Mid Devonian age.|16-MAY-23
39010|Alice Creek beds|Correlations|The unit may be a correlative of the Brovinia beds, but on fossil evidence appears slightly older.|16-MAY-23
39010|Alice Creek beds|Comments|GEOPHYSICAL EXPRESSION::  The unit has a low magnetic response.  On the K-Th-U (RGB) ternary radiometric image the unit has an indistinct response due to the limited outcrop area.  STRUCTURE::  Dips in the Alice Creek Beds are generally to the south and south-west at about 70 to 80 degrees.  Shearing has been observed in the unit to increase in intensity towards a major east west fault at the northern extent of the unit (Ross 1986).|16-MAY-23
39010|Alice Creek beds|References|CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.",1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional Geology.  ROSS, C.J.,1986,The sediments of Mt. Cross, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.  SMITH,P.E.,1974,The Geology of the Mount Cross Area, Parish of Murphy, South Eastern Queensland, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.|16-MAY-23
305|Allingham Formation|Name source|Outcrops in valley and banks of Allingham Creek around 19 degrees 43' S, 145 degrees 37' E, Townsville  1:250 000 map sheet, Hillgrove 1:100 000.|16-MAY-23
305|Allingham Formation|Type section locality|Contunuous outcrop on N bank of Allingham Creek from 5.4 to 5.8 km W of Emu Valley Homestead.|16-MAY-23
305|Allingham Formation|Extent|The unit is exposed where the creek valley cuts through plateau basalt and outcrop is threfore narrow and elongate. At present it is known over a length of 8 km.|16-MAY-23
305|Allingham Formation|Defn author|M. Archer, M.Wade, 19-SEP-1974.|16-MAY-23
29337|Almaden Granodiorite|Name source|The unit is named after Almaden township and railway siding in the southwestern part of CHILLAGOE.|16-MAY-23
29337|Almaden Granodiorite|Unit history|Previously mapped as part of the Almaden Granite (Best, 1962;  de Keyser & Wolff, 1964;  Branch, 1966), which was subsequently subdivided by Richards (1981).|16-MAY-23
29337|Almaden Granodiorite|Geomorphic expression|The unit forms mainly gently undulating terrain with scattered rounded boulders and bouldery outcrops.  A few bouldery hills are also present.  Areas underlain by the granodiorite have open drainage patterns and show mainly pale to moderate tones on aerial photographs.|16-MAY-23
29337|Almaden Granodiorite|Type section locality|The proposed type area is between the township of Almaden (GR 2530 80813) and the Ootann turnoff (GR 2514 80800) on the Burke Developmental Road to the west.  grid references are based on the AGD66 datum.|16-MAY-23
29337|Almaden Granodiorite|Description at type locality|The granodiorite forms scattered large rounded boulders and a few bouldery outcrops in this area.|16-MAY-23
29337|Almaden Granodiorite|Extent|The granodiorite forms an elongate northwest-trending pluton of about 150 km2, extending from 5 km south of Almaden to the abandoned mining centre of Calcifer.|16-MAY-23
29337|Almaden Granodiorite|General description|STRUCTURAL AND METAMORPHISM:  The Almaden Granodiorite was emplaced as an elongate northwesterly trending pluton, at relatively high crustal levels.  The northwesterly trend of the pluton parallels the prevailing trend in the adjacent Chillagoe and Hodgkinson Formations and may have been controlled by the northwesterly trending Palmerville Fault to the west as postulated by de Keyser (1963).  The granodiorite is essentially massive and unmetamorphosed.|16-MAY-23
29337|Almaden Granodiorite|Lithology|Grey, medium to coarse-grained, variably porphyritic hornblende-biotite granodiorite and biotite-hornblende granodiorite are the dominant lithologies.  The unit also includes some hornblende-biotite adamellite and tonalite, and possibly quartz monzodiorite.  Ovoid mafic xenoliths up to 30 cm across are common.   DETAILED LITHOLOGY:  Southeast of Chillagoe (at GR 381 000) granodiorite adjacent to the contact with extensively metasomatised country rocks has a sheeted appearance due to the presence of layers up to 15 cm thick of pale brown garnet-rich calc-silicate rock alternating with layers of relatively little-altered granodiorite.  Zones and vein-like bodies of magnetite-hematite rock were found granodiorite adjacent to the contact in the Calcifer area to the south.  These features may have resulted from 'back veining' of the granodiorite along joints and cracks by hydrothermal solutions involved in the widespread development of endo- and exo-skarns in the region.   ALTERATION:  The Almaden Granodiorite, in contrast to the Ruddygore Granodiorite, is generally unaltered.  However, modified granitoid (endoskarn) is common adjacent to contacts with the predominantly calcareous sediments of the Chillagoe and Mount Garnet Formations, and are particularly well developed in the region between Calcifer and Chillagoe.  The endoskarn zones are irregularly distributed and range in width from tens to hundreds of metres and extend for up to a kilometre.  The altered granitoid rocks tend to be relatively resistant to erosion and commonly form hills.  Endoskarns in this region have been briefly described by Dallwitz (in de Keyser & Wolff, 1964 and Branch, 1966) and examined in more detail by Richards (1981), who subdivided the altered granitoid rocks into two groups,  A and B.  Rocks of Richards' first group (A) commonly have a medium to coarse-grained hypidiomorphic granular texture and span the compositional range from unmodified hornblende-biotite granodiorite to sphene leucogranite. The most common rock type is clinopyroxene (diopside?) ± sphene ± epidote/clinozoisite adamellite hand specimens of which are pale grey to pale green and contain pale green clinopyroxene (diopside?) as the predominant mafic mineral.  Rocks of this group make up most of the endoskarn and occur throughout the alteration zone..Rocks of the second group (B) are essentially quartz-plagioclase-clinopyroxene rocks characterised by relatively low SiO2 and K2O and high CaO, and are found immediately adjacent to contacts with exoskarn rocks, limestone, or xenoliths of metasomatised limestone (Richards, 1981), characterised by highly variable mineralogical and chemical compositions..|16-MAY-23
29337|Almaden Granodiorite|Relationships and boundaries|The granodiorite truncates the Chillagoe and Hodgkinson Formations and also intrudes felsic volcanics (Jamtin Rhyolite) of the Featherbed Volcanic Group.  The contact between the granodiorite and Jamtin Rhyolite is well exposed in the bank of Bustard Creek, (at GR 2476 80947), where it generally appears knife-sharp.  The rhyolite adjacent to the contact is extensively recrystallised and cut by rare thin dykes granodiorite.  The granodiorite shows no significant decrease in grainsize adjacent to the contact.  The grid references are based on the AGD66 datum.    A small unnamed pluton of porphyritic hypersthene-augite-hornblende-biotite tonalite (unit Cgd) forming a prominent hill (at GR 2442 80965) east-northeast of the Harper mine, (Calcifer), is surrounded by and cut by dykes from the Almaden Granodiorite.  Inclusions of apparently similar composition are common in the granodiorite.   The Almaden Granodiorite is inferred to intrude the Ootann Granite and to be cut by the Ruddygore Granodiorite (Richards, 1981).  The shapes of intersecting intrusion boundaries were used to determine the relative ages of these plutons (younger pluton boundary convex into older pluton; White & others, 1977).  The Almaden Granodiorite is also cut by the Lucy, Retchford, Jacks, and Burke Granites, the Hiker Granodiorite, by several small unnamed stocks of and dykes of fine to medium-grained mafic granodiorite or quartz diorite, and by small unnamed stocks and dykes of aplite, aplitic granite, biotite leuco-adamellite, porphyritic microgranite and granophyre (rare).|16-MAY-23
29337|Almaden Granodiorite|Age reasons|The unit is Late Carboniferous.  The Almaden Granodiorite has yielded Rb/Sr ages ranging between 301 and 302 Ma (Richards, 1981).  Richards & others (1966) had previously obtained K/Ar ages of 290 and 300 Ma for the Almaden Granodiorite in a reconnaissance study of the region.|16-MAY-23
29337|Almaden Granodiorite|Comments|The Almaden Granodiorite closely resembles the Ruddygore Granodiorite mineralogically and chemically.  It is distinguished by its coarser grainsize, the presence of abundant and relatively large inclusions, the presence of relatively large hornblende laths, and the absence of orthopyroxene (Richards, 1981).   MINERALISATION:  The Almaden Granodiorite hosts the Perseverance lode, a fissure-vein deposit, and one of the largest producers of fluorite in the Chillagoe region.  Gold-bearing vein and fissure-fill lodes occur in the granodiorite near the contact with the Hiker Granodiorite, about 4.5 km east of Fluorspar.  Traces of gold and fluorite have also been found in thin quartz-kaolin lodes which cut the granodiorite near Bungine Creek, about 1.5 km northwest of Fluorspar railway siding.  The widespread metasomatism of the calcareous sediments of the Chillagoe Formation and alteration of the Ruddygore Granodiorite adjacent to the contacts between Calcifer and Chillagoe, with the development of exo- and endo-skarns, is noteworthy.|16-MAY-23
29337|Almaden Granodiorite|References|*BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.   *BRANCH, C.D., 1966:  Volcanic cauldrons, ring complexes, and associated granites of the Georgetown Inlier, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 76.   *DE KEYSER, F., & WOLFF, K.W., 1964:  The geology and mineral resources of the Chillagoe area.  Bureau of Mineral Resources, Australia, Bulletin 70.   *RICHARDS, D.N.G., 1981:  Granitoids of the northern Tate batholith, Chillagoe, north Queensland.  Ph.D. Thesis, James Cook University of North Queensland, Townsville (unpublished).   *RICHARDS, J.R., WHITE, D.A., WEBB, A.W., & BRANCH, C.D., 1966:  Isotopic ages of acid igneous rocks in the Cairns hinterland, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 88.   *WHITE, A.J.R., & CHAPPELL, B.W., 1977:  Ultrametamorphism and granitoid genesis.  Tectonophysics, 43, 7-22.|16-MAY-23
21120|Alpha Granite|Name source|Alpha Gully, a tributary of Homestead Creek which it joins near Allan Hills homestead .|16-MAY-23
21120|Alpha Granite|Unit history|The Alpha Granite was previously included in the felsic phase of the Ravenswood Granodiorite Complex by Wyatt & others (1971), Clarke & Paine (1970).|16-MAY-23
21120|Alpha Granite|Type section locality|A hill, at GR 3547 77474, 2.25km west of Mount Misery near Homestead in the Homestead 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
21120|Alpha Granite|Description at type locality|Here a red to pink, medium to coarse grained, biotite granite crops out. This granite comprises quartz, microperthitic K-feldspar, subhedral plagioclase (mainly oligoclase), glomerophyrric biotite clumps and minor opaques.|16-MAY-23
21120|Alpha Granite|Extent|The Alpha Granite crops out over 10km2 straddling the Flinders Highway about 2km west of Homestead (Figure 2). A further 9km2 of residual soil is thought to overlie the Alpha Granite.|16-MAY-23
21120|Alpha Granite|Lithology|Outcrop along the railway line west of Homestead comprises pink to red, medium grained granite which contains quartz, microperthitic K-feldspar, subhedral oligoclase, biotite, hornblende and minor opaques. Elsewhere in the unit, the granites are deeply weathered but appear similar to the fresher granites described above.|16-MAY-23
21120|Alpha Granite|Relationships and boundaries|The Alpha Granite intrudes the Proterozoic Cape River Metamorphics.|16-MAY-23
21120|Alpha Granite|Age reasons|The age of the Alpha Granite is not known precisely. The fresh outcrop along the railway line was analysed for Rb-Sr systematics and plotted on an isochron which yielded an age of 394+/- 30 Ma (Webb, 1971; in Wyatt and others, 1971). This age is dependent on assumptions about the 87[superscript]Sr/86[superscript]Sr initial ratio and is therefore of questionable value. The Alpha Granite also lies along the northwest trend of the Mundic Igneous Complex and may be related to this suite of intrusives.|16-MAY-23
21120|Alpha Granite|Comments|MAGNETIC SUSCEPTIBILITY::  Magnetic susceptibilities at the type locality are in the range 0-7 x 10[superscript]-5 SI units. The fresh outcrop along the railway line has values of 0-5 x 10[superscript]-5 SI units.|16-MAY-23
21120|Alpha Granite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
332|Alsace Quartzite|Name source|'Alsace' holding near the headwaters of Gunpowder and Myally Creeks, 145 km north of Mount Isa: latitude 19o25'S, longitude 139o35'E, Dobbyn 1:250 000 Sheet area.|16-MAY-23
332|Alsace Quartzite|Type section locality|Near Paroo Creek 20 km southwest of Julius dam, in the Prospector 1:100 000 Sheet area, grid reference 588575, where 400 m of grey to pink feldspathic quartzite are cut by the Mount Isa-Julius dam pipeline road; latitude 20o16'45"S, longitude 139o38'45"E to latitude 20o16'25"S, longitude 139o39'E.|16-MAY-23
332|Alsace Quartzite|Extent|The formation is exposed in a north-trending belt 200 km long by 50 km wide. Mount Isa is near the southern limit of the formation.|16-MAY-23
332|Alsace Quartzite|Thickness range|70 to 600 m; average thickness is near 350 m.|16-MAY-23
332|Alsace Quartzite|Lithology|Quartzite, sandstone, grey-pink, feldspathic to quartzose, medium to coarse-grained, massive to blocky, thick to thin-bedded; contains some clayey rock fragments; thin grey-green siltstone interbeds near the top. The formation forms resistant ridges and plateaux.|16-MAY-23
332|Alsace Quartzite|Relationships and boundaries|Conformably overlies basalt and purple siltstone of the top most Eastern Creek Volcanics (Pickwick Metabasalt Member); overlain conformably by the Bortala Formation, and unconformably by the Mount Isa Group in the Paroo Range, 30 km north of Mount Isa.|16-MAY-23
332|Alsace Quartzite|Age reasons|Carpentarian; minimum age about 1650 m.y. set by Sybella Granite intrusive into time equivalents of the Alsace Quartzite, west of Mount Isa.|16-MAY-23
332|Alsace Quartzite|Comments|This formation was formerly an undifferentiated part of the Myally Beds (Carter et al. 1961); it is now the oldest formation in the redefined Myally Subgroup of the Haslingden Group.|16-MAY-23
332|Alsace Quartzite|References|B051|16-MAY-23
332|Alsace Quartzite|Name first published by|Glikson A.V., Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
21125|Amarra Granite|Name source|Amarra homestead , on the Lolworth to Glen Dillon road, about 15km east northeast of Lolworth homestead at GR 3093 77725.  The grid reference is based on the AGD66 datum.|16-MAY-23
21125|Amarra Granite|Unit history|PREVIOUS NOMENCLATURE::  The Amarra Granite was previously included in the Lolworth Igneous Complex by Paine & others (1971) and Vine & Paine (1974)|16-MAY-23
21125|Amarra Granite|Type section locality|The type locality of the Amarra Granite is near the junction of Brandy and Bushman Creeks, at GR 3233 77681, about 6km south of the Lolworth diggings in the Lolworth 1:100 000 Sheet area. Here, a medium grained, sparsely porphyritic muscovite, biotite granite crops out.  The grid reference is based on the AGD66 datum.|16-MAY-23
21125|Amarra Granite|Description at type locality|The granite has large poikilitic K-feldspar phenocrysts in a matrix of quartz, K-feldspar, plagioclase, albite, biotite and muscovite.|16-MAY-23
21125|Amarra Granite|Lithology|Medium grained, sparsely to commonly porphyritic, biotite and muscovite biotite granite occurs over a wide area in the eastern part of the Lolworth 1:100 000 Sheet area. In the western part of the Homestead 1:100 000 Sheet area the unit is similar but is locally more altered. The granite is extensively intruded, particularly in the east, by leucocratic granite dykes and large subhorizontally layered bodies that are lithologically similar to the Grasstree Leucogranite.|16-MAY-23
21125|Amarra Granite|Relationships and boundaries|The Amarra Granite intrudes the Cape River Metamorphics in the south and southeast (Figure 2).It appears to be intruded by: the Dillons Knob Granite to the west; the Weaner Vale Granite in the Lolworth goldfield area; and the Grasstree Granite to the northeast. Leucogranites, similar to the Grasstree Leucogranite intrude the unit as dykes and large subhorizontally layered bodies, particularly in the northeast.|16-MAY-23
21125|Amarra Granite|Age reasons|The age of the Amarra Granite is Early Devonian. An age of 382 +/- 5 Ma was determined using 206[superscript]Pb/238[superscript]U from SHRIMP microprobe analysis of zircon grains on a sample from the type locality (Fanning, 1995).K-Ar and Rb-Sr ages of 400-409 Ma (recalculated using the decay constants of Steiger & Jager, 1977 and Dalyrmple, 1978) was assigned to the Lolworth Igneous Complex by Webb (1971).|16-MAY-23
21125|Amarra Granite|Comments|MAGNETIC SUSCEPTIBILITY::  Magnetic susceptibilities are 127-182 x 10[superscript]-5 SI units in the type locality and 0-400 x 10[superscript]-5 SI units within the unit. Most rocks lie in the range 100-350 x 10[superscript]-5 SI units. Rocks in the southeast of the pluton are non-magnetic and may be altered.|16-MAY-23
21125|Amarra Granite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
35059|Amarra Suite|Constituents|Amarra Granite, Dillons Knob Granite, Davey Creek Granite, Reedybed Granite, Myola Granite, Redlands Granite, Weaner Vale Granite, and Bulgin Creek Granite.|16-MAY-23
35059|Amarra Suite|Lithology|Made up of muscovite-biotite granite and comprises most of the area of the Lolworth Batholith, particularly in the west. It is characterised by the presence of quartz, large poikilitic k-feldspar, subhedral albite, plagioclase, muscovite and biotite. Magnetic susceptibilities range from non-magnetic for the more altered samples to about 800 x 10-5 SI units. Most samples average 100-300 x 10-5 SI units.|16-MAY-23
35059|Amarra Suite|Relationships and boundaries|Granites of the Amarra Suite are intruded by leucogranites of the Grasstree Suite over the whole area of the batholith.|16-MAY-23
35059|Amarra Suite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
401|Anakie Metamorphic Group|Name source|Anakie Inlier.|16-MAY-23
401|Anakie Metamorphic Group|Unit history|Jensen (1921) used the term Anakie Series for granite, porphyry, schist and slate in the Anakie area, but assigned the metamorphic rocks in the Clermont area to the Clermont Series. Reid (1936) later used the term Clermont Slates for the same rocks. The name Anakie Metamorphics was first used on the Geological Map of Queensland (1953) for 'undifferentiated Lower Palaeozoic rocks' extending from Anakie to southwest of Collinsville.   Joint mapping by the Bureau of Mineral Resources - Geological Survey of Queensland parties in 1960-1961 defined the extent of the Anakie Metamorphics (Malone & others, 1964; Veevers & others, 1964a, b), but only brief descriptions of the rocks were published. Later mapping by mineral exploration companies (Utah Development Company, 1971; Beunderman, 1974) recognised that the Anakie Metamorphics could be subdivided. Utah geologists recognised three broad divisions:Unit III - an upper sequence of micaceous quartzite, quartz-rich sandstone, phyllite, slate and minor schist, supposedly unconformable on Unit II, because of an apparent lower metamorphic grade. Unit II - a sequence of muscovite-quartz schist, chloritic near the base and becoming sericitic towards the top; Unit I - a basal sequence of regionally metamorphosed mafic volcanic rocks, interlayered with muscovite-quartz schist, massive and layered calc-silicates, recrystallised limestone lenses, and small serpentinite lenses. During mapping of RUBYVALE by the Geological Survey of Queensland (Grimes & others, 1980; Robertson, 1983), a less deformed sequence was recognised in the Fork Lagoons area, and defined as the Fork Lagoons beds (Anderson & Palmieri, 1977; Palmieri, 1978).The most recent regional mapping of the Anakie Metamorphics was to the north of the present study area in the Mount Coolon 1:250 000 Sheet area (Hutton & others, 1991). Because of the poor outcrop, no attempt was made to subdivide the unit, but the work did show that the rocks extend farther north and include much of the area previously assigned to the Ukalunda beds.|16-MAY-23
401|Anakie Metamorphic Group|Constituents|As a result of this survey, the Anakie Metamorphics in the Clermont-Emerald area have been subdivided into six major units which are herein named and given formation status. Therefore the Anakie Metamorphics are raised to group status and renamed the Anakie Metamorphic Group. The constituent units are: Wynyard Metamorphics, Monteagle Quartzite, Rolfe Creek Schist, Bathampton Metamorphics (including the Yan Can Greenstone Member and several unnamed informal subdivisions), Scurvy Creek Meta-arenite, Hurleys Metamorphics. The distribution of these units is illustrated in Figures 1 and 2. Because of the intense deformation, no definite younging sense can be demonstrated. However, the foliation and lithological layering dips westwards overall, so that there is an apparent sequence with Bathampton Metamorphics at the base passing upwards through Rolfe Creek Schist and Monteagle Quartzite to Wynyard Metamorphics. The relationships of the Scurvy Creek Meta-arenite and Hurleys Metamorphics to this sequence is uncertain, but on lithological grounds, it is possible that the Hurleys Metamorphics correlate with the Monteagle Quartzite and the Scurvy Creek Meta-arenite correlates with the Wynyard Metamorphics. The Monteagle Quartzite and Wynyard Metamorphics can be equated with Utah's Unit III. However, there is no evidence for any unconformity between the Monteagle Quartzite and the Rolfe Creek Schist. The Rolfe Creek Schist equates with part of Unit II. The Bathampton Metamorphics includes Unit I and probably part of Unit II.|16-MAY-23
401|Anakie Metamorphic Group|Relationships and boundaries|The Anakie Metamorphic Group is intruded and contact metamorphosed by the various Devonian plutons that form the Retreat Batholith. In the Rubyvale area to the south, numerous small plutons of variably foliated muscovite-biotite granite assigned to the Gem Park Granite also intrude the metamorphic rocks, possibly synchronously with the metamorphism and deformation. The contact between the Bathampton Metamorphics and the Fork Lagoons beds may be a thrust. The Anakie Metamorphic Group is overlain by a variety of younger rocks including: the Devonian Theresa Creek Volcanics and Silver Hills Volcanics; the Permian Back Creek Group, Blair Athol Coal Measures and Birimgan Formation; and Tertiary basalts and various other Cainozoic deposits.|16-MAY-23
401|Anakie Metamorphic Group|Age reasons|Age and evidence: Henderson (1980) suggested that the rocks may be Precambrian, but they have generally been regarded as early Palaeozoic (Murray & Kirkegaard, 1978; Day & others, 1983). This was based mainly on a recalculated K-Ar muscovite age of 466 Ma (Middle Ordovician) from mica schist collected west of Clermont (Webb & McDougall, 1968). In addition, syntectonic plutonic activity was suggested by Ordovician K-Ar ages ranging from 452 to 460 Ma (Webb, 1969) for granodiorite intruding schist in the core of the Telemon Anticline in the Drummond Basin, southwest of the Inlier. Another constraint was the difference in metamorphism and deformation between the Anakie Metamorphics and the Late Ordovician Fork Lagoons beds. This suggested a possible unconformity, consistent with the Middle Ordovician K-Ar age. K-Ar dating of the Anakie Metamorphic Group was carried out at the University of Queensland (Rees, 1992). A mica schist sample from a drillhole near the Peak Downs mine gave a K-Ar muscovite age of 510 Ma (Late Cambrian). A phyllite core sample from a Departmental drilling program in the Hurleys area gave a K-Ar whole-rock age of 554 Ma (Early Cambrian). Further work at the University of Queensland confirms the younger age (Withnall & others, in preparation). On the time-scale of Harland & others (1990), the dates correspond to the Late and Early Cambrian respectively. The 510 Ma age for the deformation in the Anakie Inlier corresponds with the Delamerian Orogeny that affected the Kanmantoo and Adelaide Fold Belts and the Willyama and Wonominta Blocks in the Late Cambrian to Early Ordovician (Jenkins & Sandiford, 1992). The original age of the Anakie Metamorphic Group is still uncertain, but is probably Early Cambrian or Neoproterozoic.|16-MAY-23
401|Anakie Metamorphic Group|References|ANDERSON, J.C. & PALMIERI, V., 1977: The Fork Lagoons Beds, an Ordovician unit of the Anakie Inlier, central Queensland. Queensland Government Mining Journal, 78, 260 263. **DAY, R.W., WHITAKER, W.G., MURRAY, C.G., WILSON, I.H. & GRIMES, K.G., 1983: Queensland Geology. A companion volume to the 1:2 500 000 scale geological map (1975). Geological Survey of Queensland, Publication 383. **GRIMES, K.G., ROBERTSON, A.D. & ANDERSON, J.C., 1980: Rubyvale 1:100 000 Geological Series, Sheet 8451, Preliminary edition. Geological Survey of Queensland. **HENDERSON, R.A., 1980: Structural outline and summary geological history for northeastern Australia. In Henderson, R.A. & Stephenson, P.J. (Editors): The Geology and Geophysics of Northeastern Australia. Geological Society of Australia, Queensland Division, Brisbane, 1 26. **HUTTON, L.J., GRIMES, K.G., LAW, S.R. & MCLENNAN, T.P.T., 1991: Geology of the Mount Coolon 1:250 000 Sheet area. Queensland Resource Industries Record, 1991/19. **JENSEN, H.I., 1921: The geology and mineral resources of the Carnarvon district. Queensland Government Mining Journal, 22, 401 407. **MALONE, E.J., CORBETT, D.P.W., & JENSEN, A.R., 1964: Geology of the Mount Coolon 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 64. **MURRAY, C.G. & KIRKEGAARD, A.G., 1978: The Thomson Orogen of the Tasman Orogenic Zone; In Scheibner, E. (Editor): The Phanerozoic structure of Australia and variations in tectonic style. Tectonophysics, 48, 229 325. **PALMIERI, V., 1978: Late Ordovician conodonts from the Fork Lagoons beds, Emerald area, central Queensland. Geological Survey of Queensland, Publication 369. **REES, I.D., 1992: Geology, petrogenesis and copper mineralisation of the Anakie Metamorphics, Rosevale area, Clermont, Central Queensland. B.Sc (Honours) Thesis, Department of Earth Sciences, University of Queensland (unpublished). **REID, J.H., 1936: Blair Athol coalfield. Queensland Government Mining Journal, 37, 401 407. **ROBERTSON, A.D., 1983: Notes on the geology of the central Queensland sapphire fields. Geological Survey of Queensland, Record 1983/51 (unpublished) **UTAH DEVELOPMENT COMPANY, 1971: Authority to Prospect 811M. Report on area relinquished, May 1st, 1971. Unpublished report held by the Queensland Department of Minerals and Energy as CR 3767. **VEEVERS, J.J., RANDAL, M.A., MOLLAN, R.G., & PATEN, R.J., 1964a: The geology of the Clermont 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report, 66. **VEEVERS, J.J., MOLLAN, R.G., OLGERS, F., & KIRKEGAARD, A.G., 1964b: The geology of the Emerald 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 68. **WEBB, A.W., 1969: Metallogenic epochs in eastern Queensland. Proceedings of the Australasian Institute of Mining and Metallurgy, 230, 27 39. **WEBB, A.W. & McDOUGALL, I., 1968: The geochronology of the igneous rocks of eastern Queensland. Journal of the Geological Society of Australia, 15, 313-346.|16-MAY-23
24162|Anning Granite|Name source|Anning Creek which joins the Gilbert River at GR 976 584 (Gilberton 1:100 000 Sheet area).|16-MAY-23
24162|Anning Granite|Unit history|Previously mapped as Dumbano Granite (White, 1962).|16-MAY-23
24162|Anning Granite|Type section locality|Anning Creek for about 1 km upstream from its junction with the Gilbert River. Pink medium grained equigranular biotite leucogranite crops out, locally containing small discontinuous veins and stringers of aplite and pegmatite.|16-MAY-23
24162|Anning Granite|Extent|Crops out in two main areas totaling about 150 km2 in the central eastern part of the Gilberton 1:100 000 Sheet area. The larger area occupies the western two-thirds and southern margin of the Glenmore Batholith extending from around Hanns Table Mountain south to the Anning Creek area and eastwards towards Wire Yard Mountain (GR 157 575). The smaller area occupies the eastern margin of the batholith extending south from about GR 105 755 in a belt  14 km long and 3 to 5 km long; the latter area is poorly exposed and apparently complex containing numerous large roof pendants of Einasleigh Metamorphics. Numerous small bodies of biotite leucogranite are present in the Einasleigh Metamorphics elsewhere in the southern half of the Gilberton 1:100 000 Sheet area; these are likely to be of several different ages and are presently unassigned, although some are possibly related to the Anning Granite.|16-MAY-23
24162|Anning Granite|Lithology|The larger area is predominantly cream to pink, medium grained, equigranular leucogranite containing sparse biotite, minor secondary muscovite and rare garnet; hornblende is a local constituent, particularly east of Hanns Table Mountain where the granite contains xenoliths of calc-silicate gneiss. Pegmatite and aplite veins are present but generally do not constitute a major proportion of the unit except near the contacts. The granite generally appears unfoliated, although a very weak foliation is present locally. The small eastern area consists predominantly of white biotite leucogranite; it is otherwise similar except that pegmatite and aplite are probably more abundant.|16-MAY-23
24162|Anning Granite|Relationships and boundaries|Intrudes the mid-Proterozoic Sawpit Granodiorite and intruded by Carboniferous (?) Culba Granodiorite and various rhyolite, dacite, andesite and micro-granite dykes which are mostly part of the Bagstowe Ring Dyke Complex. The Anning Granite is in contact with the Dumbano Granite but the relationship is not known because of poor outcrop; the shape of the regional contact as mapped suggests the Dumbano Granite may be younger but little reliance can be put on this as the boundary is difficult to locate; the two granites are possibly closely related in age.|16-MAY-23
24162|Anning Granite|Age reasons|Probably late Proterozoic or Devonian. Appears to post-date the second deformation in the area (1470 m.y. - Black et al., 1979); may have been intruded syntectonically with the third deformation (970 m.y.) accounting for the weak foliation. A Devonian age, however, is also possible. At present the only isotopic ages available on the Dumbano Granite, to which the Anning Granite may be related, are Silurian to Devonian (417 to 370 m.y; Black, 1973).|16-MAY-23
24162|Anning Granite|References|73/050; 80/20677; ?01/31336|16-MAY-23
24162|Anning Granite|Proposer|Withnall I.W, Bain J.H.C.|16-MAY-23
471|Annmore Quartz Monzodiorite|Name source|Annmore homestead at 8451-685424.  The grid reference is based on the AGD66 datum.|16-MAY-23
471|Annmore Quartz Monzodiorite|Geomorphic expression|The topography is primarily subdued with little variation in relief. Boulder-sized outcrop is abundant in the northeast and southwest.   On the Landsat 5 TM (1-4-7 BGR) image the Annmore Quartz Monzodiorite is well defined with an orange hue and sharp boundaries. The magnetic response is moderate to strong. Variable radiometric responses are associated with the unit. The K response is moderate to high with the latter along the southeast margin and in the northwest. Th and U are generally low with local highs along the southeast margin and in the northwest.|16-MAY-23
471|Annmore Quartz Monzodiorite|Type section locality|At 8451-624371, about 1 km southeast of Llandillo pinnacle.  The grid reference is based on the AGD66 datum.|16-MAY-23
471|Annmore Quartz Monzodiorite|Description at type locality|Grey, fine to coarse-grained, porphyritic quartz monzodiorite is exposed.|16-MAY-23
471|Annmore Quartz Monzodiorite|Extent|An equant body, 120 km2 in area, from Theresa Creek in the north to Cattle Creek in the south.|16-MAY-23
471|Annmore Quartz Monzodiorite|Lithology|The Annmore Quartz Monzodiorite is compositionally variable, ranging from granodiorite to gabbro; the rocks are generally grey to light grey, fine to coarse-grained, equigranular to porphyritic. The pluton shows a gradual increase in mafic character from east to west, but no distinct boundaries can be mapped between rock-types.|16-MAY-23
471|Annmore Quartz Monzodiorite|Relationships and boundaries|The relationship with the Kilmarnock Granodiorite is unknown. Numerous small basalt plugs of the Hoy Basalt intrude along the boundary between the units. To the north and east, Permian sedimentary rocks and Cainozoic deposits unconformably overlie the pluton.|16-MAY-23
471|Annmore Quartz Monzodiorite|Age reasons|Webb & others (1963) obtained two K-Ar biotite ages corrected to 359 Ma and 362 Ma (Late Devonian). These are probably minimum ages.|16-MAY-23
471|Annmore Quartz Monzodiorite|References|WEBB, A.W., COOPER, J.A. & RICHARDS, J.R., 1963: K-Ar ages on some Central Queensland granites. Journal of the Geological Society of Australia, 10, 317-324.|16-MAY-23
28185|Answer Slate|Name source|Named after the Answer copper mine, GR 340035, Mount Merlin 1:100 000 sheet area, Duchess 1:250 000 sheet area.|16-MAY-23
28185|Answer Slate|Type section locality|South of Limestone Creek, Mount Merlin 1:100 000 sheet area. According to Carter (1959) and Carter & others (1961), it extends for 5.6 km west from latitude 21o23'S, longitude 140o22'E, but the latitute as given is in the Malbon 1:100 000 sheet area, well to the north of Limestone Creek. The proposed revised type section is just south of Limestone Creek, 13 km north of the Answer mine, extending west from GR 339182 (about latitude 23o33'20"S, longitude 140o21'53" ) for 5.3 km. It traverses gently undulating terrain developed on interbedded slate and siltstone, some banded quartz-hematite and cherty rocks, and intrusive metadolerite. It extends from a poorly exposed concordant contact with Staveley Formation in the east to a gradational contact, partly obscured by metadolerite, with Mitakoodi Quartzite to the west.|16-MAY-23
28185|Answer Slate|Extent|Crops out in a belt up to 6 km wide extending from 13 km NNW of Kuridala southwards for 72 km to 18 km SSE of the Answer mine, Malbon and Mount Merlin 1:100 000 sheet areas, Duchess 1:250 000 Sheet area.|16-MAY-23
28185|Answer Slate|Thickness range|Uncertain because of tight foldings, but maximum maybe more than 1000 m.|16-MAY-23
28185|Answer Slate|Lithology|Main rock types are interbedded pale to dark grey (graphitic) or iron-stained slate, siltstone, and phyllite; also present are fine mica schist, thin beds of fine quartzite and feldspathic quartzite, chert, dolomitic and calcareous siltstone, schistose metagreywacke, and ridge-forming quartz-hematite bands. Quartz veins are common throughout.|16-MAY-23
28185|Answer Slate|Relationships and boundaries|The formation conformably overlies Mitakoodi Quartzite and Overhang Jaspilite, and may be overlain by Staveley Formation either conformably or unconformably. It is faulted against Agate Downs Siltstone and probably also against Double Crossing Metamorphics (new name), intruded by metadolerite, Gin Creek Granite, and Wimberu Granite, and overlain unconformably by flat-lying Cambrian Mount Birnie Beds and Mesozoic sediments.|16-MAY-23
28185|Answer Slate|Identifying features|Formation originally defined by Carter (1959).|16-MAY-23
28185|Answer Slate|Age reasons|Proterozoic.|16-MAY-23
28185|Answer Slate|Comments|The Answer Slate may be a correlative of the Marimo Slate to the north (Carter et al., 1961- B051). However, Blake et al. and Donchak et al. consider it likely that the formation is overlain unconformably by the Staveley Formation, a probable lateral equivalent of the Marino Slate, and hence regard the Answer Slate as an older unit.|16-MAY-23
28185|Answer Slate|Defn Reference|Donchak, Bultitude, Blake 1981. BMR Report 233.|16-MAY-23
526|Aramac Coal Measures|Name source|From QDM Aramac 1 well; latitude 22o56'56"S; longitude 145o17'03"E.|16-MAY-23
526|Aramac Coal Measures|Type section locality|In QDM Aramac 1 from 1018 m (3340 ft) to 1106 m (3628 ft) K.B.  Cuttings of this interval are available at the Core Library, Redbank.|16-MAY-23
526|Aramac Coal Measures|Extent|Present in wells westward from QDM Aramac 1 towards the Maneroo Platform and Beryl Ridge, and southward to approximately Latitude 23o30'S. Absent in LOL Hulton 1 well.|16-MAY-23
526|Aramac Coal Measures|Thickness range|88 m in the type section. Ranges from 28 m in LOL Saltern Creek 1 to a maximum of 100 m in LOL Marchmont 1.|16-MAY-23
526|Aramac Coal Measures|Lithology|Sandstone is typically light grey, very fine to medium, moderately and well sorted, quartzose to labile. It consists essentially of subangular to subround quartz grains in a white, argillaceous matrix. Siltstone is typically medium to dark grey, carbonaceous, and very finely micaceous. Mudstone is grey and dark grey-brown, moderately hard, fissile, carbonaceous, and very finely micaceous. Coal is grey to black, brittle and predominately dull. On wireline logs, the Aramac Coal Measures are not a distinctive unit. The base is taken arbitrarily at the bottom of the lowest significant coal seam. The top is evidenced in the gamma-ray logs of many wells by a marked decrease in radioactivity upward.|16-MAY-23
526|Aramac Coal Measures|Depositional environment|Deltaic, paludal (marshy).|16-MAY-23
526|Aramac Coal Measures|Relationships and boundaries|The Aramac Coal Measures conformably overlie the Jochmus Formation in the Aramac area and generally westward towards the Maneroo Platform and Beryl Ridge. They are unconformably overlain by correlatives of the Late Permian Colinlea Sandstone. The Aramac Coal Measures are probably a facies variant of the upper part of the Jochmus Formation in the Koburra Trough. Palynology indicates that the Aramac Coal Measures are the age correlative of the Reids Dome Beds, the Cattle Creek Formation and the Aldebaran Sandstone of the western Bowen Basin.|16-MAY-23
526|Aramac Coal Measures|Age reasons|Early Permian. Spore assemblages obtained have been assigned to Stage 3 of Evans (1969).|16-MAY-23
23340|Arch Creek Limestone Member|Name source|Arch Creek, a tributary of Jessey Creek which it joins at 7859 707512.  The grid reference is based on the AGD66 datum.|16-MAY-23
23340|Arch Creek Limestone Member|Unit history|The name was published by Withnall & others (1988), but only briefly described.|16-MAY-23
23340|Arch Creek Limestone Member|Type section locality|At 7859 716537 along Arch Creek.  The grid reference is based on the AGD66 datum.|16-MAY-23
23340|Arch Creek Limestone Member|Description at type locality|About 40 m of fossiliferous limestone.|16-MAY-23
23340|Arch Creek Limestone Member|Extent|A small lens several hundred metres long, about 2.5 km east of Jessey Springs hut.   Topography and airphoto expression.  Low outcrops, not discernible on airphotos.|16-MAY-23
23340|Arch Creek Limestone Member|Thickness range|40 m.|16-MAY-23
23340|Arch Creek Limestone Member|Lithology|Bioclastic calcarenite.|16-MAY-23
23340|Arch Creek Limestone Member|Fossils|A fauna of corals and conodonts similar to that in the Martins Well Limestone Member is present.|16-MAY-23
23340|Arch Creek Limestone Member|Relationships and boundaries|A member of the Shield Creek Formation.|16-MAY-23
23340|Arch Creek Limestone Member|Age reasons|The corals and conodonts indicates a Lochkovian to Pragian age (R. Mawson & J. Talent, unpublished data).|16-MAY-23
23340|Arch Creek Limestone Member|References|WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
585|Argylla Formation|Name source|Argylla Creek (see Carter et al., 1961).|16-MAY-23
585|Argylla Formation|Type section locality|As nominated by Carter et al., 1961, along the old Mount Isa/Cloncurry road for about 3.5 km west of latitude 20o43'30"S, longitude 139o50'20"E. The revision is necessary because the type section includes Ballara Quartzite which has been shown (Derrick et al., 1974) to unconformably overlie pink porphyritic acid volcanics that typify the Argylla Formation and because the lower boundary of the Argylla Formation is in contact with a new formation, the Magna Lynn Metabasalt.|16-MAY-23
585|Argylla Formation|Extent|See Carter et al., 1961; this revision refers only to the belt of Argylla Formation which flanks the eastern edge of the basement succession and extends from Duchess in the south for 150 km north to near Kajabbi.|16-MAY-23
585|Argylla Formation|Thickness range|From 600 to 3000 m thick.|16-MAY-23
585|Argylla Formation|Lithology|The oldest rocks in the revised type section are probably a sequence of tuff, amygdaloidal andesite and intrusive porphyry; these are overlain further east by pink, poorly foliated porphyritic acid volcanics with some possibly tuffaceous bands containing elongate, dark grey inclusions. North of the type section, in the Prospector Sheet area, thin, poorly exposed siltstone and labile fine-grained sandstone are present (Wilson et al., in prep.) intercalated with acid volcanic rocks.|16-MAY-23
585|Argylla Formation|Relationships and boundaries|Carter et al., (1961) described the Argylla Formation as overlying Leichhardt Metamorphics, generally conformably. It is now apparent that the Argylla Formation overlies the Magna Lynn Metabasalt, a new formation which was formerly part of the Leichhardt Metamorphics. The relationship appears to be conformable. The upper boundary in the type section has also been revised. Recent mapping has revealed an unconformity with slight angularity between the Argylla Formation and the Ballara Quartzite; the latter was formerly included in the Argylla Formation in the type section. It is proposed, therefore, to restrict the Argylla Formation to the predominantly acid volcanic sequence between the Magna Lynn Metabasalt and the Ballara Quartzite. To the east the Argylla Formation is conformably overlain by the Marraba Volcanics (Carter et al., 1961).|16-MAY-23
585|Argylla Formation|Identifying features|For original definition, see Carter et al., (1961)|16-MAY-23
585|Argylla Formation|Proposed publication|Queensland Government Mining Journal - 79/03449?|16-MAY-23
585|Argylla Formation|References|77/004|16-MAY-23
24167|B Creek Rhyolite|Name source|The name is derived from B Creek, which joins the Langdon River at GR 7461-081549,|16-MAY-23
24167|B Creek Rhyolite|Unit history|Branch (1966) did not formally subdivide the 'Croydon Volcanics', although he did recognise a discontinuous basal volcanic 'sheet' of grey, rhyolitic and rhyodacitic rocks probably equivalent to the B Creek Rhyolite, Wonnemarra Rhyolite, and Carron Rhyolite. Mackenzie (1983), informally named and described 'Goat Creek andesite'.|16-MAY-23
24167|B Creek Rhyolite|Geomorphic expression|Like the Carron Rhyolite, the B Creek Rhyolite is characterised by gentle to moderate relief, mostly smoothly rounded hills, and sparse vegetation cover. The soil colour is slightly darker than on the Wonnemarra, Carron, or Parrot Camp Rhyolites.|16-MAY-23
24167|B Creek Rhyolite|Type section locality|The type section of the unit is 2 km north of the junction of B Creek and Fish Hole Cree; it extends from 7460-068512 (base) to 059506 (top). The section consists of very dark grey to almost black, slightly altered and intensely recrystallised (hornfelsed?) rhyodacitic ignimbrite which grades upwards from generally coarser-grained, moderately crystal-rich, more mafic rocks with scarce, small clasts of basalt or andesite near the base to generally finer-grained, crystal poor, and more felsic rocks at the top. Also near the base are lenses of conglomerate, a few tens of centimetres thick, containing well-rounded cobbles derived from the Langlovale Group (Withnall & Mackenzie, 1983). The section is about 450 m thick, assuming a general dip of 30o, but dip is difficult to estimate because of scarcity and inconsistency of indicators. The unit is underlain here, probably unconformably, by folded, sandy to silty sediments of the Langlovale Group, and overlain by paler-grey, finer-grained, and more crystal-poor rhyolitic ignimbrite and lava of the Carron Rhyolite. A reference section containing some more mafic rocks extends from -079452 (base) to -071452, 3 km northwest of Blackfellow yards.|16-MAY-23
24167|B Creek Rhyolite|Extent|In the north of the Croydon region, the B Creek Rhyolite crops out in several separate areas near the Carron River, between Tabletop Creek (7362-362105) in the west and 7462-605155 in the east. Two small exposures are located 5 km northwest of Croydon, near 'Belmore' homestead, and 10 km north-northwest of Croydon (7361-263946); a very small exposure is located near the Gilbert River at 7462-725095. In the east, the unit crops out in two main areas. One is east of Langlo Lake, extending  from 7461-060730 in a 1 km-wide, extensively faulted belt southward to -070622; an outlier about 1.0 by 0.5 km crops out about 1 km southwest of Blackfellow yards, about -087420. Three small exposures are located further south, one near Dingo Creek (7460-057325; about 1.2 by 0.2 km), another, about 3 km long and 250-300 m wide, crossing Snake Creek at -50267, and the third, about 350 m by 200 m, near Sandy Creek at -89124.|16-MAY-23
24167|B Creek Rhyolite|Thickness range|In the eastern part of the Croydon region, the B Creek Rhyolite is up to 750-800 m thick, decreasing to about 100-200 m in the southeast. Thickness in the north is difficult to estimate, but is at least 70 m and may be up to 250 or 300 m.|16-MAY-23
24167|B Creek Rhyolite|Lithology|The B Creek Rhyolite is made up predominantly of very dark grey, altered and intensely recrystallised, crystal-poor rhyodacitic ignimbrite. Dacitic but otherwise similar ignimbrite is present in lesser amounts, mostly as lenses up to several kilometres long and up to 50 m thick, and in places associated with thinner, less extensive lenses of highly altered andesite. In the north (Carron River area), dacitic rocks are more common, and some are conspicuously 'porphyritic', with feldspar and rounded quartz crystals up to 6 mm. These rocks appear to be slightly different, at least texturally, to those in the east, and further work might result in their being separated as a distinct unit. In the southeast, near Blackfellow yards, the unit contains lenses up to 50 m thick of altered andesite similar to the Goat Creek Andesite.|16-MAY-23
24167|B Creek Rhyolite|Relationships and boundaries|The B Creek Rhyolite is partly unconformable on, and partly faulted against Middle Proterozoic Langlovale Group (Withnall & Mackenzie, 1983) and Etheridge Group (Withnall & Mackenzie, 1980) in the east of the region, where it also overlies, conformably or paraconformably, the Wonnemarra Rhyolite. In the north it overlies, with apparent conformity, Goat Creek Andesite, or  Wallabadah Siltstone, or both. It is overlain, apparently conformably, by Carron Rhyolite in the east and north, and by Parrot Camp Rhyolite in the northwest. Permian Bullseye Rhyolite (Mackenzie, 1983) unconformably overlies the unit in the east, near Langlo Lake, and it is also overlain unconformably by Mesozoic and Tertiary to Quaternary sediments. It is intruded by Esmeralda Granite, Chadshunt Granite, Macartneys Granite, Olsens Granite, and Dregger Granite. B Creek Rhyolite is distinguished from underlying and overlying volcanic rocks by its very dark colour, combined with obvious felsic (to intermediate) composition, sparse crystals, notably quartz (commonly rounded), and, commonly, apparent coarse grainsize due to recrystallisation. It is slightly more mafic than the Wonnemarra, Carron, and Parrot Camp Rhyolites.|16-MAY-23
24167|B Creek Rhyolite|Age reasons|The B Creek Rhyolite is Middle Proterozoic, as established for the Croydon Volcanic Group as a whole.|16-MAY-23
24167|B Creek Rhyolite|References|B076;  83/23589|16-MAY-23
24167|B Creek Rhyolite|Proposer|Mackenzie D.E., Warnick J.V., Henderson G.A.M.|16-MAY-23
34128|Ballabay Complex|Name source|Ballabay homestead, on the Cape River at GR 3212 77402 in the Lolworth 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
34128|Ballabay Complex|Unit history|The Ballabay Complex was not recognised on the first edition Hughenden 1:250 000 geological map (Vine & Paine, 1974; Paine & others, 1971).|16-MAY-23
34128|Ballabay Complex|Type section locality|At a crossing of a tributary of the Cape River 3km east-southeast of Bullock Paddock Bore at GR 3139 77388 in the Lolworth 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
34128|Ballabay Complex|Description at type locality|A medium grained biotite-hornblende tonalite is interlayered with dark grey to grey hornblende, plagioclase diorite to gabbro. Xenoliths of gneiss occur in the tonalite.|16-MAY-23
34128|Ballabay Complex|Extent|The Ballabay Complex crops out over 7km2 south of Oak Vale homestead (Figure 2). A further 14km2 mapped as Tertiary to Quaternary alluvium contains isolated outcrops of gabbro and deeply weathered biotite granite which are probably part of the complex.|16-MAY-23
34128|Ballabay Complex|Lithology|Rocks in the complex range from deeply weathered biotite granite, through biotite-hornblende granodiorite, biotite-hornblende tonalite to hornblende gabbro. Outcrop in the Ballabay Complex is poor so that relationships between the different rocks are not known. Fine and medium to coarse grained hornblende gabbro appears to be the dominant rock type in outcrop, forming small mounds in the alluvial plain which covers most of the area of the unit. However, deeply weathered biotite granite and biotite-hornblende granodiorite that also crop out within the area of the alluvial plain, may be the dominant rock types in the complex.|16-MAY-23
34128|Ballabay Complex|Relationships and boundaries|The Ballabay Complex appears to intrude the Cape River Metamorphics. The unit weathers recessively being covered by Tertiary to Quaternary alluvium for most of its area. The relationships of the various phases in the complex are not known.|16-MAY-23
34128|Ballabay Complex|Age reasons|The age of the Ballabay Complex is not known. A lithologically similar complex, the Larry Creek Complex (this report) occurs south of Pentland and is possibly Late Palaeozoic.|16-MAY-23
34128|Ballabay Complex|Comments|GENERAL REMARKS::  The Ballabay Complex is one of several gabbro/diorite/granite complexes in the Pentland area. Although only two are defined here, smaller bodies are mapped and may be more common than previously recognised. The age of the complexes is not known. They could be related to Permian gabbro to granite complexes that occur in the Charters Towers area (eg. the Tuckers Igneous Complex), although older gabbros and diorites are also mapped within the Ravenswood Batholith.MAGNETIC SUCEPTIBILITY::  Magnetic susceptibilities at the type locality are 17-770 x 10[supercript]-5 SI units for the gabbro/diorite to non-magnetic for the tonalite. No other magnetic susceptibilities were measured in the unit.|16-MAY-23
34128|Ballabay Complex|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
27702|Ballara Quartzite|Unit history|Revision: A new type section of the Ballara Quartzite is proposed, because the old type section described by Carter, Brooks & Walker (1961) is largely composed of sandstone and conglomerate intercalations in the acid volcanic Argylla Formation.|16-MAY-23
27702|Ballara Quartzite|Constituents|Two units are recognised in the Ballara Quartzite: a lenticular basal unit up to 700 m thick of grit, conglomerate, tuff, arkose, sericitic quartzite and minor basalt, and an upper unit from 1250 to 20 m thick of coarse to medium white to grey quartzite. Neither unit is formally defined.|16-MAY-23
27702|Ballara Quartzite|Type section locality|The proposed new type section extends from 0.7 km north of Wee McGregor mine, for 1.1 km to the north-northeast (6856 900877 to 6856 905887), 16 km south of Mary Kathleen. ( Mary Kathleen 1:100 000 Sheet area).|16-MAY-23
27702|Ballara Quartzite|Relationships and boundaries|The Ballara Quartzite overlies the Argylla Formation unconformably and is overlain conformably by the Corella Formation. In places the Ballara Quartzite is overlain unconformably by the Deighton Quartzite.|16-MAY-23
27702|Ballara Quartzite|References|Further details are contained in Derrick, Wilson, Hill, Glikson & Mitchell (1977). Geology of the Mary Kathleen 1:100 000 Sheet area, northwest Queensland. BMR Bulletin 193  **Carter, Brooks & Walker (1961)The Precambrian mineral belt of north-western Queensland. BMR Bulletin 51|16-MAY-23
23365|Bathampton Metamorphics|Name source|Parish of Bathampton (Clermont 1:100 000 Cadastral Series map). Also the name of a former settlement and State school, about 8 km northwest of Clermont.|16-MAY-23
23365|Bathampton Metamorphics|Unit history|Previously mapped as Anakie Metamorphics (Malone & others, 1964; Veevers & others, 1964a, b) and now part of the Anakie Metamorphic Group.|16-MAY-23
23365|Bathampton Metamorphics|Geomorphic expression|On Landsat 5 TM bands 1-4-7 (BGR) images, areas of Bathampton Metamorphics are generally bluish green. Some of the quartzite-rich belts have pale, cream tones, whereas others are dark green, due to thick Acacia scrub. Areas of greenstones can be identified on aerial photographs and the Landsat 5 TM images by their red or orange colours. On the radiometric geophysical images, they can be recognised by their low response in all three (K, Th and U) channels. They are also very slightly more magnetic than the metasedimentary rocks.|16-MAY-23
23365|Bathampton Metamorphics|Type section locality|The track north from the yards at 8352-477664 near Hillview homestead to the Clermont-Alpha road at 462724.  The grid references are based on the AGD66 datum.|16-MAY-23
23365|Bathampton Metamorphics|Description at type locality|Exposures are dominantly pelitic (fine-grained, grey chlorite-sericite schist), but also include white quartzite and green, fine-grained, laminated greenstone.|16-MAY-23
23365|Bathampton Metamorphics|Extent|The largest outcrop area is in CLERMONT and MONTEAGLE (Figure 1), where it forms a southeast-trending belt of greenschist facies rocks about 50 km long and up to 8 km wide from Western Creek to the Macdonalds Flat area, south of Clermont. From there it extends about 35 km west in a 10 km-wide zone, which occupies the core of a post-F2 domal structure.   The other main area is in the southern part of RUBYVALE extending into ANAKIE (Figure 2), where a belt of upper greenschist to amphibolite facies rocks, 5 to 10 km wide, extends for about 30 km southeast from near Poinsetta homestead to just north of the Capricorn Highway.  Smaller outliers tentatively assigned to the Bathampton Metamorphics occur at Mount Prairie and Mount Misery (west of Capella), along Apsley Creek, and north of Retro. The rocks in most of these areas are poorly exposed and have not been examined in detail.|16-MAY-23
23365|Bathampton Metamorphics|Lithology|In the Clermont area, the Bathampton Metamorphics are in the greenschist facies and are subdivided informally into the following lithofacies:	(a) a pelitic lithofacies consisting dominantly of fine-grained mica schist (grading to phyllite) and subordinate quartzite; (b) a more psammitic lithofacies consisting of abundant to dominant white, strongly foliated quartzite, interlayered with mica schist and phyllite; (c) commonly laminated greenstone and interbedded mica schist; (d) one formal member, the Yan Can Greenstone Member, described separately; and  (e) minor serpentinite bodies. In the Rubyvale area, the metamorphic grade is in the amphibolite facies and two lithofacies have been mapped: (a) mica schist and quartzite, neither of which are particularly dominant; and (b) massive to foliated metagabbro, laminated amphibolite and calc-silicate rocks.|16-MAY-23
23365|Bathampton Metamorphics|Relationships and boundaries|West of Clermont, the Bathampton Metamorphics occupy the core of the antiformal dome centred on Oaky Creek, and assuming the structure is not downward-facing, the unit may be the lowermost part of the Anakie Metamorphic Group in this area. It contains the Yan Can Greenstone Member and is structurally overlain by the Rolfe Creek Schist, which is distinguished by its lack of quartzite and greenstone. Northwest of Clermont, the Scurvy Creek Meta-arenite structurally underlies the Bathampton Metamorphics. However, the Scurvy Creek Meta-arenite is structurally underlain by the Hurleys Metamorphics, which in the Apsley State Forest southeast of Blair Athol, are in turn structurally underlain by rocks containing greenstone and probably equivalent to the Bathampton Metamorphics. Therefore, it is probable that either at least some of the boundaries are not stratigraphic or that unrecognised, tight, recumbent folds are present.    In the Clermont area, the Bathampton Metamorphics are intruded by small gabbro to quartz diorite plutons and micromonzonite and microgranite dykes, probably of Devonian age and related to the Retreat Batholith. In the Rubyvale area to the south, the unit is intruded and contact metamorphosed by the Devonian Kilmarnock and Mount Newsome Granodiorites and several smaller unnamed plutons that form part of the Retreat Batholith. Numerous small plutons of variably foliated muscovite-biotite granites assigned to the Gem Park Granite also intruded the metamorphic rocks, possibly synchronously with the metamorphism and deformation.    The contact between the Bathampton Metamorphics and the Fork Lagoons beds is a zone of intensely foliated, fine-grained phyllitic rocks interpreted to be phyllonite derived from mylonitisation of either the mica schists of the Bathampton Metamorphics or the arenites and cleaved mudstones of the Fork Lagoons beds. The zone is up to 1 km wide, and may represent a thrust.   The Bathampton Metamorphics are overlain by a variety of younger rocks, including the Devonian Theresa Creek Volcanics, the Permian Back Creek Group, Blair Athol Coal Measures and Birimgan Formation, Tertiary basalts and various other Cainozoic deposits.|16-MAY-23
23365|Bathampton Metamorphics|Age reasons|The original age is still uncertain, but is probably Early Cambrian or Neoproterozoic|16-MAY-23
23365|Bathampton Metamorphics|References|MALONE, E.J., CORBETT, D.P.W., & JENSEN, A.R., 1964: Geology of the Mount Coolon 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 64. **VEEVERS, J.J., RANDAL, M.A., MOLLAN, R.G., & PATEN, R.J., 1964a: The geology of the Clermont 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report, 66. **VEEVERS, J.J., MOLLAN, R.G., OLGERS, F., & KIRKEGAARD, A.G., 1964b: The geology of the Emerald 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 68.|16-MAY-23
1273|Baumans Camp Granite|Name source|The name is derived from the Baumans Camp tin-tungsten mines at 8059-683572 (misspelt as Bowmans Camp on the EWAN topographic map).|16-MAY-23
1273|Baumans Camp Granite|Geomorphic expression|The granite in both areas is generally poorly exposed and strongly weathered; locally it is lateritised.|16-MAY-23
1273|Baumans Camp Granite|Type section locality|The type area is along the track from the Ewan Racecourse to Baumans camp between 8059 649533 and 675564.  The grid reference is based on the AGD66 datum.|16-MAY-23
1273|Baumans Camp Granite|Description at type locality|The granite is mostly weathered, but fresh boulders of pale grey, moderately porphyritic, medium to coarse-grained biotite granite occur in some gullies.|16-MAY-23
1273|Baumans Camp Granite|Extent|The Baumans Camp Granite crops out as a narrow strip up to 2km wide and 11km long trending northeast from Stockyard Creek near the Ewan Racecourse|16-MAY-23
1273|Baumans Camp Granite|Lithology|The Baumans Camp Granite is generally grey, cream or pink, medium to coarse-grained, seriate to porphyritic biotite granite. The granite south of Stockyard Creek is generally similar to that described above, but finer-grained phases are also present. The Baumans Camp Granite is extensively altered in places, particularly around the Baumans Camp tin-tungsten mining area where quartz-sericite alteration zones or greisens are abundant. The alteration is commonly associated with vuggy quartz veins up to several centimetres wide. Some veins also contain tourmaline and fluorite.|16-MAY-23
1273|Baumans Camp Granite|Relationships and boundaries|The Baumans Camp Granite intrudes Argentine Metamorphics and unnamed Late Devonian or Carboniferous sandstone. It is in contact with the Malmesbury Microgranite. In a gully at 8059-603530, the Malmesbury Microgranite is finer grained and apparently chilled against the contact with the Baumans Camp Granite, suggesting that the Malmesbury Microgranite is younger. The relationship to the unassigned microgranite (map symbol Cgy) is uncertain. However, this microgranite is much more fractionated than the Baumans Camp Granite and is possibly younger. It is more likely to be the source of the fluids which caused the alteration and tin-tungsten mineralisation than the Baumans Camp Granite which is one of the least fractionated granites in the region, based on its geochemistry.  The grid reference is based on the AGD66 datum.|16-MAY-23
1273|Baumans Camp Granite|Comments|The name has also been tentatively applied to granite cropping out for at least 10km to the southwest of Stockyard Creek into HILLGROVE, but this granite may be a separate unit because it has a different expression on composite K/Th/U images processed from the AGSO airborne radiometric data. Northeast of Stockyard Creek, the granite is represented by a pink colour. The granite to the southwest is white on the images suggesting that it is more fractionated and has greater abundances of U and Th relative to the granite to the northeast.|16-MAY-23
21218|Belgravia Granodiorite|Name source|The pluton is named after Belgravia Creek, a tributary of Redcap Creek which cuts the eastern part of the pluton.|16-MAY-23
21218|Belgravia Granodiorite|Unit history|The unit was previously mapped as Almaden Granite (Best, 1962;  de Keyser & Wolff, 1964;  de Keyser & Lucas, 1968).|16-MAY-23
21218|Belgravia Granodiorite|Geomorphic expression|Over much of the area, particularly around the northern and eastern margins the granitic rocks crop out mainly as scattered large rounded boulders and pavements in low undulating country.  The western and central parts of the pluton form boulder-strewn hilly country characterised in a few places by accumulations of numerous large, black, alga-covered boulders.  These latter areas are characterised by very dark tones on aerial photographs; elsewhere the unit shows medium tones.|16-MAY-23
21218|Belgravia Granodiorite|Type section locality|The designated type area is ~400 m west of Redcap Creek, around GR 2244 81120.  The grid reference is based on the AGD66 datum.|16-MAY-23
21218|Belgravia Granodiorite|Description at type locality|The granodiorite is relatively well exposed in this area and forms boulder-strewn hills.|16-MAY-23
21218|Belgravia Granodiorite|Extent|The pluton forms a roughly circular stock with an area of 6 km2 in northeastern MUNGANA.|16-MAY-23
21218|Belgravia Granodiorite|General description|STRUCTURE AND METAMORPHISM::  The Belgravia Granodiorite is essentially massive and unmetamorphosed.  Siliciclastic sediments of the Chillagoe and Hodgkinson Formations adjacent to the contact do not appear extensively hornfelsed.  In contrast, limestones of the Chillagoe Formation exposed on southern and southwestern margins of the pluton have been extensively recrystallised to white, medium to coarse-grained marble, with lenses of magnetite-rich (now extensively oxidised) and tilleyite-bearing skarn locally developed adjacent to the contact.  The calcareous matrix in the polymictic conglomerate exposed at GR 2233 81110 has been converted to a calc-silicate granofels containing abundant quartz, plagioclase and epidote. The grid references are based on the AGD66 datum.MINERALISATION::  No mineral deposits are known to occur within the granodiorite.  There are several shallow workings in a lens of malachite-bearing magnetite-hematite-rich skarn exposed adjacent to the Belgravia Granodiorite at GR 2227 81120.  In the Redcap area calcareous units in the Chillagoe Formation have been extensively metasomatised and converted to ore-bearing skarns adjacent to the granodiorite.  The Redcap lode was the largest;  it more or less follows the Redcap Fault and includes the Redcap, Queenslander and Morrison mines as well as several smaller workings.  Both lead and copper ores were mined.  The zone of ferruginous-siliceous breccia which extends along the Redcap Fault is the surface expression of sulphide-bearing vein skarns, which probably formed at lower temperatures and later than the tilleyite-bearing magmatic skarn exposed in Redcap Creek to the north-northwest (Paved, 1972, 1981).|16-MAY-23
21218|Belgravia Granodiorite|Lithology|The Belgravia Granodiorite is typically a grey, medium-grained, porphyritic, biotite-hornblende granodiorite containing plagioclase phenocrysts up to 1 cm long and smaller quartz phenocrysts.  Rounded mafic enclaves up to 15 cm in diameter are common.  Numerous mafic 'inclusions', some up to 30 m long, are present in the granodiorite along its southern margin, adjacent to the tilleyite-bearing magmatic skarn exposed in Redcap Creek.  The irregular, crenulate shapes and, in particular, the abundant net veining of the mafic 'inclusions' by granodiorite, suggests that they formed by the mixing of granodioritic magma with more mafic magma (see Blake & others, 1965).  The mafic magma is represented by a small dyke swarm (of gabbro and diorite?) poorly exposed nearby.  Similar net-veined complexes have been found elsewhere in the Chillagoe region.The granodiorite consists of plagioclase, quartz, K-feldspar, hornblende, biotite, and accessory minerals (mainly opaque oxides, apatite, and zircon).  The mafic 'inclusions' and dykes consist mainly of the same minerals, but are finer grained, have a higher colour index and contain little or no quartz or K-feldspar.  Augite is present in some specimens and hornblende is generally much more abundant than biotite.Minor aplite and aplitic microgranite, as dykes and pods too small to be delineated on the map, have also been included in the formation.|16-MAY-23
21218|Belgravia Granodiorite|Relationships and boundaries|The granodiorite intrudes the Chillagoe and Hodgkinson Formations and the Redcap Dacite (volcanics).  It also truncates the Redcap and Walsh Faults and post-dates several other unnamed faults in the Redcap area.  It is cut by numerous dykes and small pods of aplite and aplitic microgranite.Age:  The granodiorite is most probably Late Carboniferous.  It has not been isotopically dated, but 24 samples from 10 plutons in the northern Tate Batholith have yielded Rb/Sr biotite ages ranging between 301 Ma and 302 Ma (Richards, 1981).|16-MAY-23
21218|Belgravia Granodiorite|Age reasons|The granodiorite is most probably Late Carboniferous.  It has not been isotopically dated, but 24 samples from 10 plutons in the northern Tate Batholith have yielded Rb/Sr biotite ages ranging between 301 Ma and 302 Ma (Richards, 1981).|16-MAY-23
21218|Belgravia Granodiorite|Comments|The Belgravia Granodiorite forms part of the northern Tate Batholith of Richards (1981).|16-MAY-23
21218|Belgravia Granodiorite|References|*BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.    *DE KEYSER, F., & LUCAS, K.G., 1968:  Geology of the Hodgkinson and Laura Basins, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 84.    *DE KEYSER, F., & WOLFF, K.W., 1964:  The geology and mineral resources of the Chillagoe area.  Bureau of Mineral Resources, Australia, Bulletin 70.    *RICHARDS, D.N.G., 1981:  Granitoids of the northern Tate batholith, Chillagoe, north Queensland.  Ph.D. Thesis, James Cook University of North Queensland, Townsville (unpublished).|16-MAY-23
24177|Bellenden Ker Granite|Name source|Bellenden Ker Range, located between the Mulgrave and Russell Rivers (Bartle Frere 1:100 000 sheet area).|16-MAY-23
24177|Bellenden Ker Granite|Unit history|The Bellenden Ker Granite was originally included in the Mareeba Granite (Jensen, 1923) by de Keyser (1964). Richards (1977) described the foliated, coarse-grained granite along the eastern flanks of the Bellenden Ker Range and proposed the name Mulgrave River Granite but did not define it; less deformed granite at Walshs Pyramid was included in the Yarrabah Granite (again not defined). Rubenach (1978) continued the use of this nomenclature, but it is discontinued here as it is undesirable to introduce seperate names for the same granite deformed to different degrees. Richards (1980) referred to the northern granitic intrusion (Bellenden Ker, South, Central, and North peaks) as the "Bellenden Ker batholith" and the southern area "Bartle-Frere stock" (p.230) and Bartle Frere Granite (not defined) (p240).|16-MAY-23
24177|Bellenden Ker Granite|Type section locality|Base of Kearneys Falls (Bartle Frere 1:100 000, GR 704937), in the Goldsborough Valley State Forest Park, where it is a coarse-grained porphyritic biotite granite, with large K-feldspar phenocrysts. A reference locality at the Fishery Falls (Bartle Frere 1:100 000, GR 802989) is designated in sheared coarse-grained porphyritic granite.|16-MAY-23
24177|Bellenden Ker Granite|Extent|Forms the elongated granitic massif of the Bellenden Ker Range, including Mount Bartle Frere, Mount Bellenden Ker and Walshs Pyramid; then Malbon Thompson Range east of the Mulgrave River; and Mount Josey east of the Russell River.|16-MAY-23
24177|Bellenden Ker Granite|Lithology|Medium to coarse-grained biotite granite, commonly porphyritic. Tourmaline-biotite granites with small amounts of muscovite occur on the northeastern flanks of the Bellenden Ker Range, Walshs Pyramid, and east of Green Hill in the Malbon Thompson Range. Hornblende is present in the Bartle Frere stock (Richards, 1980). Adjacent to the Mulgrave River valley, the granite has been strongly sheared. Late stage microgranite intrudes the coarse-grained granite.|16-MAY-23
24177|Bellenden Ker Granite|Relationships and boundaries|The Bellenden Ker Granite has intruded the Babalangee Amphibolite in the Mount Josey area. It also intrudes metasediments of the Hodgkinson Formation, previously termed Barron River Metamorphics, in this area. Locally, contact metamorphism has produced a narrow zone of hornfels. The relationship between the Bellenden Ker Granite and unnamed granites forming the Murray Prior Range to the north is unknown. The granite has been affected by a major shear zone in the Russell-Mulgrave valley.|16-MAY-23
24177|Bellenden Ker Granite|Age reasons|The granite was considered to be Early Permian by de Keyser (1964), Richards & others (1966), and Richards (1980). Isotopic dating by Richards & others (1966) indicated an age range of 246 to 233 m.y. (corrected isotopic ages), or latest Permian to Early Triassic. Both dating samples were taken from sheared granites and Richards (1980) considered argon loss to have occurred, thus resetting the isotopic age. The unsheared Wangetti Granite further to the north gives a Late Permian age of 255 m.y. A Late Permian to Early Triassic age is thus suggested, with deformation (shearing) being coeval with or occurring at the conclusion of magma emplacement and solidification.|16-MAY-23
24177|Bellenden Ker Granite|References|63/079;  82/22424;  98/29234;  84/24575|16-MAY-23
35123|Ben Mohr Igneous Complex|General description|Dark greenish-grey, coarse-grained, equigranular biotite-hornblende-pyroxene diorite and gabbro;Pale pink-white, medium to coarse-grained porphyritic monzogranite grading to light to pale grey, coarse to very coarse-grained porphyritic titanite-biotite-hornblende granodiorite|16-MAY-23
27075|Bernecker Creek Formation|Name source|Bernecker Creek, a tributary of Granite Creek which joins the Gilbert River at 815 678 (Gilberton 1:100 000 Sheet araea).|16-MAY-23
27075|Bernecker Creek Formation|Type section locality|White (1959) defined the Bernecker Creek Formation as a calcareous sequence underlying the Etheridge Formation and designated Bernecker Creek as the type area; no type section was specified or described. Recent BMR-GSQ mapping has shown that calcareous rocks are not as common in Bernecker Creek as White suggested; most of the rocks there are assigned to the Robertson River Formation. The calcareous rocks present probably represent only the uppermost few hundred metres of the Bernecker Creek Formation exposed in cores of anticlines. Because the structure there is relatively complex and yet poorly known, and leaching of the rocks present difficulties in distinguishing calcareous sediments from the otherwise similar non-calcareous ones, it has not been possible to map out the areas of calcaraeous rocks. As no suitable type section has been found in Bernecker Creek, two reference sections are nominated for the unit.  1. Near the Ortona copper mine along the Percy River between 645 764 (lowermost exposed part of the unit) and 633 788 (top of unit) (Gilberton 1:100 000 sheet area). About 2000 m of calcareous to non-calcareous siltstone and well-bedded fine to medium-grained calcareous quartz sandstone are exposed. The proportion of sandstone in the section ranges from about 5 to 30 percent, and some contains well-developed cross-laminae and ripple laminae. The grade of metamorphism is lower greenschist facies.  2. Along the Percyvale road from its turnoff from the Kidston-Gilberton road at 028 848, north about 3 km to 018 872 (Gilberton 1:100 000 sheet area). The rocks exposed were metamorphosed in the amphibolite facies. At the southern end of the section they consist of well-laminated muscovite-biotite-calcite-plagioclase-K-feldspar-quartz rocks and impure marble. Metamorphic grade increases to the north and the rocks grade into hornblende-diopside gneiss. The complex folding precludes any estimation of thickness of this section.|16-MAY-23
27075|Bernecker Creek Formation|Extent|Crops out in the northern half of the Gilberton 1:100 000 sheet area in four main areas, each 3 to 5 km in width: east from the Ortona mine for 11 km; west from the "Iona" turnoff from the Kidston-Gilberton road for about 8 km; east-southeast from the Lower Percy Stock camp for 15 km; and east-northeast from Mount Moran for 15 km; total area is about 200 km2.|16-MAY-23
27075|Bernecker Creek Formation|Thickness range|The original thickness of the unit is not known because the base is not exposed; the areas of outcrop where the structure is simple are in cores of anticlines. About 2000 m are exposed in the reference section in the Percy River.|16-MAY-23
27075|Bernecker Creek Formation|Lithology|Calcareous siltstone, calcareous quartz sandstone and minor impure argillaceous limestone grading eastwards into calcareous and calc-silicate-bearing schist, granofels and para-amphibolite. The low-grade rocks are generally well bedded and laminated; this is reflected in the well-developed layering of the high-grade metamorphic rocks.|16-MAY-23
27075|Bernecker Creek Formation|Relationships and boundaries|The Bernecker Creek Formation conformably underlies the Robertson River Formation. The boundary is marked by the change from predominantly calcareous to non-calcareous siltstone and sandstone in areas of low metamorphic grade, or from predominantly calc-silicate rocks to mica schist at higher grades. The change is locally sharp but is commonly gradational over a few hundred metres. High-grade Bernecker Creek Formation grades into Einasleigh Metamorphics; calc-silicate gneiss becomes increasingly more common in the latter unit towards the boundary, but it is uncertain whether this is a lateral or vertical gradation because of the complex structures. The Bernecker Creek Formation is intruded by metadolerite dykes and sills, the late Proterozoic Mount Hogan granite pluton, and the late Proterozoic or Devonian Robin Hood Granodiorite.|16-MAY-23
27075|Bernecker Creek Formation|Identifying features|Original definition: White (1959)|16-MAY-23
27075|Bernecker Creek Formation|Age reasons|Proterozoic; older than 1570 m.y., which is the age of the first deformation and metamorphic event in the Etheridge Group (Black & others, 1978).|16-MAY-23
27075|Bernecker Creek Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
27075|Bernecker Creek Formation|References|80/20677;  98/29026|16-MAY-23
38891|Berserker Group|Name source|The name was derived from the Berserker Range, in which constituent rock types are well exposed.|16-MAY-23
38891|Berserker Group|Unit history|The name was first used as the Berserker Series by Whitehouse (1930), and later the Berserker beds by Kirkegaard & others (1970). These units included the Lower Permian Berserker Group and Upper Permian Warminster Formation.|16-MAY-23
38891|Berserker Group|Constituents|The Berserker Group constitutes three formations and one member. These are shown on Figure 1 and include the Lakes Creek Formation, Chalmers Formation with the Sleipner Member, and Ellrott Formation. Relationships between these units are depicted in Figure 3.|16-MAY-23
38891|Berserker Group|Geomorphic expression|The Berserker Group is represented by topography ranging from flat areas, and low to moderate terrain, to very steep terrain especially in the central region (Figure 2). The terrain is characterised by close to widely spaced dendritic drainage pattern.|16-MAY-23
38891|Berserker Group|Extent|The Berserker Group crops out in a partly fault bounded belt approximately 90 km long and up to 15 km wide, running from the Mount Etna area in the north to the Mount Larcom area in the south. Permian rocks designated Berserker beds on the Rockhampton 1:250 000 Sheet west of Canoona were not mapped in this project; these rocks are now undifferentiated Permian until they can be compared to the rocks of the Berserker Group and Warminster Formation.|16-MAY-23
38891|Berserker Group|Thickness range|Kirkegaard and others (1970) previously interpreted the Berserker beds to be a graben fill, and approximately 3000 m thick. However, East (1946) defined an approximately 800 m thick sequence (presently defined as the Lakes Creek Formation) in the Lakes Creek area comprising (from top to bottom): dark clay shales (250-300 m); highly fossiliferous shales (100 m); massive quartzose sandstone (60 m); and interbedded sandy shales and sandstones (400 m). Current mapping supports this assessment. The Chalmers Formation, a lateral facies equivalent of the Lakes Creek Formation, is estimated to be approximately 600 m thick. In the Rockhampton-Nankin area it has been identified from sea level to no higher than 600 m. Its base is believed to be above the base of the Lakes Creek Formation (Figure 3), which suggests the Lakes Creek Formation extends to below sea level in this area.|16-MAY-23
38891|Berserker Group|Lithology|The Berserker Group comprises marine sediments dominated by siltstones, fine to coarse lithofeldspathic sandstones, felsic to intermediate intrusive and extrusive domes, and volcanic breccias with lesser conglomerates.|16-MAY-23
38891|Berserker Group|Relationships and boundaries|The Berserker Group unconformably overlies Upper Devonian to Lower Carboniferous Mount Alma Formation in the Mount Etna area, and unconformably overlies Lower Carboniferous Rockhampton Group in the Mount Larcom region. The Berserker Group is unconformably overlain by the Upper Permian Mount Warminster Formation 1 km NW of Mount Chalmers.   South of the Fitzroy River the fossiliferous beds of the Lakes Creek Formation may be close to the base of the unit. Also, the Chalmers Formation unconformably overlies the Lower Carboniferous Rockhampton Group in an area 1 km west of the peak of Mount Larcom, at the base of the Mount Larcom Range. This evidence suggests that the basement surface was higher in this area, impeding deposition of either all or a substantial part of the Lakes Creek Formation.   Present mapping suggests that the Berserker Group extended beyond its existing structural margins, and was not deposited in a graben.|16-MAY-23
38891|Berserker Group|Age reasons|Lower Permian marine fossils found in the middle of the sequence, near Rockhampton and Mount Chalmers, and at its base, in the Mount Larcom area, as well as Lower Permian U-Pb zircon dates obtained from the middle of the sequence and from the Ellrott Rhyolite, give the age constraints for the top half of the Berserker Group (Figure 3).|16-MAY-23
38891|Berserker Group|Comments|Geophysical expression:   The Lakes Creek Formation, Chalmers Formation, Sleipner Member, and Ellrott Rhyolite generally gives either a high potassium radiometric response, or a low response from potassium, thorium, and uranium. The different radiometric responses of these units presumably reflect compositional variation within the rocks. The magnetic response is low.|16-MAY-23
38891|Berserker Group|Defn Reference|SOURCE OF INFORMATION:  Crouch. S, Parfrey. S, and Taube. A  [DATE ?]. 'Geology, tectonic setting and metallogenesis of the Berserker Subprovince, northern New England Orogen'. Supplied by Ian Withnall (GSQ), September 2008.    (incomplete reference)|16-MAY-23
23382|Bevandale Granodiorite|Name source|Parish of Bevandale.|16-MAY-23
23382|Bevandale Granodiorite|Geomorphic expression|The pluton generally forms relatively subdued terrain, but hills of granite and Tertiary basalt plugs of low to moderate relief punctuate the area. The unit is best exposed as platforms and solitary boulder-sized outcrop in and adjacent to Theresa Creek.  On the Landsat TM image the Bevandale Granodiorite is delineated by cleared areas and has a yellowish hue. Two different geophysical responses occur over the outcrop area of the unit, suggesting that it may be composite. The northern part has moderate magnetic response and low K, Th and U; the southern two-thirds has low magnetic response and moderate K, Th and U.|16-MAY-23
23382|Bevandale Granodiorite|Type section locality|At 8351-339253 in Theresa Creek.  The grid reference is based on the AGD66 datum.|16-MAY-23
23382|Bevandale Granodiorite|Description at type locality|A small area of boulder-sized outcrop of grey to light grey, fine to coarse-grained, subequigranular biotite-hornblende granodiorite.|16-MAY-23
23382|Bevandale Granodiorite|Extent|A north-trending oval body 12 km2 in area bisected by Theresa Creek and centred 10 km south-southwest of Peak Vale homestead.|16-MAY-23
23382|Bevandale Granodiorite|Lithology|Dominantly grey to light grey, fine to coarse-grained, subequigranular biotite-hornblende granodiorite.|16-MAY-23
23382|Bevandale Granodiorite|Relationships and boundaries|Intrudes Anakie Metamorphic Group and is unconformably overlain by the Late Devonian to Early Carboniferous Silver Hills Volcanics. The relationship with the adjacent Central Creek Granodiorite is unknown.|16-MAY-23
23382|Bevandale Granodiorite|Age reasons|An age of 370 Ma (Middle to Late Devonian) was obtained by Rb-Sr dating of a biotite-whole rock pair.|16-MAY-23
24180|Beverly Hills Granite|Name source|Beverly Hills homestead on the eastern bank of the Robertson River at GR 050218 (Forsayth 1:100 000 sheet area).|16-MAY-23
24180|Beverly Hills Granite|Unit history|This pluton was previously mapped as Digger Creek Granite (Withnall & others, 1976).|16-MAY-23
24180|Beverly Hills Granite|Type section locality|South along the fence-line, from the road to Beverly Hills at GR 135267 (Forsayth 1:100 000 sheet area) to where it crosses Soda Creek at GR 132224. Outcrops consist mainly of pinkish-white medium-grained equigranular muscovite granite. There are subordinate outcrops of pale grey medium-grained equigranular biotite granite with biotite 'clots', and altered and weathered porphyritic biotite granodiorite with pink K-feldspar megacrysts (Oak River Granodiorite). Locally, rhyolite dykes crop out.|16-MAY-23
24180|Beverly Hills Granite|Extent|Roughly an inverted L-shaped pluton exposed on the eastern side of the Newcastle Range mainly in the south-eastern part of the Forsayth 1:100 000 Sheet area, but extending into the central western part of the Einasleigh 1:100 000 Sheet area. The total area of exposure is about 70 km2.|16-MAY-23
24180|Beverly Hills Granite|Lithology|Pale, pinkish-grey to cream, fine to medium-grained equigranular muscovite granite. Coarse-grained muscovite segregations and pegmatite are present locally. Biotite is present in some specimens. Garnet occurs locally. Outcrops are typically very weathered and fractured.|16-MAY-23
24180|Beverly Hills Granite|Relationships and boundaries|Intrudes Proterozoic Einasleigh Metamorphics and the Oak River Granodiorite. The unit is intruded by Palaeozoic rhyolite dykes, and is unconformably overlain by the Carboniferous Newcastle Range Volcanics and by Mesozoic sandstone.|16-MAY-23
24180|Beverly Hills Granite|Age reasons|Uncertain, but probably Siluro-Devonian because of the relationship with the Oak River Granodiorite, which is now also thought to be of Siluro-Devonian age.|16-MAY-23
24180|Beverly Hills Granite|Comments|Mention map legend|16-MAY-23
24180|Beverly Hills Granite|References|79/04763|16-MAY-23
24180|Beverly Hills Granite|First Reference|85/24822  September 1985|16-MAY-23
26390|Biarraville Formation|Name source|The name is derived from Biarraville homestead, 8km south-south-west of Toogoolawah.|16-MAY-23
26390|Biarraville Formation|Unit history|Campbell (1952) named the Biarraville Formation.|16-MAY-23
26390|Biarraville Formation|Geomorphic expression|The area is thickly forested, rugged in places, and forms steep country  approximately 300m above sea level.|16-MAY-23
26390|Biarraville Formation|Type section locality|Type section is located on Dry Creek (Cranfield & others, 1976).|16-MAY-23
26390|Biarraville Formation|Extent|The unit crops out near Buaraba Creek and South Buaraba Creek, Cressbrook Creek, and north of Oakey Creek (Cranfield & others, 1976).|16-MAY-23
26390|Biarraville Formation|Thickness range|The unit is about 45m thick in the type section, and probably does not exceed 50m elsewhere.|16-MAY-23
26390|Biarraville Formation|Lithology|Rock types include chert, arenite, siltstone, mudstone, sedimentary breccia, rhyolite, crinoidal limestone, and coarse-grained andesitic conglomerate.  The type section comprises conglomerate, arenite, and sedimentary breccia with a fossiliferous horizon 4.5m thick, overlain by thin conglomerate beds with abundant fossils in a bed 45cm thick and black chert with rarer fossils.  In the headwaters of South Buaraba Creek, a molluscan fauna occurs in a black calcilutite lens in a sequence of black mudstone.|16-MAY-23
26390|Biarraville Formation|Depositional environment|The presence of thin crinoidal limestones, together with arenites and conglomerates containing corals, brachiopods, bryozoans, and molluscs, indicates deposition in a marine, probably shallow water shelf environment|16-MAY-23
26390|Biarraville Formation|Fossils|The following fossils are known from the formation (after Campbell (1952):-  Brachiopods - Terrakea solida (Etheridge and Dunn), Terrakea fragilis (Dana), Strophalosia sp., Cancrinella sp., Streptorhynchus sp., Martiniopsis sp. Bryozoans - Polypora sp., Fenestella sp., Stenopora sp. Rugose corals - Eurphyllum mantuani Campbell, Eurphyllum parallelum Campbell, Eurphyllum sp. Tabulate corals - Thamnopora wilkinsoni Etheridge, Cladochonus sp. Bivalve molluscs - Glyptoleda buarabae Campbell, Aviculopecten subquinquelineatus (McCoy).     As Australian marine Permian faunas were last intensively investigated in the 1970s, this fauna needs to be re-studied.  Runnegar (1969) suggested equation of the assemblage with Fauna IV (Dickins, 1964) of possible early Late Permian age, but only on the grounds of the presence of Terrakea solida.|16-MAY-23
26390|Biarraville Formation|Relationships and boundaries|The formation conformably overlies the Hampton Road Rhyolite, and is conformably overlain by the Box Gully Formation.  It is intruded by "Champion Hills Diorite" and unconformably overlain by an outlier of the Neara Volcanics on its northern margin and by the Woogaroo Subgroup to the west.|16-MAY-23
26390|Biarraville Formation|Age reasons|Based on fossil evidence the mid- Permian age proposed by Campbell (1952) is retained.|16-MAY-23
26390|Biarraville Formation|Correlations|The unit is probably a correlative of the South Curra Limestone in the Gympie area and is approximately the same age.  The presence of white to light grey-green, partly silicified limestone, dark grey to olive shale, light grey to brown lithic labile calcareous sandstones, and green to dark green ashy and vitric tuff in PS Baylam 1 and PS Lockrose 1 wells suggests that these wells may contain the Biarraville Formation or a correlative.  PS Lockrose penetrated white dense silicified limestone, dark grey blocky pyritic shale and siltstone, light grey to grey-green medium-grained lithic labile sandstone which may be part of this unit.|16-MAY-23
26390|Biarraville Formation|Comments|GEOPHYSICAL EXPRESSION:  On the magnetic and ternary radiometric image the unit has no features to distinguish it from surounding Permian units due to its limited thickness and similar adjacent rock types.    STRUCTURE: South of the Esk-Hampton Road, the unit is exposed on the southern flank of an east- south-east plunging anticline. Here it dips between 300 and 600 and is disturbed by faulting and the intrusion of diorite.  Northeast of Mount Deongwar, the formation is folded into a northerly plunging, tight syncline with limbs dipping from 600 to vertical.  The structure is complicated by faults both parallel and normal to the axis of the syncline.|16-MAY-23
26390|Biarraville Formation|References|*CAMPBELL, K.S.W.,1952,The geology of the Cressbrook-Buaraba area,"University of Queensland.  Department of Geology Papers (New series), Regional Geology.    *CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.",1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional Geology    *DICKENS, J.M.,1964,Permian macrofossils from Homevale and from Mount Coolon 1:250 000 Sheet area. Appendix to Malone, E.J., Corbett, D.W.J., & Jensen, A.R., Geology of the Mount Coolon 1:250 000 Sheet area. Bureau of  Mineral Resources, Geology and Geophysics, Australia, Report 64, 54-65.     *RUNNEGAR, B.,N.,1969,The Permian faunal succession in eastern Australia, Geological Society of Australia, Special Publication 2, 73-98.|16-MAY-23
25784|Big Toby Granite|Name source|Big Toby Creek flows west through the Granite, 40 km west-southwest of Mount Isa, latitude 20o52'40"S, longitude 139o7'30"E (6756 050904)*.    *Australian 1:100 000 map sheet and metric grid reference (Zone 54)|16-MAY-23
25784|Big Toby Granite|Geomorphic expression|In the north the granite occurs as boulder-strewn hills and low granite tors. South of Yaringa Creek, outcrop is less continuous, consisting mostly of low bouldery east-trending ridges and groups of boulders in areas of thin sandy soil. Very weathered granite crops out along Little Toby Creek and on the slopes of the Cambrian-topped mesas.|16-MAY-23
25784|Big Toby Granite|Type section locality|The type area is near the northern limit of the granite; from a point approximately 6 km north-northwest of Gap Bore on Yaringa Creek, latitude 20o46'45", longitude 139o12'E (6756127011), it extends for 1 km north and east-northeast to include several tors of the granite and part of its contact with the Yaringa Metamorphics. In the type area the margins of the Granite consist of grey fine-grained granodiorite containing abundant dark grey xenoliths of medium-grained gneiss. Aplite and pegmatite veins occur in the marginal granodiorite and the country rock. Further from the contact the Granite is less contaminated and grades into a porphyritic fine to medium-grained granite.|16-MAY-23
25784|Big Toby Granite|Extent|The Big Toby Granite crops out discontinuously in a north-south belt less than 10 km wide which extends up to 12 km north and south of Big Toby Creek, in the Mount Isa 1:100 000 sheet area. The total area of outcrop is approximately 22 km2.|16-MAY-23
25784|Big Toby Granite|Lithology|South of Yaringa Creek the Big Toby Granite consist mostly of pinkish-grey foliated fine to medium-grained biotite granite containing some microcline phenocrysts and rare basic xenoliths. Towards the east it is more xenolithic and resembles the fine-grained granodiorite of the type area. The accessory minerals are zircon, sphene and opaque oxides. The granite is intruded by veins of quartz, quartz-hematite, aplite, and tourmaline-bearing mica pegmatite.|16-MAY-23
25784|Big Toby Granite|Relationships and boundaries|The Big Toby Granite intrudes the Yaringa Metamorphics and in the southeast it intrudes a sequence of basic volcanics that has been tentatively assigned to the Eastern Creek Volcanics. The Granite is faulted against the Mingera Beds and is unconformably overlain by Cambrian sediments. The rocks defined here as Big Toby Granite were mapped as Sybella Granite by Carter et al. (1961). The former Granite closely resembles the southern phase of the Sybella Granite from which it is separated by a fault zone containing a belt of Mingera Beds up to 5 km wide. The relations between the Big Toby Granite and the various phases of the Sybella Granite have not been established by geological mapping.|16-MAY-23
25784|Big Toby Granite|Age reasons|Although extensive radiometric dating has been done on the Big Toby Granite and the Sybella Granite this has not entirely resolved their relative ages. The earlier work yielded potassium/argon ages of 1404 m.y. and 1398 m.y. for samples of Big Toby Granite from north and south of Yaringa Creek respectively. These fall within the range (1360 to 1410 m.y.) recorded from samples of Sybella Granite (Richards et al., 1963). Some rubidium/strontium results for the northern sample of Big Toby Granite indicate a total rock age of 1566 m.y.* and a biotite age of 1450 m.y.* (Richards, 1966). These ages are similar to those Richards (1966) presents for the Sybella Granite (sensu stricto). Farquharson and Wilson (1971) combine samples from the Big Toby Granite and the Sybella Granite to locate an isochron at 1620+/-21* m.y. The Sybella microgranite and Mica Creek pegmatite which are phases of the Sybella Granite have been dated at 1520 m.y.* by total rock rubidium/strontium techniques (Farquharson and Richards, 1970). Page (pers. comm., 1974) using total rock rubidium/strontium techniques dates the Big Toby Granite at 1707+/-46 m.y.*, the foliated southern Sybella Granite at 1662+/-26 m.y., the northwestern phase of the Sybella Granite at 1577+/-13 m.y., and the Sybella microgranite at 1537+/-40 m.y. This appears to indicate that the Big Toby Granite is significantly older than all phases of the Sybella Granite, although, a uranium/lead zircon age from the northwestern phase of the Sybella Granite of 1760 to 1860 m.y. has been interpreted by Richards et al., 1966.   *Age recalculated to  decay constant^87Rb = 1.42x10^-11/ yr|16-MAY-23
25784|Big Toby Granite|Comments|Discussion: The Big Toby Granite has been distinguished from the Sybella Granite because of its geographic separation from the main mass of the latter Granite, because it intrudes different rocks which Carter et al. (1961) considered to be older than all other rocks in the region, and because rubidium/strontium age determinations indicate that it is older than the oldest phase of the Sybella Granite. Further work is needed to confirm these conclusions. The granite is possibly epizonal (Buddington, 1959) as it has sharp discordant contacts, abundant angular xenoliths and a finer grainsize towards its contacts. The foliation may be post-emplacement phenomenon associated with the regional deformation.|16-MAY-23
25784|Big Toby Granite|References|B051; 79/01427; 79/01431; 99/29861; +|16-MAY-23
25784|Big Toby Granite|Defn approved by|Queensland Sub-Committee|16-MAY-23
25784|Big Toby Granite|Name first published by|Glikson A.V., Derrick G.M., Wilson I.H., Hill R.M., 1986|16-MAY-23
1621|Bigie Formation|Name source|Parish of Bigie, County of Kamileroi|16-MAY-23
1621|Bigie Formation|Type section locality|East of Sandy Creek approximately 2.5 km north of Lily Waterhole in the Mount Oxide 1:100 000 sheet area between 400971 (base) and 405980 (top). It comprises 600 m of poorly sorted lithic hematitic sandstone and hematitic pebble conglomerate overlain by a cobble conglomerate with characteristic well rounded quartzite clasts in a hematitic matrix grading into a hematitic sandstone.|16-MAY-23
1621|Bigie Formation|Extent|In the Alhambra area of northeastern Mount Oxide 1:100 000 sheet area and southeastern Gregory Downs 1:100 000 sheet area; in a continuous band along the eastern part of the Mount Oxide and the western part of the Myally 1:100 000 sheet areas; in a thin almost continuous belt in the Alsace and Prospector 1:100 000 Sheet areas and as discontinuous outcrops in the Mount Gordon fault zone in the Mammoth Mines 1:100 000 sheet area.|16-MAY-23
1621|Bigie Formation|Thickness range|600 m in the holostratotype decreasing to 300-400 m in the Alsace and Prospector 1:100 000 sheet areas. In the Mammoth Mines 1:100 000 sheet area, the unit is thin and only locally present.|16-MAY-23
1621|Bigie Formation|Lithology|Coarse grained lithic, hematitic sandstone, commonly with pebbly layers and cobble to boulder conglomerate with well rounded clasts. In the Prospector and Alsace 1:100 000 sheet areas it comprises purple shale, marl, limestone and minor sandstone.|16-MAY-23
1621|Bigie Formation|Relationships and boundaries|The unit unconformably overlies the Quilalar Formation and Myally Sub Group. The boundary is broadly concordant but is strongly discordant in the northwestern Mount Oxide 1:100 000 sheet area. The boundary is recognised by the hematitic nature of the sediments. The unit is conformably overlain by Fiery Creek Volcanics or where these are not present, it is overlain unconformably by the Surprise Creek Formation.|16-MAY-23
1621|Bigie Formation|Age reasons|Mid Proterozoic (Carpentarian). It is equivalent to the Carters Bore Rhyolite which has been dated at 1678 m.y. (Page, 1978).|16-MAY-23
1621|Bigie Formation|References|B051;  79/19691|16-MAY-23
1621|Bigie Formation|Proposer|Hutton L.J., Cavaney R.J., Sweet I.P.|16-MAY-23
1637|Billicumidji Rhyolite Member|Name source|From Billicumidji Waterhole, at grid reference 928 487, in the Hedleys Creek 1:100 000 sheet area, Queensland (sheet 6562).|16-MAY-23
1637|Billicumidji Rhyolite Member|Type section locality|At least 2000 m, from the base at grid reference 855466 (Hedleys Creek sheet area) to the uppermost exposed beds at grid reference 175482 in the Seigal sheet area. The section runs 4.5 km in a west-northwesterly direction. At least 5 thick rhyolite flows, separated by 4 thin ignimbrite sheets (1 to 10 m thick) are present.|16-MAY-23
1637|Billicumidji Rhyolite Member|Extent|The Member is exposed over about 70 km2 in the western Hedleys Creek Sheet Area, and the eastern part of the adjacent Seigal sheet area, Northern Territory.|16-MAY-23
1637|Billicumidji Rhyolite Member|Thickness range|At least 2000 m in the type section; unknown elsewhere.|16-MAY-23
1637|Billicumidji Rhyolite Member|Lithology|Red to pink, massive and convolutely banded rhyolite. Microphenocrysts of potash and plagioclase feldspars are set in a groundmass of devitrified glass.|16-MAY-23
1637|Billicumidji Rhyolite Member|Relationships and boundaries|Conformably overlies ignimbrites of Unit 4 [unnamed ignimbrite member -Pcc>4 of Cliffdale Volcanics]. As it forms the youngest known outcrops of Cliffdale Volcanics it is overlain unconformably by Westmoreland Conglomerate. It is the only thick rhyolite sequence in the Volcanics the remainder of which are mainly ignimbrites.|16-MAY-23
1637|Billicumidji Rhyolite Member|Age reasons|Proterozoic-Carpentarian. Part of the type section of the Carpentarian System in Australia (Dunn, Plumb & Roberts, 1966). Lower units in the Cliffdale Volcanics have yielded isotopic ages of 1770 m.y. (A Webb, AMDEL Report An 1814/73, quoted in Plumb & Sweet, 1974).|16-MAY-23
1637|Billicumidji Rhyolite Member|Proposed publication|BMR Bulletin - Precambrian geology of the Westmoreland region, Northern Australia|16-MAY-23
1637|Billicumidji Rhyolite Member|References|99/30042;  79/19504|16-MAY-23
1663|Biloela Formation|Name source|The township of Biloela latitude 24o24'5"S, longitude 151o30'45"E, Monto 1:250 000 sheet area.|16-MAY-23
1663|Biloela Formation|Unit history|Kirkegaard & others (1966) in an unpublished report used the name 'Biloela Beds' for the Tertiary sedimentary rocks in the Callide Valley. However, the rocks were described as undifferentiated Tertiary sediments by Kirkegaard & others (1970) and Dear & others (1971). Grimes (1980) used the name Biloela Beds in the same sense as Kirkegaard & others (1966).|16-MAY-23
1663|Biloela Formation|Geomorphic expression|The unit is poorly exposed and is mostly flat lying. Towards the southern end of the basin the unit forms hills and ridges in proximity to overlying basalt flows. The duricrusted surface forms scattered mesas in the central and northern parts of the basin.|16-MAY-23
1663|Biloela Formation|Type section locality|The holostratotype of the Biloela Formation is defined to be between the depths of 27.2 m and 374 m in stratigraphic borehole GSQ Monto 5. The borehole is located 46 km northwest of Biloela near the eastern shore of Lake Victoria (latitude 24o02'15"S, longitude 150o17'20"E; GR 243392 Banana 1:100 000 sheet area). The holostratotype comprises 335 m of mudstone, siltstone, oil shale and sandstone with minor lignite, carbonaceous mudstone and limestone. The base of the unit is defined as the first occurrence of shale which immediately overlies basalt at 374 m. The top of the unit is defined as mudstone immediately underlying poorly consolidated silty sand at 27.2 m. A sill of basalt 11.7 m thick at 357.3 m has been excluded from the holostratotype.|16-MAY-23
1663|Biloela Formation|Extent|The Biloela Formation crops out in the Biloela Basin which is approximately 130 km long and up to 30 km wide, and covers an area of approximately 2500 km2 in the north central part of the Monto 1:250 000 sheet area and the south central part of the Rockhampton 1:250 000 sheet area.|16-MAY-23
1663|Biloela Formation|Thickness range|The formation is 335 m thick in the holostratotype and gradually thins towards the southern and northern ends of the Biloela Basin. The formation generally thickens to the west.|16-MAY-23
1663|Biloela Formation|Lithology|The unit consists mainly of mudstone, siltstone, oil shale and sandstone with minor lignite, carbonaceous mudstone and limestone. In places there is evidence that the upper part of the formation has been deeply weathered with the formation of ferruginous and silicified duricrusts.|16-MAY-23
1663|Biloela Formation|Relationships and boundaries|In the holostratotype the unit overlies unnamed basalt flows conformably and is disconformably overlain by Cainozoic alluvium. Drilling along the axis of the basin to the south of the holostratotype has also intersected unnamed basalt underlying the Biloela Formation. This relationship is not recorded in outcrop where the Biloela Formation unconformably overlies various Palaeozoic rock units of the Gogango Overfolded Zone and the Yarrol Block, and Mesozoic rock units of the Callide Basin and an outlying remnant of the Mulgildie Basin. Towards the southern end of the basin deeply weathered (ferruginised) Biloela Formation is overlain by late Oligocene basalt (K-Ar radiometric age of 25.4 m.y.).|16-MAY-23
1663|Biloela Formation|Age reasons|The Biloela Formation is probably of Early Tertiary age. The upper limit to the age of the Biloela Formation is 25.4 million years, a lower limit has not been determined.|16-MAY-23
1663|Biloela Formation|References|79/01134;  82/22417;  79/02402|16-MAY-23
24183|Birds Well Granite|Name source|Named after Birds Well (GR 725318), about 11 km SW of Duchess, Duchess 1:100 000 sheet area (Duchess 1:250 000 sheet area).|16-MAY-23
24183|Birds Well Granite|Unit history|Previously mapped as Kalkadoon Granite (Carter & Opik, 1963), which is now known to be older than Magna Lynn Metabasalt and Argylla Formation (Page, 1978).|16-MAY-23
24183|Birds Well Granite|Type section locality|About 13 km SSW of Duchess, from GR 672340 to GR 710340. Extends from Wills Creek due W across the McPhee Hills almost to track N of Mountain Paddock Tank. Mainly medium to coarse-grained, slightly to markedly porphyritic, leucocratic, weakly foliated to gneissic granite is exposed here.|16-MAY-23
24183|Birds Well Granite|Extent|The granite forms an elongate pluton W of Birds Well, and crops out over an area of about 70 sq km, Duchess 1:100 000 sheet area.|16-MAY-23
24183|Birds Well Granite|Lithology|The granite is commonly extensively recrystallised and includes some medium to coarse-grained, locally garnetiferous quartzofeldspathic gneiss and augen gneiss. Biotite is the main mafic mineral. The unit contains scattered mafic xenoliths, inclusions up to about 1 m in diameter of medium-grained gneissic granodiorite or diorite and quartz-feldspar-biotite gneiss that resemble units mapped as part of the Kalkadoon Granite batholith, and, south of Bell White Tank (GR 673421, Duchess 1:100 000 sheet area) small pendants or screens of strongly foliated medium-grained calc-silicate rocks.|16-MAY-23
24183|Birds Well Granite|Relationships and boundaries|The granite intrudes Leichhardt Volcanics, Magna Lynn Metabasalt, Argylla Formation, and granodiorite or diorite of the Kalkadoon Granite. It is cut by numerous non-foliated to foliated amphibolitic metadolerite dykes.|16-MAY-23
24183|Birds Well Granite|Age reasons|Proterozoic|16-MAY-23
24183|Birds Well Granite|Proposed publication|Blake & others, in preparation|16-MAY-23
24183|Birds Well Granite|Comments|The Birds Well Granite forms a discrete pluton geographically isolated from other intrusions.|16-MAY-23
24183|Birds Well Granite|References|R233;  98/29253;  79/19691|16-MAY-23
24184|Birimgan Formation|Name source|The name "Birimgan Formation" is derived from the property "Birimgan", 5 km southeast of the locality of the Moorlands Basin.|16-MAY-23
24184|Birimgan Formation|Type section locality|The type section (see Fig. A1) of the Birimgan Formation is the interval 10.37 m to 297.15 m from continuously cored drillhole Rutledge 1 drilled at location - AMG Reference 544204mE 7498697mN Monteagle 8352, 1:100 000 sheet. The core is stored at the core library of the Queensland Department of Mines, Zillmere.  Reference Sections: Surface reference sections of the upper part of the formation occur along small creeks in the northern and southern parts of the basin. In the northern area, the unit is exposed in a southward plunging synformal structure. A creek in the southern part of the area, north of drillhole Clermont 26, contains outcropping units mainly representative of the upper facies.|16-MAY-23
24184|Birimgan Formation|Extent|The Birimgan Formation is confined to the limits of the fault-bounded Moorlands Basin, a north-south elongate basin 7 km long by approximately 1 km wide, centred 30 km northwest of Clermont, central Queensland.|16-MAY-23
24184|Birimgan Formation|Thickness range|The thickness of the type section of the Birimgan Formation is 287 m, and throughout the basin the thickness of the formation ranges between 180 m and 287 m. The unit is thickest in the northern and southern lobes of the basin.|16-MAY-23
24184|Birimgan Formation|Lithology|The Birimgan Formation consists of mostly fine to medium grained, labile to sub-labile sandstone with interbeds of mudstone, siltstone and coal. A few coarse-grained, well-sorted massive, quartzose sandstone beds occur, mainly towards the top. The predominant framework constituent of the sandstone is quartz, with minor metamorphic rock fragments. The quartz fragments are of dominantly igneous and metamorphic origin. The interstitial material consists of clay and quartz cement. Where exposed at the surface, the formation displays pebble beds, cross-bedding and ripple marks, plant fragments and interbedded siltstone. Within the basin the formation contains two major coal bearing intervals with an aggregate thickness ranging from 3 m to 6 m. The upper coal bearing interval is present only in the northern and southern lobes of the basin, whereas the lower interval is present throughout the basin being typically as two seams.|16-MAY-23
24184|Birimgan Formation|Depositional environment|The formation is regarded as being predominantly the result of levee progradation within a deltaic interdistributary bay and includes sediments deposited in stream channels, lagoons, swamps, and tidal marshes. The presence of worm and organism burrows is indicative of periodic paralic conditions.|16-MAY-23
24184|Birimgan Formation|Fossils|The microflora of the Birimgan Formation has been described by Price (1983, 1984) from core samples which yielded diverse forms of Dulhuntyispora including D. parvitholus and towards the top of the sequence D. stellata indicating the unit spans the upper stage 5a/upper stage 5b boundary. A meagre marine macrofossil fauna near the base of the unit may be equivalent to the Wyndhamia clarkei bed indicating the unit to be of Middle Permian age.|16-MAY-23
24184|Birimgan Formation|Relationships and boundaries|The Birimgan Formation unconformably overlies the Anakie Metamorphics and is overlain unconformably by undifferentiated Cainozoic sediments and basalt.|16-MAY-23
24184|Birimgan Formation|Identifying features|The main distinguishing characteristics of the Birimgan Formation are the quartz rich sub-rounded rock fragments of its constituent sandstones, the presence of pronounced marine depositional structures and the low rank, high sulphur coal seams.|16-MAY-23
24184|Birimgan Formation|References|84/24148|16-MAY-23
33437|Bjelke Petersen beds|Name source|The unit is named after the Bjelke Petersen Dam, where it is well exposed in cuttings and quarries immediately north of the dam wall.|16-MAY-23
33437|Bjelke Petersen beds|Unit history|The unit has a characteristic limestone/basalt/turbidite association that is unique within the Yarraman Subprovince.  Reid (1925) who assigned these rocks to his "Wondai Series" and first noted the limestone (informally known as the "Barambah limestones").  Derrington (1954) described the northernmost limestones and included them in his "Wondai Metamorphics", a named he introduced in place of "Wondai Series".  Palmieri (1969) described a conodont fauna from the limestone based on earlier mapping by Sawers (1968). The limestone-bearing sequence was subsequently included in an undivided Carboniferous to Permian (C-P) unit by Murphy & others (1976), a unit that encompassed the "Wondai Metamophics", a term they discontinued. The geology of the limestone bodies was subsequently described in some detail by Martin (1977), in the context of their economic value as quarry rock.|16-MAY-23
33437|Bjelke Petersen beds|Geomorphic expression|The unit forms the eastern sloping flanks of the major ridge system formed by the adjacent Maronghi Creek beds.  The latter sheds chert-rich scree blankets over sections of the Bjelke Petersen beds.  The unit is heavily timbered, with no distinctive photo pattern.|16-MAY-23
33437|Bjelke Petersen beds|Type section locality|The unit is not well enough exposed to specify a type section. The best exposures of the unit are immediately north of the dam wall in cuttings and quarries.|16-MAY-23
33437|Bjelke Petersen beds|Extent|The unit occurs about 3km east of Murgon as a narrow (~ 1km wide), north-north-west trending sliver over 15km in strike length.|16-MAY-23
33437|Bjelke Petersen beds|Thickness range|The unit suffers from internal faulting, making an estimate of its thickness difficult. A likely thickness is probably around 500m.|16-MAY-23
33437|Bjelke Petersen beds|Lithology|The unit consists mainly of interbedded andesitic to basaltic lava, limestone, mudstone, chert, and phyllite.  The mafic volcanics are mostly dark grey-green to purple-brown in colour, amygdaloidal and locally strongly sheared.  The fine-grained clastics are generally strongly cleaved, and contain thin lensoidal beds or laminae of chert or siliceous siltstone.   The limestone occurrences range from small pods less than a metre in size to large lenses up to 300m in length and 150m in width, mapped as subunit Cbl.  The limestone and mafic volcanics commonly have thinly-interlayered or interdigitating contacts.  A similar relationship between the limestone and enclosing fine-grained clastics was observed at the southernmost limestone locality.   The limestone is moderately to strongly recrystallised, light to dark grey or pale green to pink or brown in colour. The limestone shows significant contamination by volcanic detritus near the contacts. The limestone are commonly internally brecciated and weather to clay and "terra rossa" soils.|16-MAY-23
33437|Bjelke Petersen beds|Depositional environment|The unit consists mainly of interbedded andesitic to basaltic lava, limestone, mudstone, chert, and phyllite.  The mafic volcanics are mostly dark grey-green to purple-brown in colour, amygdaloidal and locally strongly sheared.  The fine-grained clastics are generally strongly cleaved, and contain thin lensoidal beds or laminae of chert or siliceous siltstone.   The limestone occurrences range from small pods less than a metre in size to large lenses up to 300m in length and 150m in width, mapped as subunit Cbl.  The limestone and mafic volcanics commonly have thinly-interlayered or interdigitating contacts.  A similar relationship between the limestone and enclosing fine-grained clastics was observed at the southernmost limestone locality.   The limestone is moderately to strongly recrystallised, light to dark grey or pale green to pink or brown in colour. The limestone shows significant contamination by volcanic detritus near the contacts. The limestone are commonly internally brecciated and weather to clay and "terra rossa" soils.PROVENANCE:: The deep marine clastic component of the unit was probably derived from the Australian craton and was deposited during periods of volcanic quiescence|16-MAY-23
33437|Bjelke Petersen beds|Relationships and boundaries|The unit is faulted against the older Devonian-Carboniferous Maronghi Creek beds and the younger Triassic Esk Formation.  The unit is unconformably overlain by Tertiary sediments, and locally capped by Tertiary duricrust surfaces.|16-MAY-23
33437|Bjelke Petersen beds|Age reasons|Conodonts, forams, fish teeth, fish scales, annelid jaws, and crinoid fragments have been recorded from the limestone bodies (Palmieri, 1969; Martin, 1977).  The conodont fauna indicates a Namurian/Westphalian (Late Carboniferous, equivalent to an age of about 311-314Ma) age for the Bjelke Petersen beds (Palmieri, 1969).  The contact relationships suggest an autochthonous origin for the limestones, suggesting the condont dating is a reliable indicator of the true age of the unit.|16-MAY-23
33437|Bjelke Petersen beds|Correlations|Similar warm water conodont faunas have been recorded from limestone within the Goodnight beds, a probable correlative mapped to the north on the Maryborough 1:250 000 Sheet (Cranfield, 1994).  Other correlatives further to the north may include the accretionary wedge rocks of the youngest part of the Curtis Island Group (the Shoalwater Formation).|16-MAY-23
33437|Bjelke Petersen beds|Comments|GEOPHYSICAL EXPRESSION: The unit forms dark tones on AIRDATA K-Th-U ternary radiometric images and also has a low response on aeromagnetic images.   STRUCTURE: The unit has well developed, bedding-parallel, slaty cleavage in clastic rocks, extensive fracturing in limestone, and widespread development of an anastomosing schistosity in the basalt.  Strong melange-style shear fabrics occur locally.  On the eastern side of the Bjelke Petersen dam wall, elongate limestone phacoids occur within a schistose greenstone matrix.  One of the limestone bodies 4km to the south of the dam grades outwards into brecciated limestone that is cut by a 50cm wide mylonitic shear zone. Most of the internal cleavage development, shearing and brecciation is thought to have occurred during Late Palaeozoic subduction of the sequence at the eastern margin of the Australian craton.   The present structural geometry of the unit is characterised by bedding/cleavage dips that are moderate to steep to the west.  Company drilling suggests that the limestone sequence is truncated to the west along its contact with the Maronghi Creek beds by a northerly-trending fault.|16-MAY-23
33437|Bjelke Petersen beds|References|CRANFIELD, L.C. ,1994,Maryorough, Queensland Sheet SG56/06, 1:250 000 geological explanatory notes.","Department of Mines and Energy, Brisbane, Queensland.DERRINGTON, S.S,1954,The geology of the Murgon-Windera district. Unpublished Bsc Honours Thesis, Department of Geology, University of Queensland. Regional Geology,Murgon.MARTIN, J.E.,1977, Barambah Limestone deposits, Murgon, Geological Survey of Queensland, Report 20, Part B., Limestone resources.PALMIERI, V., 1969, Upper Carboniferous conodonts from limestones near Murgon, Southeast Queensland, Geological Survey of Queensland Publication 341, Palaeontological Papers, 17.REID, J.H., 1925, The Murgon-Goomeri Districts. Queensland Government Mining Journal. 26, 87-91.SAWERS, J.D.,1968, Barambah limestone deposits, Murgon, Queensland Government Mining Journal, 69, 405-407.|16-MAY-23
24188|Blackeye Granite|Name source|Named after Blackeye Creek, which drains NE to join the McKinlay River near Answer Downs homestead (at GR 995045), in the east of the Selwyn 1:100 000 Sheet area, Duchess 1:250 000 Sheet area. The outcrop area of the granite is drained by a branch of Blackeye Creek.|16-MAY-23
24188|Blackeye Granite|Unit history|Like all other granites in the eastern part of the Duchess 1:250 000 sheet area, the Blackeye Granite was mapped as Williams Granite by Carter & Opik (1963).|16-MAY-23
24188|Blackeye Granite|Type section locality|Central part of outcrop area, at GR 905977, Selwyn 1:100 000 sheet area, where medium to fine-grained leucocratic granitic rocks are exposed along an eastward-draining creek.|16-MAY-23
24188|Blackeye Granite|Extent|The Blackeye Granite forms a clearly defined N-trending outcrop 1.6 km long and 0.4 km wide centred at GR 905977, 6 km WNW of Glenholme homestead, Selwyn 1:100 000 sheet area.|16-MAY-23
24188|Blackeye Granite|Lithology|Medium to fine-grained, even-grained, foliated, leucocratic granodiorite; minor quartz-feldspar pegmatite. The granodiorite contains about 5 percent dark minerals (amphibole+/-biotite+/-clinopyroxene).|16-MAY-23
24188|Blackeye Granite|Relationships and boundaries|Intrudes the Doherty Formation (new name).|16-MAY-23
24188|Blackeye Granite|Age reasons|Proterozoic|16-MAY-23
24188|Blackeye Granite|Comments|The Blackeye Granite forms a well-defined intrusive body geographically separated from other granitic intrusives. It is probably related to the petrographically similar but more heterogeneous Cowie and Maramungee Granites (new names) to the west and north, respectively. All [these] granites previously mapped as Williams Granite, together with the Wimberu Granite, make up the Williams Batholith (new structural term).|16-MAY-23
24188|Blackeye Granite|References|R233;  98/29253|16-MAY-23
2259|Boondooma Igneous Complex|Name source|From Boondooma Creek, located at grid reference 4240 7400, on Chinchilla 1:250 000 sheet SG56-9.|16-MAY-23
2259|Boondooma Igneous Complex|Unit history|Boyne River Granite, McTaggart (1963). "Yarraman Igneous Complex", Exon et al. (1968).|16-MAY-23
2259|Boondooma Igneous Complex|Constituents|Rgbo - Coarsely K-feldspar-phyric to megacrystic biotite granite, K-feldspar-phyric medium grained granite, even grained medium grained biotite granite, microgranite, rhyolite and microgranite dykes.  Rgbo[p] - Coarsely K-feldspar-phyric to megacrystic biotite granite.   Rgbo[k] - Kaolinised granite.   Rgbo[d] - Pyroxene - hornblende diorite.   PRgb - Even grained medium to coarse grained biotite granite commonly strongly jointed and weathered.   PRgb[g] - Grey-pink medium grained granite, coarse grained pink granite.  Locally hydrothermally altered (shown by screen on map).   PRgb[d] - Dark grey even grained diorites to granodiorites.   PRgb[k] - Light grey to white deeply weathered and kaolinised granite.|16-MAY-23
2259|Boondooma Igneous Complex|Type section locality|On the Burnett-Condamine Highway from 478 725 (Yard grid) 26o22'S, 151o43'E, to 440 725 (Yard grid) 26o23'S, 151o22'E.|16-MAY-23
2259|Boondooma Igneous Complex|Extent|The unit crops out from grid reference 4150 7390, in the west to grid reference 5000 7250, in the east, from grid reference 4920 6490 in the south to grid reference 4400 7780, Mundubbera 1:250 000 sheet SG 56-5 in the north.|16-MAY-23
2259|Boondooma Igneous Complex|Lithology|The lithology is extremely variable and includes granodiorite, granite, diorite, adamellite, and gabbro.|16-MAY-23
2259|Boondooma Igneous Complex|Relationships and boundaries|The complex intrudes undifferentiated Palaeozoic metamorphics. The complex is overlain by Middle Triassic Aranbanga Beds, Upper Triassic Tarong Beds, Upper Triassic to Lower Jurassic Bundamba Group and Tertiary Main Range Volcanics.|16-MAY-23
2259|Boondooma Igneous Complex|Relationships and boundaries|Rgbo, Rgbo[d] - Intrudes PRgb, Chahpingah Meta-Igneous Complex.    PRgb - Intrudes Maronghi Creek beds, overlain by Tarong beds|16-MAY-23
2259|Boondooma Igneous Complex|Age reasons|K/Ar radiometric ages of 239 m.y., 253 m.y., and a Rb/Sr age of 274 m.y. were obtained by Webb and McDougall (1968). Murphy et al. (in prep.) [79/01628] obtained K/Ar ages of 231 m.y., 234 m.y., 217 m.y., 245 m.y., 257 m.y.  A Permo-Triassic age is assigned to the Complex.|16-MAY-23
2259|Boondooma Igneous Complex|Age reasons|Rgbo - Age dates in the unit are sparse, indicating a generally Early Triassic age - 248+/-2.1, 238.9 Ma.   PRgb - Age dates vary from greater than 250Ma (253, 257, 254) to 215 Ma.   PRgb[g] - Age dates are variable - 260.2 Ma, 249 Ma.    PRgb[d] - 267.9 +/- 8 Ma.   PRgb[k] - Age date of 252+/- 2.6 Ma, 272.7 +/- 9 Ma.|16-MAY-23
2259|Boondooma Igneous Complex|References|68/053;  98/28955;  99/29928.      *EXON, N.F., REISER, R.F., JENSEN, A.R., BURGER, D., &  THOMAS, B.M.,1968,The Geology of the Chinchilla 1:250 000 Sheet Area, Bureau of Mineral Resources, Australia, Record 1968/53.    *McTAGGART, N.R.",1963,Geology of the northeastern Surat Basin, Australian Oil and Gas Journal, 9(12), 44-52.",Regional Geology.    *MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96, Regional Geology, Gympie 1:250 000 Sheet.    *WEBB, A.W. & MCDOUGALL, I.1968, The geochronology of the igneous rocks of eastern Queensland. , Journal of the Geological Society of Australia., 15, 313-346.|16-MAY-23
2259|Boondooma Igneous Complex|Name first published by|Geological Survey of Queensland 1975|16-MAY-23
2321|Border Waterhole Formation|Name source|Unit name derived from Border Waterhole, located at approximately (GDA94) 18degrees36’44”S 137degrees59’33”E, about 2.5 km northwest of Highland Plains homestead.|
2321|Border Waterhole Formation|Unit history|Unit first named by Öpik (1960). Described in further detail by Carter and Öpik (1961). Name has not been revised since.|
2321|Border Waterhole Formation|Geomorphic expression|Typically forms low rubbly ridges; rough limestone faces with open joints in places (Carter and Öpik, 1961). Obscured in places by regolith of chert breccia and pebbles (Rawlings et al, 2008).|
2321|Border Waterhole Formation|Type section locality|No type section defined. Measured section M376 of Carter and Öpik (1961) nominated herein as a reference section for the lower Border Waterhole Formation, located at approximately (pre-AGD66) 18degrees37’S 138degrees01’E (54K 185178mE 7938968mN) on the LAWN HILL 1:250 000 mapsheet in Queensland. Reference area for this formation nominated in the vicinity of (GDA94) 18degrees38’S 138degrees01’E (54K 185209mE 7937122mN) on the LAWN HILL 1:250 000 mapsheet.|
2321|Border Waterhole Formation|Extent|The unit is present across the western LAWN HILL 1: 250 000 mapsheet in Queensland, and the eastern MOUNT DRUMMOND 1:250 000 mapsheet in the Northern Territory (Rawlings et al, 2008).|
2321|Border Waterhole Formation|Thickness range|Not recorded at reference section. Varies from approx. 30 to 45 m thick across LAWN HILL 1:250 000 mapsheet (Carter and Öpik, 1961). The unit varies in thickness from approx. 30 to 180 m (Shergold and Druce, 1980).|
2321|Border Waterhole Formation|Lithology|Contorted but generally south-dipping (20-30degrees), friable, siliceous shale with ptychoparlids, agnostids and stenotheca (Carter and Öpik, 1961).|
2321|Border Waterhole Formation|Depositional environment|Depositional environment of the Border Waterhole Formation is presumably shallow marine, due to the presence of limestone (inc. bioclast floatstone and rudstone) (Rawlings et al, 2008), and trilobite fossils such as Xystridura, Lyriaspis, Peronopsis (Carter and Öpik, 1961).|
2321|Border Waterhole Formation|Fossils|Trilobites including Redlichia, Xystridura, Lyriaspis, Pagetia and Peronopsis. Molluscs including Stenotheca and Helcionella. Hyoliths include Biconulites. Sponge spicules (Öpik, 1960; Carter and Öpik, 1961; de Keyser, 1969; Rawlings et al, 2008).|
2321|Border Waterhole Formation|Relationships and boundaries|The Border Waterhole Formation unconformably (sometimes with an angular discordance) overlies the Plain Creek Formation or the Lawn Hill Formation of the McNamara Group (Lawn Hill Platform), and is conformably overlain by the Currant Bush Limestone (Rawlings et al, 2008).|
2321|Border Waterhole Formation|Identifying features|Formation is typically distinguished by the presence of abundant chert breccia and pebbles (Rawlings et al, 2008).|
2321|Border Waterhole Formation|Structure and Metamorphism|Beds of the Border Waterhole Formation display steep dips (up to 80°) in proximity to fault zones (e.g. Little Range Fault) (Carter and Öpik, 1961).|
2321|Border Waterhole Formation|Age reasons|Trilobites indicate a middle Cambrian (Series 2) age (Rawlings et al, 2008).|
2321|Border Waterhole Formation|Correlations|Correlated with the Beetle Creek Formation of the Georgina Basin (Smith, 1972).|
2321|Border Waterhole Formation|Alteration and Mineralisation|This unit hosts the Highland Plains phosphate deposit, which straddles the Northern Territory – Queensland border (Rawlings et al, 2008).|
2321|Border Waterhole Formation|Geophysical Expression|Weak magnetic response|
2321|Border Waterhole Formation|Defn author|Elliot Foley, Jack Simmons, Ben Williams, Charles Verdel (Northern Territory Geological Survey), Chris Carson (Geoscience Australia) 31-MAY-2023.|
2321|Border Waterhole Formation|Comments|Standard series 1: 100 000 and 1: 250 000 mapsheet names are shown in uppercase.|
2321|Border Waterhole Formation|References|Carter EK and Öpik AA, 1961. Lawn Hill- 4-mile geological series. Explanatory notes No. 21. Bureau of Mineral Resources, Canberra.
Carson, C. J., Kositcin, N., Anderson, J. R., and Henson, P. A. in prep. A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia  -  insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences  **de Keyser F, 1969. The phosphate-bearing Cambrian formations in the Lawn Hill and Lady Annie districts, northwestern Queensland. Bureau of Mineral Resources, Record 1969/147.  **Öpik AA, 1960. Cambrian and Ordovician geology of Queensland. Journal of the Geological Society of Australia 7, 89-109  **Rawlings DJ, Sweet IP and Kruse PD, 2008. Mount Drummond, NT (Second Edition). 1:250 000 Geological Map Series Explanatory Notes, Sheet SE 53-12. Northern Territory Geological Survey, Darwin, Northern Territory.  **Roberts HG, Rhodes JM and Yates KR, 1963. Calvert Hills, Northern Territory (First Edition). 1:250 000 geological map series explanatory notes, SE 53‑8. Bureau of Mineral Resources, Canberra.  **Shergold JH and Druce EC, 1980. Upper Proterozoic and Lower Palaeozoic rocks of the Georgina Basin: in Henderson RA and Stephenson PJ (editors), 'The geology and geophysics of northeastern Australia'. Geological Society of Australia, Queensland Division, 149–174.  **Simmons JM, Williams B, Carson, C and Verdel C, 2023a. Mount Drummond, Northern Territory 1:250 000 Geological Map, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.  **Simmons JM, Williams B, Carson, C and Verdel C, 2023b. Mount Drummond, Northern Territory 1:250 000 Geological Map Explanatory Notes, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.  **Smith KG, 1972. Stratigraphy of the Georgina Basin. Bureau of Mineral Resources, Bulletin 111.|
28307|Boroston Formation|Name source|Parish of Boroston, County of Philp (Clarke River 1:250 000 Cadastral map).|16-MAY-23
28307|Boroston Formation|Unit history|Previously mapped as Bundock Creek Formation (now Group) by White (1959, 1962, 1965) and 'upper' Bundock Creek Formation by Wyatt & Jell (1980).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
28307|Boroston Formation|Geomorphic expression|The unit is expressed as a series of generally low strike ridges, but the lower conglomeratic unit forms a high ridge, especially in the north.  It contrasts with the generally recessive Teddy Mount Formation.|16-MAY-23
28307|Boroston Formation|Type section locality|An unnamed tributary of McKinnons Creek between 7859 375566 (base) and 7759-370577 (top).   The grid reference is based on the AGD66 datum.|16-MAY-23
28307|Boroston Formation|Description at type locality|The base is the bottom of a distinctive, ridge-forming, very coarse-grained, quartzose sandstone to cobble conglomerate.  The remainder of the unit is medium to coarse-grained, micaceous, lithofeldspathic sublabile to quartzose sandstone, conglomerate and mudstone. The section is 1050 m thick.|16-MAY-23
28307|Boroston Formation|Extent|In several synclinal cores from Mount Brown and Bullock Dray Creeks in the south to Teddy Mount in the north, and west to near 'Oak Valley'.|16-MAY-23
28307|Boroston Formation|Thickness range|1050 m in the type section, but probably only about 200 m in the Boroston Syncline.|16-MAY-23
28307|Boroston Formation|Lithology|Medium to coarse-grained, micaceous, lithofeldspathic sublabile sandstone and mudstone. Local quartzose sandstone and cobble conglomerate. The sandstones are trough cross-bedded.|16-MAY-23
28307|Boroston Formation|Fossils|No fossils have been recorded from the unit.|16-MAY-23
28307|Boroston Formation|Relationships and boundaries|The Boroston Formation overlies the Teddy Mount Formation with apparent conformity, and is distinguished from it by the abundant, sublabile to quartzose sandstone.  It is conformably overlain by the tuffaceous Harry Creek Formation, and is intruded by the Carboniferous or ?Permian Montgomery Range Igneous Complex.|16-MAY-23
28307|Boroston Formation|Age reasons|An Early Carboniferous age, probably Tournaisian, is considered most likely for the unit, because it overlies the Late Devonian to Early Carboniferous Teddy Mount Formation.|16-MAY-23
28307|Boroston Formation|References|*WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.    *WHITE, D.A., 1962:  Clarke River - Qld E/55-13.  Bureau of Mineral 	Resources, Australia 1:250 000 Geological Series Explanatory Notes.    *WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.    *WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.D., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.    *WYATT, D.H. & JELL, J.S., 1980:  Devonian and Carboniferous stratigraphy of the northern Tasman Orogenic Zone in the Townsville hinterland.  In. Henderson, R.A. & Stephenson, P.J. (editors), The Geology and Geophysics of Northeastern Australia.  Geological Society of Australia, Queensland Division, Brisbane, 201-228.|16-MAY-23
2347|Bortala Formation|Name source|Bortala' holding near Bull Creek, 140 km north of Mount Isa, latitude 19o40'S, longitude 139o35'E; Dobbyn 1:250 000 sheet area.|16-MAY-23
2347|Bortala Formation|Type section locality|Between Paroo and Conglomerate Creeks, 17 km south-southwest of Julius dam, in the Prospector 1:100 000 sheet area, grid reference 600576, from latitude 20o16'25"S, longitude 139o39'E, to latitude 20o16'24"S, longitude 139o40'E. Pale brown to grey siltstone and sandstone 400 m thick are cut by the Mount Isa-Julius dam pipeline road.|16-MAY-23
2347|Bortala Formation|Extent|The formation is exposed in a north-trending belt 200 km long and 50 km wide. Mount Isa is near the southern limits of the formation.|16-MAY-23
2347|Bortala Formation|Thickness range|80 to 700 m: the formation thins from south to north.|16-MAY-23
2347|Bortala Formation|Lithology|Highly feldspathic brown to purple grey sandstone and siltstone, flaggy to blocky, thin-bedded to laminated. Parallel bedding is dominant. Minor quartzose sandstone and grey shale. The formation is valley forming.|16-MAY-23
2347|Bortala Formation|Relationships and boundaries|Conformable between the underlying Alsace Quartzite and the overlying Whitworth Quartzite; overlain unconformably by the Mount Isa Group in the Paroo Range, 30 km north of Mount Isa.|16-MAY-23
2347|Bortala Formation|Age reasons|Carpentarian; minimum age about 1650 m.y. set by intrusion of the Sybella Granite into Bortala Formation equivalents west of Mount Isa.|16-MAY-23
2347|Bortala Formation|Comments|This formation was formerly an undifferentiated part of the Myally Beds (Carter et al., 1961); the very high plagioclase feldspar content (50%) is characteristic of the unit.|16-MAY-23
2347|Bortala Formation|References|B051|16-MAY-23
2347|Bortala Formation|Name first published by|Glikson A.Y., Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
2360|Bottletree Formation|Name source|Named after Bottletree Hummock (GR 532756), in the NW part of the Duchess 1:100 000 sheet area, Duchess 1:250 000 sheet area.|16-MAY-23
2360|Bottletree Formation|Unit history|Previously mapped as Leichhardt Metamorphics, Argylla Formation and Mount Guide Quartzite (Carter & Opik, 1963). The sequence extends north into southwestern part of the Mary Kathleen 1:100 000 sheet area where it has been mapped as Argylla Formation by Derrick & others (1977).|16-MAY-23
2360|Bottletree Formation|Type section locality|From GR 514542 to GR 518540, Duchess 1:100 000 sheet area. Here the formation is about 400 m thick. The track between Bushy Park and Mount Guide homesteads crosses the formation about 1 to 2 km N of the type section. The lower part of the section, in the E, consists mainly of schistose amygdaloidal and massive metabasalt, and interlayered lenses of quartzite, commonly epidotic. The overlying sequence contains foliated, rhyolitic to dacitic metavolcanics and interlayered greywacke, greywacke conglomerate, arkose and conglomeratic arkose, together with some schistose amphibolite units. Clasts in the conglomeratic metasedimentary rocks are well rounded to angular, up to 1 m (but generally less than 20 cm) across, and consist mainly of felsic metavolcanics, amphibolite, granite and quartzite. The upper part of the unit consists of schistose metabasalt similar to that found in the basal part.|16-MAY-23
2360|Bottletree Formation|Extent|The formation forms a N-trending belt about 30 km west of Duchess, and extends S into the Dajarra 1:100 000 sheet area, and SW into the Ardmore 1:100 000 sheet area.|16-MAY-23
2360|Bottletree Formation|Thickness range|The thickness of the formation is very variable; a maximum of about 3000 m is attained in the NW of the Duchess 1:100 000 sheet area. The variable thickness may be attributed partly to localised volcanism and partly to deposition on an irregular surface.|16-MAY-23
2360|Bottletree Formation|Lithology|The formation consists mainly of sparsely to richly porphyritic, rhyolitic to dacitic lava flows and ash-flow deposits, and interlayered beds of greywacke and greywacke conglomerate and grit. Sheared, schistose, amygdaloidal to massive metabasalt is common at or near the base and top of the formation. Other rock types present include arkose, arkosic grit, bedded tuff or siltstone, ?agglomerate, meta-arenite and quartzite, epidotic quartzite, and laminated para-amphibolite. The formation has been regionally metamorphosed, mainly to greenschist or amphibolite facies.|16-MAY-23
2360|Bottletree Formation|Relationships and boundaries|The Bottletree Formation unconformably overlies Kalkadoon Granite and undivided Tewinga Group, and is interpreted to be conformably overlain by the Yappo Mbr. Conglomeratic metasediments similar to those in the Bottletree Formation make up much of the Yappo Member (of Mount Guide Quartzite).|16-MAY-23
2360|Bottletree Formation|Age reasons|Provisionally dated by the U-Pb-zircon method at about 1800 m.y. (R.W. Page, BMR, personal communication, 1980).|16-MAY-23
2360|Bottletree Formation|References|R233;  98/29253;  B193|16-MAY-23
2360|Bottletree Formation|Apprdate|10-DEC-1980|16-MAY-23
2360|Bottletree Formation|Defn approved by|Whitaker W.|16-MAY-23
2360|Bottletree Formation|Proposer|Bultitude R.J.|16-MAY-23
24196|Bowlers Hole Granite|Name source|Named after Bowlers Hole Dam, GR 771635, in NE of Duchess 1:100 000 sheet area (Duchess 1:250 000 sheet area).|16-MAY-23
24196|Bowlers Hole Granite|Unit history|Mapped as Kalkadoon Granite by Carter & Opik (1963), but is now known to intrude units significantly younger than Kalkadoon Granite (Page, 1978).|16-MAY-23
24196|Bowlers Hole Granite|Type section locality|About 9.5 km north of Bowlers Hole Dam, from GR 766740 to GR 798718, Duchess 1:100 000 sheet area. Area is 1.5 km W of Duchess-Fountain Springs track and is drained by unnamed tributary of the Malbon River. Mainly foliated, pink, medium to coarse-grained, slightly porphyritic, biotite-hornblende granite here.|16-MAY-23
24196|Bowlers Hole Granite|Extent|The granite forms an elongate pluton 11 km long and up to 3.5 km wide, extending from GR 781756 to GR 762635, with rare, small satellitic pods, north of Bowlers Hole Dam, Duchess 1:100 000 sheet area.|16-MAY-23
24196|Bowlers Hole Granite|Lithology|Consists mainly of foliated, slightly porphyritic, biotite-hornblende granite. Minor rock types include gneissic biotite granite, microgranite, aplite, pegmatite, and some mafic-rich ?contaminated granite. Granite contains mafic xenoliths and inclusions of probable extensively recrystallised felsic metavolcanics and coarse-grained granite.|16-MAY-23
24196|Bowlers Hole Granite|Relationships and boundaries|The granite intrudes the Magna Lynn Metabasalt and Leichhardt Volcanics. Some pegmatite veins thought to be related to the granite cut the Argylla Formation. The granite is intruded by metadolerite, now mainly schistose amphibolite, dykes.|16-MAY-23
24196|Bowlers Hole Granite|Age reasons|Proterozoic|16-MAY-23
24196|Bowlers Hole Granite|Comments|The Bowlers Hole Granite is geographically isolated from other granite bodies in the region.|16-MAY-23
24196|Bowlers Hole Granite|References|R233;  98/29253;  79/19691|16-MAY-23
24196|Bowlers Hole Granite|First Reference|82/22710;  82/22663|16-MAY-23
80377|Bowthorn Member|Name source|Name derived from Bowthorn Homestead, located at approximately (GDA94) 18degrees5’52”S 138degrees18’08”E, on the BOWTHORN 1:100 000 mapsheet (Sweet, 1981; Sweet et al, 1981).|
80377|Bowthorn Member|Unit history|Unit originally mapped as undifferentiated Constance Sandstone in the First Edition MOUNT DRUMMOND 1:250 000 mapsheet (Smith and Roberts, 1963a, b). Unit subsequently remapped as the “Bowthorn Siltstone Member” of the Constance Sandstone in the BOWTHORN 1:100 000 mapsheet (Slater and Mond, 1980) and the HEDLEYS CREEK 1:100 000 mapsheet (Sweet, 1981; Sweet et al, 1981). Unit renamed as the “Bowthorn Member” of the Constance Sandstone by Sweet (2017).|
80377|Bowthorn Member|Geomorphic expression|The unit is predominantly recessive and outcrops poorly in scarps and slopes due to its fine-grained, siltstone-dominated nature, causing marked topographic contrast with more resistant sandstone units. More sandstone-dominated intervals within the Bowthorn Member form topographic benches (Sweet, 2017).|
80377|Bowthorn Member|Type section locality|Type section located along a low ridge approximately 1.5 km south of the access road to Bowthorn Homestead, on the BOWTHORN 1:100 000 mapsheet. Base of type section located at approximately (GDA94) 18degrees07’18”S 138degrees21’37”E (54K 220664mE 7994351mN). Top of type section located at approximately 18degrees07’35”S 138degrees21’15”E (220024mE 7993819mN; Sweet, 1981; Sweet et al, 1981).|
80377|Bowthorn Member|Extent|The unit is present in the BOWTHORN and HEDLEYS CREEK 1:100 000 mapsheets, which form the western sector of the LAWN HILL 1:250 000 mapsheet in Queensland. It also occurs on the CLEANSKIN 1:100 000 mapsheet, which forms the north-eastern sector of the MOUNT DRUMMOND 1:250 000 mapsheet in the Northern Territory (Sweet, 2017).|
80377|Bowthorn Member|Thickness range|Approximately 300 m thick in the type section, yet elsewhere on the BOWTHORN 1:100 000 mapsheet, it varies from approximately 100 m to 400 m thick (Sweet, 2017). The unit is approximately 220 m thick in the northeastern portion of the MOUNT DRUMMOND 1:250 000 mapsheet (Simmons et al, 2023b).|
80377|Bowthorn Member|Lithology|Laminated purple and brown micaceous siltstone; a few thin interbeds of quartz sandstone occur to the north and west of the type section (Sweet et al, 1981).|
80377|Bowthorn Member|Depositional environment|Depositional setting is primarily that of a storm-dominated, shallow-marine shelf, with more coarse-grained units representing upper shoreface deposits (Sweet, 2017).|
80377|Bowthorn Member|Relationships and boundaries|The base of the Bowthorn Member is placed at the base of the first substantial siltstone interbed in the Constance Sandstone, with the sandstone succession below this horizon assigned to the Schultz Sandstone Member. The Bowthorn Member constitutes approximately half of the overall Constance Sandstone succession. The top of the Bowthorn Member (and therefore the top of the Constance Sandstone) is located at the top of the uppermost siltstone in the section. The contact with the overlying Elizabeth Formation is typically represented by an angular unconformity, with discordance visible in many areas (Sweet, 2017).|
80377|Bowthorn Member|Identifying features|The unit upper contact with the Elizabeth Formation is marked by an angular unconformity.|
80377|Bowthorn Member|Age reasons|Maximum depositional ages derived from U-Pb SHRIMP dating of detrital zircons: Bukalara Sandstone (stratigraphically overlies Bowthorn Member): GA sample 2777481 - 1316 +/- 27 Ma (Kositcin et al, 2020). Constance Sandstone: GA sample 2678595 - 1591 +/- 18 Ma (Anderson et al, 2019). Constance Sandstone: GA sample 1987412 - 1599 +/- 19 Ma (Anderson et al, 2019). Constance Sandstone: GA sample 2678593 - 1578 +/- 53 Ma (Anderson et al, 2019). Constance Sandstone: GA sample 2678591- 1569 +/- 37 Ma (Anderson et al, 2019). Constance Sandstone: GA sample 2678383 - 1468 +/- 36 Ma (Kositcin et al, 2020). Schultz Sandstone Member (stratigraphically underlies Bowthorn Member): GA Sample 1990594 - 1577 +/- 21 Ma (Carson et al, 2011).
Therefore, the potential depositional age range for the Bowthorn Member can be considered to extend from ca. 1578 +/- 53 Ma to 1316 ± 27 Ma.|
80377|Bowthorn Member|Correlations|The Bowthorn Member of the Constance Sandstone has been correlated with the upper sections of the Mittiebah Sandstone in the MOUNT DRUMMOND 1:250 000 mapsheet by Rawlings et al (2006, 2008). This correlation is supported by similar maximum depositional age estimates acquired for the Constance Sandstone and the Mittiebah Sandstone (Anderson et al, 2019). Based on U-Pb SHRIMP maximum depositional age estimates for the Constance Sandstone (Anderson et al, 2019), the Bowthorn Member may be correlative with units of the Favenc package or possibly the overlying Wilton package (Rawlings, 1999) of the McArthur Basin.|
80377|Bowthorn Member|Geophysical Expression|Moderate to high magnetic response, likely due to the unit’s close proximity to sandstone formations in the South Nicholson Group, such as the Playford Sandstone, which display a moderate to high magnetic response due to "subtle magnetic layering" (Rawlings et al, 2008).|
80377|Bowthorn Member|Defn author|Elliot Foley, Jack Simmons, Ben Williams, Charles Verdel (Northern Territory Geological Survey), Chris Carson (Geoscience Australia). 31-MAY-2023.|
80377|Bowthorn Member|Comments|Note: All locations are based on the GDA94 geodetic datum. Standard series 1: 100 000 and 1: 250 000 mapsheet names are shown in uppercase.|
80377|Bowthorn Member|References|Anderson JR, Lewis CJ, Jarrett AJM, Carr LK, Henson P, Carson CJ, Southby C and Munson TJ, 2019. New SHRIMP U–Pb zircon ages from the South Nicholson Basin, Mount Isa Province and Georgina Basin, Northern Territory and Queensland. Geoscience Australia, Record 2019/10.
Carson CJ, Hutton LJ, Withnall IW, Perkins WG, Donchak PJT, Parsons A, Blake PR, Sweet IP, Neumann NL and Lambeck A, 2011. Summary of results: Joint GSQ-GA geochronology project Mount Isa region, 2009-2010. Geological Survey of Queensland, Record 2011/03.
Carson, C. J., Kositcin, N., Anderson, J. R., and Henson, P. A. in prep. A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia - insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences.
Kositcin N, Carson CJ, Anderson JR, Doublier MP and Murr J, 2020. Exploring for the Future – New SHRIMP geochronology constraints on the basin evolution of the South Nicholson region. Geoscience Australia, Record 2020/25.
Rawlings DJ, 1999. Stratigraphic resolution of a multiphase intracratonic basin system: the McArthur Basin, northern Australia. Australian Journal of Earth Sciences 46(5), 703–723.
Rawlings DJ, Sweet IP and Kruse PD, 2006. Mount Drummond, NT (Second Edition). 1:250 000 Geological Map, Sheet SE 53-12. Northern Territory Geological Survey, Darwin, Northern Territory.
Rawlings DJ, Sweet IP and Kruse PD, 2008. Mount Drummond, NT (Second Edition). 1:250 000 Geological Map Series Explanatory Notes, Sheet SE 53-12. Northern Territory Geological Survey, Darwin, Northern Territory.
Simmons JM, Williams B, Carson, C and Verdel C, 2023a. Mount Drummond, Northern Territory 1:250 000 Geological Map, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.
Simmons JM, Williams B, Carson, C and Verdel C, 2023b. Mount Drummond, Northern Territory 1:250 000 Geological Map Explanatory Notes, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.  **Slater PJ and Mond A, 1980. Constance Range region, Queensland (Preliminary Edition). 1:100 000 geological map series, portion of 6560, 6561. Bureau of Mineral Resources, Canberra.  **Smith JW and Roberts HG, 1963a. Mount Drummond, NT (First Edition). 1:250 000 Geological Map Series Explanatory Notes, Sheet 53-12. Bureau of Mineral Resources, Canberra.  **Smith JW and Roberts HG, 1963b. Mount Drummond, NT (First Edition). 1:250 000 Geological Map Series, Sheet SE 53-12. Bureau of Mineral Resources, Canberra.  **Sweet IP, 1981. Definitions of new stratigraphic units in the Seigal and Hedleys Creek 1:100 000 sheet areas, Northern Territory and Queensland. Bureau of Mineral Resources, Report 225.  **Sweet IP, 2017. The geology of the South Nicholson Group, northwest Queensland. Queensland Geological Record 2017/07.  **Sweet IP, Mitchell JE and Mock CM, 1981. Seigal, Northern Territory and Hedleys Creek, Queensland. 1:100 000 Geological Map Commentary. Bureau of Mineral Resources, Geology and Geophysics, Canberra.|
2445|Box Gully Formation|Name source|The Box Gully Formation is a name originally established by Campbell (1952) for a sequence of predominantly conglomerate and arenite in the vicinity of Box Gully, a tributary of Buaraba Creek. The name was formalised in Cranfield & others (1976).|16-MAY-23
2445|Box Gully Formation|Geomorphic expression|The formation occupies an area of 20km2, varying from steep rugged boulder strewn slopes to undulating hills between 200 and 400m above sea level.|16-MAY-23
2445|Box Gully Formation|Extent|The Box Gully Formation is mostly exposed around Buaraba Creek on ESK.  A small outcrop occurs on Buaraba Creek (South Branch) in the Mt Cross Inlier.  Three areas have been tentatively assigned to Box Gully Formation between Kipper and Well Station, north-west of Esk.|16-MAY-23
2445|Box Gully Formation|Thickness range|The Box Gully Formation is about 1200 m thick in the vicinity of Buaraba Creek.|16-MAY-23
2445|Box Gully Formation|Lithology|The formation consists predominantly of granule and pebble conglomerate and arenite with minor siltstone, shale and andesitic volcanics.  The conglomerate, which grades into arenite, consists of angular to sub-rounded pebbles of black and grey quartz, pink rhyolite, metamorphics, and arenite set in a sandy matrix.  The arenite is black to grey, even-grained and non-calcareous; fine-grained beds are carbonaceous in places.  Vesicular grey-green andesite and agglomerate is locally interbedded with the arenite and shale.|16-MAY-23
2445|Box Gully Formation|Depositional environment|The interbedded conglomerates and arenites point to a shallow shelf or perhaps a continental environment of deposition.|16-MAY-23
2445|Box Gully Formation|Relationships and boundaries|The unit conformably overlies the Biarraville Formation, and is conformably overlain by the Buaraba Mudstone.  In the vicinity of Buaraba Creek, the unit is intruded by Triassic feldspar porphyrite, quartz diorite, and diorite.  The "Champion Hills Diorite" and "Buaraba Granodiorite" and "South Buaraba Microdiorite" and unit PRg intrude the unit to the south of and within the main outcrop area.  In the north it is unconformably overlain by an outlier of Neara Volcanics near Well Station and the Woogaroo Subgroup unconformably overlies the unit to the west of Buaraba Creek and in the Mt Cross area.|16-MAY-23
2445|Box Gully Formation|Structure and Metamorphism|STRUCTURE::  In the vicinity of Buaraba creek the Box Gully Formation outcrops with a general north-east to south-west strike.  Within the zone of outcrop dips vary from 10 to 90 degrees and folding occurs about north-east trending axies.  Locally, fault blocks rotate the strike to a north-westerly trend (Hegarty, 1981).  In the Mt Cross area the unit dips at about 30 to 50 degrees to the north and north-east (Stegman, 1982).  Between Kipper and Well Station dips are variable due to more complex faulting and folding of the Permian units in the area.|16-MAY-23
2445|Box Gully Formation|Age reasons|In the absence of fossil evidence the formation is tentatively assigned the same age as the underlying Biarraville Formation, i. e. mid-Permian.|16-MAY-23
2445|Box Gully Formation|Correlations|There are no known correlatives in south-east Queensland.  The unit may be stratigraphically at about the same level as the Tamaree Formation in the Gympie area.|16-MAY-23
2445|Box Gully Formation|Geophysical Expression|GEOPHYSICAL EXPRESSION::  Magnetic response over the unit is variable.  In the vicinity of Buaraba Creek the magnetic response is probably influenced by underlying volcanics and intrusive rocks with a higher magnetic susceptibility.  On the K-Th-U (rgb) ternary radiometric image the response is mottled purple-pink tones.|16-MAY-23
2445|Box Gully Formation|References|CAMPBELL, K.S.W.,1952,The geology of the Cressbrook-Buaraba area,"University of Queensland.  Department of Geology Papers (New series), Regional Geology.CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.",1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional Geology.HEGARTY, R.A.,1981,Geology of the Buaraba District, Southeast Queensland, Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology.STEGMAN, C., 1982, The geology of the Mount Cross Area, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.|16-MAY-23
24760|Bracteata Mudstone|Name source|Bracteata Creek, which joins Dosey Creek at 7858-590400. The grid reference is based on the AGD66 datum.|16-MAY-23
24760|Bracteata Mudstone|Unit history|Previously mapped as part of the Broken River Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
24760|Bracteata Mudstone|Geomorphic expression|Forms recessive topography with generally poor outcrop.|16-MAY-23
24760|Bracteata Mudstone|Type section locality|About 40 m of mudstone, nodular limestone and calcareous arenite exposed at 7858-576388 in a small gully near the head of a tributary of Dosey Creek.  This is section SD198 sampled by Mawson & Talent (in press).   REFERENCE SECTIONS:  In Lomandra Creek between 7858-609398 (base) and 608402 (top), consisting of 175 m of mudstone and fine-grained sandstone.  This is part of section SD170 of Mawson & Talent (in press).  Also in the Broken River, between 7859-612441 (base) and 611441 (top), consisting of 45 m of mudstone and minor limestone.  See Withnall & others (1988, figures 28 and 30).|16-MAY-23
24760|Bracteata Mudstone|Description at type locality|The base is a narrow outcrop of Shield Creek Formation, and the top is overlain by Lomandra Limestone.|16-MAY-23
24760|Bracteata Mudstone|Extent|Intricately folded with other units of the Broken River Group, mainly south of the Broken River, from near Six Mile Dam at 7859-670473 to between Storm Dam at 7858-55437 and the head of Bull Creek at 7858-670400.|16-MAY-23
24760|Bracteata Mudstone|Thickness range|~40m.|16-MAY-23
24760|Bracteata Mudstone|Lithology|Grey to brown mudstone and lesser interbedded very fine to medium-grained calcareous lithofeldspathic sandstone, which becomes more dominant to the west and south.  Thin nodular and lenticular limestone beds crop out locally, particularly near the top.|16-MAY-23
24760|Bracteata Mudstone|Fossils|The unit is generally poorly fossiliferous, but locally contains plant fragments, bivalves, brachiopods, solitary corals, and lesser crinoid ossicles, ostracods, trilobites, small stromatoporoids, and conodonts.|16-MAY-23
24760|Bracteata Mudstone|Relationships and boundaries|The Bracteata Mudstone is the lowermost unit of the Wando Vale Subgroup of the Broken River Group in the Dosey-Broken River area.  It disconformably(?) overlies the Shield Creek Formation and is generally conformably overlain by the Lomandra Limestone.  Near Storm Dam, the latter lenses out, and the Bracteata Mudstone is conformably overlain by the Storm Hill Sandstone.|16-MAY-23
24760|Bracteata Mudstone|Age reasons|The conodonts indicate a late Emsian age (Mawson & Talent, in press).|16-MAY-23
24760|Bracteata Mudstone|References|*MAWSON, R., & TALENT, J.A., in press:  Late Emsian-Givetian stratigraphy and conodont biofacies - carbonate slope and offshore shoal to sheltered lagoon and nearshore carbonate ramp - Broken River, north Queensland.  Courier Forschungs-Institute Senckenburg.WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.    *WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of 	Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes.    *WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.    *WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
26294|Brae Formation|Name source|Brae Holding, Parish Blackman, County Dawson, central Queensland.|16-MAY-23
26294|Brae Formation|Unit history|Wass (1965) and subsequent authors included this sequence in the Buffel or Oxtrack Formations.|16-MAY-23
26294|Brae Formation|Type section locality|The type section is located normal to the strike 2 km NW of Cracow Station from the base of the unit on the western slope of Pindari Hills at grid reference 262917 Cracow 1:100 000 sheet 8947, to the junction with the overlying Oxtrack Formation just below an earth dam at GR 257918, consisting of 55 m of calcareous mudstone, 5 m of siltstone, 10 m no outcrop, 10 m of sandstone, 83 m of mudstone, 4 m of spicule rich bioturbated mudstone at the top.|16-MAY-23
26294|Brae Formation|Extent|The unit crops out as discontinuous patches in gullies and places of sheet erosion to the west of the Pindari Hills. It extends from SW of Cracow homestead northwards through Brae Holding to the west of Cracow where it is obscured by younger flat lying sediments. The unit crops out east of Theodore (GR 140392) and to the west of the Leichhardt Highway crossing at Lonesome Creek (GR 127525). Isolated occurrences lie to the north of Banana. The interval 163-213 m in GSQ drill hole Banana NS1 may represent the Brae Formation.|16-MAY-23
26294|Brae Formation|Thickness range|Approximately 160 m thick in type section and relatively uniform thickness throughout the mapped area.|16-MAY-23
26294|Brae Formation|Lithology|The unit consists of a characteristic green to buff coloured mudstone generally well bedded. A prominent horizon of calcareous concretions occurs approximately 25 m above the base of the unit.  Several sandstone horizons occur in the lower 50 m and are a few tens of centimetres thick and show intense bioturbation.|16-MAY-23
26294|Brae Formation|Fossils|Brachiopods, molluscs, bryozoans, corals, gastropods.|16-MAY-23
26294|Brae Formation|Relationships and boundaries|Conformably overlying Pindari Formation and unconformably overlain by the Oxtrack Formation.|16-MAY-23
26294|Brae Formation|Age reasons|The fauna includes Echinalosia, Lethamia, Terrakea, Cancrinella, Stenoscisma, Trigonotreta, Pustuloplica, Martiniopsis, Notospirifera and Spinomartinia and is upper Baigendzinian I.e. Krasnoufimian (Early Permian) in age.|16-MAY-23
26294|Brae Formation|References|98/29407|16-MAY-23
26294|Brae Formation|Proposer|Flood P.G., Jell J.S., Waterhouse J.B.|16-MAY-23
2534|Brick Kiln Member|Name source|From attempted brick making on the area of Fireclay Mining Lease 196 (1909-1912) which covered part of the subcrop of the Brick Kiln Member. Location about 302,200E 7,383,000N Gladstone 1:100 000 topographic sheet.|16-MAY-23
2534|Brick Kiln Member|Unit history|Part of The Narrows Beds (Kirkegaard et al, 1970) and part of the Rundle Formation (Henstridge and Missen, 1982).|16-MAY-23
2534|Brick Kiln Member|Type section locality|123 m of oil shale with minor interbeds of claystone, rare carbonaceous shale and occasional impersistent dolomite; from 143.3 to 266.3 m in drill hole ERD 169 (GR 300,999E, 7,380,998N, Gladstone 1:100 000 topographic sheet). The dark yellowish-brown to olive-brown oil shale contains two major greyish-green claystone beds (from 174.4 to 176.5 m and 248.8 to 252.7 m in type section) and a persistent dark grey carbonaceous shale layer towards the top of the member (from 154.5 to 155.0 m in type section). Minor moderately thick to thick claystone to clayey oil shale beds also occur from 194.2 to 195.0 m, 227.0 to 227.5 m and 244.2 to 245.7 m in type section. A distinctive very thick olive grey, poorly laminated oil shale bed occurs towards the middle of the member (from 205.0 to 208.0 m in type section). Cyclicity of lithologies is a feature with oil shale grading upwards through clayey oil shale to claystone, commonly overlain by carbonaceous material. The unit is calcareous but there is a marked decrease in carbonate (fossil content) towards the top, with an associated increase in the amount of coaly material.|16-MAY-23
2534|Brick Kiln Member|Extent|Subcrops in an area of about 55 km2 in The Narrows Graben, NW of Gladstone, Queensland. Sparse, weathered outcrops (particularly adjacent to The Narrows channel and exposed in the mudflats at grid reference 300,750E 7,384,250N) are recorded. The member has been identified from drill hole core.|16-MAY-23
2534|Brick Kiln Member|Thickness range|123 m (estimated true thickness 121.1 m corrected for an apparent dip of 9o in ERD 169) in type section. Range of true thickness of the member as intersected in drill holes is 52.5 to 148 m.|16-MAY-23
2534|Brick Kiln Member|Lithology|Oil shale, dark yellowish-brown to olive-brown; well laminated to poorly laminated, brecciated and peloidal in part; very thinly to very thickly bedded (up to 3 m); calcareous, clayey and carbonaceous cyclicity. Minor interbeds of greyish-green claystone; rare very dark grey carbonaceous shale and occasional discontinuous yellowish-grey impure dolomite concentrations. Dolomite concentrations tend to thicken and are in greater abundance to the east and northwest in The Narrows Graben. Claystone beds also thicken and contain more silt and sand along the eastern margin. Claystone and brecciated clayey oil shale beds often show bioturbation features. Ostracode tests are abundant with minor gastropods, vertebrate remains (crocodile, turtle), fish elements and coprolites. There are abundant plant remains within the persistent upper carbonaceous layer.|16-MAY-23
2534|Brick Kiln Member|Relationships and boundaries|The member is conformable with the underlying Ramsay Crossing Member and is the contact between oil shale and claystone. The upper boundary is conformable with the Humpy Creek Member and is the sharp contact between oil shale and carbonaceous shale. The member is faulted against Devonian to Carboniferous rocks of the Curtis Island Group along the western edge of The Narrows Graben.|16-MAY-23
2534|Brick Kiln Member|Age reasons|Mid to late Eocene - as for the Rundle Formation.|16-MAY-23
2534|Brick Kiln Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
2534|Brick Kiln Member|Comments|Note: Drill-core from ERD 169 is stored at Southern Pacific Petroleum's Research and Core Storage Facility located in Gladstone, Queensland.|16-MAY-23
2534|Brick Kiln Member|References|79/02402; +;|16-MAY-23
28306|Broken River Group|Name source|Broken River which joins the Clarke River at 7858-804392.  The grid reference is based on the AGD66 datum.|16-MAY-23
28306|Broken River Group|Unit history|Previously the Broken River Formation (White, 1959, 1962, 1965); raised to group status by Withnall & others (1988).|16-MAY-23
28306|Broken River Group|Constituents|Dosey-Broken River  area: Mytton Formation (including Stanley Limestone Member), Papilio Mudstone (including  Spanner Limestone Member), Dosey Limestone, Storm Hill Sandstone,Lomandra Limestone, Bracteata Mudstone.    Gorge Creek-Diggers Creek area: Mytton Formation, Papilio Mudstone, Burges Formation.    Jessey Springs area : Mytton Formation, Burges Formation, Jessey Springs Limestone.  Dip Creek area::  Mytton Formation, Papilio Mudstone, Dip Creek Limestone, Tank Creek Sandstone.   Lockup Well area :	Lockup Well Limestone.  Pandanus Creek area: Mytton Formation, Chinaman Creek Limestone, Tank Creek Sandstone.   All units, with the exception of the Mytton Formation, comprise the Wando Vale Subgroup.|16-MAY-23
28306|Broken River Group|Extent|A sinuous folded belt up to 6 km wide extending from near 'Pandanus Creek' in the north, extending for about 50 km to 'Dosey' and the Clarke River in the south|16-MAY-23
28306|Broken River Group|Thickness range|Up to 2000 m.|16-MAY-23
28306|Broken River Group|Lithology|Limestone, mudstone, labile to quartzose sandstone, and polymictic conglomerate.|16-MAY-23
28306|Broken River Group|Fossils|The limestones and mudstone units contain rich shallow marine faunas including corals and stromatoporoids, as well as brachiopods, bivalves, gastropods, nautiloids, crinoids, trilobites, bryozoa, ostracods, fish, and conodonts, and algal and vascular plants.|16-MAY-23
28306|Broken River Group|Relationships and boundaries|The Group generally overlies the Shield Creek Formation, which consists of feldspathic arenite, with possible disconformity.  West of the Six Mile Syncline, the Shield Creek Formation is difficult to recognise, and the Broken River Group may lie directly on the Graveyard Creek Group.  Further west it is faulted against the Silurian Dido Tonalite of the Georgetown Province.  In the Dosey area, northwest of Storm Hill, the Broken River Group (Storm Hill Sandstone) unconformably overlies the Judea Formation.  In the southwest, near 'Gregory Springs', the Broken River Group unconformably overlies granitoids and metamorphic rocks of the Georgetown Province.   The Group is overlain by the Bundock Creek Group with slight angular unconformity to disconformity.  The boundary is generally marked by polymictic, pebble to cobble conglomerate overlain by redbeds.|16-MAY-23
28306|Broken River Group|Age reasons|Studies of the corals (Hill in White, 1965; Jell, 1967; Jell in Wyatt & Jell, 1967) and conodonts (Telford, 1975; Mawson, 1987; Mawson & others, 1985; Mawson & Talent, in press and unpublished data) indicate that the Group ranges from Emsian to early Frasnian in age.  See also the summary in Withnall & others (1988).|16-MAY-23
28306|Broken River Group|References|*JELL, J.S., 1967:  Geology and Devonian rugose corals of Pandanus Creek, north Queensland.  Ph.D. Thesis, University of Queensland (unpublished)    *MAWSON, R., 1987:  Documentation of conodont assemblages across the Early Devonian-Middle Devonian boundary, Broken River, north Queensland, Australia.  Courier Forschungs-Institut Senckenburg, 92, 251-273.   *MAWSON R., JELL, J.S., & TALENT, J.A., 1985:  Stage boundaries within the Devonian:  implications for application to Australian sequences.  Courier Forschungs-Institut Senckenburg, 75, 1-16.  *MAWSON, R., & TALENT, J.A., in press:  Late Emsian-Givetian stratigraphy and conodont biofacies - carbonate slope and offshore shoal to sheltered lagoon and nearshore carbonate ramp - Broken River, north Queensland.  Courier Forschungs-Institute Senckenburg.    *WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.    *WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of 	Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes.    *WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.    *WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.    *WYATT, D.H. & JELL, J.S., 1967:  Devonian of the Townsville 	hinterland, Queensland, Australia; in Oswald, D.H. (editor), International Symposium on the Devonian System, Volume 2.  Alberta Society of Petroleum Geologists, Calgary, 99-105.|16-MAY-23
24198|Bronco Stromatolith Bed|Name source|The Bed is named after Bronco Waterhole, a waterhole on Brumby Creek located 15 km SSW of Thorntonia Station at latitude 19o37'S, longitude 138o52'E or grid reference 764288 on the Undilla 1:100 000 topographic sheet.|16-MAY-23
24198|Bronco Stromatolith Bed|Type section locality|The type locality is situated on the northern side of the toe of a prominent east-west ridge of terraced limestone, grid reference 813368 on the Undilla 1:100 000 topographic sheet. The locality occurs beneath the base of the type section for the Gowers Formation which is situated at a small tree-covered sinkhole located some 300 m due west of the SSW-SW kink in the access track that follows the fence SSW from Gowers Bore.|16-MAY-23
24198|Bronco Stromatolith Bed|Extent|The Bed crops out to the south of Thorntonia Station as a prominent limonite-stained horizon on the uppermost terrace of the Thorntonia Limestone. Its southernmost outcrop is found to the S.W. of D-Tree Bore, a distance of 27 kms from Thorntonia Station. West of Thorntonia Station where outcrop is subdued the Bed outcrops discontinuously on rubble strewn slopes.|16-MAY-23
24198|Bronco Stromatolith Bed|Thickness range|The Bed forms a laterally persistent horizon of flat and domal laminated stratiform stromatolites that vary from 1-30 cm in thickness|16-MAY-23
24198|Bronco Stromatolith Bed|Lithology|At the type locality the Bed forms a 15 cm thick interval of limonite-stained flat and domal laminated stratiform stromatolites. The principal Lithologies are dolostone and limonitic dolostone, with subordinate phosphate coquinas, packstones and phoscrete crusts. Oncolites occur locally.|16-MAY-23
24198|Bronco Stromatolith Bed|Relationships and boundaries|The Bronco Stromatolith Bed drapes over an irregular erosion surface developed on phosphatic dolostones and dolostones of the Thorntonia Limestone. The Bed forms the uppermost unit of the Thorntonia Limestone. The upper surface of the Bronco Stromatolith Bed and therefore the Thorntonia Limestone is a disconformity.|16-MAY-23
24198|Bronco Stromatolith Bed|Age reasons|Fauna from the Stromatolith Bed at its type locality has been examined by Shergold and Laurie in Shergold and Southgate (1986). This work indicates that the Bronco Stromatolith Bed is of Ordian age.|16-MAY-23
24198|Bronco Stromatolith Bed|Defn approved by|Queensland Sub-Committee|16-MAY-23
29857|Brookdale Granite|Name source|Brookdale homestead at GR 348299 approximately 1.5km NE of Pentland in the Pentland 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
29857|Brookdale Granite|Unit history|This unit was included in the Ravenswood Granodiorite Complex by Paine & others (1971) as granite phase ODa.|16-MAY-23
29857|Brookdale Granite|Type section locality|A road cutting along the Flinders Highway at GR 359316 where a grey to pink, strongly foliated biotite granitoid crops out.  The grid reference is based on the ASGD66 datum.|16-MAY-23
29857|Brookdale Granite|Extent|The Brookdale Granite crops out as an elongate northwest-trending body covering approximately 17km2 from north of Brookdale homestead to near the junction of Sapling Creek and Betts Creek (east of Brookdale homestead).|16-MAY-23
29857|Brookdale Granite|Lithology|The Brookdale Granite is a grey to pink equigranular fine grained biotite granite, with hornblende locally. A strong foliation is commonly defined by biotite and locally hornblende. A crude mineral banding can be recognised in some outcrops. The foliation dips southwest at moderate to steep angles consistent with the regional trend. Paine & others (1971) report almost horizontal foliation within this unit near Pentland. At GR 381328 (a road cut in the Flinders Highway) the foliation is defined by alignment of hornblende crystals. Rare pyrite grains up to 0.5 cm wide are present in some outcrops. A blocky fracture/jointing pattern is common with the unit forming low recessive landforms.  The grid reference is based on the AGD66 datum.|16-MAY-23
29857|Brookdale Granite|Relationships and boundaries|The Brookdale Granite intrudes the Cape River Metamorphics and Fat Hen Creek Complex. It is intruded by andesitic dykes and overlain along its northern and southern margins by extensive Tertiary-Quaternary cover.|16-MAY-23
29857|Brookdale Granite|Age reasons|The age of the Brookdale Granite is uncertain but a Middle Ordovician age is assigned due to its similarity with foliated granites of the Ravenswood Batholith (Hutton & others, 1994).|16-MAY-23
29857|Brookdale Granite|Comments|MAGNETIC SUSCEPTIBILITY:  Magnetic susceptibility within the unit is 0-496 x 10[superscript]-5 SI units. Two populations appear to be present in most localities, those at or near zero and those in the range 120-500 x 10[superscript]-5 SI units.|16-MAY-23
29857|Brookdale Granite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
39025|Buaraba Granodiorite|Name source|Campbell (1952) informally called the unit the 'Buaraba Quartz Diorite'.  Later investigations suggest that there is a higher proportion of granodiorite and tonalite than diorite, and the name has been changed to Buaraba Granodiorite.|16-MAY-23
39025|Buaraba Granodiorite|Unit history|This unit was first mapped and informally called the 'Buaraba Quartz Diorite' by Campbell (1952).  Other workers who studied the unit were Houtgraaf (1974), Vonhoff (1975), Costello (1975), and Tudor (1985) from the University of Southern Queensland and Hegarty (1981), McCabe (1982), Early (1984), Irvine (1987) and Slijderink 1988 from the Queensland University of Technology.Campbell informally called the unit the 'Buaraba Quartz Diorite'.  Campbell's mapping was accepted in the production of the Ipswich 1:250 00 map (Cranfield and Schwarzbock, 1973).  Because of contact and intrusive relationships the Buaraba Granodiorite was considered to be younger than the South Buaraba Microdiorite and the Champion Hills Diorite.  Work by later authors has agreed with this, but the rock type was generally considered to be more in the granodiorite to tonalite range, with diorite occurring as a more minor phase.|16-MAY-23
39025|Buaraba Granodiorite|Geomorphic expression|The Buaraba Granodiorite generally has a relatively low topographic expression with creek flats and rolling hills from 140 to 200m in the main body, with an associated sandy soil.  It is generally well cleared with sparse outcrop and is covered by regolith and alluvium near the creeks and larger gullies.  Topography in the western area around the South Buaraba Microdiorite is up to 520m, is steep and is influenced by the surrounding country rocks.  In this area Tudor (1985) notes the Buaraba Granodiorite occurs as boulders up to 3m in diameter and as rubbly outcrop, with poor exposure and hidden contacts.|16-MAY-23
39025|Buaraba Granodiorite|Type section locality|The type area is designated as north of Buaraba Creek around AMG 429600 6974200.  The grid reference is based on the AGD66 datum.|16-MAY-23
39025|Buaraba Granodiorite|Extent|The outcrop occupies about 8 km2 mostly on the north bank of Buaraba Creek and also forms a possible ring dyke structure around the South Buaraba Microdiorite which occurs to the west of the main body of Buaraba Granodiorite.|16-MAY-23
39025|Buaraba Granodiorite|Lithology|Costello (1975) described the main body along Buaraba Creek as being mostly a grey, even textured, medium to coarse-grained granodiorite containing zoned and twinned plagioclase, quartz, orthoclase, hornblende (green), biotite, and minor magnetite and with minor occurrences of leucogranodiorite.  The leucogranodiorite was described as even-textured, medium to coarse-grained, pink-grey in colour, in hand specimen, and containing mainly plagioclase, with a strong core rim difference in composition and with oscillatory and patchy zoning, and albite twinning.  Quartz has undulose extinction, orthoclase with carlsbad twinning, and other constituents in thin section include hornblende (green), biotite (brown) and minor magnetite.  Campbell (1952) described the leucogranodiorite as a greyish rock sometimes with a pinkish tint holocrystalline, medium grained and even textured.  Quartz is always abundant and hornblende is predominantly green but varies to the dark brown (basaltic) variety.  Biotite is less abundant than hornblende and chlorite is a common secondary mineral.  Orthoclase is present in small amounts.  Apatite, zircon and magnetite occur as accessories.  Campbell (1952) considered the main rock type to be quartz diorite.  McPhee (1974) noted that the less mafic leucogranodiorite parts tended to be pinker and that there are a numerous minor intrusions including diorite, microdiorite, and porphyrite dykes.  Houtgraaf (1974) commented that microdiorite occurs as small isolated bodies generally along the chilled margins of the granodiorite.  Tudor (1985) described the ring shaped portion of the body, around the `South Buaraba Microdiorite¿ as a tonalite.  He described it as medium to coarse grained, massive, and even textured, containing plagioclase, quartz, biotite and hornblende, in hand specimen and as containing 30-55% plagioclase, 22-54% quartz, 5-10% hornblende, 5-8% biotite, 0-10% chlorite, with accessory magnetite, zircon, apatite, and epidote in thin section.|16-MAY-23
39025|Buaraba Granodiorite|Relationships and boundaries|The Buaraba Granodiorite intrudes South Buaraba Microdiorite, Champion Hills Diorite and units of the Cressbrook Creek Group, and is overlain by Woogaroo Sub Group.|16-MAY-23
39025|Buaraba Granodiorite|Age reasons|A K/Ar radiometric age was initally reported as 187 +/- 7Ma and interpreted as minimum age due to possible argon loss by Cranfield &others (1976).  The currently used age is 237.9 +/- 7my Holcombe, pers comm, 1999.  An early to mid Triassic age has been assigned to the unit.|16-MAY-23
39025|Buaraba Granodiorite|Comments|GEOPHYSICAL EXPRESSION:: The Buaraba Granodiorite has a variable intermediate magnetic response and a mottled pinkisk and blueish radiometric response on the K-Th-U radiometric image.  Neither response is distinctive.ASSOCIATED MINERALISATION:: Vonhoff (1975) reported molybdenite occurring as thin veins in a piece of float of fractured granodiorite.  A location was not given but it appears to be related to Buaraba Granodiorite on the north-west side of the South Buaraba Microdiorite.Houtgraaf (1974) noted minor cubic pyrite along the granodiorite sediment contact to the Cressbrook Creek Group.|16-MAY-23
39025|Buaraba Granodiorite|References|CAMPBELL, K.S.W.,1952,The geology of the Cressbrook-Buaraba area,"University of Queensland.  Department of Geology Papers (New series), Regional Geology.COSTELLO, C.M.1975,The geology of part of the Buaraba Creek area, north of Gatton, South-East Queensland. Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.CRANFIELD, L.C. & SCHWARZBOCK, H., 1973, Ipswich 1:250 000 Geological Map,Queensland Department of Mines.CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.",1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional Geology.IRVINE,1987....................HEGARTY, R.A.,1981,Geology of the Buaraba District, Southeast Queensland, Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology.HOUTEGRAFF, M.J., 1974,The geology of east of the north- and south branch Buaraba Creeks South Eastern Queensland. Unpublished Thesis, Department of Geology, Darling Downs Institute of Advanced Education.McCABE, S.,1982, Geology of the South Bauraba District, South-East Queensland, Unpublished honours thesis, Department of Geology, Queensland University of Technology.MCPHIE, K.A., 1974,The geology of the Verandah-Middle Creek area, Buaraba district, southeast Queensland, Unpublished Thesis, Department of Geology, Darling Downs Institute of Advanced Education.SLIDJERINK, P.,1988, Geology of the Buaraba Creek-North Branch project area, Unpublished Bsc honours thesis, Department of Geology, Queensland University of Technology.VONHOFF, J.D.,1975, The geology of the North and South Branch Buaraba Creeks, South Eastern Queensland, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.|16-MAY-23
26428|Buaraba Mudstone|Name source|Outcropping to the south of Buaraba Creek.|16-MAY-23
26428|Buaraba Mudstone|Unit history|Campbell (1952) erected this name for a mudstone sequence with minor interbedded arenite and conglomerate cropping out to the south of Buaraba Creek.  The sequence in GSQ Ipswich 19-22R consists of a uniform dark grey mudstone with conspicuous jointing and calcareous veining. Allen (1972) referred to this sequence as Buaraba Mudstone based on its lithology and spore age.|16-MAY-23
26428|Buaraba Mudstone|Geomorphic expression|The unit forms low undulating hills from 120 to 240 m above sea level in the vicinity of Buaraba Creek, and occupies the creek bed and lower slopes in the Alice Creek and Paradise Creek areas up to 280 m.  In the Mt Cross area the Buaraba Mudstone forms hilly country 400 to 500m above sea level .|16-MAY-23
26428|Buaraba Mudstone|Extent|The unit crops out over an area of 8 km2 in the vicinity of Buaraba Creek, 2 km2 in the north of the Mt Cross area, 3 km2 in the Alice Creek area and, 2 km2 in the Paradise Creek area.|16-MAY-23
26428|Buaraba Mudstone|Thickness range|The maximum thickness of the unit is unknown due to onlap by the Woogaroo Subgroup; about 1200 m were suggested as the thickness of exposure in the type section by Cranfield & others (1976).|16-MAY-23
26428|Buaraba Mudstone|Lithology|South of Buaraba Creek the predominant rock type is mudstone which is black or brown, in part carbonaceous, and usually massive. In places it is rhythmically interbedded with arenite. Minor conglomerate bands similar to those of the underlying Box Gully Formation, and vesicular andesite also occur in some parts of the unit. Allison (1992) found burrows in mudstone and plant fragments at several localities.  In the Mt Cross, Paradise Creek and Alice Creek areas fine grained sediments are probably either correlative with the Buaraba Mudstone south of Buaraba Creek, or form part of that unit.  In the Paradise Creek area, Skerman (1973) described green-grey to dark grey mudstone, siltstone, interbedded tuff, a porphyritic andesite, andesitic breccia, and minor chert.  Pan continental (ATP 3820M) mapping of the area suggests that there are more volcaniclastic sediments (including some rhyolitic and andesitic tuffs) in the sequence than suggested by Skerman.  In the Alice Creek area mapping by Pan Continental (ATP 3820M, GR16596) shows similar rock types to those in Paradise Creek.  The majority of the Alice Creek area consists of light grey to dark grey tuffaceous siltstones, arenaceous volcaniclastics and tuff and fine grained volcanic-derived sediments.  Grey to dark grey siltstone is also present, but is much less than in the Paradise Creek section.   Andesitic volcanics occur in Paradise Creek at AMG 413500 6963600 and in a tributary at AMG 412200 6964600. In Alice Creek, a porphyritic andesite flow occurs at AMG 415000 6961150.  This andesitic flow may be a correlative of the andesitic volcanic marker identified by Campbell (1952) in the Buaraba Mudstone south of Buaraba Creek.  To the south of the andesitic volcanics in the Paradise Creek inlier, marine fossils occur at four localities and either form two separate marker beds or a single marker beds repeated by folding.  In the Alice Creek area marine fossils have been located in a similar stratigraphic position relative to an andesite.  In the Buaraba Mudstone south of Buaraba Creek worm burrows were identified in a similar stratigraphic position relative to an andesite horizon described by Campbell (1952).|16-MAY-23
26428|Buaraba Mudstone|Depositional environment|The presence of crinoids, fenestella and worm burrows in at least one marker bed in the Buaraba Mudstone indicates marine shallow water ?shelfal deposition.  Carbonaceous matter in the mudstone is indicative of nearby terrestrial depositional environment.|16-MAY-23
26428|Buaraba Mudstone|Relationships and boundaries|The unit conformably overlies the Box Gully Formation in the vicinity of Buaraba Creek and is unconformably overlain by the Woogaroo Subgroup.  The formation is intruded by Triassic "Champion Hills Diorite" and "Buaraba Granodiorite", and is overlain by Triassic rhyolite in the vicinity of Buaraba Creek.  Buaraba Mudstone in the northern part of the Mt Cross inlier is faulted with serpentinite, dioritic and rhyolitic intrusions infilling faults (Ross 1986).  The unit has a faulted contact with gabbro of the Mt Cross Igneous Complex to the south.  Porphyritic andesite dykes intrude the Alice Creek area.  Skerman (1973) considered that the Buaraba Formation conformably overlies Hampton Road Rhyolite in the Paradise Creek area, with the contact being gradational.  Interpretation of the regional geology suggests that an extension of faulting from the east, near Mt Cross, should be found at or near the contact.  The contact with Hampton Road Rhyolite in Paradise Creek has therefore been interpreted as faulted.|16-MAY-23
26428|Buaraba Mudstone|Structure and Metamorphism|South of Buaraba Creek rocks from the unit dip generally between 300 and 600 on the southern flank of a broad south-east plunging anticline.  In the east, to the south of Verandah Creek, dips of between 40 to 90 degrees indicate localised folding and possible faulting with a north-east trend (Hegarty 1982, Irvine 1987).  In the Mt Cross area steep southerly dips occur in siltstones with minor conglomerate interbeds.  East-west faulting disrupts bedding.  Rhyolites diorites and serpentinites have been intruded along these faults.  Magnetometer surveys across the serpentinite indicate steep southerly to vertical dips (Smith 1974, Stegman 1981). In the Alice Creek area dips generally vary between 20 and 50 degees towards the south and south-east.  In the Paradise Creek area in the north, dips are between 60 and 90 degrees towards the south-south-west, decreasing towards the south.  Skerman (1973) identified open folding, with fold axes trending about 320 degrees, south of the andesitic volcanics.  In GSQ Ipswich 19-22R Gray (1975) tentatively identified bedding dips of 30 to 40 degrees.|16-MAY-23
26428|Buaraba Mudstone|Age reasons|The Buaraba Mudstone was assigned a mid-Permian age by Cranfield & others (1976).  De Jersey (1973) identified Permian miospores in shale samples from 766 and 854 m in GSQ Ipswich 19-22R.  This unit is probably either correlative with the Buaraba Mudstone, or forms part of that unit. In the Paradise Creek area Skerman (1973) found worm burrows and crinoids at AMG 412100 6964150, crinoids at AMG 412550 6963400 in siltstones and fenestella and crinoids at AMG 413150 6963450 in fissile mudstone (location accuracy 150m).  Lindsay (1986) collected a crinoidal mudstone sample from AMG 412200 6965100.  Allison (1992) found burrows and plant fragments in mudstone at several localities, and located a Conularia fossil at AMG 428650 6970170 south of Buaraba Creek.  Ross (1986) identified bioturbation and worm burrows in a siltstone at AMG 419300 6964400, on Alice Creek north of Mt Cross.  In the Alice Creek area Missen (1975) located marine fossils and wood fragments at AMG 414300 6960200.  These were later described by McClung (1977) as Brachipodea - Terrakea elongata?, Bryozoa - Denmeadopora? sp., and  Gastropoda - Mourlonopsis strzeleckianan.  Gibson (1975) located marine fossils in the Buaraba Mudstone in the Mt Cross area at AMG 421200 6964300.  These were described by McClung (1977) as Bivalvia - Aviculopecten sp. indet., Bryozoa - Denmeadopora? sp., Coelenterata -Thamnopora sp. and several types of crinoid columnals, including large eliptical forms whose maximum diameter is greater than 10 mm.  McClung assigned a probable Late Permian age to the fossils.  The Buaraba Mudstone has been assigned a Late Permian age on fossil evidence.|16-MAY-23
26428|Buaraba Mudstone|Correlations|The Buaraba Mudstone has no known correlatives.  It may be the unit outlined by Allen (1972) at the base of GSQ Ipswich 19-22R near Toowoomba.  It may also be younger than units near Gympie.|16-MAY-23
26428|Buaraba Mudstone|Geophysical Expression|The unit generally has a low magnetic response in the vicinity of Mt Cross, Paradise Creek and Alice Creek and occurs as light tones on the K-Th-U (rgb) ternary radiometric image where outcrop is extensive enough to not be masked by the surrounding Woogaroo Sub Group response.  South of Buaraba Creek the magnetic response is influenced by a broad intermediate response probably from underlying more highly magnetic intrusive rocks.|16-MAY-23
26428|Buaraba Mudstone|References|*ALLEN, R.J.,1972, Petroleum stratigraphic core-drilling on the Ipswich 1:250 000 Sheet area, 1968-71.Queensland Government Mining Journal, 73, 453-456.    *ALLISON, C.,1992,Geology to the south of Buarba Creek, between Box Gully Creek and Kavanaghs, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.    *CAMPBELL, K.S.W.,1952,The geology of the Cressbrook-Buaraba area,"University of Queensland.  Department of Geology Papers (New series), Regional Geology.    *HEGARTY, R.A.,1981,Geology of the Buaraba District, Southeast Queensland, Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology.    *LINDSAY, P.,1986,The geology of the Racecourse Creek Palm Tree area of south-east Queensland, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education. Mount Cross Igneous Complex, Esk.      *MISSEN, D.D.,1975, The geology of the Alice Creek - Mount Cross area, South-east Queensland, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.    *ROSS, C.J.,1986,The sediments of Mt. Cross, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.    *ROSS, L.A. 1988,An investigation of the geology and fault relations of the Western Border Fault of the south western Esk Trough, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.    *SKERMAN,W.R.,1973, The geology of the Paradise Creek -Racecourse Creek area, south eastern Queensland, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.    *SMITH,P.E.,1974,The Geology of the Mount Cross Area, Parish of Murphy, South Eastern Queensland, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.|16-MAY-23
2809|Buddawadda Basalt Member|Name source|From Buddawadda Swamp, a circular lagoon about 1 km across, 1.5 km north of the Nicholson River, at grid reference 103224, in the Hedleys Creek 1:100 000 sheet area.|16-MAY-23
2809|Buddawadda Basalt Member|Type section locality|Along the banks and bed of Wire Creek, from the base at grid reference 916366 to the top at 935342, in the Hedleys Creek sheet area.|16-MAY-23
2809|Buddawadda Basalt Member|Extent|In an east-northeast-trending arcuate belt up to 3 km wide, across the central part of the Hedleys Creek 1:100 000 Sheet area, Queensland. Several isolated outcrops occur adjacent to a fault zone in the southern Seigal sheet area.|16-MAY-23
2809|Buddawadda Basalt Member|Thickness range|Up to 600 m.|16-MAY-23
2809|Buddawadda Basalt Member|Lithology|Numerous thin basalt flows, many of them vesicular and amygdaloidal, and some with brecciated tops. Many flows are capped by thin siltstone interbeds. At least 2 thicker flows occur - they are porphyritic, non-vesicular, and less weathered than the thin flows. A fine-grained sandstone bed occurs near the top of the Member.|16-MAY-23
2809|Buddawadda Basalt Member|Relationships and boundaries|Forms basal part of Peters Creek Volcanics. Sharp contact with underlying Wire Creek Sandstone, but no evidence of unconformity. Similarly sharp contact with overlying lavas, which are predominantly rhyodacite. Contact recognised by abrupt change from basic to acid volcanics, but no evidence of erosion or unconformity.|16-MAY-23
2809|Buddawadda Basalt Member|Identifying features|Name of host formation: Peters Creek Volcanics, described and defined by Carter, Brooks & Walker (1961).|16-MAY-23
2809|Buddawadda Basalt Member|Age reasons|Proterozoic-Carpentarian. Correlated with the Seigal Volcanics, which form part of the strato-type of the Carpentarian System.|16-MAY-23
2809|Buddawadda Basalt Member|Proposed publication|BMR Report on geology of the Hedleys Creek 1:100 000 Sheet area.|16-MAY-23
2809|Buddawadda Basalt Member|References|B051|16-MAY-23
2809|Buddawadda Basalt Member|Defn approved by|Queensland Sub-Committee|16-MAY-23
27076|Buffel Formation|Name source|Buffel Hill (grid reference 268906, Cracow 1:100 000 Sheet 8947) 1 km west of Cracow homestead.|16-MAY-23
27076|Buffel Formation|Unit history|Wass (1965) defined the Buffel Formation to include the calcareous sequence described above but also included the overlying strata now referred to the Pindari and Brae Formations.  Wass (1965) provided a summary of the synonymy to that date and subsequent workers have accepted the definition of Wass such as Mollan et al. (1972), Dickins and Malone (1973), Whitaker et al. (1974), and Gray and Haywood (1978).|16-MAY-23
27076|Buffel Formation|Type section locality|(Holostratotype): As defined by Wass (1965) "Buffel Hill west to 32018441" (GR refers to Mundubbera 1:253 440 military map), the type section is located on Camboon Andesite, over the crest and southwestwards down the western slope (GR 265905) where again it passes into Camboon Andesite on the other limb of the fold. The type section is predominantly limestone (middle limestone member) and Wass estimated the thickness as 640 feet.  (The sequence is not complete and is repeated, no estimate of the true thickness in the section is attempted).|16-MAY-23
27076|Buffel Formation|Description at type locality|Reference Section (Hypostratotype): The section from GR 270900 on the southeastern slope to GR 265900 on the southwestern slope includes 45 m of calcareous sandstone, 30 m of limestone, and 55 m of siltstone and is considered to be complete. The upper siltstone member does not occur in the type section.|16-MAY-23
27076|Buffel Formation|Extent|In the Cracow homestead area, this unit occurs along the eastern and western limbs of a doubly plunging syncline whose main fold axis is orientated NNE-SSW. Parts of the unit are also exposed on the eastern side of Pindari Hills and south of these Hills towards Cracow Creek. It has previously been recorded over a distance of almost 100 km from south of Cracow homestead to Mt Brest in the north.|16-MAY-23
27076|Buffel Formation|Thickness range|This unit is of the order of 130 m thick in the hypostratotype.|16-MAY-23
27076|Buffel Formation|Lithology|The lower sandstone member consists of greenish-coloured fine calcareous sandstone. The middle limestone member consists of finely laminated calcilulite and coarse, thick-bedded calcarenite-calcirudite. Lateral facies changes are evident. Abundant bioclastic fragments of brachiopods, bivalves, sponges, bryozoans, and crinoids occur. The calcareous siltstone member includes regularly interbedded siltstones and sandstones which display extensive bioturbation.|16-MAY-23
27076|Buffel Formation|Fossils|The fauna awaits detailed description. Eurydesma and Taeniothaerus are prominent in the lower and middle members; the latter unit is also characterized by "Harridonia" mitis Hill. The upper member contains Echinalosia, Anidanthus springsurensis (Booker), Terrakea pollex Hill, and Tomiopsis ovata (Campbell).|16-MAY-23
27076|Buffel Formation|Relationships and boundaries|In places the Camboon Andesite is overlain by the lower sandstone member and elsewhere by the middle limestone member. Clearly the contact is unconformable and the Buffel Formation occurs as a valley fill. It is probably conformably overlain by the Pindari Formation.|16-MAY-23
27076|Buffel Formation|Age reasons|Asselian to Sakmarian (Early Permian).|16-MAY-23
27076|Buffel Formation|Comments|Notes: This redefinition of the Buffel Formation is in accord with the holostratotype which has been shown by recent mapping not to represent the complete sequence of calcareous sediments above the Camboon Andesite nor the units that Wass included in the unit but which can be identified as separate lithological units.|16-MAY-23
23435|Bulgeri Formation|Name source|Bulgeri Block of Lyndhurst Holding (Clarke River 4-Mile Cadastral map).|16-MAY-23
23435|Bulgeri Formation|Unit history|The unit was previously mapped as part of the Bundock Creek Formation (now Group) by White (1959, 1962, 1965), and the 'lower' Bundock Formation by Wyatt & Jell (1980).  The name was first published by Coote (1986), but not described.  Withnall & others (1988) fully described the unit but did not formally define it.|16-MAY-23
23435|Bulgeri Formation|Geomorphic expression|The unit is expressed as a series of low strike ridges, dominated by a high strike ridge, the Red Range, straddling the Broken River in the southwest.  The unit is traversed by a trellised drainage pattern.  Sparse silver-leaf ironbarks are ubiquitous on the drab sandstone and conglomerate which are represented by pale tones on aerial photographs.  Redbeds commonly support quinine bush and have dark reddish to purple tones on aerial photographs.|16-MAY-23
23435|Bulgeri Formation|Type section locality|In the Broken River between 7859 578447 (base) and 530460 (top).  The grid reference is based on the AGD66 datum.|16-MAY-23
23435|Bulgeri Formation|Description at type locality|The section consists of 3660 m of grey to greenish grey (drab), fine to coarse-grained lithofeldspathic to feldspathic sandstone, greenish grey siltstone, mudstone, fine-grained redbeds (greyish red sandstone, siltstone, and mudstone), and lesser polymictic conglomerate and reworked tuff.  See Withnall & others (1988, figures 50, 52, and 53, and pages 77-85) for more details.|16-MAY-23
23435|Bulgeri Formation|Thickness range|The unit is up to 3660 m thick in the main outcrop area in the south between the Clarke River Fault and the Broken River.  However, it thins considerably to the northeast particularly over the Atherton Creek Anticlinorium where it is locally absent and is onlapped by the Turrets Formation over the Broken River Group.  Between 'Pandanus Creek' and the Six-Mile Syncline the formation again thickens to about 1200 m.|16-MAY-23
23435|Bulgeri Formation|Lithology|Fine to coarse-grained drab, lithofeldspathic to feldspathic sandstone, polymictic conglomerate, fine-grained redbeds, greenish grey siltstone and mudstone, local green to pink tuff, minor calcirudite and oolitic calcareous sandstone.  The sandstones contain small to large-scale trough and tabular cross-beds, soft-sediment deformation, ripple marks, horizontal planar laminae, parting lineation, and rip-up clasts.  Rare fish remains occur on foresets, and fossil wood and fish remains occur in channel lags.  The redbeds contain desiccation cracks, bioturbation, root casts, rare fish remains, and locally abundant calcareous pedogenic nodules.|16-MAY-23
23435|Bulgeri Formation|Fossils|Rare Cyrtospirifer sp. and bivalves have been found near the base in both outcrop and GSQ Clarke River 2 (Lang, 1985, 1986a; Law, 1986); a brachiopod-dominated fauna including Cyrtospirifer occurs in calcareous sandstone in the northwestern part of the formation near the Teddy Mount Fault.  A fauna listed by Hill (in White & others, 1959) and including bivalves, gastropods, brachiopods, pteropods, and tentaculitids came from near the top of the formation.  A brachiopod, bivalve, and ostracode fauna occurs near the top of the unit in the Broken River section.  Scattered lycopod log and stem impressions, mainly Leptophloeum australe, occur throughout the unit.  A carbonised palynoflora recovered from core in GSQ Clarke River 1 included Granulatisporites frustulentus (Lang, 1985, 1986a, b).  Non-marine fish remains have been recovered from the lower part of the formation.|16-MAY-23
23435|Bulgeri Formation|Relationships and boundaries|The Bulgeri Formation is the basal unit of the Bundock Creek Group, and overlies the Broken River Group with a slight angular unconformity (a few degrees) to disconformity.  In the type section, the base is marked by a pebble to cobble conglomerate dominated by quartz and quartzite clasts, which sharply overlies pencil-cleaved shales of the Mytton Formation.  The abundant redbeds are characteristic of the Bulgeri Formation and serve to distinguish the unit from the conformably overlying Turrets Formation.  It is faulted against Proterozoic metamorphic rocks and early Palaeozoic granitoids of the Lolworth-Ravenswood and Georgetown Provinces along the Clarke River and Teddy Mount Faults, respectively.  It is intruded by the Carboniferous or ?Permian Montgomery Range Igneous Complex.|16-MAY-23
23435|Bulgeri Formation|Age reasons|A Frasnian(?) to Fammenian age is inferred from the fossil evidence and superpositional relationships.|16-MAY-23
23435|Bulgeri Formation|References|COOTE, S.M., 1986:  Departmental stratigraphic drilling in Queensland, 1983 to 1986.  Queensland Government Mining Journal, 87, 306-326. **LANG, S.C., 1985:  Devonian-Carboniferous stratigraphy of the southeastern Bundock Basin, Broken River area, north Queensland. B.Sc. (Hons) Thesis, University of Queensland (unpublished). **LANG, S.C., 1986a:  Devonian-Carboniferous stratigraphy of the southeastern Bundock Basin, Broken River area, north Queensland. Geological Survey of Queensland, Record 1986/5 (unpublished). **LAW, S.R., 1986: GSQ Clarke River 2 - preliminary lithological log and composite log.  Geological Survey of Queensland, Record 1986/53 (unpublished). **WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 	3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. **WHITE, D.A., 1962:  Clarke River - Qld E/55-13. Bureau of Mineral Resources, Australia 1:250 000 Geological Series Explanatory Notes. **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.D., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5. **WYATT, D.H. & JELL, J.S., 1980:  Devonian and Carboniferous stratigraphy of the northern Tasman Orogenic Zone in the Townsville hinterland.  In. Henderson, R.A. & Stephenson, P.J. (editors), The Geology and Geophysics of Northeastern Australia.  Geological Society of Australia, Queensland Division, Brisbane, 201-228.|16-MAY-23
21357|Bulgin Creek Granite|Name source|Bulgin Creek, a tributary of the Cape River, joining it south of Mount Davenport at GR 3355 77372.  The grid reference is based on the AGD66 datum.|16-MAY-23
21357|Bulgin Creek Granite|Unit history|The Bulgin Creek Granite is included in the Ravenswood Granodiorite complex on the Charters Towers 1:250 000 Sheet (Clarke & Paine, 1970; Vine & Paine, 1974).|16-MAY-23
21357|Bulgin Creek Granite|Type section locality|In Bulgin Creek at GR 7957 290438.  The grid reference is based on the AGD66 datum.|16-MAY-23
21357|Bulgin Creek Granite|Description at type locality|Outcrops as white to grey, sparsely porphyritic, muscovite-biotite granite.|16-MAY-23
21357|Bulgin Creek Granite|Extent|The Bulgin Creek Granite crops out over about 52km2 from near Cornelia homestead to the Mount Stewart road and south east to the Flinders Highway.|16-MAY-23
21357|Bulgin Creek Granite|Lithology|The unit consists of a white to grey (locally pink) biotite-muscovite granite. Jointing is locally at greater than 1 metre spacing resulting in large whalebacks such as at the type locality. North of Cornelia homestead, a pink biotite granite is tentatively assigned to the Bulgin Creek Granite. The unit is intruded by locally numerous layered aplite/leucogranite/pegmatite dykes similar to the Grasstree Leucogranite.|16-MAY-23
21357|Bulgin Creek Granite|Relationships and boundaries|The Bulgin Creek Granite intrudes the Cape River Metamorphics east of Cornelia homestead.  It is intruded by aplite/leucogranite/pegmatite dykes similar to the Grasstree Leucogranite. Its relationship to the Amarra Granite to the north and north-east is not known.|16-MAY-23
21357|Bulgin Creek Granite|Age reasons|The age of the Bulgin Creek Granite is not known precisely. An age of Late Silurian to Early Devonian is assigned due to its textural and mineralogical similarity to other rocks in the Lolworth Batholith.|16-MAY-23
21357|Bulgin Creek Granite|Comments|MAGNETIC SUSCEPTIBILITY::  Magnetic susceptibilities at the type locality are in the range 377-960 x 10[superscript] -5 SI units. Elsewhere in the unit, susceptibilities are in the range 74-573 x 10-5 SI units.|16-MAY-23
21357|Bulgin Creek Granite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
24202|Bulmung Sandstone Member|Name source|Parish of Bulmung, County of Gregory.|16-MAY-23
24202|Bulmung Sandstone Member|Unit history|The rocks of the Bulmung Sandstone Member were previously mapped as Lawn Hill Formation by Carter & others (1961).|16-MAY-23
24202|Bulmung Sandstone Member|Type section locality|Holostratotype: The holostratotype of the Bulmung Sandstone Member is part of the hypostratotype of the Lawn Hill Formation. It forms that part of the section which lies between 549061 (base) and 548061 (top) in the Lawn Hill 1:100 000 Sheet area. Approximately 40 m of flaggy to blocky micaceous lithic and conglomeratic sandstone crop out in the type section.|16-MAY-23
24202|Bulmung Sandstone Member|Extent|The unit crops out as a single sinuous strike ridge which extends from the Gregory River, 6 km west of Riversleigh homestead to Accident Creek, 20 km east of Bowthorn homestead. It has been mapped in an inlier of Lawn Hill Formation in the headwaters of Stockyard Creek, 75 km northwest of Lawn Hill homestead in the Bowthorn Sheet area. It thins eastward and lenses out east of Lawn Hill Creek.|16-MAY-23
24202|Bulmung Sandstone Member|Thickness range|The thickness in the holostratotype is 40 m. In the headwaters of Stockyard Creek, approximately 150 m of Bulmung Sandstone Member are exposed.|16-MAY-23
24202|Bulmung Sandstone Member|Lithology|The lithologies of the type section are typical of the entire unit.|16-MAY-23
24202|Bulmung Sandstone Member|Relationships and boundaries|The unit is conformably overlain and underlain by tuff and siltstone of the Lawn Hill Formation. It is a sandstone sequence in a tuffaceous and silty sequence.|16-MAY-23
24202|Bulmung Sandstone Member|Age reasons|Mid Proterozoic (Carpentarian).|16-MAY-23
27077|Bundock Creek Group|Name source|Bundock Creek, which joins the Einasleigh River at 7759-263895.  The grid reference is based on the AGD66 datum.|16-MAY-23
27077|Bundock Creek Group|Unit history|Bundock Creek Formation of White (1959, 1962, 1965).  Wyatt & Jell (1980) referred to an informal 'lower' and 'upper' Bundock Creek Formation separated by an unconformity.  Lang (1985, 1986a) determined that no unconformity exists, and Withnall & others (1988) raised the unit to group status.  The Bulgeri Formation corresponds to the lower subunit of Wyatt & Jell, whereas the upper unit is the sequence from Turrets Formation to Harry Creek Formation.|16-MAY-23
27077|Bundock Creek Group|Constituents|Harry Creek Formation, Boroston Formation, Teddy Mount Formation (including the Dyraaba Member), 	Turrets Formation, Bulgeri Formation (including the Rockfields Member and Stopem Blockem Conglomerate Member).|16-MAY-23
27077|Bundock Creek Group|Extent|The Group crops out in a roughly rectangular area of about 1000 km2 in the headwaters of the Einasleigh and Broken Rivers.  It extends from the Clarke and Gregory Rivers in the south, 35 km to Teddy Mount in the north, and from 'Pandanus Creek' in the east, 50 km to near 'Oak Valley' in the west.|16-MAY-23
27077|Bundock Creek Group|Lithology|Generally labile sandstone, polymictic conglomerate, siltstone, mudstone, tuff, and minor dirty limestone; the Bulgeri Formation is characterised by redbeds.|16-MAY-23
27077|Bundock Creek Group|Relationships and boundaries|The Bundock Creek Group overlies the Broken River Group with slight angular unconformity to disconformity, and is faulted against Proterozoic metamorphic rocks and early Palaeozoic granitoids of the Georgetown and Lolworth-Ravenswood Provinces along the Teddy Mount and Clarke River Faults, respectively.  It is intruded by the Carboniferous or ?Permian Montgomery Range Igneous Complex.|16-MAY-23
27077|Bundock Creek Group|Age reasons|Late Devonian (Frasnian or Famennian) to Early Carboniferous (Visean?).|16-MAY-23
84105|Burangoo Formation|Name source|Name derived from Burangoo (or Connelly) Waterhole in the Nicholson River, at approximately (GDA94) 17°53’S, 138°15’E.|
84105|Burangoo Formation|Unit history|Unit mapped as undifferentiated Constance Sandstone in First Edition 1:250 000 mapsheets of LAWN HILL (Carter and Öpik, 1960), WESTMORELAND (Carter, 1959), CALVERT HILLS (Roberts et al, 1963), and MOUNT DRUMMOND (Smith and Roberts, 1963a, b). Distinguished as Psa2 sandstone unit of the Constance Sandstone in Second Edition 1:250 000 mapsheets of LAWN HILL (Hutton and Grimes, 1983), WESTMORELAND (Grimes and Sweet, 1979), and CALVERT HILLS (Ahmad and Wygralak, 1989), following the scheme of Sweet et al (1981). Subsequently mapped as “Burangoo Sandstone Member” of the Constance Sandstone on Second Edition 1:250 000 mapsheet of MOUNT DRUMMOND by Rawlings et al (2006, 2008). Elevated to formation status as “Burangoo Sandstone” by Sweet (2017).|
84105|Burangoo Formation|Geomorphic expression|In areas of low dip, the Burangoo Formation forms extensive rocky plateaux, commonly with pseudokarstic weathering surfaces; in rare steeply dipping outcrops, the unit forms sharp rocky ridges.|
84105|Burangoo Formation|Type section locality|Along the northern side of the Nicholson River in WESTMORELAND 1:250 000 mapsheet. Base of type section located at approximately 17°52’24”S 138°15’38”E (54K 209699mE 8021697mN). Top of type section located west to west-southwest at approximately 17°53’21”S 138°14’15”E (207280mE 8019908mN). Type section accessible via Bowthorn Station and a tourist track to Burangoo Waterhole.|
84105|Burangoo Formation|Extent|Outcrops north of Elizabeth Creek in northern LAWN HILL, south of Hedleys Creek in southwestern WESTMORELAND, and adjacent parts of southeastern CALVERT HILLS and northeast and central MOUNT DRUMMOND 1:250 000 mapsheets.|
84105|Burangoo Formation|Thickness range|Estimated to be a 320 m thick in the type section, based on a dip of 5° in the type section in the WESTMORELAND 1:250 000 mapsheet; the formation thins to approximately 50 m thick in the southernmost outcrops in the HEDLEYS CREEK 1:100 000 mapsheet; the unit is over 300 m thick in the SEIGAL 1:100 000 mapsheet, and ranges from approximately 130 m to 300 m thick in the MOUNT DRUMMOND 1:250 000 mapsheet.|
84105|Burangoo Formation|Lithology|Fine- to coarse-grained, lithic, sublithic and quartzose sandstone, with scattered grains and layers of quartz granules and pebbles up to 1 cm in diameter; strongly trough cross-bedded in many outcrops; also planar cross-beds, planar bedding and hummocky cross-stratification.|
84105|Burangoo Formation|Depositional environment|Predominantly fluvial, with shallow-marine influence (intertidal to upper shoreface) present in the lower sections of the formation.|
84105|Burangoo Formation|Relationships and boundaries|The lower contact with the underlying Pandanus Formation is sharp and likely represents a minor unconformity, due to movement on the Calvert Fault on the HEDLEYS CREEK 1:100 000 mapsheet (Sweet, 2017). The upper contact with the overlying Wallis Formation is sharp but conformable, displaying a significant change from fine- to coarse-grained sandstones to more fine-grained, more thinly bedded, deeper-water facies (Rawlings et al, 2008; Sweet, 2017). In northern MOUNT DRUMMOND, the Schultz Sandstone Member of the Constance Sandstone truncates the Wallis Formation to lie disconformably on the Burangoo Sandstone (Rawlings et al, 2008).|
84105|Burangoo Formation|Identifying features|Fine- to coarse-grained, lithic, sublithic and quartzose sandstone of the Burangoo Formation is lithologically distinct from much more fine-grained, siltstone and mudstone dominated units of the Pandanus Formation (below) and Wallis Formation (above).|
84105|Burangoo Formation|Age reasons|Maximum depositional ages derived from U-Pb SHRIMP dating of detrital zircons: Constance Sandstone (stratigraphically overlies Burangoo Sandstone): GA sample 2678595 - 1591 ± 18 Ma (Anderson et al., 2019). Burangoo Formation: GA sample 1990590 - 1566 ± 46 Ma (Carson et al, 2011). Burangoo Formation: GA sample 2786169 - 1752 ± 4 Ma (Kositcin and Carson, 2019). Playford Sandstone (stratigraphically underlies Burangoo Formation): GA sample 2785615 -1615 ± 15 Ma (Kositcin and Carson, 2019). Therefore, the potential depositional age range for the Burangoo Formation can be considered to extend from ca. 1615 ± 15 Ma to 1591 ± 18 Ma.|
84105|Burangoo Formation|Correlations|No precise correlations at the formation level are known. Given the potential depositional age range of ca. 1630 Ma to 1573 Ma, the Burangoo Formation may be correlative with components of the upper Glyde package to the Favenc package (Rawlings, 1999) of the McArthur Basin.|
84105|Burangoo Formation|Geophysical Expression|Moderate to high magnetic response, likely due to the formation’s close proximity to sandstone formations in the South Nicholson Group which display a moderate to high magnetic response due to “subtle magnetic layering”, such as the Playford Sandstone (Rawlings et al, 2008).|
84105|Burangoo Formation|Geochemistry|see Carson CJ, Jarrett AJM, Anderson JR, Champion DC and Henson PA, 2020. Exploring for the Future – Whole rock geochemistry data release of sedimentary and igneous rocks from the South Nicholson region, Northern Territory and Queensland. Geoscience Australia, Record 2020/02.|
84105|Burangoo Formation|Defn author|Elliot Foley, Jack Simmons, Ben Williams, Charles Verdel (Northern Territory Geological Survey), Chris Carson (Geoscience Australia) 31-MAY-2023.|
84105|Burangoo Formation|Comments|Note: Standard series 1: 100 000 and 1: 250 000 mapsheet names are shown in uppercase.|
84105|Burangoo Formation|References|Ahmad M and Wygralak AS, 1989. Calvert Hills, Northern Territory (First Edition). 1:250 000 metallogenic map series explanatory notes, Sheet SE 53-8. Northern Territory Geological Survey, Darwin, Northern Territory. **Anderson JR, Lewis CJ, Jarrett AJM, Carr LK, Henson P, Carson CJ, Southby C and Munson TJ, 2019. New SHRIMP U–Pb zircon ages from the South Nicholson Basin, Mount Isa Province and Georgina Basin, Northern Territory and Queensland. Geoscience Australia, Record 2019/10. **Carson CJ, Hutton LJ, Withnall IW, Perkins WG, Donchak PJT, Parsons A, Blake PR, Sweet IP, Neumann NL and Lambeck A, 2011. Summary of results: Joint GSQ-GA geochronology project Mount Isa region, 2009-2010. Geological Survey of Queensland, Record 2011/03.  **Carson CJ, Jarrett AJM, Anderson JR, Champion DC and Henson PA, 2020. Exploring for the Future – Whole rock geochemistry data release of sedimentary and igneous rocks from the South Nicholson region, Northern Territory and Queensland. Geoscience Australia, Record 2020/02.  **Carson, C. J., Kositcin, N., Anderson, J. R., and Henson, P. A. in prep. A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia - insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences.  **Carter EK, 1959. New stratigraphic units in the Precambrian of north-western Queensland. Queensland Government Mining Journal 60(92), 437–431. **Carter EK and Öpik AA, 1960. Lawn Hill – 4-mile geological series. Explanatory notes No. 21. Bureau of Mineral Resources, Canberra.  **Grimes KG and Sweet IP, 1979. Westmoreland, Queensland (Second Edition). 1:250 000 geological map series explanatory notes, SE 54-5. Bureau of Mineral Resources, Canberra.  **Hutton LJ and Grimes KG, 1983. Lawn Hill, Queensland (Second Edition). 1:250 000 geological map series explanatory notes, SE 54-9. Bureau of Mineral Resources, Canberra.  **Kositcin N and Carson CJ, 2019. New SHRIMP U-Pb zircon ages from the South Nicholson and Carrara Range regions, Northern Territory. Geoscience Australia, Record 2019/09.  **Rawlings DJ, 1999. Stratigraphic resolution of a multiphase intracratonic basin system: the McArthur Basin, northern Australia. Australian Journal of Earth Sciences 46(5), 703–723.  **Rawlings DJ, Sweet IP and Kruse PD, 2006. Mount Drummond, NT (Second Edition). 1:250 000 Geological Map, Sheet SE 53-12. Northern Territory Geological Survey, Darwin, Northern Territory.  **Rawlings DJ, Sweet IP and Kruse PD, 2008. Mount Drummond, NT (Second Edition). 1:250 000 Geological Map Series Explanatory Notes, Sheet SE 53-12. Northern Territory Geological Survey, Darwin, Northern Territory.  **Roberts HG, Rhodes JM and Yates KR, 1963. Calvert Hills, Northern Territory (First Edition). 1:250 000 geological map series explanatory notes, SE 53‑8. Bureau of Mineral Resources, Canberra.  **Simmons JM, Williams B, Carson, C and Verdel C, 2023a. Mount Drummond, Northern Territory 1:250 000 Geological Map, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.  **Simmons JM, Williams B, Carson, C and Verdel C, 2023b. Mount Drummond, Northern Territory 1:250 000 Geological Map Explanatory Notes, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.  **Smith JW and Roberts HG, 1963a. Mount Drummond, NT (First Edition). 1:250 000 Geological Map Series Explanatory Notes, Sheet 53-12. Bureau of Mineral Resources, Canberra.  **Smith JW and Roberts HG, 1963b. Mount Drummond, NT (First Edition). 1:250 000 Geological Map Series, Sheet SE 53-12. Bureau of Mineral Resources, Canberra. **Sweet IP, 2017. The geology of the South Nicholson Group, northwest Queensland. Queensland Geological Record 2017/07. **Sweet IP, Mitchell JE and Mock CM, 1981. Seigal, Northern Territory and Hedleys Creek, Queensland. 1:100 000 Geological Map Commentary. Bureau of Mineral Resources, Geology and Geophysics, Canberra|
26256|Burges Formation|Name source|Burges 1:100 000 Sheet area.|16-MAY-23
26256|Burges Formation|Unit history|The unit was previously mapped as part of the Broken River Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
26256|Burges Formation|Geomorphic expression|Generally low, undulating, recessive topography.|16-MAY-23
26256|Burges Formation|Type section locality|In the Broken River between 7859-611441 (base) and 610442 (base).  The grid reference is based on the AGD66 datum.   REFERENCE SECTION: In Diggers Creek between 7859-684488 (base) and 670500 (top).  The thickness is unknown because of fold repetition, but is probably of the order of 800 m.  It consists of thin to very thick-bedded, massive to laminated mudstone, thin-bedded, fine-grained arenite, polymictic conglomerate, and limestone lenses (predominantly calcarenite, calcirudite, and lesser calcilutite).|16-MAY-23
26256|Burges Formation|Description at type locality|The section is 127 m thick and consists of polymictic pebble and cobble conglomerate, calcirudite, and calcareous lithic arenite (Withnall & others, 1988, figure 30 and pages 71-72 and 164).  The unit is relatively thin in this section, but it is the only unfolded section known.|16-MAY-23
26256|Burges Formation|Extent|The unit crops out mainly to the north of the Broken River, between about 7859-650555 and 611441 in the south to northeast of Jessie Springs at about 740550.  The grid reference is based on the AGD66 datum.|16-MAY-23
26256|Burges Formation|Thickness range|120 to 800 m.|16-MAY-23
26256|Burges Formation|Lithology|The Burges Formation is relatively heterogeneous.  Four lithofacies are recognised (Withnall & others, 1988, pages 71-76).  They are (a) polymictic conglomerate-calcirudite-arenite; (b) thinly interbedded mudstone-limestone-arenite; (c) limestone (thin to medium-bedded calcarenite, calcirudite, and lesser calcilutite); and (d) massive mudstone and minor arenite.|16-MAY-23
26256|Burges Formation|Fossils|The calcareous mudstones contain plant remains, tabulate and solitary rugose corals, small stromatoporoids, brachiopods, and crinoidal ossicles.  The limestones contain tabulate and rugose corals, stromatoporoids up to 1 m in diameter, brachiopods, crinoids, bryozoa, bivalves, nautiloids, fish, and conodonts.|16-MAY-23
26256|Burges Formation|Relationships and boundaries|The Burges Formation is part of the Wando Vale Subgroup of the Broken River Group.  It disconformably(?) overlies the Shield Creek Formation in the north near Jessie Springs, but conformably overlies the Bracteata Mudstone in the Broken River.  In the north it passes laterally into the Jessey Springs Limestone, and also conformably overlies and underlies this unit in places.  South of the Broken River it passes laterally into Bracteata Mudstone, Lomandra Limestone, Storm Hill Sandstone, and Dosey Limestone.  It is conformably overlain by the Papilio Mudstone.  The Burges Formation is interpreted as  slope deposits, whereas the other units are regarded as having been deposited in shelf environments.|16-MAY-23
26256|Burges Formation|Age reasons|The age range is Emsian to early Givetian.|16-MAY-23
26256|Burges Formation|References|*WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.    *WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes.    *WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.    *WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
25823|Burstall Granite|Name source|Mount Burstall, 8 km east-southeast of Mary Kathleen, latitude 20o48'20"S, longitude 140o3'20"E (6956 017992).|16-MAY-23
25823|Burstall Granite|Geomorphic expression|Rounded elevated bouldery hills and irregular maturely dissected plateaux.|16-MAY-23
25823|Burstall Granite|Type section locality|Mount Burstall, 8 km east-southeast of Mary Kathleen. Granite in this area is pink, foliated, coarse-grained, even-grained to porphyritic, and contains aligned xenoliths of porphyritic microgranite and recrystallised calc-silicate rocks, especially in the south. Fluorite is recognisable in some hand specimens.|16-MAY-23
25823|Burstall Granite|Extent|The Burstall Granite forms discrete plutons in a north to north-northeast trending belt 8 km wide and 40 km long which extends from Duchess to Mount Philp, and in a similar belt east of Mary Kathleen extending from Mount Burstall to the Mount Godkin Range. The two belts were probably collinear, but have been separated by up to 25 km of dextral displacement along the Fountain Range Fault. The larger intrusions are in the Mount Godkin Range 30 km north-northeast of Mary Kathleen (20 km2), north of Mount Burstall 8 km east of Mary Kathleen (20 km2), south of Fountain Range 32 km south-southwest of Mary Kathleen (22 km2), and 8 km north of Duchess (25 km2). Smaller plutons and aplite and pegmatite veins are common in the country rocks north and south of the main belts, and one small outcrop of granite 21 km west-northwest of Mary Kathleen has also been assigned to the Burstall Granite.|16-MAY-23
25823|Burstall Granite|Lithology|The main rock type is leucocratic coarse to medium-grained even-grained to porphyritic slightly foliated granite. Minor tonalite and diorite are found near contacts with the Lunch Creek Gabbro. Potassic and sodic aplite, tourmaline-bearing pegmatite fluorite veins, and rhyolite and microgranite dykes are associated with the granite. The main mafic minerals are biotite and amphibole (?ferrohastingsite) and the accessory minerals are sphene, opaque oxides, zircon, fluorite, allanite and tourmaline. The rhyolite dyke phase 2 to 3 km east and southeast of Mary Kathleen mine contains high anomalous amounts of uranium (Derrick, 1977).|16-MAY-23
25823|Burstall Granite|Relationships and boundaries|The Burstall Granite intrudes the Corella Formation, some amphibolitic dolerite masses, and the less altered pyroxenic Lunch Creek Gabbro. It is intruded by unnamed dolerite dykes, and by the undeformed Lakeview Dolerite.|16-MAY-23
25823|Burstall Granite|Age reasons|Proterozoic: Green (1975) presents potassium/argon and argon/argon ages in the range 1325 to 1440 m.y., but considers there is evidence of a separate thermal event at about 1400 m.y. Rubidium/strontium isochron studies (Page, pers. Comm., 1974) have indicated ages of 1417+/-45 m.y. and 1595+/- m.y. for the Burstall Granite.|16-MAY-23
25823|Burstall Granite|Comments|Discussion: The areas of Burstall Granite were mapped previously as Wonga Granite (Carter et al., 1961) but they have been separated from it because of their less foliated texture, less elongate outcrops, distinct topographic expression, and reasonable geographic separation. The Burstall Granite is a higher level late-tectonic to post-tectonic granite, but the mineralogically similar but more strongly foliated Wonga Granite may be a deeper seated equivalent. The Wonga Granite may have intruded early in the regional metamorphism, and the Burstall Granite later, the latter as a series of small satellitic intrusions marginal to the main mass of Wonga Granite.  The name Burstall Granite has previously been published by Whittle (1960), in the 19th Annual Report of the Australian Atomic Energy Commission 1970-1971, in Plumb & Derrick (1975) and in Derrick (1977). In all these publications the name refers specifically to that mass of Burstall Granite north of Mount Burstall and 8 km east of Mary Kathleen, and which is associated with the uranium mineralisation at Mary Kathleen.|16-MAY-23
24204|Bushy Park Gneiss|Name source|The formation is named after the Bushy Park pastoral lease, northeast of Duchess township, Duchess 1:100 000 Sheet area (Duchess 1:250 000 Sheet area).|16-MAY-23
24204|Bushy Park Gneiss|Unit history|Previously mapped as Argylla Formation, Corella Formation and Kalkadoon Granite (Carter & Opik, 1963).|16-MAY-23
24204|Bushy Park Gneiss|Type section locality|Railway cutting, west of Duchess-Myubee track, 11 km northwest of Duchess township, at GR 750460, Duchess 1:100 000 Sheet area. Here the unit consists mainly of medium to coarse quartzofeldspathic gneiss and foliated to gneissic granite containing pink feldspar megacrysts, and minor finer grained leucocratic biotite granite.|16-MAY-23
24204|Bushy Park Gneiss|Extent|The gneiss is confined to a narrow north-trending belt west of Duchess|16-MAY-23
24204|Bushy Park Gneiss|Lithology|The main rock types are medium to coarse-grained quartz-feldspar-biotite-hornblende orthogneiss and augen gneiss which locally form large massive to bouldery outcrops. Minor rock types include medium to coarse-grained, slightly foliated to gneissic, porphyritic biotite granite, fine-grained leucocratic gneiss, medium to coarse leucocratic granite, and tourmaline-bearing pegmatite.|16-MAY-23
24204|Bushy Park Gneiss|Relationships and boundaries|The gneiss forms a series of intrusive pods and elongate lenses interlayered with the Corella Formation and Magna Lynn Metabasalts.|16-MAY-23
24204|Bushy Park Gneiss|Age reasons|Proterozoic|16-MAY-23
24204|Bushy Park Gneiss|Comments|The Bushy Park Gneiss may represent intensely deformed, pre or syntectonic stocks and dykes, and may be equivalent to similar units in the Wonga Granite to the north of Duchess (Derrick & others, 1977).|16-MAY-23
79123|Calton Andesite Member|Name source|Named in 1996 mapping after Calton Terrace or Calton Hill in Gympie. Remapping in 2014 showed that these outcrops are not Calton but the lithologically similar Kidgell Andesite.|16-MAY-23
79123|Calton Andesite Member|Unit history|Equivalent to Dunstan's (1911) First Volcanic Group 'Altered diabase' (1VC, 1VF).  First used informally at Monkland Mine as Calton andesite for the coherent facies and Calton clastics for the fragmental facies.  Both were subsequently referred to in Cranfield (1999), Sivell & Arnold (1999) and Sivell & McCulloch (2001) Li & others (2015),  but the term Calton clastics now abandoned.|16-MAY-23
79123|Calton Andesite Member|Type section locality|In a cutting along the Heritage Railway in the Monkland block off Union Street, Gympie (AMG 467655mE; 7101240mN; Lat: -26°12'29"  Long: 152°40'34"). Reference drill sections: BHP drill hole G023: 134-186 m at north end of Monkland Mine. GEGM drill hole G135: 142-168 m near the Aurelia shoot, Monkland Mine.  GEGM drill hole G137: 399-507 m at Monkland Mine. Clastic facies Reference sections: GEGM drill hole G224: 35-140 m at South Inglewood GEGM drill hole G227: 197-215 m at South Inglewood (MGA 469900mN; 7098795mN).|16-MAY-23
79123|Calton Andesite Member|Description at type locality|Coherent andesite - see Lithology.|16-MAY-23
79123|Calton Andesite Member|Extent|At least 6 km long, from east of Dawn Mine to the centre of Gympie. In Monkland, Phoenix, Six Mile, Sovereign and Dawn blocks and the Inglewood Horst. Limited or absent in northern Phoenix Block and the north (Dugdale, 2004). Also present at the Partridge, Wylly and Butterfly prospects.|16-MAY-23
79123|Calton Andesite Member|Thickness range|Up to 50m thick at Monkland, 40-50m at Partridge and Inglewood Horst, and 60m in the Six Mile Block.|16-MAY-23
79123|Calton Andesite Member|Lithology|Two facies, a dominant coherent andesite and a subordinate fragmental to conglomeratic facies.  The coherent andesite is massive, greenish grey, feldspar-phyric, characterized by distinctive euhedral  plagioclase phenocrysts, 1 to 4 mm in size; some are  in clusters, some flow-oriented, constituting 25-35% of the rock within a fine groundmass of albitised plagioclase microlites and small chloritised mafic crystals.  All feldspars are variably altered to albite, sericite and epidote though some retain visible twinning.  In more intensely altered zones, phenocrysts are barely visible, being altered to a turbid mass of sericite-epidote, clays and fine carbonate within a chloritised sericitised groundmass of similar composition which gives them a ghostlike texture. Altered mafic phenocrysts constitute about 5-15% of the rock, usually completely replaced by carbonate and chlorite.  Accessory titanomagnetite, partly or totally replaced by leucoxene. Sparse hematite may be present.  Many parts of the andesite have undergone autobrecciation  some with jigsaw-fit texture. The clastic facies is an immature chaotic reworked epiclastic to conglomeratic facies equivalent of the Calton Andesite, found adjacent to the coherent andesite. The clastic unit can occur as subrounded, coarse-grained cobble beds with a high proportion of Calton volcanic clasts, or can be polymict with some mafic input (Photograph 14). This unit should not be confused with the basal beds of the Nash Clastics above the andesite which contain a large amount of feldspathic detritus derived from the underlying andesite.|16-MAY-23
79123|Calton Andesite Member|Relationships and boundaries|Occurs as a flow, underlain by Eldorado Clastics Member and overlain by Nash Clastics Member. In places the coherent andesite is underlain by, or extends laterally into, a fragmental andesite facies mapped separately by GEGM at Monkland Mine as Calton clastics.|16-MAY-23
79123|Calton Andesite Member|Alteration and Mineralisation|Low grade alteration to albite, chlorite, sericite, epidote, leucoxene.|16-MAY-23
79123|Calton Andesite Member|Geochemistry|Sivell & McCulloch (2001) and Sivell & Arnold (1999) identified these volcanic rocks as high-K andesite.|16-MAY-23
79123|Calton Andesite Member|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie, 12-JAN-2017.|16-MAY-23
79123|Calton Andesite Member|References|Dunstan, B., 1911: Geology map of Gympie and environs. GSQ Publ. No. 221b. **Cranfield, L.C., 1999: Gympie Special Sheet 9445, Part 9545, Queensland 1:100,000 Geological Map Commentary. Queensland Department of Mines and Energy, Brisbane.  **Sivell, W.J. and Arnold, G.O. 1999:	Geochemical and volcanic stratigraphy of a segment of an island arc - Gondwana rim accretion zone, Gympie Province, southeast Queensland.  IN Flood, P.G. (Editor): Regional Geology, Tectonics and Metallogenesis, New England Orogen, NEO '99 Conference, 255-266.  **Sivell, W.J. and McCulloch, M.T. 2001: Geochemical and Nd-isotopic systematics of the Permo-Triassic Gympie Group, southeast Queensland.  Australian Journal of Earth Sciences 48, 377-394. **Li, P., Rosenbaum, G., Yang, J-H. and Hoy, D. 2015 Australian-derived detrital zircons in the Permian-Triassic Gympie terrane (eastern Australia): Evidence for an autochthonous origin. Tectonics, 34, 858-874.|16-MAY-23
25687|Candlow Formation|Name source|Candlow Creek, a major tributary of the Langdon River, which it joins at GR 7460-097365 (Esmeralda 1:100 000 Sheet area); also Candlow Dam and Candlow mustering camp, near GR 7560-147315 (North Head 1:000 000).|16-MAY-23
25687|Candlow Formation|Unit history|Mapped as (the upper) part of the Etheridge Formation by White (1959, 1962, 1965), who recognised the Stockyard Creek Siltstone Member.|16-MAY-23
25687|Candlow Formation|Geomorphic expression|Forms a generally very subdued to flat topography with sparse outcrop, generally where steep-sided gullies cut through to less weathered rock. The White Bull and Stockyard Creek Siltstone Members generally form more prominent ridges, the former characterised by prominently outcropping beds of siliceous siltstone, the latter by steep-sided hills with a dense cover of Acacia shirleyi (lancewood).|16-MAY-23
25687|Candlow Formation|Type section locality|About 5 km northeast of White Bull Bore, between GR 7560-236389 (base) and -216377 (top). The track from White Bull to Carnes Dam crosses the section at -224 381. In the type section, lithologies are as follows (from top to bottom): Light to dark grey, locally carbonaceous siltstone and fine lithic sandstone; some siliceous siltstone and quartzose sandstone; minor intraformational breccia...560 m. Black carbonaceous pyritic (or ex-pyritic) siltstone - 170 m (Stockyard Creek Siltstone Member). Grey to white (weathered) siltstone and minor lithic sandstone, commonly purple (ferruginous) towards top; white efflorescence of hydrated Mg sulphates common, due to minor dolomitic component of rocks...680 m. Grey - 200 m. Mainly light to dark grey siltstone, carbonaceous in part; minor siliceous/quartzose siltstone...400 m.|16-MAY-23
25687|Candlow Formation|Extent|Exposed in the southwest of Forest Home (west of Pinnacle Creek - about 143o09'E) and the west of North Head (west of about 143o13'E) 1:100 000 Sheet areas, between the Gilbert River (18o15'S) and about 18o50'S in the headwaters of the Langdon River and in the Reedy Creek area. Small inliers exposed north of the Gilbert River near GR 7561-165885.|16-MAY-23
25687|Candlow Formation|Thickness range|About 2000 m in the type area; ranges from about 1000 m in the Candlow area (about GR 7560-200310) to about 3500 m in the Pinnacle Creek area (approximately GR 7561-240680).|16-MAY-23
25687|Candlow Formation|Lithology|These lithologies are typical of the Formation, but there is considerable variation. In some areas, the uppermost part is predominantly sandy and variably pyritic; in the north, intraformational breccias containing abundant quartz are common. The middle part in places lacks sandstone and/or is strongly pyritic. The lowermost part commonly contains lithic and lithic-quartz sandstones. All rocks particularly finer-grained ones, are variably phyllitic or cleaved, or show incipient cleavage.|16-MAY-23
25687|Candlow Formation|Relationships and boundaries|Conformably overlain by the Langdon River Siltstone which consists of characteristic dark grey and maroon banded phyllitic siltstone (without  the common sandy rocks of the Candlow Formation), commonly has a strongly carbonaceous bed at its base, and forms a much more rugged topography. Underlain conformably by Heliman Formation which contains a much higher proportion of prominently outcropping dark grey siliceous siltstone beds. Intruded by Forest Home Granodiorite and Esmeralda Granite. Commonly capped by a Tertiary deep-weathering profile with or without a blanket of ferruginised valley fill, colluvium, or fanglomerate.|16-MAY-23
25687|Candlow Formation|Age reasons|Probably mid-Proterozoic: a minimum age of 1570+/-30 m.y. can be inferred from dating in underlying rocks (Black et al., in press) of a deformation-metamorphism event which has affected the Candlow Formation.|16-MAY-23
3458|Candover Metamorphics|Name source|Candover Holding, which lies just south of Surprise Creek, in the PROSPECTOR (1:100 000 Sheet area indicated by capitals). |16-MAY-23
3458|Candover Metamorphics|Unit history|The Candover Metamorphics were mapped as Argylla Formation and Eastern Creek Volcanics intruded by Ewen Granite by Carter & others (1961). The portion of the unit in PROSPECTOR was mapped as Eastern Creek Volcanics by Wilson & others (1977) but was amended to Leander Quartzite on the Prospector 1:100 000 Geological Series 1st edition map. On the Alsace 1:100 000 Geological Series preliminary map the unit was unnamed, but in the accompanying record (Derrick & Wilson, 1982) and on the Alsace 1:100 000 Geological Series 1st edition map, the informal name Candover beds was introduced. |16-MAY-23
3458|Candover Metamorphics|Geomorphic expression|Psa - ridges and low hills of rubbly sandstone outcrop; Pls - poorly outcropping low strike ridges with much sand cover; Pv - low ridges and pavements; Pb - bouldery hills and ridges.|16-MAY-23
3458|Candover Metamorphics|Type section locality|No single section adequately represents the four main lithological subunits in the Candover Metamorphics. The holostratotype is defined as a 3.5 km long section along Surprise Creek in southern ALSACE from 6858-605894 in the west to 6858-637888 in the east. The eastern end of the section is about 500 m east of a holding paddock on the north bank of a large waterhole on Surprise Creek. This section contains adequate exposures of three of the lithological subunits and a minor exposure of the fourth lithological subunit. Because of poorly preserved stratigraphy and tight folding, the relative stratigraphic positions of these subunits have not been resolved. The section from west to east comprises: labile quartzite, sheared greywacke, psammitic schist, and micaceous schist (subunit Ps); meta-arkose, pebbly meta-arkose, quartz-magnetite rock, and mica schist (subunit Psa); basic schist (subunit Pb); and at the eastern end of the type section meta-arkose, metamorphosed acid volcanics, and quartz-magnetite rocks (subunit Psa). Pegmatite veins are common throughout the section and dolerite dykes occur in the west. The fourth subunit (Pv) is mapped only north of the holostratotype where a parastratotype is defined from 6858-642927 to 6858-637936. It contains recrystallised porphyritic acid volcanics, rhyolite, mica schist, phyllonite, quartzite, siltstone, and acid crystal tuff.|16-MAY-23
3458|Candover Metamorphics|Extent|A wedge-shaped area mostly north of Surprise Creek in ALSACE. The total area of outcrop is 36 km2, of which approximately 1 km2 is in PROSPECTOR.|16-MAY-23
3458|Candover Metamorphics|Thickness range|Unknown; approximate minimum thicknesses of the four mapping subunits are Ps-600 m; Pv-400 m; Psa-500 m; Pb-400 m.|16-MAY-23
3458|Candover Metamorphics|Lithology|Subunit Ps: mica schist, psammitic schist, labile quartzite, and tuffaceous greywacke breccia. As mapped, easternmost areas of Ps are largely tuffaceous greywacke breccia, with some acid volcanics; the western area of Ps is of mainly schistose rocks. Metamorphic grade apparently increases from east to west, because mica grain size increases in that direction. In Surprise Creek micaceous quartzite and mica schist are intruded by microgranite, later pegmatite, and metadolerite. Subunit Pv: green-grey fluidal rhyolite, porphyritic acid volcanics, and crystal tuff, schistose in places; some mica schist and phyllonite; minor quartzite and siltstone. Subunit Psa: meta-arkose, conglomerate, quartz-magnetite rock (banded iron formation?), mica schist; minor rhyolitic and dacitic to andesitic tuff, metabasalt, quartzite, greywacke breccia. Some rock types are common with other subunits, but Psa is essentially an arenaceous subunit. Greywacke and arkose conglomerate contains clasts of the BIF. Acid to intermediate volcanics are interlayered with sediments near 6858-630883. Subunit Pb: massive and amygdaloidal metabasalt, intimately veined by granite and pegmatite. This subunit forms extensive outcrops to the north, near 6858-615975; mappable bands of metabasalt within Psa and Ps are also included in Pb.|16-MAY-23
3458|Candover Metamorphics|Relationships and boundaries|The Candover Metamorphics are not in contact with older units, hence their basal boundary criteria are not defined. The upper boundary is defined by the unconformity beneath quartzite and conglomerate mapped as Lena Quartzite Member of Eastern Creek Volcanics. The unit is intruded by pegmatite and granite, the larger masses of which are mapped as Ewen Granite, and by dolerite dykes. Most contacts with the Myally Subgroup, Eastern Creek Volcanics, and Fiery Creek Volcanics are faulted. Derrick & Wilson (1982) suggest that Pv is the oldest subunit. Although subunit Ps contains no reliable facing structures, it may be youngest because it is exposed to the west of the generally west-facing Ps.|16-MAY-23
3458|Candover Metamorphics|Structure and Metamorphism|Structure and metamorphism: Subunit Ps contains rocks which are strongly foliated, and a fracture cleavage is widely developed. Schistosity is common in the other mapping subunits, and north-northeast plunging folds have been noted in subunit Psa although the subunit generally faces west. Pegmatite, granite, and dolerite which cut the Candover Metamorphics are themselves deformed; some acid veins show folding and boudinage. Greenschist facies metamorphism (up to actinolite/biotite grade) is evident in the metabasalt. Cordierite in one specimen may indicate low amphibolite facies. The feldspathic quartzite from subunit Psa shows development of triple-point grain boundary junctions, typical of a high metamorphic grade.|16-MAY-23
3458|Candover Metamorphics|Age reasons|The Candover Metamorphics are intruded by a granite which is mapped as Ewen Granite. In MYALLY the Ewen Granite is dated by U-Pb zircon techniques as 1840+/-50 Ma (Page & others, 1982) and hence the Candover Metamorphics are inferred to be older than this date. Thus the metamorphics may correlate with the Leichhardt Metamorphics, about 1865 Ma old (Page, 1978). Other possibilities, discussed by Derrick & Wilson (1982), consider that the granite which intrudes the metamorphics may be younger than the Ewen Granite and that the volcanic submunit, Pv, may correlate with the Argylla Formation (1777+/-7 Ma, Page, 1978) or volcanics in the basal Leander Quartzite.|16-MAY-23
3458|Candover Metamorphics|Comments|Discussion: The Candover Metamorphics are older than Eastern Creek Volcanics, but other relationships are poorly understood. They are most likely correlatives of the Tewinga Group but could be correlatives of the lower Haslingden Group. The sequence of arkose, conglomerate, mica schist, metabasalt, greywacke breccia, and dacitic to andesite tuff resembles similar rocks or slightly lower metamorphic grade in basal Leander Quartzite in KENNEDY GAP (Wilson & others, 1979). If this correlation is accepted, it follows that the Candover Metamorphics may correlate with the older parts of the Mount Guide Quartzite (Derrick & others, 1977) and Bottletree Formation in DUCHESS (Bultitude & others, 1978). Correlation of the Candover Metamorphics with the Leichhardt Metamorphics of the Tewinga Group is based on their relationships to the Ewen Granite. The abundance of metasedimentary rocks distinguishes the Candover Metamorphcis from most areas of Leichhardt Metamorphics but can be explained by facies variation towards the western edge of the volcanic province or by a local depression on the volcanics containing (slightly) younger sediments.|16-MAY-23
33429|Canoe Creek Granite|Name source|The unit is named after Canoe Creek, which flows through the southwestern corner of the intrusion.|16-MAY-23
33429|Canoe Creek Granite|Unit history|Murphy & others (1976) previously mapped the unit as part of the Wigton Adamellite. The northern part of the unit on the MARYBOROUGH 1: 250 000 Sheet was mapped as an undivided Permo-Triassic granite by Cranfield (1992), and was also studied as part of a Queensland University of Technology honours study (Stensen, 1997).|16-MAY-23
33429|Canoe Creek Granite|Geomorphic expression|The unit forms low, bouldery hills interspersed with sandy plains.|16-MAY-23
33429|Canoe Creek Granite|Type section locality|The type area is designated as the headwaters of Twelve Mile Creek around AMG 365200 7122300.  he grid reference is based on the AGD66 datum.|16-MAY-23
33429|Canoe Creek Granite|Extent|Only the southern part of the unit (covering around 30km2) is exposed on the GYMPIE 1:250 000 Sheet, 18km north of Proston. The unit forms part of a larger, roughly circular pluton covering over 150 km2, mainly on the MARYBOROUGH 1:250 000 Sheet.|16-MAY-23
33429|Canoe Creek Granite|Lithology|The granite is pale grey to pink in colour, and is mostly fine to locally medium grained. It is characteristically sparsely porphyritic, with small (up to 3mm in length) euhedral feldspar phenocrysts, scattered through a finer matrix commonly altered pink matrix.  The granite has a low mafic content with biotite and locally minor hornblende making up to around 1 to 3% of the rock.  In thin section, the quartz-feldspar matrix sporadically displays very fine graphic intergrowth textures, and contains coarse accessory sphene and common fine opaque grains (probably mostly magnetite, accounting for the moderate magnetic response on geophysical images).  The phenocrysts are mainly plagioclase and alkali feldspar, both generally showing strong sericitic alteration.  Epidote/chlorite/calcite alteration is common throughout the pluton. Mafic clots and small xenoliths are only common locally within the granite.|16-MAY-23
33429|Canoe Creek Granite|Relationships and boundaries|The unit is considered to intrude the Late Triassic Aranbanga Volcanic Group. Small areas of Tertiary duricrust are developed in places on the granite. The unit is locally intruded by rhyolite dykes and small aplite bodies.|16-MAY-23
33429|Canoe Creek Granite|Age reasons|No radiometric age dating of the unit has been undertaken, but the granite is considered to most likely intrude the Late Triassic Aranbanga Volcanic Group, and to be of Late Triassic age.|16-MAY-23
33429|Canoe Creek Granite|Comments|GEOPHYSICAL EXPRESSION:: The unit occurs as mid to dark pink on the ternary radiometric images, distinct from the paler pink tones of the adjoining Aranbanga Volcanic Group to the south.  The unit has a moderate response on aeromagnetic images.GEOCHEMISTRY::  Based on whole rock geochemistry Stensen (1997) interpreted the unit as an S-type granite, forming a mostly peraluminous, high K,  calc-alkaline intrusion derived from in situ fractional crystallisation and differentiation of a sedimentary source.|16-MAY-23
33429|Canoe Creek Granite|References|CRANFIELD, L.C., 1992...........MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.STENSON, M.P.,1997, The Occurrence and Petrogenesis of the Wigton Granite, SE Queensland. Unpublished Bsc honours thesis, Department of Geology, Queensland University of Technology.|16-MAY-23
28102|Carew Greenstone|Lithology|Discordant greenish-black metabasalt, metadolerite; tremolite/actinolite, epidote, chlorite or hornblende amphibolite, with garnet, chlorite, talc, ilmenite, chromite; dark grey medium-grained equigranular hornblende-feldspar amphibolite; discordant greenish grey chlorite-actinolite-sericite-talc rock, relict minerals include hornblende, pyroxene and actinolite|16-MAY-23
24212|Carnes Granodiorite|Name source|Carnes' pastoral holding a subdivision of the old 'Forest Home' holding, in the upper Pinnacle Creek-Black Gin Creek area. The granodiorite lies wholly within the area of this holding.|16-MAY-23
24212|Carnes Granodiorite|Unit history|Tentatively assigned by Branch (1966) to the Prestwood Micro-granite, although Branch infers that it may be an "outer" of the "Forsayth Batholith". Rossiter (1978) assigned the pluton to the Forest Home Granodiorite.|16-MAY-23
24212|Carnes Granodiorite|Geomorphic expression|Moderately subdued topography: low, rolling hills, very open woodland with short grasses, producing a patchy light tone on airphotographs. Contact metamorphic aureole forms a slightly raised 'rim' to the pluton.|16-MAY-23
24212|Carnes Granodiorite|Type section locality|In and near a tributary of Black Gin Creek, near the track to the "Knights of Malta" mine and Green Hills outstation (GR 7560-236507).|16-MAY-23
24212|Carnes Granodiorite|Extent|In the middle reaches of Black Gin Creek. It is a roughly elliptical pluton with the ends of the long axis at GR 7560-193510 and -264520; the short axis almost coincides with Black Gin Creek, and the intrusive contacts intersect the creek at GR 7560-211528 and -229499.|16-MAY-23
24212|Carnes Granodiorite|Lithology|Medium to medium-coarse-grained biotite granodiorite, containing moderately abundant red-brown biotite with prominent dark haloes around minute zircon inclusions. Orthoclase, and, to a lesser degree, quartz, tending poikilitic; complexly twinned, strongly zoned plagioclase. Trace of late-stage (?) muscovite.|16-MAY-23
24212|Carnes Granodiorite|Relationships and boundaries|Intrudes Heliman and Townley Formations, which it has contact metamorphosed to produce an aureole 250 m wide.|16-MAY-23
24212|Carnes Granodiorite|Age reasons|Probably mid-Proterozoic, by analogy with the Forest Home Granodiorite, with which it shares many similarities.|16-MAY-23
3649|Carney Creek Quartz Diorite|Name source|Carney Creek which joins Theresa Creek at 8451-515525.   The grid reference is based on the AGD66 datum.|16-MAY-23
3649|Carney Creek Quartz Diorite|Geomorphic expression|The unit is generally poorly exposed forming undulating terrain and reddish sandy soil.  On the Landsat 5 TM (1-4-7 BGR) the Carney Creek Quartz Diorite is yellowish-brown and exhibits low relief. The magnetic anomaly of this pluton is swamped by the signature of the Sunny Park Granodiorite to the north. It has low U and Th responses, and shows weak to moderate K anomalies.|16-MAY-23
3649|Carney Creek Quartz Diorite|Type section locality|Along the Clermont-Peak Vale road between 8351-477558 and 8351-483535.  The grid reference is based on the AGD66 datum.|16-MAY-23
3649|Carney Creek Quartz Diorite|Description at type locality|Outcrops of dark grey, fine to medium-grained hornblende diorite and biotite-hornblende quartz diorite.|16-MAY-23
3649|Carney Creek Quartz Diorite|Extent|An east-trending rectangular body 6 km2 in area, centred about 2 km southeast of Sunny Park homestead.|16-MAY-23
3649|Carney Creek Quartz Diorite|Lithology|Dark grey to greenish grey, fine to medium-grained, and variable in composition, ranging from biotite-hornblende quartz diorite and quartz monzodiorite to hornblende diorite.|16-MAY-23
3649|Carney Creek Quartz Diorite|Relationships and boundaries|Intrudes the Anakie Metamorphic Group and is faulted against the Late Devonian to Early Carboniferous Silver Hills Volcanics. Its relationship with the adjacent Sunny Park Granodiorite is uncertain, but is possibly intruded by it.|16-MAY-23
3649|Carney Creek Quartz Diorite|Age reasons|A Devonian age has been assigned to the Carney Creek Quartz Diorite because of its similarity to the Stevenson Quartz Monzodiorite.|16-MAY-23
26297|Carron Rhyolite|Name source|The Carron River, in the northwestern part of Gilbert River 1:100 000 Sheet (7461) area.|16-MAY-23
26297|Carron Rhyolite|Unit history|White (1965) and Branch (1966) included the Carron Rhyolite in their 'Croydon Volcanics' (undivided); Branch (1966), in a tectonic sketch-map accompanying his geological map of the 'Croydon Cauldron Subsidence Area' showed areas of 'rhyodacitic flows' which correspond in part with some of the Carron Rhyolite, particularly in the east. The unit was informally named 'Carron rhyolite' and described by Mackenzie (1983).|16-MAY-23
26297|Carron Rhyolite|Geomorphic expression|The Carron Rhyolite is distinguished by gentle, rounded to moderately steep  and rugged hills with a very sparse, low tree cover and pale-toned grasses. A distinctive, closely-spaced rectilinear drainage pattern is developed in several areas. Areas of altered rock generally form relatively higher, more rugged terrain with a denser tree cover, dominated by Acacia shirleyii ("lancewood").|16-MAY-23
26297|Carron Rhyolite|Type section locality|The type section is between GR 7361-275931 (base) and -293941 (top) near Golden Gate Creek, 8 km northwest of Croydon, and consists of about 500 m of medium to dark grey, fine-grained, crystal-poor rhyolitic ignimbrite with fine, streaked-out, eutaxitic foliation; it is sericitised near the base. The base is a concordant, possibly paraconformable contact with the Nancy Lee Sandstone Member (Parrot Camp Rhyolite), and the top is a conformable contact with greenish-grey, medium-grained, moderately crystal-rich rhyolitic ignimbrite (Idalia Rhyolite).|16-MAY-23
26297|Carron Rhyolite|Description at type locality|(1) along a track to 'Homeward Bound' and 'Waterfall' mines, between GR 7361-334918 on the Croydon-'Tabletop' road (base not exposed; faulted against Idalia Rhyolite) and -349939 (top - conformably overlain by Idalia Rhyolite), where a 400-metre section of typical outcrop with well-developed eutaxitic foliation can ben seen; (2) between GR 7460-049319 and -010349 along the southern side of Dingo Creek, where excellent exposures with contorted eutaxitic foliation and flow-banding can be seen in a 700+ m-thick section which overlies medium-dark grey, medium-grained, crystal-rich rhyolitic ignimbrite (Wonnemarra Rhyolite) and is conformably overlain by Idalia Rhyolite.|16-MAY-23
26297|Carron Rhyolite|Extent|The unit crops out in a discontinuous belt, about 7 to 10 km wide, extending from 10 km northwest of Croydon township to the Gilbert River, then discontinuously along the southwestern side of the river to near "Lake Carlo" homestead (GR 7461-893960). It also crops out discontinuously in a 5 km wide belt along the eastern side of the Gregory Range (between GR 7461-000820 and 7460-055180), and also in a 670 km2 area straddling the Yappar River, about 12 km west of 'Glenora' homestead (around 7460-940980).|16-MAY-23
26297|Carron Rhyolite|Thickness range|The thickness probably averages 500 m, possibly up to 700 m in places; it is commonly difficult to estimate because of deformed foliation and/or complex structure.|16-MAY-23
26297|Carron Rhyolite|Lithology|The Carron Rhyolite consists mostly of dark grey to bluish-grey, densely welded, crystal-poor rhyolitic ignimbrite, which commonly shows fine, streaked out, eutaxitic foliation resembling flow lamination; in places, this foliation is deformed to resemble soft-sediment slump folds (due to plastic flow of hot ignimbrite after compaction and welding). There is also some flow-laminated to banded rhyolite, notably in southeast Esmeralda 1:100 000 Sheet, and rare rhyolitic fine ash tuff and dacitic(?) ignimbrite. The unit typically contains sparsely scattered crystals of quartz, K-feldspar, and plagioclase about 1 mm across, scarce biotite (mostly chloritised), and very rare garnet; it also typically contains sparsely scattered graphite pellets up to 5-7 mm long, as well as disseminated graphite flakes. The rocks are moderately to intensely altered (mostly to sericite) over extensive areas, particularly in the north of Croydon and Gilbert River 1:100 000 Sheets, where they are generally pale green.|16-MAY-23
26297|Carron Rhyolite|Relationships and boundaries|The Carron Rhyolite overlies, apparently conformably, B Creek Rhyolite, and, in parts of the north of Croydon 1:100 000 Sheet area, Parrot Camp Rhyolite; it overlies, with apparent unconformity, Malacura Sandstone in a small area near GR 7461-810020. It is overlain, with apparent conformity, by Idalia Rhyolite, and is intruded by Esmeralda, Mooremount, Chadshunt, Olsens, and Nonda Granites, and by several small, unnamed granitic stocks. It is unconformably overlain by Permian volcanic rocks and sediments (Bullseye Rhyolite), and by Mesozoic and younger sediments.|16-MAY-23
26297|Carron Rhyolite|Age reasons|The Carron and Idalia Rhyolites were dated as 1400 +/- 75 m.y., i.e. Middle Proterozoic, by Richards & others (1966) and Black (1973).|16-MAY-23
29310|Carrs Granite|Name source|The unit is named after Carrs Creek which drains part of the southeastern outcrop area.|16-MAY-23
29310|Carrs Granite|Unit history|Previously mapped as Herbert River Granite (Best, 1962;  de Keyser & Wolff, 1964).|16-MAY-23
29310|Carrs Granite|Geomorphic expression|The adamellite forms gently undulating to hilly terrain with scattered pavements, boulders and bouldery outcrops.  The country underlain by the unit has an open drainage pattern and is characterised by medium tones on aerial photographs.|16-MAY-23
29310|Carrs Granite|Type section locality|The designated type area is on the southern side of the Chillagoe-Bolwarra road, about 18 km southwest of Chillagoe, at GR 2223 80905.  The grid reference is based on the AGD66 datum.|16-MAY-23
29310|Carrs Granite|Description at type locality|There the adamellite forms large rounded boulders and extensive pavements.|16-MAY-23
29310|Carrs Granite|Extent|The unit forms an elongate, northwesterly-trending pluton ~15 to 20 km southwest of Chillagoe.  It crops out over an area of ~75 km2 in MUNGANA, and extends into CHILLAGOE (~25 km2).|16-MAY-23
29310|Carrs Granite|General description|STRUCTURE AND METAMORPHISM::  The unit forms massive, non-foliated outcrops.  It is surrounded by a narrow contact metamorphic aureole in which hornfelses containing cordierite porphyroblasts up to 3 cm across are locally developed in schistose metasediments of the McDevitt Metamorphics adjacent to the contact.MINERALISATION:: No ore deposits of economic potential have been found in the adamellite.|16-MAY-23
29310|Carrs Granite|Lithology|Fine to medium-grained, grey to pale pink (altered), slightly porphyritic hornblende-biotite adamellite (Fig. ? , Table?   ) is the predominant rock type.  Minor biotite leucogranite and aplite are present locally.  The adamellite does not show a marked decrease in grainsize adjacent to contacts with the country rocks, in most places.The Carrs Granite consists of quartz, plagioclase, K-feldspar, biotite, hornblende, and accessory and secondary minerals.  Rounded mafic enclaves up to 5 cm across are fairly common.  Adamellite exposed at GR ??        contains inclusions up to ~1 m across of more mafic granodiorite and diorite.  The adamellite also contains small secondary iron oxide-stained patches which probably indicate the former presence of pyrite.Quartz forms irregular, anhedral grains (up to 1 mm long), generally characterised by undulose extinction.  The grains commonly form rounded or ovoid aggregates resembling phenocrysts, up to 1 cm across.K-feldspar occurs as subhedral to anhedral grains up to 2 mm across and as sparse scattered phenocrysts up to about 1 cm long.  It is commonly microperthitic; rare grains also show cross-hatched twinning typical of microcline.  Small inclusions of quartz, biotite, and plagioclase are present in many grains.  Granophyric intergrowths characterise some specimens.Plagioclase forms white to pale pink (altered), complexly zoned, subhedral laths up to about 6 mm long.  Biotite forms euhedral flakes (up to ~2 mm x 1 mm) pleochroic from dark red-brown to straw yellow, and containing small inclusions of opaque oxide and zircon.  In some specimens hornblende is present in roughly equal proportions to biotite;  in others it is scarce, probably at least partly the result of preferential replacement by chlorite.  Hornblende tends to form euhedral to subhedral grains up to about 1 mm long and pleochroic from bluish green to pale yellowish green.  Accessory minerals are mainly opaque oxide(s) as scattered euhedral to subhedral grains up to 0.3 mm across), zircon (relatively common), zoned allanite, and sphene.|16-MAY-23
29310|Carrs Granite|Relationships and boundaries|The Carrs Granite intrudes the Dargalong and McDevitt Metamorphics, Nundah Granodiorite, and the Ootann(?) and Quaker Granites.  It is cut by rare dykes of strongly porphyritic, relatively mafic microgranite (sensu lato) and by several pods and dykes of pale pink, fine-grained biotite leucogranite, which tend to form hills and ridges - most of these bodies have not been delineated on the map.  The leucogranite contains small miarolitic cavities (e.g., at GR 2220 80902).  The dykes of strongly porphyritic microgranite have northwesterly and possibly northeasterly trends and extend up to ~14 km.  Phenocrysts consist mainly of white to dark pink feldspar (up to ~3 cm), together with subordinate quartz (up to ~1 cm).|16-MAY-23
29310|Carrs Granite|Age reasons|The adamellite has not been isotopically dated, but it is most probably Late Carboniferous - all units of the northern Tate Batholith isotopically dated have yielded ages of ~300 Ma.|16-MAY-23
29310|Carrs Granite|Comments|The Carrs Granite is similar mineralogically and chemically to Late Carboniferous granites of the Ootann Supersuite mapped farther east (in CHILLAGOE).  The pronounced northwesterly-elongation of the pluton, more or less parallel to the Palmerville Fault, is noteworthy.  It probably indicates that emplacement of the pluton was influenced by regional structures related to the Palmerville Fault.|16-MAY-23
29310|Carrs Granite|References|BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.DE KEYSER, F., & WOLFF, K.W., 1964:  The geology and mineral resources of the Chillagoe area.  Bureau of Mineral Resources, Australia, Bulletin 70.|16-MAY-23
3701|Carters Bore Rhyolite|Name source|Carters Bore, on Black Creek, 30 km southwest of Mount Isa, latitude 20o56'S, 139o18'25"E (6756 239841).|16-MAY-23
3701|Carters Bore Rhyolite|Geomorphic expression|The Carters Bore Rhyolite is a recessive unit and is exposed on weathered pediments in alluviated valleys.|16-MAY-23
3701|Carters Bore Rhyolite|Type section locality|About 100 m north of a track that heads west from Six Mile Mill on Mingera Creek, 48 km northwest of Mount Isa, from latitude 20o25'45"S, longitude 139o9'20"E (6757 076398) to latitude 20o25'40"S, longitude 139o9'12"E (6757 074401). The type section contains approximately 200 m of pink, rather weathered sheared porphyritic rhyolite. |16-MAY-23
3701|Carters Bore Rhyolite|Extent|Mount Isa and Kennedy Gap 1:100 000 Sheet area; as discontinuous areas along the May Downs fault zone, south for 30 km from a point 25 km north-northwest of Carters Bore, in a narrow area from near the May Downs gold mine to the Barkly Highway between 8 and 10 km west of 29-Mile Bore and then southeast to about 4 km south of 29-Mile  Bore, and in several isolated outcrops to the north of the Highway (near 085485, fro 5 km north of 188485, and for 8 km northeast of 117770).|16-MAY-23
3701|Carters Bore Rhyolite|Thickness range|At least 200 m; the top of the unit is probably not exposed.|16-MAY-23
3701|Carters Bore Rhyolite|Lithology|Quartz-microcline porphyry, rhyolite tuff, minor agglomerate, muscovite schist containing relict quartz phenocrysts, and flow-banded rhyolite. In some sections the phenocrysts tend to be smaller and the colour of the rhyolite paler towards the top of the unit. Minor flows of altered basalt ar present in the north of the Kennedy Gap 1:100 000 Sheet area. |16-MAY-23
3701|Carters Bore Rhyolite|Relationships and boundaries|The Carters Bore Rhyolite overlies the Judenan Beds possibly slightly unconformably. It is overlain unconformably by the Gunpowder Creek Formation and an equivalent unit, the Mingera Beds. The Rhyolite contrasts sharply with the underlying and overlying arenaceous rocks.|16-MAY-23
3701|Carters Bore Rhyolite|Age reasons|Carpentarian (Middle Proterozoic). Page (pers. comm., 1976) obtained a Rb-Sr model age of 1555+/-20 m.y. and a U-Pb zircon age of 1678+/-1 m.y. for this unit. He atatributed the discrepancy in ages to a disturbance of the Rb-Sr total rock system.|16-MAY-23
3701|Carters Bore Rhyolite|Comments|The quartz grains in the Carters Bore Rhyolite typically have a bipyramidal habit similar to the quartz in the northwestern Sybella Granite. The groundmass of the Rhyolite is finer grained and it is possible that the Rhyolite is an extrusive equivalent of this high-level intrusive phase of the Sybellla Granite. Acid volcanics recorded from the Seymour River area 170 km north-northwest of Mount Isa may be equivalent to the Carters Bore Rhyolite.|16-MAY-23
3863|Central Creek Granodiorite|Name source|Central Creek, which joins Tomahawk Creek at 8451-529344.  The grid reference is based on the AGD66 datum.|16-MAY-23
3863|Central Creek Granodiorite|Geomorphic expression|The granite forms low to moderately undulating terrain and poorly exposed with rare, usually weathered, boulder-sized outcrop.   The Central Creek Granodiorite cannot be distinguished from the adjacent Mount Newsome Granodiorite on the Landsat TM imagery. No consistent geophysical response can be identified for this unit as currently mapped.|16-MAY-23
3863|Central Creek Granodiorite|Type section locality|Outcrops of grey biotite medium-grained granite at 8351-343253.  The grid reference is based on the AGD66 datum.|16-MAY-23
3863|Central Creek Granodiorite|Extent|A V-shaped body 20 km2 area, in the southwest of the Retreat Batholith.|16-MAY-23
3863|Central Creek Granodiorite|Lithology|Light grey to white, fine to medium-grained biotite granite.|16-MAY-23
3863|Central Creek Granodiorite|Relationships and boundaries|Intrudes Anakie Metamorphics and is unconformably overlain by Late Devonian to Early Carboniferous Silver Hills Volcanics. The relationships with the adjacent Mount Newsome Granodiorite and Kilmarnock Granodiorite are unknown. It is distinguished from the Mount Newsome Granodiorite and Kilmarnock Granodiorite by an absence of hornblende.|16-MAY-23
3863|Central Creek Granodiorite|Age reasons|The precise age is unknown. A Devonian age has been assigned because of the similarities to other components of the Retreat Batholith, for which Middle to Late Devonian ages have been determined.|16-MAY-23
33435|Chahpingah Meta-Igneous Complex|Name source|The unit is named after the locality of Chahpingah situated between Kingaroy and Durong and is herein renamed the Chahpingah Meta-Igneous Complex.|16-MAY-23
33435|Chahpingah Meta-Igneous Complex|Unit history|The unit was first recognised as an area of undifferentiated Palaeozoic metamorphics by Exon & others (1968), Reiser (1971) and Murphy & others (1976) during reconnaissance mapping of the Chinchilla and Gympie 1:250 000 sheets. The unit was studied in more detail by Hubbard (1985), and this mapping was followed up by Holcombe & others (1997) who first applied the term 'Chahpingah Complex', naming the unit after the locality of Chahpingah, 16 km south-east of the village of Durong.  The latter workers studied the structure of the unit, and undertook limited Ar/Ar age dating of the rocks.|16-MAY-23
33435|Chahpingah Meta-Igneous Complex|Geomorphic expression|The unit forms low undulating scrubby country.  Exposure is generally poor, although moderate to good outcrops occur on some hillsides and in stream pavements.|16-MAY-23
33435|Chahpingah Meta-Igneous Complex|Extent|The unit forms two large adjoining lobate outcrop areas (each around 100 km2), straddling the JANDOWAE/BOONDOOMA sheet boundary and extending to the south-east into KINGAROY and MURGON.|16-MAY-23
33435|Chahpingah Meta-Igneous Complex|Lithology|The dominant rock type is a cream to grey, fine to medium grained, strongly foliated, banded granitic to granodioritic biotite gneiss.  The gneiss commonly contains scattered layer-parallel quartz and locally ptygmatically folded pegmatite veins that in many places appear to be migmatitic in origin.  Massive cross-cutting, steeply-dipping pegmatite and fine to locally medium grained, equigranular granite dykes also occur, as well as layer-parallel sills and small intrusions.  Small areas of mica schist also present in places. The gneiss locally grades into massive relatively homogeneous biotite-rich microgranite.  Biotite-rich xenoliths are common in these meta-granites, where they locally form discontinuous trains representing remnants of earlier meta-sedimentary layering.  The internally-laminated xenoliths are locally tightly to isoclinally folded with the dominant foliation (here designated Sm) as axial plane. Remnant "ghost layering" is visible in the granitic matrix between the xenoliths, suggesting derivation of the rock fom in situ melting of a meta-sedimentary protolith.  In many places the xenolith trains define well-developed intersection lineations on foliation surfaces as well as a parallel lineation defined by biotite clots. These features are well exposed adjacent to the Burrandowan road around AMG 357200 7063500.  Similar lineations defined by biotite alignment occur elsewhere throughout the unit, but some of these may represent stretching lineations defining directions of tectonic transport. The major Sm foliation in the gneiss is defined by alternating mafic biotite-rich layers and quartzofeldspathic layers.  The component minerals are mainly quartz and biotite, locally combined with K-feldspar, plagioclase, muscovite and/or garnet.  In rare cases, small rootless isoclinal fold hinges of the gneissic lamination are present parallel to the main layering, indicating a transposition origin for the Sm foliation.  Isoclinally folded quartz veinlets also occur locally. At one locality (road cut at GR355117/ 7063690), the usually massive granitic gneiss contains occasional layers up to 20cm thick of aplitic material, which may either represent remnant lithological layering or a series of parallel igneous veins. The layers have been folded into trains of open to isoclinal parasitic folds with the dominant Sm foliation as axial plane, indicating that the layers predate the dominant gneiss-forming deformation event.  In the eastern part of the complex on KINGAROY, small-unmapped bodies of strongly foliated K-feldspar-phyric biotite granite containing thin (to 5cm) pegmatite veins intrude the gneiss.  In this region, the complex is also locally intruded by medium grained biotite granite to microgranite (e.g. at AMG 381192 7039776; 381070 7040312; and 381995 7041270).  Foliated gneiss locally comprises up to almost 50% migmatitic leucogranite sweats (e.g. the road verge at AMG 353989 7052319).  Grid references are Based on the AGD66 datum.|16-MAY-23
33435|Chahpingah Meta-Igneous Complex|Relationships and boundaries|The unit is intruded by various phases of the Boondooma Igneous Complex, and has a concordant relationship with the adjacent the Mountefontein Metamorphics, which it probably syntectonically intruded and metamorphosed. Basalts of the Tertiary Main Range Volcanics and Late Triassic sediments of the Surat basin unconformably overlie the unit.  The unconformity between the basal sediments of the Surat Basin and the older gneisses is well exposed at AMG 352307 7050672.  The basal conglomerate of the Surat Basin is a quartz-rich conglomerate (derived from pegmatite bodies in the gneiss) and contains rutile concentrations along the bedding planes. The grid reference is based on the AGD66 datum.|16-MAY-23
33435|Chahpingah Meta-Igneous Complex|Structure and Metamorphism|The unit is interpreted to represent a series of synkinematic granitic intrusions, intruded during a period of deep level crustal scale extension that produced the strong Sm foliation. The unit is sporadically cut by regular to chaotic broad crenulations, warps and folds (the axial planes of which are here designated S2) which may reflect the presence of large scale regional folding of the gneissic layering.|16-MAY-23
33435|Chahpingah Meta-Igneous Complex|Age reasons|The unit has been radiometrically dated by the Ar/Ar method, as well as by U-Pb zircon SHRIMP dating.  The former method gives ages in the 250 Ma range (Rod Holcombe, personal communication) whereas the latter gives a magmatic age of Late Carboniferous (303Ma) age (Cranfield & others, 1998) which is considered to be the age of metamorphism, melting and emplacement of the essentially synkinematic granitic complex.  The younger ages are considered to be reset by the effect of the Hunter-Bowen orogeny in this area.|16-MAY-23
33435|Chahpingah Meta-Igneous Complex|Correlations|The unit probably represents a series of syntectonic intrusions associated with the metamorphism of the adjacent Mountefontein Metamorphics. This intrusive/metamorphic sequence is similar in age and origin to comparable granites and metamorphics mapped in the North D¿Aguilar Subprovince on the eastern margin of the Esk Trough - the Claddagh, Karandah and Gallangowan Granodiorites, and associated metamorphics of the Claddagh- Manumbar assemblage of Little (1993).|16-MAY-23
33435|Chahpingah Meta-Igneous Complex|Geophysical Expression|The unit has a uniformly low magnetic response on geophysical images, but has a characteristic pale green (Th-rich) tinge on the K-Th-U (RGB) ternary radiometric images|16-MAY-23
33435|Chahpingah Meta-Igneous Complex|References|CRANFIELD, L.C., DONCHAK, P.D., RANDALL, R.E., CROSBY, G.C., & OSBORNE, J.1998, Investigations in the Yarraman Sub-Province, southeast Queensland - Preliminary results of 1997 field work. Queensland Government Mining Journal, 99 (No 1160), 11-22. Regional Geology. **EXON, N.F., REISER, R.F., JENSEN, A.R., BURGER, D., &  THOMAS, B.M.,1968,The Geology of the Chinchilla 1:250 000 Sheet Area, Bureau of Mineral Resources, Australia, Record 1968/53. **HUBBARD, B.J.,1985, Reconnaisance geology of the Chahpingah Area, South-East Queensland. Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education. **LITTLE, T.A.,1993,Geology of the northern part of the North D'Aguilar Block, southeast Queensland. Department of Minerals and Energy, Record 1993/3. **MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96, Regional Geology, Gympie 1:250 000 Sheet. **REISER, R.F.1971,Chinchilla, Qld - 1:250,000 Geological Series. Bureau of Mineral Resources, Geology and Geophysics, Australia, Explanatory Notes, SG/56-9.|16-MAY-23
38892|Chalmers Formation|Name source|This formation is named after Mount Chalmers.|16-MAY-23
38892|Chalmers Formation|Geomorphic expression|Topographic expression is generally low to moderate for the Chalmers Formation with higher terrain found adjacent to rhyolite to dacite domes. The drainage ranges from a close to widely spaced dendritic pattern.|16-MAY-23
38892|Chalmers Formation|Type section locality|The type area is located 300 m south of Mount Archer, from GR 252161 7416360 to GR 251641 7415509, and consists of interbedded thick to very thick beds of grey to olive siltstone, fine sandstone, and grey to green-grey, volcaniclastic, feldspatholithic sandstone and breccia (Figure 6).|16-MAY-23
38892|Chalmers Formation|Extent|The Chalmers Formation is the most extensive unit in the Berserker Group. It extends from Mount Belmont in the north to the Mount Larcom area in the south.|16-MAY-23
38892|Chalmers Formation|General description|The Chalmers Formation is a new geological unit encompassing sediments similar to those in the Lakes Creek Formation interbedded with rhyolitic to andesitic volcaniclastics. It also contains fossil rich beds slightly younger than those in the Lakes Creek Formation, situated in the middle to upper part of the unit.|16-MAY-23
38892|Chalmers Formation|Thickness range|The Chalmers Formation is considered to be approximately 600 m thick. This is based on two criteria. First, although the unit is gently to moderately folded, its regional orientation is relatively flat lying; and second, the unit has been identified from sea level to close to the top of many of the peaks in the region, including the highest, Mount Archer at 604 m.|16-MAY-23
38892|Chalmers Formation|Lithology|The Chalmers Formation is composed of sediments similar to the Lakes Creek Formation as well as pyroclastic rocks and granule to pebble volcanic breccia containing siltstone to sandstone clasts and felsic to intermediate volcanic clasts (Figure 7). Disrupted contacts between underlying siltstone-sandstone and overlying volcanic breccia can be seen at a road cutting 1 km SSE of Mount Archer, and also in Nankin Creek, 2 km SW of Mount Chalmers. The fossiliferous beds consist of grey-green, medium to thick bedded sandstone and granule to pebble breccia.A thick bedded calcareous sandstone containing Lower Permian fossils was mapped 1 km south of Mount MacDonald. A similar looking horizon of interbedded calcareous  and non-calcareous sandstone found 5 km further south, and along strike, was unfossiliferous and contained well rounded, pebble to cobble sized sedimentary or volcanic clasts (Figure 9).Approximately 1.5 km NNW of Broadmount there is a relatively small area of schist and tectonite which is adjacent to the Tungamull-Yarrol Fault (Figure 10). Their origin is uncertain as is their relationship with the Chalmers Formation. The most likely explanation is that these rocks are Chalmers Formation which were deformed during the westerly compressional event in the latest Permian. their orientation is slightly south of west.The volcaniclastic rocks are generally grey to green-grey, medium to very thick bedded, matrix supported to clast supported, and moderately to poorly sorted. These rocks contain crystals, lithics and pumice (Figure 8). The crystals are mostly feldspar and to a lesser extent quartz with some rocks containing rare hornblende, pyroxene or biotite. Feldspar is fine to coarse grained (up to 6mm), quartz is fine to medium grained, and mafic minerals are mostly fine grained. Lithics are sedimentary and volcanic, although in many cases they are difficult to distinguish from each other. Volcanic clasts dominate, and are granule to cobble in size, usually angular to subangular, and range from rhyolitic to andesitic in composition. The pyroclastic rocks are generally unwelded with rare fiamme. Pumice fragments are up to 50 mm in length, angular, either elongate or irregular in shape, and are flattened due to compaction. Tube pumice is common.|16-MAY-23
38892|Chalmers Formation|Depositional environment|The Chalmers Formation is considered to represent incursion of volcaniclastic sands and breccias into a sedimentary basin receiving silts and sands equivalent to the Lakes Creek Formation. The fauna of brachipods and molluscs indicate water depths of around 30-50 m, and no deeper than 200 m. Good preservation of the fossils suggests that the sediments were deposited below wave base. Sainty (1992) suggests that both the macrofossils and trace fossils indicate a shallow-marine shelf setting.|16-MAY-23
38892|Chalmers Formation|Fossils|Marine fossils correlative with faunas of the Lower Permian Buffel Formation of the Bowen Basin have been collected 2 km SW of Mount Chalmers, 1 km SE of Mount MacDonald, and 2 km NW of Mount Kilner. These include Echinalosia warwicki (Maxwell, 1954), Terrakea geniculata (Waterhouse,1986), Eurydesma sp, relatively few fenestellid byrozoans, and lack Taeniothaerus n. sp. There is also rare Euryphyllum sp. The ranges of the fossils found in the Chalmers Formation are slightly younger than those found in the Lakes Creek Formation (Figure 12).Sainty (1992) observed trace fossils throughout sediments now assigned to the Chalmers Formation. The burrows include Teichichnus, Planolites, and abundant vertically orientated, upward-branched traces, with scattered Rhizocorallium- and Zoophycus-type burrows. These trace fossils belong to the Cruziana ichnofacies.|16-MAY-23
38892|Chalmers Formation|Relationships and boundaries|The Chalmers Formation is interpreted to be laterally equivalent to the Lakes Creek Formation, although mapping in the Mount Archer area suggests that the Chalmers Formation locally rests on Lakes Creek Formation (Figure 3). In the Mount Larcom area, mapping suggests that the unit unconformably overlies Lower Carboniferous Rockhampton Group. An angular unconformity is inferred.Five kilometres north of Broadmount, in an area immediately east of the Tungamull-Yarrol Fault, is a large outcrop of rock similar to the Chalmers Formation. Its relationship with the Devonian-Carboniferous Coastal Block is uncertain but the Permian unit would persumably underlie the older rock. This area was defined as Lower Permian Berserker beds on the 1:250 000 Rockhampton geological series (1974) but was later interpreted as the Balnagowan volcanic member of the Devonian-Carboniferous Doonside Formation on the 1:100 000 Rockhampton Region geological special (1984).The Chalmers Formation is intruded by rhyolites and dacites, andesite dykes and gabbro and granodiorite bodies forming sharp, shallow to steep contacts. The U-Pb zircon dates obtained from the Ellrott Rhyolite suggests the latter was synchronous with the deposition of at least the upper half of the Chalmers Formation.|16-MAY-23
38892|Chalmers Formation|Age reasons|A U-Pb zircon age of 277±4 Ma (Early Permian) was obtained from a volcaniclastic bed interpreted to be in the middle of the Chalmers Formation (M. Fanning, personal communication, 1998).|16-MAY-23
38892|Chalmers Formation|Defn Reference|SOURCE OF INFORMATION --Crouch. S, Parfrey. S, and Taube. A  [DATE ?]. 'Geology, tectonic setting and metallogenesis of the Berserker Subprovince, northern New England Orogen'. Supplied by Ian Withnall (GSQ), September 2008.(Incomplete reference)|16-MAY-23
39079|Champion Hills Diorite|Name source|Campbell (1952) informally called the unit the 'Champion Hills Basic Diorite', but the name has been modified to Champion Hills Diorite for this report.|16-MAY-23
39079|Champion Hills Diorite|Unit history|This unit was first mapped and informally described by Campbell (1949, 1952).  Other workers who have studied the unit are McPhee (1974) Costello (1975), Reimers (1977), Ross (1988) and Murphy (1989) from the University of Southern Queensland and Hegarty (1981), McCabe (1982) and Slijderink (1988) from the Queensland University of Technology.|16-MAY-23
39079|Champion Hills Diorite|Geomorphic expression|The larger bodies of Champion Hills Diorite form hilly to sloping country 140 to310 m above sea level, that is generally well cleared and used for grazing.  Many of the smaller bodies occur as intrusions in the Hampton Road Rhyolite, which is rugged and well forested.|16-MAY-23
39079|Champion Hills Diorite|Type section locality|The type area designated by Campbell (1952) for this unit is accepted for this report.|16-MAY-23
39079|Champion Hills Diorite|Extent|The unit covers an area of about 9.5km2 south of the Esk Hampton road.  The larger bodies occur in the vicinity of Oaky Creek and Verandah Creek.  Bodies with a north south elongation occur near the intersection of Verandah Creek and Buaraba Creek.  Scattered small diorite and gabbroic intrusions between Buaraba Creek and the Esk Hampton road have also been included in this unit.|16-MAY-23
39079|Champion Hills Diorite|Lithology|Rock types described from the unit include gabbro, dolerite, pyroxenite, basic diorite, and quartz diorite.  Rocks are grey green, occasionally dark grey, when fresh and range from fine to coarse grained, porphyritic (up to 7mm) in parts.  Chlorite alteration is common.McPhee (1974) describes thin sections from the unit.  An ophitic and subophitic texture is common with replacement of augite by actinolitic hornblende and overgrowths of hornblende over augite.  At AMG 432400 6975000 the rock type is a plagioclase dolerite containing 65% plagioclase, 19% augite, 10% hornblende and minor chlorite and leucoxene.  The augite was partially altered to chlorite, secondary hornblende and minor epidote.At AMG 430600 6976200 is an altered dolerite containing 51% plagioclase, 45% hornblende/augite, and minor magnetite and chlorite.  Augite was almost completely replaced by actinolitic hornblende and remnant ophitic texture remains.  At AMG 429200 6975300 is exposure of dark grey gabbro containing 54% plagioclase, 27% augite and 15% hornblende with minor magnetite.  Fibrous green amphiboles occur as alteration products of hornblende.At AMG 428400 6974500 is an exposure of pyroxenite containing >70% pyroxene and plagioclase, hornblende, magnetite and quartz.  McPee comments that `pyroxene content is variable¿ in the area so this rock may represent an extreme example of pyroxene enrichment.Campbell (1952) identified plagioclase (mostly andesine), titaniferous and common augite, chlorite and golden yellow chlorite, clinozoisite, zircon, magnetite, ilmenite and quartz in the dioritic rocks.  A gabbro at AMG.431000 6975100 contained calcic plagioclase, diallage, augite, hornblende, sphene, uralite, quartz and chlorite, with ophitic structures common. Ilmenite is present as skeletal crystals and inclusions in augite.  Murphy (1989) suggested that several small gabbroic/doleritic outcrops in the North Buaraba Creek area are part of one intrusive event that includes all of the gabbroic rocks of the region.The grid references are based on the AGD66 datum.|16-MAY-23
39079|Champion Hills Diorite|Relationships and boundaries|The `Champion Hills Diorite' intrudes the Cressbrook Creek Group.  Roof pendants of Cressbrook Creek Group suggest that it is the upper parts of the batholith that are exposed in the main outcrop area of the unit.  Porphyry dykes of the South Buaraba Microdiorite and the Buaraba Granodiorite intrude the Champion Hills Diorite.  The Woogaroo Sub Group unconformably overlies the unit.  Ross (1988) also described a slickensided contact between lithic sandstones of the Woogaroo Sub Group and Champion Hills Diorite at AMG.432800 6975200.The grid references are based on the AGD66 datum.|16-MAY-23
39079|Champion Hills Diorite|Age reasons|Porphyry dykes of the South Buaraba Microdiorite, which is assigned an early to mid Triassic age, intrude the Champion Hills Diorite.  The Champion Hills Diotite intrudes the late Permian age Buaraba Mudstone of the Cressbrook Creek Group.  The Champion Hills Diorite has been assigned an Early to Middle Triassic age.|16-MAY-23
39079|Champion Hills Diorite|Comments|GEOCHEMISTRY:: No samples for geochemistry were processed as part of the Yarraman Project.ASSOCIATED MINERALISATION:: Reimers (1977) states that `in some areas chalcopyrite and pyrite are found in a disseminated form in the dolerites.¿  No further details of this mineralisation are available.GEOPHYSICAL EXPRESSION:: Magnetic response of this unit is variable and is significantly high in the vicinity of AMG 430000 6977000.  Similar high responses to the east of Verandah Creek may indicate that small areas of Champion Hills Diorite also occur beneath the cover of Woogaroo Sub Group.  The ternary radiometric image has shows generally dark tones over the outcrop area of the unit.|16-MAY-23
39079|Champion Hills Diorite|References|CAMPBELL, K.S.W.,1952,The geology of the Cressbrook-Buaraba area,"University of Queensland.  Department of Geology Papers (New series), Regional Geology.COSTELLO, C.M.1975,The geology of part of the Buaraba Creek area, north of Gatton, South-East Queensland. Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.HEGARTY, R.A.,1981,Geology of the Buaraba District, Southeast Queensland, Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology.McCABE, S.,1982, Geology of the South Bauraba District, South-East Queensland, Unpublished honours thesis, Department of Geology, Queensland University of Technology.MCPHIE, K.A., 1974,The geology of the Verandah-Middle Creek area, Buaraba district, southeast Queensland, Unpublished Thesis, Department of Geology, Darling Downs Institute of Advanced Education.MURPHY, T.J.,1989,The geology surrounding the north branch of the Buaraba Creek South - Eastern Queensland. Unpublished Thesis, Department of Geology, Darling Downs Institute of Advanced Education.REIMERS, D.W.,1977,The geology of the North Buaraba - Oaky Creek area, Buaraba district, South east Queensland.  Unpublished Thesis, Department of Geology, Darling Downs Institute of Advanced Education.ROSS, L.A., 1988,An investigation of the geology and fault relations of the Western Border Fault of the South Western Esk Trough. Unpublished thesis, Department of Geology, Darling Downs Institute of Advanced Education.SLIDJERINK, P.,1988, Geology of the Buaraba Creek-North Branch project area, Unpublished Bsc honours thesis, Department of Geology, Queensland University of Technology.|16-MAY-23
27078|Chinaman Creek Limestone|Name source|Chinaman Creek (shown on some maps as Graveyard Creek), which joins Graveyard Creek at 7859-669696.  The grid reference is based on the AGD66 datum.|16-MAY-23
27078|Chinaman Creek Limestone|Unit history|The unit was referred as 'A' lens of the Broken River Formation (now Group) by White (1965), and was subsequently defined as a member of the Broken River Formation by Jell (1968).  It was raised to formation status by Withnall & others (1988), but was not redefined.|16-MAY-23
27078|Chinaman Creek Limestone|Geomorphic expression|The unit forms a series of ridges and low bluffs of limestone with karst features (including caves), separated by recessive areas corresponding to siliciclastic intervals.|16-MAY-23
27078|Chinaman Creek Limestone|Type section locality|South Chinaman Creek between 7859-604689 (base) and 597689 (top).  The section described by Jell (1968) is 640 m thick and contains three main limestone units each separated by siliciclastic intervals.  The grid references ares based on the AGD66 datum.|16-MAY-23
27078|Chinaman Creek Limestone|Description at type locality|Contains three main limestone units each separated by siliciclastic intervals::  The lower limestone is 152 m thick and consists of unbedded detrital bioclastic  calcarenite, bedded calcarenite, calcareous mudstone, coralline limestone, and interbedded mudstone and sandstone.  It is overlain by 60 m of sublithic to lithic sandstone with some small bioherms and associated detrital limestone interbedded.  The middle limestone is 230 m thick and consists of bedded calcarenite and calcareous shale with a few large lenses of non-bedded coarse bioclastic calcarenite and calcirudite, biostromal limestone and incipient bioherms.  About 45 m of fine to coarse-grained lithic sandstone with occasional shale and conglomerate interbeds overlie the middle limestone.The upper limestone consists of 152 m of bedded calcarenite, biomicrite, calcareous mudstone, thick bioclastic calcarenite, calcilutite, and interbeds of lithic sandstone.|16-MAY-23
27078|Chinaman Creek Limestone|Extent|A narrow, linear belt up to 1 km wide and 10.5 km long, west of 'Pandanus Creek' and trending north from the Tank Creek Fault to the hinge of the Six Mile Syncline.|16-MAY-23
27078|Chinaman Creek Limestone|Thickness range|Up to 650 m.|16-MAY-23
27078|Chinaman Creek Limestone|Lithology|Mainly thin to very thick, massive beds of bioclastic calcarenite and calcirudite, with thinner biomicrite and sporadic interbeds of calcareous mudstone, fine to coarse-grained lithic to quartzose sandstone, and pebble conglomerate.  Bioherms 2 km long and 30 m thick occur in the lower part of the sequence|16-MAY-23
27078|Chinaman Creek Limestone|Fossils|The limestones contain rich shallow marine faunas including corals and stromatoporoids, and lesser brachiopods, bivalves, gastropods, crinoids, trilobites, bryozoa, ostracods, and conodonts and algae.|16-MAY-23
27078|Chinaman Creek Limestone|Relationships and boundaries|The unit is part of the Wando Vale Subgroup of the Broken River Group.  It conformably overlies the Tank Creek Sandstone north of 'Pandanus Creek', whereas to the south it directly overlies the Shield Creek Formation, probably disconformably.  At its northern end it is abruptly abutted by undifferentiated sandstone and mudstone of the Wando Vale Subgroup.|16-MAY-23
27078|Chinaman Creek Limestone|Age reasons|Studies of the corals (Jell, 1967; Jell in Wyatt & Jell, 1967) and conodonts (Telford, 1975; Mawson & Talent, 1987) indicate that the unit ranges from middle Emsian to middle Givetian in age.  Three rugose coral faunas were recognised.  See the summary in Withnall & others (1988).|16-MAY-23
27078|Chinaman Creek Limestone|References|JELL, J.S., 1968:  New Devonian rock units of the Broken River Embayment, north Queensland.  Queensland Government Mining Journal, 69, 6-8.MAWSON, R., 1987:  Documentation of conodont assemblages across the Early Devonian-Middle Devonian boundary, Broken River, north Queensland, Australia.  Courier Forschungs-Institut Senckenburg, 92, 251-273. ***TELFORD, P.G., 1975:  Lower and Middle Devonian conodonts from the Broken River Embayment, north Queensland, Australia.  Special Papers in Palaeontology, 15. ***WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. ***WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5. ***WYATT, D.H. & JELL, J.S., 1967:  Devonian of the Townsville hinterland, Queensland, Australia; in Oswald, D.H. (editor), International Symposium on the Devonian System, Volume 2.  Alberta Society of Petroleum Geologists, Calgary, 99-105.|16-MAY-23
4064|Chumvale Breccia|Unit history|The Chumvale Breccia was formally defined by Carter et al. (1961) with reference to a type section exposed about 2 km northeast of Butcher Bore, which is about 22 km west southwest of Cloncurry and 3 km south  of the Barkly Highway.|16-MAY-23
4064|Chumvale Breccia|Type section locality|Of Carter et al. (1961):  type section exposed about 2 km northeast of Butcher Bore, which is about 22 km west southwest of Cloncurry and 3 km south  of the Barkly Highway.|16-MAY-23
4064|Chumvale Breccia|Extent|Detailed mapping has shown that the western-most outcrop mapped by Carter et al. (1961) consists largely of Tommy Creek Microgranite (Derrick at al., 1971). Further outcrops have been mapped at and near the top of the Overhang Jaspilite extending for 10 km to the west of Butcher Bore and for about 35 km around the Duck Creek Anticline east and southeast almost to Overhang mine. it has been mapped in the Marraba 1:100 000 sheet area only but may extend south of the Overhang mine into the Malbon 1:100 000 sheet area.|16-MAY-23
4064|Chumvale Breccia|Lithology|Typically it consists of irregular fragments of jaspilite and ferruginous quartzite obviously derived from the Overhang Jaspilite, contained in a siliceous, or less commonly calcareous matrix. Iron amd manganese staining, typical of the Jaspilite, is also characteristic of the Breccia.|16-MAY-23
4064|Chumvale Breccia|Depositional environment|Genesis: Two main processes have been proposed for the formation of the Chumvale Breccia. Derrick et al. (1971) suggested that it formed from the Overhang Jaspilite in stages: a) Folding and faulting of the Jaspilite results in the fracturing of  jaspilite and quartzite beds interbedded with carbonate; b) Continued deformation accompanied by disorientation of the quartzite blocks, and recrystallisation of the carbonate groundmass, forms a quartzite/jaspilite clast-carbonate matrix breccia; c) Leaching of the carbonate matrix and replacement by silica forms  the siliceous breccia as an end product. The silicification may be related to faulting and possibly to much younger laterisation. An alternative process is the weathering and selective leaching of carbonate from the uppper jaspilite/carbonate sections of the Overhang Jaspilite, partial collapse, and silicification of exposed parts of the sequence before deposition of the Corella Formation (R.Fardon, pers comm., 1973). This alternative implies that the Corella Formation unconformably overlies the Overhang Jaspilite.|16-MAY-23
4064|Chumvale Breccia|Relationships and boundaries|The Chumvale Breccia is everywhere associated with the Overhang Jaspilite. Outcrop trends of the Breccia generally parallel beding trends in the surrounding Jaspilite. Carter et al. (1961) believed that the Chumvale Breccia was underlain, probably unconformably, by the Corella Formation but recent mapping indicates that these underlying metasediments belong to the Overhang Jaspilite. The Chumvale Breccia mostly overlies but also forms conformable lenses withing the upper part of the Overhang Jaspilite.|16-MAY-23
4064|Chumvale Breccia|Defn author|Derrick, G.M., Wilson, I.H., Hill, R.M. Approved 3-NOV-1976 H.R.E. Staines. To be published in Qld Govt Mining Journal|16-MAY-23
4064|Chumvale Breccia|References|Carter, E.K., Brooks, J.H., Walker, K.R., 1961. The Precambrian mineral belt of north-western Queensland. Bureau of Mineral Resources, Bulletin 51. **Derrick, G.M., Wilson, I.H., Hill, R.M., Mitchell, J.E., 1971. Geology of Marraba 1:100 000 sheet area, Qld. Bureau of Mineral Resources, Record 1971/56|16-MAY-23
4077|Claddagh Granodiorite|Name source|"Claddagh" homestead, grid reference 53377412, Gympie 1:250 000 Sheet area.|16-MAY-23
4077|Claddagh Granodiorite|Unit history|"Claddagh Porphyritic Granodiorite", Smith ;(1964); "Claddagh granodiorite" and "Coppermine Creek granite", Brooks et al. (1974).|16-MAY-23
4077|Claddagh Granodiorite|Type section locality|The southern body, grid reference 53557377.|16-MAY-23
4077|Claddagh Granodiorite|Extent|The uinit occurs in two bodies; the northern body is 2 km west of Kilkivan and crops out over approximately 18 km2; the southern body ;is 16 km south of Kilkivan and crops out over apprximately 10 km2.|16-MAY-23
4077|Claddagh Granodiorite|Lithology|Coarse grained, flow laminated, biotite granodiorite.|16-MAY-23
4077|Claddagh Granodiorite|Relationships and boundaries|Intrudes and is faulted against undifferentiated Palaeozoic metamorphics; overlain by Lower to Middle Triassic Neara Volcanics.|16-MAY-23
4077|Claddagh Granodiorite|Age reasons|A K/Ar radiometric age of 292+/-8 m.y. (Late Carboniferous) was obtained by Hayden (1971).|16-MAY-23
25711|Clarke River Group|Name source|The Clarke River, a tributary of the Burdekin River.|16-MAY-23
25711|Clarke River Group|Unit history|Clarke River Formation (White, 1959).|16-MAY-23
25711|Clarke River Group|Constituents|The constituent formations of the Clarke River Group are (in ascending stratigraphic order) the Venetia Formation and the Lyall Formation. The Lyall Formation contains the Furry Hoop Member and Meath Rhyolite Member.|16-MAY-23
25711|Clarke River Group|Extent|The exact limits of the Clarke River Basin have not been established, but erosional remnants assigned to the sequence occur over an area of about 400 km2. The main outcrop area is a belt up to 25 km wide and 60 km long adjacent to the Clarke River 40 km south-southeast of Greenvale. Outliers occur to the north in the Blue Range, and in the Gray Creek area approximately 15 km south of Greenvale.|16-MAY-23
25711|Clarke River Group|Thickness range|The thickness of the group is difficult to determine because of irregular open folds and faulting, and because of the erosion of the upper portion of the Lyall Formation. A composite of type sections from constituent formations approximates 1200 m in thickness. This is only a rough estimate because the units within the Clarke River Group range considerably in thickness across the basin.|16-MAY-23
25711|Clarke River Group|Lithology|Poorly sorted, gritty to pebbly lithofeldspathic sandstones, volcanolithic sandstones, micaceous siltstones and tuffs. The sedimentary rocks are locally calcareous and may contain carbonaceous fragments and silicified logs.|16-MAY-23
25711|Clarke River Group|Relationships and boundaries|The Clarke River Group unconformably overlies (and is locally faulted against) deformed, mainly flyschoid, sedimentary rocks of the Broken River Embayment. These include the Wairuna, Pelican Range, Perry Creek, Kangaroo Hills, and Graveyard Creek Formations. To the south the Clarke River Group is unconformably overlain by Cainozoic basalt, and to the north it is mantled by Tertiary laterite. In the east the group abutts the Oweenee Granite and intermediate igneous rocks. The relationship here is uncertain. Small quartz porphyry bosses and stocks intrude the group.|16-MAY-23
25711|Clarke River Group|Identifying features|The sedimentary rocks in the Clarke River Basin were defined by White (1959) as the Clarke River Formation and subsequently described by Wyatt & others (1960), White (1962, 1965), Wyatt & others (1970). Wyatt & Jell (1980) and Jell & Playford (in press) reviewed the geology of the basin based partly on work carried out by AFMECO during a uranium exploration program in the 1970's (Fouques, 1975; Coles, 1979; Marlow, 1977; Dalgarno, 1977; Mouthier & Rippert, 1980). Fieldwork by GSQ officers in 1984 recognised two distinct lithological units within the Clarke River Formation. In this revised definition the name of the unit is changed to the Clarke River Group, which is divided into two formations.|16-MAY-23
25711|Clarke River Group|Age reasons|The Clarke River Group ranges from Tournaisian to Late Carboniferous (Jell & Playford, in press), but may extend down into the latest Devonian and up into the Early Permian. Several hiatuses (disconformities) could occur in the sequence.|16-MAY-23
23490|Clemant Microgranite|Name source|The name is derived from the Parish of Clemant, County of Wilkie Gray.|16-MAY-23
23490|Clemant Microgranite|Unit history|Wyatt & others (1970) mapped the Clemant Microgranite unnamed granite (C-Pg) and porphyritic microgranite (C-Pp).|16-MAY-23
23490|Clemant Microgranite|Type section locality|A small area of outcrop protruding from the coastal alluvial plain 700-800m from the Bruce Highway (8159-144884) is designated as the type area.  The grid reference is based on the AGD66 datum.|16-MAY-23
23490|Clemant Microgranite|Description at type locality|It consists of pink, abundantly porphyritic, biotite microgranite, containing large euhedral potassic feldspar phenocrysts that display rapakivi texture.|16-MAY-23
23490|Clemant Microgranite|Extent|The Clemant Microgranite crops out in several areas in the northeast quarter of ROLLINGSTONE. The microgranite forms an irregularly shaped body 72km2 in area, forming the eastern margin of the Paluma Range between Hencamp and Leichhardt Creeks. It also forms an arcuate intrusive body or ring dyke (220km2 in area) cutting across the Paluma Range from the Black Fellow Creek area to the headwaters of Keelbottom Creek (East Branch), and three irregularly shaped bodies (1-3km2) in the centre of the Paluma Range.  The Clemant Microgranite is somewhat more recessive than the adjacent Paluma Rhyolite and Saint Giles Volcanics. This characteristic aided aerial photographic interpretation of boundaries within the tropical rain forest of the Paluma Range.|16-MAY-23
23490|Clemant Microgranite|Lithology|As in the type area, the Clemant Microgranite (CPgc) is grey to dark pink (predominantly pink), abundantly porphyritic, biotite microgranite. It is very similar to the Malmesbury Microgranite which crops out south of the Sybil Graben and was described by Scott (1988) and Gunther & Withnall (1992). The microgranite contains sparse dark, subrounded, dioritic xenoliths up to 5cm across.  Phenocrysts comprise 55-65% of the microgranite. Quartz phenocrysts (20-25%) are subhedral to euhedral, exhibit straight extinction, and are up to 5mm in diameter. K-feldspar (20-25%) forms large euhedral crystals up to 4cm long with rapakivi texture (albite rims 2 3mm wide).|16-MAY-23
23490|Clemant Microgranite|Relationships and boundaries|The Clemant Microgranite intrudes the Carboniferous Paluma Rhyolite, Saint Giles Volcanics, early Paalaozoic Holborn Granodiorite and Proterozoic(?) Argentine Metamorphics. The close spatial relationships with the Early Carboniferous Paluma Rhyolite and Saint Giles Volcanics and the fact that the Clemant Microgranite forms ring dykes, suggests that the microgranite may have intruded its own volcanic pile, with ring dykes forming during and after caldera collapse and resurgence.|16-MAY-23
23490|Clemant Microgranite|Age reasons|The suggestion above is consistent with a U-Pb zircon (SHRIMP) age of 337±7 Ma on a sample from the Clemant Microgranite (8159-420858) (Appendix 1).  The grid reference is based on the AGD66 datum.|16-MAY-23
23490|Clemant Microgranite|References|*GUNTHER, M.C. & WITHNALL, I.W., 1992: Late Palaeozoic igneous rocks of the Rollingstone and Ewan 1:100 000 Sheet areas. Queensland Resource Industries Record 1992/17.    *SCOTT, M. 1988: Oweenee Rhyolite and Malmesbury Microgranite   new and revised stratigraphic units in north Queensland. Queensland Government Mining Journal, 89, 284 289.    *WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127|16-MAY-23
4212|Coane Range Granite Complex|Name source|From the Coane Range.|16-MAY-23
4212|Coane Range Granite Complex|Unit history|It was previously mapped as Oweenee Granite by Wyatt & others (1970).|16-MAY-23
4212|Coane Range Granite Complex|Geomorphic expression|The complex crops out well, except in the east where the rainfall is higher and the rocks are more weathered. It forms extremely rugged, boulder-strewn, hilly topography with a local relief of 350 m. Access is extremely difficult except around the northwestern and western contacts and along the Hidden Valley-Paluma road. Field data is thus restricted to these areas.|16-MAY-23
4212|Coane Range Granite Complex|Type section locality|The type area of the Coane Range Granite Complex is along the lower gorge of the Running River between 8059-871905 and 872880.  REFERENCE SECTION::  A reference area is the hills on the eastern side of the Laroona-Ewan road between the Running River bridge at 8059-851849 and 862823, where the granite is generally finer grained.   The grid references are based on the AGD66 datum.|16-MAY-23
4212|Coane Range Granite Complex|Description at type locality|Here pink to orange medium to coarse-grained biotite granite with local pegmatite and aplite segregations crops out.|16-MAY-23
4212|Coane Range Granite Complex|Extent|The Coane Range Granite Complex is the northeasternmost part of the Oweenee Batholith. It is roughly semi-circular in outline and 25km long and up to 13km wide. It is bounded to the south by the Spinifex Creek Granite, to the north along the Running River by the Running River Metamorphics, and to the east by the Paluma Rhyolite.|16-MAY-23
4212|Coane Range Granite Complex|Lithology|As noted above, the Coane Range Complex is a composite unit. It ranges from microgranite to granite. In most places observed, the granite is fine or medium grained and equigranular to porphyritic. The microgranite is generally porphyritic with phenocrysts of quartz and feldspar. Some coarse-grained seriate to porphyritic biotite granite was observed locally, particularly along the Paluma-Hidden Valley road, the lower gorge of the Running River, and along the Ravenshoe power line; in these areas coarse-grained outcrops commonly occur in close proximity to fine-grained granite and microgranite. Coarse-grained porphyritic biotite granite containing pink K-feldspar crystals up to 2cm was observed along the Ravenshoe power line at 8160-979997. The textures of the granites and microgranites are therefore highly variable. Graphic intergrowths are present in some specimens and miarolitic cavities are common. The medium to coarse granites locally have pegmatitic segregations, commonly as cores to irregular aplitic pods and veins.|16-MAY-23
4212|Coane Range Granite Complex|Relationships and boundaries|The Coane Range Complex intrudes the Proterozoic(?) Running River Metamorphics and Falls Creek Tonalite, the Late Devonian to Early Carboniferous Keelbottom Group, and the Carboniferous Paluma Volcanics. It is also thought to intrude the Spinifex Creek Granite. Contacts with the Running River Metamorphics are sharp on the small scale, but dykes of porphyritic microgranite extend into the country rocks for up to 100m in places, and rafts of metamorphic rocks occur in the granite near the contact.|16-MAY-23
4212|Coane Range Granite Complex|Age reasons|A sample from the northern part of the Coane Range Granite Complex along the Hidden Valley-Paluma road was included in the Rb-Sr isochron for the 'Oweenee Granite' which produced an age of 342±7 Ma* (Wyatt & others, 1970). However, because the isochron included samples from several different units, it is probably not reliable, although an Early Carboniferous age is consistent with the relationships. An Early Carboniferous Rb-Sr biotite-total rock age of 331±2 Ma was obtained by AGSO from the Falls Creek Tonalite which is intruded by the Coane Range Complex and Kallanda Granite (D. Wyborn, personal communication, 1989). The Falls Creek Tonalite is deformed and is probably Proterozoic or early Palaeozoic in age. It is hornfelsed by the Carboniferous granites. Thus the Rb-Sr age may reflect the age of hornfelsing and hence the intrusion of the granites.|16-MAY-23
4212|Coane Range Granite Complex|Comments|Because of the lack of data from within the unit and because our limited observations indicate that the unit is composite, the term 'Complex' has been adopted.  The southern half of the Complex appears to lack the prominent lineaments that characterise the Spinifex Creek Granite, although smaller lineaments and joint trends can be identified on aerial photographs and Landsat images. However, to the north of Deception Creek, major east and southeast-trending lineaments occur, suggesting that the rocks there may belong to a different unit to that in the south. The large tongue of Running River Metamorphics extending along Deception Creek may be a screen partly separating the units. Nevertheless, the AGSO airborne radiometric data indicate that the rocks are similar geochemically, because they are consistently high in the Total Count, U, K and Th channels. On the composite image processed from this data, the Complex is uniformly white, contrasting with the pinkish tints of the Spinifex Creek Granite. This indicates that the rocks of the Complex are the most fractionated in the batholith, and this is confirmed by its geochemistry (Gunther & Withnall, 1992).|16-MAY-23
4212|Coane Range Granite Complex|References|GUNTHER, M.C. & WITHNALL, I.W., 1992: Late Palaeozoic igneous rocks of the Rollingstone and Ewan 1:100 000 Sheet areas. Queensland Resource Industries Record 1992/17. **WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127|16-MAY-23
24855|Cobbold Metadolerite|Name source|Cobbold Creek, which joins the Robertson River at GR 536182 (North Head 1:100 000 Sheet area).|16-MAY-23
24855|Cobbold Metadolerite|Unit history|Cobbold Dolerite (White, 1959, 1965).|16-MAY-23
24855|Cobbold Metadolerite|Geomorphic expression|Generally well exposed and forms prominent boulder-strewn hills in some places. The metadolerite has a dark red-brown to brown colour on aerial photographs.|16-MAY-23
24855|Cobbold Metadolerite|Type section locality|White (1959) gave the type area of the Cobbold Dolerite simply as Cobbold Creek. As noted above, most of the basic rocks in Cobbold Creek are now interpreted as extrusives and mapped as Dead Horse Metabasalt. Probable metadolerite intruding the metabasalt crops out in Cobbold Creek at GR 520125 and 520109 (North Head 1:100 000 Sheet area), but because it is relatively uncommon there, reference localities are designated for the Cobbold Metadolerite. These are metadolerite and metagabbro outcrops along the Georgetown-Forsayth road at GR 656608 and 2 km north of the Lornevale turnoff (Georgetown 1:100 000 Sheet area), and along the Georgetown-Abingdon Downs road from GR 618966 to the Ironhurst turnoff at 604986 (Forest Home 1:100 000 Sheet area).|16-MAY-23
24855|Cobbold Metadolerite|Extent|The Cobbold Metadolerite forms a multitude of separate intrusions, mainly sills, within the Robertson River Subgroup and Bernecker Creek Formation, in a belt up to 50 km wide, extending for about 150 km from near Gilberton homestead in the south to near Dagworth homestead in the north. Most amphibolite in the Einasleigh Metamorphics probably can be equated with the Cobbold Metadolerite, thus extending its distribution to most of the eastern two-thirds of the Georgetown Inlier.|16-MAY-23
24855|Cobbold Metadolerite|Lithology|Metadolerite and metagabbro grading into amphibolite.|16-MAY-23
24855|Cobbold Metadolerite|Relationships and boundaries|The Cobbold Metadolerite intrudes the Bernecker Creek Formation and Robertson River Subgroup, mainly as sills. None occurs in the conformably overlying Townley Formation. Much of the amphibolite in the Einasleigh Metamorphics probably can be equated with the Cobbold Metadolerite, although some is known to be extrusive in origin. The Dead Horse Metabasalt is probably comagmatic with some of the Cobbold Metadolerite.|16-MAY-23
24855|Cobbold Metadolerite|Identifying features|All metamorphosed basic rocks in the Georgetown Inlier were assigned to the Cobbold Dolerite by White (1959, 1965). However, many basic rocks, including most of those in the type area, are now recognised as extrusive metabasalt, and assigned to the Dead Horse Metabasalt. Withnall & others (1980) abandoned usage of the name Cobbold Dolerite for the basic intrusives but did not rename them. The rocks form a multitude of separate intrusions (see Distribution). However, they are all petrographically and chemically similar, and probably genetically related, although they may have been intruded in at least two separate pulses during the deposition of the Robertson River Subgroup. It is convenient to assign them to a single named unit as has been done for small but geographically separate granitoid plutons in the Georgetown area (Withnall & others, 1976). The name Cobbold Dolerite is well established in the literature, and should be retained, but because the primary igneous minerals have mostly been altered, the name Cobbold Metadolerite is proposed. The unit is redefined to incorporate two reference localities into the definition.|16-MAY-23
24855|Cobbold Metadolerite|Age reasons|Intruded during deposition of the Robertson River Subgroup. The minimum age of 1570+/-20 m.y. (mid-Proterozoic) obtained for the Etheridge Group (Black & others, 1979), therefore also applies to the Cobbold Metadolerite.|16-MAY-23
24855|Cobbold Metadolerite|References|98/29026; B071; 80/20677;  79/04763; 82/22380|16-MAY-23
25854|Cone Creek Metabasalt Member|Name source|Cone Creek, 2 km south-southwest of Mitakoodi siding, latitude 20o58'S, longitude 140o18'E.|16-MAY-23
25854|Cone Creek Metabasalt Member|Geomorphic expression|The unit forms scattered outcrops in low rises and plains in the eastern areas, and low rocky hills in the north and northwest.|16-MAY-23
25854|Cone Creek Metabasalt Member|Type section locality|An east-west section 4 km north of Mitakoodi Siding and 32 km southwest of Cloncurry, from latitude 20o54'S, longitude 140o17'E to latitude 20o54'S, longitude 140o19'E, i.e. grid reference 6956-251870 (base) to 6956-285870 (top). Thickness of the metabasalt is about 2500 m. Outcrop in the type section is good, and as in most other areas occupied by the member, the unit is cut by a network of dolerite dykes.|16-MAY-23
25854|Cone Creek Metabasalt Member|Extent|This is the most extensive member of the Marraba Volcanics. North of 21oS latitude it forms a continuous M-shaped belt between 140o3'E and 140o19'E longitude, in the north-plunging Duck Creek and Bulonga anticlines (Fig. 1). The eastern limb of the Duck Creek anticline contains a discontinuous extension of the member to 21o42'S latitude. The member has been mapped in detail in the Marraba 1:100 000 Sheet area, and is known to occur in the Malbon and Mount Merlin 1:100 000 Sheet areas.|16-MAY-23
25854|Cone Creek Metabasalt Member|Thickness range|Thickness ranges from about 2800 m in the east to 900 m in the west.|16-MAY-23
25854|Cone Creek Metabasalt Member|Lithology|Massive metabasalt, amygdaloidal metabasalt; minor arkose, agglomerate, and siltstone. The rocks have been metamorphosed in the greenschist facies.|16-MAY-23
25854|Cone Creek Metabasalt Member|Relationships and boundaries|The Cone Creek Metabasalt Member overlies the Argylla Formation apparently conformably, and is overlain conformably by the Mount Start Member of the Marraba Volcanics. The Wimberu Granite and numerous dolerite dykes and sills intrude the member.|16-MAY-23
24864|Constance Sandstone|Name source|From the Constance Range, a prominent escarpment trending meridionally through western LAWN HILL, northwestern Queensland.|16-MAY-23
24864|Constance Sandstone|Constituents|The formation comprises several sandstone and siltstone members, from base to top: Hedleys Sandstone Member* Pandanus Siltstone Member, Burangoo Sandstone Member* Wallis Siltstone Member, Schultz Sandstone Member* (which includes the rocks formerly assigned to the now obsolete Bowthorn Siltstone Member).|16-MAY-23
24864|Constance Sandstone|Geomorphic expression|Ridge and plateau forming, as the formation is dominated by resistant sandstone. Several siltstone members are recessive and form valleys or plains between sandstone uplands.|16-MAY-23
24864|Constance Sandstone|Type section locality|Stated by Carter et al (1961) to be "from lat. 18deg27'35'S, long. 138deg17'00', east-south-east about 4 miles to the base of the formation." Reference sections: The type section nominated by Carter et al (1961) contains minor faulting and folding, and is far from the best section within LAWN HILL. Nor does it contain any of the siltstone members recognised by Roberts et al (1963) or Grimes & Sweet (1979) in CALVERT HILLS and WESTMORELAND respectively. Accordingly, two reference sections have been nominated to address these shortcomings. Reference section A is a more compact section (than the type section) in northern LAWN HILL, but neither does it contain the siltstone members. Reference section B, in WESTMORELAND, includes all the siltstone and sandstone members that are recognised in outcrops north of the Elizabeth Creek Fault Zone, but because of faulting does not include the uppermost part of the formation (this is included in the type section for the Schultz Sandstone Member). Both reference sections are more easily accessed from existing tracks than is the type section. Section A, in the Constance Range escarpment 4 km south of Elizabeth Creek, runs from the base of the Constance Sandstone, at Latitude 18deg14'41"S Longitude 138deg23'28"E (224125E 7980770N), southwest for 1.7 km to the top of the Constance Sandstone, at Latitude 18deg14'57"S Longitude 138deg22'37"E (222623E 7980270N). It is accessed from a station track following Elizabeth Creek. Section B, in southwestern WESTMORELAND, begins at Latitude 17deg52'50'" Longitude 138deg3'42"E (188622E 8020570N) and runs along Gorge Creek for 9.3 km, mostly south to south-southeast, ending at Latitude 17deg57'47"S Longitude 138deg4'49"E (190723E 8011471N), against a fault within the Nicholson River Fault Zone. It is accessed from an old exploration track from the access road into Nadjaburra Aboriginal settlement. A more compact section showing the siltstone members is not possible, because dips in the region are so low, and steeper-dipping sections are fault-affected.|16-MAY-23
24864|Constance Sandstone|Extent|Widely distributed in northwestern LAWN HILL and southwestern WESTMORELAND (both in Queensland), and southern CALVERT HILLS, and eastern MOUNT DRUMMOND (both in the Northern Territory).|16-MAY-23
24864|Constance Sandstone|Thickness range|Estimated by Carter et al (1961) to range from 300 to 1100 m in LAWN HILL; thickness in the type section cannot easily be estimated because of structural complexity. It also reaches up to 1100 m in southwestern WESTMORELAND and northeastern MOUNT DRUMMOND, and thins to less than 100 m in central MOUNT DRUMMOND. Reference section A is around 800 m thick, and Section B approaches 1100 m (Sweet et al 1981).|16-MAY-23
24864|Constance Sandstone|Lithology|Very fine- to coarse-grained, and granule-rich to pebbly sandstones, ranging from lithic to quartzose; most are in the sub-lithic category.|16-MAY-23
24864|Constance Sandstone|Depositional environment|Most sandstones are trough cross-bedded, and indicate shallow marine, intertidal or shelf environments. The very fine sandstones are associated with siltstone and shale intervals, and indicate storm-dominated shelf facies. Planar bedding, current lineation and current and wave ripples, and mudstone intraclasts are common; desiccation cracks are rare.|16-MAY-23
24864|Constance Sandstone|Relationships and boundaries|Lies with pronounced angular unconformity, or disconformity, on the McNamara Group in eastern MOUNT DRUMMOND, LAWN HILL and WESTMORELAND. In western MOUNT DRUMMOND it lies mainly disconformably, but locally with angular unconformity, on the Wild Cow Subgroup. The upper contact, with the Mullera Formation, is apparently sharp but conformable; it appears to be a rapid transition over a metre or so into shale and fine siltstone. Overlain unconformably by Cambrian and Cretaceous rocks.|16-MAY-23
24864|Constance Sandstone|Age reasons|The interpreted age range for the whole South Nicholson Group, of 1500-1400 Ma, is based on its correlation with the Roper Group of the southern McArthur Basin (Dunn et al 1966) with which it makes up the Roper Superbasin (Jackson et al 1999, Abbott and Sweet 2000, Abbott et al 2001). Ages of 1492±4 and 1493±4 Ma for tuffaceous material from the lower Roper Group (Jackson et al 1999) provide the most reliable estimate for the age of that Group, and hence for the lower South Nicholson Group. The Constance Sandstone is judged to lie near the middle of the age range 1500-1400 Ma, given that the whole Wild Cow Subgroup lies beneath it in western MOUNT DRUMMOND.|16-MAY-23
24864|Constance Sandstone|Correlations|None known, but it is likely that a sandstone unit/s in the middle Renner Group (Hussey et al 2001) and the Roper Group (Jackson et al 1999) are in part correlative, given the overall correlation between these groups.|16-MAY-23
24864|Constance Sandstone|Defn author|Sweet, I.P., [APR-2005] (after Carter et al 1961)|16-MAY-23
24864|Constance Sandstone|Comments|The formal recognition of three previously unnamed sandstone members within the Constance Sandstone necessitates this redefinition (see Constituent Units).|16-MAY-23
24864|Constance Sandstone|References| **ABBOTT S.T. and Sweet I.P. 2000. Tectonic control on third-order sequences in a siliciclastic ramp-style basin: an example from the Roper Superbasin (Mesoproterozoic), northern Australia. Australian Journal of Earth Sciences, 47, 637-657.  **ABBOTT S.T., Sweet I.P., Plumb K.A., Young D.N., Cutovinos A., Ferenczi P.A., Brakel A. and Pietsch B.A., 2001. Roper region: Urapunga and Roper River special, Northern Territory (Second Edition); 1:250 000 Geological Map Series, sheets SD53-10,11. Northern Territory Geological Survey-Australian Geological Survey Organisation (NGMA), Map and Explanatory Notes.  **CARTER E.K., Brooks J.H. and Walker K.R., 1961. The Precambrian mineral belt of northwestern Queensland. Bureau of Mineral Resources, Bulletin, 51.  **DUNN P.R., Plumb K.A. and Roberts H.G. 1966. A proposal for time-stratigraphic subdivision of the Australian Precambrian. Journal of the Geological Society of Australia, 13, 593-608.  **HUSSEY K.J., Beier P.R., Crispe A.J., Donnellan N. and Kruse P.D. 2001. Helen Springs, Northern Territory (Second Edition); 1:250 000 geological series, sheet SE53-10.   **JACKSON M.J., Sweet I.P., Page R.W. and Bradshaw B.E., 1999. The South Nicholson and Roper Groups: evidence for the early Proterozoic Roper Superbasin. In: Bradshaw B.E. and Scott D.L. (Eds.), Integrated basin analysis of the Isa Superbasin using seismic, well-log and geopotential data: an evaluation of the economic potential of the northern Lawn Hill Platform. Australian Geological Survey Organisation, Record 1999/19 (unpaginated).    **SWEET I.P., Mock C.M. and Mitchell J.E., 1981. Seigal, Northern Territory; Hedleys Creek, Queensland (First Edition); 1:100,000 geological series, sheets 6462 and 6562. Bureau of Mineral Resources, Geology and Geophysics, Explanatory Notes.|16-MAY-23
24864|Constance Sandstone|Parent|The Constance Sandstone is a component of the newly defined Accident Subgroup, of the South Nicholson Group.|16-MAY-23
24222|Coocerina Formation|Name source|The Coocerina Formation is named after the Coocerina copper mine 19 km west-northwest of Quamby (latitude 20o16'50"S, longitude 140o7'48"E; GR 092572).|16-MAY-23
24222|Coocerina Formation|Unit history|The Coocerina Formation was included in the Corella Formation by Carter & others (1961) but placed in the Knapdale Quartzite by Wilson & others (1979b).|16-MAY-23
24222|Coocerina Formation|Geomorphic expression|The unit is characterised by low elevations and little relief. It forms a gently undulating plain with local moderately incised drainage.|16-MAY-23
24222|Coocerina Formation|Type section locality|The type section is defined as an east-west section extending 500 m from the base of the scarp which marks the western edge of the Knapdale Range 1 km south of the Coocerina mine (latitude 20o17'25"S, longitude 140o7'45"E, GR 092562) to the track which provides access along the western side of the range at latitude 20o17'25"S, longitude 140o7'30"E (GR 087562). The section is moderately to poorly exposed and consists of grey siltstone, black shale, scapolitic siltstone, and muscovite-biotite schist which have a total thickness of approximately 400 m.|16-MAY-23
24222|Coocerina Formation|Extent|The unit is exposed as a narrow north-trending belt immediately west of the Knapdale Range near the middle of the Quamby 1:100 000 Sheet area. The total area of outcrop is 4 km2.|16-MAY-23
24222|Coocerina Formation|Thickness range|The formation is approximately 400 m thick everywhere along its exposure.|16-MAY-23
24222|Coocerina Formation|Lithology|The Coocerina Formation consists of grey, mostly calcareous black shale, scapolitic siltstone, and minor pyritic shale, black to bluish grey micaceous metasiltstone, fine-grained sandstone, and laminated calcareous granofels. Strongly fractured and sheared grey scapolitic siltstone commonly occurs near the contact with the Knapdale Quartzite.|16-MAY-23
24222|Coocerina Formation|Relationships and boundaries|The Coocerina Formation conformably overlies the Knapdale Quartzite. The boundary is locally sheared but the grain size grades abruptly from the sandstone of the older unit into the siltstone of the younger unit. This boundary coincides with the base of the scarp which marks the western edge of Knapdale Quartzite. The upper contact of the Coocerina formation is faulted and poorly exposed. It is defined by the change from grey siltstone and granofels to the black or dark brown laminated dolomite of the Lady Clayre Dolomite. The relationship is interpreted to be conformable because of the general parallelism of bedding in both units adjacent to the boundary.|16-MAY-23
24222|Coocerina Formation|Structure and Metamorphism|Bedding in the Coocerina Formation generally dips about 60o to the west. Younging is also to the west in the few places it has been determined. Bedding is steeper in the north and dips are to the west-northwest. The siltstone near the base of the unit is commonly fractured whereas the upper part of the unit is mostly schistose. Mineral elongation is recognised in the south. The rocks in the formation appear to be metamorphosed within the lower greenschist facies. Scapolite porphyroblasts are widely developed and some of calcareous granofels contains actinolite porphyroblasts.|16-MAY-23
24222|Coocerina Formation|Age reasons|The age of the Coocerina Formation is poorly constrained. It is younger than the Corella Formation which was deposited between 1760 and 1740 Ma age (Page, 1981), and older than the regional metamorphism which occurred between 1450 and 1670 Ma (Page, 1978).|16-MAY-23
24222|Coocerina Formation|Comments|Discussion: Both the Coocerina Formation and the White Blow Formation which crops out 55 km to the southwest in the Mary Kathleen 1:100 000 Sheet area (Derrick & others, 1977b) overlie thick quartzose units (Knapdale Quartzite and Deighton Quartzite) which disconformably or unconformably overlie the Corella Formation. The quartzites were correlated by Carter & others (1961) and Derrick & others (1977a). Therefore, the Coocerina Formation probably can be correlated with the White Blow Formation and included in the Mount Albert Group of Derrick & others (1977a).|16-MAY-23
27285|Corbett Formation|Name source|Parish of Corbett, County of Victor.|16-MAY-23
27285|Corbett Formation|Geomorphic expression|The Corbett Formation forms hilly terrain, although the schist facies has more subdued relief. Bedding trends are generally poorly developed except for the ridge-forming interval at the top of the formation.|16-MAY-23
27285|Corbett Formation|Type section locality|A complete section is exposed along Slatey Creek for about 2.5 km between GR 479125 (base) and 477150 (top) (North Head 1:100 000 Sheet area), and is designated as the holostratotype. The lower part of the formation is grey, slightly carbonaceous, laminated, cleaved mudstone, whereas the upper part consists of a monotonous sequence of greenish grey, only sparsely laminated, cleaved mudstone, locally containing chloritoid. All of the rocks are well cleaved to phyllitic. The thickness of the section is not known because of the lack of bedding and probable repetition by folding. A maximum of 1500 m is present but the true thicknesss is probably less than 1000 m. This section was formerly a reference section (hypostratotype) designated by Withnall & Mackenzie (1980) for the Robertson River Formation, which is now redefined as a supgroup.|16-MAY-23
27285|Corbett Formation|Description at type locality|Reference section: Better exposed, but incomplete sections of the Corbett Formation crop out in the Percy River for about 0.6 km between GR 617802 (base) and a synclinal hinge at 615808 (Bellfield 1:100 000 Sheet area), and for about 3.5 km along Stake Yard Creek, from the Forsayth-North Head road crossing at GR 400192 to 413159 (top), (North Head 1:100 000 Sheet area). These are designated as parastratotypes and contain similar rocks to those in the holostratotype.  The section along Kangaroo Creek between GR 674142 and 670183 (Forsayth 1:100 000 Sheet area) provides a parastratotype for the 'schist facies' of the unit. It contains mica schist, commonly with biotite and staurolite porphyroblasts, and includes the Tin Hill Quartzite Member (Withnall & Mackenzie, 1980).|16-MAY-23
27285|Corbett Formation|Extent|The Corbett Formtion crops out from near Gilberton homestead to near North Head homestead, and from there, it extends east for about 40 km between the Robertson River and Ropewalk Range. Further north it forms a narrow belt between Lornevale and Mount Turner homesteads, and then northeast to the Newcastle Range. The total area is about 1000 km2.|16-MAY-23
27285|Corbett Formation|Thickness range|Probably up to 1000 m, but repetition by complex, multiple folding prevents measurement of thickness in many areas.|16-MAY-23
27285|Corbett Formation|Lithology|Cleaved phyllitic mudstone as in the type section. This grades eastwards into mica schist which commonly contains porphyroblasts of garnet, staurolite and andalusite in the lower amphibolite facies. Porphyroblasts of biotite are also common and persist to higher grades. A distinctive, thin, pure quartzite unit, the Tin Hill Quartzite Member, occurs within the 'schist facies' of the formation.|16-MAY-23
27285|Corbett Formation|Relationships and boundaries|The Corbett Formation conformably overlies the Dead Horse Metabasalt. In the northern area, where the metabasalt is absent, the Corbett Formation conformably overlies the Daniel Creek Formation, from which it is distinguished by its lack of quartzite. The Lane Creek Formation conformably overlies the Corbett Formation and is recognised by its abundant carbonaceous rocks. A resistant ridge-forming interval of more quartzose phyllite marks the top of the formation in many places. This can be traced into the 'schist facies' in places, but where it is absent, the Corbett Formation schists can also be distinguished from those in the Lane Creek Formation by the presence of staurolite and/or biotite porphyroblasts. The Tin Hill Quartzite Member which was formerly defined as a member of the Robertson River Formation, is now a member of the Corbett Formation. The Corbett Formation is intruded by sills of Proterozoic Cobbold Metadolerite, as well as by numerous Proterozoic granitoids of the Forsayth Batholith, and some late Palaeozoic hypabyssal rocks. The formation is unconformably overlain by the Devonian-Carboniferous Gilberton Formation, the late Palaeozoic Newcastle Range and Agate Creek volcanics, and the Jurassic Hampstead Sandstone.|16-MAY-23
27285|Corbett Formation|Age reasons|The minimum age of 1570+/-20 Ma (mid-Proterozoic) obtained for the Etheridge Group (Black & others, 1979) also applies to the Corbett Formation.|16-MAY-23
4727|Corella Formation|Constituents|Three major but as yet unnamed subdivisions of the Corella Formation have been recognised in most areas (Derrick et al. 1971, 1974; Wilson et al. in prep [in 1976]. In addition, several members have been mapped, only one of which, the Lime Creek Metabasalt Member, is formally named and defined in this paper.|16-MAY-23
4727|Corella Formation|Type section locality|The Corella Formation was formally defined by Carter et al. (1961) with reference to a type section exposed along the old Mount Isa/Cloncurry road from a point a little less than 1 km east of the Federal mine northwesterly for about 5 km to the Wonder Valley turnoff, and then in a southwesterly direction along a disused Mary Kathleen access track for about 16km to an outcrop of Wonga Granite. We propose it be retained, except for about 3 km at the western end of the section which consists of recrystallized acid volcanics of the Argylla Formation. REFERENCE SECTION proposed extending 1.7 km east from a point (6857 825430) [AGD 66, AMG?] 3 km east northeast of barbara (Green Monster) copper mine, about 34 km north-northwest of mary Kathleen. 2nd REFERENCE SECTION, very similar to the first, but more readily accessible, is proposed just south o fthe Barkly Highway, 16 km west of Mary Kathleen (extending from 6856 778037 to 6856 797035)[ [AGD 66, AMG?]|16-MAY-23
4727|Corella Formation|Description at type locality|Our detailed mapping in this section has verified the observations of Carter et al. (1961), who noted many faults, intricate folding and the repetition and possible omission of strata. We consider  that the top of the formation is not defined and that the lower part of the formation is poorly represented in this section. However it does contain many excellent exposures of typical metasediments of the Corella Formation. REFERENCE SECTION description:  Although the Corella Formation is unconformably overlain by the Deighton Quartzite in this section, it is believed to be almost complete.|16-MAY-23
4727|Corella Formation|Extent|The detailed mapping has shown that the Charley Creek Formation, defined by Carter et al. (1961) is partly Corella Formation and partly Deighton Quartzite, and the name can be discarded. Also, areas previously mapped as part of the the Corella Formation have been subdivided and included in new formations such as the Overhang Jaspilite and White Blow Formation, or have been shown to be part of previously defined formations such as the Ballara Quartzite or Argylla Formation. However the distribution of the formatin is braodly the same as described by Carter et al. (1961).|16-MAY-23
4727|Corella Formation|General description|The major units are: a basal calcareous unit (PLkc1) characterized by black-weathering banded calc-silicate granofels, laminated grey to black metasiltstone and shale interlayered with fine-grained feldspathic quartzite and minor grey bedded marble and calcareous quartzite; a middle unit (PLkc2) of massive laminated calcareous quartzite, ortho-quartzite, feldspathic metasitlstone, pelitic schist, phyllite and slate and minor metabasalt and tuff; and a topmost unit (PLkc3) very similar to the lower unit, but tending to be more calcareous and to contain less metasiltstone. the minor members mapped included lenses of quartzite, conglomerate, skarn, breccia, limestone and marble, tuff and agglomerate, metabasalt, cordierite-anthophyllite  rocks, andalusite schist, siltstone and shale, and pyrrhotitic black shale.|16-MAY-23
4727|Corella Formation|Thickness range|The thickness of the Corella Formation exposed in the first reference section is 1090 m; in the second reference along the Barkly Highway it is anout 1200 m. although the Corella Formation is overlain unconformably by the Deighton Quartzite in both sections, the sections are believed to be nearly complete. In the Marraba 1:100 000 sheet area the middle arenaceous and pelitic unit is much thicker than in the type section and the total thickness of the formation may be up to 4000 m.|16-MAY-23
4727|Corella Formation|Relationships and boundaries|The Corella Formation conformably overlies  the Ballara Quartzite and conformably or possibly unconformably overlies the Overhang Jaspilite.  It unconformably overlies the Soldiers Cap Group. It is unconformably or disconformably overlain by the Deighton  and Roxmere Quartzites of the Mount Albert Group (Derrick et al in prep [1976]), and the Quamby Conglomerate. The Corella Formation is intruded by dolerite of at least three ages, the Lunch Creek Gabbro, the Tommy Creek Microgranite, the Burstall Granite, the Hardway Granite, and phases of the Naraku Granite and Wonga Granite.|16-MAY-23
4727|Corella Formation|Defn author|Derrick, Geoff.  Approved 3-NOV-1976 H.R.E. Staines.|16-MAY-23
4727|Corella Formation|References|Carter, E.K., Brooks, J.H., Walker, K.R., 1961. The Precambrian mineral belt of north-western Queensland. Bureau of Mineral Resources, Bulletin 51. **Derrick, G.M., Wilson, I.H., Hill, R.M., Mitchell, J.E., 1971. Geology of Marraba 1:100 000 sheet area, Qld. Bureau of Mineral Resources, Record 1971/56. **Derrick, G.M., Wilson, I.H., Hill, R.M., in prep [1976] Revision of stratigraphic nomenclature in the Precambrian of northwestern Queensland. VII: Mount Albert Group. **Derrick, G.M., Wilson, I.H., Hill,R.M., in prep [1976] Revision of stratigraphic nomenclature in the Precambrian of northwestern Queensland. VI: Mary Kathleen Group. **Derrick, G.M., Wilson, I.H., Hill, R.M., Glikson, A.Y., Mitchell, J.E., 1974. Geology of the Mary Kathleen 1:100 000 sheet area, Queensland. Bureau of Mineral Resources Record 1974/90. **Wilson, I.H., Derrick, G.M.,  Hill, R.M., Duff, B.A., Noon, T.A., Ellis, D.J. in prep[1976]. Geology  fo the Prospector 1;100 000 sheet area, Queensland. Bureau of Mineral Resources Record.|16-MAY-23
34130|Cornelia Orthogneiss|Name source|Cornelia homestead located north of the Cape River at GR 3255 77409 in the Lolworth 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
34130|Cornelia Orthogneiss|Unit history|The Cornelia Orthogneiss was partly mapped as part of the Ravenswood Granodiorite (partly felsic phase, ODa and partly as ODn) by Paine and others (1971).|16-MAY-23
34130|Cornelia Orthogneiss|Type section locality|On a hill 6km northwest of Cornelia homestead at GR 3217 77453 in the Lolworth 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
34130|Cornelia Orthogneiss|Description at type locality|Here a grey, fine grained, foliated, biotite orthogneiss comprises recrystallised quartz, subhedral oligoclase, anhedral microcline, aligned biotite with minor zircon and opaques.|16-MAY-23
34130|Cornelia Orthogneiss|Extent|The Cornelia Orthogneiss crops out over about 20km2 in a belt about 1-2km wide extending from just west of Capeville to west of Gorge Creek .|16-MAY-23
34130|Cornelia Orthogneiss|Lithology|The rocks at the type locality are similar to those throughout the unit. A ridge about 3km east-southeast of Cornelia homestead is formed by foliated felsic orthogneiss. The foliation is unevenly developed with domains of well-developed foliation defined by aligned biotite flakes interspaced with less foliated zones. The rock types in the less foliated zones appears to have a fine to medium grained, equigranular granitic texture. In the headwaters of Gorge Creek, a locally foliated diorite/gabbro is interlayered with the Cornelia Orthogneiss and may be part of the sequence.|16-MAY-23
34130|Cornelia Orthogneiss|Relationships and boundaries|The Cornelia Orthogneiss is interlayered with amphibolite and quartzite of the Cape River Metamorphics to the east-southeast of Cornelia homestead. This relationship appears to be crosscutting near GR 3295 77401 suggesting that the Cornelia Orthogneiss may intrude the Cape River Metamorphics.  The grid reference is based on the AGD66 datum.|16-MAY-23
34130|Cornelia Orthogneiss|Age reasons|The age of the Cornelia Orthogneiss is not known precisely. A probable age of Cambrian to Early Ordovician is assigned. The unit may have been felsic volcanics interbedded with the Mesoproterozoic Cape River Metamorphics or granitoids related to the late Mesoproterozoic Gorge Creek Granite Complex.|16-MAY-23
34130|Cornelia Orthogneiss|Comments|MAGNETIC SUSCEPTIBILITY::  Magnetic Susceptibilities at the type locality are 14-1550 x 10[superscript]-5 (average 625) SI units. Elsewhere, the unit has high susceptibilities for a felsic igneous rock ranging from 180-2745 x 10[superscript]-5 (average 907) SI units.|16-MAY-23
34130|Cornelia Orthogneiss|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
4749|Corrie Member|Name source|From Corrie Downs Property (140'06", 22o18"), Boulia 1:250 000 Sheet area.|16-MAY-23
4749|Corrie Member|Unit history|Generally equates with Unit 5 of Casey (1968), Member (iv) of Druce (1976), and the Encrinite Member of Jones et al. (1971).|16-MAY-23
4749|Corrie Member|Type section locality|Black Mountain (140o17'E, 22o32'S), the interval between 500 m and 590 m within the Ninmaroo Formation from 251094 (140o16'15"E, 22o31'15"S) to 246097 (140o16'00", 22o31'05"S).|16-MAY-23
4749|Corrie Member|Extent|The unit extends as a 95 km belt from Mt Datson in the south to the Swift Hills in the north.|16-MAY-23
4749|Corrie Member|Thickness range|90 m at Black Mountain; 200 m at Mt Datson; 170 m at Mt Ninmaroo.|16-MAY-23
4749|Corrie Member|Lithology|Medium to thick bedded limestone (pelmatozoan grainstone (grain supported carbonate rocks (Dunham, 1962)) ooid and peloidal (pellet-like) grainstone, skeletal peloidal clast grainstone); minor cross-stratified dolomitic sandstone.|16-MAY-23
4749|Corrie Member|Relationships and boundaries|The unit conformably overlies the Mort Member and is conformably overlain by the Datson Member. The unit is characterised by encrinites (pelmatozoan grainstones): they are usually light grey, weather spheroidally and have uniform crystalline textured appearance.|16-MAY-23
4749|Corrie Member|Age reasons|Apart from pelmatozoan fragments the unit has yielded conodonts which indicate an Early Ordovician (middle Warendian) age (Jones et al. 1971).|16-MAY-23
4749|Corrie Member|Defn author|Smith E.L., 1978|16-MAY-23
4749|Corrie Member|Proposed publication|BMR 1:100 000 Special Map - The Southern Burke River Structural Belt. BMR publication.|16-MAY-23
27951|Cowie Granite|Name source|Named after Cowie prospect, GR 862890, 10 km ESE of Squirrel Hills homestead, Selwyn 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
27951|Cowie Granite|Unit history|Like all other granites in the eastern part of the Duchess 1:250 000 Sheet area, the Cowie granite was mapped as Williams Granite by Carter & Opik (1963).|16-MAY-23
27951|Cowie Granite|Type section locality|In the vicinity of GR 855937, 5 km NNW of Cowie prospect, where the unit forms undulating terrain with extensive low rocky and rubbly exposures of heterogeneous, leucocratic, granitic rocks.|16-MAY-23
27951|Cowie Granite|Extent|Crops out in belt up to 3 km wide trending NNE for 11.5 km from a point 4.5 km W of Cowie prospect, Selwyn 1:100 000 Sheet area. The outcrop area is centred on GR 855940.|16-MAY-23
27951|Cowie Granite|Lithology|The unit consists of heterogeneous, biotite-bearing leucocratic granite, granodiorite and tonalite. The granitic rocks range from fine-grained to pegmatitic, and from massive to foliated; they are commonly xenolithic, but not porphyritic.|16-MAY-23
27951|Cowie Granite|Relationships and boundaries|Cowie Granite intrudes and locally forms migmatitic complexes with the Soldiers Cap Group and also intrudes the Doherty Formation (new name). It is inferred to be intruded by Squirrel Hills Granite to the west, and is cut by porphyritic microgranite considered to be related to the Squirrel Hills Granite.|16-MAY-23
27951|Cowie Granite|Age reasons|Proterozoic.|16-MAY-23
27951|Cowie Granite|Comments|Differs petrographically from, and inferred to be older than, adjacent Squirrel Hills Granite to the west. It is separated geographically from the petrographically similar and probably related Blackeye Granite to the east and Maramungee Granite to the north, and is one of the granites previously mapped as Williams Granite which together with the Wimberu Granite to the west, make up the Williams Batholith (new structural term).|16-MAY-23
4838|Craigie Tonalite|Name source|Craigie Outstation, 7858-705360.  The grid reference is based on the AGD66 datum.|16-MAY-23
4838|Craigie Tonalite|Unit history|White (1959b) defined the unit as Craigie Granodiorite. The name was modified to Craigie Tonalite by Withnall & Lang (1992), but has not been formally redefined. Tonalite is the dominant rock type. White (1959b, 1962) also included 'granodiorite' that crops out north of the Broken River in the Craigie Granodiorite, and suggested a correlation with 'granodiorite' in the Gray Creek Complex. Both of these are north of the Clarke River Fault, and are probably Late Ordovician. They intrude the Early Ordovician Judea Formation, and have since been named the Netherwood Tonalite and Saddington Tonalite respectively by Withnall (1989a) and Withnall & Lang (1992, 1993). They are excluded from the Craigie Tonalite as defined from the type area.|16-MAY-23
4838|Craigie Tonalite|Type section locality|White (1959b) gave the type area as 'good outcrop in Sheepyard Creek on the track from Wando Vale Station, half a mile east of Craigie Outstation'. Assuming that the position of the track has not changed since the 1950s, this location is 7858-705360, just downstream of the crossing. This locality is at the mapped contact between the Craigie Tonalite and the Clarke River Fault/Mylonite Zone. This locality was not re-examined in the present survey, although McLennan (1986) reported that the 'Craigie Granodiorite' was well exposed along the creek and in the Clarke River. Good exposure of grey, medium to coarse grained, equigranular hornblende biotite tonalite occurs near where the track crosses the Clarke River at 720341, and this is given as a reference locality.|16-MAY-23
4838|Craigie Tonalite|Extent|The Craigie Tonalite is the northernmost unit in the batholith, and was described by McLennan (1986) from the 'Craigie' area. It has been mapped as a west-southwest-trending belt up to 5km wide for about 30km along the Clarke River to at least the junction with the Gregory River.|16-MAY-23
4838|Craigie Tonalite|Lithology|The Craigie Tonalite consists mainly of grey, medium to coarse grained, equigranular hornblende biotite tonalite, locally cut by tourmaline pegmatite dykes. Chlorite and epidote alteration are common features of this unit.  Chlorite replaces biotite and locally hornblende. Epidote alteration is also common and occurs in veins (up to 20 cm wide) and as alteration of hornblende, biotite and plagioclase. Calcite alteration after plagioclase is also locally common. Rare small rafts (<2m long) of schist occur within the tonalite up to 2 km from the northern.  Small well rounded tabular xenoliths (up to 30 cm long) of fine to medium grained granodlorite or diorite rock are also present.The tonalite commonly has a foliation defined by alignment of hornblende, biotite and quartz, and is locally sheared. The minerals also define a lineation. The foliation is sub parallel to the trend of the Clarke River Fault. McLennan (1986) interpreted it as a primary flow foliation, overprinted by a later tectonic, mylonitic foliation.|16-MAY-23
4838|Craigie Tonalite|Relationships and boundaries|Because it contains xenoliths of schist, the Craigie Tonalite is inferred to intrude the Cape River Metamorphics that occur along the Clarke River Fault/Mylonite Zone. At Craigie, the zone is a belt of sheared and mylonitised metamorphic rocks about 1km wide. Thin mylonites are common adjacent to the zone, indicating that the tonalite pre-dates the mylonitisation, and therefore the contact may be faulted rather than intrusive. Rocks at the junction of the Clarke River with the Gregory River are also mylonitised, although a younger brittle fault separates these rocks from the Late Devonian Bulgeri Formation of the Broken River Province. To the south, the Craigie Tonalite is mapped in contact with the Blanders Granodiorite. The contact is partly mapped as a fault. Tertiary and Quaternary basalts overlie the Craigie Tonalite over much of the area.|16-MAY-23
4838|Craigie Tonalite|Age reasons|A K Ar hornblende age of 406+/-3Ma was obtained for the Craigie Tonalite on a sample from the Clarke River near the crossing south of Craigie (unpublished AMDEL report to GSQ, 1985). This is a minimum age in view of the deformation.|16-MAY-23
4838|Craigie Tonalite|References|WHITE, D.A., 1959b:  New names in Queensland stratigraphy, Parts 3.  Australian Oil and Gas Journal, 5(10) 31 36.WHITE, D.A., 1962:  Clarke River   1:250000 Geological Series. Bureau of Mineral Resources, Australia, Explanatory Notes E/55 13.WITHNALL, I.W., 1989a:  Revision of the stratigraphy of the Broken River area, north Queensland   Ordovician and Silurian units.  Queensland Government Mining Journal, 90, 213 218.WITHNALL, I.W. & LANG, S.C., 1992: Broken River Special 1:100 000 map. Department of Resource Industries.WITHNALL, I.W. & LANG, S.C. (Editors), 1993: Geology of the Broken River Province, north Queensland. Queensland Geology 7.|16-MAY-23
4885|Cressbrook Creek Group|Unit history|Bryan (1928) first referred to Permo-Carboniferous fossiliferous sediments and rhyolite to the west of Esk as the "Cressbrook Creek Series".  Campbell (1952) defined five formations in the vicinity of Cressbrook Creek, which Swindon (1971) referred to in passing as the Cressbrook Creek Group.  The group is considered equivalent to the original Cressbrook Creek "Series" and was defined by Cranfield & others (1976) as comprising the Pinecliff Formation, Hampton Road Rhyolite, Biarraville Formation, Box Gully Formation, and Buaraba Mudstone|16-MAY-23
4885|Cressbrook Creek Group|Constituents|Defined by Cranfield & others (1976) as comprising the Pinecliff Formation, Hampton Road Rhyolite, Biarraville Formation, Box Gully Formation, and Buaraba Mudstone.........DEFINITIONS  for each unit are separately presented in this database.|16-MAY-23
4885|Cressbrook Creek Group|References|BRYAN, W.H.,1928,A Glossary of Queensland Stratigraphy, University of Queensland.CAMPBELL, K.S.W.,1952,The geology of the Cressbrook-Buaraba area,"University of Queensland.  Department of Geology Papers (New series), Regional Geology.CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.",1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional Geology.|16-MAY-23
27755|Cromwell Metabasalt Member|Name source|From Cromwell Creek, about 64 km north-northeast of Mount Isa, latitude 20o9'S, longitude 139o39'E, and 3 km southwest of Julius dam. The name "Cromwell Beds" was introduced as an informal name by Robinson (1968); the redefined Cromwell Metabasalt Member includes the "Paroo Beds" of Robinson, as well as the "Cromwell Beds", since the distinction between these units (differences in the proportions of basalt and minor sediment) cannot be sustained with certainty over large areas of the Eastern Creek Volcanics.|16-MAY-23
27755|Cromwell Metabasalt Member|Type section locality|From 8 to 2 km east of Mount Isa, just south of the Cloncurry road i.e. 6856 511077 to 6856 452074. This type section was nominated by Robinson (1968) and by Carter et al. (1961). Another reference section is in the Gum Creek area, 16 km northeast of Mount Isa. The type section contains 3600 m of massive amygdaloidal metabasalt and sheared basic rocks interbedded with thin quartzite, epidote quartzite, dolomitic siltstone and tuff. Flows are up to 60 m thick and predominate over sediments.|16-MAY-23
27755|Cromwell Metabasalt Member|Extent|As for the Eastern Creek Volcanics, in a north-trending belt (centred on Mount Isa) 300 km long and up to 40 km wide, mainly in the Cloncurry, Urandangi, Dobbyn, and Mount Isa 1:250 000 Sheets.|16-MAY-23
27755|Cromwell Metabasalt Member|Thickness range|Thickness ranges from 1750 m to 5430 m east and northeast of Mt Isa. A thickness of 3900 m is quoted by Robinson (1968).|16-MAY-23
27755|Cromwell Metabasalt Member|Lithology|Metabasalt, amygdaloidal metabasalt, flow top breccia, sandstone, dolomitic sandstone, siltstone, chert, quartzite.|16-MAY-23
27755|Cromwell Metabasalt Member|Relationships and boundaries|Overlie the Mount Guide Quartzite and Leander Quartzite, and underlies the Lena Quartzite Member conformably. Locally it overlies the basement unconformably viz. at Dynamite Creek, 140 km north of Mount Isa, conglomeratic arkose of the basal Eastern Creek Volcanics overlies the Ewen Granite unconformably (Carter et al., 1961).|16-MAY-23
27755|Cromwell Metabasalt Member|Age reasons|Carpentarian, between 1700 and 1650 m.y. (Plumb & Derrick, 1975).|16-MAY-23
27755|Cromwell Metabasalt Member|Comments|Remarks: The unit was designated the "Cromwell-Paroo Metabasalt member" on the BMR Preliminary Edition of the Mary Kathleen 1:100 000 Sheet area, and the Cromwell Metabasalt Member in the subsequent First Edition map in preparation.|16-MAY-23
27382|Crooked Creek Conglomerate|Name source|Crooked Creek, a tributary of Dinner Creek, which it joins at 7859-776864.  The grid reference is based on the AGD66 datum.|16-MAY-23
27382|Crooked Creek Conglomerate|Unit history|The unit was previously defined as the Crooked Creek Conglomerate Member of the Graveyard Creek Formation (now Group) (White, 1959, 1962, 1965).  It was given formation status by Withnall & others (1988), but not formally redefined.|16-MAY-23
27382|Crooked Creek Conglomerate|Geomorphic expression|The unit forms generally subdued topography, but slightly more elevated than the Quinton Formation, with weak strike trends discernible on aerial photographs.  Where outcrop is poor, a litter of pebbles and cobbles on the ground serve to indicate the presence of the unit.|16-MAY-23
27382|Crooked Creek Conglomerate|Type section locality|White (1959) gave the type area in Dinner and Crooked Creeks.  A type section is chosen in Dinner Creek between 7859 784867 (base) and 754870 (synclinal hinge).  Polymictic pebble to boulder conglomerate (abundant clasts of amphibolite, granite, schist), lithic arenite, and minor mudstone.  Thickness is unknown because of small-scale folding.REFERENCE SECTION::   The other part of White's type area in Crooked Creek, between 7859 725842 (base) and 760837 (synclinal hinge) is designated as a reference section.  The rocks are similar to those in the type section, but clasts of amphibolite are dominant.|16-MAY-23
27382|Crooked Creek Conglomerate|Extent|A southwest trending belt, between Dinner Creek and Gray Creek   rocks near Top Hut Yards are also assigned to unit.|16-MAY-23
27382|Crooked Creek Conglomerate|Thickness range|0 to 300 m at least.|16-MAY-23
27382|Crooked Creek Conglomerate|Lithology|Pebble to boulder, polymictic conglomerate, lithic arenite, and minor mudstone.  The rocks are thick to very thick bedded, but commonly massive and poorly bedded.  The beds have common erosive bases, local grading and pebble imbrication, and rare medium to large scale cross bedding.  Large olistoliths of amphibolite and limestone occur locally.|16-MAY-23
27382|Crooked Creek Conglomerate|Fossils|Corals and conodonts in limestone clasts indicate a Silurian age (probably Llandovery from stratigraphic relationships)|16-MAY-23
27382|Crooked Creek Conglomerate|Relationships and boundaries|The unit is the basal part of the Graveyard Creek Group, and unconformably overlies Judea Formation, and is faulted against and possibly locally unconformably overlies the Proterozoic Halls Reward Metamorphics.  It is conformably overlain by the Quinton Formation from which it is distinguished by the abundance of polymictic conglomerate.|16-MAY-23
27382|Crooked Creek Conglomerate|Age reasons|Corals and conodonts in limestone clasts indicate a Silurian age (probably Llandovery from stratigraphic relationships|16-MAY-23
27382|Crooked Creek Conglomerate|References|WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4. Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.WHITE, D.A., 1962:  Clarke River 1.250 000 Geological series. Bureau of Mineral Resources, Australia, Explanatory Notes, E/55-13.WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
4958|Crows Nest Granite|Unit history|This name, first used by Jones (1955), was formally defined by Cranfield and Schwarzbock (1974b).|16-MAY-23
4958|Crows Nest Granite|Geomorphic expression|The outcrop area forms a north-northwesterly trending belt occupying approximately 100 km2 and is bounded by Pierce's Creek to the north, and the Esk-Hampton Road to the south.  The average elevation is 470 m; however, in places (e. g. near Perseverance Creek Dam), coarser-grained variants form steep cliffs up to 630 m above sea level.|16-MAY-23
4958|Crows Nest Granite|Type section locality|The type locality extends along the Crow's Nest-Perseverance Creek Dam road from about AMG 40980 69803 to 41180 69813.  The grid references are based on the AGD66 datum.|16-MAY-23
4958|Crows Nest Granite|Lithology|Cranfield & others (1976) described the constituent rock types as granite, with minor adamellite and pegmatite.  Under the UIGS nomenclature both granite and adamellite are now considered as granite.  Petrologically they consist of coarse perthitic intergrowths, minor oligoclase, quartz, biotite altering to chlorite, and euhedral sphene accessories (up to 3 mm in diameter).  Cranfield & others (1976) described late stage hydrothermal alteration of the granite producing kaolinitic clay at about AMG 4070 69920.  A pegmatitic phase of the granite occurs in the vicinity of Perseverance Creek, where cassiterite and fluorite occur as accessory minerals.  Minor aplite dykes that are more common south of Ballard Creek cut the unit.  The unit is conspicuously jointed, with a dominant easterly trend and a strong complementary northerly trend. The locus of intrusion of late stage emanations from the granite (e. g. aplite dykes and volatiles) is controlled by these two master joint systems, so that the late stage aptite dykes and veins are elongated east-west.  The unit was mapped in student project theses by Will (1974), Vonhoff (1975) and Holden (1991).   Holden (1991) recognised 5 granite members and an aplite member that forms a marginal phase and numerous dykes.  He informally named these units `Rocky Creek Granite¿, Central Granite, `Vonhoff Granite¿, `Woodville Granite¿ Paradise graniteand the `Rangeview Aplite¿.  The approximate location and outcrop and thin section characteristics of his subdivisions are given in Table 12 (Cranfield et al 2001).  Holden (1991) also recognised three phases of dykes in the granite ¿ aplite within the Crows Nest Granite, dolerite in the Sugarloaf metamorphics and rhyolite in the Eskdale Granodiorite.|16-MAY-23
4958|Crows Nest Granite|Relationships and boundaries|Holden (1991) could not identify the relative ages between his different subunits of the Crows Nest granite.  The granite intrudes the Sugarloaf Metamorphics and the Permian Cressbrook Creek Group and is unconformably overlain by the Triassic- Jurassic Bundamba Group and the Tertiary Main Range Volcanics.  The zone of hornfels of the Crow's Nest Granite is very narrow, usually less than 30 m, and is best represented in the vicinity of Pierce's Creek where a zone of dark brown flinty hornfels is developed in the Sugarloaf Metamorphics.  The relationship of the Crows Nest granite to the Eskdale Igneous Complex is unknown. Clowes (1997) considered there were two possibilities: -- The Crows Nest granite intruded prior to the Eskdale and the Eskdale intruded through it leaving roof pendants of Crows Nest Granite at the core of unit Rges1 alternatively,- The Crows Nest Granite represents a fractionated product of the Eskdale.  Clowes (1997) indicated that there were no definite geochemical trends to support this proposal.|16-MAY-23
4958|Crows Nest Granite|Age reasons|Radiometric dating of biotite from this granite has given ages of 234 and 237 +/- 8 Ma, (K/Ar) and 242Ma (Rb/Sr), indicating a Late Permian or Early Triassic age.|16-MAY-23
4958|Crows Nest Granite|Comments|GEOCHEMISTRY::  Holden (1991) carried out geochemistry on the Crows Nest Granite and showed that each of the phases had very similar spidergram patterns.  The CIPW mineralogy of the samples indicated normative corundum and hypersthene which was interpreted by Holden (1991) to indicate that the Crows nest granite had an s-type affinity.|16-MAY-23
4958|Crows Nest Granite|References|CLOWES,1997,Use of GIS in the assessment of local and regional changes in granitoids,Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology","Eskdale Granodiorite, Crows Nest granite geochemistry.CRANFIELD, L.C. & SCHWARZBOCK, H., 1974, New and revised stratigraphic names for the Ipswich 1:250 000 Sheet area.,"Queensland Government Mining Journal, 75, 322-323.CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.",1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional GeologyHOLDEN, A.,1991,A study of the northern part of the Crow's nest Granite Batholith., Unpublished Thesis, Department of Geology, university of Southern QueenslandJONES, J.B.,1955, The petrology and economic potentialities of the Eskdale Complex, Unpublished honours thesis, Department of Geology, University of Queensland.VONHOFF, J.D.,1975, The geology of the North and South Branch Buaraba Creeks, South Eastern Queensland, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.|16-MAY-23
4968|Croydon Volcanic Group|Name source|The name is derived from Croydon township, at grid reference (GR) 7361 (CROYDON 1:100 000 Sheet) 315868, or 142o21'E, 18o10'S.|16-MAY-23
4968|Croydon Volcanic Group|Unit history|Jensen (1923) used the name 'Croydon Series' for the igneous rocks of the Croydon area, and Honman (1937) used the term 'Croydon Felsite' for the volcanic rocks of the area. White (1959) defined 'Croydon Felsite', then changed the name to 'Croydon Volcanics' (White, 1965), which was redefined by Branch (1966). Mackenzie (1983) informally named and described the 'Croydon volcanic group'.|16-MAY-23
4968|Croydon Volcanic Group|Constituents|The Croydon Volcanic Group consists of the following units, in descending stratigraphic order: Idalia Rhyolite, including Democrat Rhyolite Member. Carron Rhyolite, including Littleton Dacite Member. Parrot Camp Rhyolite, including Nancy Lee Sandstone Member. B Creek Rhyolite. Wonnemarra Rhyolite. Goat Creek Andesite. Wallabadah Siltstone.|16-MAY-23
4968|Croydon Volcanic Group|Extent|The Croydon Volcanic Group extends over approximately 3100 km2 from the Carron River in the north (17o57'S) to the Yappar River in the south (19o04'S), from the Gilbert River in the northeast to the Croydon area (about 142o11'E) in the northwest, and from near the Langdon River in the east (142o58'E) to between 142o42' and 142o27' in the southern and central areas.|16-MAY-23
4968|Croydon Volcanic Group|Lithology|Rhyolitic to rhyodacitic ignimbrite makes up the bulk of the Croydon Volcanic Group; dacitic ignimbrite, rhyolitic to dacitic lava, basaltic andesite, and quartzose sandstone and siltstone are minor constituents, and rhyolitic tuff is rare. Most rocks are characterised by the presence of up to 1-2 percent graphite, either disseminated or in rounded pellets up to 1 cm in diameter.|16-MAY-23
4968|Croydon Volcanic Group|Relationships and boundaries|The Croydon Volcanic Group is flanked to the east by low-grade metasedimentary rocks of the Early to Middle Proterozoic Etheridge and Langlovale Groups (Withnall & Mackenzie, 1980, 1983). For most of its length, the contact is faulted, but in places it appears to be an angular unconformity (e.g. north of Snake Creek where the Wonnemarra Rhyolite overlies the Proterozoic metasediments). The volcanics are intruded by Middle Proterozoic Esmeralda, Nonda, Mooremount, Little Bird, Chadshunt, Macartneys, Olsens, Dregger, Bimba, and Illewanna Granites, by the Permian Awring Granodiorite, and the Permian? Wallys Dolerite. The Group is unconformably overlain by the Middle to Late Proterozoic Inorunie Group, the Permian Bullseye Rhyolite, Linley Rhyolite, Little Pocket Dacite, and McFarlanes Andesite, the Mesozoic Eulo Queen Group, Gilbert River Formation, and Wallumbilla Formation, the late Mesozoic to Tertiary Bulimba Formation, and late Tertiary to Quaternary fluviatile and residual sediments including the Claraville Formation.|16-MAY-23
4968|Croydon Volcanic Group|Age reasons|The Idalia Rhyolite and Democrat Rhyolite Member have been isotopically dated at 1400+/-75 Ma (Richards & others, 1966; Black, 1973). Preliminary results of a re-evaluation of the Rb/Sr isochron and elimination of determinations from altered and/or weathered samples show that the age may be closer to 1440 Ma (R. Holmes, pers. comm., 1984).|16-MAY-23
24233|Culba Granodiorite|Name source|Parish of Culba, County of Percy|16-MAY-23
24233|Culba Granodiorite|Unit history|Previously mapped as Dumbano Granite (White, 1962).|16-MAY-23
24233|Culba Granodiorite|Type section locality|Between GR 027 678 and 008 690 (Gilberton 1:100 000 Sheet area), upstream along Pinnacle Creek and one of its tributaries. Grey medium grained equigranular hornblende-biotite granodiorite is exposed between GR 027 678 and 014 688, and pink fine grained biotite granite is exposed between GR 014 688 and 008 690.|16-MAY-23
24233|Culba Granodiorite|Extent|Forms the northern part of the Glenmore batholith about 12 km west of Glenmore homestead. The intrusion is 9 km long (from north to south) and 5 km wide in the north, tapering southwards. The total area is about 35 km2.|16-MAY-23
24233|Culba Granodiorite|Lithology|Two rock types as described in the type area; the fine to medium grained, equigranular, non-foliated hornblende-biotite granodiorite is the most extensive; the younger, generally finer grained biotite granite is restricted to the southwestern margin of the unit.|16-MAY-23
24233|Culba Granodiorite|Relationships and boundaries|Intrudes the Proterozoic Einasleigh Metamorphics and late Proterozoic or Devonian Anning Granite and Dumbano Granite. Intruded by members of the Carboniferous Bagstowe Ring Complex.|16-MAY-23
24233|Culba Granodiorite|Age reasons|Probably Carboniferous; it has a massive, unfoliated character and is petrographically similar to other late Palaeozoic granitoids in north Queensland, e.g. the Yataga Granodiorite (Withnall & others, 1976).|16-MAY-23
24237|Curlew Formation|Name source|Curlew Spit; grid reference 290 000E, 7 395 000N Bajool 1:100 000 Sheet area.|16-MAY-23
24237|Curlew Formation|Unit history|Part of The Narrows Beds of Kirkegaard and others (1970).|16-MAY-23
24237|Curlew Formation|Type section locality|From 2 to 121 metres depth (fully cored below 18 metres) in RDD66 (grid reference 299441E, 7 382 121N Gladstone 1:100 000 Sheet area).|16-MAY-23
24237|Curlew Formation|Extent|Subcrops in an area of about 10 km2 in The Narrows Graben, NW of Gladstone, Qld. Very sparse (mostly weathered) outcrops are present; the formation has been identified from drill hole core.|16-MAY-23
24237|Curlew Formation|Thickness range|119 m down-hole (vertical) in the type section (estimated true thickness 115 m assuming 15o dip of strata).|16-MAY-23
24237|Curlew Formation|Lithology|Greenish-grey to pale grey claystone with interbedded black carbonaceous to coaly shale and minor calcareous sandstone and limestone beds (latter up to 0.7 m thick).|16-MAY-23
24237|Curlew Formation|Relationships and boundaries|The base of the formation is conformable with the Rundle Formation and is defined by a thick (generally about 20 metres) interbedded carbonaceous shale and grey claystone bed which grades into carbonaceous oil shale, for up to 5 metres, above the contact with the Rundle Formation. The top of the formation is eroded. It is unconformably overlain by Quaternary overburden, and is faulted against Palaeozoic rocks (basement) at the western margin of The Narrows Graben.|16-MAY-23
24237|Curlew Formation|Age reasons|The Curlew Formation is middle to late Eocene on megaspore evidence (Foster and Harris, 1981).|16-MAY-23
24237|Curlew Formation|Proposed publication|Bulletin of the American Association of Petroleum Geologists|16-MAY-23
24237|Curlew Formation|Comments|The drill core from RDD66 is currently stored in Southern Pacific Petroleum's core shed at Rundle. To be transferred at a later date to Southern Pacific Petroleum's core shed located in Gladstone, Qld.|16-MAY-23
33424|Dangore Volcanics|Unit history|Murphy & others (1976) previously mapped the unit as part of the mainly mafic Tertiary Main Range Volcanics.  Unpublished Geological Survey mapping indicated the presence of felsic volcanic in the vicinity of Dangore Mountain.  Field checking of an area of high radiometric signature on the ternary K-Th-U radiometric image resulted in the determination of a mainly acid volcanic sequence dominated by rhyolitic volcanics.|16-MAY-23
33424|Dangore Volcanics|Geomorphic expression|The unit forms elevated heavily wooded country including a 140m elevation change from the adjacent country at Mount Dangore.  The unit ranges from about 460m to600m at Mount Dangore.|16-MAY-23
33424|Dangore Volcanics|Extent|The unit is situated 25km north-west of Kingaroy south of the Chinchilla-Wondai road, where it is exposed as a roughly rectangular area covering around 25km2.|16-MAY-23
33424|Dangore Volcanics|Thickness range|The unit appears to be shallow dipping (to 150); thickness of approximately 200m is suggested herein.|16-MAY-23
33424|Dangore Volcanics|Lithology|The unit is composed of rhyolite breccia and rhyolitic ignimbrite in a section along the Dangore Mountain Road.  The rhyolite breccia is mottled and weathered and comprises angular, granule to cobble -size clasts of flow-banded rhyolite in an ashy groundmass at AMG 359315 7073198 and 360893 7073778.  The rhyolitic ignimbrite is strongly jointed and typically forms low pavement exposure along the Dangore Mountain Road and an adjacent forestry track to the north of the road.  The ignimbrite has steep jointing and is crystal-rich in exposures at AMG 360054 7073578, 359602 70749910 and 360248 7073530, and both crystal-rich and clast-rich at 360054 7073578 and 359602 70749910.  A thin section ignimbrite from AMG 360054 7073578 is a clast-bearing crystal-rich pyroclastic rock.  Crystals which comprise close to 45 % of the rock consist dominantly of broken, altered subhedral plagioclase (90%, to 2mm), quartz as resorbed broken crystals (5%, to 1.5 mm), and chlorite (? After biotite and associated with opaques (2%, to 2mm).  Clasts (~ 15% of the rock) consist dominantly of pumice (70%, 0.5- 3mm).  The pumice is strongly flattened and recrystallised and has locally been altered to quartz-carbonate masses.  The groundmass is light brown in thin section and comprises a strongly welded mass of pumice and welded glass shards. The grid reference is based on the AGD66 datum.|16-MAY-23
33424|Dangore Volcanics|Age reasons|The unit is lithologically similar to the Aranbanga Volcanic Group, and in a similar structural position; it is assumed to be of Late Triassic age.|16-MAY-23
33424|Dangore Volcanics|Correlations|The unit is assumed to be an age correlative of the Aranbanga Volcanic Group.|16-MAY-23
33424|Dangore Volcanics|Comments|STRUCTURE:: The unit appears to be shallowly dipping throughout and unconformable on unit Rgbo of the Boondooma Igneous Complex.GEOPHYSICAL EXPRESSION:: The unit is characterised by a roughly square-shaped brown-coloured radiometric anomaly on the K-Th-U ternary image that covers the outcrop of the Dangore Volcanics, and a complex moderate to high composite north-east-trending magnetic anomaly that covers a larger area than the outcrop of the unit|16-MAY-23
33424|Dangore Volcanics|References|MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.|16-MAY-23
26300|Daniel Creek Formation|Name source|Daniel Creek, which joins Lane Creek at GR 602013 (Forest Home 1:100 000 Sheet area).|16-MAY-23
26300|Daniel Creek Formation|Unit history|The rocks in the Daniel Creek Formation were previously included in the Robertson River Formation of Withnall & Mackenzie (1980).|16-MAY-23
26300|Daniel Creek Formation|Geomorphic expression|The unit produces moderate to hilly relief with moderate to good exposure in the Gilberton and Forsayth areas. In the Georgetown area, it has more subdued relief and poor exposure. Well-defined bedding trends occur in some areas, particularly where quartzite is more abundant.|16-MAY-23
26300|Daniel Creek Formation|Type section locality|The holostratotype is along the Percy River for about 1.4 km, between GR 633788 (Gilberton 1:100 000 Sheet area) and 622796 (Bellfield, 1:100 000 Sheet area). This was formerly a reference section (hypostratotype) designated by Withnall & Mackenzie (1980) for the Robertson River Formation which is now redefined as a subgroup. In this section, which is about 1000 m thick, the unit consists predominantly of cleaved mudstone and siltstone with lesser amounts of fine-grained, locally slightly calcareous, subfeldspathic to quartzose sandstone. However, towards the top, several hundred metres of the sequence contains up to 50 percent of thick-bedded sandstone. The sandstone beds are laminated and locally cross-bedded on a small scale. They commonly contain ellipsoidal calcareous concretions. This sandy interval is thought to be equivalent to the Mount Helpman Member, mapped in the higher grade parts of the formation (see below).|16-MAY-23
26300|Daniel Creek Formation|Description at type locality|Reference section: The section exposed downstream along Bull Creek and one of its tributaries from GR 737106 to 711149 (Forsayth 1:100 000 Sheet area) is designated as a reference section (parastratotype) for the 'schist facies' (inferred to be the base and top of the unit respectively). The rocks exposed in this section are mica schist, micaceous quartzite and minor calc-silicate rocks. This section includes the type section (holostratotype) of the Mount Helpman Member (GR 723132 to 714147).|16-MAY-23
26300|Daniel Creek Formation|Extent|The main outcrop area is in the Gilberton and Forsayth 1:100 000 Sheet areas, and extends from the Gilberton Fault north to about the Robertson River. In this area it is infolded with the Bernecker Creek Formation, Dead Horse Metabasalt, and Corbett Formation. In the Georgetown and Forest Home 1:100 000 Sheet areas, it extends from Talbot Creek north for about 40 km along the western side of the Newcastle Range, and as screens in the Forsayth Batholith for 15 km to northwest of Georgetown. The total area is about 1500 km2.|16-MAY-23
26300|Daniel Creek Formation|Thickness range|In the Gilberton area, the formation is 1000 to 2000 m thick. Elsewhere the thickness cannot be determined because of repetition byh the complex multiple folding events.|16-MAY-23
26300|Daniel Creek Formation|Lithology|Cleaved mudstone, siltstone and sandstone as in the type section grading eastwards into mica schist, quartzite and minor calc-silicate rocks.|16-MAY-23
26300|Daniel Creek Formation|Relationships and boundaries|The formation is the lowermost unit of the Robertson River Subgroup. It conformably overlies the Bernecker Creek Formation, and the base is defined by the change from predominantly calcareous to non-calcareous sandstone, siltstone and mudstone (or their metamorphic equivalents). In the Gilberton area the formation is conformably overlain by the Dead Horse Metabasalt is absent. In the Georgetown area however, the Dead Horse Metabasalt is absent and schistose equivalents of the Daniel Creek Formation are conformably overlain by the Corbett Formation, which is distinguished by its lack of quartzite. The Mount Helpman Member, which is characterised by a greater abundance of micaceous quartzite, has been mapped in the higher-grade (schist facies) of the Daniel Creek Formation. Its low-grade equivalents have been recognised in some sections, but have not been mapped out. The Daniel Creek Formation is thought to be a more pelitic lateral equivalent of the biotite gneiss facies of the Einasleigh Metamorphics; mica schist of the Daniel Creek Formation grades into biotite gneiss of the Einasleigh Metamorphics with increasing feldspar content. The Daniel Creek Formation is intruded by sills of Proterozoic Cobbold Metadolerite, as well as by numerous Proterozoic granitoids, the Siluro-Devonian Robin Hood Granodiorite, and late Palaeozoic hypabyssal rocks. The formation is unconformably overlain by the Devonian-Carboniferous Gilberton Formation, the late Palaeozoic Newcastle Range and Agate Creek Volcanics, and the Jurassic Hampstead Sandstone.|16-MAY-23
26300|Daniel Creek Formation|Age reasons|The minimum age of 1570+/-20 m.y. (mid-Proterozoic) obtained for the Etheridge Group (Black & others, 1979), also applies to the Daniel Creek Formation.|16-MAY-23
5263|Datson Member|Name source|From Mount Datson (140o23'E, 22o47'S) on Boulia 1:250 000 Sheet area.|16-MAY-23
5263|Datson Member|Unit history|Generally equates with Unit 6 of Casey (1968). Laminated Dolomite Member of Jones et al. (1971) and Member(v) of Druce (1976).|16-MAY-23
5263|Datson Member|Type section locality|Black Mountain (140o17'E, 22o32'S), the interval from 585 m to the top of the section within the Ninmaroo Formation from 246097 (140o16'00"E, 22o31'05"S) to 240101 (140o15'30"E, 22o31'00"S).|16-MAY-23
5263|Datson Member|Extent|The unit is exposed in a 95 km belt from Mount Datson in the south to the Swift Hills in the north.|16-MAY-23
5263|Datson Member|Thickness range|At least 200 m thick at Black Mountain; 295 m at Mount Datson; 62 m+ at Mt Ninmaroo.|16-MAY-23
5263|Datson Member|Lithology|Thin to thick bedded limestone or dolostone (skeletal grainstone, boundstone, peloidal (pellet-like) grainstone, clast grainstone and lime mudstone (Dunham, 1962)). Characterised by dolomitisation and interlaminated cherts.|16-MAY-23
5263|Datson Member|Relationships and boundaries|The Datson Member conformably overlies the Corrie Member. The unit is overlain by the Swift Formation which is in part, a weathering product of the Ninmaroo Formation. Field evidence suggests that in some places there is no break in the Ninmaroo-Swift sequence whereas in other places (Mt Ninmaroo) there is evidence of mild folding in the Ninmaroo Formation (Datson Member) but not in the Swift Formation. Dolomitization and silicification is characteristic of the unit.|16-MAY-23
5263|Datson Member|Age reasons|The unit contains conodonts and trilobites which suggest an Early Ordovician (late Warendan to early ?Arenigian) age (Jones et al., 1971).|16-MAY-23
5263|Datson Member|Proposed publication|BMR publication, BMR 1:100 000 Special - The Southern Burke River Structural Belt.|16-MAY-23
21622|Davey Creek Granite|Name source|Davey Creek which joins Lolworth Creek at GR 2933 77644 in the Lolworth 1:100 000 Sheet area.   The grid reference is based on the AGD66 datum.|16-MAY-23
21622|Davey Creek Granite|Unit history|The Davey Creek Granite was previously included in the Lolworth Igneous Complex by Paine & others (1971) and Vine & Paine (1974).|16-MAY-23
21622|Davey Creek Granite|Type section locality|Beside the Pentland-Lolworth road, 4km north of Goldsborough homestead at GR 2912 77552 in the Lolworth 1:100 000 Sheet area. The grid reference is based on the AGD66 datum.|16-MAY-23
21622|Davey Creek Granite|Description at type locality|Here a pink, medium grained, equigranular to slightly porphyritic, muscovite-biotite granite crops out.|16-MAY-23
21622|Davey Creek Granite|Extent|The Davey Creek Granite crops out over about 45km2 in a roughly east-west belt from northwest of Goldsborough homestead to Reedy Creek.|16-MAY-23
21622|Davey Creek Granite|Lithology|The rocks are mostly similar to those at the type locality throughout the unit, but there is some variation probably reflecting alteration. In the eastern part of the pluton, pink, medium grained, slightly porphyritic muscovite-biotite granite has much lower magnetic susceptibility and is probably more altered. The Davey Creek Granite is intruded by leucogranite sheets and dykes that are similar to the Grasstree Leucogranite.|16-MAY-23
21622|Davey Creek Granite|Relationships and boundaries|The Davey Creek Granite intrudes the Proterozoic Cape River Metamorphics near Goldsborough homestead (Figure 2). It is intruded by leucogranite dykes similar to the Grasstree Leucogranite. It is part of the 'background granites' in the Lolworth Batholith.|16-MAY-23
21622|Davey Creek Granite|Age reasons|The age of the Davey Creek Granite is Late Silurian to Early Devonian. K-Ar ages of 400 +/- 12 Ma (biotite) and 404 +/- 12 Ma (muscovite) were reported by Webb (in Paine & others 1971, recalculated to new constants), on a sample from the Davey Creek Granite.|16-MAY-23
21622|Davey Creek Granite|Comments|MAGNETIC SUSCEPTIBILITY::  Magnetic susceptibilities of rocks at the type locality are in the range 435-600 x 10[superscript]-5 SI units. Elsewhere in the unit, magnetic susceptibilities are much less and are 0-75 x 10[superscript]-5 SI units.|16-MAY-23
21622|Davey Creek Granite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
79120|Dawn Formation|Name source|After Dawn Mine southwest of Gympie.|16-MAY-23
79120|Dawn Formation|Unit history|This unit was first identified informally as the Alma unit by Arnold (1996) for Gympie Eldorado Gold Mines at Monkland Mine and was referred to as such by Cranfield (1999), Sivell & Arnold (1999), Sivell & McCulloch (2001) and Li & others (2015) .  The term Alma is already in use elsewhere in Queensland. Equivalent to Dunstan's (1911) tuff and shale members of his Third Slate Group (3MS, 3LT, 3LS). Known to early miners as the 'Third bed of slate'. Rands (1889) described it as 'fine grained greywacke with beds of black and grey shale' and 'purplish chloritic rock'.|16-MAY-23
79120|Dawn Formation|Constituents|Hall Clastics Member, Kidgell Andesite Member, Excelsior Conglomerate Bed|16-MAY-23
79120|Dawn Formation|Type section locality|Located along a road cutting on Dobbo's Road off Fisherman's Pocket Road (MGA 460595mE; 7105660mN,  Lat: -26°10'05",  Long: 152°36'21"). Reference section: GEGM drill hole G215: 216.6-263.8 m at North Inglewood (MGA 467424mE; 7101493mN). Core held at Zillmere core library. Other sections: A well-bedded section is exposed in a cutting on the Bruce Highway at the northern end of Spring Valley Road and a safer exposure can be seen in a deep cutting on Spring Valley Road, about 700 m south of the Kilkivan turnoff (QFG8340; MGA 457505mE, 7109890mN) where thrust faulting is also present.|16-MAY-23
79120|Dawn Formation|Extent|Throughout the goldfield. Surface exposures are found from Curra quarry in the northwest, through Chatsworth on either side of the Highbury range of hills, down to Glastonbury Road. In mine workings it was encountered in numerous early shafts sunk to the 'Third bed of slate' in the Phoenix and Monkland blocks, such as Ellen Harkins and Wilmot Extended (Rands, 1889), and at depth in Monkland Mine and North Inglewood. Widespread below shallow cover in the Dawn Block, and intersected below the Curra Thrust in West Phoenix and Sovereign blocks.|16-MAY-23
79120|Dawn Formation|General description|The Dawn Formation incorporates five of the units that were used at Monkland Mine. This is a variation on the proposal by Arnold (in Murray et al., 2002, appendix 13). The bulk of the formation consists of distinctive pale greenish siltstones, mudstones and 'chert', intercalated with dacitic pyroclastic rocks (Alma unit of GEGM) which are particularly widespread on either side of the Highbury hills and around Chatsworth. These fine-grained clastics and tuffs grade upwards into a coarse-grained pyroclastic unit (Hall Clastics) of basaltic and andesitic provenance, intercalated with flows of Tozer basalt and Kidgell Andesite. Within both these volcanoclastic units are carbonaceous shale beds of varying thickness, here referred to informally as Ellen Harkins shale. At the base is the Excelsior bed, a narrow conglomerate marker horizon capping the Highbury Basalt.|16-MAY-23
79120|Dawn Formation|Thickness range|50 to 200 m thick, 150 m at West Phoenix. Could be considerably thicker southwest of Highbury hills.|16-MAY-23
79120|Dawn Formation|Lithology|At the type locality dome-shaped dacitic tuff occurs within shallow dipping tuffaceous siltstones.  In drill core the dominant lithology is a light grey to pale green tuffaceous siltstone or mudstone, interspersed with beds spattered with dark grey vitric shards and wispy flattened pumice of probable dacitic composition. The dark chloritic pumice beds are a diagnostic feature of the unit, some with phenocrysts of feldspar and some quartz.  Also within the sequence are zones of pervasive hematite, both in siltstone and sandstone, generally around 15-20m thick.  Devitrification and alteration of the glass-rich ash has produced silicified intervals of fine grained cherty rock. Evidence of reworking is lacking. The same assemblage can be readily recognized in outcrop; volcaniclastic to cherty mudstone, siltstone and minor sandstone, dacitic tuff,  ignimbrite and rare dacite flows.  Weathered mudstone beds can be finely penciled.|16-MAY-23
79120|Dawn Formation|Relationships and boundaries|In Monkland overlies the hematitic Excelsior conglomerate member, is intruded by Tozer basalt dykes, and grades upwards into coarse volcanogenic sediments of the Hall Clastics.  Where Hall Clastics Member absent the unit is capped by Kidgell Andesite or Mary/Tozer Basalt.|16-MAY-23
79120|Dawn Formation|Age reasons|Li et al. (2015) determined U-Pb ages of detrital zircons extracted from sample GY1312 located just off Rammutt Road at MGA 461987mE, 7108831mN within light greenish dacitic siltstone. The youngest provenance age for this sample peaked at ~302 Ma, indicating that deposition must be younger than this age.|16-MAY-23
79120|Dawn Formation|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie, 12-JAN-2017.|16-MAY-23
79120|Dawn Formation|References|Dunstan, B., 1911: Geology map of Gympie and environs. GSQ Publ. No. 221b.  **Rands, W.H. 1899:Geological Map of part of Gympie Goldfield.  Geological Survey of Queensland.  **Arnold, G.O., 1996. Geology of the Southern Gympie Goldfield from core logging, and implications for mineralisation.  Unpublished report to Gympie Eldorado Gold Mines Pty Ltd.  **Cranfield, L.C., 1999: Gympie Special Sheet 9445, Part 9545, Queensland 1:100,000 Geological Map Commentary. Queensland Department of Mines and Energy, Brisbane.  **Sivell, W.J. and Arnold, G.O. 1999: Geochemical and volcanic stratigraphy of a segment of an island arc ¿ Gondwana rim accretion zone, Gympie Province, southeast Queensland.  IN Flood, P.G. (Editor): Regional Geology, Tectonics and Metallogenesis, New England Orogen, NEO ¿99 Conference, 255-266.  **Sivell, W.J. and McCulloch, M.T. 2001: Geochemical and Nd-isotopic systematics of the Permo-Triassic Gympie Group, southeast Queensland.  Australian Journal of Earth Sciences 48, 377-394.  **Li, P., Rosenbaum, G., Yang, J-H. and Hoy, D. 2015. Australian-derived detrital zircons in the Permian-Triassic Gympie terrane (eastern Australia): Evidence for an autochthonous origin. Tectonics, 34, 858-874.  **MURRAY, A., McQUITTY, B., HOUSTON, M., BECKTON, J. & CRAN, J., 2002: Exploration Permits for Minerals 6031, 10578, 11122, 11123, 12298. Gympie Project. Annual combined report for period ending 31st October 2002.|16-MAY-23
27080|Dead Horse Metabasalt|Name source|Dead Horse Creek which flows into the Gilbert River at GR 588834 (Bellfield 1:100 000 Sheet area).|16-MAY-23
27080|Dead Horse Metabasalt|Unit history|Dead Horse Metabasalt Member (Withnall & Mackenzie, 1980).|16-MAY-23
27080|Dead Horse Metabasalt|Geomorphic expression|The unit generally produces a subdued relief and has a characteristic reddish-brown tone on colour aerial photographs.|16-MAY-23
27080|Dead Horse Metabasalt|Type section locality|The holostratotype of the Dead Horse Metabasalt, as defined by Withnall & Mackenzie (1980), is along an unnamed tributary of the Percy River between GR 632823 (bottom) and 633813 (top), parallel to the track between Iona homestead and Agate Creek a few hundred metres east of it. Most of the section consists of fine-grained, green, massive metabasalt, but the upper 200 m (approx.) contains well-preserved pillows, hyaloclastic breccias, and amygdales. Beds of grey-green phyllitic shale and siltstone up to 10 m thick occur in several parts of the section. Some coarser-grained basic rocks may be metadolerite sills or dykes.|16-MAY-23
27080|Dead Horse Metabasalt|Description at type locality|Reference sections: The section exposed for about 1 km along the Percy River between GR 622796 (bottom) and 617802 (top) (Bellfield 1:100 000 Sheet area) is herein designated as a reference section (hypostratotype) for the Dead Horse Metabasalt. The section lies between the holostratotype of the Daniel Creek Formation and one of the parastratotypes of the Corbett Formation. It contains similar rocks to those in the holostratotype, but is better exposed. Fine-grained amphibolite containing relict amygdales and possible pillow structures and hyaloclastites is exposed in Bull Creek between GR 711149 and 711151 (Forsayth 1:100 000 Sheet area), about 700 m downstream of the Robin Hood-Middle Yard track. This section is designated as a hypostratotype for the more highly metamorphosed part of the Dead Horse Metabasalt.|16-MAY-23
27080|Dead Horse Metabasalt|Extent|The Dead Horse Metabasalt is exposed in the northwestern quarter of the Gilberton 1:100 000 Sheet area, where it has a total area of approximately 80 km2. In the North Head 1:100 000 Sheet area, the unit crops out over about 150 km2 in a belt extending east from near South Head homestead to the Robertson River. Amphibolites, which are more highly metamorphosed equivalents of the metabasalt crop out in the Forsayth 1:100 000 Sheet area in a narrow sinuous belt extending north from Agate Pocket to the Robertson River and then northeast to the Newcastle Range.|16-MAY-23
27080|Dead Horse Metabasalt|Thickness range|In the Gilberton and North Head areas the unit is 300 to 1000 m thick, but in the Georgetown area it has pinched out entirely and the Corbett Formation directly overlies the Daniel Creek Formation.|16-MAY-23
27080|Dead Horse Metabasalt|Lithology|The Dead Horse Metabasalt consists of metabasalt and minor interbedded quartzite, siltstone and shale. The unit is metamorphosed mostly in the greenschist facies. The metabasalt is mostly massive, but pillows, amygdales, and hyaloclastic breccias occur in places. A weak schistosity is developed locally. However, to the east, in the Forsayth 1:100 000 Sheet area, where the rocks are of amphibolite facies, the unit consists of fine-grained, generally well-foliated amphibolite interlayered with schist.|16-MAY-23
27080|Dead Horse Metabasalt|Relationships and boundaries|The Dead Horse Metabasalt conformably overlies the Daniel Creek Formation and is conformably overlain by the Corbett Formation. The Dead Horse Metabasalt is intruded by sills of Proterozoic Cobbold Metadolerite, and by the Siluro-Devonian Robin Hood Granodiorite and some late Palaeozoic hypabyssal rocks. It is unconformably overlain by the Devonian-Carboniferous Gilberton Formation and Jurassic Hampstead Sandstone.|16-MAY-23
27080|Dead Horse Metabasalt|Identifying features|Withnall & Mackenzie (1980) defined the Dead Horse Metabasalt Member as part of the Robertson River Formation which has now been further subdivided and redefined as a subgroup. The Dead Horse Metabasalt Member is therefore redefined as a formation. The definition is basically as given by Withnall & Mackenzie (1980), but two reference sections are added, and some more highly metamorphosed metabasalts are included in the unit.|16-MAY-23
27080|Dead Horse Metabasalt|Age reasons|The minimum age of 1570+/-20 Ma obtained for the Etheridge Group (Black & others, 1979), also applies to the Dead Horse Metabasalt.|16-MAY-23
27080|Dead Horse Metabasalt|Defn Reference|83/23587 (redefined)|16-MAY-23
21634|Deep Water Creek Granophyre|Name source|Deep Water Creek, which joins White Mountains Creek at GR 2755 77502 in the White Mountains 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
21634|Deep Water Creek Granophyre|Unit history|The Deep Water Creek Granophyre was not shown on the first edition Hughenden 1:250 000 geological map (Vine & Paine, 1974; Paine & others, 1971.|16-MAY-23
21634|Deep Water Creek Granophyre|Type section locality|At 2825 77507 along the Goldsborough-Cargoon boundary fence.  The grid reference is based on the AGD66 datum.|16-MAY-23
21634|Deep Water Creek Granophyre|Description at type locality|Abundant outcrop consists of pink, fine to medium-grained, slightly porphyritic granophyre.|16-MAY-23
21634|Deep Water Creek Granophyre|Extent|The Deep Water Creek Granophyre is a circular pluton approximately 5km in diameter, centred about 2810 77490, 11km west-southwest of Goldsborough homestead.  The grid reference is based on the AGD66 datum.|16-MAY-23
21634|Deep Water Creek Granophyre|Lithology|The Deep Water Creek Granophyre consists of pink, fine to medium-grained, locally porphyritic granophyre. In thin section it consists of graphical intergrowths of quartz and K-feldspar up to 2mm across, subhedral plagioclase laths (generally to 2mm and locally as phenocrysts up to 4mm), and sparse ragged, partly chloritised biotite flakes to 1mm. Miarolitic cavities are common and are partly filled with carbonate.|16-MAY-23
21634|Deep Water Creek Granophyre|Relationships and boundaries|The Deep Water Creek Granophyre intrudes or is faulted against the Cape River Metamorphics along its western and northern margins. To the east, the granophyre appears to intrude an unnamed sequence of rhyolitic ignimbrite of presumed Carboniferous or Early Permian age and possibly related to the Elimeek Volcanics (see below). The Cape River Metamorphics are strongly brecciated over an oblong area of about 5km2 immediately to the north of the pluton. The spatial relationship of this breccia, the ignimbrite and the granophyre, suggests that the area may have been a volcanic centre, and the granophyre may represent magma that has intruded into its volcanic pile. Scattered outliers of the Late Permian Betts Creek beds overlie the unit.|16-MAY-23
21634|Deep Water Creek Granophyre|Age reasons|The Deep Water Creek Granophyre is probably Carboniferous or Permian, and may be related to the Mundic Igneous Complex in the eastern part of the Lolworth 1:100 000 Sheet area. Paine & others (1971) reported granophyre from the complex.|16-MAY-23
21634|Deep Water Creek Granophyre|Comments|MAGNETIC SUSCEPTIBILITY::  The Deep Water Creek Granophyre is weakly magnetic. Magnetic susceptibilities are about 100-200 x 10[superscript]-5 SI units.|16-MAY-23
21634|Deep Water Creek Granophyre|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
24242|Democrat Rhyolite Member|Name source|The name is derived from Democrat Creek, which joins Moonlight Creek at GR 7361-471824.|16-MAY-23
24242|Democrat Rhyolite Member|Unit history|The Democrat Rhyolite Member was previously an undifferentiated part of the Croydon Volcanics (Branch, 1966); it was informally named 'Democrat rhyolite member' and described by Mackenzie (1983).|16-MAY-23
24242|Democrat Rhyolite Member|Geomorphic expression|The area underlain by the unit has moderate to gentle relief, with some steep slopes and common bouldery outcrops. Vegetation cover is grasses and sparse trees; tone on airphotos is pale, but perhaps slightly less so than the Idalia Rhyolite.|16-MAY-23
24242|Democrat Rhyolite Member|Type section locality|The type section extends from GR 7361-482823, near Democrat Creek (base; contact with Esmeralda Granite) to -494833 (top; gradational contact with paler grey, less altered and recrystallised Idalia Rhyolite) on the old Georgetown-Croydon road, and consists of about 30 m of dark bluish-grey, recrystallised, medium-grained, moderately crystal-rich rhyolitic ignimbrite. An informative reference section, which also includes rocks affected by low-temperature, late-stage alteration, is between -563727, 6 km east of Flanigans Gap, and -572740; it is about 60-70 m thick. A more accessible reference section, about 60 m thick and consisting of typical dark grey recrystallised ignimbrite with some late-stage alteration, is along the track east from Stanhills Battery, between 7361-581580 and 7461-594577.|16-MAY-23
24242|Democrat Rhyolite Member|Extent|The unit extends in a belt about 1-2.5 km wide from 1 km north of the Gulf Developmental Highway near Laycocks Crek (7361-583579) southeastward to the White Hill area (-570800), then south of Nonda Creek at about 7461600505. A few small outliers, up to 1 km2, are exposed at the head of Ten Mile Creek (7361-568632), and near the southern end of the belt, northwest of Nonda Creek.|16-MAY-23
24242|Democrat Rhyolite Member|Thickness range|The unit ranges in thickness from about 70 m in the central portion to about 30 m in the north and 20 m in the south.|16-MAY-23
24242|Democrat Rhyolite Member|Lithology|The Democrat Rhyolite Member consists of medium to dark, greenish to bluish grey, moderately crystal-poor to rich rhyolitic ignimbrite, variably altered and/or recrystallised. The crystals, or crystal fragments, are 0.5 to 4 mm across: quartz is commonly bluish, purple, or violet; plagioclase is generally intensely sericitised; K-feldspar, mostly sanidine, is commonly overgrown by graphic quartz-K feldspar intergrowths; biotite (up to 3%) is chloritised. 'Spongy', inclusion-packed grains of garnet are present in trace amounts in all rocks, and graphite is ubiquitous.|16-MAY-23
24242|Democrat Rhyolite Member|Relationships and boundaries|The Democrat Rhyolite Member is a member of the Idalia Rhyolite, but its (upper) boundary with the Idalia Rhyolite is diffuse and imprecisely defined. It was originally thought to be simply a contact-metamorphosed equivalent of the Idalia Rhyolite because of its relationship to the Esmeralda Granite, but petrographic studies have shown that it is slightly richer in chlorite (or biotite), garnet, and graphite than the Idalia Rhyolite. Its distribution, and fluid-inclusion evidence of hydrothermal fluids, suggest that it might also represent an altered carapace over the adjacent tin-mineralised zone in the Esmeralda and Nonda Granites with which it has an intrusive lower contact.|16-MAY-23
24242|Democrat Rhyolite Member|Age reasons|Middle Proterozoic, as for Idalia Rhyolite.|16-MAY-23
24242|Democrat Rhyolite Member|Defn author|Mackenzie D.E., Henderson G.A.M., Warnick J.V., Bain J.H.C., 1985. 86/25125. Mention Map legend|16-MAY-23
24242|Democrat Rhyolite Member|Proposer|Mackenzie D.E., Warnick J.V., Henderson G.A.M.|16-MAY-23
5474|Digger Creek Granite|Name source|Digger Creek which joins the Little Robertson River at GR 669 114 (Forsayth 1:100 000 Sheet area).|16-MAY-23
5474|Digger Creek Granite|Unit history|Included in the Robin Hood Granite (now Granodiorite) and Forsayth Granite by White (1962c).|16-MAY-23
5474|Digger Creek Granite|Type section locality|In Digger Creek between GR 720 074 and 738 068 (Forsayth 1:100 000 Sheet area). Cream garnetiferous muscovite leucogranite and muscovite pegmatitic crop out.|16-MAY-23
5474|Digger Creek Granite|Extent|Crops out in the following parts of the Forsayth and Gilberton 1:100 000 Sheet areas: (a) In the Robertson River catchment west of the Newcastle Range where it forms numerous small granite bodies and pegmatite dykes scattered throughout the Robertson River Metamorphics;  (b) An east-west belt of roof pendants in Robin Hood Granodiorite extending about 20 km west from near "Percyvale" Homestead;  (c) On the eastern side of the Newcastle Range near "Beverly Hills" Homestead;  (d) An area about 16 km south-southeast of "Beverly Hills" Homestead.  Other muscovite leucogranites in the Georgetown and Gilberton 1:100 000 Sheet areas may be related to the Digger Creek Granite.|16-MAY-23
5474|Digger Creek Granite|Lithology|White, grey, and cream to pink varieties of aplitic to pegmatitic muscovite leucogranite; minor biotite, garnet locally present. Foliated in places. Pegmatite dykes common. Large bodies are mustly medium grained.|16-MAY-23
5474|Digger Creek Granite|Relationships and boundaries|Intrusive into the Proterozoic Einasleigh Metamorphics, Robertson River Metamorphics, Oak River Granodiorite (new name), and possibly the Forsayth Granite. Intruded by the Siluro-Devonian Robin Hood Ganodiorite and late Palaeozoic rhyolite, andesite and dolerite dykes. Unconformably overlain by the Carboniferous Newcastle Range Volcanics and Jurassic-Cretaceous sandstone.|16-MAY-23
5474|Digger Creek Granite|Age reasons|Proterozoic; K/Ar dating of a sample of muscovite from a pegmatite near "Robin Hood" Homestead gave a minimum age of 1120 million years (Richards et al., 1966). Recent dating of a sample from the type area by the Ar40/Ar39 incremental heating method indicated a minimum age of 1320 million years; the age obtained by total degassing was 1170 million years.|16-MAY-23
5474|Digger Creek Granite|References|01/31334; 98/29234|16-MAY-23
21660|Dillons Knob Granite|Name source|Dillons Knob, located south of Lolworth Creek at GR 3000 77668.  The grid reference is based on the AGD66 datum.|16-MAY-23
21660|Dillons Knob Granite|Unit history|The Dillons Knob Granite was previously mapped in the Lolworth Igneous Complex by Paine & others (1971) and Vine & Paine (1974).|16-MAY-23
21660|Dillons Knob Granite|Type section locality|Dillons Knob, located south of Lolworth Creek at GR 3000 77668, 8km east of Lolworth Homestead.|16-MAY-23
21660|Dillons Knob Granite|Description at type locality|Here a white to grey, fine to medium grained, porphyritic, garnetiferous muscovite biotite granite forms small knolls. The granite contains clumps of finely felted biotite.|16-MAY-23
21660|Dillons Knob Granite|Lithology|Throughout the outcrop area rocks are similar to those at the type locality and comprise fine to medium grained, white to grey porphyritic muscovite-biotite granite. Felted biotite clumps up to 2cm in diameter are common throughout the unit. About 6km south of Dillons Knob in the headwaters of Flaggy and Brumby Creeks, a pink to grey variant is non-magnetic and is interpreted to be more altered. The unit crops out, particularly in the north of the pluton, as small knolls.|16-MAY-23
21660|Dillons Knob Granite|Relationships and boundaries|The Dillons Knob Granite intrudes the Fat Hen Creek Complex, the intrusive relationship being displayed around GR 3050 77521. Intrusive contacts are interpreted with the Cape River Metamorphics south of Lolworth homestead. The Dillons Knob Granite intrudes the Goldsborough and Oak Vale Granites to the south. Its relationship to the Amarra Granite to the east is not known. To the north it is overlain by Tertiary to Quaternary basalt.  The grid reference is based on the AGD66 datum.|16-MAY-23
21660|Dillons Knob Granite|Age reasons|The age of the Dillons Knob Granite is not known precisely. An age of Late Silurian to Early Devonian is interpreted from the Rb-Sr and K-Ar ages of 400-409 Ma (Recalculated using the decay constants of Steiger and Jager (1977) and Dalyrmple (1978)) that were assigned to the Lolworth Igneous Complex by Webb (1971). The Dillons Knob Granite is petrologically similar to the Amarra Granite which has yielded a  SHRIMP microprobe age of 382 +/- 5 Ma.|16-MAY-23
21660|Dillons Knob Granite|Comments|MAGNETIC SUSCEPTIBILITY::  10-227 x 10[superscript]-5 SI units at the type locality with most samples in the range 140-200 x 10[superscript]-5 SI units. Magnetic susceptibilities in the altered zone are zero.|16-MAY-23
21660|Dillons Knob Granite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
28100|Dinah Formation|Lithology|Fine-grained, medium grey slate, some fine to medium-grained graphite-muscovite phyllite (minor garnet) with subordinate (interbedded) quartzite and schist; grey, sillimanite-graphite-mica schist, commonly quartzose, muscovite-biotite schist and muscovite schist; sillimanite-mica schist, muscovite-garnet gneiss; some graphite-mica schist and quartzite|16-MAY-23
5547|Djuan Tonalite|Unit history|Cranfield and Schwarzbock (1974) applied this name to a tonalite that occurred adjacent to the Crow's Nest-Blackbutt Road.|16-MAY-23
5547|Djuan Tonalite|Geomorphic expression|The unit occupies approximately 95 km2 in the nortwestern margin of ESK and forms a basinal area of undulating sparsely timbered, grazing country, generally between 390m and 420m in elevation.|16-MAY-23
5547|Djuan Tonalite|Type section locality|Type locality along is along the Crow's Nest-Blackbutt Road from about AMG 40100 700400.  The grid reference is based on the AGD66 datum.|16-MAY-23
5547|Djuan Tonalite|Extent|The unit occurs in the north-west corner of ESK and the north-east corner of OAKEY.|16-MAY-23
5547|Djuan Tonalite|Lithology|The main part of the tonalite (PRgj) is grey to dark grey, distinctly xenolithic, and generally variable in grain size and modal composition.  Clots of ferromagnesian minerals commonly form dark patches.  The rock contains plagioclase, quartz, hornblende, biotite, and rarely potash feldspar and clinopyroxene. Accessory magnetite, sphene, apatite, and zircon are present; the major alteration products include sericite, laumontite, chlorite, epidote, iron oxide, and leucoxene.  The rocktypes of the xenoliths in the tonalite vary considerably; some are blocks of Sugarloaf Metamorphics (from fragments of wall rock broken off during intrusion of the tonalite); others are of igneous derivation.  The xenoliths are either round or elongate, and range from a few centimetres to large blocks up to 1 m in diameter.  Most of the xenoliths appear as dark patches of hornblende-rich material containing plagioclase phenocrysts.  The latter are sometimes rounded, or near the boundary of the xenolith is aligned subparallel to the general lineation of hornblende prisms.  Student work by Scott (1963) defined a well-developed platy flow foliation in the unit.  An overall trend of this foliation parallels the trend in the Sugarloaf Metamorphics.  Hornblende laths are strongly aligned resembling metamorphic amphibolites.  Quartz is only a very minor constituent of the rock.Unit Rgjh is characterised by a conspicuous zone of hornblende rich rocks, in the vicinity of the junction of Sandy Waterhole Creek and Emu Creek.Appinite bodies up to 1 km long and 100 m wide, and comprising 50 to 80 percent hornblende (1-10 mm long), occur along the margins of the tonalite.Foliation of the Djuan Tonalite is very prominent and parallels the schistosity of the Sugarloaf Metamorphics, except at the contact where a general east-west trend predominates. Further detailed lithology available in Cranfield et al (2001).|16-MAY-23
5547|Djuan Tonalite|Relationships and boundaries|The Djuan Tonalite intrudes the Palaeozoic Sugarloaf Metamorphics and Maronghi Creek Beds.  The relationship to the Woolshed Mountain Granodiorite is poorly exposed; the units may be of similar age.  The Triassic Tarong beds and Tertiary Main Range Volcanics unconformably overlie the unit.|16-MAY-23
5547|Djuan Tonalite|Age reasons|The K/Ar age of the Djuan Tonalite was quoted as 230 +/- 8 Ma by Cranfield & others (1976) and recalculated to 234.8+/-8 ie late Middle Triassic.  This age was collected from the eastern margin of the unit at AMG 401256 7007103.  Ar/Ar age dates from the unit indicate an older (Permian) age 258.5+/-0.9 (biotite) and 263.7+/-0.9 (hornblende) (Vasconceles & Feng, 2000) from AMG 398768 6999826 on the western margin of the intrusion. Based on the age variations in the unit it is grouped with the Permian to Triassic suite of intrusions in the Yarraman Sub Province.  The grid reference is based on the AGD66 datum.|16-MAY-23
5547|Djuan Tonalite|References|CRANFIELD, L.C. & SCHWARZBOCK, H., 1974, New and revised stratigraphic names for the Ipswich 1:250 000 Sheet area.,"Queensland Government Mining Journal, 75, 322-323.CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.",1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional Geology.SCOTT, I.F.,1963, The geology of the Emu Creek area southeast Queensland.,University of Queensland Bsc honours thesis (unpublished).VASCONCELOS, P. & FENG, Y.,2000, 40Ar/39Ar analyses of biotite and hornblende single crystals from igneous intrusions in SE Queensalnd, Unpublished University of Queensland report|16-MAY-23
24924|Donaldsons Well Volcanic Member|Name source|Donaldsons Well (Clarke River 4 Mile Cadastral Map), about 3 km north northwest of Top Hut Yards.|16-MAY-23
24924|Donaldsons Well Volcanic Member|Unit history|The volcanic rocks were previously mapped as an unnamed member of the Judea beds (Arnold & Henderson, 1976).  The name was first published and described by Withnall & others (1988), but not formally defined.|16-MAY-23
24924|Donaldsons Well Volcanic Member|Geomorphic expression|The unit has a low topographic expression, except in areas recently exhumed from beneath Tertiary basalt cover.  On coloured aerial photographs, it has a reddish brown tone.|16-MAY-23
24924|Donaldsons Well Volcanic Member|Type section locality|Broken River between 7859 670443 (anticlinal hinge) and 666441 (top), where about 250 m of altered basalt and keratophyre are exposed.  The grid references are based on the AGD66 datum.|16-MAY-23
24924|Donaldsons Well Volcanic Member|Thickness range|Less than 1000 m.|16-MAY-23
24924|Donaldsons Well Volcanic Member|Lithology|Altered basalt, dacite (keratophyre), and minor andesite, and jasper. Pillow structures are locally present in the lavas.|16-MAY-23
24924|Donaldsons Well Volcanic Member|Relationships and boundaries|The unit is the lowermost exposed part of the Judea Formation.  It is intruded by the Saddington and Netherwood Tonalites, and locally overlain unconformably by the Poley Cow Formation.|16-MAY-23
24924|Donaldsons Well Volcanic Member|Age reasons|Early Ordovician (interpreted from relationships).|16-MAY-23
24924|Donaldsons Well Volcanic Member|References| ARNOLD, G.O. & HENDERSON, R.A., 1976:  Lower Palaeozoic history of 	the southwestern Broken River Province, north Queensland.  Journal of the Geological Society of Australia, 23, 73-93. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
5619|Doomadgee Formation|Name source|From Doomadgee Mission Station, at metric grid reference 269015 in the Westmoreland 1:250 000 Sheet area, Queensland (SE/54-5).|16-MAY-23
5619|Doomadgee Formation|Unit history|Included by Carter (1959) in the Wollogorang Formation, a name now restricted to an older formation in the Tawallah Group in the McArthur Basin. Roberts et al. (1963) included Doomadgee Formation in the Fickling Beds, which now become the Fickling Group.|16-MAY-23
5619|Doomadgee Formation|Type section locality|180 m of sandstone, siltstone and dolomite exposed in a section 1 km northeast of Gorge Creek, in the southwestern Hedleys Creek Sheet area. The base of the section is at grid reference 878265, and the top is 1.6 km to the southeast, at grid reference 890214.|16-MAY-23
5619|Doomadgee Formation|Extent|The unit is exposed over about 150 km2 in the southwestern part of the Hedleys Creek 1:100 000 Sheet area, Queensland (Sheet 6562) and the adjacent southeastgern part of the Seigal 1:100 000 Sheet area, Northern Territory (6462). The unit extends southward into the northeast corner of the Cleanskin 1:100 000 Sheet area, Northern Territory.|16-MAY-23
5619|Doomadgee Formation|Thickness range|From 180 m at the type section, to over 400 m in the southern Seigal Sheet area.|16-MAY-23
5619|Doomadgee Formation|Lithology|The formation includes conglomerate, sandstone, siltstone, shale and dolomitic rocks. The conglomerate occurs as lenses at the base of the unit, and contain pebbles and cobbles of underlying units, particularly chert and dolomite from the Walford Dolomite. A prominent finely laminated siltstone and black shale member is present in the middle of the formation. Above the member thin bedded manganese-stained fine sandstone is interbedded with dolomite. A prominent lens of conglomerate contains dolomite intraclasts and green clasts or flakes of clay or siltstone.|16-MAY-23
5619|Doomadgee Formation|Relationships and boundaries|Disconformable on Mount Les Siltstone and Walford Dolomite. The contact is marked by pebbly sandstone and conglomerate lenses. The formation is overlain disconformably in the east, and with angular unconformity in the west, by Constance Sandstone.|16-MAY-23
5619|Doomadgee Formation|Age reasons|Proterozoic-Carpentarian. Correlation of part of the underlying Peters Creek Volcanics with the Hobblechain Rhyolite Member of the Masterton Formation in the McArthur Basin suggest an age of less than 1575 m.y. (age of the Hobblechain Rhyolite Member). Younger age limit provided by 1280 m.y. old dolerites which intrude equivalents of the South :Nicholson Group. which unconformably overlies Mount Les Siltstone.|16-MAY-23
5619|Doomadgee Formation|Defn author|Ian Sweet, 1976.|16-MAY-23
5619|Doomadgee Formation|Proposed publication|BMR Bulletin - Precambrian geology of the Westmoreland region, Northern Australia|16-MAY-23
5619|Doomadgee Formation|Defn Reference|82/22568|16-MAY-23
23555|Dosey Limestone|Name source|Dosey Creek, which joins the Broken river at 7859-618443.  The grid reference is based on the AGD66 datum.|16-MAY-23
23555|Dosey Limestone|Unit history|The Dosey Limestone was previously mapped as part of the Broken River Formation (now Group) (White, 1959, 1962, 1965) (parts of 'F', 'G', 'H', and 'I' lenses of White (1965)).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
23555|Dosey Limestone|Geomorphic expression|Generally forms low ridges of limestone outcrops and rubble, and locally low bluffs with karst features.|16-MAY-23
23555|Dosey Limestone|Type section locality|Lomandra Creek, between 7858-608410 (boundary with Storm Hill Sandstone) and 608410 (boundary with Papilio Mudstone).  The section is 230 m thick, and is part of section SD170 of Mawson & Talent (in press).REFERENCE SECTION::  Broken River between 7859-610442 (boundary with the Burges Formation) and 609443 (boundary with the Papilio Mudstone).  The section is 55 m thick and consists mainly of calcarenite and calcirudite (Withnall & others, 1988, figure 30).|16-MAY-23
23555|Dosey Limestone|Description at type locality|The lowermost 100 m is composed of calcarenite, calcirudite, and calcilutite, which are represented by interbedded packstone, wackestone, and mudstone.  The middle part (120 m) is much coarser-grained and consists of thin to very thick-bedded calcarenite and calcirudite (mostly packstone and wackestone with some grainstone).  The uppermost 110 m is mainly cross-bedded sandy limestone and calcareous sandstone.  See Withnall & others (1988, figure 28 and pages 69-70) for more details.|16-MAY-23
23555|Dosey Limestone|Extent|.  Intricately folded with other units in the Broken River Group, from 7859-634461 to the headwaters of Dosey Creek and Spanner Hill at 7858-520360.  The grid references are based on the AGD66 datum.|16-MAY-23
23555|Dosey Limestone|Thickness range|Up to 250 m.|16-MAY-23
23555|Dosey Limestone|Lithology|Mainly bioclastic limestone (calcirudite, calcarenite, and  calcilutite, represented by packstone and wackestone with lesser grainstone, mudstone, and boundstone).  Lesser sandy limestone and calcareous sandstone, locally with pebbles and cobbles of limestone.|16-MAY-23
23555|Dosey Limestone|Fossils|The limestone contains a rich fauna of stromatoporoids dominated by Amphipora and lesser lamellar and hemispherical types.  Corals, crinoid ossicles, brachiopods, and minor gastropods, ostracods, conodonts, algae, and fish remains also occur.  The Sanidophyllum fauna of the Chinaman Creek Limestone (Wyatt & Jell, 1967) is present.|16-MAY-23
23555|Dosey Limestone|Relationships and boundaries|The Dosey Limestone is part of the Wando Vale Subgroup of the Broken River Group.  It conformably overlies the Storm Hill Sandstone, and where the latter is absent it lies directly on the Lomandra Limestone.  The presence of Amphipora packstones distinguishes it from the Lomandra Limestone.  Along the Broken River, it passes laterally  into and partly overlies the Burges Formation.  It is overlain by the Papilio Mudstone.|16-MAY-23
23555|Dosey Limestone|Age reasons|Conodont studies indicate an Eifelian to early Givetian age (Mawson & Talent, in press).|16-MAY-23
23555|Dosey Limestone|References|MAWSON, R., & TALENT, J.A., in press:  Late Emsian-Givetian 	stratigraphy and conodont biofacies - carbonate slope and offshore shoal to sheltered lagoon and nearshore carbonate ramp - Broken River, north Queensland.  Courier Forschungs-Institute Senckenburg.WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of 	Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes.WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River 	area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.WYATT, D.H. & JELL, J.S., 1967:  Devonian of the Townsville 	hinterland, Queensland, Australia; in Oswald, D.H. (editor), International Symposium on the Devonian System, Volume 2.  Alberta Society of Petroleum Geologists, Calgary, 99-105.|16-MAY-23
24253|Double Crossing Metamorphics|Name source|Double Crossing Bore, GR 305056, Mount Merlin 1:100 000 Sheet area.|16-MAY-23
24253|Double Crossing Metamorphics|Unit history|None; included within Williams Granite by Carter & Opik (1963).|16-MAY-23
24253|Double Crossing Metamorphics|Type section locality|From a point 1.3 km E of the Answer Mine east for 2.5 km to GR 377032, Mount Merlin 1:100 000 Sheet area, Duchess 1:250 000 Sheet area. This section traverses undulating terrain formed of Double Crossing Metamorphics from a concordant, possibly faulted, contact with phyllite and fine-schist of the Answer Slate to the W to a similar contact with fine-grained mica schist and schistose meta-arenite of the Staveley Formation to the E. Medium to coarse schist, gneiss, migmatite, feldspathic quartzite, amphibolite and abundant concordant to cross-cutting granite veins are exposed in the type section.|16-MAY-23
24253|Double Crossing Metamorphics|Thickness range|Unknown, because of tight folding and because no stratigraphic sequences have been determined within unit, but probably at least 1000 m.|16-MAY-23
24253|Double Crossing Metamorphics|Lithology|Rock types present are micaceous and felsic gneiss and schist, migmatitic gneiss with leucosome 'sweats', amphibolite, quartzite, banded quartz-hematite and quartz-tourmaline rocks, meta-arkose, and many concordant to cross-cutting veins and veinlets of pegmatite, leucogranite, and quartz.|16-MAY-23
24253|Double Crossing Metamorphics|Relationships and boundaries|Intruded by and intemately associated with Gin Creek Granite; its relationships to adjacent Answer Slate and Stavely Formation are uncertain - it may be exposed in the core of an anticline, in which case it is probably partly overlain unconformably by, and partly faulted against, these two formations.|16-MAY-23
24253|Double Crossing Metamorphics|Age reasons|Proterozoic; the unit may be part of the Early Proterozoic basement of the Mount Isa Inlier.|16-MAY-23
24253|Double Crossing Metamorphics|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
24253|Double Crossing Metamorphics|Comments|Remarks: The Double Crossing Metamorphics are of higher metamorphic grade than adjacent formations, and are different in composition, being predominantly quartzofeldspathic, rather than pelitic. Hence they form a distinctive mappable unit.|16-MAY-23
24253|Double Crossing Metamorphics|Defn Reference|82/22920|16-MAY-23
21699|Duck Granodiorite|Name source|Duck Creek a tributary of Balfe Creek which it joins at GR 3880 77551 in the Homestead 1:100 000 Sheet area. The grid reference is based on the AGD66 datum.|16-MAY-23
21699|Duck Granodiorite|Unit history|The Duck Granodiorite was not recognised by previous workers being mapped as Tertiary laterite by Wyatt & others (1971), Clarke & Paine (1970).|16-MAY-23
21699|Duck Granodiorite|Type section locality|A knoll at GR 3908 77523, beside the track south of Duck Creek yards on Powlathanga homestead in the Homestead 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
21699|Duck Granodiorite|Description at type locality|Here a grey, medium grained biotite granodiorite to granite crops out. The rock comprises quartz, subhedral plagioclase, unevenly distributed poikilitic K-feldspar, biotite with minor opaques and muscovite. A pink to cream, less mafic variety at the type locality has similar mineralogy but less biotite.|16-MAY-23
21699|Duck Granodiorite|Lithology|The rock type at the type locality occurs throughout the outcrop area. However the presence or absence of large, unevenly distributed K-feldspar grains gives rise to a variety of compositions from tonalite to granite.|16-MAY-23
21699|Duck Granodiorite|Relationships and boundaries|The Duck Granodiorite intrudes migmatites and gneisses of probable Ordovician age. Its relationship to other adjacent units is masked by younger sediments.|16-MAY-23
21699|Duck Granodiorite|Age reasons|The age of the Duck Granodiorite is not known precisely. An age of Late Silurian to Early Devonian is assigned on the basis of lithological similarity to other units of this age in the Ravenswood Batholith (Hutton & others, 1994).|16-MAY-23
21699|Duck Granodiorite|Comments|MAGNETIC SUSCEPTIBILITY::  Magnetic susceptibilities at the type locality are 278-425 x 10[superscript]-5 SI units for the more mafic variety and 65-137 x 10[superscript]-5 SI units for the less mafic variety. Throughout the outcrop area magnetic susceptibilities are 152-817 (averaging 362) x 10[superscript]-5 SI units.|16-MAY-23
21699|Duck Granodiorite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
5776|Dugald River Shale Member|Name source|The Dugald River Shale Member is named after the Dugald River lead-zinc prospect which occurs in the unit. The prospect lies 19 km northwest of Quamby and 2.5 km west of Dugald River, in the Quamby 1:100 000 Sheet area.|16-MAY-23
5776|Dugald River Shale Member|Unit history|The Dugald River Shale Member has been previously mapped as part of the Corella Formation (Carter & others, 1961; Wilson & others, 1979b). Whitcher (1975) referred to it as the Dugald River Shale and Connor & others (1982) termed it the Dugald Slates.|16-MAY-23
5776|Dugald River Shale Member|Geomorphic expression|The Dugald River Shale Member forms a persistent rounded strike ridge which rises a few tens of metres above the surrounding calc-silicate rocks and dolomitic limestone.The gossanous zones are characterised by a total absence of eucalypt trees and spinifex but are covered with a poor growth of 'copper grass' Tephrosia (Cole, 1980).|16-MAY-23
5776|Dugald River Shale Member|Type section locality|The type section is defined in the vicinity of the Dugald River lead-zinc prospect, in a small east-flowing tributary of Dugald River from latitude 20o15'24"S, longitude 140o9'23"E (GR 119598) to latitude 20o15'24"S, longitude 140o9'10"E (GR 115598). The exposed sequence in the type section of the Dugald River Shale Member is, from east to west: approximately 25 m of black laminated shale, a gossanous sequence approximately 20 m thick, 140 m of blacl laminated shale containing minor zones of gossanous shale and slate, and 70 m of spotted schist.|16-MAY-23
5776|Dugald River Shale Member|Extent|The unit is exposed in two areas. The main area is a narrow north-trending belt near the middle of the Quamby 1:100 000 Sheet area, centred approximately on the Dugald River lead-zinc prospect, and the other area is a small outcrop west of the Lady Clayre mine approximately 4 km southwest of the main area. The total area of outcrop is 2 km2.|16-MAY-23
5776|Dugald River Shale Member|Thickness range|At the surface the thickness of the unit ranges from about 60 m in the north to about 500 m in the south. At depth the unit htins to about 35 m (Connor & others, 1982).|16-MAY-23
5776|Dugald River Shale Member|Lithology|In addition to the rock types noted in the type section, grey to black pyritic/pyrrhotitic shale, cordierite (?), and andalusite(?), spotted schist, and calcareous siltstone occur and are more common in the south of the main area of exposure. The area near the Lady Clayre mine consists of grey spotted schist, pyritic shale, and andalusite(?) slate. Thin highly potassic tyff or fine-grained volcaniclastic beds and siltstone containing casts or pseudomorphs of the evaporite minerals shortite and gypsum have been reported in the Dugald River Shale Member by Connor & others (1982). The mineralised horizons contain pyrrhotite, pyrite, sphalerite, and galena in graphitic slate and a quartz-carbonate gangue (Connor & others, 1982). At depth the shale is mostly graphitic. Primary sedimentary structures and soft-sediment deformation structures are particularly evident in drill core.|16-MAY-23
5776|Dugald River Shale Member|Relationships and boundaries|The Dugald River Shale lMember overlies a dolomitic limestone (the footwall limestone) which is in the upper most third of the Corella Formation. The basal contact is a transition over less than 1 m from grey to green laminated or brecciated calc-silicate rocks to dark grey to black (carbonaceous) shale, and is taken as the top of the highest band of calc-silicate rocks. In places, the member is faulted against older calc-silicate rocks of the Corella Formation. The member is overlain, apparently conformably, by a poorly exposed sequence of calc-silicate rocks, siltstone, shale, and schist which is regarded as the uppermost part of the Corella Formation in this area. This sequence is disconformably overlain by the Knapdale Quartzite (Connor & others, 1982).|16-MAY-23
5776|Dugald River Shale Member|Structure and Metamorphism|The Dugald River Shale Member in the main outcrop area dips west at 50o to 80o and predominantly youngs to the west, although isoclinal folding and a large-scale fold axis have been recognised in the south of this area. The sequence in the Lady Clayre mine area is tightly to isoclinally folded. Metamorphic grade is probably of low to middle greenschist facies. Cordierite(?) and andalusite(?) were reported by Whitcher (1975), but the recent identification of evaporite minerals introduces some doubt as to the existence of these metamorphic minerals (Connor & others, 1982).|16-MAY-23
5776|Dugald River Shale Member|Age reasons|The Dugald River Shale Member is regarded as part of the upper Corella Formation, which overlies the 1760 Ma Argylla Formation and is intruded by the 1740 Ma Burstall Granite (Page, 1981).|16-MAY-23
5776|Dugald River Shale Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
5776|Dugald River Shale Member|Comments|Discussion: The Dugald River Shale Member is regarded as a lacustrine deposit in a non-marine restricted clastic sedimentary basin (Connor & others, 1982). Minor volcanic input is evidenced by the tuffaceous beds. The enclosed ore bodies are typical stratiform black shale hosted lead-zinc deposits. The reserves are 60 Mt of ore containing 10 percent zinc, 1 percent lead, and 30 g/t silver, extending to a depth of 1000 m (Connor & others, 1982). Whitcher (1975) correlated the Dugald River Shale Member with the Mount Isa Group but more recent geochronological data (Page, 1981) indicated it is probably older.|16-MAY-23
5886|Dynamite Creek Member|Name source|Dynamite Creek, a tributary of Gunpowder Creek, in the south of MYALLY (1:100 000 Sheet areas indicated by capitals).|16-MAY-23
5886|Dynamite Creek Member|Unit history|The Dynamite Creek Member was not distinguished from the Eastern Creek Volcanics by Carter & others (1961) and was hown as an unnamed member (Pheq) of the volcanics on the Alsace 1:100 000 Geological Series preliminary map.|16-MAY-23
5886|Dynamite Creek Member|Geomorphic expression|The unit commonly occurs as cuestas with the gentler western dip slope contrasting with the steep eastern slope.|16-MAY-23
5886|Dynamite Creek Member|Type section locality|The holostratotype of the Dynamite Creek Member is defined as a section about 800 m long at the base of a low ridge in the north bank of Dynamite Creek in MYALLY from 6859-585458 (base) to 6859579456 (top). The section, approximately 9 km south of Alsace Camp on Gunpowder Creek, comprises approximately 100 m of conglomerate overlain by 50 m of feldspathic and labile sandstone. The conglomerate contains rounded clasts of granite and acid volcanics up to 60 cm in diameter, and some smaller clasts of quartzite and vein quartz. The conglomerate fines upward.|16-MAY-23
5886|Dynamite Creek Member|Extent|A discontinuous north-trending linear belt extending for 25 km from 5 km south of Mistake Creek in ALSACE to 5 km north of Dynamite Creek in MYALLY. The areas of outcrop in each of these sheet areas total 5 km2 and 6 km2, respectively.|16-MAY-23
5886|Dynamite Creek Member|Thickness range|The Dynamite Creek Member is thickest in the south, where it is at least 200 m thick and may be as thick as 350 m (Derrick & Wilson, 1982). North of the type section (where it is 150 m thick) it thins rapidly and is only about 1 m thick in the most northerly outcrops.|16-MAY-23
5886|Dynamite Creek Member|Lithology|Conglomerate is best developed within 2 km of the type section, but pebbly conglomerate containing acid volcanic and quartzite clasts occurs at the base and as thin lenses within the member in most sequences. Labile sandstone containing acid volcanic and shale fragments and feldspathic sandstone are the other main rock types; minor siltstone is interbedded with sandstone. In the north, the member contains a basal pinkish brown medium-grained pebbly feldspathic sandstone with siltstone interbeds, overlain by brown laminated fine-grained labile sandstone and buff slightly feldspathic sandstone.|16-MAY-23
5886|Dynamite Creek Member|Relationships and boundaries|The Dynamite Creek Member overlies the Ewen Granite unconformably and is overlain conformably by metabasalt flows of the Cromwell Metabasalt Member of the Eastern Creek Volcanics (Wilson & Grimes, in press). The basal unconformity is clearly evident at 6859-588498, 4 km north of the type section. The first appearance of sedimentary rocks above the Ewen Granite defines the base of the Dynamite Creek Member. The upper boundary is defined by the base of the first basaltic lava flow in the overlying member. The unit is intruded by dolerite dykes.|16-MAY-23
5886|Dynamite Creek Member|Structure and Metamorphism|The Dynamite Creek Member is a shallow west-dipping unit which is locally faulted. Metamorphic effects are not evident in the sedimentary rocks, but the overlying metabasalt contains low greenschist facies mineral assemblages.|16-MAY-23
5886|Dynamite Creek Member|Age reasons|The Dynamite Creek Member is younger than the Ewen Granite which has been dated by U-Pb zircon techniques as 1840+/-50 Ma (Page & others, 1982). The unit must also be younger than the Bottletree Formation (Blake & others, 1981) which unconformably underlies the Eastern Creek Volcanics to the south of Mount Isa and has yielded U-Pb zircon dates of 1790+/-9 and 1808+/-20 Ma (Page & others, 1982). Minimum ages for the Dynamite Creek Member are provided by U-Pb zircon dates on the Sybella Granite which intrudes the Eastern Creek Volcanics (1670 to 1710? Ma; Page & others, 1982), and on the Carters Bore Rhyolite (1678+/-1 Ma; Page, 1978) which occurs at a higher stratigraphic level than the Eastern Creek Volcanics to the west of Mount Isa. A minimum age of 1740 Ma can be inferred from the Burstall Ganite (Page, 1981) which intrudes the Corella Formation, a correlative of the Qulalar Formation (Derrick & others, 1980) which overlies the Eastern Creek Volcanics. From these data, the Dynamite Creek Member is probably between approximately 1800 Ma and 1740 Ma old.|16-MAY-23
5886|Dynamite Creek Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
5886|Dynamite Creek Member|Comments|Discussion: Some of the rocks mapped as Lena Quartzite Member of the Eastern Creek Volcanics in the southern half of ALSACE probably correlate with the Dynamite Creek Member. The Dynamite Creek Member is in a similar stratigraphic position to the Mount Guide and Leander Quartzites (Derrick & others, 1976) which underlie the Cromwell Metabasalt Member conformably to the southeast and north-northwest of Mount Isa. The Dynamite Creek Member probably formed in a fluvial environment along the western edge of the elevated Ewen Block during the infilling of the Mount Isa fault trough (Glikson and others, 1976; Derrick, 1982, fig. 4).|16-MAY-23
5887|Dyraaba Member|Name source|Parish of Dyraaba, County of Lyndhurst (Clarke River 1:250 000 Cadastral map).|16-MAY-23
5887|Dyraaba Member|Unit history|Previously mapped as part of the Bundock Creek Formation (now Group) by White (1959, 1962, 1965) and 'upper' Bundock Creek Formation by Wyatt & Jell (1980).  The name was first published and described by Withnall & others (1988), but not formally defined.|16-MAY-23
5887|Dyraaba Member|Geomorphic expression|Low hilly topography which is strongly dissected and gullied.  It is covered by low scrub, eucalypts, and is well grassed in places.|16-MAY-23
5887|Dyraaba Member|Type section locality|In a tributary of Mount Brown Creek between 7859 499462 (base) and 497466 (top).   The grid reference is based on the AGD66 datum.|16-MAY-23
5887|Dyraaba Member|Description at type locality|It is 385 m thick, and consists of fine to medium-grained, micaceous, feldspathic to lithofeldspathic, muddy sandstone, siltstone, and mudstone.  The base of the member is placed at the bottom of a medium to thick-bedded, medium to very coarse-grained, calcareous, micaceous sandstone which overlies a thick mudstone unit in the Teddy Mount Formation.  Numerous fossil logs and stems litter the surface above the boundary.  The upper half of the unit is generally finer grained, but it coarsens again towards the top.|16-MAY-23
5887|Dyraaba Member|Extent|As presently mapped, it is confined to the Boroston Syncline in the headwaters of Mount Brown Creek and its tributaries, but similar lithologies have been noted elsewhere in the Teddy Mount Formation.|16-MAY-23
5887|Dyraaba Member|Thickness range|385 m in the type section, but the thickness elsewhere is difficult to determine because of folding|16-MAY-23
5887|Dyraaba Member|Fossils|Abundant lepidodendroid and calamitean plant remains occur throughout the unit, and suggest a Late Devonian or Early Carboniferous age.  Rare disarticulated brachiopods also occur, but are not diagnostic.|16-MAY-23
5887|Dyraaba Member|Relationships and boundaries|Forms the upper part of the Teddy Mount Formation, and is distinguished by being more sandy, and containing abundant plant remains.  It is conformably overlain by the Boroston Formation, and is distinguished from it by the lack of quartz-rich sandstone and the presence of abundant plant remains.  It is intruded by the Carboniferous or ?Permian Montgomery Range Igneous Complex.|16-MAY-23
5887|Dyraaba Member|Age reasons|The lepidendroid and calamitean plant remains throughout the unit, suggest a Late Devonian or Early Carboniferous age.  The unit is possibly early Tournaisian, in view of the conodont ages lower in the Teddy Mount Formation.|16-MAY-23
5887|Dyraaba Member|References|WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. **WHITE, D.A., 1962:  Clarke River - Qld E/55-13.  Bureau of Mineral Resources, Australia 1:250 000 Geological Series Explanatory Notes.  **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.D., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
27145|Edie Tuff Member|Name source|Edie county, the county in which QDM Hexham 1 was drilled. The co-ordinates of the well are: Latitude 22o48'22"S; Longitude 145o57'08"E.|16-MAY-23
27145|Edie Tuff Member|Type section locality|In ENL Lake Galilee 1, from 1346 m (4416 ft) to 1478 m (4849 ft (K.B. The co-ordinates of the well are: Latitude 22o11'30"S; Longitude 145o58'32"E. Cuttings and a core of this interval are available at the Core Library, Redbank.|16-MAY-23
27145|Edie Tuff Member|Extent|Present in the majority of wells in the northeastern Galilee Basin; cannot be recognised in AAO Beryl 1, MPC Corfield 1 and AAE Towerhill 1. Absent in AOD Jericho 1 because of erosion.|16-MAY-23
27145|Edie Tuff Member|Thickness range|132 m in the type section; maintains a fairly uniform thickness of between 110 and 120 m. Thins to 94 m in PON Muttaburra 1 Well.|16-MAY-23
27145|Edie Tuff Member|Depositional environment|Calm water, lacustrine environment with contemporaneous vulcanism.|16-MAY-23
27145|Edie Tuff Member|Relationships and boundaries|The Edie Tuff Member is a member within the Jochmus Formation.|16-MAY-23
27145|Edie Tuff Member|Age reasons|Early Permian. Spore assemblages obained have been assigned to Stages 2 and 3 Evans (1969).|16-MAY-23
23575|Eland Metavolcanics|Lithology|Chlorite and actinolite schist (meta-andesite to dacite) with common relict plagioclase phenocrysts or clast, volcaniclastic meta-arenite and meta-rudite muscovite schist, phyllite and minor marble; locally mylonitic with strongly stretched clasts; metachert|16-MAY-23
79124|Eldorado Clastics Member|Name source|From Eldorado Road near Monkland Mine, Gympie.|16-MAY-23
79124|Eldorado Clastics Member|Unit history|This unit was first used informally as Lower Nash Clastics by Gympie Eldorado Gold Mines at Monkland Mine and subsequently referred to by Cranfield (1999), Sivell & Arnold (1999), Sivell & McCulloch (2001), Li & others (2015)  . Equivalent to Dunstan's (1911) Second Slate Group (2S).|16-MAY-23
79124|Eldorado Clastics Member|Type section locality|BHP Drill Hole G023, depth 188-227m from the north end of Monkland Mine (collar 468180mE; 7100900mN; Lat: -26°12'40"  Long: 152°40'53" ) held in Zillmere storage facility, Brisbane. Reference drill holes: GEGM drill hole G135: 168 -196 m near the Aurelia shoot, Monkland Mine GEGM drill hole G137: 507- 538 m at Monkland Mine. Core also stored at Zillmere. No outcrops have been identified.|16-MAY-23
79124|Eldorado Clastics Member|Extent|Drilling shows the unit occurs throughout the Monkland, Six Mile and Dawn blocks, and at Partridge and Wylly prospects.|16-MAY-23
79124|Eldorado Clastics Member|Thickness range|5 to 20 m at Monkland, 8-15 m at Partridge and Inglewood Horst.|16-MAY-23
79124|Eldorado Clastics Member|Lithology|At Monkland Block mostly consists of medium grained, volcaniclastic sandstone, derived largely from the underlying Mary Basalt but also with some apparent andesitic input.  It is weakly bedded to massive, part unsorted, part reworked into alternating finer and coarser layers. Grain size is usually 0.3mm to 5mm with minor pebble beds. Coarse conglomeratic beds with clasts to 100mm, some resembling pyroclasts, occur at the base of the unit. Grains and clasts are commonly hematised, more so than the Nash Clastics above the Calton Andesite.  They are derived from oxidized flow top basalt, felted, micritic, aphanitic and vesicular basalt, and phenocrysts.  Most are altered to sericite-chlorite-hematite. Larger clasts include porphyritic basalt with plagioclase, pyroxene and possibly rare altered olivine phenocrysts.  Magnetite grains are locally concentrated in poorly defined beds.|16-MAY-23
79124|Eldorado Clastics Member|Relationships and boundaries|Conformably overlies Mary Basalt and overlain by Calton Andesite.|16-MAY-23
79124|Eldorado Clastics Member|Alteration and Mineralisation|Altered to sericite-chlorite-hematite.|16-MAY-23
79124|Eldorado Clastics Member|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie, 12-JAN-2017.|16-MAY-23
79124|Eldorado Clastics Member|References|Dunstan, B., 1911: Geology map of Gympie and environs. GSQ Publ. No. 221b.  **Cranfield, L.C., 1999: Gympie Special Sheet 9445, Part 9545, Queensland 1:100,000 Geological Map Commentary. Queensland Department of Mines and Energy, Brisbane.  **Sivell, W.J. and Arnold, G.O. 1999: Geochemical and volcanic stratigraphy of a segment of an island arc - Gondwana rim accretion zone, Gympie Province, southeast Queensland.  IN Flood, P.G. (Editor): Regional Geology, Tectonics and Metallogenesis, New England Orogen, NEO '99 Conference, 255-266.  **Sivell, W.J. and McCulloch, M.T. 2001: Geochemical and Nd-isotopic systematics of the Permo-Triassic Gympie Group, southeast Queensland.  Australian Journal of Earth Sciences 48, 377-394.  **Li, P., Rosenbaum, G., Yang, J-H. and Hoy, D. 2015. Australian-derived detrital zircons in the Permian-Triassic Gympie terrane (eastern Australia): Evidence for an autochthonous origin. Tectonics, 34, 858-874.|16-MAY-23
24263|Eleven-B Granite|Name source|11B' Pinnacles at GR 089172 (Einasleigh 1:100 000 Sheet area). The name is spelt out to avoid confusion in typescript.|16-MAY-23
24263|Eleven-B Granite|Unit history|Previously mapped as Forsayth Granite (White, 1962).|16-MAY-23
24263|Eleven-B Granite|Type section locality|An unnamed creek from GR 091217 (Einasleigh 1:100 000 Sheet area) upstream to GR 098232. The creek forms a valley between two mesas of basalt; pink, medium-grained, equigranular, muscovite-biotite granite is exposed.|16-MAY-23
24263|Eleven-B Granite|Extent|The main body is a roughly oval-shaped pluton about 30 km2 in area extending for about 15 km southwest from Carpentaria Downs Homestead. Other smaller plutons which are similar to and may be related to the main body total about 20 km2 in area. They are located about 15 km south-southeast of Einasleigh, 4 km north and 8 km northwest of Carpentaria Downs homestead, and on the northwestern side of Mount Tabletop.|16-MAY-23
24263|Eleven-B Granite|Lithology|Pinkish-grey medium-grained equigranular to slightly porphyritic ;muscovite-biotite granite. Locally there are more muscovite-rich outcrops. Pegmatite veins are common.|16-MAY-23
24263|Eleven-B Granite|Relationships and boundaries|The granite intrudes the Proterozoic Einasleigh Metamorphics. It is in contact with the Oak River Granodiorite, but no contact relationship has been observed. It is overlain by Tertiary Basalt.|16-MAY-23
24263|Eleven-B Granite|Age reasons|The granite is locally strongly foliated and is probably Middle Proterozoic in age.|16-MAY-23
24263|Eleven-B Granite|Proposer|Warnick J.V.|16-MAY-23
35080|Elimeek Volcanics|Name source|Elimeek homestead at GR 3285 77253.  The grid reference os based on the AGD66 datum.|16-MAY-23
35080|Elimeek Volcanics|Unit history|Paine & others (1965) mapped the unit as unnamed Upper Permian Volcanics (Puv) and reported that the pyroclastics and volcanics in this area may be related to the Permian Mundic Complex.|16-MAY-23
35080|Elimeek Volcanics|Type section locality|Adjacent to Betts Creek (GR 3255 77253) where flow banded rhyolite lava forms sparsely vegetated ridges.  The grid reference is based on the AGD66 datum.|16-MAY-23
35080|Elimeek Volcanics|Description at type locality|These lavas are commonly spherulitic with feldspar phenocrysts in a fine cryptocrystalline groundmass. Ignimbrite sheets crop out to the north of this locality and discontinuously throughout the unit.|16-MAY-23
35080|Elimeek Volcanics|Extent|The Elimeek Volcanics crop out intermittently over 6km2 in the northeastern quadrant of the Pentland 1:100 000 Sheet area (Figure 2). The eastern margin is approximately 2km southwest of Elimeek homestead with the western margin forming a hill south of Golden Mount.|16-MAY-23
35080|Elimeek Volcanics|Lithology|This unit consists of pale brown, commonly spherulitic and flow-banded rhyolite lava and minor ignimbrite. A hill south of Golden Mount around GR 3204 77265 is formed from a volcanic breccia complex (Morrison, 1993). Within the breccia complex both matrix and clast-supported pyritic breccia with dacite and microtonalite intrusions are present. Breccia clasts are dominantly volcanic material but some quartzite and schist fragments from the Cape River Metamorphics are present. Tuffs, tuffaceous sediments and ignimbrite occur locally. This breccia complex is interpreted as a vent breccia and may be the source for the lavas further to the east. Columnar jointing is developed in some lava flows south of Betts Creek.  The grid reference is based on the AGD66 datum.|16-MAY-23
35080|Elimeek Volcanics|Relationships and boundaries|The Elimeek Volcanics overlie the Cape River Metamorphics. They are overlain by conglomerate and sandstone of the Late Permian Betts Creek Beds (Galilee Basin) in a railway cutting at GR 3272 77235. Vine & Paine (1974) consider that these volcanics may be a 'facies equivalent of the Betts Creek Beds that were deposited nearer to a volcanic centre'.  The grid reference is based on the AGD66 datum.|16-MAY-23
35080|Elimeek Volcanics|Age reasons|The age of the Elimeek Volcanics is not known precisely. A Carboniferous or Permian age has been assigned to the Elimeek Volcanics, because of similarities to other volcanics of this age in the Townsville hinterland.|16-MAY-23
35080|Elimeek Volcanics|Comments|Magnetic Susceptibility:Magnetic susceptibility for the lava is 120-484 x 10-5 SI units. Ignimbrite gives a weaker response with values of 14-20 x 10[superscript]-5 SI units. Intrusive rocks within the breccia complex are considerably more magnetic with readings of 1003-4069 x 10-5 SI units. Alteration of these rocks appears to have produced a lower magnetic response.|16-MAY-23
35080|Elimeek Volcanics|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
84108|Elizabeth Formation|Name source|Name derived from Elizabeth Creek, in the northwest LAWN HILL 1:250 000 mapsheet, Queensland.|
84108|Elizabeth Formation|Unit history|Unit mapped as undifferentiated Constance Sandstone in First Edition 1:250 000 MOUNT DRUMMOND mapsheet (Smith and Roberts, 1963a, b). Unit subsequently remapped as an unnamed member of the Constance Sandstone (Psa4) on BOWTHORN 1:100 000 mapsheet by Slater and Mond (1980), and on the HEDLEYS CREEK 1:100 000 mapsheet by Sweet (1981) and Sweet et al (1981). Unit elevated to formation status and termed “Elizabeth Sandstone” by Sweet (2017).|
84108|Elizabeth Formation|Geomorphic expression|The formation forms the distinct outcrop ridge of the Bluff Range on the eastern MOUNT DRUMMOND 1:250 000 mapsheet. Extensive exposures of the formation occur in gorges on the LAWN HILL 1:250 000 mapsheet in Queensland.|
84108|Elizabeth Formation|Type section locality|Type area located in the northern Constance Range, approximately 20 km south-southeast of Bowthorn Homestead, at approximately 18°16’56”S 138°23’44”E (54K 224652mE 7976626mN; Sweet, 2017). Originally designated as ‘type section’, but base and top not defined by Sweet (2017).|
84108|Elizabeth Formation|Extent|Formation is present across the western LAWN HILL 1:250 000 mapsheet, Queensland and the eastern MOUNT DRUMMOND 1:250 000 mapsheet, Northern Territory (Sweet, 2017).|
84108|Elizabeth Formation|Thickness range|The formation is approximately 167 m thick in the type section, and reaches approximately 200 m thick elsewhere on the BOWTHORN 1:100 000 mapsheet (Sweet, 2017).|
84108|Elizabeth Formation|Lithology|The formation consists of thick-bedded, large-scale trough cross-bedded, coarse- to very coarse and granule-rich sandstone. The upper part of the formation is marginally more fine-grained and better sorted, with medium-scale trough cross-beds (15–20 cm sets), some displaying possible herringbone patterns, and extensive flat bedding planes separating cosets (Sweet, 2017).|
84108|Elizabeth Formation|Depositional environment|The formation consists, primarily, of shallow-marine, mainly upper shoreface deposits. Some deposits may reflect slightly deeper-water conditions, likely within the middle to upper shoreface (Sweet, 2017).|
84108|Elizabeth Formation|Relationships and boundaries|In the type section, the Elizabeth Formation unconformably overlies the Bowthorn Member of the Constance Sandstone, with evidence of an erosive surface. Elsewhere on the BOWTHORN 1:100 000 mapsheet there is evidence of angular discordance and a thin regolith interval between the Bowthorn Member and the overlying Elizabeth Formation. The upper contact of the Elizabeth Sandstone with the overlying Mullera Formation is sharp but apparently conformable in all areas of outcrop (Sweet, 2017).|05-OCT-23
84108|Elizabeth Formation|Identifying features|The predominantly coarse-grained, quartzose Elizabeth Formation is stratigraphically underlain and overlain by much more fine-grained and recessive units (Bowthorn Member of the Constance Sandstone below and Mullera Formation above), making its outcrop pattern more prominent.|
84108|Elizabeth Formation|Age reasons|Maximum depositional ages derived from U-Pb SHRIMP dating of detrital zircons: Bukalara Sandstone (stratigraphically overlies Elizabeth Formation): GA sample 2777481 – 1316 ± 27 Ma (Kositcin et al, 2020). Mittiebah Sandstone (stratigraphically underlies Elizabeth Formation): GA sample 2676116 – 1586 ± 7 Ma (Anderson et al., 2019). Therefore, the potential depositional age range for the Elizabeth Formation can be considered to extend from ca. 1586 ± 7 Ma to 1316 ± 27 Ma.|
84108|Elizabeth Formation|Correlations|No precise correlations at the formation level are known. Given the potential depositional age range of ca. 1586 ± 7 Ma to 1316 ± 27 Ma, the Elizabeth Formation may be correlative with components of the Favenc and/or the Wilton packages (Rawlings, 1999) of the McArthur Basin.|
84108|Elizabeth Formation|Geophysical Expression|Weak magnetic response.|
84108|Elizabeth Formation|Defn author|Elliot Foley, Jack Simmons, Ben Williams, Charles Verdel (Northern Territory Geological Survey), Chris Carson (Geoscience Australia) 31-MAY-2023.|
84108|Elizabeth Formation|Comments|Note: All locations are based on the GDA94 geodetic datum. Standard series 1: 100 000 and 1: 250 000 mapsheet names are shown in uppercase.|
84108|Elizabeth Formation|References|Anderson JR, Lewis CJ, Jarrett AJM, Carr LK, Henson P, Carson CJ, Southby C and Munson TJ, 2019. New SHRIMP U–Pb zircon ages from the South Nicholson Basin, Mount Isa Province and Georgina Basin, Northern Territory and Queensland. Geoscience Australia, Record 2019/10. 
 **Carson, C. J., Kositcin, N., Anderson, J. R., and Henson, P. A. in prep. A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia - insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences. 
 **Kositcin N, Carson CJ, Anderson JR, Doublier MP and Murr J, 2020. Exploring for the Future - New SHRIMP geochronology constraints on the basin evolution of the South Nicholson region. Geoscience Australia, Record 2020/25.  **Rawlings DJ, 1999. Stratigraphic resolution of a multiphase intracratonic basin system: the McArthur Basin, northern Australia. Australian Journal of Earth Sciences 46(5), 703-723. 
 **Simmons JM, Williams B, Carson, C and Verdel C, 2023a. Mount Drummond, Northern Territory 1:250 000 Geological Map, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.  **Simmons JM, Williams B, Carson, C and Verdel C, 2023b. Mount Drummond, Northern Territory 1:250 000 Geological Map Explanatory Notes, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.  **Slater PJ and Mond A, 1980. Constance Range region, Queensland (Preliminary Edition). 1:100 000 geological map series, portion of 6560, 6561. Bureau of Mineral Resources, Canberra.  **Smith JW and Roberts HG, 1963a. Mount Drummond, NT (First Edition). 1:250 000 Geological Map Series Explanatory Notes, Sheet 53-12. Bureau of Mineral Resources, Canberra.  **Smith JW and Roberts HG, 1963b. Mount Drummond, NT (First Edition). 1:250 000 Geological Map Series, Sheet SE 53-12. Bureau of Mineral Resources, Canberra.  **Sweet IP, 1981. Definitions of new stratigraphic units in the Seigal and Hedleys Creek 1:100 000 sheet areas, Northern Territory and Queensland. Bureau of Mineral Resources, Geology and Geophysics, Report 225.  **Sweet IP, 2017. The geology of the South Nicholson Group, northwest Queensland. Queensland Geological Record 2017/07.  **Sweet IP, Mitchell JE and Mock CM, 1981. Seigal, Northern Territory and Hedleys Creek, Queensland. 1:100 000 Geological Map Commentary. Bureau of Mineral Resources, Geology and Geophysics, Canberra.|
38893|Ellrott Rhyolite|Name source|The name was introduced by Taube (1979) - origin is not specified unfortunately (per email I. Withnall 5 Sep'08).|16-MAY-23
38893|Ellrott Rhyolite|Geomorphic expression|The rhyolite to dacite domes form topographic highs because of their resistant nature relative to the surrounding country rock, and are probably responsible for the elevated country from Mount Belmont to Mount Kilner.|16-MAY-23
38893|Ellrott Rhyolite|Type section locality|Cabbage Tree Hill is the type area. It represents a massive, dark grey, porphyritic rhyolite-dacite with visible feldspar and quartz. Mafic xenoliths are also present.|16-MAY-23
38893|Ellrott Rhyolite|Extent|The volcanic domes have been mapped from Mount Belmont south to an area 10 km north of Mount Larcom. Large outcrops of rhyolite to dacite have been mapped at Mount Belmont, the Mount Archer-Cabbage Tree Hill-Nankin area, and also between Mount MacDonald and Mount Kilner. There is also a large body of rhyolite between Mount Chalmers and Mount MacDonald.|16-MAY-23
38893|Ellrott Rhyolite|General description|The term Ellrott Rhyolites was previously defined by Taube (1979). It comprises rhyolite and dacite volcanic domes, some of which may be extrusive. These are widespread within the Berserker Group, scattered throughout the Rockhampton and Mount Larcom regions and up to several square kilometres in area. The rocks are typically dark grey, massive, and porphyritic in feldspar. Visible quartz is rare.|16-MAY-23
38893|Ellrott Rhyolite|Lithology|The domes range from rhyolite to dacite in composition although some of the rocks with pyroxene may be andesitic. They are either massive or flow-banded, and display porphyritic texture, although aphyric rocks are found locally (Figure 14). Some of the flow-banded rocks are also autobrecciated. Amygdales filled with silica or calcite are common, as are ferromagnesian clots. Xenoliths are not common and seem to be abundant only in the Cabbage Tree Hill area. They are up to 20 cm in size and are massive or trachytic, porphyritic andesite.The groundmass is microcrystalline and exhibits devitrification. Feldspar crystals are commonly fine to coarse grained (usually up to 6 mm although up to 15 mm in some cases), and are anhedral to euhedral. Andesine to albite plagioclase and orthoclase are observed in thin section. The plagioclase is zoned; some crystals are deformed and broken. Myrmekite is rare and the plagioclase crystals are generally altered to clay, sericite and in some cases epidote. Orthoclase forms either aggregates or is interstitial, and is weakly to strongly altered to clay. Quartz is generally sparse, usually fine to medium grained, (although some rocks have quartz up to 10 mm), and is anhedral in shape. Most crystals display undulose character, and some are skeletal in texture. Hornblende is the most common mafic mineral. It is fine to medium grained, anhedral to euhedral, and in most cases is weakly to strongly chloritised. Many grains are poikilitic, and some have pyroxene cores. Pyroxene is rare and is usually altered to amphibole or removed leaving a void. Biotite is also rare, and is generally associated with the more felsic intrusives. It is fine to medium grained (up to 3 mm), anhedral to euhedral, and is typically altered to chlorite. Secondary calcite is present in the intermediate compositions.Many of the massive domes are adjacent to monomictic breccia which tends to suggest brecciation of the margins. On the margin of a large body at the northern boundary of Mount Archer National Park, 2 km west of Cabbage Tree Hill, a possible peperite is defined by minor amounts of siltstone to fine sandstone anastomosing through the dacite.|16-MAY-23
38893|Ellrott Rhyolite|Relationships and boundaries|The Ellrott Rhyolite is synchronous with deposition of the Chalmers Formation, and is a likely source of the Sleipner Member. The monomictic breccia adjacent to the margins of some of the domes is similar in appearance to the Sleipner Member. The Ellrott Rhyolite is intruded by andesite to basalt dykes, rhyolite dykes, gabbros, and granodiorites. The relationship with the Upper Permian Mount Warminster Formation is unknown.|16-MAY-23
38893|Ellrott Rhyolite|Age reasons|A Lower Permian age is assigned to the Ellrott Rhyolite based on two U-Pb zircon dates of 276±4 Ma and 268±4 Ma (M. Fanning, personal communication, 1998).|16-MAY-23
38893|Ellrott Rhyolite|Defn Reference|SOURCE OF INFORMATION --Crouch. S, Parfrey. S, and Taube. A  [DATE ?]. 'Geology, tectonic setting and metallogenesis of the Berserker Subprovince, northern New England Orogen'. Supplied by Ian Withnall (GSQ), September 2008.(Incomplete reference)|16-MAY-23
39098|Eskdale Igneous Complex|Unit history|Cranfield and Schwarzbock (1974) formally defined the Eskdale Granodiorite.  More recent work has been carried out in this unit by student projects from the University of Southern Queensland and Queensland University of Technology (Hayward, 1985; Snape, 1991 and Sparks, 1985).  The Eskdale Igneous Complex is an update of the name Eskdale Granodiorite as used by Campbell (1960) and defined by Cranfield & others (1976).|16-MAY-23
39098|Eskdale Igneous Complex|Geomorphic expression|The Eskdale Igneous Complex generally forms a depressed basin-shape topography of rolling hills ranging from 200 to 400m in elevation, is well cleared and mostly used for grazing of cattle.  Locally a more rugged topography is formed that is often forested.  Hornfelsed sediments at the margins of the complex are almost always are topographically higher except where the generally north east trending drainages leave the basin.|16-MAY-23
39098|Eskdale Igneous Complex|Extent|The main body of Eskdale Igneous Complex (Rges1-4) occurs within the limits of AMG 407000 7009000 and AMG 428000 6979000, from just south of Cressbrook Dam to just north of Nukinenda Homestead.  Another body adjacent to and faulted against the Esk Trough occurs as a north south elongate body, extending from Cressbrook Creek to Ivory Creek.  Scattered small intrusions (<3km2) assigned to the Eskdale Granodiorite occur north and north east of Ravensbourne, around Mount Deongwar, near Glen Oak and also near Greenvale on ESK.|16-MAY-23
39098|Eskdale Igneous Complex|Lithology|The Eskdale Igneous Complex comprises the following subunits - Rges (undivided), RgesL, Rgesa, Rgesg, Rgesgr, Rgesa, Rges1, Rges2, Rges3, and Rges4 (Table 11).  Areally the largest units of the complex (Rges1, Rges2, Rges3, and Rges4) are concentrically zoned around an inner core of granodiorite (Rges1).  Unit RgesL occurs along the eastern margin immediately north of the Anduramba Molybdenum Prospect.  Undivided Eskdale Igneous Complex is are now mainly confined to small bodies to the south of Cressbrook Creek Dam that intrude units of the Cressbrook Creek Group and the Sugarloaf Metamorphics.  Units Rgesg, Rgesga and Rgesgr occur mainly as satellitic bodies to the main intrusion. Sub-unit Rges (undivided) - granodiorite, tonalite, diorite, gabbro, aplite, granite, minor pegmatite.Sub-unit Rges1 - grey medium-grained hornblende-biotite granodiorite. Sub-unit Rges2 - hornblende-biotite granodiorite. Sub-unit Rges3 - biotite granite, granodiorite, minor gabbro. Sub-unit Rges4 - hornblende-biotite granodiorite. Sub-unit Rgesgr - pink-grey medium to coarse granite; locally strongly altered. Sub-unit Rgesa - includes 'Anduramba porphyry'; quartz feldspar, porhyritic rhyolite, aplite. Sub-unit Rgesg - Diorite, gabbro, hornblende gabbro, hornblende microgabbro. Sub-unit Rgesga - Altered granodiorite. Sub-unit RgesL - leuco granodiorite.|16-MAY-23
39098|Eskdale Igneous Complex|Comments|Very detailed lithology available in Cranfield et al (2001).|16-MAY-23
39098|Eskdale Igneous Complex|References|CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.",1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional Geology. **CLOWES,1997,Use of GIS in the assessment of local and regional changes in granitoids,Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology","Eskdale Granodiorite, Crows Nest granite geochemistry. **HAYWARD, S.B.,1985, Structural and metamorphic geology of the Mount Sevastopol-Perkins Knob area, South-East Queensland. Undergraduate Thesis, Darling Downs Institute of Advanced Education, Toowoomba. **SNAPE, M.,1991, A tin exploration programme in the Cressbrook Creek Dam area, South-East Queensland,Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology. **SPARKS, G.J.,1985,The geology of the Buckmara Creek district Ravensbourne Parish, S.E. Qld. Unpublished Thesis, Department of Geology, Darling Downs Institute of Advanced Education. **WEBB, A.W. & MCDOUGALL, I.1968, The geochronology of the igneous rocks of eastern Queensland. ,"Journal of the Geological Society of Australia., 15, 313-346.|16-MAY-23
6279|Esmeralda Granite|Name source|Esmeralda Homestead, 79 km south-southeast of Croydon at GR 7460-655144.|16-MAY-23
6279|Esmeralda Granite|Type section locality|The type locality as designated by White (1959) is on the Croydon-Esmeralda road, 3 km north of Esmeralda homestead (GR 7560-666175); there, the unit consists of grey, massive, coarse-grained biotite granite with scarce pegmatitic pods and lenses, and rare xenoliths of graphite and graphitic metasediments. Reference locality:  Turkey Knob Hill, alongside the Gulf Developmental Road about 13 km southeast of Croydon (GR 7361-423817) is a prominent tor made up of grey coarse-grained biotite granite, typical of the Esmeralda Granite as redefined.|16-MAY-23
6279|Esmeralda Granite|Extent|The Esmeralda Granite crops out along the western margin of the Croydon Volcanic Group as an elongate batholith with a northwesterly trending axis. The total area of exposure is about 850 km2 in central and southeastern CROYDON, western ESMERALDA and a small part of the southwestern corner of GILBERT RIVER. The batholith probably extends to the west under Mesozoic and younger sedimentary cover.|16-MAY-23
6279|Esmeralda Granite|Lithology|Grey, massive, medium to coarse,-even-grained to slightly porphyritic (muscovite-) biotite granite. Locally, at or near the roof of the pluton, especially in the Croydon area, it contains graphite and/or graphitic metasedimentary enclaves; greisenisation is widespread in the Mount Cassiterite-Stanhills area.|16-MAY-23
6279|Esmeralda Granite|Relationships and boundaries|The Esmeralda Granite intrudes the Idalia Rhyolite (including the Democrat Rhyolite Member) and Carron Rhyolite and probably also Parrot Camp Rhyolite and B Creek Rhyolite, of the Proterozoic Croydon Volcanic Group. It is unconformably overlain by the Jurassic Hampstead Sandstone and Loth Formation, and the Jurassic-Cretaceous Gilbert River Formation. The Nonda Granite is considered to be a fine-grained marginal variant of the Esmeralda Granite, or perhaps a slightly earlier, genetically related, intrusive phase; however, no unequivocal contact relationships have been observed.|16-MAY-23
6279|Esmeralda Granite|Identifying features|The Esmeralda Granite was originally defined by White (1959), and described by Branch (1966), as a medium-grained, grey biotite adamellite grading into granodiorite, which forms a batholith on the western side of the Croydon Volcanic Group and various-sized stocks east-northeast of Croydon and along the eastern margin of the volcanics. Field mapping by a joint Bureau of Mineral Resources-Geological Survey of Queensland party in 1980 showed that the plutons in the east, although similar in most respects to the Esmeralda Granite are sufficiently different and geographically separated to be excluded from it and assigned to the following new units: Mooremount Granite, Chadshunt Granite, Macartneys Granite, Olsens Granite, Dregger Granite, Illewanna Granite, Bimba Granite and Awring Granodiorite. The Nonda Granite, another new unit, is considered to be a marginal variant of the Esmeralda Granite. The name Esmeralda Granite is therefore restricted to the medium to coarse-grained biotite granite constituting the bulk of the largest exposed pluton on the western margin of the volcanics, and including the original type area (White, 1959).|16-MAY-23
6279|Esmeralda Granite|Age reasons|The Esmeralda Granite is mid-Proterozoic; it has a Rb-Sr muscovite age of 1444 Ma* (Black, 1973).          *Corrected using the 87Rb decay constant of 1.42x10-11 yr-1 recommended by Steiger & Jager (1977).|16-MAY-23
6279|Esmeralda Granite|Proposed publication|Queensland Government Mining Journal - 86/25571|16-MAY-23
6282|Esperanza Formation|Name source|Esperanza mine, 500 m west of Mammoth mine at 280215 in the Mammoth Mines 1:100 000 Sheet area.|16-MAY-23
6282|Esperanza Formation|Type section locality|Holostratotype: On the southern side of Gunpowder Creek, approximately 10 km downstream from its junction with Paradise Creek and approximately 2 km west of Esperanza mine, between 260200 (base) and 263200 (top) in the Mammoth Mines 1:100 000 Sheet area. The lower boundary of the Esperanza Formation in the type section is placed at the base of the lowermost stromatolitic chert. The upper boundary is placed at the top of a stromatolitic chert which is overlain by a ferruginous breccia included in the Lady Loretta Formation. Hypostratotype: The best exposed section of Esperanza Formation along Paradise Creek between 135170 and 108190 in the Mammoth Mines 1:100 000 Sheet area, is defined as the hypostratotype. Here three bands of massive cherts containing contiguous domal stromatolite bioherms, and "organ pipe" (Conophyton) stromatolites are interbedded with fine grained dolomitic sandstone, siltstone and minor quartzite. The overlying Lady Loretta Fromation is not exposed in this section.|16-MAY-23
6282|Esperanza Formation|Extent|It is recognised around the Kamarga Dome in the Lawn Hill 1:100 000 Sheet area; in the cores of anticlines and synclines in the Lawn Hill and Riversleigh 1:100 000 Sheet areas; in a narrow belt along the western side of the Mount Oxide and Memmoth Mines 1:100 000 Sheet areas; and in fault bounded blocks in the Mammoth Mines, Kennedy Gap and Yelvertoft 1:100 000 Sheet areas.|16-MAY-23
6282|Esperanza Formation|Proposer|Hutton L.J., Cavaney R.J., Sweet I.P.|16-MAY-23
25899|Ethabuka Sandstone|Name source|The name Ethabuka Sandstone is derived from Ethabuka Holding, 170 km southwest of Boulia on the western side of the Mount Whelan and Bedourie 1:250 000 Sheet areas.|16-MAY-23
25899|Ethabuka Sandstone|Unit history|The unit was first recognised as unit OM-11 by Pritchard (1960), and as an unnamed Middle Ordovician sandstone by Smith, Vine & Milligan (1961). However, Reynolds (1964; in Smith, 1965) included all sandstones overlying the Mithaka Formation, in the Siluro-Devonian Cravens Peak Beds. Alliance Oil Development N.L. (1975) recognised the "Ethabuka Beds" in AOD Ethabuka No. 1. The Ethabuka Sandstone was then recognised in outcrop, and referred to as "unnamed sandstone unit" (Shergold, Druce, Radke & Draper, 1976). The Cravens Peak Beds of Reynolds  contains three distinct units (Draper, 1976; Draper, Jones & Turner, in preparation): the Middle Ordovician Ethabuka Sandstone, the Devonian Cravens Peak Beds (sensu stricto), and a post-Devonian valley fill conglomeratic unit. The unit referred to by Harrison (1979) as the Ethabuka Beds is the Ethabuka Sandstone.|16-MAY-23
25899|Ethabuka Sandstone|Type section locality|The type section (holostratotype) is in AOD Ethabuka No. 1 (23o41'20"S; 138o25'30"E) (Alliance Oil Development, 1975). The base of the sequence is at 1202 m where sandstones overlie the shales of the Mithaka Formation. The upper boundary occurs at 55 m where the unit is unconformably overlain by the Jurassic Hooray Sandstone. This upper boundary has been the subject of some conjecture in the past. Alliance Oil Development (1975) fixed the top of the "Ethabuka Beds" at 1024 m despite the fact that in Appendix 1 they report the presence of probable Ordovician fossils at the top of an interval they assign to the Devonian Cravens Peak Beds. Harrison (1978), on the basis of seismic records, on velocity grounds, and the flat lying nature of the thin Mesozoic sequence at outcrop, placed virtually all of the rocks above 1202 m in the "Ethabuka Beds" except for the top 30 m which he assigns to the Cretaceous. This latter view is accepted here in principle although the Mesozoic boundary is lowered slightly (to 55 m). The boundary is taken at the change to more poorly sorted sandstone and from mottled clay into unmottled clay from the Ethabuka Sandstone into the Hooray Sandstone which contains possible plant remains. The seaction comprises a basal 244 m of very fine to fine sandstone with siltstone interbeds and rare pebbly layers; the siltstone is more common in the upper part of this sequence. Overlying this is a 875 m thick sequence of fine to medium grained sandstone. The upper 28 m comprises fine to medium grained sandstone interbedded with claystone. Samples of cuttings from AOD Ethabuka No. 1 are held by the Bureau of Mineral Resources and the Geological Survey of Queensland. The reference section (hypostratotype) is on a low ridge 100 m east of Toomba Bore (latitude 23o05'S, longitude 137o59'E) on Hay River 1:250 000 Sheet area, Northern Territory. It comprises 36 m of medium bedded, very fine to fine grained, sublabile sandstone containing clay pellets. Lamination, cross lamination and parting lineation are present. The base of the unit is obscured by alluvium. The upper contact is an unconformity with sandstones of the Devonian Cravens Peak Beds (Draper, jones & Turner, in preparation).  Reference localities. The basal contact of the unit can be seen at the top of the scarp 1.5 km southeast of PAP Netting Fence No. 1. Other useful outcrops of the basal part of the unit can be seen at Lake Amaroo (23o30'S; 138o40'E) on Mount Whelan 1:250 000 Sheet area. A stratigraphically higher portion of the unit, not present in the reference section, crops out at only one locality (22o58'S; 138o07'E on Glenormiston 1:250 000 Sheet area) as three small mesas and one slight rise. The rocks consist of weathered sandstone containing numerous biogenic structures. The contact with the overlying Cravens Peak Beds is obscured. Access is difficult with no permanent tracks in the area.|16-MAY-23
25899|Ethabuka Sandstone|Extent|The Ethabuka Sandstone crops out poorly along the inner margin of the Toko Syncline and is present on the Mount Whelan, Glenormiston and Hay River 1:250 000 Sheet areas. The unit is present in the subsurface in AOD Ethabuka No. 1.|16-MAY-23
25899|Ethabuka Sandstone|Thickness range|The maximum thickness observed in outcrop is 35 m, but 1147 m are present in AOD Ethabuka No. 1.|16-MAY-23
25899|Ethabuka Sandstone|Lithology|In outcrop, the Ethabuka Sandstone comprises very fine to fine-grained quartzose to sublabile sandstone, with some mudstone and siltstone interbeds. Clay pellets are present in some beds, and are occasionally present as thin clay pellet conglomerates. Friable, fine-grained sandstone with minor phosphate pellet conglomerate is present above the quartzose to sublabile sandstone. Bedding in the quartzose to sublabile sandstone is mainly thin to medium with minor thick bedding and flaser bedding. Bedding in the friable sandstone is thick to massive. The middle and upper portions of the type section are not present in outcrop.|16-MAY-23
25899|Ethabuka Sandstone|Fossils|In the lower part, pelecypods are the dominant fauna, but trilobites and nautiloids are present. In the upper part of the un;it the fossils occur as fragments, and comprise pelecypods, gastropods and linguloid brachiopods. The fauna has not yet been described although Fleming (in Alliance Oil Development, 1975) made a tentative identification of several fossils from AOD Ethabuka No. 1 and suggested an Ordovician age for the fauna.|16-MAY-23
25899|Ethabuka Sandstone|Relationships and boundaries|The un;it conformably overlies the Methaka Formation and is unconformably overlain by Devonian Cravens Peak Beds, or Mesozoic rocks where Cravens Peak Beds are absent, as is the situation in the vicinity of AOD Ethabuka No. 1.|16-MAY-23
25899|Ethabuka Sandstone|Structure and Metamorphism|Inorganic sedimentary structures present in outcrop in the quartzose to sublabile sandstone include: cross lamination, lamination, asymmetric, linguoid and interference ripplemarks, load casts, parting and streaming lineation, flute marks, brush marks, gouge marks, current crescents and sand shadows. Biogenic sedimentary structures include Cruziana, tracks and trails, walking traces, Rusophycus and rare burrows. The friable sandstone is extensively bioturbated; Cruziana is common, whereas U-tubes and various other burrows are less common.|16-MAY-23
25899|Ethabuka Sandstone|Age reasons|Superpositional evidence suggests a middle Ordovician age; this is supproted by the presence of probable Ordovician fossils in AOD Ethabuka No. 1.|16-MAY-23
25899|Ethabuka Sandstone|Name first published by|Harrison P.L., 1979|16-MAY-23
6300|Etheridge Group|Unit history|The name "Etheridge Formation" was applied by White (1965) to the Candlow, Heliman and Townley Formations, and part of the Robertson River Formation. See Introduction.|16-MAY-23
6300|Etheridge Group|Constituents|The Etheridge Group consists of, from top to bottom: Langdon River Formation; Candlow Formation; Heliman Formation; Townley Formation; Robertson River/Bernecker Creek Formation Einasleigh Metamorphics.|16-MAY-23
6300|Etheridge Group|Type section locality|A composite of the type sections of all the component stratigraphic units as defined separately.|16-MAY-23
6300|Etheridge Group|Extent|The Etheridge Group includes rocks that crop out over much of the Georgetown Inlier. It extends from the Langdon River valley east to the Newcastle Range, northeast to the Maureen area and past "Dagworth" homestead across the Einasleigh River, and southeast through the Gilberton-upper Gilbert River area to the Werrington-Lyndhust area where it is bounded by the Burdekin Fault Zone and the Balcooma Mylonite Zone. From the upper Gilbert River area, the Group is discontinuously exposed along the eastern side of the Newcastle Range northward almost to the Einasleigh River; it is bounded to the east by the Tertiary McBride basaltic province and the Balcooma Mylonite Zone. North of the Einasleigh River, Precambrian rocks in the Dargalong Inlier, the McDevitt and Dargalong Metamorphics, may be equivalent to the Robertson River Formation and Einasleigh Metamorphics. South of the upper Gilbert River area, isolated outliers of Precambrian rocks in the area from the Woolgar goldfield to Chasm Creek and the Cape River area, and an area of metamorphics in the Gregory Springs-Clarke Hills area may also be equivalent to part of the Etheridge Group.|16-MAY-23
6300|Etheridge Group|Thickness range|Difficult to estimate because of the variability of thickness of the component units, their complex folding, and the non-exposure of the bases of the lowermost units. Langdon River Siltstone 800 to 1400m.  Candlow Formation 1000 to 3500 m. Heliman Formation 800 to 1500 m. Townley Formation 400 to 1500 m. Robertson River Formation/Bernecker Creek Formation/Einasleigh Metamorphics at least 3000 m.    =  6000 to 11000 m.|16-MAY-23
6300|Etheridge Group|Lithology|Phyllite, slate, mica schist, mica-feldspar-quartz gneiss, quartzite, calc-silicate rocks, metabasalt, metadolerite, metagabbro, amphibolite, migmatite; cleaved to phyllitic sericitic or quartz-lithic siltstone to fine sandstone; variably ferruginous and/or carbonaceous siltstone, fine sandstone, and rare shale; quartzose siltstone and fine sandstone; dark grey siliceous siltstone and fine sandstone.|16-MAY-23
6300|Etheridge Group|Relationships and boundaries|The base of the Group, as presently known, is not exposed. The top is defined by marked angular unconformity at the base of the Malacura Formation, which contains detritus derived from the Etheridge Group. Intruded by a wide variety of Proterozoic granitic rocks, including the Forsayth granitic suite, and by a variety of Late Palaeozoic igneous rocks. Partly overlain (unconformably) by late Palaeozoic acid volcanics (Newcastle Range, Maureen, Dismal Creek and Cumberland Range Volcanics) and sandstones of the late Mesozoic Eulo Queen Group and Gilbert River Formation.|16-MAY-23
6300|Etheridge Group|Identifying features|White (1965) divided the Precambrian metasedimentary rocks of the Georgetown Inlier between the Newcastle Range (Newcastle Range Volcanics) and the Gregory Range (Croydon Volcanics) into three units: Robertson River Metamorphics, Etheridge Formation, and Langdon River Formation. Work by BMR-GSQ field parties during 1977 and 1978 has shown that the upper three-quarters of White's "Etheridge Formation" can be divided into three units, the Candlow, Heliman, and Townley Formations. The lower part of the "Etheridge Formation" grades into and is inseparable from White's "Robertson River Metamorphics"; accordingly, these rocks have been grouped together and redefined as Robertson River Formation. Conformably underlying, and perhaps in part transitional into the Robertson River Formation is the Bernecker Creek Formation. This calcareous unit can be traced, with increasing metamorphic grade, into the Einasleigh Metamorphics where it either underlies or overlies (facings are not yet resolved) metapelitic rocks that may be equivalent to (part of?) the Robertson River Formation. In places, where calc-silicate metamorphics are absent, pelitic schists/gneisses of the Einasleigh Metamorphics grade into Robertson River Formation. Thus it is proposed to upgrade "Etheridge Formation" to Etheridge Group and include in it all rocks of the previous "Formation", along with all contiguous and lithologically related units above and below. The Group therefore includes all rocks between the unconformity at the top of the Langdon River Siltstone and the (unknown) base of the Einasleigh Metamorphics.|16-MAY-23
6300|Etheridge Group|Age reasons|Probably Middle Proterozoic. A minimum age of 1570+/-30 m.y. has been obtained from dating of the earliest deformation-metamorphism event in the Einasleigh Metamorphics (Black et al., in press). The Forsayth Granite, which intrudes the Group, is dated at about 1600 m.y. (L.P. Black, pers. comm., 1978).|16-MAY-23
6319|Etonvale Formation|Type section locality|Galloway (1970) redefined the type section to 2011.7-2335.4m to exclude the Log Creek and Buckabie Formations, but still included the Cooladdi Dolomite Member and the Boree Salt Member. These were excluded by Auchincloss (1976) and Boreham and De Boer (1998) respectively, so the type section is here taken to be the 2011.7-2298 m interval in PPC Etonvale-1. (reported in McKillop et al., 2007)|16-MAY-23
6400|Eva Creek Microgranite|Name source|Eva Creek which rises in the eastern Newcastle Range and joins McMillan Creek at grid ref. 119796 (Georgetown 1:100 000 Sheet area).|16-MAY-23
6400|Eva Creek Microgranite|Unit history|Branch (1966) and Bain et al. (1975) assigned the rocks to the Elizabeth Creek Granite. A new unit is defined because of (1) the spatial separation of the Eva Creek Microgranite and type Elizabeth Creek Granite and consequent uncertainty as to their temporal and genetic relationships, (2) the fact that microgranite is only a minor component of the Elizabeth Creek Granite as currently defined, and (3) possible future re-study and revision of the Elizabeth Creek Granite.|16-MAY-23
6400|Eva Creek Microgranite|Type section locality|Bush track from the left hand branch of Eva Creek at grid ref. 157749 (Georgetown 1:100 000 Sheet area) to abandoned tin miner's camp at grid ref. 130759 (Georgetown 1:100 000 Sheet area). Rocks cropping out in this area are mainly grey and pink, buff-weathering, porphyritic microgranite with minor biotite and hornblende; the rocks weather to rounded boulders and tors. Grey quartz-rich greisen dykes and quartz veins with cassiterite and minor molybdenite, chalcopyrite and galena cut the microgranite locally. The microgranite is commonly chloritized adjacent to such dykes and veins.|16-MAY-23
6400|Eva Creek Microgranite|Extent|A roughly rectangular area of 11 km2 in the northern part of the eastern Newcastle Range about 40 km east of Georgetown.|16-MAY-23
6400|Eva Creek Microgranite|Lithology|Mainly grey and pink porphyritic microgranite with 10 to 50 percent quartz and feldspar phenocrysts, and up to 5 percent biotite and hornblende phenocrysts. Feldspar phenocrysts are perthite and subsidiary plagioclase (oligoclase-andesine). Subsidiary fine grained porphyritic granite, grey quartz-rich greisen. Minor chloritized microgranite, pink aplite.|16-MAY-23
6400|Eva Creek Microgranite|Relationships and boundaries|Intrudes and has locally metamorphosed volcanic and sedimentary rocks in the eastern sequence of the Newcastle Range Volcanics.|16-MAY-23
6400|Eva Creek Microgranite|Age reasons|Probably Late Palaeozoic. The Newcastle Range Volcanics in the eastern part of the range are probably Carboniferous, like those in the main range. The Eva Creek Microgranite is lithologically similar to some varieties of the Late Palaeozoic Elizabeth Creek Granite; mineralisation is similar to that in the Elizabeth Creek Granite.|16-MAY-23
80204|Excelsior Conglomerate Marker Bed|Name source|After Excelsior Road, Gympie.|16-MAY-23
80204|Excelsior Conglomerate Marker Bed|Unit history|This unit was first used informally as the Excelsior haematitic member by Gympie Eldorado Gold Mines at Monkland Mine.|16-MAY-23
80204|Excelsior Conglomerate Marker Bed|Type section locality|Reference drill hole at the Zillmere core library in Brisbane is GEGM drill hole G215, 271.1-286.1 m (MGA 467424mE; 7101493mN, Lat: -26°12'21"  Long: 152°40'26"). No known surface exposure. The relationship of this unit within Dawn Formation is illustrated in Stidolph et al. (2016) Figure 6 (on page 45).|16-MAY-23
80204|Excelsior Conglomerate Marker Bed|Extent|Intersected in drill holes from the deeper levels of Monkland Mine and at shallower depths beneath Kidgell Andesite at Deep Creek.|16-MAY-23
80204|Excelsior Conglomerate Marker Bed|Thickness range|5-15m.|16-MAY-23
80204|Excelsior Conglomerate Marker Bed|Lithology|The Excelsior bed consists of conglomerate in a red hematitic siltstone matrix with sandy bands.  The clasts are of exotic provenance and include pink granite, quartzite and free quartz suggesting they were not derived locally from the underlying basalt.|16-MAY-23
80204|Excelsior Conglomerate Marker Bed|Relationships and boundaries|Probably marks an unconformity between the Highbury and Dawn formations.|16-MAY-23
80204|Excelsior Conglomerate Marker Bed|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie, 12-JAN-2017.|16-MAY-23
25903|Fahey Range Andesite|Name source|FAHEY RANGE; grid reference 785768, Caboolture 1:100 000 Sheet area (9443).|16-MAY-23
25903|Fahey Range Andesite|Type section locality|(250 m to 275 m) of andesitic volcanics exposed over a horizontal distance of 405 m along Cedar Creek (a tributary of the South Pine River) from grid references 778778 (bottom) to 781776 (top of section), Caboolture 1:100 000 Sheet area (9443). The base is identified by a grey to dark grey andesitic agglomerate 45 m thick which is overlain by very fine-grained andesite, andesite (porphyritic), and andesitic agglomerate flows dipping at 40o to 60o to the northeast. The top is identified by a very fine-grained hornfelsed andesite, 14 m thick.|16-MAY-23
25903|Fahey Range Andesite|Extent|The unit crops out over approximately 3 km2 from Mount D'Aguilar 781794 to Mount Glorious 778768, Caboolture 1:100 000 Sheet area (9443).|16-MAY-23
25903|Fahey Range Andesite|Thickness range|250 m to 275 m within type section.|16-MAY-23
25903|Fahey Range Andesite|Lithology|Andesitic agglomerate, grey to dark grey, very fine-grained groundmass containing fragments of andesite and minor argillaceous material to 23 cms in diameter. Andesite, dark grey, very fine-grained groundmass, porphyritic, euhedral phenocrysts of plagioclase to 5 mm in diameter. Very fine-grained andesite, dark grey, aphanitic. Total absence of plagioclase phenocrysts. Hornfelsed by contact metamorphism with Mount Samson Granodiorite (Phillips, 1964).|16-MAY-23
25903|Fahey Range Andesite|Relationships and boundaries|The unit unconformably overlies the Devonian to Carboniferous Nerangleigh-Fernvale Beds and was intruded by the Triassic Mount Samson Granodiorite which has been dated at 217 million years by the potassium-argon method (Cranfield, et al., in prep.). The base and top of the section are the contacts of the andesitic volcanics with the diorite and microdiorite phases of the Mount Samson Granodiorite.|16-MAY-23
25903|Fahey Range Andesite|Age reasons|Permian to Triassic|16-MAY-23
25903|Fahey Range Andesite|Proposed publication|Report of the Geological Survey of Queensland|16-MAY-23
6511|Falls Creek Tonalite|Name source|No name source given.|16-MAY-23
6511|Falls Creek Tonalite|Unit history|The main mass of Falls Creek Tonalite was not recognised by Wyatt & others (1970), but they did map two of the smaller masses which they assigned to the Ravenswood Granodiorite|16-MAY-23
6511|Falls Creek Tonalite|Geomorphic expression|The tonalite generally forms relatively subdued topography with light tones on aerial photographs.  It crops out poorly, but is well exposed along the Running River and Falls Creek from which the unit takes its name.|16-MAY-23
6511|Falls Creek Tonalite|Type section locality|The type area of the Falls Creek Tonalite is along Falls Creek from 8059-923979 downstream to the junction with the Running River at 924962.  Partially hornfelsed biotite tonalite is exposed.  At 923979 (just upstream of the Ewan-Hidden Valley road) the tonalite is well exposed in a small waterfall and is one of the least hornfelsed outcrops observed.  The grid refernces are based on the AGD66 datum.|16-MAY-23
6511|Falls Creek Tonalite|Extent|The Falls Creek Tonalite forms a belt about 6 km long and up to 2 km wide along the valley floor of the Running River, southwest from the settlement of Hidden Valley.  It is bounded to the northwest and southeast by more rugged ranges formed by Carboniferous granites.  At least four other masses of tonalite have been mapped intruding the Running River Metamorphics further to the southwest along the Running River valley.  They are tentatively equated with the Falls Creek Tonalite.|16-MAY-23
6511|Falls Creek Tonalite|Lithology|The Falls Creek Tonalite consists of pale to dark grey, medium-grained, equigranular biotite tonalite.  The tonalite contains quartz (30%), plagioclase (50-60% - andesine, locally with normal oscillatory zoning), and biotite (5-20%).  Because of the proximity to large Carboniferous granite batholiths, the Falls Creek Tonalite, like the Running River Metamorphics, has been hornfelsed.  The quartz is recrystallised and forms aggregates up to 5 mm across of unstrained subequant to elongate subgrains (<0.5 mm) which have smooth to slightly interlocking margins.  The biotite is brown and generally recrystallised to aggregates of fine decussate flakes.  In the main pluton, the least hornfelsed area observed is in the vicinity of the type locality in Falls Creek, where the biotite is only slightly replaced by decussate aggregates.The tonalite generally has at least a weak foliation defined by the alignment of biotite and quartz aggregates.  In some outcrops, the quartz forms a mortar texture around the plagioclase crystals.  A streaky layering defined by different proportions of biotite is locally present.  The darker layers may be assimilated metamorphic rocks.  Veins of more leucocratic tonalite cut the darker layers, and these are folded in places.  Rafts of amphibolite up to several metres long are locally aligned parallel to the streaky layering and foliation.  Larger outcrops of metamorphics up to several hundred metres long and cut by dykes of tonalite have been observed within the main pluton, for example 8059-932984 along the Ewan-Hidden Valley road.  The grid reference is based on the AGD66 datum. The smaller masses of tonalite are essentially similar to the main mass, and consist of grey, variably foliated, medium-grained, equigranular, biotite tonalite.  They are generally less hornfelsed, being further away from the Carboniferous batholiths.|16-MAY-23
6511|Falls Creek Tonalite|Relationships and boundaries|The Falls Creek Tonalite intrudes the Running River Metamorphics which, as discussed elsewhere, may be of Proterozoic or early Palaeozoic age.  It is foliated parallel to the general northeast trends in the metamorphic rocks and has probably been deformed with them.  The nature of the contact with the Running River Metamorphics is probably irregular, but has not been studied in detail.  The granitoids tentatively assigned to the unit in the area between Zig Zag and Naven Creeks are certainly complex, with abundant metamorphic screens in the granitoid and granitoid dykes and veins in the adjacent metamorphic rocks.|16-MAY-23
6511|Falls Creek Tonalite|Age reasons|A Carboniferous Rb-Sr biotite-total rock age of 331+2 Ma was obtained by the BMR (D. Wyborn, personal communication, 1989), but this undoubtedly records the age of hornfelsing by the Carboniferous granites that intrude the tonalite and form extensive batholiths to the north and south of the Running River valley.  A Sm-Nd T[subscript] DM (depleted mantle) model age of about 1453 Ma suggests that it was sourced from rocks generated from the mantle in the mid-Proterozoic, but its intrusive age is as yet uncertain.|16-MAY-23
6511|Falls Creek Tonalite|References|WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127.|16-MAY-23
33427|Farquharson Granite|Name source|The granite is named after Farquharson Creek that drains the northern end of the outcrop area.|16-MAY-23
33427|Farquharson Granite|Unit history|Reiser (1971) previously mapped the unit as part of a large area of undivided granite of possible Permian age on the CHINCHILLA 1:250 000 sheet.|16-MAY-23
33427|Farquharson Granite|Geomorphic expression|The unit forms low flat country rising to low wooded hills with elevation between 320 and 340m in elevation. Tertiary duricrust mesas are developed in places on the unit.|16-MAY-23
33427|Farquharson Granite|Type section locality|The type area of the Farquharson Granite is in the headwaters of Farquharson Creek on BOONDOOMA.|16-MAY-23
33427|Farquharson Granite|Extent|The unit forms a roughly rectangular-shaped body outcropping over an area of approximately 25km2, 7km west of Boondooma Homestead, 30km west of Proston.  Subunit Rgqd occurs on the northwestern margin of the main body as a north-north-west trending elongate body about 1km wide.|16-MAY-23
33427|Farquharson Granite|Lithology|Rgq: :  The granite is pale pinkish grey in colour, medium-grained, equigranular to locally porphyritic hornblende-biotite granite.  It has a hypidiomorphic granular texture in thin section and contains prominent mainly euhedral accessory sphene crystals.  Hornblende and biotite occur in roughly equal proportions.  The rock is also relatively rich in opaque iron oxide grains, accounting for the unit's moderate to high magnetic susceptibility values.  Along the eastern margin of the unit, thin-section textures some evidence of quenching, with coarser crystals and crystal aggregates enveloped in a matrix of very fine grained feldspar and quartz. Rgqd: :  The unit consists of dark-grey, medium to coarse grained, equigranular quartz diorite and diorite containing roughly equal proportions of hornblende and biotite. The rock displays an idiomorphic to hypidiomorphic granular texture in thin-section.|16-MAY-23
33427|Farquharson Granite|Relationships and boundaries|The magnetic image of the unit suggests that the Rgqd unit is part of the same magnetic entity as the Farquharson Granite and follows a similar magnetic trend. The two units may be roughly of similar age and may share a co-genetic relationship. Rgqd is therefore provisionally mapped as a more mafic phase of the main granite body represented by areas mapped as subunit Rgq. Along its northern margin the Farquharson Granite is partly faulted against the Toondahra Granite along a west-northwest trending fault.  The unit probably has an intrusive relationship with the Toondahra Granite, and the microscopic quench textures near its contact with the Boondooma Igneous Complex to the east also suggests a similar relationship.|16-MAY-23
33427|Farquharson Granite|Age reasons|No age dating of the unit has been undertaken, but a Middle to Late Triassic age is considered most likely.|16-MAY-23
33427|Farquharson Granite|Comments|GEOPHYSICAL EXPRESSION:: The radiometric response of the unit is almost indistinguishable from that of the surrounding rocks.  However, the unit has a moderate to high magnetic susceptibility, which constrasts with the surrounding poorly magnetised units.  The magnetic image shows the unit to apparently consist of a number of amalgamated north-trending dyke-like bodies, between which slivers of Toondahra Granite have been mapped.  Subunit Rgqd has a distinctively high magnetic susceptibility and appears to form part of the same magnetic entity as the adjacent Farquharson Granite to the west, and has consequently been mapped as a subunit of that body.|16-MAY-23
33427|Farquharson Granite|References|REISER, R.F.1971,Chinchilla, Qld - 1:250,000 Geological Series. Bureau of Mineral Resources, Geology and Geophysics, Australia, Explanatory Notes, SG/56-9.|16-MAY-23
31117|Fat Hen Creek Complex|Name source|Fat Hen Creek, a tributary of the Cape River which it joins about 600 metres east of Ballabay at GR 7957 218402 .  The grid reference is based on the AGD66 datum.|16-MAY-23
31117|Fat Hen Creek Complex|Unit history|The Fat Hen Creek Complex was previously mapped as undivided Ravenswood Granodiorite Complex (ODn) by Paine and others (1971).|16-MAY-23
31117|Fat Hen Creek Complex|Type section locality|West of a mill on Fat Hen Creek at GR 3192 77441.  The grid reference is based on the AGD66 datum.|16-MAY-23
31117|Fat Hen Creek Complex|Description at type locality|Here a medium grained, grey to black, foliated biotite orthogneiss crops out. The gneiss comprises strained quartz, plagioclase, K-feldspar, red/brown biotite, and muscovite/chlorite/green mica grains (alteration after cordierite?). In the upper reaches of Fat Hen Creek, quartz-muscovite-biotite-garnet schist represents high grade metamorphics grading into the granitic gneiss. Also in the upper reaches of Fat Hen Creek at GR 3176 77452, about 1km west of the biotite schist, layered migmatite probably forms an intermediate stage between biotite schist and granitic gneiss. A similar sequence occurs in deeply weathered schist, migmatite, and granitic gneiss east of Ballabay and in the area between Ballabay and Pentland.  The grid reference is based on the AGD66 datum.|16-MAY-23
31117|Fat Hen Creek Complex|Extent|The Fat Hen Creek Complex forms a belt about 5km wide trending west northwest from about 10km southwest of Pentland to near the Mount Emu diggings on the Flinders River south of Reedy Springs homestead (Figure 2). Garnet-biotite gneiss reported from near Lake Cargoon are also part of this unit. The belt has been truncated by granites of the Lolworth Batholith to the northwest of the type area and granites of the Reedy Springs Batholith near the Mount Emu diggings.|16-MAY-23
31117|Fat Hen Creek Complex|Lithology|The Fat Hen Creek Complex comprises mainly biotite orthogneiss, with minor migmatite, biotite schist, calc-silicate and amphibolite. The unit is defined to include all of the granitic orthogneiss. Because the contact with the Cape River Metamorphics is complex, including zones of migmatite and schist interlayered with granitic orthogneiss, some of these lithologies (which are usually part of the Cape River Metamorphics) are mapped with the complex. Biotite-rich schlieren are very common and more refractory calc-silicate and amphibolite occur as residual xenoliths in the granitic orthogneiss.|16-MAY-23
31117|Fat Hen Creek Complex|Relationships and boundaries|Biotite orthogneiss in the Fat Hen Creek Complex is interpreted as 'S-type' granite (Chappell & White, 1974) derived from partial melting of the Cape River Metamorphics. The belt is about 5km wide and is broadly parallel to, but may locally cut across, lithological units within the metamorphics. Calc-silicates and amphibolites form xenoliths in the granitic orthogneiss. It is intruded by the granites of the Mesoproterozoic Gorge Creek Granite Complex and by Late Silurian to Early Devonian granites of the Lolworth Batholith.|16-MAY-23
31117|Fat Hen Creek Complex|Age reasons|The age of the Fat Hen Creek Complex is probably Mesoproterozoic. Zircons separated from the Gorge Creek Granite Complex are of two types: equant, multi-faceted grains interpreted by Fanning (1995) as being formed `during a high grade metamorphism in the lower crust¿; and simple euhedral grains of probable magmatic origin. These two types of zircon grains have statistically indistinguishable SHRIMP microprobe 207[superscript]Pb/206[superscript]Pb ages at 1109+/- 22 Ma. The deep crustal metamorphism suggested by Fanning (1995) may be the migmatisation and partial melting which gave rise to the Fat Hen Creek Complex granitic gneiss.|16-MAY-23
31117|Fat Hen Creek Complex|Comments|MAGNETIC SUSCEPTIBILITY::  In the type area, the Fat Hen Creek Complex biotite orthogneiss is non-magnetic. However, south of the Cape River at GR 3160 77738, cordierite-muscovite-biotite orthogneiss has magnetic susceptibilities in the range 427-1145 x 10[superscript]-5 SI units.  The grid reference is based on the AGD66 datum.|16-MAY-23
31117|Fat Hen Creek Complex|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
6639|Fiery Creek Volcanics|Name source|From Fiery Creek which flows through the northern part of the Mount Oxide 1:100 000 Sheet area.|16-MAY-23
6639|Fiery Creek Volcanics|Unit history|Rocks now included in the Fiery Creek Volcanics were previously included in the Myally Beds, Ploughed Mountain Beds and Surprise Creek Beds by Carter & others (1961). The name was first published by Cavaney 1975.|16-MAY-23
6639|Fiery Creek Volcanics|Type section locality|Holostratotype: 1 km southeast of Fiery Creek, approximately 7 km southeast of the junction of Black Tea Tree Creek and Fiery Creek in the Mount Oxide 1:100 000 Sheet area between 170893 (base) and 165902 (top). This section comprises 85 m of vesicular mafic volcanics overlain by 160 m of rhyolitic agglomerate. A quartz feldspar porphyry band may be intrusive or extrusive.|16-MAY-23
6639|Fiery Creek Volcanics|Extent|Best developed in the Gregory Downs and the northern part of the Mount Oxide 1:100 000 Sheet areas; in a continuous belt along the western margin of the Myally 1:100 000 Sheet area; and discontinuously in the Mammoth Mines and Alsace 1:100 000 Sheet areas.|16-MAY-23
6639|Fiery Creek Volcanics|Thickness range|The unit is 250 m thick in the type section. Elsewhere the thickness varies considerably.|16-MAY-23
6639|Fiery Creek Volcanics|Lithology|Massive rhyolite agglomerate is the main lithology in the Gregory Downs and northern part of the Mount Oxide 1:100 000 Sheet areas. Throughout the rest of the outcrop area, the unit comprises flow banded rhyolite, ferruginous sandstone, and vesicular mafic volcanics in varying proportions. Massive rhyolite domes occur in the northeastern part of the Mount Oxide 1:100 000 Sheet area.|16-MAY-23
6639|Fiery Creek Volcanics|Relationships and boundaries|The unit is overlain with slight angular unconformity by sandstone of the Surprise Creek Formation. It rests conformably on the Bigie Formation and where this is not present, it rests unconformably on the Quilalar Formation or Myally Sub Group.|16-MAY-23
6639|Fiery Creek Volcanics|Age reasons|Mid Proterozoic (Carpentarian). It is equivalent to the Carters Bore Rhyolite which has been dated at 1678 m.y. (Page 1978).|16-MAY-23
6639|Fiery Creek Volcanics|Proposed publication|Queensland Government Mining Journal|16-MAY-23
6639|Fiery Creek Volcanics|First Reference|80/21252|16-MAY-23
6639|Fiery Creek Volcanics|Proposer|Hutton L.J., Cavaney R.J., Sweet I.P.|16-MAY-23
33434|Fifer Creek Metamorphics|Name source|The unit is named after Fifer Creek, which traverses through the centre of the outcrop belt, 1km west of Melrose homestead|16-MAY-23
33434|Fifer Creek Metamorphics|Unit history|Murphy & others (1976) previously mapped the unit on the GYMPIE 1:250 000 sheet as unit Pz-an undifferentiated sequence of Palaeozoic metamorphics, sediments and volcanics.|16-MAY-23
33434|Fifer Creek Metamorphics|Geomorphic expression|The metamorphics are moderately well exposed as a series of partially cleared strike ridges.|16-MAY-23
33434|Fifer Creek Metamorphics|Extent|The Fifer Creek Metamorphics form a north-north-west trending, 3-4km wide belt extending for over 30km in the western half of MURGON.|16-MAY-23
33434|Fifer Creek Metamorphics|Lithology|The unit is variably metamorphosed and deformed, but, in general, the degree of metamorphism and intensity of deformation increases with increasing proximity to the Boondooma Igneous Complex.  Higher-grade rocks also occur in many places close to the eastern margin of the unit bordered by the Hivesville and Stuart River Granites and the Melrose Igneous Complex.  Lower grade, less-deformed rocks are more common in the centre of the belt, mainly for around 3-4km north and south of Meyhar Creek. A lower grade sequence along Meyhar Creek consists mainly of mudstone, siltstone and arenite, with scattered thin-bedded chert horizons.  The arenites are variably recrystallised, range from quartzose to lithofeldspathic in composition, and form medium to thick beds sporadically interlayered with the mudstone/siltstone packages.  The siltstones are thin-bedded to laminated (or rarely medium-beddded) and very rarely exhibit cross-lamination and grading.  They are sporadically siliceous in composition, forming thin beds with a chert-like appearance within the mudstones. Discontinuous intervals and horizons of haematitic chert (locally brecciated) and cream silicified chert occur sporadically throughout the sequence.  The cherts are thin and lensoidally bedded, and show well developed chaotic chevron-style slump? folds as well as sporadic tectonic folds (east-verging around AMG 364000 7089400). Where the cherts and metacherts are extensive, they have been mapped as subunit DCic.  Local intense cleavage development has locally converted the mudstones to slates.  In the east adjacent to the Hivesville Granite, the sequence is annealed and slightly micaceous, and coarse-grained granite sills and rare ¿sweat¿ veins intrude the sediments.......The higher grade belts within the unit contain meta-argillite (locally fine schist) and meta-silstone packages as well as intervals of massive, variably recrystallised meta-arenite with scattered strongly to moderately recrystallised, well-bedded chert and meta-chert horizons and locally-developed mylonites and phyllonites...............Thermally metamorphosed rafts of Fifer Creek Metamorphics are well exposed within the Boondooma Igneous Complex north of the Proston water supply pumping station on the Boyne River.  These rocks comprise thin to laminated meta-siltstone bands within dark grey meta-argilllite, forming open to tight folds with a well developed axial plane schistosity dipping steeply to the south-west.  Scattered pegmatite and aplite veins (some with tourmaline-rich cores) occur along the axial plane schistosity, and medium grained granite sills occur locally. Fine porphyroblastic biotite is common throughout. Swarms of "lit-par-lit"- style coarse-grained biotite granite sills up to 2m wide occur locally in this area, associated with an increase in the degree of recrystallisation over a distance of only a few metres forming interlayered felsic gneiss and biotite schist.|16-MAY-23
33434|Fifer Creek Metamorphics|Relationships and boundaries|The unit is intruded by numerous large granitoid bodies, including the Hivesville, Wooroolin and Stuart River Granites, and the Boondooma Igneous Complex, as well as smaller bodies (unitsPRg1, Rir, Rg1, Rg2, Rg3, Rggd).  Basalts of the Tertiary Main Range Volcanics unconformably overlie the unit.|16-MAY-23
33434|Fifer Creek Metamorphics|Structure and Metamorphism|The dominant bedding and cleavage dips are steep to the west. Slates with fine discontinuous siltstone laminae locally display open to isoclinal, gently plunging folds about the major bed-parallel slaty cleavage. Intensive shearing occurs locally within the unit, the most notable exposure being in the spillway of the Gordonbrook Dam. At this locality, the siltstone/mudstone/fine arenite sequence has been cataclastically sheared to form phyllonite and quartzite, with bedding being destroyed by shearing.|16-MAY-23
33434|Fifer Creek Metamorphics|Age reasons|The unit is considered to represent deeper level more metamorphosed equivalents of the less deformed Maronghi Creek beds, together forming part of the Devonian-Carboniferous accretionary wedge assemblage extending the length of the northern New England Orogen.|16-MAY-23
33434|Fifer Creek Metamorphics|Alteration and Mineralisation|MINERALISATION:: Minor subeconomic silver/lead mineralisation occurs at the Ronald John prospect south of Melrose homestead (AMG 361400 7088600) within silicified, metasomatised metamorphic rocks adjacent to the contact to the Boondooma Igneous Complex|16-MAY-23
33434|Fifer Creek Metamorphics|Geophysical Expression|The unit registers as pale mottled brown tones on the K-Th-U (RGB) ternary radiometric images, and has a low magnetic response indistinguishable from most of the adjacent units on AIRDATA magnetic images.|16-MAY-23
33434|Fifer Creek Metamorphics|References|MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.|16-MAY-23
6682|Fish River Formation|Name source|From Fish River, a south-flowing tributary of the Nicholson River in the southern Seigal Sheet area.|16-MAY-23
6682|Fish River Formation|Type section locality|Roberts et (1963) nominated a reference section in the Seigal Sheet area, but since this has not been published as a type section, a complete well exposed section in and adjacent to Wire Creek in the Hedleys Creek Sheet area is nominated as the type section. The base of the section is in the east bank of Wire Creek at grid reference 957314. The section runs southeast along the creek bank for 1.3 km to a cliff, then for a distance of 0.7 km due east to the to of the formation at grid reference 974305.|16-MAY-23
6682|Fish River Formation|Extent|The unit forms a series of disconnected ridges trending east-northeast across the southern part of the Seigal Sheet area, Northern Territory, and crops out in a belt up to 4 km wide with similar trend in the central part of the Hedleys Creek Sheet area, Queensland.|16-MAY-23
6682|Fish River Formation|Thickness range|250 m in type section; 10-200 m in Seigal Sheet area.|16-MAY-23
6682|Fish River Formation|Lithology|Fine to medium-grained quartz sandstone, with minor lithic sandstone, conglomeratic sandstone, siltstone and shale.  A lens of siltstone and shale (Ptf2), has been mapped in the Hedleys Creek Sheet area, and divides the lower (Ptf1) and upper (Ptf3) sandstones in the unit.|16-MAY-23
6682|Fish River Formation|Relationships and boundaries|The contact with the underlying Peters Creek Volcanics is sharp, and is marked by a thin (1 m) conglomerate at the base of the Fish River Formation. It appears disconformable in outcrop, but on a regional scale is an angular unconformity - successively older units of the Peters Creek Volcanics are truncated the farther west one goes. The upper contact is also sharp and is recognised by an abrupt change from sandstone (with gritty lenses) to poorly outcropping shale, and silicified stromatolitic dolomite.|16-MAY-23
6682|Fish River Formation|Identifying features|The name was first published by Roberts, Rhodes and Yates (1963) but the unit was not defined. During mapping in 1972 the unit was completely remapped and a suitable type section nominated. Although the unit is predominantly sandstone, the term "Formation" has been retained, because the name has been in use for 15 years, and is in wide use in literature. It is not entirely inaccurate anyway, because conglomerate and siltstone are both prominent rock types in the type area.|16-MAY-23
6682|Fish River Formation|Age reasons|Proterozoic-Carpentarian. It is correlated on lithological grounds with the sandstone in the Masterton Formation in the nearby McArthur Basin (which is part of the "type" Carpentarian).|16-MAY-23
6682|Fish River Formation|Defn author|I. Sweet, 1978.|16-MAY-23
6682|Fish River Formation|Proposed publication|BMR Report on geology of Hedleys Creek 1:100 000 Sheet area.|16-MAY-23
6682|Fish River Formation|Defn approved by|Queensland Sub-Committee|16-MAY-23
6682|Fish River Formation|Defn Reference|82/22568|16-MAY-23
6682|Fish River Formation|Reserved? Yes/No|Already published|16-MAY-23
6827|Forsayth Granite|Name source|Forsayth township situated 40 km south of Georgetown at longitude 143o36'E, latitude 18o35'S, Georgetown 1:250 000 Sheet area.|16-MAY-23
6827|Forsayth Granite|Unit history|White (1959, 1965) included, in the Forsayth Granite, rocks which are now assigned to the Oak River Granodiorite, Digger Creek Granite, White Springs Granodiorite, Mistletoe Granite, Lighthouse Granite and Talbot Creek Granodiorite. The Forsayth Granite is thus redefined to exclude these units and to restrict the name to Middle? Proterozoic granitic rocks in the type area and their correlatives to the north and west as discussed above. Bain et al. (1975) used the name "Forsayth Complex" synonomously because of the impossibility of mapping the numerous varieties at 1:100 000 scale; the original name is retained however, so as to conform with the nomenclatural style used for the other granitic rock units in the region.|16-MAY-23
6827|Forsayth Granite|Type section locality|Main Georgetown-Forsayth road between the two townships, excluding areas of Robertson River Metamorphics and Cobbold Dolerite. Rocks exposed in the type area are mainly grey melanocratic to leucocratic, equigranular to porphyritic, biotite granite with minor local muscovite; the rocks are commonly foliated.|16-MAY-23
6827|Forsayth Granite|Extent|Two main areas: (1) 375 km2 centred on Forsayth and extending from the Ropewalk Range north to Talbot Creek, (2) 500 km2 extending from near Telegraph Creek, 3 km east of Georgetown, 30 km west to Somerset Creek, north to within 3 km of "Ironhurst" homestead, and south to the Mount Sullivan area. Numerous small bodies and apophyses surround the two main areas, extending as far north as the Yataga Granodiorite; there are none east of the Newcastle Range. Rocks tentatively correlated with the Forsayth Granite occur in the Cumberland Range area about 8 km north of "Green Hills" outstation.|16-MAY-23
6827|Forsayth Granite|Lithology|Grey, locally pink, leucocratic to melanocratic biotite granite with minor muscovite (mainly secondary) locally. The granite is equigranular to porphyritic, the latter variety having feldspar megacrysts 2 to 7 cm long, and is commonly foliated; grey, locally foliated, muscovite-biotite leucogranite which is equigranular to porphyritic (feldspar megacrysts up to 2 cm long); minor dark grey biotite microtonalite. Some varieties of muscovite-biotite granite cropping out in the Cumberland Mine area west of Georgetown (Forest Home 1:100 000 Sheet area) but absent from the type area are included in the unit because of their close spatial relationships to and/or gradational contacts with muscovite-biotite granite in the type area.|16-MAY-23
6827|Forsayth Granite|Relationships and boundaries|Intrudes Robertson River Metamorphics, Cobbold Dolerite and probably Einasleigh Metamorphics; contact metamorphic effects are slight. The Forsayth granite is intruded by the Digger Creek Granite; relationships with other Proterozoic granites are not known with certainty, although it is believed that the Forsayth Granite is younger than the Mistletoe and Lighthouse Granites.|16-MAY-23
6827|Forsayth Granite|Age reasons|Probably Middle Proterozoic. Preliminary isotope data suggest an age of about 1500 million years (L.P. Black, pers. Comm.).|16-MAY-23
6827|Forsayth Granite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
6827|Forsayth Granite|Status|1|16-MAY-23
27288|Furry Hoop Member|Name source|Furry Hoop Creek, a tributary of the Clarke River.|16-MAY-23
27288|Furry Hoop Member|Unit history|Previously part of the Clarke River Formation (now Group) (White, 1959).|16-MAY-23
27288|Furry Hoop Member|Type section locality|The holostratotype of the Furry Hoop Member (approximately 320 m thick) is located between GR 960516 (base) and 951515 (top). Most of the section consists of fine-grained, red-green, micaceous sandstone/siltstone with rare conglomerate intervals. These features combined with the abundance of carbonate material in these rocks distinguish the member from the rest of the Lyall Formation.|16-MAY-23
27288|Furry Hoop Member|Extent|The member has been mapped in the centre of the Clarke Rivr Basin, mainly around a domal structure north of the junction of the Clarke River with Keppel Creek South, and extending northeast in a thin belt for about 12 km. The member is likely to be represented elsewhere in the basin, but has not yet been mapped out.|16-MAY-23
27288|Furry Hoop Member|Thickness range|In the type section the unit is approximately 320 m thick, but elsewhere it ranges from 100 to 150 m (in the west of the basin) to 260 to 320 m (in the east), and thins to the north.|16-MAY-23
27288|Furry Hoop Member|Lithology|The rock types range from shale to coarse-grained sandstone to conglomerate, tuff and limestone. The rocks are characteristically red or green. The coarser sandstones contain small-scale cross-stratification, scour-and-fill structures and channel development. In contrast, the very fine-grained sandstones and siltstones, although well laminated, have few other sedimentary structures. Sporadic deposits of bimodal conglomerate contain jasper, argillite, quartz, quartzite and acid volcanic fragments in a coarse volcanolithic matrix. Jasper occurs in the member in several forms apart from pebbles in conglomerate; namely, as massive bands and as jasper fragments/sinuous bodies in calcareous, volcanolithic sandstone.|16-MAY-23
27288|Furry Hoop Member|Relationships and boundaries|The Furry Hoop Member is part of the Lyall Formation, and locally directly overlies the Venetia Formation (with probable disconformity), which is distinguished by the lack of acid volcanic components and the absence of the red-green colour typical of the Furry Hoop Member; elsewhere it is underlain by other sedimentary rocks of the Lyall Formation (mainly volcanolithic sandstone and conglomerate). The Furry Hoop Member is characterised by relatively flat, low relief. It crops out poorly and is covered by a veneer of alluvium in much of the area.|16-MAY-23
27288|Furry Hoop Member|Age reasons|Late Visean (Jell & Playford, in press).|16-MAY-23
83549|Galah Tuff Bed|Name source|This distinctive tuff horizon in the Betts Creek beds is named for the parish of Galah, which covers the northern section of Porcupine Gorge where the type section is located.|16-MAY-23
83549|Galah Tuff Bed|Type section locality|The type section is recognised within a 10 m thick succession of medium- to very coarse-grained quartzose sandstone in the uppermost exposures of the Betts Creek beds, ~2 km NNE of the base of the Pyramid Trail, approximately 300 m north of the Pyramid in Porcupine Gorge National Park, ~63 km northeast of the town of Hughenden, North Queensland, Australia (WGS84 20deg19'58.22"S
144deg28'15.45"E).|16-MAY-23
83549|Galah Tuff Bed|Extent|The Galah Tuff Bed is confined to outcrop exposures in Porcupine Gorge National Park in North
Queensland, observable in lateral extent for ~80 m in the cliff face. While a similar stratigraphic
interval was intercepted in drill core GSQ Hughenden 6, no tuff horizon was recorded. However, it is
notable that ~3 m of core was not recovered from this bore traversing the boundary between the Betts Creek beds and Porcupine Gorge Formation, and this may have contained the Galah Tuff Bed.
|16-MAY-23
83549|Galah Tuff Bed|Thickness range|In the type section, the Galah Tuff Bed attains a maximum thickness of 1.5 m but averages 0.5 m.|16-MAY-23
83549|Galah Tuff Bed|Lithology|The Galah Tuff Bed is white, porphyritic, and typically internally massive. It contains rounded
phenocrysts of coarse-grained quartz clasts and clay clasts that range in size from 0.2-3.0 mm but are generally <1 mm. These phenocrysts constitute ~5?10% of the tuff and are evenly distributed within a very fine-grained matrix. The clay clasts are likely the result of feldspar weathering and give a soapy feel to the rocks. Based on this grain size and distribution, the Galah Tuff Bed is classified as a volcanic ash-fall tuff.|16-MAY-23
83549|Galah Tuff Bed|Relationships and boundaries|The Galah Tuff Bed is highly limited in extent in Porcupine Gorge, where it is situated ~5 m below the
top of the Betts Creek beds. Based on the age assignment of 251.9 +/- 3 Ma, the Galah Tuff Bed is
roughly equivalent in age to the Gibraltar Ignimbrite (251.6 +/- 3.2 Ma; Campbell et al., 2015), as well as the Yarrabee Tuff (252.54 +/- 0.04 Ma ? 253.07 +/- 0.22 Ma; Phillips et al., 2018).|16-MAY-23
83549|Galah Tuff Bed|Age reasons|LA-ICP-MS zircon geochronology provided an age of 251.9 +/- 3.0 Ma (latest Permian-earliest Triassic) for the Galah Tuff Bed. This confirms the late Permian assignation of the Betts Creek beds and provides a robust stratigraphic marker for the overlying Triassic strata.
|16-MAY-23
83549|Galah Tuff Bed|Defn author|Todd et al. (2022).|16-MAY-23
83549|Galah Tuff Bed|References|Campbell, M., Rosenbaum, G., Shaanan, U., Fielding, C. R., & Allen, C. (2015). The tectonic
significance of lower Permian successions in the Texas Orocline (Eastern Australia). Australian
Journal of Earth Sciences, 62, 789?806. https://doi.org/10.1080/08120099.2015.1111259  **Gehrels, G. (2012). Detrital Zircon U-Pb Geochronology: Current Methods and New Opportunities. In C. Busby & A. Azor (Eds.), Tectonics of Sedimentary Basins (pp. 45?62). John Wiley & Sons.
https://doi.org/10.1002/9781444347166.ch2  **Phillips, L. J., Crowley, J. L., Mantle, D. J., Esterle, J. S., Nicoll, R. S., McKellar, J. L., & Wheeler, A. (2018). U-Pb geochronology and palynology from Lopingian (upper Permian) coal measure strata of the Galilee Basin, Queensland, Australia. Australian Journal of Earth Sciences, 65 (2), 153?173. https://doi.org/10.1080/08120099.2018.1418431   **Stacey, J. S., & Kramers, J. D. (1975). Approximation of terrestrial lead isotope evolution by a two-stage model. Earth and Planetary Science Letters, 26(2), 207?221. https://doi.org/10.1016/0012-821x(75)90088-6 In Appendix 3|16-MAY-23
27411|Gallangowan Granodiorite|Name source|Gallangowan Forestry Settlement, grid reference 54517169, Gympie 1:250 000 Sheet area.|16-MAY-23
27411|Gallangowan Granodiorite|Type section locality|Road cuttings on entrance road to Gallangowan settlement, grid reference 54457157.|16-MAY-23
27411|Gallangowan Granodiorite|Extent|The unit crops out over 15 km2 in the central portion of the Gympie 1:250 000 Sheet area (SG 56-10) near the headwaters of Butcher Creek in the Brisbane Range.|16-MAY-23
27411|Gallangowan Granodiorite|Lithology|Coarse-grained, grey, biotite granodiorite.|16-MAY-23
27411|Gallangowan Granodiorite|Relationships and boundaries|Intrudes undifferentiated Palaeozoic metamorphics, and is intruded by the Permo-Triassic Kingaham Creek granodiorite.|16-MAY-23
27411|Gallangowan Granodiorite|Age reasons|A K/Ar radiometric age of 313+/-10 m.y. (Late Carboniferous) was obtained by McNaughton (1973).|16-MAY-23
27411|Gallangowan Granodiorite|Proposed publication|Report of the Geological Survey of Queensland|16-MAY-23
27411|Gallangowan Granodiorite|Name first published by|Geological Survey of Queensland 1975.|16-MAY-23
24282|Garden Creek Porphyry|Name source|Named after Garden Creek, which flows SE to join Wills Creek E of Dajarra, Dajarra 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24282|Garden Creek Porphyry|Unit history|Previously mapped as Kalkadoon Granite (e.g. Carter & Opik, 1963), which pre-dates the Mount Guide Quartzite.|16-MAY-23
24282|Garden Creek Porphyry|Type section locality|5.5 km NE of Dajarra, at GR 503039, Dajarra 1:100 000 Sheet area. Here the Garden Creek Porphyry, consisting of porphyritic microgranite, is exposed mainly as small spheroidal boulders on a low ridge, flanked by narrow depressions developed on poorly exposed amphibolitic metadolerite, between higher strike ridges of Mount Guide Quartzite to the east and west.|16-MAY-23
24282|Garden Creek Porphyry|Extent|Forms N-trending band up to 250 m wide within the range of Mount Guide Quartzite N of Dajarra; extends for 37 km from GR 501035, NW Dajarra 1:100 000 Sheet area, to GR 516407, SW Duchess 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24282|Garden Creek Porphyry|Thickness range|0-250 m.|16-MAY-23
24282|Garden Creek Porphyry|Lithology|Massive to locally sheared pink to grey microgranite containing euhedral to subhedral plagioclase and K-feldspar phenocrysts, some more than 1 cm across, and smaller rounded phenocrysts of glassy quartz; also contains small dark biotite-rich inclusions.|16-MAY-23
24282|Garden Creek Porphyry|Relationships and boundaries|Intrudes the Mount Guide Quartzite more or less concordantly; commonly flanked by metadolerite.|16-MAY-23
24282|Garden Creek Porphyry|Age reasons|Proterozoic; postdates the Mount Guide Quartzite.|16-MAY-23
24282|Garden Creek Porphyry|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
24282|Garden Creek Porphyry|Comments|Remarks: The unit forms a steeply dipping intrusive tabular body which may represent the central part of a composite sheet.|16-MAY-23
24282|Garden Creek Porphyry|Defn Reference|82/22920|16-MAY-23
24282|Garden Creek Porphyry|First Reference|81/21497|16-MAY-23
24282|Garden Creek Porphyry|Proposer|Blake D.H.|16-MAY-23
7050|Gatton Sandstone|Name source|The name is derived from the township of Gatton in the Laidley Valley, Ipswich 1:250 000 Sheet area, Queensland.|16-MAY-23
7050|Gatton Sandstone|Unit history|The unit was originally named Gatton Sandstone Member by McTaggart (1963).  Although the 'Blaxland Fossil Wood Conglomerate Member' of McElroy (1962) was never adequately defined it is evident that it is equivalent to the Gatton Sandstone. Although McElroy's (1962) unit name has priority, we prefer to use Gatton Sandstone because - 1. it has gained wide acceptance and is entrenched in the literature, particularly in Queensland where the Marburg Subgroup is well documented; 2) the term 'Blaxland Fossil Wood Conglomerate Member' has not been widely used or accepted, and is commonly used in a variety of ways and we prefer to avoid further confusion by redefining the formation, and retaining the name Gatton Sandstone.|16-MAY-23
7050|Gatton Sandstone|Constituents|The Calamia Member constitutes a thin unit at the base of the Gatton Sandstone and the Koreelah Conglomerate Member composes the base of the Gatton Sandstone where the formation overlaps basement rocks. A prominent thin unit near the base of the Gatton Sandstone is characterised by the abundance of large fossil wood fragments, commonly ferruginised, in a coarse grained, conglomeratic sandstone matrix. The beds occur in outcrop along the western and southern flanks of the basin and are best exposed in road cuttings on the Gwydir Highway, Bruxner Highway and on the Copmanhurst-Jackadgery road (GR MN 697.317; Grafton 1:100 000 Sheet). The thickness of this unit is estimated in the range 5 to 10 m and contains blocks and logs of fossil wood up to 20 m long and nearly 1 m in diameter. Further study of these beds may show that they constitute an important marker bed near the base of the Gatton Sandstone and deserve formal status. However definition and naming of this unit should wait until it can be shown that it forms a continuous member in the formation.|16-MAY-23
7050|Gatton Sandstone|Geomorphic expression|Mostly rounded hillslopes of low relief. No characteristic topographic features.|16-MAY-23
7050|Gatton Sandstone|Type section locality|McTaggart (1963) did not give a type section for the Gatton Sandstone Member but Gray (1975) nominated GSQ Ipswich 18 over the interval 1368.1' (417.07 m) to 2955.0' (900.7 m) as the reference section and it is here designated as the type section.|16-MAY-23
7050|Gatton Sandstone|Description at type locality|The lithological succession and thickness in the type section is shown in GSQ Ipswich 18 drill log attached. (Fig. 11). The principal rock types in the type section are - Sandstone - quartz-lithic to lithic, cross-bedded, medium to very coarse grained in multistorey fining up sequences, interspersed clasts, in white silty matrix; carbonaceous laminae, pebbly at channel bases, mostly poorly sorted and bedded, subangular, in part feldspathic, occasional volcanic clasts and coal spars, clay pellets, in part finely micaceous, parallel laminated, cross-laminated and ripple cross-laminated, common fossil wood fragments.  Conglomerate - pebble and cobble, mostly at base of channel sands, clasts of jasper, quartzites, volcanics metasediments; very coarse grained quartzose/quartz/lithic/feldspathic matrix.  Siltstone/shale - dark grey to black, wavy irregular bedding, possible relict soil intervals, thin interlaminae of siltstone, in part bioturbated, occasional load casts.  Coal - very thin laminae in siltstone.|16-MAY-23
7050|Gatton Sandstone|Extent|The formation is present basin wide in the Marburg Subgroup.|16-MAY-23
7050|Gatton Sandstone|Lithology|The lithology of the formation varies little throughout the basin except where it overlaps the Palaeozoic basement rocks in the west. Here the formation is much coarser grained and contains beds of conglomerate and grades downwards into thick conglomerate. This conglomerate is formally defined in this paper as the Koreelah Conglomerate Member of the Gatton Sandstone. The upper boundary of the Gatton Sandstone is marked by the change from uniform quartz-lithic and lithic-sandstone to a variable sequence of quartzose and quartz lithic sandstone, siltstone, shale and some coal of the overlying Koukandowie Formation. The lower boundary is delineated by a change in sandstone composition to clean quartz sandstone of the Ripley Road sandstone, and in places either by the base of the locally developed Koreelah Conglomerate Member, or the Calamia Member.|16-MAY-23
7050|Gatton Sandstone|Depositional environment|Predominantly low sinuosity fluvial deposits in high energy environments.|16-MAY-23
7050|Gatton Sandstone|Fossils|Fossils include wood fragments, plant remains and spores, pollen grains, and sporadic acritarchs.|16-MAY-23
7050|Gatton Sandstone|Diastems or hiatuses|Minor diastems and hiatusus are present in the formation but no major depositional breaks are recorded.|16-MAY-23
7050|Gatton Sandstone|Relationships and boundaries|Upper and lower contacts are apparently conformable, except where the formation overlaps Palaeozoic basement in which case the lower boundary is an angular unconformity. A regional unconformity separates the Gatton Sandstone from the Raceview Formation of the Woogaroo Subgroup in the southeast at the Coast and Dirty Creek Ranges.|16-MAY-23
7050|Gatton Sandstone|Identifying features|The stratigraphic position and lithology of the sequence are the main distinguishing features. The sandstone in the formation is predominantly very coarse grained, poorly sorted, quartz-lithic and lithic sandstone in channel sand bodies and minor overbank deposits. The formation commonly contains fossil wood.|16-MAY-23
7050|Gatton Sandstone|Age reasons|The formation is basal Early Jurassic in age and includes elements of palynostratigraphic assemblages C and D (de Jersey, 1976; McKellar, 1981b) and unit J1 of Evans (1963, 1966). Palynofloras of assemblage D collected from the upper part of the formation indicate a Toarcian age (McKellar, 1974; Helby et al. 1987) equivalent to assemblages from the immediate pre-oolitic ironstone sequence of the Ma Ma Creek Member (McKellar, 1981).|16-MAY-23
7050|Gatton Sandstone|Correlations|The Gatton Sandstone is correlated with part of the Evergreen Formation of the Surat Basin.|16-MAY-23
7050|Gatton Sandstone|Proposed publication|A.T. Wells et al. BMR Journal of Geology and Geophysics|16-MAY-23
7050|Gatton Sandstone|State(s)|NSW and QLD|16-MAY-23
7050|Gatton Sandstone|Status|1|16-MAY-23
23611|Gem Park Granite|Name source|Gem Park homestead at 8450-675956.   The grid reference is based on the AGD66 datum.|16-MAY-23
23611|Gem Park Granite|Geomorphic expression|The granite forms terrain of low to moderate relief and is poorly exposed. On Landsat 5 TM 1-4-7 (BGR) images, the Gem Park Granite is represented by cleared areas with a yellow-orange hue. On geophysical images, magnetic response is low; the K counts are moderate-high, Th counts are generally moderate, and U counts are usually moderate to high.|16-MAY-23
23611|Gem Park Granite|Type section locality|At 8450-596978, 4.9 km southeast of Silver Hills homestead. The outcrop consists of foliated, cream to pink, fine to coarse-grained garnet-muscovite-biotite granite.  The grid reference is based on the AGD66 datum.|16-MAY-23
23611|Gem Park Granite|Description at type locality|The outcrop consists of foliated, cream to pink, fine to coarse-grained garnet-muscovite-biotite granite.|16-MAY-23
23611|Gem Park Granite|Extent|The Gem Park Granite crops out as elongate bodies in a south-southeast trending belt between Rubyvale and the Capricorn Highway. The two largest bodies are south of Retreat Creek, and are up to 8 km long by 2 km wide, separated by a narrow belt of Bathampton Metamorphics. Other areas assigned to the Gem Park Granite, partly for convenience, are smaller narrow, linear bodies up to 4 km long, intruding the metamorphic rocks farther north near Rubyvale and Reward.|16-MAY-23
23611|Gem Park Granite|Lithology|Cream to pink and grey, strongly foliated and locally mylonitised, muscovite and muscovite-biotite granite.  The easternmost of the two main bodies is the most strongly deformed, particularly along its western contact, where a zone of intense foliation and mylonitisation up to 400 m wide is developed.  The bodies in the Rubyvale-Reward area are mostly strongly foliated two-mica granite and commonly have a strong, shallowly plunging stretching lineation.|16-MAY-23
23611|Gem Park Granite|Relationships and boundaries|Contacts between the Gem Park Granite and the Anakie Metamorphic Group are complex. Increasingly abundant screens of metamorphic rocks in the granite pass out into metamorphic rocks that contain abundant dykes and veins of leucogranite and pegmatite.  The Gem Park Granite is intruded by components of the Retreat Batholith, including the Mount Newsome Granodiorite, Whitdale Granodiorite, Keilambete Tonalite and unassigned granodiorite bodies. The Late Devonian to Early Carboniferous Silver Hills Volcanics and sedimentary rocks of the Drummond Basin unconformably overlie the Gem Park Granite.|16-MAY-23
23611|Gem Park Granite|Age reasons|The age is uncertain, but may be Cambrian. The strong foliation in the smaller bodies is parallel to that in the adjacent Anakie Metamorphic Group, suggesting that the two units were deformed together. The age of the deformation and metamorphism is probably Cambrian (Withnall & others, 1993). The Gem Park Granite is S-type and was possibly generated during the metamorphism.|16-MAY-23
23611|Gem Park Granite|References|WITHNALL, I.W., BLAKE, P.R., CROUCH, S.B.S., TENISON-WOODS, K., HAYWARD, M. & HUTTON, L.J., 1993: Geological mapping of the southern Anakie Inlier, central Queensland - progress report. Queensland Government Mining Journal, 94.|16-MAY-23
36985|Gilla Volcanics|Unit history|The Gilla Volcanics is a new name for the Gilla Andesite and has been assigned to the unit to better reflect the wide range of volcanic and volcaniclastic rock types present.  Gradwell (1949) first named it the Gilla Andesite after noting its dominantly andesitic composition.  Further studies by Murphy and others (1976), Barrie (1982), Brown (1982), Topping (1985) and Wherle (1995) indicated the unit is composed of volcanic and volcaniclastic rock types ranging from intermediate to acid in composition.  Six sub-units have been identified within the unit and are tabulated below (Table 12).Table 12:  Units of the Gilla Volcanics (as follows): PRgl	Undifferentiated intermediate to acid volcanics, PRgla Dark grey aphyric to porphyritic andesite, minor rhyolite and dacite, some intercalated volcaniclastics, PRgld Rhyodacite-dacite, PRglp Feldspar porphyritic dacite, PRglr	 Flow banded rhyolite, rhyolitic breccia and conglomerate, PRgls Volcaniclastic sediments, PRglt	Dacitic-rhyolitic tuff.|16-MAY-23
36985|Gilla Volcanics|Geomorphic expression|The Gilla Volcanics generally form rolling grassy hills but also include small areas of thick native and plantation forest.  Elevations range from approximately 320m to 550m.|16-MAY-23
36985|Gilla Volcanics|Extent|Exposure of the Gilla Volcanics occurs on the south-western margin of NANANGO and south-eastern KINGAROY.  It consists of a single large (~55km2) subdivided body (PRgla PRgld PRglr PRgls PRglt PRglp) centred approximately 10km north-west of Blackbutt township and three smaller undivided bodies (PRgl) eight to eleven kilometres south and south-west of the township.  Sub-unit PRgla is the largest sub-unit and makes up the bulk of the subdivided body.  The rhyodacite-dacite sub-unit (PRgld) is exposed over approximately 1km2 and is located on the eastern margin of the subdivided body east of Cooyar Creek.  Sub-unit PRglr has the second largest exposure and covers a total area of approximately 8km2.  Three discrete bodies have been identified with the largest exposed over 5km2 and located approximately 12km south of Nanango.  Of the other two exposures, one forms an arcuate body of approximately 2.5km2 south of the previously mentioned exposure.  The smallest body of this sub-unit (0.5km2) is west of Cooyar Creek, approximately 9km north-north-west of Blackbutt.  Feldspar porphyritic dacite (PRglp) is present adjacent to the rhyodacite-dacite unit and covers an area of approximately 1km2.Volcanogenic sedimentary deposits (PRgls) of sandstones, conglomerates and breccias make up only a small percentage of the Gilla Volcanics (Wherle, 1995).  Although they are often intercalated with volcanic flows or pyroclastic deposits, an area (0.6km2) of volcanogenic sediments has been identified on the northern margin of the Gilla Volcanics.Pyroclastic rocks, similar to the volcanogenic sedimentary deposits, are often intercalated with the primary volcanic flows.  Some areas of pyroclastic deposits (PRglt) are large enough to be mapped as separate sub-units and have been identified in the northern (~1km2), central (0.2km2) and southern (0.8km2) parts of the main body of the Gilla Volcanics.  Wherle (1995) estimated as much as 15% of the total volume, of the southern area of the main body, is pyroclastic deposits.  Five areas of undivided Gilla Volcanics (PRgl) have been identified.  The major area is located on the southern margin of the Taromeo Igneous Complex (PRgmgd3) and covers an area of approximately 4.5km2.  Two other bodies are present close by, one 4km to the east (0.5km2) and one 2km to the north-west (0.2km2).  The final two small bodies are located approximately 2km south of Mount Mellera, and approximately 9km north of Blackbutt.|16-MAY-23
36985|Gilla Volcanics|Lithology|Gradwell (1949) described andesite, andesitic and rhyolitic agglomerate, feldspar porphyry and rhyolite from the Gilla Volcanics.  Rock types noted by Wherle (1995) include andesite, rhyolite, flow-banded rhyolite, dacite and feldspar porphyry.  He also observed rapid and complex changes in the rock types along with abrupt facies changes, most typically from andesite flows to volcaniclastic deposits.  Although the contacts are often obscured relationships can be observed along the roughly flat lying creek exposures. Dennis (1974) described the rocks south of the Taromeo Igneous Complex (Rgmgd1) and north of Emu Creek, as a series of acid volcanics (PRgl?) in contact with the southern boundary of the granodiorite.  He summarised the unit as being made up of rhyolites, dacites, andesite, andesitic tuffs and other tuffaceous rocks.  Rocks close to the contact with the granodiorite have been recrystallised and may show disseminated pyrite.The rhyolites range in colour from light green to grey-brown and contain feldspar phenocrysts to 3mm.  In some of the flow-banded rhyolites, the feldspar phenocrysts are roughly aligned to the flow bands.  The meta-rhyolite is light coloured and contains red weathered phenocrysts of feldspar to 2mm.  The dacites are generally light-coloured, porphyritic, and contain feldspar and mafic phenocrysts to 4mm.   Andesites range from sparsely to abundantly porphyritic with a weakly to moderately well developed trachytic texture.  Andesitic tuffs occur with feldspar crystals to 3mm in a fine dark grey groundmass............Sub-unit PRgla is composed primarily of andesitic flows with lesser intercalated andesitic to rhylolitic volcaniclastics..........An example of a flow-banded rhyolite lava within PRgla is present beside a track on the side of a hill at AMG 406090 7029636.  In outcrop the rock shows well-defined contorted flow bands with raised finer grained resistant bands................Intercalated with some of the flows are andesitic to rhyolitic pyroclastics.  At AMG 404581 7035149 a layer of andesitic welded rheomorphic ignimbrite occurs above a sparsely porphyritic andesite lava flow................Sub-unit PRglp is exposed north of sub-unit PRgld and is composed of coarse feldspar porphyritic andesite-dacite............Sub-unit PRglr is composed of flow-banded rhyolite, rhyolitic breccia and conglomerate.........Sub-unit PRgls comprises bedded volcanogenic sandstones, conglomerates and breccias............Rocks of sub-unit PRglt show a range of compositions and textures (Wherle, 1995).  They are often difficult to distinguish from epiclastic deposits in the field and thin section analysis is generally needed to confirm their classification......An exposure in the southern part of the Gilla Volcanics, at AMG 404400 7028500, shows large unsorted andesitic blocks in an ash matrix.  Pyroclastic flows have been identified further north in Yarraman Creek, stratigraphically below andesite lava flows (Wherle, 1995).|16-MAY-23
36985|Gilla Volcanics|Relationships and boundaries|The Gilla Volcanics unconformably overlie the Devonian-Carboniferous Maronghi Creek beds and Sugarloaf Metamorphics.  Hornfelsing of the volcanics indicate they have been intruded by at least part of the Permo-Triassic Taromeo Igneous Complex.  Finally, Tertiary Main Range Volcanics have overlain the unit.|16-MAY-23
36985|Gilla Volcanics|Structure and Metamorphism|The Gilla Volcanics probably represents remnants of a collapsed caldera.  Bedding of the volcanic flows and volcaniclastic beds dip generally towards the centre of the main body consistent with a collapsed caldera model.|16-MAY-23
36985|Gilla Volcanics|Age reasons|Gradwell (1949) suggested a Permian age for the Gilla Volcanics on the basis of lithological and stratigraphic correlation with similar volcanic units.  Murphy and others (1976) believed the distribution and composition of the volcanics were consistent with being co-magmatic with the Taromeo Igneous Complex.  Wherle (1995) agreed and showed the Gilla Volcanics had similar normalised REE patterns to the Taromeo Igneous Complex.  He suggested they are genetically related but have formed from different parental magma.  Geochemical samples of the Gilla Volcanics plot with the younger phases of the Taromeo Igneous Complex on TAS diagrams indicating a similar source.|16-MAY-23
36985|Gilla Volcanics|Geophysical Expression|Airborne ternary radiometric images of the Gilla Volcanics give an overall mottled white-green-purple signature, though it has a range of responses.  It is similar to parts of the Taromeo Igneous Complex though it lacks the yellow-orange tones of that unit.  The body of the unit adjacent to the southernmost exposure of the Taromeo Igneous Complex has a signature showing higher levels of red, indicating relatively higher levels of potassium.No unique pattern attributable to the Gilla Volcanics was distinguished on the airborne magnetic image.  The volcanics have an overall low magnetic response with no significant contrast to surrounding units.  Hand-held magnetic susceptibility readings gave values ranging from 10-4000 x 10-5 SI units for andesite and 0-500 x 10-5 SI units for rhyolite-dacite.  Although individual andesites gave relatively high magnetic susceptibility readings the overall low volumes of rock, strong response from the underlying Taromeo Igneous Complex and patchy exposure of outcrop failed to give the unit a characteristic signature.|16-MAY-23
36985|Gilla Volcanics|References|BARRIE, B.,1982,Geology of the central Cooyar Creek district, Blackbutt, Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology",Regional Geology,Nanango.BROWN, G.C.,1982,Calc-alkaline intrusive rocks: their diversity, evolution, and relation to volcanic arcs In: Thorpe, R.S. (editor), Andesites. Orogenic Andesites and Related Rocks. A Wiley-Interscience Publication.  John Wiley and Sons,Geochemistry, Tectonics.CAS R.A.F. & WRIGHT J.V.  ,1987,Volcanic Successions.  Modern and ancient. A geological approach to processes, products and successions. Chapman and Hall,Volcanic Rocks, Rock Classifications.DENNIS,1974,The geology of the Googa Googa Creek area, south of Blackbutt, south-east Queensland.","Unpublished student thesis, Darling Downs Institute of Advanced Education, Toowoomba.FISHER, ? 1979..............GRADWELL, R.,1949,The petrology of the eruptive rocks of the Yarraman district. Papers, Department of Geology, University of Queensland. 3(8).MCPHIE J., DOYLE M. & ALLEN R.,1993, Volcanic Textures. AQ guide to the interpretation and textures of volcanic rocks. Centre for Ore Deposits and Exploration Studies. University of Tasmania. Volcanic Rocks.MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.ROBERTSON, S.D.,1987,The geology of Yarraman, Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology.TOPPING, T.K.,1985, The geology of the Talona Creek, Nanango, Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology.WEHRLE, A.C.1995,The Complexity of Granitoid Pulses that Comprise the Taromeo Tonalite.,"Honours Thesis, School of Natural Resource Sciences, Queensland University of Technology.|16-MAY-23
7245|Gin Creek Granite|Name source|Named after Gin Creek, a tributary of the Mort River, and Gin Creek Bore (at GR 378988), Mount Merlin 1:100 000 Sheet area, Duchess 1:250 000 Sheet area. Gin Creek and its tributaries drain much of the outcrop area of the unit.|16-MAY-23
7245|Gin Creek Granite|Unit history|Named Gin Creek Granite and briefly described in an unpublished report by White (BMR Record 1957/94), and referred to as Gin Creek Granite by Brooks (1960). Like all other granites in the eastern part of the Duchess 1:250 000 Sheet area, it was mapped as Williams Granite by Carter & Opik (1963).|16-MAY-23
7245|Gin Creek Granite|Type section locality|Low hilly country 4 km NE of Gin Creek Bore, in vicinity of GR 412022. The three main granitic types making up the unit are exposed in this area: mainly foliated xenolithic biotite granite and fine-grained to pegmatitic leucogranite in the western part, and mainly non-foliated biotite granite containing feldspar phenocrysts up to 5 cm across in the eastern part.|16-MAY-23
7245|Gin Creek Granite|Extent|Restricted to E part of Mount Merlin 1:100 000 Sheet area. Main outcrop, 24 km long (N to S) and up to 6 km wide, lies E of Gin Creek bore. A few small outcrops are present to the west.|16-MAY-23
7245|Gin Creek Granite|Lithology|Main rock types exposed are medium to coarse-grained and locally porphyritic biotite granite, fine to coarse-grained, xenolithic, commonly porphyritic, weakly foliated to gneissic biotite granite (which predominates on the W and N sides of the main outcrop); and fine-grained to pegmatitic leucogranite containing tourmaline and muscovite. Minor fine-grained biotite granite, aplite and greisen are also present.|16-MAY-23
7245|Gin Creek Granite|Relationships and boundaries|Gin Creek Granite intrudes Double Crossing Metamorphics (new name), Answer Slate, Staveley Formation, Kuridala Formation and metadolerite, and is overlain by flat-lying Mesozoic sediments. Tourmaline-muscovite granite locally cuts the other two main granitic types.|16-MAY-23
7245|Gin Creek Granite|Age reasons|Proterozoic.|16-MAY-23
7245|Gin Creek Granite|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
7245|Gin Creek Granite|Comments|Remarks: Gin Creek Granite consists of three spacially associated types of granite, and may represent three or more separate intrusions. It forms part of the Williams Batholith (new structural term), which comprises all granites previously mapped as Williams Granite, together with the Wimberu Granite.|16-MAY-23
7245|Gin Creek Granite|Defn Reference|82/22920|16-MAY-23
79122|Glanmire Conglomerate Member|Name source|This unit is crossed by Glanmire Gully at MGA 468100mE; 7101440mN and Glanmire Street at MGA 467250mE; 7103450mN, from which the name is derived.|16-MAY-23
79122|Glanmire Conglomerate Member|Unit history|Equates with Dunstan's (1911) Conglomerate Group;  Included in Runnegar & Ferguson's (1969) original definition as conglomerate at the top of Rammutt Rd, Chatsworth.  Termed Top conglomerate in GEGM's informal stratigraphy used at Monkland Mine, implying its position at the top of the Highbury-Rammutt sequence, capped by the South Curra Limestone. Subsequently referred to by Cranfield (1999), Sivell & Arnold (1999), Sivell & McCulloch (2001), Li & others (2015).|16-MAY-23
79122|Glanmire Conglomerate Member|Type section locality|A cutting on the Heritage rail line at the southern end of Gympie railway station, between the junction of Mellor St and Station Rd.  MGA 467095mE; 7103390mN. Lat: -26°11'19"  Long: 152°40'14". Reference sections: BHP drill hole G023: 3-31 m at north end of Monkland Mine.  GEGM drill hole G137: 181-189 m at Monkland Mine. Core held at Zillmere core library [2016].|16-MAY-23
79122|Glanmire Conglomerate Member|Description at type locality|Polymictic conglomerate is exposed in a cutting on the Heritage rail line at the southern end of Gympie railway station (Photograph 6a), between the junction of Mellor Street and Station Road (QFG8364; MGA 467100mE; 7103390mN). It contains well rounded volcanic clasts, 1-30 cm in diameter (Photograph 6b). Runnegar & Ferguson¿s (1969) original definition along Rammutt Road, Chatsworth includes poorly exposed, matrix supported volcanic conglomerate at MGA 462155mE; 7109040mN (QFG8346).|16-MAY-23
79122|Glanmire Conglomerate Member|Extent|Mostly absent or up to 10 m thick in the south (Dawn & Six Mile blocks), increasing to about 20 m beneath the Curra Thrust at Monkland Mine and 15-35 m in the Partridge Graben. Thickness increases significantly to the north. In the Phoenix Block near the railway station Rands (1889) reported a thickness of 110 m which however includes significant underlying sandstone, similar to that in the Nash Clastics Member. It is particularly thick in the southern Two Mile Block, where the conglomerate and Nash Clastics member merge; conglomerate in Freeport drill hole G002 just north of the Peter and Paul Fault (MGA 465205mE, 7104930mN) is 70-90 m thick and 1.5 km further north in Freeport drill hole G005 (MGA 465265mE, 7106420mN) is 35 m thick underlain by 160 m of sandstone. Beyond G005 the northern extent of the unit is not well exposed. Cobble conglomerate outcrops and some sandstone have been traced as far north as Greenhalgh Road and have been interpreted as Glanmire Conglomerate but they could also be part of the Nash Clastics Member. West of the Laing Fault the conglomerate is widespread above the Curra Thrust, at least 100 m thick in the Pinewoods Block, 50 m in West Phoenix, and 30 m in the Sovereign Block at Butterfly.|16-MAY-23
79122|Glanmire Conglomerate Member|Thickness range|Mostly 20-35m thick but increases to over 100m in the vicinity of the industrial site west of Gympie golf course.|16-MAY-23
79122|Glanmire Conglomerate Member|Lithology|A coarse-grained, polymictic, mainly clast-supported, volcanoclastic conglomerate, consisting of well rounded, intermediate feldspar porphyry (andesite), mafic volcanic, siliceous and other clasts, commonly cobble size, ranging from 1 cm to 10 cm diameter, in rare cases up to 30 cm, in a medium to coarse sandy matrix (Photographs 7a & 7b). Gritty sandstone lenses are present, often rich in leucoxene. Locally this unit can contain strongly carbonaceous (graphitic) and pyritic lenses or breaks aligned near parallel to bedding, particularly in the Pinewoods Block.|16-MAY-23
79122|Glanmire Conglomerate Member|Relationships and boundaries|Occurs immediately below the South Curra Limestone, commonly separated by the Curra thrust (e.g. : at Monkland Mine). It appears to disconformably or unconformably overlie the rest of the Rammutt Group, particularly in the southern part of the Two Mile Block. Faunal evidence found by Waterhouse & Balfe (1987) indicates a major break below the limestone and conglomerate, adding support to the presence of an unconformity. In the Monkland Block and southern part of the Phoenix Block it is underlain by the Langton Dolerite.|16-MAY-23
79122|Glanmire Conglomerate Member|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie 12-JAN-2017.|16-MAY-23
79122|Glanmire Conglomerate Member|References|Dunstan, B., 1911: Geology map of Gympie and environs. GSQ Publ. No. 221b.  **Runnegar, B. and Ferguson, J.A. 1969: Stratigraphy of the Permian and Lower Triassic marine sediments of the Gympie District, Queensland.  Pap Dept Geol Univ Qld. **Cranfield, L.C., 1999: Gympie Special Sheet 9445, Part 9545, Queensland 1:100,000 Geological Map Commentary. Queensland Department of Mines and Energy, Brisbane.  **Sivell, W.J. and Arnold, G.O. 1999: Geochemical and volcanic stratigraphy of a segment of an island arc - Gondwana rim accretion zone, Gympie Province, southeast Queensland.  In Flood, P.G. (Editor): Regional Geology, Tectonics and Metallogenesis, New England Orogen, NEO ¿99 Conference, 255-266.  **Sivell, W.J. and McCulloch, M.T. 2001: Geochemical and Nd-isotopic systematics of the Permo-Triassic Gympie Group, southeast Queensland.  Australian Journal of Earth Sciences 48, 377-394.  ** Li, P., Rosenbaum, G., Yang, J-H. and Hoy, D. 2015. Australian-derived detrital zircons in the Permian-Triassic Gympie terrane (eastern Australia): Evidence for an autochthonous origin. Tectonics, 34, 858-874.|16-MAY-23
21868|Glenroy Mill Granodiorite|Name source|Glenroy Mill south of the Flinders Highway at GR 3767 77587 in the Homestead 1:100 000 Sheet area.|16-MAY-23
21868|Glenroy Mill Granodiorite|Unit history|The Glenroy Mill Granodiorite was mapped as Ravenswood Granodiorite Complex by Wyatt & others (1971), and Clarke & Paine (1970).|16-MAY-23
21868|Glenroy Mill Granodiorite|Type section locality|The Glenroy Mill Granodiorite crops out over about 11km2 around Glenroy Mill (Figure 2). It occurs on both sides of the Flinders Highway. Much of the outcrop area is made up of red/brown soils with only poor outcrop.The Glenroy Mill Granodiorite was mapped as Ravenswood Granodiorite Complex by Wyatt & others (1971), and Clarke & Paine (1970).|16-MAY-23
21868|Glenroy Mill Granodiorite|Description at type locality|Here a medium to coarse grained hornblende granodiorite to tonalite comprises strained quartz, altered plagioclase feldspar, hornblende (possible alteration after pyroxene?), and opaques.|16-MAY-23
21868|Glenroy Mill Granodiorite|Extent|The Glenroy Mill Granodiorite crops out over about 11km2 around Glenroy Mill (Figure 2). It occurs on both sides of the Flinders Highway. Much of the outcrop area is made up of red/brown soils with only poor outcrop.|16-MAY-23
21868|Glenroy Mill Granodiorite|Lithology|Only a few fresh outcrops of the Glenroy Mill Granodiorite were found in the present survey. About 1km north of the type locality, a porphyritic biotite granodiorite comprises phenocrysts of altered plagioclase, recrystallised quartz, and glomerophyric biotite in a fine grained matrix of quartz, plagioclase, K-feldspar, biotite and opaques. Elsewhere in the unit, generally weathered medium to coarse grained biotite-hornblende granodiorite is reported (unpublished company maps).|16-MAY-23
21868|Glenroy Mill Granodiorite|Relationships and boundaries|The Glenroy Mill Granodiorite is surrounded by Tertiary and Quaternary sediments and hence its relationships to other older units are not known.|16-MAY-23
21868|Glenroy Mill Granodiorite|Age reasons|The age of the Glenroy Mill Granodiorite is not known precisely. An Ordovician age is assigned on the basis of its strained and recrystallised nature and its similarity to Ordovician granitoids in the Ravenswood Batholith (Hutton & others, 1994).|16-MAY-23
21868|Glenroy Mill Granodiorite|Comments|MAGNETIC SUSCEPTIBILITY::   The rock types at the type locality are non-magnetic. However outcrops to the north are in the range 0-150 x 10[superscript]-5 SI units.|16-MAY-23
21868|Glenroy Mill Granodiorite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
24292|Goat Creek Andesite|Name source|The name is derived from Goat Creek, which joins Nannygoat Creek, a tributary of Pleasant Creek, at GR 7461-008798.|16-MAY-23
24292|Goat Creek Andesite|Unit history|Goat Creek Andesite was previously part of the undivided "Croydon Volcanics" of Branch (1966); it was informally named 'Goat Creek andesite' and described by Mackenzie (1983).|16-MAY-23
24292|Goat Creek Andesite|Geomorphic expression|The Goat Creek Andesite is characterised by very low to flat topography with sparse vegetation cover and dark brown to red-brown soil.|16-MAY-23
24292|Goat Creek Andesite|Type section locality|The type section is along the "Tabletop"-Wallabadah outstation road, between GR 7362-396108 (base) and -395107 (top). The unit here consists of altered, amygdaloidal, sparsely porphyritic, fine-grained basaltic andesite at least 30 m, and possibly up to 100 m, thick. At its base is the poorly outcropping, white, deeply weathered Wallabadah Siltstone, and its top is marked by an abrupt transition into bouldery outcrops of massive rhyolitic ignimbrite assigned to the Parrot Camp Rhyolite, or to the Carron Rhyolite. This is the only reasonably accessible section; however, exposure is not good, and the unit is better exposed around GR 500115, on the southern side of a large inlier of volcanics near the Carron River, east of "Wallabadah" outstation. Rocks assigned to the Goat Creek Andesite are well exposed, though deeply weathered, about GR 7461-028792, between Pleasant and Nannygoat Creeks, but there is some doubt about the age of the mafic lavas in this area (see below).|16-MAY-23
24292|Goat Creek Andesite|Extent|In the Croydon 1:100 000 Sheet area, the unit crops out discontinuously in an arc from near the Tabletop-Wallabadah road to the eastern border of the sheet area. Other small bodies, each less than 0.5 km2, crop out at GR 7361-537095, -502111, -513113 and -539137, in the area south and southwest of Round Hole Hut. In the Gilbert River 1:100 000 Sheet area, the unit crops out discontinuously over a wide area in the valleys of Goat, Nannygoat, Bullseye and Black Soil Creeks, around GR 7461-000780.|16-MAY-23
24292|Goat Creek Andesite|Thickness range|In the type area, the unit is at least 30 m, and possibly up to 100 m thick; its thickness in the Pleasant Creek-Nannygoat Creek area is unknown.|16-MAY-23
24292|Goat Creek Andesite|Lithology|The Goat Creek Andesite consists of variably amygdaloidal, sparsely plagioclase-phyric, basaltic andesite to andesite. It is intensely altered (spilitised), and the amygdales commonly contain agate, up to 5 cm in diameter.|16-MAY-23
24292|Goat Creek Andesite|Relationships and boundaries|Goat Creek Andesite conformably overlies Wallabadah Siltstone, and is conformably or paraconformably overlain by B Creek Rhyolite or Carron Rhyolite in the type area and nearby areas. It is also unconformably overlain by Jurassic-Cretaceous Gilbert River Formation, Pliocene-Pleistocene Claraville Formation, and other Tertiary to Quaternary sediments in these areas. In the Pleasant Creek area, rocks assigned to the Goat Creek Andesite are apparently confined to fault-bounded depressions, faulted against B Creek, Carron and Idalia Rhyolites, and overlain by Permian Bullseye Rhyolite (Mackenzie, 1983); they are also unconformably overlain by Mesozoic Gilbert River Formation and Quaternary sediments. In parts of this area the mafic rocks appear to overlie the Croydon Volcanic Group, and, perhaps, the Inorunie Group, and may be, at least in part, equivalent to the Permian McFarlanes Andesite (Mackenzie, 1983). However, basaltic to andesitic rocks intersected in a drill hole at GR 7461-043759 (J. Fawckner, pers. comm., 1982) are petrographically and chemically unlike the McFarlanes Andesite (Mackenzie, in prep, and are petrographically similar to Goat Creek Andesite in the Wallabadah-Carron River area, and to andesitic rocks in the B Creek Rhyolite.|16-MAY-23
24292|Goat Creek Andesite|Age reasons|In the type area the unit is of Middle Proterozoic age, as for the remainder of the Croydon Volcanic Group. However, some of the basaltic to andesitic rocks in the Nannygoat Creek-Pleasant Creek area assigned to the Goat Creek Andesite by Mackenzie & others (1981, 1983) and Mackenzie (1983) are probably Permian. More field and laboratory data would be required to properly resolve this issue.|16-MAY-23
24292|Goat Creek Andesite|Defn author|Mackenzie D.E., Henderson G.A.M., Warnick J.V., Bain J.H.C., 1985. 86/25125. Mention Map legend.|16-MAY-23
24292|Goat Creek Andesite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24292|Goat Creek Andesite|Proposer|Mackenzie D.E., Warnick J.V., Henderson G.A.M.|16-MAY-23
35065|Goldsborough Granodiorite|Name source|Goldsborough homestead, located on the Cape River at GR 2921 77509.  The gris reference is based on the AGD66 datum.|16-MAY-23
35065|Goldsborough Granodiorite|Unit history|The Goldsborough Granodiorite was previously included in the Lolworth Igneous Complex by Paine & others (1971) and Vine & Paine (1974).|16-MAY-23
35065|Goldsborough Granodiorite|Type section locality|In Reedy Creek about 3km from its junction with the Cape River at GR 3068 77492 in the Lolworth 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
35065|Goldsborough Granodiorite|Description at type locality|Here, a grey, medium grained, rarely porphyritic hornblende-biotite granite to granodiorite crops out. It comprises quartz, large poikilitic K-feldspar, plagioclase, hornblende, biotite with minor sphene, opaques, apatite, epidote and zircon. Magnetic susceptibilities at the type locality are 435-1016 x 10[superscript]-5 SI units.|16-MAY-23
35065|Goldsborough Granodiorite|Lithology|Most of the area of outcrop of the Goldsborough Granodiorite is deeply weathered hornblende-biotite granitoid. The type locality was the freshest part of the pluton observed.|16-MAY-23
35065|Goldsborough Granodiorite|Relationships and boundaries|The Goldsborough Granodiorite appears to be intruded by the Dillons Knob Granite, and appears to be faulted, on both sides, against the Fat Hen Creek Complex and Cape River Metamorphics. Its relationship to the Davey Creek Granite and the Mount Elvan Granite is unclear.|16-MAY-23
35065|Goldsborough Granodiorite|Age reasons|The age of the Goldsborough Granodiorite is uncertain. An age of Late Silurian is assigned because of its similarity to the Hodgon Granodiorite.|16-MAY-23
35065|Goldsborough Granodiorite|Comments|MAGNETIC SUSCEPTIBILITY::  Only a few outcrops of the Goldsborough Granodiorite were studied in the current survey. All magnetic susceptibilities were in the range 267-1016 x 10[superscript]-5 SI units, averaging 500-700 x 10[superscript]-5 SI units.|16-MAY-23
35065|Goldsborough Granodiorite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
24295|Gongora Granodiorite|Name source|Parish of Gongora, County of Lang, within whicha rea the pluton is exposed.|16-MAY-23
24295|Gongora Granodiorite|Unit history|Tentatively assigned by Branch (1966) to the Prestwood Microgranite, although Branch states that this is only per airphoto-interpretation, and the intrusion could be (to paraphrase Branch) an outlier of the Forsayth Batholith.|16-MAY-23
24295|Gongora Granodiorite|Geomorphic expression|The otherwise very subdued topography of the pluton is dominated by its capping of Hempstead Sandstone, which is intricately dissected to form a shape like a hand with fingers spread.|16-MAY-23
24295|Gongora Granodiorite|Type section locality|The northern-northwestern end of the pluton, near the major eastern branch of Stockyard Creek (about GR 7560-365400).|16-MAY-23
24295|Gongora Granodiorite|Extent|The Gongora pluton is elliptical, or, more accurately, egg-shaped, with the ends of the long axis at GR 7560-377409 and -380317, and the ends of the short axis at -349360 and -407360. The area of the pluton is about 175 km2.|16-MAY-23
24295|Gongora Granodiorite|Lithology|Medium to coarse-grained biotite granodiorite with abundant deep yellow-brown biotite and semi-poikilitic orthoclase and quartz; complexly twinned and strongly zoned plagioclase. Porphyritic to strongly porphyritic in places near margins.|16-MAY-23
24295|Gongora Granodiorite|Relationships and boundaries|Intrudes Robertson River, Townley, and Heliman Formations, and is partly overlain by Hampstead Sandstone. The pluton has a contact metamorphic aureole about 200 m wide.|16-MAY-23
24295|Gongora Granodiorite|Age reasons|Probably mid-Proterozoic. Intrudes rocks that have been affected by metamorphic events dated at 1570+/-30 m.y. and 1470+/-20 m.y., but does not appear to have been affected by these events. Similar to the Forest Home Granodiorite which is at least 1265 m.y. old. Overlain by Jurassic sandstone.|16-MAY-23
34116|Gorge Creek Granite Complex|Name source|Gorge Creek, a tributary of the Cape River which it joins at GR 3109 77442 in the Lolworth 1:100 000 Sheet area.|16-MAY-23
34116|Gorge Creek Granite Complex|Unit history|The Gorge Creek Granite Complex was previously mapped as Ravenswood Granodiorite Complex (unit ODn) on the Hughenden 1:250 000 geological map (Paine & Clarke, 1970).|16-MAY-23
34116|Gorge Creek Granite Complex|Type section locality|In Gorge Creek, from GR 3114 77462 to GR 3123 77470.  The grid references are based on the AGD66 datum.|16-MAY-23
34116|Gorge Creek Granite Complex|Description at type locality|Deformed hornblende-biotite granitic gneiss intrusions are interlayered with biotite granitic gneiss of the Fat Hen Creek Complex. A sample from GR 3114 77462 comprises quartz, microcline and microperthite, oligoclase to andesine, albite, biotite, hornblende, subhedral epidote, opaques with minor sphene. A second granite from GR 3123 77470 comprises quartz, microcline, large porphyritic albite, oligoclase, biotite and hornblende.  The grid references are based on the AGD66 datum.|16-MAY-23
34116|Gorge Creek Granite Complex|Extent|The Gorge Creek Granite Complex crops out over about 5km2 in a belt about 1km wide parallel to the Cape River. Hornblende-bearing granitic gneiss which occurs at the station dump near Lolworth homestead may be part of this episode.|16-MAY-23
34116|Gorge Creek Granite Complex|Lithology|The type section is the only part of the unit where outcrop has been found. The distribution of the unit has been determined by air photo interpretation and is only approximate. Deformed hornblende-bearing granites near Lolworth homestead may be part of the same magmatic event but are not included in the unit at the present.|16-MAY-23
34116|Gorge Creek Granite Complex|Relationships and boundaries|The Gorge Creek Granite Complex intrudes the Fat Hen Creek Complex. Some of the hornblende-bearing granite cuts across the foliation of the Fat Hen Creek Complex granitic gneiss while some are strongly foliated and appear to have been deformed by the same event.|16-MAY-23
34116|Gorge Creek Granite Complex|Age reasons|The age of the Gorge Creek Granite Complex is late Mesoproterozoic. A 207[superscript]Pb/206[superscript]Pb age of 1109 +/- 22 Ma was determined using the SHRIMP microprobe on zircons (Fanning, 1995).|16-MAY-23
34116|Gorge Creek Granite Complex|Comments|MAGNETIC SUSCEPTIBILITY::  Magnetic susceptibilities in the type section are in the range 0-1308 x 10[superscript]-5 SI units.|16-MAY-23
34116|Gorge Creek Granite Complex|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
31678|Gorge Quartzite|Lithology|Cream to buff muscovite quartzite, saccharoidal and thick-bedded; medium-grained quartzite with muscovite, biotite, hematite, andalusite, garnet in places; partly interlayered with Strathburn Formation; muscovite quartzite, sillimanite-muscovite-quartz schist; andalusite garnet or graphite locally; Schistose muscovite-biotite quartzite, garnet-mica-hematite schist, andalusite-staurolite-garnet-graphite-mica schist, chloritoid, tourmaline in places|16-MAY-23
24300|Gowers Formation|Name source|Gowers Bore, a water bore on Thorntonia Station, GR 825381; Undilla 1:100 000 topographic sheet. Latitude 19o33'S Longitude 138o50'E.|16-MAY-23
24300|Gowers Formation|Unit history|Opik (1979) assigned these rocks to the basal Currant Bush Limestone de Keyser & Cook (1972) placed some of these rocks in an informal unit, the Chummy Bore Formation.|16-MAY-23
24300|Gowers Formation|Type section locality|6.3 m of bituminous limestone and phosphatic limestone, with minor dolostone toward the base. Chert nodules common in the lower 4 m of section. Outcrop occurs on the northern side of the toe of a prominent east-west ridge of terraced limestone; GR 813368, Undilla 1:100 000 topographic sheet. The section commences at a small tree-covered sinkhole located some 300 m due west of the SSW-SW kink in the access track that follows the fence SSW from Gowers Bore. The base is marked by a 20-40 cm thick phosphatic dolostone that disconformably overlies a 2-10 cm thick horizon of limonite stained stromatolites, named the Bronco Stromatolith Bed. The top consists of a 1 m thick sequence of cream-brown laminated limestone.|16-MAY-23
24300|Gowers Formation|Extent|The Formation crops out to the south of Gowers Bore along West Thornton Creek for a distance of 8 km. Traced to the west of Gowers Bore the Formation crops out over a northwest trending arc to Plumtree Bore, a distance of 13 km.|16-MAY-23
24300|Gowers Formation|Thickness range|0-15 + metres. Formation is wedge-shaped thinning to the southwest and thickening westwards. Formation is absent to the south of Beantree Bore.|16-MAY-23
24300|Gowers Formation|Lithology|Medium olive grey, bituminous limestone, phosphatic limestone, minor phosphorite and chert are the dominant lithologies east of Chummy Bore. Light grey, vuggy and recrystallised dolostone and phosphatic dolostone are the dominant lithologies west of Chummy Bore. Phosphatic hardgrounds and phoscrete crusts are locally abundant.|16-MAY-23
24300|Gowers Formation|Relationships and boundaries|Disconformably overlies the Bronco Stromatolith Bed, a unit of limonite-stained stromatolites and phoscrete crusts that caps the Thorntonia Limestone. Along West Thornton Creek the Gowers Formation is disconformably overlain by the non-phosphatic Currant Bush Limestone. West of Plumtree Bore, the upper contact is unknown.|16-MAY-23
24300|Gowers Formation|Age reasons|An abundant and well preserved fauna that includes agnostoid and polymeroid trilobites, inarticulate and articulate brachiopods, molluscs and hyolithes. Jell (1975) and Opik (1979) place these rocks in the Euagnostus opimus zone which assigns them to the Floran Stage of the Middle Cambrian. Fauna includes Criotypus lemniscatus, Euagnostus opimus Onymagnostus (Agnostonymus semiermis), Rhodotypiscus nasonis, Triplagnostus diremptus (Opik, 1979). Many fossils are preserved as phosphatic internal moulds. Molluscs from this Formation are described by Runnegar & Jell (1976).|16-MAY-23
35070|Grasstree Leucogranite|Name source|Grasstree Ranges west of Barrington homestead in the Homestead 1:100 000 Sheet area.|16-MAY-23
35070|Grasstree Leucogranite|Unit history|The Grasstree Leucogranite was previously mapped as Lolworth Igneous Complex by Wyatt & others (1971), Clarke & Paine (1970), Paine & others (1971) and Vine & Paine (1974).|16-MAY-23
35070|Grasstree Leucogranite|Type section locality|At GR 3571 77705 along a track crossing the Grasstree Ranges west of Barrington station.  The grid reference is based on the AGD66 datum.|16-MAY-23
35070|Grasstree Leucogranite|Description at type locality|Here, a white, medium grained, garnet muscovite leucogranite is interlayered with white pegmatite and white aplite. No background granite was found interlayered with the leucogranite at this locality.|16-MAY-23
35070|Grasstree Leucogranite|Lithology|Rock types similar to those at the type locality occur throughout the outcrop area. Where the layered sheet complexes are thickest, mainly in the area between Barrington station and Mount Stewart in the western part of the Homestead 1:100 000 Sheet area, medium to coarse grained garnet-muscovite leucogranite is the dominant rock type. Coarse pegmatite, up to 15cm in grainsize, is common, particularly in the thicker sheets.|16-MAY-23
35070|Grasstree Leucogranite|Relationships and boundaries|The Grasstree Leucogranite forms a series of layered sheets/dykes intruding the Amarra and Hodgon suites. Contacts between the Grasstree Leucogranite and granites of the Amarra and Hodgon suites are sharp.  Unnamed dykes of similar rock types also intrude adjacent units such as the Fat Hen Creek Complex, Shovel Creek Complex, Cape River Metamorphics, and Glenroy Mill Granodiorite.|16-MAY-23
35070|Grasstree Leucogranite|Age reasons|The age of the Grasstree Leucogranite is not known precisely. Webb (1971), reported K-Ar ages of 398-409 +/- 12 Ma recalculated using the decay constants of Steiger & Jager, 1977 & Dalyrmple, 1978) for the granites of the Lolworth Igneous Complex. He reported no detectable difference between ages from the leucogranites to ages from the muscovite/biotite granites. This suggests that the Grasstree Leucogranite is much the same age as the Amarra suite. A sample from an unnamed leucogranite sheet from 1km north east of Barrington station yielded a SHRIMP microprobe 206Pb/238U age of 414 +/- 5 Ma. This age was obtained on a single zircon grain and appears older than expected because the Grasstree Leucogranite intrudes rock types dated at 382 +/- 5 Ma by the same technique. The zircon grain yielding the 414 +/- 5 Ma age is morphologically similar to zircon from the adjacent Hodgon Granodiorite which also yielded an age of 414 +/- 5 Ma. It is possible that the single zircon grain dated from the leucogranite dyke is a xenocryst from the adjacent granodiorite rather than crystallising from the leucogranite.|16-MAY-23
35070|Grasstree Leucogranite|Comments|The Grasstree Leucogranite and associated dykes/sheets are consistently non-magnetic. Petrographic examinations of rock types of this unit reveal a lack of any opaque phases in almost all samples.|16-MAY-23
35070|Grasstree Leucogranite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
35068|Grasstree Suite|Constituents|Suite includes the Grasstree Leucogranite and many unnamed leucogranite/aplite/pegmatite dykes that intrude granites of the Amarra and Hodgon suites as layered sheets and dykes.|16-MAY-23
35068|Grasstree Suite|Lithology|The granites commonly comprise quartz, albite, plagioclase, K-feldspar, muscovite and garnet. Biotite is absent from most granites in this suite and they are also mainly non-magnetic.|16-MAY-23
35068|Grasstree Suite|Comments|The Grasstree Suite is best developed northwest of Barrington station where it forms sub-horizontally layered sheets up to 200 metres thick. It is also well developed north and northeast of Cornelia station in the Lolworth 1:100 000 Sheet area. Elsewhere in the batholith, the suite occurs as ubiquitous layered dykes/sheets intruding the Amarra and Hodgon suites.|16-MAY-23
27083|Graveyard Creek Group|Name source|Graveyard Creek, which joins Gray Creek at 7859-686690.  The creek branches at 669696 and most topographic maps show Graveyard Creek as the east-flowing branch.  According to local usage the south-flowing branch is Graveyard Creek, and the other branch is Chinaman Creek.|16-MAY-23
27083|Graveyard Creek Group|Unit history|Graveyard Creek Formation of White (1959, 1962, 1965), which was raised to group status by Withnall & others (1988).|16-MAY-23
27083|Graveyard Creek Group|Constituents|Northern area:-  Quinton Formation, Crooked Creek Conglomerate. Southern area:- Jack Formation, Poley Cow Formation.|16-MAY-23
27083|Graveyard Creek Group|Extent|The Group crops out in two main areas. The larger, in which the Quinton Formation and Crooked Creek Conglomerate crop out, extends from 'Pandanus Creek' homestead east to Tomcat Creek, and from the middle reaches of Dinner Creek south to the large laterite plateau in the central part of BURGES.  The other area is a southwest-trending belt about 25 km long and 6 km wide from the southern edge of the plateau in the headwaters of Back Creek to the Dosey Creek area.  The Poley Cow and Jack Formations crop out in this area.|16-MAY-23
27083|Graveyard Creek Group|Lithology|Lithofeldspathic to lithic (and locally quartzose) arenite, polymictic conglomerate, mudstone, and limestone.|16-MAY-23
27083|Graveyard Creek Group|Fossils|The Group contains a diverse fauna which includes graptolites, trilobites, corals and conodonts, and indicates an Early Silurian to earliest Devonian age.  See Withnall & others (1988)  for more details.|16-MAY-23
27083|Graveyard Creek Group|Relationships and boundaries|The Group unconformably overlies the Judea Formation, and is disconformably overlain by the Early Devonian Shield Creek Formation and locally the Middle Devonian Storm Hill Sandstone.|16-MAY-23
27083|Graveyard Creek Group|Age reasons|The Group contains a diverse fauna which includes graptolites, trilobites, corals and conodonts, and indicates an Early Silurian to earliest Devonian age.  See Withnall & others (1988)  for more details.|16-MAY-23
27083|Graveyard Creek Group|References|WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4. Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.WHITE, D.A., 1962:  Clarke River 1.250 000 Geological series.  Bureau of Mineral Resources, Australia, Explanatory Notes, E/55-13.WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
7781|Gregory Downs Limestone|Name source|Gregory Downs' property; GR 198940y - Lawn Hill 1:250 000 Sheet area.|16-MAY-23
7781|Gregory Downs Limestone|Type section locality|The poor outcrop and flat lying nature of the unit prevents the description of a measured section. The type locality is the bed and banks of Macadam Creek where it is crossed by the road from Gregory Downs to Lawn Hill (GR 191940y - Lawn Hill 1:250 000 Sheet area). The outcrop at the type area has been described and illustrated in Grimes (1974). Here 5 m of limestone are exposed and the upper boundary is marked by the junction with the overlying dark clay of the Armraynald Beds. The lower boundary is not exposed at the type locality.|16-MAY-23
7781|Gregory Downs Limestone|Extent|Scattered outcrops occur in creek beds and across the black soil plains to the NW, W, and SW of Gregory Downs Homestead. It is also recorded in drillholes to the N and NE, making a total areal extent of about 500 km2.|16-MAY-23
7781|Gregory Downs Limestone|Thickness range|Up to 5 m in outcrops, a maximum of 12 m in water bore R 30163, 5 km SW of the type locality. The thickness is very variable and the limestone pinches out completely in some places.|16-MAY-23
7781|Gregory Downs Limestone|Lithology|In outcrops the formation comprises white massive or thick-bedded fine to coarsely crystalline limestone with small pale green clay shards in some beds. There are some thin beds of soft white or yellow calcareous and sandy clay, and of pink calcarenite. Veins and nodules of chert occur within the limestone. Thin sections exhibit both sparry calcite and cloudy micrite with a scattering of quartz grains (Grimes, 1974; Cox, 1973).|16-MAY-23
7781|Gregory Downs Limestone|Relationships and boundaries|The limestone underlies the dominantly clayey Armraynald Beds at the type locality and in the bore holes. The lower boundary of the unit is less well defined. The base is not exposed at the type locality and in the nearest borehole (IWSC Gregory Downs No. 1 - Cox, 1973) the limestone appears to have pinched out. However in the next bore to the east (IWSC Gregory Downs No. 2, 4 km from the type area) there is a bed of "soft weathered limestone" between 9 and 12 m depth which underlies the clay and gravel beds of the Armraynald Beds and overlies gravel and clay of the Floraville Formation. The depth of 12 m in this borehole is taken as the base of the Gregory Downs Limestone. The Floraville Formation in this area has limestone bands interbedded with its dominantly clay, sand and gravel lithologies. These limestone bands should not be confused with the overlying thick limestone of the Gregory Downs Limestone.|16-MAY-23
7781|Gregory Downs Limestone|First Reference|79/20075|16-MAY-23
25038|Gunpowder Creek Formation|Name source|Gunpowder Creek which joins the Leichhardt Rivr at 6859-925733.|16-MAY-23
25038|Gunpowder Creek Formation|Unit history|The Gunpowder Creek Formation as defined in this paper, includes part of the Gunpowder Creek Formation, Mingera Beds, and Ploughed Mountain Beds of Carter & others (1961). Cavaney (1975) proposed the name '"Gunpowder Siltstone" for this unit.|16-MAY-23
25038|Gunpowder Creek Formation|Type section locality|Hypostratotype: Along 2.5 km of an unnamed tributary of Gunpowder Creek between 222176 (base) and 195187 (top) in the Mammoth Mines 1:100 0000 Sheet area. Approximately 770 m of medium grained sandstone, blocky fine grained micaceous sandstone, purple micaceous siltstone, dolomitic siltstone and leached carbonaceous shale crop out in the hypostratotype.|16-MAY-23
25038|Gunpowder Creek Formation|Extent|The Gunpowder Creek Formation crops out extensively in the Mammoth Mines and Kennedy Gap 1:100 000 Sheet areas, in the west and southeast of the Mount Oxide 1:100 000 Sheet area, and around the Kamarga Dome in the Lawn Hill 1:100 000 Sheet area.|16-MAY-23
25038|Gunpowder Creek Formation|Thickness range|The unit is variable in thickness with a maximum of 770 m in the hypostratotype. Only a few metres of Gunpowder Creek Formation are present in the Mount Gordon fault zone in the Mammoth Mines 1:100 000 Sheet area. Most sections are between 300 to 400 m in thickness.|16-MAY-23
25038|Gunpowder Creek Formation|Lithology|The dominant lithology is a laminated red and green micaceous siltstone and fine grained micaceous sandstone. Dolomite, dolomitic siltstone and leached carbonaceous shale are common toward the top of the sequence. In the Lawn Hill 1:100 000 Sheet area, the unit comprises sandstone and carbonaceous shale and siltstone.|16-MAY-23
25038|Gunpowder Creek Formation|Relationships and boundaries|The unit conformably overlies the Torpedo Creek Quartzite and is overlain conformably by the Paradise Creek Formation. The top boundary is placed at the base of the Mount Oxide Chert Member, a prominent basal marker bed of the Paradise Creek Formation. The base of the unit is placed immediately above the massive orthoquartzite or conglomerate of the Torpedo Creek Quartzite. Where the Torpedo Creek Quartzite is absent, the Gunpowder Creek Formation unconformably overlies the Surprise Creek Formation, Myally Subgroup, Judenan Beds, Fiery Creek Volcanics, Bigie Formation and Eastern Creek Volcanics.|16-MAY-23
25038|Gunpowder Creek Formation|Age reasons|Mid Proterozoic (Carpentarian).|16-MAY-23
25038|Gunpowder Creek Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
21934|Gypsy Pocket Granodiorite|Name source|Gypsy Pocket bore at 2855 77518 in the White Mountains 1:100 000 Sheet area. Gypsy Pocket is an elongate area of low-lying undulating topography surrounded by hills of Cape River Metamorphics, centred about 7km west of Goldsborough homestead.  The grid reference is based on the AGD66 datum.|16-MAY-23
21934|Gypsy Pocket Granodiorite|Unit history|The Gypsy Pocket Granodiorite was shown as unnamed Palaeozoic granitoid on the first edition Hughenden 1:250 000 geological map, but its eastern extent was exaggerated (Vine & Paine, 1974; Paine & others, 1971|16-MAY-23
21934|Gypsy Pocket Granodiorite|Type section locality|At 2861 77521 along a track west from Goldsborough homestead to the boundary with Cargoon Holding.  The grid reference is based on the AGD66 datum.|16-MAY-23
21934|Gypsy Pocket Granodiorite|Description at type locality|Low bouldery outcrops consist of grey fine to medium-grained, equigranular biotite-hornblende granodiorite with sparse mafic xenoliths.|16-MAY-23
21934|Gypsy Pocket Granodiorite|Extent|A roughly triangular-shaped body that crops out over about 5km2 in Gypsy Pocket .|16-MAY-23
21934|Gypsy Pocket Granodiorite|Lithology|The Gypsy Pocket Granodiorite appears to be mainly fine to medium-grained, equigranular biotite-hornblende granodiorite, although Paine & others (1971, p29) described it as adamellite with subsidiary microdiorite and quartz diorite. The latter were not seen during the present survey. The granodiorite consists of laths of plagioclase (andesine with oscillatory zoning), interstitial relatively unstrained quartz, anhedral K-feldspar (poikilitically enclosing plagioclase), subhedral green hornblende prisms, ragged brown biotite flakes and accessory sphene. Sparse, small rounded xenoliths and veins of pink aplite or fine-grained leucogranite up to 10cm wide are commonly present. The granodiorite is generally poorly exposed and covered by alluvium and colluvium derived from the surrounding hills of Cape River Metamorphics.|16-MAY-23
21934|Gypsy Pocket Granodiorite|Relationships and boundaries|The Gypsy Pocket Granodiorite intrudes the Cape River Metamorphics. It is locally intruded by rhyolite dykes of presumed late Palaeozoic age. The unit weathers recessively, being covered by Quaternary alluvium over much of its area.|16-MAY-23
21934|Gypsy Pocket Granodiorite|Age reasons|The age of the Gypsy Pocket Granodiorite is not definitely known, but is probably Carboniferous or Permian because its unfoliated, unstrained nature and relatively fine grainsize suggest a high-level emplacement late in the history of the region.|16-MAY-23
21934|Gypsy Pocket Granodiorite|Comments|MAGNETIC SUSCEPTIBILIY::  Magnetic susceptibilities at the type locality are about 3000 to 4500 x 10[superscript]-5 SI units.|16-MAY-23
21934|Gypsy Pocket Granodiorite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
79131|Hall Clastics Member|Name source|After Hall Road near the West of Scotland shaft, Gympie.|16-MAY-23
79131|Hall Clastics Member|Unit history|This unit was described informally as  Hall clastics by Houston and others (2003) at Monkland Mine.  It was formally registered as a member in 2002 after Cranfield (1999). Referred to by Sivell & Arnold (1999), Sivell & McCulloch (2001) and Li & others (2015). Equivalent to Dunstan's (1911) Third Slate Group of shales, tuffs and conglomerates (3TS, 3TT, 3MS).|16-MAY-23
79131|Hall Clastics Member|Type section locality|None available. Typical reference drill holes were destroyed and no known outcrop.  See photos in Stidolph et al. (2016). Reference core of typical lithologies was collected from GEGM drill holes M155 and M157 and is kept at Zillmere storage facility, Brisbane.  An atypical section  from the northern limits of the member in the Zillmere core library in Brisbane is GEGM drill hole G215, 98.4-113.8 m (MGA 467424mE; 7101493mN, Lat: -26°12'21"  Long: 152°40'26"); this does not show typical lithologies described below.|16-MAY-23
79131|Hall Clastics Member|Extent|Found mainly in the deeper levels of Monkland Mine and at shallower depths beneath Kidgell Andesite at Deep Creek. Identified in many air core holes in Jones Hill area and Dawn block but could not be verified as distinct from the main Dawn Formation lithotypes. Thins out at North Inglewood (Figure 11) and not recognised north of Monkland block.|16-MAY-23
79131|Hall Clastics Member|Thickness range|Up to 200 m thick in Monkland block.|16-MAY-23
79131|Hall Clastics Member|Lithology|This unit is a sequence of sub-aqueous, medium to coarse grained, volcaniclastic sediments or pyroclastic deposits which have derived the bulk of their material from the reworking of Tozer basalt flows and Kidgell Andesite.  This gives them a large degree of variability depending on the maturity and provenance of the sediments. The dominant lithology is a greenish volcanogenic conglomerate which contains sub-rounded clasts to lapilli size, dominantly basaltic, as well as localized feldspar-phyric andesite and scattered rip-up clasts of angular, yellow-green, dacitic tuff/siltstone.  The conglomerate is interlayered with Tozer basalt, hyaloclastic basalt and redeposited hyaloclastite, consisting of close-packed amygdaloidal pyroxene-phyric clasts.  These coarser pyroclasts are interbedded with light green, cherty, de-vitrified, fine grained, ashy sediments, typical of the formation as a whole, but containing detrital pyroxene, presumably reworked from or erupted with the Tozer Volcanics. These characteristics were only recognised in drill holes.|16-MAY-23
79131|Hall Clastics Member|Relationships and boundaries|Overlain by Tozer Basalt and has an ill-defined gradational contact with the underlying dacitic tuffs and siltstones which constitute the bulk of Dawn Formation. Intruded by numerous Tozer dykes.|16-MAY-23
79131|Hall Clastics Member|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie, 12-JAN-2017.|16-MAY-23
79131|Hall Clastics Member|References|Houston, M, McQuitty B., Beckton, J and Groves, S, 2003: Exploration Permit for Minerals 6031.         Annual report for the year ending 6th September 2003. GEGM report to DNR&M. Report number VIII 16.  **Dunstan, B., 1911: Geology map of Gympie and environs. GSQ Publ. No. 221b.  **Cranfield, L.C., 1999: Gympie Special Sheet 9445, Part 9545, Queensland 1:100,000 Geological Map Commentary. Queensland Department of Mines and Energy, Brisbane.  **Sivell, W.J. and Arnold, G.O. 1999: Geochemical and volcanic stratigraphy of a segment of an island arc - Gondwana rim accretion zone, Gympie Province, southeast Queensland.  In Flood, P.G. (Editor): Regional Geology, Tectonics and Metallogenesis, New England Orogen, NEO '99 Conference, 255-266.  **Sivell, W.J. and McCulloch, M.T. 2001: Geochemical and Nd-isotopic systematics of the Permo-Triassic Gympie Group, southeast Queensland.  Australian Journal of Earthsciences 48, 377-394.  **Li, P., Rosenbaum, G., Yang, J-H. and Hoy, D. 2015	Australian-derived detrital zircons in the Permian-Triassic Gympie terrane (eastern Australia): Evidence for an autochthonous origin. Tectonics, 34, 858-874.|16-MAY-23
76907|Hampden Slate|Name source|The Hampden group of mines at Kuridala (White, 1957). GDA94 coordinates lat. -21.28081 and long. 140.50402, MALBON 1:100 000 Sheet area.|16-MAY-23
76907|Hampden Slate|Unit history|The name Hampden Slate Member was originally used for the upper part of the Kuridala Formation (White, 1957; Carter, 1959; Carter et al., 1961). Later mapping showed the rocks as an unnamed member of the Kuridala Formation (Donchak et al., 1983; Betts et al., 2000; Giles et al., 2006). As a result of revised GSQ mapping the name Hampden Slate was reinstated and raised to formation status as a constituent of the Kuridala Group (GSQ, 2011; Withnall & Hutton, 2013). The unit has never been formally defined.|16-MAY-23
76907|Hampden Slate|Type section locality|The proposed type section for the Hampden Slate is on the western limb of the Mort River Anticline. It is located in the eastern area of the MOUNT MERLIN (6954) 1:100 000 Sheet area from lat. -21.713519, and long. 140.498045 (base) to lat. -21.696208 and long. 140.479902 (faulted contact with the Staveley Formation). Boundary reference-section: The basal contact is conformable with the Hampden Slate, with a gradational contact on the western limb of the Hampden Synform at lat. -21.273089 and long. 140.495581. The upper contact has not been observed.|16-MAY-23
76907|Hampden Slate|Extent|The Hampden Formation crops out in three main areas: in the core of the Hampden Syncline at Kuridala, 65 km south of Cloncurry; on the eastern and western limbs of the Mort River Anticline 20 km SSE of the former township of Selwyn; and within cores of synclines 30 km south of Selwyn along an access road to the Osbourne Mine.|16-MAY-23
76907|Hampden Slate|Thickness range|Tentatively calculated at ~2000 m, although due to the complex structure and likely repetition, this is likely to be an overestimate.|16-MAY-23
76907|Hampden Slate|Lithology|Carbonaceous slate and micaceous phyllitic schist with rare medium to thin-bedded, fine to medium-grained, quartz sandstone.|16-MAY-23
76907|Hampden Slate|Depositional environment|Hydrodynamically calm, mostly anoxic, deep marine(?) conditions|16-MAY-23
76907|Hampden Slate|Relationships and boundaries|Conformably underlain by the Starcross Formation. An intercalated gradational contact relationship can be observed on the western limb of the Hampden Syncline at lat. -21.273089 and long. 140.495581. No upper boundary is exposed, because the Hampden Slate either occurs in synformal cores or is faulted against adjacent units. The Hampden Slate is intruded by numerous sills of metadolerite and metagabbro.|16-MAY-23
76907|Hampden Slate|Identifying features|Predominantly pelitic, contrasting with the psammopelitic Starcross Formation. Commonly carbonaceous.|16-MAY-23
76907|Hampden Slate|Structure and Metamorphism|The Hampden Slate was complexly folded and deformed during the during the 1600-1570 Isan Orogeny and exhibits strong cleavage and crenulation foliations. The metamorphic grade is probably upper greenschist to amphibolite facies, based on assemblages in the mafic intrusions. Metamorphic index minerals are rare in the pelites, but the carbonaceous slate exhibits an apparent lower metamorphic grade than surrounding non-carbonaceous rocks.|16-MAY-23
76907|Hampden Slate|Age reasons|Paleoproterozoic (Statherian). A maximum deposition age of 1650 ± 8 Ma has been determined by Lewis et al. (2018, this record). An age of 1684.5 ± 5.0 Ma was determined by Cross et al. (2015) on a volcaniclastic rock, although Withnall (in preparation) has suggested that this is largely an inherited age and proposed an alternative age of 1659 ± 15 Ma. Data interpreted as giving a maximum depositional age of 1686 ± 7 Ma (Lambeck, 2011) has been reinterpreted as 1661 ± 17 Ma (Withnall, in preparation). A felsic phase from a metadolerite sill intruding the Hampden Slate has an age of 1659.4 ± 4.2 Ma providing a minimum age for deposition (Lambeck, 2011). The Hampden Slate was deformed during the during the 1600-1570 Isan Orogeny.|16-MAY-23
76907|Hampden Slate|Correlations|Probably correlates with the Toole Creek Volcanics in the Soldiers Cap Group.|16-MAY-23
76907|Hampden Slate|Alteration and Mineralisation|Hosts the Kuridala, Hampden, Mount Elliot, Swan, Mount Dore, Stuart and Victoria North copper deposits and the Merlin molybdenum¿rhenium deposit.|16-MAY-23
76907|Hampden Slate|Defn author|Alexander P. Slade, Allan Parsons and Ian W. Withnall, Geological Survey of Queensland, 21/03/2018|16-MAY-23
76907|Hampden Slate|Proposed publication|Queensland Geological Record|16-MAY-23
76907|Hampden Slate|References|Betts, P.G., Ailleres, L., Giles, D. and Hough, M., 2000. Deformation history of the Hampden Synform in the Eastern Fold Belt of the Mt Isa terrane. Australian Journal of Earth Sciences, 47(6), 1113-1125. **Carter, E.K., 1959. New stratigraphic units in the Precambrian of north-western Queensland. Queensland Government Mining Journal, 60(692), 437-431. **Carter, E.K., Brooks, J.H. and Walker, K.R., 1961. The Precambrian mineral belt of north-western Queensland. Bureau of Mineral Resources, Australia, Bulletin 51. **Cross, A.J., Dunkley, D.J., Bultitude, R.J., Brown, D.D., Purdy, D.J., Withnall, I.W., Von Gnielinski, F.E., and Blake, P.R., 2015. Summary of results Joint GSQ-GA geochronology project: Thomson Orogen, New England Orogen and Mount Isa region, 2010-2012. Queensland Geological Record 2015/01. **Donchak, P.J.T., Blake, D.H., Noon, T.A. and Jaques, A.L., 1983. Kuridala Region, 1: 100 000 Geological Map Commentary. Bureau of Mineral Resources, Canberra. **Giles, D., Betts, P.G., Ailleres, L., Hulscher, B., Hough, M. and Lister, G.S., 2006. Evolution of the Isan Orogeny at the southeastern margin of the Mt Isa Inlier. Australian Journal of Earth Sciences, 53(1), pp. 91-108. **GSQ, 2011. North-West Queensland Mineral and Energy Province Report. Department of Employment, Economic Development and Innovation. Queensland Government. **Lambeck, A., 2011. Basin analysis and the geochemical signature of Paleoproterozoic sedimentary successions in northern Australia: Constraints on basin development in respect to mineralisation and paleoreconstruction models. The University of Adelaide. PhD thesis (unpublished). **Lewis, C.J, Hutton, L.H., Withnall, I.W., Slade, A.P., Sargeant, S., 2018. Summary of results Joint GSQ¿GA geochronology project: Mount Isa region, 2016-2017. Queensland geological Record. **White, W.C., 1957. Preliminary report on the geology of the Selwyn area of N.W. Queensland. Bureau of Mineral Resources, Canberra. Australian Record 1957/094. **Withnall, I.W., in preparation. Review of zircon ages for the eastern Succession of the Mount Isa Province. Queensland Geological Record. **Withnall, I.W., and Hutton, L.J., 2013. Chapter 2: North Australian Craton, in Jell, P. A., editor, Geology of Queensland. Brisbane, Geological Survey of Queensland, 23-112.|16-MAY-23
8033|Hampton Road Rhyolite|Unit history|Campbell (1952) applied this name to a sequence of interbedded rhyolitic flows, pyroclastics, arenite, conglomerate, and silicified mudstone.  It is well exposed along the Esk - Hampton Road along the type section designated by Cranfield & others (1976).|16-MAY-23
8033|Hampton Road Rhyolite|Geomorphic expression|The airphotopattern is dominated by deeply incised valleys adjacent to indurated steep hills that are locally demonstrably dip slopes.|16-MAY-23
8033|Hampton Road Rhyolite|Extent|The unit occupies an area of approximately 35 km2 of thickly forested, dominantly rugged country, between 480 and 580 m above sea level along the Esk-Hampton Road and environs.|16-MAY-23
8033|Hampton Road Rhyolite|Thickness range|In the south the unit is 1500 m thick; in the north it thins to less than 30 m.|16-MAY-23
8033|Hampton Road Rhyolite|Lithology|The unit contains thick rhyolite flows and pyroclastics and minor interbedded arenite, conglomerate, and chert.  The rhyolite flows are glassy, spherulitic or fluidal, and form blocky outcrops that are grey, white, or black.  Three marker bands of agglomerate, consisting of purple rhyolitic fragments set in a fine-grained green tuffaceous matrix, occur near the base of the rhyolite.  South of the Esk-Hampton Road pyroclastics predominate; these become coarse-grained to the south, indicating an eruptive centre in this direction.|16-MAY-23
8033|Hampton Road Rhyolite|Relationships and boundaries|The unit conformably overlies the Pinecliff Formation, and is conformably overlain by the Biarraville Formation.  In the east, the Hampton Road Rhyolite is faulted against the Toogoolawah Group and the Woogaroo Subgroup by the Western Border Fault. West of this fault, outliers of Woogaroo Subgroup overlie the unit. South of the Esk - Hampton Road small bodies of the "Champion Hills Diorite" intrude the unit.|16-MAY-23
8033|Hampton Road Rhyolite|Structure and Metamorphism|STRUCTURE:  Rocks of the unit dip at 450 to 800 on the southern flank of an east-south-east trending anticline, and at 450 to 600 on the northern flank. Northeast of Mount Deongwar, it is exposed on the flanks of a northerly plunging syncline, but has been differentiated only on the western limb at the present scale of mapping.|16-MAY-23
8033|Hampton Road Rhyolite|Age reasons|No fossils are known from the type area of this unit; it was tentatively assigned an Early Permian age based on its similarity with the lower half of the Gympie Group (Rammutt Formation).  Beutel (1973) listed a fauna including Eurydesma in a dark green cherty rock from 4.5 km west of Mount Perseverance, thus indicating an Early Permian age at this locality.|16-MAY-23
8033|Hampton Road Rhyolite|Correlations|This unit appears lithologically similar to the Rammutt Formation in the Kin Kin Subprovince of the Gympie Province near Gympie.|16-MAY-23
8033|Hampton Road Rhyolite|Geophysical Expression|The unit has a strong potassic (pink) signature on the ternary K-Th-U radiometric image and a moderate to high magnetic response.|16-MAY-23
8033|Hampton Road Rhyolite|Comments|.|16-MAY-23
8033|Hampton Road Rhyolite|References|*CAMPBELL, K.S.W.,1952,The geology of the Cressbrook-Buaraba area,"University of Queensland.  Department of Geology Papers (New series), Regional Geology.    *CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.",1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional Geology.|16-MAY-23
8085|Hardway Granite|Name source|Hardway mine (M.L. 5633, Cloncurry Mining District) is immediately west of the most southerly mass of the Granite, 9 km west-northwest of Mary Kathleen, latitude 20o45'25"S, longitude 139o53'45"E (6856 853047).|16-MAY-23
8085|Hardway Granite|Geomorphic expression|Tors, boulder-strewn hills, and sandy pediments.|16-MAY-23
8085|Hardway Granite|Type section locality|The King's Cross mine area in the southern mass, latitude 20o45'S, longitude 139o54'45"E (6856 866057) is mostly leucocratin and fine-grained but contains some coarse-grained porphyritic granite, leucogranite, and micro-granite plugs and dykes.|16-MAY-23
8085|Hardway Granite|Extent|The three main masses of Hardway Granite are aligned roughly north-south in the east of the Mary Kathleen 1:100 000 Sheet area; the largest and most southerly mass covers 12 km2, and is exposed from 1 km south to 4 km north of the Barkly Highway between 5 and 8 km west of Mary Kathleen. To the north of this mass and east of Deighton Pass another mass of this granite covers 5 km2, while a third mass a further 3 km to the north covers 2 km2. These masses were formerly a single granite mass which has been cut by strike-slip faults of the Wonga Fault System, along which up to 3 km of dextral movement has taken place.|16-MAY-23
8085|Hardway Granite|Lithology|In the south, the Granite is relatively leucocratic and fine-grained, and is extensively veined by aplite, but is coarser-grained and richer in biotite in the northern masses. In the north medium-grained tonalite, granodiorite and diorite occur towards the contacts of the Granite with Leichhardt Metamorphics. The accessory minerals are opaque oxides, sphene, apatite and allanite.|16-MAY-23
8085|Hardway Granite|Relationships and boundaries|Northern masses of the Hardway Granite intrude the Leichhardt Metamorphics and the Argylla Formation; the southern mass intrudes the Corella Formation 1 km east of the Mount Frosty mine. Many contacts are faulted. The areas now called Hardway Granite were mapped as Kalkadoon Granite by Carter et al. (1961) and are shown as that Granite on the Mary Kathleen 1:100 000 Preliminary Geological Map. Derrick et al. (1974) thought the Hardway granite was similar to the Wonga Granite although its generally massive character indicates less deformation than in areas of Wonga Granite about 5 km to the east.|16-MAY-23
8085|Hardway Granite|Age reasons|No reliable isotopic age determinations are available for the Hardway granite. A sample of diorite from the northern mass yielded a Rb/Sr age of 1645+/-67 m.y. (Page, pers. comm., 1974).|16-MAY-23
8085|Hardway Granite|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1978|16-MAY-23
8085|Hardway Granite|Proposed publication|Queensland Government Mining Journal, 79 (1978)|16-MAY-23
8085|Hardway Granite|Comments|Discussion: The Hardway Granite is distinguished from the Kalkadoon Granite because of its distinctive structural setting, its location, and its intrusive relations with the Corella Formation. Compositional variation from north to south, from diorite and tonalite to granodiorite, granite, leucogranite and aplite, accompanied by progressively younger country rock, probably reflects depth zoning in the original pluton, the northern mass having formed at the deepest level. Subsequent to its intrusion, the Hardway Granite was faulted, and probably folded, to form its present configuration after uplift and erosion. Numerous dolerite dykes cut the Granite.|16-MAY-23
8085|Hardway Granite|Defn approved by|Queensland Sub-Committee|16-MAY-23
8085|Hardway Granite|Name first published by|Glikson A.Y., Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
24305|Harpur Creek Member|Name source|Harpur Creek, GR 69000E 87000N Rosedale 1:100 000 Sheet area.|16-MAY-23
24305|Harpur Creek Member|Unit history|Part of the Lowmead Beds of Cribb, 1960; Mack, 1972; and Ellis and Whitaker, 1976.|16-MAY-23
24305|Harpur Creek Member|Type section locality|91 m (estimated true thickness 90.5 m) from 56 m to 147 m in LDD1 (GR 67628E, 93690N, Miriam Vale 1:100 000 Sheet area). The interval is within the type section of the Lowmead Formation. The dominant rock type is claystone, beds of which are up to 6.45 m thick. There are abundant interbeds of oil shale (up to 4.43 m thick), sandy claystone (up to 6 m thick) and sandstone (up to 6.25 m thick). The member is calcareous. The upper boundary of the member is the contact between green claystone and carbonaceous oil shale of the Wheatley Oil Shale Member. The boundary is the contact between green sandstone and red sandstone of the Hobble Creek Member.|16-MAY-23
24305|Harpur Creek Member|Description at type locality|The interval is within the type section of the Lowmead Formation. The dominant rock type is claystone, beds of which are up to 6.45 m thick. There are abundant interbeds of oil shale (up to 4.43 m thick), sandy claystone (up to 6 m thick) and sandstone (up to 6.25 m thick). The member is calcareous. The upper boundary of the member is the contact between green claystone and carbonaceous oil shale of the Wheatley Oil Shale Member. The boundary is the contact between green sandstone and red sandstone of the Hobble Creek Member. Claystone is dusky yellow green to greyish olive green, moderately hard to soft (puggy) and massive to laminated in part. Gastropod fragments are abundant. Oil shale is dark yellow-brown to olive-grey, hard and very thinly laminated. There are sporadic ostracod and chitinous fragments and claystone laminae. There is an oil shale bed from 76.3 m to 91.6 m in the type section which is a "marker" within the Harpur Creek Member. It is dusky yellow-brown to olive-grey oil shale. The top 1 m is carbonaceous oil shale. Sandstone is fine to coarse grained, massive, and sand grains are poorly sorted, sub-angular and of low sphericity. There are interbeds of clayey sandstone to sandy claystone.|16-MAY-23
24305|Harpur Creek Member|Extent|Subcrops in an area of about 37 km2 in the vicinity of Harpur Creek, extending 7 km north. Sparse weathered outcrop is known. The member has been identified from drill core.|16-MAY-23
24305|Harpur Creek Member|Thickness range|91 m in type section; true thickness is 90.5 m (corrected for 6o dip of strata in drill hole). The member ranges in thickness from 6.5 m to 149.7 m.|16-MAY-23
24305|Harpur Creek Member|Fossils|Gastropod fragments are abundant.|16-MAY-23
24305|Harpur Creek Member|Relationships and boundaries|The Harpur Creek Member in part unconformably overlies igneous rocks of the Miriam Vale Granodiorite and Agnes Waters Volcanics (Ellis & Whitaker, 1976) and in part conformably overlies the Hobble Creek Member of the Lowmead Formation. It is conformably overlain by the Wheatley Oil Shale Member of the Lowmead Formation. The member is faulted against the igneous rocks it in part overlies along the boundaries of the Lowmead Graben.|16-MAY-23
24305|Harpur Creek Member|Age reasons|Early Tertiary - as for the Lowmead Formation.|16-MAY-23
24305|Harpur Creek Member|Defn author|McConnochie M.J., Henstridge D.A. 1985. 86/25154 Described p.211.|16-MAY-23
24305|Harpur Creek Member|Comments|Note: Drill core of LDD14 is stored at Southern Pacific Petroleum's Research and Core Storage facility in Gladstone, Queensland.|16-MAY-23
23642|Harry Creek Formation|Name source|Harry Creek, which joins McKinnons Creek at 7859 412615.  The grid reference is based on the AGD66 datum.|16-MAY-23
23642|Harry Creek Formation|Unit history|Previously mapped as the Bundock Creek Formation (now Group) by White (1959, 1962, 1965) and 'upper' Bundock Creek Formation by Wyatt & Jell (1980).  The name was first used and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
23642|Harry Creek Formation|Geomorphic expression|The Harry Creek Formation generally forms recessive, gullied topography, although light-coloured strike lines due to tuff and sandstone beds are readily discernible on aerial photographs.|16-MAY-23
23642|Harry Creek Formation|Type section locality|About 560 m is exposed in an unnamed tributary of McKinnons Creek between 7759 371601 (base) and 365588 (synclinal hinge).  The grid reference is based on the AGD66 datum.|16-MAY-23
23642|Harry Creek Formation|Description at type locality|The base is marked by a conglomerate horizon containing quartz and quartzite pebbles and cobbles in a very coarse-grained sublabile sandstone matrix.  The remainder of the unit consists of pale green to reddish brown fine-grained to lapilli tuffs and volcaniclastic sandstone.|16-MAY-23
23642|Harry Creek Formation|Extent|Several synclinal cores in the Mount Brown Creek, Bullock Dray Creek, and Harry Creek areas.|16-MAY-23
23642|Harry Creek Formation|Thickness range|The 560 m in the type section is probably close to the maximum thickness exposed.  The original total thickness is unknown, because the unit is restricted entirely to synclinal cores.|16-MAY-23
23642|Harry Creek Formation|Lithology|Fine-grained to lapilli tuff, volcaniclastic sandstone, conglomerate, and siltstone.  Some tuffs are cross-bedded and laminated, and were probably water-lain and reworked.|16-MAY-23
23642|Harry Creek Formation|Fossils|No fossils have been found in this unit.|16-MAY-23
23642|Harry Creek Formation|Relationships and boundaries|Conformably overlies the Boroston Formation, and is distinguished from it by the abundant tuff and volcaniclastic sandstone.  Intruded by the Carboniferous or ?Permian Montgomery Range Igneous Complex.|16-MAY-23
23642|Harry Creek Formation|Age reasons|The unit is probably Early Carboniferous (Visean?) and may be a correlative of the lithologically similar Lyall Formation in the Clarke River Group (Scott & Withnall, 1987; Withnall & others, 1988; Playford, 1988).|16-MAY-23
23642|Harry Creek Formation|References|PLAYFORD, G., 1988:  Early Carboniferous miospores from GSQ Clarke River 3-4R and 5, north Queensland.  Queensland Government Mining Journal, 89, 527-533. **SCOTT, M. & WITHNALL, I.W., 1987:  New and revised stratigraphic units in the Clarke River Basin, north Queensland.  Queensland Government Mining Journal, 88, 50-58. **WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. **WHITE, D.A., 1962:  Clarke River - Qld E/55-13.  Bureau of Mineral 	Resources, Australia 1:250 000 Geological Series Explanatory Notes. **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.D., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
8130|Haslingden Group|Name source|From 'Haslingden' pastoral holding, about 20 km north-northeast of Mount Isa, latitude 20o35'S, longitude 139o35'E, Cloncurry 1:250 000 Sheet area.|16-MAY-23
8130|Haslingden Group|Type section locality|No type section can be specified because of variations in the distribution of type sections of the constituent formations. An almost complete section of the Group is found in a fault block centred on the Counter uranium lease 14 km northeast of Mount Isa.|16-MAY-23
8130|Haslingden Group|Extent|The Haslingden Group occurs in a north-trending belt, centred on Mount Isa, 300 km long and up to 50 km wide. It is found in the Urandangi, Duchess, Mount Isa, Cloncurry, Camooweal and Dobbyn 1:250 000 Sheet areas.|16-MAY-23
8130|Haslingden Group|Thickness range|The group is predominantly an arenite sequence containing interbedded basalt and minor acid volcanic units. From top to bottom, the constituent formations are as follows: Myally Subgroup - Lochness Formation 700-1200 m; Police Creek Siltstone Member 0-400 m; Whitworth Quartzite 100-2000 m; Bortala Formation 80-700 m; Alsace Quartzite 70-600 m; Eastern Creek Volcanics 3600-7200 m; Mount Guide Quartzite up to 6200 m; May Downs Gneiss Member; Leander Quartzite 1500 m.|16-MAY-23
8130|Haslingden Group|Relationships and boundaries|The Haslingden Group unconformably overlies acid volcanics of the Leichhardt Metamorphics, and the Kalkadoon and Ewen Granites which intrude the Leichhardt Metamorphics. The Haslingden Group conformably or disconformably overlies the Argylla Formation, and is unconformably overlain by the Mount Isa Group; it is overlain conformably or disconformably by the Surprise Creek Beds. West of Mount Isa the Sybella Granite intrudes the Mount Guide Quartzite and Eastern Creek Volcanics. The Haslingden Group is broadly equivalent to the Malbon Group near Cloncurry and the Tawallah Group in the Northern Territory.|16-MAY-23
8130|Haslingden Group|Age reasons|The Sybella Granite, part of which is dated at about 1650 m.y. places a minimum age on the Haslingden Group. A maximum age of about 1700 m.y. is inferred from Rb/Sr dates on Kalkadoon Granite and Leichhardt Metamorphcis in the basement (Plumb & Derrick, 1975).|16-MAY-23
8130|Haslingden Group|Defn author|Derrick G.M., Wilson, I.H., Hill R.M., 1976|16-MAY-23
8130|Haslingden Group|Proposed publication|Queensland Government Mining Journal. The name has been previously published by Plumb & Derrick (1975), but its usage is incorrect because the Group incorporated the Myally and Judenan Beds, which were at the time not validly defined formations.|16-MAY-23
8130|Haslingden Group|Comments|Remarks: Sediments of the Haslingden Group were deposited in a relatiavely stable shallow water environment, which persisted despite repeated extrusion of basalt, but was terminated by tectonism accompanying Sybella Granite intrusion. Plumb & Derrick (1975) included Judenan Beds & Carters Bore Rhyolite in the Haslingden Group. The Judenan Beads are equivalent to the Myally Subgroup, but cannot be included in the Group until they are formally renamed or defined; the Carters Bore Rhyolite is probably unconformable on Myally Subgroup rocks west and northwest of Mount Isa, and cannot be included in the Group.|16-MAY-23
84101|Hedleys Formation|Name source|Name derived from Hedley’s Creek, an east-southeast-flowing tributary of the Nicholson River. Confluence of those water bodies is located at (GDA94) 18.8775° 137.4083°, in the WESTMORELAND 1:250 000 mapsheet in Queensland.|
84101|Hedleys Formation|Unit history|Unit mapped as undifferentiated Constance Sandstone in First Edition 1:250 000 mapsheets of LAWN HILL (Carter and Öpik, 1960), WESTMORELAND (Carter, 1959), CALVERT HILLS (Roberts et al, 1963), and MOUNT DRUMMOND (Smith and Roberts, 1963a, b). Distinguished as Psa1 sandstone unit of the Constance Sandstone in Second Edition 1:250 000 mapsheets of LAWN HILL (Hutton and Grimes, 1983), WESTMORELAND (Grimes and Sweet, 1979), and CALVERT HILLS (Ahmad and Wygralak, 1989), following the scheme of Sweet et al (1981). Subsequently mapped as "Hedleys Sandstone Member" of the Constance Sandstone on Second Edition 1:250 000 mapsheet of MOUNT DRUMMOND by Rawlings et al (2006, 2008). Elevated to formation status as "Hedleys Sandstone" by Sweet (2017).|
84101|Hedleys Formation|Geomorphic expression|Ranges from low narrow ridge where unit is thin or steeply dipping, to broad rocky ridges and plateaux where unit is thicker or gently dipping.|
84101|Hedleys Formation|Type section locality|Type section located south of Wire Creek in the WESTMORELAND 1:250 000 mapsheet (Queensland). Base of type section located at (GDA94) 17.8375degrees S 138.1590degrees E (54K 198869mE 8025504mN); top of type section located approximately 500 m to the southeast at 17.8395degrees S 138.1613degrees E (199116mE 8025287mN; Sweet, 2017).|
84101|Hedleys Formation|Extent|Crops out north of Elizabeth Creek in the following 1:250 000 mapsheets: northern LAWN HILL, south of Hedleys Creek in southwestern WESTMORELAND (Queensland), in adjacent parts of southeastern CALVERT HILLS and in northeastern and central MOUNT DRUMMOND. Unit is only distinguished to the north of the Elizabeth Creek Fault Zone.|
84101|Hedleys Formation|Thickness range|Approximately 35 m thick in the type section, thinning westward. In northeastern and central MOUNT DRUMMOND, the unit is approximately 10 to 15 m thick.|
84101|Hedleys Formation|Lithology|In the type section, the basal interval of the formation comprises a few metres of conglomerate and conglomeratic sandstone, which gradually fines upwards into thick-bedded, medium- to coarse-grained, strongly cross-bedded sandstone. The conglomerate clasts are pebbles, cobbles and small boulders of predominantly well-rounded sandstone and quartzite, some quartz, and subangular to angular pebbles and cobbles of chert and silicified carbonate rocks. The matrix comprises quartz-rich but somewhat lithic medium- to very coarse-grained sandstone. The upper sandstones of the formation are less conglomeratic but commonly display scattered granules (even small pebbles) and granule lags at the base of cross-bed sets (Sweet, 2017; p. 10).|
84101|Hedleys Formation|Depositional environment|Predominantly a high-energy fluvial setting, possibly with shallow-marine influence.|
84101|Hedleys Formation|Fossils|None.|
84101|Hedleys Formation|Diastems or hiatuses|None|
84101|Hedleys Formation|Relationships and boundaries|In the type section, the Hedleys Formation unconformably overlies the Doomadgee Formation (Fickling Group ). In MOUNT DRUMMOND, the unit disconformably overlies the Caulfield Formation to the north, and the Doomadgee Formation to the northeast.  The Hedleys Formation conformably underlies the Pandanus Formation with a sharp contact denoting a change from fine- to medium-grained quartz sandstone to laminated or thinly interbedded shale, siltstone and fine-grained lithic sandstone.|
84101|Hedleys Formation|Identifying features|Basal, metres-thick pebble to cobble conglomerate containing clasts of well-rounded sandstone, quartz, and quartzite. Unconformable relationship with underlying units; unconformity is angular in some areas (Sweet, 2017).|
84101|Hedleys Formation|Structure and Metamorphism|None described, except variability of dip from steep to gentle (see thickness variations).|
84101|Hedleys Formation|Age reasons|Maximum depositional ages derived from U-Pb SHRIMP dating of detrital zircons: Constance Sandstone (stratigraphically overlies Hedleys Formation): GA sample 2678595 - 1591 +/- 18 Ma (Anderson et al, 2019). Doomadgee Formation (stratigraphically underlies Hedleys Formation): GA sample 2678601- 1612 +/- 11 Ma (Anderson et al, 2019). Therefore, the potential depositional age range for the Hedleys Formation can be considered to extend from ca. 1612 +/- 11 Ma to 1591+/- 18 Ma. [NO. Hedleys Fm depositional age could still be younger than max dep age of overlying Constance Sandstone].|
84101|Hedleys Formation|Correlations|No precise correlations at the formation level are known. Given the potential depositional age range of ca. 1623 Ma to 1573 Ma, the Hedleys Formation may be correlative with components of the upper Glyde to Favenc packages (Rawlings, 1999) of the McArthur Basin.|
84101|Hedleys Formation|Alteration and Mineralisation|None known.|
84101|Hedleys Formation|Geophysical Expression|Weak to moderate magnetic response, likely due to close proximity to sandstone formations in the South Nicholson Group that display a moderate to high magnetic response due to "subtle magnetic layering", such as within the Playford Sandstone (Rawlings et al, 2008).|
84101|Hedleys Formation|Defn author|Elliot Foley, Jack Simmons, Ben Williams, Charles Verdel (Northern Territory Geological Survey), Chris Carson (Geoscience Australia) 31-MAY-2023.|
84101|Hedleys Formation|Comments|Note: Standard series 1: 100 000 and 1: 250 000 mapsheet names are shown in uppercase.|
84101|Hedleys Formation|References|Ahmad M and Wygralak AS, 1989. Calvert Hills, Northern Territory (First Edition). 1:250 000 metallogenic map series explanatory notes, Sheet SE 53-8. Northern Territory Geological Survey, Darwin, Northern Territory.  **Anderson JR, Lewis CJ, Jarrett, AJM, Carr LK, Henson P, Carson CJ, Southby C and Munson TJ, 2019. New SHRIMP U-Pb zircon ages from the South Nicholson Basin, Mount Isa Province and Georgina Basin, Northern Territory and Queensland. Geoscience Australia, Record 2019/10.  **Carson, C. J., Kositcin, N., Anderson, J. R., and Henson, P. A. in prep. A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia  -  insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences  **Carter EK, 1959. New stratigraphic units in the Precambrian of north-western Queensland. Queensland Government Mining Journal 60(92), 437-431.  **Carter EK and Öpik AA, 1960. Lawn Hill - 4-mile geological series. Explanatory notes No. 21. Bureau of Mineral Resources, Canberra.  **Grimes KG and Sweet IP, 1979. Westmoreland, Queensland (Second Edition). 1:250 000 geological map series explanatory notes, SE 54-5. Bureau of Mineral Resources, Canberra.  **Hutton LJ and Grimes KG, 1983. Lawn Hill, Queensland (Second Edition). 1:250 000 geological map series explanatory notes, SE 54-9. Bureau of Mineral Resources, Canberra.  **Rawlings DJ, 1999. Stratigraphic resolution of a multiphase intracratonic basin system: the McArthur Basin, northern Australia. Australian Journal of Earth Sciences 46(5), 703-723.  **Rawlings DJ, Sweet IP and Kruse PD, 2006. Mount Drummond, NT (Second Edition). 1:250 000 Geological Map, Sheet SE 53-12. Northern Territory Geological Survey, Darwin, Northern Territory.  **Rawlings DJ, Sweet IP and Kruse PD, 2008. Mount Drummond, NT (Second Edition). 1:250 000 Geological Map Series Explanatory Notes, Sheet SE 53-12. Northern Territory Geological Survey, Darwin, Northern Territory.  **Roberts HG, Rhodes JM and Yates KR, 1963. Calvert Hills, Northern Territory (First Edition). 1:250 000 geological map series explanatory notes, SE 53‑8. Bureau of Mineral Resources, Canberra.  **Simmons JM, Williams B, Carson, C and Verdel C, 2023a. Mount Drummond, Northern Territory 1:250 000 Geological Map, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.  **Simmons JM, Williams B, Carson, C and Verdel C, 2023b. Mount Drummond, Northern Territory 1:250 000 Geological Map Explanatory Notes, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.  **Smith JW and Roberts HG, 1963a. Mount Drummond, NT (First Edition). 1:250 000 Geological Map Series Explanatory Notes, Sheet 53-12. Bureau of Mineral Resources, Canberra.  **Smith JW and Roberts HG, 1963b. Mount Drummond, NT (First Edition). 1:250 000 Geological Map Series, Sheet SE 53-12. Bureau of Mineral Resources, Canberra.  **Sweet IP, 2017. The geology of the South Nicholson Group, northwest Queensland. Queensland Geological Record 2017/07.  **Sweet IP, Mitchell JE and Mock CM, 1981. Seigal, Northern Territory and Hedleys Creek, Queensland. 1:100 000 Geological Map Commentary. Bureau of Mineral Resources, Geology and Geophysics, Canberra.|02-OCT-23
84101|Hedleys Formation|Parent|Wild Cow Subgroup; South Nicholson Group.|
8248|Heifer Creek Sandstone Member|Name source|The name is derived from Heifer Creek in the southern Laidley Valley area in southeast Queensland.|16-MAY-23
8248|Heifer Creek Sandstone Member|Unit history|The term was first published by McTaggart (1963) but no type section was nominated and its full extent was not adequately described. The unit as redefined corresponds to the upper predominantly quartzose sandstone of McTaggart's (1963) Heifer Creek Sandstone Member, described chiefly from the southern part of the Laidley Valley and in southeast Queensland.|16-MAY-23
8248|Heifer Creek Sandstone Member|Geomorphic expression|The Heifer Creek Sandstone Member is resistant to erosion and commonly forms low but steep cliff faces, benches, and abrupt changes in hill slopes.|16-MAY-23
8248|Heifer Creek Sandstone Member|Type section locality|Reference Section: No type section was given for the Heifer Creek Sandstone Member by McTaggart (1963). Gray (1975) subsequently nominated the interval 62-315 m in GSQ Ipswich 18 as the lithological reference section for the member. This section is considered to be lithologically atypical of the member, the boundaries with adjacent units are not readily redefined, and therefore is not suitable for a type section.  Type Section: The section exposed on the Clifden-Gatton road between GR 9342. 110.265/116.316 on the Helidon 1:100 000 Sheet area (9342) is here defined as the type section.|16-MAY-23
8248|Heifer Creek Sandstone Member|Description at type locality|The Heifer Creek Sandstone Member is composed predominantly of quartz rich and some quartz lithic, medium to very coarse grained sandstone in thick to very thick beds, with steep planar cross-beds. The sandstone occurs mostly in thick fining up sequences with thin beds of granule conglomerate at the base, and grading through fine sandstone to siltstone beds at the top of the sequence. The Heifer Creek Sandstone Member is about 125 m thick in the Clifden-Gatton road section, but is about half this thickness in the southern and western parts of the basin.|16-MAY-23
8248|Heifer Creek Sandstone Member|Extent|The Heifer Creek Sandstone Member is present mainly along the western and southern flanks and central parts of the Clarence-Moreton Basin. The member has not so far been distinguished in well sections from the central part of the Clarence-Moreton Basin. The member extends almost continuously from Murphys Creek in the north, to the upper reaches of Heifer Creek, to Warwick, Koreelah Creek, Bruxner Highway, Gwydir Highway, OBX Creek, Georges Knob, Kangaroo Creek, Glenreagh and probably as far southeast as the Dirty Creek and Coast Ranges. |16-MAY-23
8248|Heifer Creek Sandstone Member|General description|REGIONAL ASPECTS: The member occurs at a progressively lower stratigraphic level in the Heifer Creek Formation from north to south. In the Clifden-Gatton road section the member occurs at the top of the Marburg Subgroup; on the Bruxner Highway near Tabulam it occurs near the middle of the Subgroup above the upper boundary of the Gatton Sandstone; at Blaxlands Flat it immediately overlies the Gatton Sandstone, and at Kangaroo Creek it is in contact with the Towallum Basalt which in turn overlies the Gatton Sandstone.|16-MAY-23
8248|Heifer Creek Sandstone Member|Depositional environment|The depositional environment is low sinuosity, fluvial, stacked channel sand deposits.|16-MAY-23
8248|Heifer Creek Sandstone Member|Fossils|Plant microfossils, including spores, pollen grains and sporadic acritarchs; non-diagnostic plant impressions and fossil wood.|16-MAY-23
8248|Heifer Creek Sandstone Member|Relationships and boundaries|Boundaries with other units are conformable. A contact with extrusives is present in the south where the Heifer Creek Sandstone Member overlies the Towallum Basalt. The Heifer Creek Sandstone Member has a variable stratigraphic position within the Koukandowie Formation (Fig. 3). It may underlie either undifferentiated Koukandowie Formation, or the Walloon Coal Measures and overlie the Gatton Sandstone, undifferentiated Koukandowie Formation or the Towallum Basalt. Some well intersections indicate an interdigitating relationship of the member with the Koukandowie Formation. The upper boundary of the member is taken as the change from predominantly light coloured, medium to coarse and very coarse grained quartzose sandstone to silty, finer grained, khaki weathered quartz-lithic sandstone of the Koukandowie Formation, or in places by the contact with dark grey to black shale, carbonaceous shale, and volcaniclastic, quartz poor, fine grained sandstone of the Walloon Coal Measures. The lower boundary is taken as the change from predominantly medium to very coarse grained quartzose sandstone to quartz-lithic, yellow brown and khaki weathered sandstone and shale of the Koukandowie Formation, or in places, quartz and quartz lithic sandstone and grey shale and siltstone of the Ma Ma Creek Member of the Koukandowie Formation.|16-MAY-23
8248|Heifer Creek Sandstone Member|Identifying features|The quartzose lithology, coarse grainsize, pebble beds, thick to very thick beds, prominent steep planar cross beds and the scarp forming habit of the member are the principal distinguishing features.|16-MAY-23
8248|Heifer Creek Sandstone Member|Age reasons|The age is late Early Jurassic on the evidence of spores and pollen grains from the member in the northern part of the basin chiefly in the Ipswich 1:250 000 Sheet area, where the member ranges in age from Toarcian to Bajocian, and contains palynofloras similar to those of the post-oolitic ironstone section of the upper Evergreen Formation, Hutton Sandstone and lower Eurombah Formation of the Surat Basin (De Jersey, 1971; McKellar, 1981). The Heifer Creek Sandstone Member occurs at different stratigraphic levels within the Koukandowie Formation, and may be time transgressive.|16-MAY-23
8248|Heifer Creek Sandstone Member|Correlations|The Heifer Creek Sandstone Member is lithologically similar to the Hutton Sandstone of the Surat Basin sequence.|16-MAY-23
8248|Heifer Creek Sandstone Member|Proposed publication|Wells A.T. et al., BMR Journal of Geology and Geophysics|16-MAY-23
8248|Heifer Creek Sandstone Member|State(s)|NSW and Qld|16-MAY-23
8264|Heliman Formation|Name source|The name is derived from Heliman Creek, which joins the Gilbert River at GR 7560-396o2935, after crossing the Heliman Formation in two placeas (around GR 7560-330245 and -303246.|16-MAY-23
8264|Heliman Formation|Unit history|Included by White (1965) in the 'Etheridge Formation', in which White noted the presence of 'black and grey quartz siltstone,...fine-grained quartz sandstone (locally silicified to quartzite), and lenses of chert,". Rossiter (1978) used the name Heliman Formation in referring to rocks conformably overlying the "Robertson River Metamorphics". The rocks to which he referred and which he illustrated were originally mapped by us as part of the Heliman Formation, but subsequent work has shown that they are part of a new unit, the Townley Formation, which underlies the Heliman Formation.|16-MAY-23
8264|Heliman Formation|Geomorphic expression|Forms rounded ridges and hills on which are commonly exposed prominent beds of siliceous siltstone/fine sandstone. These beds are also prominent on airphotographs, on which the Heliman Formation generally has a light tone, especially where the sparse vegetation cover is dominated by the almost characteristic spinifex.|16-MAY-23
8264|Heliman Formation|Type section locality|From the junction of the eastern and western branches of upper Black Gin Creek (GR 7560-252464) (bottom) southward along the western branch to GR 7560-246451.|16-MAY-23
8264|Heliman Formation|Extent|Patchy exposure from beneath Mesozoic-Tertiary cover north of the Gilbert River (around GR 7561-202880). Exposed virtually continuously from the southern bank of the Gilbert River (GR 7561-250770), south along Pinnacle Creek, then through much of the western half of North Head 1:100 000 Sheet area. Near the southern edge of Forest Home 1:100 000 Sheet area (upper Pinnacle Creek), the Formation divides into two major 'limbs'. One swings west into the Black Gin Creek area, then continues generally south and southeast, around (or in) several large-amplitude folds, into the upper Langdon River (GR 7560-136198) and Reedy Creek (-240150 areas where it is covered by :Mesozoic sediments. This 'limb' crosses the Gilbert in one place (extremity near GR 7560-420270). The eastern 'limb' swings southeast, across the Gilbert River between Green Hills outstation and Mount MacDonald, and ends in the Table top Creek area (about GR 7560-530510). A major synformal 'outlier', about 22 km long and 2-4 km wide extends from GR 7561-300540 (head of Pinnacle Creek) to the Glenrown Creek area (GR 7560-480430), south of and parallel to the eastern 'limb'. Small synclinal outliers are in the headwaters of Pinnacle Creek (GR 7561-287545) and in the lower Mosquito Creek area (GR 7560-495365).|16-MAY-23
8264|Heliman Formation|Thickness range|About 1225 m in the type section; ranges from about 800 m in the headwaters of Heliman Creek to about 1500 m along Black Gin Creek. However, thickness is difficult to estimate in many areas because of complex interfering folds..|16-MAY-23
8264|Heliman Formation|Lithology|The type section consists of lowermost (500 m) and uppermost (525 m) intervals of lithic-quartz siltstone and sandstone (70-90%) and prominent beds of very dark grey siliceous siltstone and quartzose sandstone (10-30%) which are separated by a 200 m-thick interval of siltstone and fine lithic sandstone with some carbonaceous siltstone and minor siliceous siltstone. Elsewhere in the area, micaceous and/or lithic quartzose sandstones, sandy siltstone, quartzite, phyllite, and phyllitic siltstone are common, but the very dark grey siliceous siltstone-fine sandstone remains prominent and characteristic.|16-MAY-23
8264|Heliman Formation|Relationships and boundaries|Underlain conformably by the Townley Formation, from which the Heliman Formation differs principally in the abundance and prominence in it of hard, very dark grey, 'cherty' or 'flinty' siliceous siltstone'fine sandstone. Overlain conformably by the Candlow Formation, the lowermost part of which is dominantly soft dark grey siltstone, with only very minor amounts of siliceous siltstone.|16-MAY-23
8264|Heliman Formation|Age reasons|Probably mid-Proterozoic; a minimum age of 1570+/-30 m.y. can be inferred from dating in underlying rocks of a deformation-metamorphism event (Black et al., in press) which has affected the Heliman Formation. The Formation is also intruded by granitic rocks closely similar to the type Forsayth Granite, for which a preliminary isotopic age of 1600 m.y. has been obtained (L.P. Black, pers. comm., 1978).|16-MAY-23
8264|Heliman Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
8264|Heliman Formation|Name first published by|Rossiter A.G., 1978.|16-MAY-23
79121|Highbury Basalt|Name source|From Highbury Hill, Chatsworth.|16-MAY-23
79121|Highbury Basalt|Unit history|Equivalent to Dunstan's (1911) Third Volcanic (diabase) Group.|16-MAY-23
79121|Highbury Basalt|Type section locality|Fisherman's Pocket No 1 road, west of Chatsworth, nominated by Runnegar & Ferguson (1969). Also in the Highbury hills (Photograph 37) and exposed in cuttings along the Bruce Highway between Fraser Road and the southern entrance to Spring Valley Road. Reference section: GEGM drill hole G215: 302.6-459.0 m at North Inglewood. Core held at Zillmere core library.|16-MAY-23
79121|Highbury Basalt|Extent|Pinewoods Block west of Bruce Highway. The formation then plunges southwards, to a depth of about 200 m at West Phoenix, 300 m at North Inglewood and below 18 Level (900 m deep) at Monkland Mine.|16-MAY-23
79121|Highbury Basalt|Thickness range|No drill holes have completely penetrated this unit. Is at least 200 m thick in GEGM drill hole G238 (MGA 466974mE; 7101245mN). Government stratigraphic drill hole Gympie No 2 (Mount Pleasant) bore referred to in Runnegar & Ferguson (1969) at MGA 467115mE; 7101785mN appears to have tested the top 350 m of this unit in the Monkland block (Dugdale, 2004, in E-W section along AMG-Northing 7101600mN). Drill holes at North Inglewood penetrated over 300 m.|16-MAY-23
79121|Highbury Basalt|Lithology|Pyroxene-phyric basalt, similar to the Mary Basalt but more amygdaloidal. Consists of lavas and flow breccias and may include probable spatter deposits. Typically, hematitic. Can be more magnetic than the Mary Basalt although not diagnostic.|16-MAY-23
79121|Highbury Basalt|Depositional environment|Regarded by Sivell & Waterhouse (1987) and Cranfield (1990) as the product of an island arc.|16-MAY-23
79121|Highbury Basalt|Relationships and boundaries|Base of the formation not known. Capped by the Excelsior conglomerate bed. The main outcrop in the Highbury hills is interpreted as the core of an anticline.|16-MAY-23
79121|Highbury Basalt|Age reasons|Based on their stratigraphic position Runnegar & Ferguson (1969) assigned an early Permian age to these basalts. Li et al. (2015) acknowledged that the age is poorly constrained and assumed them to be an early Permian extensional arc formed in response to an eastward trench. However, they obtained a youngest provenance age peak of ~302 Ma for detrital zircons in the overlying Dawn Formation. Therefore, there is the unproved possibility that Highbury Basalt commenced deposition in the late Carboniferous, as inferred by Dugdale (2004).|16-MAY-23
79121|Highbury Basalt|Defn author|Taken from Stidolph et al. (2016) GSQ Record 2016/05.|16-MAY-23
21962|Hiker Granodiorite|Name source|The unit is named after the Hiker gold mine (abandoned).|16-MAY-23
21962|Hiker Granodiorite|Unit history|Previously mapped as Almaden Granite (Best, 1962;  Branch, 1966;  de Keyser & Lucas, 1968) or tentatively classed as a mafic variant of the Almaden Granite (de Keyser & Wolff, 1964).|16-MAY-23
21962|Hiker Granodiorite|Geomorphic expression|The unit forms mainly prominent bouldery hilly country.  The boulders are generally covered by a black alga and the unit is characterised by medium to dark tones on aerial photographs.|16-MAY-23
21962|Hiker Granodiorite|Type section locality|The proposed type area is around GR 2490 80915, about 1 km west of Crooked Creek. The grid reference is based on the AGD66 datum.|16-MAY-23
21962|Hiker Granodiorite|Extent|The granodiorite crops out over ~1 km2, 4.5 km east of Fluorspar.|16-MAY-23
21962|Hiker Granodiorite|General description|STRUCTURE AND METAMORPHISM:: The Hiker Granodiorite is essentially massive and unmetamorphosed.MINERALISATION::  Narrow tabular gold-bearing vein and fissure-fill lodes occur in the Hiker Granodiorite not far from its contact with the Almaden Granodiorite.  The gold was concentrated in small but commonly extremely rich shoots in a kaolinite-rich gangue.|16-MAY-23
21962|Hiker Granodiorite|Lithology|The unit consists mainly of grey, medium-grained, porphyritic, augite-biotite hornblende granodiorite and hornblende-biotite granodiorite, containing rounded mafic enclaves up to 8 cm in diameter.Plagioclase and hornblende form euhedral to subhedral phenocrysts up to 3 cm long.  Rounded quartz grains up to 1 cm in diameter also occur in some samples.  There is a considerable range in grainsize and relative mineral abundances.  Plagioclase grains typically have cores of labradorite (An56), oscillatory zoned mantles of labradorite to oligoclase (An50 - An25), and rims of oligoclase (An18) (Richards, 1981).  Richards (1981) reported plagioclase core compositions ranging from An63 to An48 in different samples.  Slightly different rock types with a fluidal texture are intimately associated in places.  Richards (1981) interpreted this texture to have resulted from the mixing of two slightly different magmas, possibly related pulses, which failed to homogenise.  Rounded mafic enclaves up to about 10 cm across are common.  These have a similar mineralogy to the host granodiorite, but the minerals are present in different proportions.|16-MAY-23
21962|Hiker Granodiorite|Relationships and boundaries|The unit is inferred to intrude the Almaden Granodiorite.  Its relationship with Retchford Granite is not known.  The granodiorite intrudes the Jamtin Rhyolite and is cut by thin aplite dykes.|16-MAY-23
21962|Hiker Granodiorite|Age reasons|The Hiker Granodiorite has not been isotopically dated.  It is most probably Late Carboniferous and of similar age to the other members of the Almaden Supersuite.  It cuts the Jamtin Rhyolite which has yielded an Rb-Sr white rock-biotite age of 301 ± 11 Ma (D.E. Mackenzie, personal communication, 1992).|16-MAY-23
21962|Hiker Granodiorite|Comments|The Hiker Granodiorite is a complex heterogeneous pluton.  The presence of tabular hornblende phenocrysts up to 3 cm long is noteworthy.|16-MAY-23
21962|Hiker Granodiorite|References|BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.BRANCH, C.D., 1966:  Volcanic cauldrons, ring complexes, and associated granites of the Georgetown Inlier, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 76.DE KEYSER, F., & LUCAS, K.G., 1968:  Geology of the Hodgkinson and Laura Basins, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 84.DE KEYSER, F., & WOLFF, K.W., 1964:  The geology and mineral resources of the Chillagoe area.  Bureau of Mineral Resources, Australia, Bulletin 70RICHARDS, D.N.G., 1981:  Granitoids of the northern Tate batholith, Chillagoe, north Queensland.  Ph.D. Thesis, James Cook University of North Queensland, Townsville (unpublished).|16-MAY-23
33425|Hivesville Granite|Name source|The unit is named after the township of Hivesville where good exposures of the granite are readily accessible.|16-MAY-23
33425|Hivesville Granite|Unit history|The northern part of this body was previously mapped by Murphy & others (1976), as part of the Wigton Adamellite, whereas they mapped the southern section as part of the Boondooma Igneous Complex.  The current mapping indicates that the comparable textural and lithological characteristics of both areas require their unification as one unit.  Gradwell (1956) has also described the unit in the type area.|16-MAY-23
33425|Hivesville Granite|Geomorphic expression|The unit forms recessive bouldery terrain or low undulating heavily wooded terrain that ranges in elevation from about 320m to 400m.|16-MAY-23
33425|Hivesville Granite|Type section locality|The type area is designated as the western outskirts of the township of Hivesville around AMG 369100 7104170.  The grid reference is based on the AGD66 datum.|16-MAY-23
33425|Hivesville Granite|Extent|The unit is irregularly distributed over a roughly triangular area, extending southeasterly from the Hivesville-Proston area to the Tingoora-Durong road. The granite is exposed over an area of roughly 200 km2.|16-MAY-23
33425|Hivesville Granite|Lithology|The typical rock type of the unit is a cream to pale grey or pink, inequigranular, coarsely megacrystic biotite granite, displaying a characteristic rapakivi texture in the type area.  The matrix is commonly a quenched aggregate of fine or medium grained quartz, feldspar and biotite. In many outcrops, the quenched matrix also contains coarse rounded quartz aggregates up to 1.5cm across as well as large feldspar phenocrysts (averaging 2-3cm across).  Where quenching has not occurred, the granite ranges from coarse to very coarse in grain size, and as the phenocryst/megacryst density increases the rocks range from porphyritic to more even grained varieties (consisting of closely packed coarse feldspar crystals).  Biotite within the granites occurs as clots, disseminated flakes or sliver-like aggregates (the latter in association with mafic xenoliths) making up to 8% of the rock. The biotites are locally aligned parallel to a tectonic or flow foliation. The phenocrysts are generally composed of perthitic alkali feldspar with subordinate plagioclase.  Where a rapakivi texture is developed, the alkali feldspars are rimmed by albite containing groundmass grains (generally quartz) which locally display micrographic intergrowth textures.  Biotite flakes are associated with accessory sphene and to a lesser extent, zircon.  Accessory opaque minerals (such as magnetite) are rare, which accounts for the low magnetic response of the granite on geophysical images.  The quartz in the granites ranges from moderately strained to strongly dynamically recrystallised.  In the most intense examples, fine subgrain aggregates of dynamically recrystallised quartz anastamose around coarser relatively undeformed feldspar aggregates and phenocrysts (e.g. around AMG 368300 7106300). A significant amount of matrix recrystallisation is commonly present in rocks that appear macroscopically undeformed.Scattered mafic xenoliths (mostly porphyritic microdiorites, tonalites) are common within the granites.  At AMG 362047 7068580 tor exposure in the creek of coarse-grained k-feldspar-phyric biotite xenolithic granite cut by rare medium grained granite dyke; xenoliths of biotite and tonalite (some foliation).  Mafic dykes sporadically intrude the unit.  They are of similar composition to the xenoliths and commonly contain feldspar phenocrysts similar to those in the granite.  The mafic/felsic contacts range from knife-sharp to crenulate in nature, the latter suggesting local liquid-liquid contact of the two magmas.  At one locality (AMG 365800 7109800), the granite displays a flow foliation around a small microdiorite body.  The granite is intruded locally by dykes and small bodies of dolerite, gabbro, andesite, aplite, rhyolite and dacite. The grid references are based on the AGD Datum.|16-MAY-23
33425|Hivesville Granite|Relationships and boundaries|The Hivesville Granite is intruded by unnamed granodiorite (Rgugd, Rg3), diorite (Rgd), gabbro/diorite (Rggd), porphyritic microgranite (Rgip), and granite bodies (Rg4) of probable Triassic age.  The teardrop shaped, Permo-Triassic Stuart River Granite also probably intrudes the unit.  Tertiary sediments and basic lavas of the Main Range Volcanics overlie the granite.  The granite is locally strongly weathered and kaolinised with a well-developed Tertiary laterite capping.|16-MAY-23
33425|Hivesville Granite|Structure and Metamorphism|DEFORMATION ::  At a few localities the granite is foliated and extensively recrystallised over zones ranging from tens of metres in width to narrow mylonitic shears up to a few centimetres wide.  The foliations are mostly north to north-northwest trending and steeply dipping.  More detailed mapping is required to determine if the foliated parts of the granite can be related to distinct map-scale faults or continuous shear zones.|16-MAY-23
33425|Hivesville Granite|Age reasons|The unit at Hivesville has yielded a 274+/-28Ma Rb/Sr whole rock age and a 250.1Ma K/Ar biotite age (Webb & McDougall, 1968).  The most recent radiometric dates from the unit in this project are Ar/Ar dates on hornblende and biotite from two sites in the unit (AMG 368913, 7104100 and 366500, 7108800).  These gave age dates of 254.5 +/- 1.1 and 260.5 +/- 0.8 respectively (Vasconceles & Feng, 2000).  All these dates indicate a possible age range from Permian to Late Triassic.  The grid references are based on the AGD datum.|16-MAY-23
33425|Hivesville Granite|Comments|GEOPHYSICAL EXPRESSION:: The unit has a uniformly low magnetic response on magnetic images, and has pale to medium pink tones on the standard radiometric images.|16-MAY-23
33425|Hivesville Granite|References|GRADWELL, R.,1956, Note on the Rapakiwi Granite of the Hivesville - Proston District, Papers (University of Queensland. Department of Geology), Vol.4, no.13 (1956), p.7, Hivesville GraniteMURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.VASCONCELOS, P. & FENG, Y.,2000, 40Ar/39Ar analyses of biotite and hornblende single crystals from igneous intrusions in SE Queensalnd, Unpublished University of Queensland report.WEBB, A.W. & MCDOUGALL, I.1968, The geochronology of the igneous rocks of eastern Queensland. ,"Journal of the Geological Society of Australia., 15, 313-346.|16-MAY-23
24311|Hobble Creek Member|Name source|Hobble Creek, GR 71750E 87000N Rosedale 1:100 000 Sheet area.|16-MAY-23
24311|Hobble Creek Member|Unit history|Part of the Lowmead Beds of Cribb, 1960; Mack, 1972; and Ellis & Whitaker, 1976.|16-MAY-23
24311|Hobble Creek Member|Type section locality|From 25.7 m to 47.2 m in drill hole LDD 16 (GR 69066E 94908N Miriam Vale 1:100 000 Sheet area). This interval is part of the type section of the Lowmead Formation. The rock type is reddish-brown, sandy claystone. The upper boundary is the contact between green claystone of the Harpur Creek Member and red sandy claystone. The lower boundary is an unconformity with igneous rocks.|16-MAY-23
24311|Hobble Creek Member|Description at type locality|The sandy claystone is reddish-brown, massive with green mottling in part. There are lateral variations within the member to red clayey sandstone and white clayey sandstone to sandstone (in beds up to 14 m thick).|16-MAY-23
24311|Hobble Creek Member|Extent|Identified from drill core only.|16-MAY-23
24311|Hobble Creek Member|Thickness range|21.5 m in type section; true thickness unknown. The member ranges in thickness from 2.3 m to 40 m.|16-MAY-23
24311|Hobble Creek Member|Relationships and boundaries|The Hobble Creek Member unconformably overlies igneous rock of the Miriam Vale Granodiorite and Agnes Waters Volcanics (Ellis & Whitaker, 1976). It is conformably overlain by the Hobble Creek Member [?Harpur Member?] of the Lowmead Formation. The boundary being the contact between red (Hobble Creek Member) and green rock types. The member is contained within the Lowmead Graben and has been identified in cored drill holes LDD 1, LDD 16 and CRAE rotary drill holes (Mack, 1972).|16-MAY-23
24311|Hobble Creek Member|Age reasons|Early Tertiary - as for the Lowmead Formation.|16-MAY-23
24311|Hobble Creek Member|Defn author|McConnochie M.J., Henstridge D.A., 1985.  86/25154. Briefly described P.208.|16-MAY-23
24311|Hobble Creek Member|Comments|Note: Drill core of LDD 16 is stored at Southern Pacific Petroleum's Research and Core Storage facility in Gladstone, Queensland.|16-MAY-23
8404|Hodgkinson Formation|Lithology|Labile arenite, mudstone; minor chert, metabasalt, conglomerate, conglomeratic arenite, quartzose arenite, siltstone, hematitic mudstone, shale, ferruginous chert, (andalusite-) mica schist, phyllite; rare limestone, cordierite-bearing hornfels; calc-silicate rocks, talc-carbonate schist|16-MAY-23
35064|Hodgon Granodiorite|Name source|Hodgon Creek, a tributary of Dillon Creek which it joins at Top Dillon Mill at GR 3809 77810.  The grid reference is based on the AGD66 datum.|16-MAY-23
35064|Hodgon Granodiorite|Unit history|The Hodgon Granodiorite was previously mapped as Lolworth Igneous Complex by Wyatt & others (1971), Clarke & Paine (1970).|16-MAY-23
35064|Hodgon Granodiorite|Type section locality|At GR 3565 77761 in the Homestead 1:100 000 Sheet area, about 2km west of Hodgon yards.  The grid reference is based on the AGD66 datum.|16-MAY-23
35064|Hodgon Granodiorite|Description at type locality|Here a white to grey, medium grained, hornblende-biotite, granodiorite is intruded by dykes of medium grained biotite granite and layered garnet leucogranite sheets/dykes. The granodiorite comprises quartz, plagioclase, poikilitic K-feldspar, biotite, hornblende, sphene and opaques. The granodiorite at the type locality is lithologically and magnetically similar to Late Silurian granitoids in the Ravenswood Batholith to the east and different to the granites of the Amarra and Grasstree Suites which make up the bulk of the Lolworth Batholith.|16-MAY-23
35064|Hodgon Granodiorite|Extent|The Hodgon Granodiorite crops out over only about 6-8km2 north of Barrington homestead (Figure 2). However much of this area is covered by Tertiary to Quaternary Campaspe Formation. The presence of zircons of similar age and morphology in dyke rocks from about 1km northeast of Barrington station suggests that the unit may occur over about 30-40km2 north of Barrington homestead.|16-MAY-23
35064|Hodgon Granodiorite|Lithology|Only a few fresh outcrops of the Hodgon Granodiorite have been found as much of the potential area of outcrop is covered by Tertiary sediments. About 10km southeast of the type area, medium grained biotite granodiorite is also assigned to this unit. The biotite granodiorite comprises quartz, plagioclase, minor K-feldspar, and recrystallised biotite which indicates that this unit may be older than the Amarra suite. It is possible that the biotite granite intruding the hornblende-biotite granodiorite at the type locality may belong to the Amarra Suite.|16-MAY-23
35064|Hodgon Granodiorite|Relationships and boundaries|The relationship of the Hodgon Granodiorite to the Reedybed Granite is uncertain. However the Hodgon Granodiorite is older than the Amarra Granite and may also be older than the Reedybed Granite.|16-MAY-23
35064|Hodgon Granodiorite|Age reasons|SHRIMP microprobe dating of zircon from the Hodgon Granodiorite and yielded a 206[superscript]Pb/238[superscript]U age of 414 +/- 5 Ma, and this is interpreted as the crystallisation age of the granitoid (Fanning 1995). One grain yielded a 207[superscript]Pb/206[superscript]Pb age of about 800 Ma, which is interpreted as an inherited age.|16-MAY-23
35064|Hodgon Granodiorite|Comments|MAGNETIC SUSCEPTIBILITY::  Magnetic susceptibilities in the type area are 963-1550 x 10-5 SI units. Away from the type locality, susceptibilities are 175-326 x 10-5 SI units.|16-MAY-23
35064|Hodgon Granodiorite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
35062|Hodgon Suite|Constituents|Includes the Hodgon Granodiorite and the Goldsborough Granodiorite.|16-MAY-23
35062|Hodgon Suite|Lithology|Hornblende-biotite granodiorites.|16-MAY-23
35062|Hodgon Suite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
8421|Holborn Granodiorite|Name source|Name is derived from the Parish of Holborn, County of Wilkie Gray.|16-MAY-23
8421|Holborn Granodiorite|Unit history|The name Holborn Granodiorite is herein given to two masses north of Ponto Hut.|16-MAY-23
8421|Holborn Granodiorite|Geomorphic expression|Outcrop is generally poor, and restricted to weathered outcrop in gullies.  The main exception are rocky hills in the vicinity of the reference locality.  Fresh exposures also occur in the bed of the Little Star River (North Branch) in the southern mass, such as at the type locality.  The unit generally forms subdued topography which contrasts with the hillier topography of the Argentine Metamorphics in this area.  The unit has paler tones on aerial photographs.|16-MAY-23
8421|Holborn Granodiorite|Type section locality|The type locality is designated in the bed of the north branch of the Little Star River at 8159-230751 where grey, medium to coarse-grained, equigranular, muscovite-biotite granodiorite to tonalite crops out.  A reference locality for the northern mass is just east of the Townsville-Ravenshoe power line at 8159-210787, where grey, fine to medium-grained, equigranular biotite-muscovite granodiorite forms a treeless hill.  The grid reference is based on the AGD66 datum.|16-MAY-23
8421|Holborn Granodiorite|Extent|Holborn Granite forms  two masses north of Ponto Hut.  The largest, in the upper reaches of Black Fellow Creek and its tributaries, is about 25 km2 in area, although it has only been examined south of Blackfellow Creek, mainly adjacent to the Townsville-Ravenshoe powerline.  Its northern extent is based solely on airphoto interpretation.  The other mass, in the middle reaches of the north and south branches of the Little Star River, is about 10 km2.  The plutons are separated by a narrow belt of Argentine Metamorphics.  The unit was not recognised by previous mapping (Wyatt & others, 1970).  Its name is derived from the Parish of Holborn, County of Wilkie Gray.|16-MAY-23
8421|Holborn Granodiorite|Lithology|The southern mass consists of grey, foliated, medium to coarse-grained muscovite-biotite granodiorite to tonalite.  Regular-sided veins of muscovite pegmatite up to 1 m wide with sharp contacts cut the granodiorite in places.  No xenoliths were observed.  The foliation is generally defined by alignment of biotite, but in places the fabric is best described as a lineation rather than a foliation, and is defined by alignment of quartz.  In thin section, the quartz (30%) forms aggregates up to 1 cm of strained subgrains with highly sutured margins.  Plagioclase (40-50%) is oligoclase and occurs as subhedral, subequant grains, generally 1-3 mm across.  Microcline (<10 %) is present as anhedral, interstitial grains <1 mm.  Plagioclase shows myrmekitic replacement adjacent to microcline grains.  Biotite (15%) forms clusters of reddish brown, partly chloritised flakes up to 3 mm long.  They are deformed and commonly crosscut by muscovite flakes up to 1.5 mm long.  Muscovite (5%) also forms discrete flakes up to 3 mm across.  The northern mass is generally finer grained and more muscovite-rich.  It consists mainly of well-foliated, grey, fine to medium-grained, biotite-muscovite granodiorite.  The foliation is defined by the alignment of quartz aggregates and mica flakes.  In thin section, quartz (30%) forms aggregates up to 3 mm of subequant subgrains.  Plagioclase (40-50%) is Na-andesine, commonly showing oscillatory zoning, and occurs as subequant, subhedral grains 0.5-1 mm across.  Interstitial microcline (<10%) is associated with myrmekitic replacement of plagioclase.  Muscovite (5-10%) commonly forms large flakes up to 5 mm across, and also smaller flakes cutting across biotite flakes.  Biotite (5%) flakes are reddish brown and up to 1 mm; they are locally chloritised.  Garnet occurs in some outcrops (for example 210802) as pink, embayed, euhedral crystals up to 2 mm in diameter.  As described, the northern mass is somewhat different to the southern mass, and with further mapping could possibly be assigned to a separate unit.  However, the two are grouped at this stage, because both are muscovite-bearing, have similar geochemistry, and the full range of rock-types in both masses is not yet known.  The foliation in both masses strikes approximately east-west.|16-MAY-23
8421|Holborn Granodiorite|Relationships and boundaries|The Holborn Granodiorite intrudes the Argentine Metamorphics (Subunits PLa[subscript]s).  It is overlain to the west by the Late Devonian to Carboniferous Keelbottom Group (formerly Star beds) and Ponto Basalt Member of the Carboniferous Tareela Volcanics.  To the east it is overlain by and faulted against Carboniferous ignimbrites of the St Giles Volcanics.  Large dykes of microgranite intrude the granodiorite along the contact with the ignimbrite, and plugs of rhyolite also intrude it.  No isotopic data are available on this unit either, and its age is therefore uncertain.  However, it is likely to be in the range Ordovician to Early Devonian like most of the components of the Ravenswood and Lolworth Batholiths in the southern part of the province (Hutton & others, 1990b).|16-MAY-23
25952|Humpy Creek Member|Name source|Humpy Creek; GR 307,500E, 7,370,000N Gladstone 1:100 000 topographic sheet.|16-MAY-23
25952|Humpy Creek Member|Unit history|Part of The Narrows Beds (Kirkegaard et al, 1970) and part of the Rundle Formation (Henstridge and Missen, 1982).|16-MAY-23
25952|Humpy Creek Member|Type section locality|23 m of oil shale and carbonaceous shale with lesser interbeds of claystone, minor impure discontinuous dolomite and rare siderite concentrations, from 120.3 to 143.3 m in drill hole ERD 169 (GR 300,999E, 7,380,998N Gladstone 1:100 000 topographic sheet. The dark yellowish-brown to dusky yellowish-brown oil shale contains two major very dark grey carbonaceous shale beds (from 125.0 to 126.0 m and 142.3 to 143.3 m in type section) and two dusky green claystone beds (from 120.3 to 120.9 and 126.0 to 127.1 m in type section). Minor greenish-grey claystone to clayey oil shale beds and impersistent carbonaceous shale layers are also interbedded with the oil shale. Minor yellowish grey impure dolomite and rare greyish-yellow siderite concentrations are recorded. Cyclicity of lithologies is a feature with oil shale grading upwards through clayey oil shale, commonly overlain by carbonaceous material. The unit is characteristically carbonaceous and generally non-calcareous.|16-MAY-23
25952|Humpy Creek Member|Extent|Subcrops in an area of about 39 km2 in The Narrows Graben, NW of Gladstone, Queensland. The member has been identified from drill hole core.|16-MAY-23
25952|Humpy Creek Member|Thickness range|23 m (estimated true thickness 22.7 m corrected for an apparent dip o 9o in ERD 169) in type section. Range of true thickness of the member as intersected in drill holes is 9.7 m to 29.7 m.|16-MAY-23
25952|Humpy Creek Member|Lithology|Oil shale, dark yellowish-brown to dusky yelllowish-brown brecciated, rarely peloidal, poorly laminated to well laminated in part; very thinly to very thickly bedded (up to 3 m); carbonaceous and clayey cyclicity. Lesser thick to very thick interbeds of very dark grey carbonaceous shale and dusky green carbonaceous claystone; ;minor yellowish-grey impure dolomite and rare greyish-yellow siderite concentrations. From north to south in The Narrows Graben there is a marked increase in carbonaceous content. Ostracode tests are sporadically recorded in the oil shale with minor gastropods, vertebrate remains (crocodile, turtle), fish elements and coprolites. There are abundant plant remains within the persistent basal carbonaceous shale bed.|16-MAY-23
25952|Humpy Creek Member|Relationships and boundaries|The member is conformable with the underlying Brick Kiln Member and is the sharp contact between carbonaceous shale and oil shale. The upper boundary is the conformable, sharp contact between carbonaceous claystone and oil shale. The Member is faulted against Devonian to Carboniferous rocks of the Curtis Island Group along the western edge of The Narrows Graben.|16-MAY-23
25952|Humpy Creek Member|Age reasons|Mid to late Eocene - as for the Rundle Formation.|16-MAY-23
25952|Humpy Creek Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
25952|Humpy Creek Member|Comments|Note:  Drill-core from ERD 169 is stored at Southern Pacific Petroleum's Research and Core Storage Facility located in Gladstone, Queensland.|16-MAY-23
8599|Hurleys Metamorphics|Name source|Hurleys Diggings, the name of an area of old alluvial gold workings, centred about 18 km northwest of Clermont. Hurleys dam is at 8352-506889.|16-MAY-23
8599|Hurleys Metamorphics|Unit history|Previously mapped as Anakie Metamorphics (Malone & others, 1964; Veevers & others, 1964a, b) and now part of the Anakie Metamorphic Group.|16-MAY-23
8599|Hurleys Metamorphics|Geomorphic expression|The Hurleys Metamorphics generally form undulating topography with local strike ridges formed by quartzite. Overall the unit is more resistant and more densely wooded than the adjacent Scurvy Creek Meta-arenite. It has a low magnetic response similar to most of the other metasedimentary units and its radiometric response is also not particularly distinctive.|16-MAY-23
8599|Hurleys Metamorphics|Type section locality|Cuttings along the northern side of the Blair Athol rail loop from 8452-538926 to 522920. The grid references are based on the AGD66 datum.|16-MAY-23
8599|Hurleys Metamorphics|Description at type locality|Strongly folded, white, mainly fine-grained, foliated quartzite and green to grey phyllite are well exposed in the cuttings. Exposures of Permian breccia and claystone occur in two cuttings in the loop, but these are easily distinguished from metamorphic rocks.|16-MAY-23
8599|Hurleys Metamorphics|Extent|Two separate parallel belts of metamorphic rocks up to 5 km wide, extending for about 30 km north-northwest from the Clermont-Laglan road, and separated by a belt of Scurvy Creek Meta-arenite. A third, poorly exposed belt containing quartzite, about 10 km southeast of Blair Athol in the Apsley Creek area, is tentatively assigned to the unit.|16-MAY-23
8599|Hurleys Metamorphics|Lithology|Similar to the Monteagle Quartzite and the quartzite-rich facies of the Bathampton Metamorphics, but of lower metamorphic grade. White quartzite is interlayered with grey to greenish grey phyllite or fine-grained mica schist and slate. The metamorphic grade is greenschist facies (chlorite to biotite zone).|16-MAY-23
8599|Hurleys Metamorphics|Relationships and boundaries|The Hurleys Metamorphics structurally underlie a belt of Scurvy Creek Meta-arenite that crops out to the west, the same relationship as between the Monteagle Quartzite and Wynyard Metamorphics. However, another belt of Scurvy Creek Meta-arenite to the east apparently structurally underlies the Hurleys Metamorphics. The reason for this repetition is not certain. It could be due to thrusting or to an overturned F2 antiform, of which the Hurleys Metamorphics represent the core. The Hurleys Metamorphics crop out east of the second belt of Scurvy Creek Meta-arenite, again either by thrust repetition or an F2 synform.   Farther east again, in the Apsley State Forest, the Hurleys Metamorphics are bounded by a belt of metapelitic rocks that contain some greenstone and have thus been equated with the Bathampton Metamorphics. The exposure in this area is very poor, and there is little structural data available, so that the relationships are not known.   The Hurleys Metamorphics are unconformably overlain by the Permian sediments of the Blair Athol Coal Measures, Tertiary basalt, and unassigned Cainozoic superficial deposits.|16-MAY-23
8599|Hurleys Metamorphics|Age reasons|The original age is still uncertain, but is probably Early Cambrian or Neoproterozoic.|16-MAY-23
8599|Hurleys Metamorphics|References|MALONE, E.J., CORBETT, D.P.W., & JENSEN, A.R., 1964: Geology of the Mount Coolon 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 64.VEEVERS, J.J., RANDAL, M.A., MOLLAN, R.G., & PATEN, R.J., 1964a: The geology of the Clermont 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report, 66.VEEVERS, J.J., MOLLAN, R.G., OLGERS, F., & KIRKEGAARD, A.G., 1964b: The geology of the Emerald 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 68.|16-MAY-23
24314|Idalia Rhyolite|Name source|The name is derived from the Now-abandoned 'Idalia' homestead, near the Croydon-'Esmeralda' road, at GR 7461-656585, and close to the type section.|16-MAY-23
24314|Idalia Rhyolite|Unit history|The Idalia Rhyolite forms part of the undivided 'Croydon Felsite', later 'Croydon Volcanics' of White (1959, 1965) and Branch (1966); see also definition of Croydon Volcanic Group. It was informally named 'Idalia rhyolite' and described by Mackenzie (1983).|16-MAY-23
24314|Idalia Rhyolite|Geomorphic expression|The Idalia Rhyolite is characterised by moderately steep, rugged, and mostly very bouldery terrain with a medium grass cover and sparsely scattered, low trees. The tone on airphotos is very pale, and on many hillsides, numerous step-like breaks in slope, which represent boundaries of ignimbrite flow sheets, are visible. |16-MAY-23
24314|Idalia Rhyolite|Type section locality|The type section extends eastward from GR 7461-661583 on Nonda Creek near 'Idalia', along the northern side of the creek to 0674577, thence east-northeast to -683580, and northeast to -688586 (crest of ridge). This section consists of about 200 m of greenish to bluish-grey, medium-grained, moderately crystal-rich rhyolitic ignimbrite in about 20 separate flow sheets. The base of the section is a contact with Tertiary sediments, close to an intrusive contact with Nonda Granite. The top of the section is the stratigraphically highest ignimbrite flow unit preserved in the area; the top of the Idalia Rhyolite is probably not preserved. A useful reference section is along the Croydon-'Tabletop' road, between 7361-335972 (lower conformable(?) contact with Carron Rhyolite) and 366012 (upper, faulted contact with Caron Rhyolite), in which is exposed about 250 m of typical, greenish-grey, moderately crystal-rich rhyolitic ignimbrite.|16-MAY-23
24314|Idalia Rhyolite|Extent|The Idalia Rhyolite crops out over about 2500 km2 (over 80% of the outcrop area of the Croydon Volcanic Group), extending almost continuously in a 110 km-long, arcuate belt from south of the Carron River (between 18o and 18o09'S) to the Yappar River (18o59'S). This belt is 30-40 km wide over most of its length, but narrows to about 12 km at its southern end. In the Croydon area, several eastward-tilted, elongated blocks have been isolated from the main outcrop area by normal faults along their eastern sides. The largest, to the east and northeast of Croydon, is 30 km long and up to 15 km wide; a second, north of Croydon, is 17 km long and up to 8 km wide. A third block, 5 km by 1 km, forms the Surrey Hills, 7 km southeast of Croydon, and the fourth fault block, 15 km southeast of Croydon, is 9 km by 2 km.|16-MAY-23
24314|Idalia Rhyolite|Thickness range|Because the top of the Idalia Rhyolite is almost certainly not preserved at any location, original thickness cannot be estimated with any certainty. Thickness as exposed is about 100 m over much of the area, and ranges from about 40 to 60 m in the south and west to about 150 m between Maitland and Three X Creeks. A thickness of 250 m is estimated for the fault block northeast of Croydon, but this may be affected by folding, or faulting, or both.|16-MAY-23
24314|Idalia Rhyolite|Lithology|The Idalia Rhyolite is made up of medium greenish to bluish-grey, moderatley crystal-poor to moderately crystal-rich rhyolitic ignimbrite, which is variably altered and recrystallised. It contains 10-25% (typically 15-20%) crystals, including about 1% biotite and, in some rocks, a trace of garnet, ranging from less than 0.5 mm up to 3-4 mm. Most rocks contain a small amount of graphite (up to 1%), mostly aggregated into rounded 'pellets' up to 1 cm in diameter. Eutaxitic foliation, defined by fiamme ranging from a few mm long to several cm long and about 1 cm thick, are present in some rocks, mostly from near the top or the bottom of the unit.|16-MAY-23
24314|Idalia Rhyolite|Relationships and boundaries|The Idalia Rhyolite overlies apparently conformably, the Carron Rhyolite, which is finer-grained, markedly less crystal-rich, and commonly displays pseudo flow banding, or, more rarely, true flow banding/lamination. It appears to grade westward and stratigraphically downward into the darker, more mafic, and more intensely recrystallised Democrat Rhyolite Member. The unit is intruded by the Middle Proterozoic Esmeralda, Nonda, Mooremount, Macartneys and Olsens Granites, the Permian Awring Granodiorite, and the Permian? Wallys Dolerite. It is unconformably overlain by the Middle to Late Proterozoic Inorunie Group, the Mesozoic Eulo Queen Group, Gilbert River Formation, and Wallumbilla Formation, the Late Cretaceous to Tertiary Bulimba Formation, and a variety of Cainozoic fluviatile and residual deposits.|16-MAY-23
24314|Idalia Rhyolite|Age reasons|The Idalia Rhyolite, together with its component member, the Democrat Rhyolite Member, and the Carron Rhyolite haave been isotopically dated at 1400+/-75 Ma (Richards & others, 1966; Black, 1973).|16-MAY-23
24314|Idalia Rhyolite|Defn author|Mackenzie D.E., Henderson G.A.M., Warnick J.V., Bain J.H.C., 1985. 86/25125. Mention Map legend.|16-MAY-23
24314|Idalia Rhyolite|Proposer|Mackenzie D.E., Warnick J.V., Henderson G.A.M.|16-MAY-23
8773|Iron Hut Quartz Monzonite|Name source|Iron Hut Creek that flows into Theresa Creek at 8452-568590.   The grid reference is based on the AGD66 datum.|16-MAY-23
8773|Iron Hut Quartz Monzonite|Geomorphic expression|The terrain is gentle to moderately undulating. Tors such as Mount Pleasant, Mount Livingstone, and Mount Hammond dominate the south of the pluton. Elsewhere, isolated boulder-sized outcrop is common.  The Iron Hut Quartz Monzonite has a yellow-orange hue on the Landsat 5 TM 1-4-7 (BGR) image where it is not concealed by purple-coloured Cainozoic cover. The area is only partly cleared, and the pluton is characterised by areas of low, and moderate to high relief. The Iron Hut Quartz Monzonite is very strongly magnetic, and has low to weak Th anomalies, strong K response, and patchy U response.|16-MAY-23
8773|Iron Hut Quartz Monzonite|Type section locality|The quarry near at 8452-572786 Theresa Creek Dam. Grey, fine to medium-grained, equigranular hornblende-biotite quartz monzonite is exposed, and is locally intruded by dykes of dark grey porphyritic micromonzonite. Complex crenulate contacts to the dykes suggest that the quartz monzonite was still partly molten when the dykes were emplaced.  The grid reference is based on the AGD66 datum.|16-MAY-23
8773|Iron Hut Quartz Monzonite|Description at type locality|Grey, fine to medium-grained, equigranular hornblende-biotite quartz monzonite is exposed, and is locally intruded by dykes of dark grey porphyritic micromonzonite. Complex crenulate contacts to the dykes suggest that the quartz monzonite was still partly molten when the dykes were emplaced.|16-MAY-23
8773|Iron Hut Quartz Monzonite|Extent|A large irregular body 60km2 in area, centred on Theresa Creek Dam.|16-MAY-23
8773|Iron Hut Quartz Monzonite|Lithology|Grey, fine to medium-grained, equigranular to porphyritic hornblende-biotite quartz monzonite and pink to grey, fine to medium-grained porphyritic micromonzonite.|16-MAY-23
8773|Iron Hut Quartz Monzonite|Relationships and boundaries|The Iron Hut Quartz Monzonite intruded and hornfelsed the Early to Middle Devonian Theresa Creek Volcanics and is unconformably overlain by the Late Devonian to Early Carboniferous Silver Hills Volcanics, which separate it from the Sunny Park Granodiorite. Its relationship to the Stevenson Quartz Monzodiorite is unknown. Several small plugs of Tertiary Hoy Basalt intrude the southern part of the unit.|16-MAY-23
8773|Iron Hut Quartz Monzonite|Age reasons|The precise age is uncertain, but because of its relationships to the Theresa Creek Volcanics and Silver Hills Volcanics and similarity to the Stevenson Quartz Monzodiorite a Devonian age has been assigned.|16-MAY-23
8773|Iron Hut Quartz Monzonite|References|REFERENCESDARBY, F. 1969: North Bowen Basin gravity survey, Queensland 1963. Bureau of Mineral Resources, Australia, Report 138.FORDHAM, B.G., 1992: Chronometric calibration of mid-Ordovician to Tournaisian conodont zone: a compilation from recent graphic-correlation and isotope studies. Geological Magazine, 129, 709-721.OLGERS, F., 1968: Emerald, Queensland - 1:250 000 Geological Series. Bureau of Mineral Resources, Australia, Explanatory Notes SF55-15.OLGERS, F., 1969: Clermont, Queensland - 1:250 000 Geological Series. Bureau of Mineral Resources, Australia, Explanatory Notes SF55-11.STEIGER, R.H. & JAGER, E., 1977: Subcommission on geochronology; convention on the use of decay constants in geo- and cosmochronology. Earth and Planetary Science Letters, 36, 359-362.VEEVERS, J.J., RANDAL, M.A., MOLLAN, R.G. & PATEN, R.J., 1964a: The geology of the Clermont 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 66.VEEVERS, J.J., MOLLAN, R.G., OLGERS, F. & KIRKEGAARD, A.G., 1964b: The geology of the Emerald 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 68.WEBB, A.W., COOPER, J.A. & RICHARDS, J.R., 1963: K-Ar ages on some Central Queensland granites. Journal of the Geological Society of Australia, 10, 317-324.WEBB, A.W. & MCDOUGALL, I., 1968: The geochronology of the igneous rocks of Eastern Queensland. Journal of the Geological Society of Australia, 15, 313-346.WITHNALL, I.W., BLAKE, P.R., CROUCH, S.B.S., TENISON-WOODS, K., HAYWARD, M. & HUTTON, L.J., 1993: Geological mapping of the southern Anakie Inlier, central Queensland - progress report. Queensland Government Mining Journal, 94.|16-MAY-23
27085|Jack Formation|Name source|Jack Hills, a ridge of limestone north of the Broken River.  The ridge was named after geologist R.L. Jack by White (1959), and appears on the Clarke River 1.250 000 1st edition geological sheet.|16-MAY-23
27085|Jack Formation|Unit history|The unit was previously defined as the Jack Limestone Member of the Graveyard Creek Formation (now Group) (White, 1959, 1962, 1965).  It was given formation status by Withnall & others (1988), but not formally redefined.|16-MAY-23
27085|Jack Formation|Geomorphic expression|The unit forms a broad ridge, the Jack Hills , which consist of two lines of prominent limestone bluffs and outcrops with typical karst features, and which are readily discernible on aerial photographs.  Only one line of outcrops occurs northeast of Gorge Creek.|16-MAY-23
27085|Jack Formation|Type section locality|Jack Hills Gorge on the Broken River, between 7859 660453 and 655455, where  580 m of limestone (in two main lenses at the top and bottom of the section), arenite, and mudstone as described below are exposed.  See Fleming (1987) and Withnall & others (1988, figure 27, 81, and 82, and pages 152-155) for more details.  The grid references are based on the AGD66 datum.|16-MAY-23
27085|Jack Formation|Extent|Interfolded with the Poley Cow and Shield Creek Formations in a belt about 20 km long from the headwaters of Back and Poley Cow Creeks to Storm Dam and Dosey Creek.|16-MAY-23
27085|Jack Formation|Thickness range|580 m in the type section, thinning to the south.  The limestone lenses out both to the south and north, but in the north the siliciclastic rocks probably maintain the overall thickness.|16-MAY-23
27085|Jack Formation|Lithology|Limestone, micaceous labile arenite, pebbly quartzose arenite, and mudstone. Limestone in large lenses is thick to very thick-bedded or unbedded and massive. Local oolites and oncolites in some small lenses.  Arenites are generally thick bedded and locally cross bedded.  Further lithological details included in the Relationships section..|16-MAY-23
27085|Jack Formation|Fossils| A locally rich fauna of favositid, heliolitid, and rugose corals, stromatoporoids, brachiopods, trilobites, and very rare conodonts indicates a Ludlow to early Lochkovian age.  See Withnall & others (1988) for more details.|16-MAY-23
27085|Jack Formation|Relationships and boundaries|The unit conformably or possibly disconformably overlies the Poley Cow Formation, and locally unconformably overlies the Judea Formation.  It is disconformably(?) overlain by the Shield Creek Formation, and locally by the Storm Hill Sandstone.  In the type area and adjacent area, the large limestone lenses at the top and base distinguish the unit.  These lens out to the south and north.  To the north, discontinuous lenses of quartzose arenite and conglomerate mark the base of the unit.  Arenites within the unit are generally more micaceous than in the Poley Cow Formation.  The overlying units consist of coarse-grained feldspathic and quarzose arenite.|16-MAY-23
27085|Jack Formation|Age reasons|A Ludlow to early Lochkovian age is indicated by the fossil record (see section above).  See Withnall & others (1988) for more details.|16-MAY-23
27085|Jack Formation|References|WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4. Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. **WHITE, D.A., 1962:  Clarke River 1.250 000 Geological series.  Bureau of Mineral Resources, Australia, Explanatory Notes, E/55-13.  **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
26308|Jayah Creek Metabasalt|Name source|Named after Jayah Creek, whose tributaries drain part of the northern outcrop area, Ardmore 1:100 000 Sheet area (Urandangi 1:250 000 Sheet area).|16-MAY-23
26308|Jayah Creek Metabasalt|Unit history|Mapped as Eastern Creek Volcanics by Noakes & others (1959), and described by Joplin (1955; page 38) as an 'older metamorphic complex'. Extensions to the north in the Oban 1:100 000 Sheet area have been mapped as Eastern Creek Volcanics.|16-MAY-23
26308|Jayah Creek Metabasalt|Type section locality|From GR 291069 to GR 343114, about 17 km NW of Dajarra, Ardmore 1:100 000 Sheet area. The old main road between Dajarra and Mount Isa via Sulieman Bore and an abandoned railway track cross the western part of the type section. A complete section from the base to the top of the sequence is not exposed. The formation (including the Timothy Creek Sandstone Member) in the type section consists mainly of foliated to schistose fine-grained amygdaloidal and massive metabasalt, and numerous interlayered lenses of quartzose, sericitic and feldspathic meta-arenite and quartzite, glassy or epidotic quartzite, and muscovite quartzite. Minor rock types include recrystallised limestone, muscovite schist, and quartz-biotite schist. The Timothy Creek Sandstone Member is a relatively thick unit of mainly pebbly meta-arenite.|16-MAY-23
26308|Jayah Creek Metabasalt|Extent|The sequence forms a NNW-trending belt in the central part of the Ardmore 1:100 000 Sheet area. It extends S and N into the Glenormiston 1:250 000 and Oban 1:100 0000 Sheet areas respectively.|16-MAY-23
26308|Jayah Creek Metabasalt|Thickness range|The thickness of the sequence is unknown; it appears to be about 6200 m thick in the type section, and has an apparent maximum thickness of about 15 000 m, 20.5 km SW of Dajarra.|16-MAY-23
26308|Jayah Creek Metabasalt|Lithology|Mainly foliated to schistose, fine-grained, amygdaloidal and massive meta-basalt, fine to medium-grained amphibole schist, quartz + muscovite + biotite +/- feldspar +/- cordierite schist and gneiss, quartzite, muscovite quartz, and quartzose, sericitic, and feldspathic meta-arenite and quartzite. Minor rock types include para-amphibolite, siliceous and micaceous metasiltstone, pebbly labile meta-arenite and quartzite, recrystallised limestone, quartz-muscovite-biotite rock (at GR 299858) containing numerous cordierite poikiloblasts, calcareous meta-arenite, laminted biotite-rich rocks (?mafic tuffs) and conglomerate (rare). The sequence is characterised by numerous metasedimentary units, interlayered with the metabasalts and ranging in thickness from less than 1 m up to about 2000 m (Timothy Creek Sandstone Member). In the NW argillaceous metasediments are very common, whereas in the central and southern parts of the belt arenaceous and ?tuffaceous metasediments are relatively common.|16-MAY-23
26308|Jayah Creek Metabasalt|Relationships and boundaries|The Jayah Creek Metabasalt is truncated by the Wonomo Fault in the east and by the Rufus Fault Zone in the west. The contact between Jayah Creek Metabasalt and Sulieman Gneiss about 23 km SW of Dajarra appears to be gradational. However, coarse chlorite rock developed in the Sulieman Gneiss in places adjacent to this contact may indicate that the contact is faulted. Alternatiavely, the chlorite is generally closely associatead with northerly trending pegmatite veins and its formation may have been related to the intrusion of the pegmatites (which may or may not have been intruded along a fracture zone separating the two formations). The formation may be unconformably overlain by a poorly exposed sequence of relatively unmetamorphosed meta-arenite, metasiltstone, and shale, tentatively assigned to the Mount Isa Group, about 6 km W of Rundle Bore (GR 391829). It is unconformably overlain by flat-lying to gently dipping Middle Cambarian and ?Mesozoic sediments in the S. The sequence is cut by numerous pods and dykes of metadolerite, by granite mapped as part of the Sybella Granite batholith, and by numerous veins of quartz, and quartz+feldspar+muscovite+/-tourmaline pegmatite. The formation is also cut by thin (<20 m) dykes of quartz porphyry, and quartz-feldspar porphyry.|16-MAY-23
26308|Jayah Creek Metabasalt|Age reasons|Precambrian, probably Proterozoic.|16-MAY-23
26308|Jayah Creek Metabasalt|Proposed publication|Blake  & others, in preparation.|16-MAY-23
26308|Jayah Creek Metabasalt|Comments|Remarks: The regional metamorphic grade increases from east to west and may possibly be attributed to relatively low-pressure high-temperature metamorphism associated with the emplacement of the Sybella Granite batholith. The presence of cordierite in argillaceous metasediments in the western part of the belt indicates amphibolite facies of regional metamorphism (Winkler, 1976). Joplin (1955) recorded cordierite, andalusite, and sillimanite in a gneiss collected a few metres west of the old Dajarra Mount Isa road, about 10.5 km NW of Sulieman Bore (GR 323027). The metamorphic grade in the east may be about upper greenschist facies. The Jayah Creek Metabasalt may be equivalent to the regionally metamorphosed, lithologically similar sequence mapped as Eastern Creek Volcanics west of the Mount Isa Fault, in the Mount Isa 1:100 000 Sheet area to the north (Derrick & others, 1976). However, it is shown as a separate formation on the Ardmore 1:100 000 map because it has several characteristics not shared with rocks mapped as Eastern Creek Volcanics in the eastern part of the sheet area - for example, conglomeratic sediments containing abundant felsic volcanic clasts are very common in the east, whereas conglomerate is very rare in the Jayah Creek Metabasalt ahd no pebbles or felsic volcanics have been positively identified. Meta-argillite, para-amphibolite, and ?tuffaceous metasediments are abundant in places in the Jayah Creek Metabasalt, but are scarce or absent in the Eastern Creek Volcanics to the east. Such differences may be the result of facies variations from east to west, or they may indicate that the two formations are not equivalent.|16-MAY-23
26308|Jayah Creek Metabasalt|Defn Reference|82/22920|16-MAY-23
26308|Jayah Creek Metabasalt|Resdate|05-NOV-1980|16-MAY-23
25962|Jericho Formation|Name source|From AOD Jericho 1 well; Latitude 23o46'19"S; Longitude 146o05'11"E.|16-MAY-23
25962|Jericho Formation|Type section locality|In ENL Lake Galilee 1 from 1815 m (5955 ft) to 2578 m (8458 ft) K.B. Cuttings and Cores from this interval are available at the Core Library, Redbank.|16-MAY-23
25962|Jericho Formation|Extent|Present in the majority of wells in the northeastern Galilee Basin; absent in AAO Beryl 1, WNL Brookwood 1 and MPC Corfield 1 on the Beryl Ridge and LOL Hulton 1 on the Hulton-Rand structure. The unit has been continuously cored in GSQ Jericho 2 and GSQ Springsure 13 (Gray, in prep.).|16-MAY-23
25962|Jericho Formation|Thickness range|763 m in the type section; 699 and 733 m in AOD Jericho 1 and GSQ Jericho 2 respectively. The formation thins westward onto the Beryl Ridge as a result of the progressive onlap of rising basement.|16-MAY-23
25962|Jericho Formation|Lithology|The Jericho Formation in the type section consists of mudstone, siltstone and minor sandstone. A conspicuous siltstone member - defined below as the Oakleigh Siltstone Member - occurs within the formation. Cores 23 to 30 inclusive were cut in the type section, and are described in detail by Pemberton in Exoil N.L. (1965). Mudstone is dark grey, green-grey and brown, and fissile. Siltstone is green, brown and grey, and carbonaceous. Sandstone is generally light grey, green, fine to medium, labile to sub-labile and slightly calcareous. The Jericho Formation is readily distinguished from the overlying Jochmus Formation on wireline logs. The top of the Jericho Formation is taken at the top of the highest, thick mudstone or siltstone below the dominantly sandy lower Jochmus Formation. This position is distinguishable on the majority of wireline logs, particularly the resistivity and gamma-ray logs. The base of the Jericho Formation is taken at the top of the highest, thick bed of silicified sandstone as indicated by the wireline logs. The lithological contrast between mudstone and clean silicified sandstone is great enough to produce sharp changes on the wireline logs.|16-MAY-23
25962|Jericho Formation|Depositional environment|Probably a complex fluviatile and lacustrine environment with a glacial influence. Arthropod trails and ?mud cracks were observed in the core of GSQ Jericho 2, suggesting periodic subaerial exposure.|16-MAY-23
25962|Jericho Formation|Relationships and boundaries|The Jericho Formation conformably overlies the Lake Galilee Sandstone in the Lake Galilee and Jericho areas; elsewhere it rests unconformably on crystalline basement or pre-Late Carboniferous sediments. It is conformably overlain by the Jochmus Formation.|16-MAY-23
25962|Jericho Formation|Age reasons|Late Carboniferous to Early Permian. Spore assemblages characteristic of Stages 1 and 2 of Evans (1969) have been recorded.|16-MAY-23
25962|Jericho Formation|Defn author|Gray, A.R.G., Swarbrick. C.F.J., 1975|16-MAY-23
25962|Jericho Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
25962|Jericho Formation|Name first published by|Geological Survey of Queensland 1975|16-MAY-23
8952|Jiggamore Member|Name source|From Jiggamore Bore (140o11'15"E, 22o05'S) Boulia 1:250 000 Sheet area.|16-MAY-23
8952|Jiggamore Member|Unit history|Generally equates with Unit 3 of Casey (1968) and Member (ii) of Druce (1976) and the upper part of the Variegated Limestone/Dolomite member of Jones et al. (1971).|16-MAY-23
8952|Jiggamore Member|Type section locality|Black Mountain (140o17'E, 22o32'S), the interval from 165 m to 371 m within the Ninmaroo Formation from 259087 (140o16'45"E, 22o31'40"S) to 257090 (140o16'35"E, 22o31'30"S).|16-MAY-23
8952|Jiggamore Member|Extent|The unit is exposed in a 120 km belt from Mt Datson in the south (Boulia 1:250 000 sheet area) to Mt Merlin in the north (Duchess 1:250 000 sheet area).|16-MAY-23
8952|Jiggamore Member|Thickness range|206 m at Black Mountain; 92 m at Mt Datson; 130 m at Mt Ninmaroo.|16-MAY-23
8952|Jiggamore Member|Lithology|Thin to thick bedded limestone (micrite, frequently bioturbated; clast peloidal and peloidal grainstone (Dunham, 1962), minor ooid grainstone, diagnostic two-tone limestone), dolostone, dolomite breccia (pressure solution origin); calcareous siltstone.|16-MAY-23
8952|Jiggamore Member|Relationships and boundaries|Diagnostic two-tone patterns are a conspicuous diagenetic overprint which has gradational limits. The lower boundary is drawn at the first major occurrent of two-tone limestones in a sequence which is generally composed of such limestones. The upper boundary is drawn at the incoming of relatively abundant flat-pebble conglomerates. Regionally stratiform and apparently conformable, the boundaries may be discordant at a smaller scale.|16-MAY-23
8952|Jiggamore Member|Age reasons|The unit yields conodonts (Druce & Jones, 1971), rostroconch mulluscs (Pojeta et al., 1977 and nautiloids. These indicate an Early Ordovician (Datsonian) age.|16-MAY-23
8952|Jiggamore Member|Proposed publication|BMR publication, BMR 1:100 000 Special - the Southern Burke River Structural Belt|16-MAY-23
8991|Jochmus Formation|Name source|From Jochmus parish, the parish in which ENL Lake Galilee 1 well was drilled. The co-ordinates of the well are: Latitude 22o11'30"S; Longitude 145o58'32"E.|16-MAY-23
8991|Jochmus Formation|Type section locality|In ENL Lake Galilee 1 from 1060 m (3476 ft) to 1815 m (5955 ft) K.B. Cores and cuttings of this interval are available at the Core Library, Redbank.|16-MAY-23
8991|Jochmus Formation|Extent|Present in all exploratory wells drilled in the northeastern Galilee Basin except AAO Beryl 1 and MPC Corfield 1 on the Beryl Ridge.|16-MAY-23
8991|Jochmus Formation|Thickness range|755 m in the type section; thins westward, being 466 m and 358 m in QDM Aramac 1 and PON Muttaburra 1 respectively. Thins Southwards by erosion to 529 m and 319 m in QDM Hexham 1 and AOD Jericho 1 respectively.|16-MAY-23
8991|Jochmus Formation|Lithology|The Jochmus Formation consists of a lower part composed mainly of sandstone, a middle part composed of mudstone, siltstone and tuff and an upper part composed of sandstone, siltstone and mudstone. The middle part is defined as the Edie Tuff Member. Cores 14 to 24 inclusive were cut in the type section and are described in detail by Pemberton in Exoil N.L. (1965). Sandstones are generally light grey, green, rarely brown and reddish, fine to medium, moderately to well sorted, labile and locally conglomeratic. Porosity is developed in parts. Siltstone is light to medium grey and grey-green, argillaceous to sandy, hard, brittle, and carbonaceous. Mudstone is grey-green, silty, tuffaceous in part, slightly micaceous and carbonaceous; bedding is varve-like in part. The Jochmus Formation contains the "Red Tuff Marker" of Cundill, Meyers and Schultz (1971). It occurs at three or more different stratigraphic levels depending on the amount of truncation of the Jochmus Formation. The commonest occurrence is in the lower part of the Edie Tuff Member.|16-MAY-23
8991|Jochmus Formation|Depositional environment|A complex fluvial and lacustrine environment with a glacial influence.|16-MAY-23
8991|Jochmus Formation|Relationships and boundaries|Conformably overlies the Jericho Formation; conformably overlain by the Aramac Coal Measures in the western part of the basin and unconformably overlain by the Colinlea Sandstone correlative in the eastern part.|16-MAY-23
8991|Jochmus Formation|Age reasons|Early Permian. Spore assemblages obtained have been assigned to Stages 2 and 3 of Evans (1969).|16-MAY-23
8991|Jochmus Formation|Defn author|Gray A.R.G., Swarbrick C.F.J., 1975|16-MAY-23
8991|Jochmus Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
8991|Jochmus Formation|Name first published by|Geological Survey of Queensland, 1975.|16-MAY-23
28230|Joe Joe Group|Name source|The name Joe Joe Creek Series was used by Shell Queensland Development (1952) and amended to Joe Joe Creek Formation by Hill (1957); it was abbreviated to Joe Joe Formation by Mollan et al. (1969). The name is derived from Joe Joe Creek in the northwestern part of the Springsure 1:250 000 Sheet area; the type area is in the vicinity of the creek. A type section was not proposed. Recent stratigraphic drilling (Gray, in prep.) has demonstrated that the Joe Joe Formation of the type area consists almost entirely of the Jericho Formation of the subsurface. The name Joe Joe Formation has been used in surface mapping in the Tambo and Jericho Sheet areas for strata which recent stratigraphic drilling has shown to consist of the Jochmus Formation, the Jericho Formation and the Lake Galilee Sandstone of the subsurface. Therefore, it is appropriate to raise the name Joe Joe to group status. The Joe Joe Group is defined as that succession of formations which is unconformably overlain by the Colinlea Sandstone and it's lateral correlative, and unconformably overlies strata of the Adavale and Drummond Basins or other pre-Late Carboniferous rocks. The Joe Joe Group consists of the Lake Galilee Sandstone (lowermost), the Jericho Formation, the Jochmus Formation and the Aramac Coal Measures. The type sections of the lower three formations are designated in ENL Lake Galilee 1 to avoid the possibility of a miscorrelation. The type section of the Aramac Coal Measures is designated in QDM Aramac 1 well. The maximum known thickness of the Joe Joe Group is 1781 m in ENL Lake Galilee 1 well. The Joe Joe Group consists entirely of non-marine sediments; a glacial influence is apparent in parts. It has yielded spore assemblages assigned to Stages 1, 2 and 3 of Evans (1969); its age is presumed to be Late Carboniferous to Early Permian.|16-MAY-23
28230|Joe Joe Group|Defn author|Gray A.R.G., Swarbrick C.F.J., 1975|16-MAY-23
28230|Joe Joe Group|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24322|Juandah Coal Measures|Name source|Parish of Juandah, Fortescue County, Qld. (Wandoan Sheet 8845)|16-MAY-23
24322|Juandah Coal Measures|Unit history|New name. Previously intervals 7 and 8 of the Injune Creek Group (Swarbrick 1973).  Equivalent to intervals 7 and 8 of the Injune Creek Group (Swarbrick, 1973. Informally termed the Upper Coal Measures (Zillman, 1979).|16-MAY-23
24322|Juandah Coal Measures|Type section locality|GSQ, Roma 4 (grid reference 783300E 7093800N, Wandoan Sheet 8845). Occurs between the depths of 254.2 metres and 413.6 metres.|16-MAY-23
24322|Juandah Coal Measures|Extent|Crops out along strike from south of Wandoan to Injune. Intersected in the subsurface in numerous coal exploration holes and deep petroleum wells.|16-MAY-23
24322|Juandah Coal Measures|Thickness range|Range:  50 to 200 m. Average: 160 m. The formation thins towards Injune. Type Section: 159.4 m.|16-MAY-23
24322|Juandah Coal Measures|Lithology|Upward fining sequences of fine to medium grained lithic and feldspathic sandstone, siltstone, mudstone and coal. Coal members become more common towards the top of the unit. The bulk of the coal reserves outlined to date within the northeastern Surat Basin occur within these measures. Individual coal members can be up to 15 m thick but are commonly much thinner and exhibit rapid lateral thickness variations. The formation is typified by sparse outcrop.|16-MAY-23
24322|Juandah Coal Measures|Relationships and boundaries|The Juandah Coal Measures conformably overlies the Tangalooma Sandstone. The top of the unit is marked by the top of the last major coal lmember. This boundary can be observed in outcrop as well as in subsurface borehole intersections.|16-MAY-23
24322|Juandah Coal Measures|Age reasons|Middle Jurassic (Gould, 1968).|16-MAY-23
24322|Juandah Coal Measures|Proposed publication|Coal Geology|16-MAY-23
24322|Juandah Coal Measures|Defn Reference|82/22851|16-MAY-23
24322|Juandah Coal Measures|First Reference|82/22484|16-MAY-23
24322|Juandah Coal Measures|Proposer|Jones G.D., Patrick R.B.|16-MAY-23
25723|Judea Formation|Name source|Judea Block on Wando Vale Holding (Clarke River 4-Mile Cadastral Map).|16-MAY-23
25723|Judea Formation|Unit history|White (1959, 1962, 1965) mapped the unit as part of the Wairuna Formation, but it was subsequently mapped and defined as the Judea beds by Arnold & Henderson (1976).  It was given formation status by Withnall & others (1988), but not redefined.|16-MAY-23
25723|Judea Formation|Geomorphic expression|The Judea Formation generally produces low hilly topography, slightly more elevated than surrounding units.  Strike lines are not well developed, and the photo-pattern is relatively uniform.  The unit is commonly covered with a low scrub of quinine bush and stunted eucalypts.|16-MAY-23
25723|Judea Formation|Type section locality|Broken River between 7859 670443 (anticlinal hinge) and 662442 (unconformity with Poley Cow Formation).  Fine-grained quartzose arenite, mudstone, basalt and keratophyre are exposed.  The thickness is not known because of small-scale folding, but is estimated as less than 700 m.  The grid references are based on the AGD66 datum.|16-MAY-23
25723|Judea Formation|Extent|Forms a narrow strip up to 2km wide between Greenvale and Tomcat Creek, and also occurs in anticlinal cores in the Broken River area.|16-MAY-23
25723|Judea Formation|Thickness range|Less than 1500 m.|16-MAY-23
25723|Judea Formation|Lithology|Fine-grained quartzose arenite, mudstone, basalt, and keratophyre. Arenites are thin to very thick bedded, and show grading, horizontal stratification, cross laminae, soft sediment deformation, flutes and load casts.  The rocks are commonly strongly deformed with disrupted bedding and melange.|16-MAY-23
25723|Judea Formation|Fossils|Rare Tetragraptus sp. (Withnall & others, 1988) indicates an Early Ordovician age.  Limestone from west of the Gray Creek Complex contains poorly preserved favositids and heliolitids as well as conodonts which suggest a Middle Ordovician age (Palmieri, 1984).|16-MAY-23
25723|Judea Formation|Age reasons|Rare Tetragraptus sp. (Withnall & others, 1988) indicates an Early Ordovician age.  Limestone from west of the Gray Creek Complex contains poorly preserved favositids and heliolitids as well as conodonts which suggest a Middle Ordovician age (Palmieri, 1984).|16-MAY-23
25723|Judea Formation|References|ARNOLD, G.O. & HENDERSON, R.A., 1976:  Lower Palaeozoic history of the southwestern Broken River Province, north Queensland.  Journal of the Geological Society of Australia, 23, 73-93.***PALMIERI, V., 1984:  Conodont analysis of limestone samples from the Broken river Embayment, north Queensland.  Geological Survey of Queensland, Record 1984/38 (unpublished). ***WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4. Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. ***WHITE, D.A., 1962:  Clarke River 1.250 000 Geological series.  Bureau of Mineral Resources, Australia, Explanatory Notes, E/55-13. ***WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. ***WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
26309|Juntala Metamorphics|Name source|Parish of Juntala, County of Percy; also Juntala Holding in which part of the unit crops out.|16-MAY-23
26309|Juntala Metamorphics|Unit history|White (1962a,b: 1965) equated the schist and quartzite near Werrington with the Paddys Creek Formation, whose main outcrop area and type area are in the Greenvale area, about 90-100 km to the northeast. Because the relationship between the Proterozoic rocks in the Greenvale area and those in the rest of the Georgetown Province are uncertain, it is considered that renaming the rocks near Werrington is justified.|16-MAY-23
26309|Juntala Metamorphics|Type section locality|The best and most continuous outcrop occurs along Yarraman Creek. The outcrop is about 50 percent for 12 km from 570912 to 474910 (Lyndhurst 1:100 000 Sheet area - 7759) and passes through approximately 4000-6000 m of section. The type section is overlain in the north by alluvium. In the south it is faulted against gneisses of the Einasleigh Metamorphics. The compositional layering in general is vertically dipping, strikes NNE-NE and has been folded by at least three of the regional folding events recognised in the Georgetown Inlier (D1, D2, D4). All sedimentary textures are destroyed except for the compositional layering (bedding); therefore no younging criteria occur. The sequence consists of interbedded mica schists, graphitic schists, micaceous quartzites, quartzites, amphibolites, pegmatites, and minor granitic phases. The main rock types are the mica schists and quartzites, interbedded with a zone of distinctive graphitic schist which may or may not be a single 'lithological' unit. The mica schist and graphitic schists are the dominant rock types in the north of the section with minor bands of quartzite and micaceous quartzite. The quartzites and micaceous quartzites become more prominent towards the south of the section. Occasionally interlayered with the other rock types are minor bands of amphibolite, 1-10 m thick. These also tend to be more common in the south of the section. Pegmatites also become more common towards the southern end of the section, occurring as small (a few centimetres) to quite large (10-20 m) veins parallel to the layering. Minor bodies of fine grained biotite granitic rock are present; they are possibly related to the pegmatites.|16-MAY-23
26309|Juntala Metamorphics|Extent|The Juntala Metamorphics are exposed over an area of approximately 144 km2 in the central western part of the Clark River 1:250 000 Sheet area (SE 55-13), due west of Werrington homestead. These rocks also extend into the eastern part of the Gilberton 1:250 000 Sheet area (SE 54-16) (southeastern part of the Gilberton 1:100 000 Sheet area (7659)).|16-MAY-23
26309|Juntala Metamorphics|Thickness range|Unknown because of the complex deformation.|16-MAY-23
26309|Juntala Metamorphics|Lithology|Mica schist - contains quartz, feldspar, mica (muscovite and/or biotite), and locally garnet, andalusite, staurolite, chlorite, chloritoid, and minor graphite. These rocks are often interlayered with narrow bands of quartzite of the order of a few centimetres thick. Graphitic schist - black schist, consisting of quartz, feldspar, mica (muscovite and/or biotite), and graphite; andalusite is present locally. Quartzite - ranges from micaceous quartzite to relatively pure quartzite, and from finely laminated to massive.  Amphibolite - metamorphosed gabbro still showing the original gabbroic texture, and consisting of hornblende, feldspar and rare garnet.  Pegmatite - quartz-feldspar-muscovite pegmatite occurs as veins in the schists and quartzites.  Granite - fine grained biotite granite, possibly related to the pegmatites.   All rocks are deformed and all contain the S2 foliation. The schists and quartzites and possibly the amphibolites were deformed by D1, which produced a strong slaty cleavage parallel to the lithological layering. All      rocks included in the unit were deformed by the D2 event which produced an intense crenulation cleavage in the previously deformed rocks, and a good slaty cleavage in the granitic rocks. Effects of later deformations are common, especially D4 and D5.|16-MAY-23
26309|Juntala Metamorphics|Relationships and boundaries|The Juntala Metamorphics are faulted against gneisses of the Einasleigh Metamorphics along the entire eastern margin. Along the western margin the schists and quartzites grade into and are partly faulted against more gneissic rocks mapped as Einasleigh Metamorphics, and are intruded by younger granitic rocks which may be equated with Proterozoic or Siluro-Devonian Anning Granite, and Proterozoic Digger Creek Granite. To the south the metamorphics are intruded by and possibly faulted against the Carboniferous Purkin Granite. The unit crops out poorly along its northern margin and is overlain by alluvium.|16-MAY-23
26309|Juntala Metamorphics|Age reasons|Proterozoic. Because of the similarity of style and number of deformation events in the Juntala Metamorphics to those of the Robertson River Metamorphics and Einasleigh Metamorphics, it is considered that the units are all of similar age; the deformational and metamorphic events in the Juntala Metamorphics should have similar ages to those in the Robertson River Metamorphics and Einasleigh Metamorphics. Black & others (1979) dated the first three events D1, D2 and D3 at approximately 1570, 1470 and 970 million years, respectively. The schists, quartzites, and possibly the amphibolites in the Juntala Metamorphics are pre-D1 in age, and the granitic rocks are pre- or Syn-D2 in age.|16-MAY-23
26309|Juntala Metamorphics|Proposed publication|Queensland Government Mining Journal and/or the Journal of Structural Geology|16-MAY-23
26309|Juntala Metamorphics|First Reference|80/20650|16-MAY-23
26309|Juntala Metamorphics|Proposer|Duncan A.C.|16-MAY-23
9108|Kajabbi Formation|Name source|The town of Kajabbi 90 km northwest of Cloncurry; latitude 20o1'55"S, longitude 140o2'10"E (6957-993847).|16-MAY-23
9108|Kajabbi Formation|Unit history|Most of the Kajabbi Formation was previously mapped as Proterozoic Corella Formation (Carter et al., 1961).|16-MAY-23
9108|Kajabbi Formation|Geomorphic expression|The quartzite in the south occurs as low, rounded ridges. The limestone tends to be recessive and is exposed in stream channels and breakaways that cut through the Mesozoic cover rocks. Some well exposed pavements and blocky slightly disturbed flat-lying to gently dipping sheets of limestone occur.|16-MAY-23
9108|Kajabbi Formation|Type section locality|The type section is located along a low escarpment near the south bank of the Leichhardt River from a point 2.5 km south-southwest of Kajabbi (latitude 20o3'8"S, longitude 140o2'45"E; 6957-002832). The oldest rocks in the type section are approximately 30 m of brecciated thinly-bedded cross-bedded coarse-grained sandstone which are exposed in the west of the section adjacent to the Pinnacle Fault. The sandstone is overlain by a laminated partly brecciated chert sequence approximately 15 m thick. The chert sequence is overlain by about 140 m of grey thin-bedded to laminated silty limestone and calcareous siltstone. The base of the unit is not exposed in the type section because of faulting. Faulting also complicates the basal relations of the unit in other outcrops to the south of the type section. The basal relation is defined in the diamond drill core from a depth of 257 m in BHP 4 which is sited 400 m west of the eastern end of the type section (6957--996832). In this drill core, poorly sorted sandstone overlies folded quartzose metasediments that are correlated with the Corella Formation. The upper boundary of the Kajabbi Formation is an erosional unconformity with ferruginous clayey conglomerate of Mesozoic age which is exposed in the east of the type section. To the east and south of the type section three other holes drilled by BHP penetrate a total of more than 300 m of additional Cambrian strata which are not exposed. This sequence is regarded as the upward extension of the Kajabbi Formation and the three drill holes, BHP 1 (6957-076825), BHP 2 (6957-046774) and BHP 3 (6957-005704) are designated reference sections of this part of the formation. The top of the type section and the top of BHP 4 occur at approximately the same stratigraphic level which is tentatively correlated with rocks at about 150 m in BHP 3. The overlying sequence in BHP 3 contains laminated micaceous argillaceous calcareous siltstone (67 to 150 m), a cyclic unit consisting of rhythmic repetitions of laminated siltstone, limestone and carbonaceous shale (53 to 67 m), and grey laminated calcareous siltstone (0 to 53 m). The cyclic unit is correlated with the section from 136 to 165 m in BHP 2 and the basal part of BHP 1 (222 to 240 m). The upper part of the Cambrian sequence is most complete in BHP 1 where the cyclic unit is overlain by finely banded and laminated calcareous siltstone and silty limestone (85 to 222 m) and thinly bedded limestone and calcareous siltstone (41 to 85 m).|16-MAY-23
9108|Kajabbi Formation|Extent|The unit is exposed at eight localities from 1 km to 36 km south of Kajabbi and has a total area of outcrop of about 8 km2. All known outcrops are in the Quamby 1:100 000 Sheet area but the unit probably extends to the north as subcrop in the Landsborough Graben.|16-MAY-23
9108|Kajabbi Formation|Thickness range|The thickness estimated from the composite drill sections is at least 500 m and may exceed 600 m.|16-MAY-23
9108|Kajabbi Formation|Lithology|The Kajabbi Formation consists of two distinct lithologic units: a lower sandy unit which is exposed mostly in the south, and an upper silty limestone unit which is exposed in the north. The rocks in the upper unit are mainly pinkish brown to grey, massive to laminated calcareous siltstone, grey, silty limestone, laminated and brecciated chert, and whitish grey finely laminated siltstone. The limestones are locally pyritic and the siltstone contains rare fossils. In the south, buff, fine to medium grained poorly sorted quartzite and feldspathic calcareous sandstone of the lower unit predominate. From the BHP drill logs (Broken Hill Proprietary Co. Ltd, 1977) the base of the Cambrian sequence in the west consists of approximately 5 m of poorly sorted calcareous sandstone grading upward into sandy limestone and pure massive limestone about 20 m thick. This is overlain by deep red to pale grey coarse-grained, porous, slightly pyritic sandstone about 80 m thick, and then fractured massive dolomite or limestone with numerous chert bands and pyritic bands. The remainder of the Cambrian sequence is a very uniform laminated to thin-bedded calcareous siltstone and silty limestone about 400 m thick.  This sequence contains minor carbonaceous layers and zones of disseminated pyrite, and generally becomes more calcareous towards the top. It also contains some breccia zones from 1 to 3 m thick and a "cyclic" unit about 14 m thick. The cycles are 1 to 2 m thick and grade from a basal laminated calcareous siltstone upward into a limestone which becomes carbonaceous towards the top of the cycle. The top of each cycle is marked by a layer of carbonaceous shale generally less than 1 cm thick. The breccia zones and the "cyclic" unit have been used as stratigraphic markers in the four diamond drill holes.|16-MAY-23
9108|Kajabbi Formation|Relationships and boundaries|Most of the contacts with older rocks are faulted but some of the contacts of the quartzite near Cabbage Tree Creek and the upper unit of the Mount Albert Group may be unconformable. In diamond drillhole BHP 4, the Cambrian strata appear to overlie the Corella Formation with an angular unconformity. The Cambrian strata are overlain unconformably by Mesozoic sandstone and Cainozoic sediments.|16-MAY-23
9108|Kajabbi Formation|Structure and Metamorphism|The Kajabbi Formation generally dips less than 30o but near the Pinnacle Fault dips of 75o to vertical are more typical.|16-MAY-23
9108|Kajabbi Formation|Age reasons|A middle Cambrian age was determined from brachiopod and trilobite fossils. Druce (cited in Broken hill Proprietary Co., 1977) correlated specimens from 5 km south of Kajabbi (6957-983797) with the transition between the Inca Formation and the Pomegranate Limestone of the Georgina Basin. Fleming (1978) described a collection of Cambrian agnostid trilobites from 2.5 km south-southwest of Kajabbi (6957-988820). The species recognised were Ptychagnostus cassis, P. nathorsti?, Diplagnostus c.f. humilis, and Pseudophalacroma dubium. This fauna indicates a correlation with the laevigata I Zone (cassis Zone) of Opik (1961), corresponding to the Roaring Siltstone in the northern part of the Burke River Outlier and part of the Devoncourt Limestone in the southern part of the Outlier.|16-MAY-23
9108|Kajabbi Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
9108|Kajabbi Formation|Defn Reference|8020668|16-MAY-23
9136|Kalkadoon Granodiorite|Name source|Kalkadoon Copper Mine, ALSACE 1:100 000 Sheet area GR 862092 (Carter & others, 1961).|16-MAY-23
9136|Kalkadoon Granodiorite|Unit history|Previously mapped as part of the Kalkadoon Granite (Carter & others, 1961).|16-MAY-23
9136|Kalkadoon Granodiorite|Type section locality|No type area nominated by Carter & others (1961). A lectostratotype has been designated on DAJARRA, at grid reference 542772, 0.5 km west of Dajarra-Boulia road, 25 km SSE of Dajarra. This locality is the U-Pb zircon age determination site, 79205309. 1 km to the east, the granodiorite intrudes undivided Tewinga Group, whilst 3 km west of the site, the granodiorite is unconformably overlain by Haslingden Group (Blake & others, 1982). The dominant rock type at the lectostratotype is a porphyritic granodiorite containing some mafic xenoliths. The locality is cut by dolerite dykes and aplite veins.|16-MAY-23
9136|Kalkadoon Granodiorite|Extent|Extends in a narrow north-trending belt, up to 15 km wide, for 200 km between Dobbyn and Dajarra on the ALSACE, PROSPECTOR, MARY KATHLEEN, DUCHESS, and DAJARRA 1:100 000 Sheet areas. Total outcrop area is 1280 km2.|16-MAY-23
9136|Kalkadoon Granodiorite|Lithology|The Kalkadoon Granodiorite is medium to coarse-grained and ranges from a K-feldspar-free tonalite, through granodiorite to monzogranite (IUGS nomenclature, Streckeisen, 1973), with granodiorite being the most abundant. Tonalites are even-grained, with K-feldspar forming sparse phenocrysts up to 1 cm long in the more felsic varieties. The more mafic granodiorites are strongly porphyritic, and contain K-feldspar phenocrysts up to 5 cm long. The phenocrysts decrease in abundance from the granodiorite into the monzogranite as the rocks become more even-grained. Most of the Kalkadoon Granodiorite has been regionally metamorphosed, and primary igneous textures are rarely present.|16-MAY-23
9136|Kalkadoon Granodiorite|Relationships and boundaries|The Kalkadoon Granodiorite intrudes rocks of the Leichhardt Volcanics, Leichhardt Metamorphics, and undivided Tewinga Group. It is intruded by dolerite, Wills Creek Granite, Woonigan Granite and granophyre. It is unconformably overlain by rocks of the Bottletree Formation, Haslingden Group, and Quilalar and Surprise Creek Formations in the west (Bultitude & others, 1982; Blake & others, 1982; Derrick & others, 1980) and the Magna Lynn Metabasalt, Argylla Formation, and Mary Kathleen Group in the east (Plumb & others, 1980).|16-MAY-23
9136|Kalkadoon Granodiorite|Age reasons|Early Proterozoic. A U-Pb zircon age determination of 1856+/-11/9 m.y. was obtained on a sample from the lectostratotype (Page & Wyborn, in press). This is in agreement with a zircon age of 1862+/-27/29 m.y. from samples on MARY KATHLEEN 1:100 000 Shet area. All Rb-Sr age determinations are reset (Page, 1978).|16-MAY-23
9136|Kalkadoon Granodiorite|Proposed publication|BMR Journal of Australian Geology & Geophysics, 8(1)|16-MAY-23
9136|Kalkadoon Granodiorite|Comments|Remarks - The original definition of Carter & others (1961) for the Kalkadoon Granite was essentially referring to a "geographical entity" in which the granite was "composite, containing rocks of different ages and compositions" (Carter & others, 1961, p.143). Essentially, their definition was that of a granite batholith, i.e., a structural term. However, Carter & others (1961) and Joplin & Walker (1961) noted that the dominant phase within the Kalkaloon Granite was a granodiorite, intrusive into the Leichhardt Metamorphics. The name change proposed here restricts the name Kalkadoon Granodiorite to a particular intrusive phase (aged between 1850 and 1870 m.y.) in which the dominant rock type is granodiorite. Although Derrick & others (1977) recorded a dominance of syenogranite, this result is at variance with the work of Carter & others (1961), Joplin & Walker (1961), and Wyborn & Page (in press). In the last study, rock nomenclature was based on accurate point counts made on 15 x 10 cm stained rock slabs, which, in view of the medium to coarse grain size and sometimes porphyritic rock types, would be more accurate than the estimated modal analyses on 5 x 2 cm thin sections used by Derrick & others (1977). The name Kalkadoon Granite of Carter & others (1961) is essentially synonomous with the structural term, Kalkadoon Batholith of Wyborn & Page (in press). Kalkadoon Batholith now encompasses the proposed Kalkadoon Granodiorite and the One Tree, Woonigan, and Wills Creek Granites of Blake & others (1981).|16-MAY-23
24330|Kallala Quartzite|Name source|Named after QT Kallala Bore, located about 36 km SSW of Ardmore homestead, Urandangi 1;250 000 Sheet area.|16-MAY-23
24330|Kallala Quartzite|Unit history|Mapped as Eastern Creek Volcanics by Noakes & others (1959).|16-MAY-23
24330|Kallala Quartzite|Type section locality|From GR 173681 to GR 189672 in the S of the Ardmore 1:100 000 Sheet area, about 1.5 km to 3.5 km NW of the Pinnacles Dam. Most of the section consists of ridge-forming thin to medium-bedded, medium to coarse-grained, glassy quartzite, feldspathic quartzite, and muscovite quartzite. The section also contains minor hornblende+/- biotite schist and gneiss, at least some of which probably represents metadolerite. No facing evidence has been found in the quartzites.|16-MAY-23
24330|Kallala Quartzite|Extent|The Kallala Quartzite forms a narrow N-trending belt in the far S of the central part of the Ardmore 1:100 000 Sheet area, and extends S into the Glenormiston 1:250 000 Sheet area.|16-MAY-23
24330|Kallala Quartzite|Thickness range|Unknown, probably at leat 350 m. The formation has been tightly folded and dips are steep to vertical.|16-MAY-23
24330|Kallala Quartzite|Lithology|The rocks are generally as in the type section.|16-MAY-23
24330|Kallala Quartzite|Relationships and boundaries|The formation appears to have a concordant, probably conformable contact with the Sulieman Gneiss, and, to the west, a concordant, possible conformable, contact with a sequence of schistose amphibolite (metabasalt) and interlayered metasediments tentatively mapped as Jayah Creek Metabasalt. It may be younger then the Sulieman Gneiss and older than the Jayah Creek Metabasalt. The Kallala Quartzite is intruded by the Sybella Granite and by quartz and pegmatite veins.|16-MAY-23
24330|Kallala Quartzite|Age reasons|Precambrian.|16-MAY-23
24330|Kallala Quartzite|Proposed publication|Blake & others, in preparation|16-MAY-23
24330|Kallala Quartzite|Comments|Remarks: Bedding tends in the quartzite are mainly northerly, and dips are moderately steep to vertical. Trend lines and variations in the direction of dip indicate that the sequence has been tightly folded about mainly north to northeast-trrending axes. A northerly trending axial-plane fracture cleavage is well developed in the hinge zones of folds. The sequence has been regionally metamorphosed to amphibolite grade.|16-MAY-23
24330|Kallala Quartzite|Defn Reference|82/22920|16-MAY-23
23679|Kallanda Granite|Name source|None given.|16-MAY-23
23679|Kallanda Granite|Geomorphic expression|The granite crops out well and forms extremely rugged, boulder-strewn, hilly topography with a local relief of 350 m. Conspicuous lineaments trending southeast can be identified on aerial photographs and Landsat images. Strong southeasterly orientated trend lines in the southwestern end of the batholith may be dykes or joints. They are aligned with a similar belt of trends in the Macauley Creek Granite.|16-MAY-23
23679|Kallanda Granite|Type section locality|The type area for the Kallanda Granite is designated along the road from Ewan to Waverley between 8059-747925 and 752965.  The grid reference is based on the AGD66 datum.|16-MAY-23
23679|Kallanda Granite|Description at type locality|Pink to cream, coarse-grained, seriate biotite granite crops out along the road.|16-MAY-23
23679|Kallanda Granite|Extent|The Kallanda Granite forms a large northeast-trending batholith about 35km long and 10 to 15km wide in the northern part of EWAN extending into KANGAROO HILLS. The batholith probably consists of two bodies partly separated by a septum of Perry Creek Formation, although no discernible differences between the two have been observed, and they are both assigned to the one unit. It is bounded to the south by the Silurian Perry Creek Formation and ?Proterozoic Running River Metamorphics, and to the north by the Silurian-Devonian Kangaroo Hills Formation. The smaller southeastern body lies along the Endeavour Fault, the continuation of the Clarke River Fault which forms the boundary between the Broken River and Lolworth-Ravenswood Provinces.|16-MAY-23
23679|Kallanda Granite|Lithology|The Kallanda Granite is mainly coarse-grained, seriate, biotite granite. It ranges from pink or orange, particularly in the west, to cream. It is characterised by quartz 'eyes' which range up to 1cm across and alkali feldspar crystals up to 1.5cm.  Chloritic alteration zones are common throughout the Kallanda Granite. The zones are up to several metres wide and generally trend east-southeast. Some greisen zones also occur but are less common. Both are associated with tin and tungsten mineralisation.|16-MAY-23
23679|Kallanda Granite|Relationships and boundaries|The Kallanda Granite intrudes the (?)Proterozoic Running River Metamorphics and Falls Creek Tonalite, the Silurian Perry Creek Formation and Late Silurian to Early Devonian Kangaroo Hills Formation, and Early(?) Carboniferous Ewan Formation.|16-MAY-23
23679|Kallanda Granite|Age reasons|Fanning (Appendix 1) has obtained a U-Pb zircon (SHRIMP) age of 330±4 Ma on a sample of Kallanda Granite from north of EWAN on KANGAROO HILLS (8060-706010). This age is consistent with ages derived by Webb (1969) and a Rb-Sr biotite-total rock age of 331±2 Ma obtained by AGSO from the Falls Creek Tonalite (D. Wyborn, personal communication, 1989). The Falls Creek Tonalite has been intruded by the Coane Range Granite Complex and Kallanda Granite and the Rb-Sr age may reflect the age of hornfelsing and hence the age of the intrusive granites.|16-MAY-23
23679|Kallanda Granite|Comments|The AGSO airborne radiometric data indicate that the rocks are similar geochemically to the Coane Range Complex, because they are consistently high in the Total Count, U, K and Th channels. This indicates that the rocks of the complex are highly fractionated. This is confirmed by the geochemistry (Gunther & Withnall, 1992) and is consistent with the widespread tin-tungsten mineralisation.|16-MAY-23
23679|Kallanda Granite|References|GUNTHER, M.C. & WITHNALL, I.W., 1992: Late Palaeozoic igneous rocks of the Rollingstone and Ewan 1:100 000 Sheet areas. Queensland Resource Industries Record 1992/17. **WEBB, A.W., 1969: Metallogenic epochs in eastern Queensland.  Proceedings of the Australasian Institute of Mining and Metallurgy, 230, 27 39.|16-MAY-23
9156|Kamarga Volcanics|Name source|Kamarga homestead at latitude 18o47'6"S and longitude 139o9'53"E in the Lawn Hill 1:250 000 Sheet area (UE 061 218 on the Gregory Downs 1:100 000 Sheet area).|16-MAY-23
9156|Kamarga Volcanics|Unit history|Carter & others (1961) included these rocks in the Myally Beds. Cavaney (1975) included them in the Fiery Creek Volcanics.|16-MAY-23
9156|Kamarga Volcanics|Type section locality|1000 m of massive and amygdaloidal weathered basic volcanics interbedded with thin sandstone beds exposed between grid reference TE 826 213 and GR TE 845 200 in the Lawn Hill 1:100 000 Sheet area. Section is situated approximately 8 km east of the road connecting Rankins Yard to the Lawn Hill to Gregory Downs road and about 15 km due north of Rankins Yard on the Gregory River. A reference section is defined between grid reference TE 877 227 and grid reference 886 223 in the Lawn Hill 1:100 000 Sheet area and about 5 km east of the type section. The reference section comprises a sequence of 400 metres of alternating hard and soft bands of thickly bedded feldspathic sublabile to arkosic sandstones which conformably overlie the basic volcanics of the type section.|16-MAY-23
9156|Kamarga Volcanics|Extent|Crops out over 25 km2 in the faulted core of a dome in the eastern part of the Lawn Hill 1:100 000 Sheet area.|16-MAY-23
9156|Kamarga Volcanics|Thickness range|Observed thickness of 1400 m; Base of unit not exposed.|16-MAY-23
9156|Kamarga Volcanics|Lithology|Massive and amygdaloidal basic volcanics with interbeds of quartzose and arkosic sandstones up to 50 metres thick conformably overlain by feldspathic sublabile, arkosic, and conglomerate sandstones.|16-MAY-23
9156|Kamarga Volcanics|Relationships and boundaries|Forms the lowermost part of the sequence in the Lawn Hill 1:100 000 Sheet area. Unconformably overlain by sandstones of the Gunpowder Creek Formation. Intruded by the Weberra Granite. Could be a correlative of either the Fiery Creek Volcanics (Cavaney, 1975) or the Eastern Creek Volcanics (Carter & others, 1961).|16-MAY-23
9156|Kamarga Volcanics|Age reasons|Part of the Carpentarian sequence in the Precambrian rocks of northwest Queensland. Specific age unknown. A total rock K/Ar age on a sample of basalt of 1532+/-20 m.y. (Orridge & Dundas, 1974) may be unreliable due to argon loss.|16-MAY-23
9156|Kamarga Volcanics|Proposer|Hutton L.J., Sweet I.P.|16-MAY-23
27171|Karana Quartz Diorite|Name source|Karana' estate, north side of Brisbane River; GR 5980 5842 on the Ipswich 1:250 000 Sheet area.|16-MAY-23
27171|Karana Quartz Diorite|Unit history|Bryan and Jones (1950) informally referred to this body as the Mount Crosby quartz diorite. Gradwell (1958) first published the name Kholo Creek Quartz Diorite and this name was also used by Kirk (1973). However, this name is unacceptable due to the previous usage of the name Kholo by Denmead (1955) in his "Kholo Series" (which was later upgraded in the same sense to Kholo Sub Group by Allen 1961). Cranfield et al. (in press) listed this body under Undifferentiated Triassic Intrusions and used the term "Kholo Creek Quartz Diorite" in parenthesis as an informal name.|16-MAY-23
27171|Karana Quartz Diorite|Type section locality|A type locality is herein defined as in a disused quarry pit at GR 5980 5862 on the Ipswich 1:250 000 Sheet area and consists of medium to coarse grained quartz diorite consisting of plagioclase, quartz, biotite, pyroxene and iron ore.|16-MAY-23
27171|Karana Quartz Diorite|Extent|The unit is exposed over 6 km2 around the headwaters of Kholo Creek in the eastern part of the Ipswich 1:250 000 Sheet area (SG 56-14).|16-MAY-23
27171|Karana Quartz Diorite|Lithology|Quartz Diorite is the dominant lithology with minor associated late stage pegmatites.|16-MAY-23
27171|Karana Quartz Diorite|Relationships and boundaries|Intrudes both the Neranleigh-Fernvale Beds and the Brookfield Volcanics.|16-MAY-23
27171|Karana Quartz Diorite|Age reasons|Age of 222 million years (Middle Triassic) was obtained using the Ar39/Ar40 method on biotite (Kirk, 1973).|16-MAY-23
27171|Karana Quartz Diorite|Proposed publication|Report of the Geological Survey of Queensland|16-MAY-23
27171|Karana Quartz Diorite|First Reference|80/20584|16-MAY-23
9284|Karin Granite|Name source|Karin railway siding at 8452-790668. The grid reference is based on the AGD66 datum.|16-MAY-23
9284|Karin Granite|Geomorphic expression|The Karin Granite is characterised by gently undulating terrain and produces light coloured sandy loam.   The Karin Granite is defined on the Landsat TM image as cleared areas with a yellow-orange hue that contrasts with the dark hues of the surrounding basalt-derived soils. It is not within the area of the detailed airborne geophysical survey, but has a low magnetic response on the Bureau of Mineral Resources regional data. It also corresponds with a gravity low (Darby, 1969).|16-MAY-23
9284|Karin Granite|Type section locality|At 8451-022486, on the north side of the Gregory Highway, 3 km west of Capella. The grid reference is based on the AGD66 datum.|16-MAY-23
9284|Karin Granite|Description at type locality|Isolated boulder-sized outcrops of pink, fine to medium-grained, equigranular biotite granite.|16-MAY-23
9284|Karin Granite|Extent|The main exposure of the Karin Granite is an equant body, 13 km2 in area, which crops out as platforms and isolated boulders about 2 km west of Capella. Numerous smaller poorly exposed areas (up to 5 km2) occur up to 30 km northwest of Capella in windows in the Cainozoic basalt cover.|16-MAY-23
9284|Karin Granite|Lithology|Pink, fine to medium-grained, equigranular biotite granite and microgranite.|16-MAY-23
9284|Karin Granite|Relationships and boundaries|Intrudes the Anakie Metamorphic Group, and is unconformably overlain by Permian Aldebaran Sandstone and Cainozoic basalt and colluvial deposits.|16-MAY-23
9284|Karin Granite|Age reasons|The age is uncertain. A Devonian to Carboniferous age has been assigned because it predates the Permian rocks.|16-MAY-23
9284|Karin Granite|References|DARBY, F. 1969: North Bowen Basin gravity survey, Queensland 1963. Bureau of Mineral Resources, Australia, Report 138. **VEEVERS, J.J., MOLLAN, R.G., OLGERS, F. & KIRKEGAARD, A.G., 1964b: The geology of the Emerald 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 68.|16-MAY-23
23688|Karmoo Quartz Diorite|Name source|Karmoo homestead at 8351-387473.   The grid reference is based on the AGD66 datum.|16-MAY-23
23688|Karmoo Quartz Diorite|Geomorphic expression|The pluton is poorly exposed and forms low undulating terrain with reddish soil, and contrasts with the hilly terrain of the surrounding Anakie Metamorphic Group.  The Karmoo Quartz Diorite is delineated on the Landsat 5 TM (1-4-7 BGR) image by cleared areas that have a yellowish hue. Only the eastern part of the pluton was covered by the geophysical survey. Complex magnetic dipoles characterise this area, but the data suggest that a strong positive anomaly lies over the western half of the pluton. K, Th and U responses are generally low, but higher responses within 3 km of the eastern margin, possibly reflecting the abundant metamorphic enclaves.|16-MAY-23
23688|Karmoo Quartz Diorite|Type section locality|Along the Clermont-Barcaldine powerline, between 8351-413468 and 327442.   The grid reference is based on the AGD66 datum.|16-MAY-23
23688|Karmoo Quartz Diorite|Description at type locality|At type locality a diverse range of rock types ranging from hornblende gabbro to hornblende-biotite tonalite crops out.|16-MAY-23
23688|Karmoo Quartz Diorite|Extent|An elongate, west-southwest trending pluton, 30 km2 in area, on the northwestern margin of the Retreat Batholith near Karmoo homestead and Sandy Creek.|16-MAY-23
23688|Karmoo Quartz Diorite|Lithology|The Karmoo Quartz Diorite is a composite pluton of grey, fine to medium-grained, equigranular, biotite-hornblende quartz diorite and tonalite with subordinate hornblende-biotite granodiorite, biotite-hornblende diorite, hornblende gabbro and rare biotite granodiorite. Xenoliths and pendants of hornfelsed schist and quartzite are abundant in the eastern part of the pluton.|16-MAY-23
23688|Karmoo Quartz Diorite|Relationships and boundaries|Intrudes the Anakie Metamorphic Group and is probably faulted against the Kilmarnock Granodiorite by the Kettle Creek Fault.|16-MAY-23
23688|Karmoo Quartz Diorite|Age reasons|An age of 384 Ma (Middle Devonian) was obtained by Rb-Sr dating of a biotite-whole rock pair.|16-MAY-23
9375|Keepera Group|Name source|From Keepera Ridges, southwestern TOBERMORY.|16-MAY-23
9375|Keepera Group|Unit history|Part of Field River beds (Smith 1963a); Wonnadinna Dolomite (Walter 1980) in part; Oorabra Arkose Member (Smith 1964) of Elyuah Formation in part; basal Central Mount Stuart beds (Smith and Milligan 1964) in part; tilloid of lower part of Mount Birnie beds (Opik 1960) sensu de Keyser (1968) in part.|16-MAY-23
9375|Keepera Group|Constituents|Black Stump Arkose, Wonnadinna Dolostone, Oorabra Arkose, Boko Formation, Sun Hill Arkose, Little Burke Tillite.|16-MAY-23
9375|Keepera Group|Extent|BARROW CREEK, ALCOOTA, HUCKITTA, TOBERMOREY, HAY RIVER, MOUNT WHELAN, DUCHESS.|16-MAY-23
9375|Keepera Group|Relationships and boundaries|Disconformably overlies Yardida Tillite and Mount Cornish Formation of Aroota Group, unconformable on Amesbury Quartzite of Plenty Group, or where these are absent, unconformable on Palaeoproterozoic rocks. Disconformable or with slight angular unconformity beneath Gnallan-a-Gea Arkose and Elyuah Formation (Walter 1980), and disconformable beneath Central Mount Stuart Formation of Mopunga Group or where these are absent, disconformable beneath Sylvester Sandstone (conformable according to Shergold and Druce 1980) or unconformable beneath Mount Birnie beds of Shadow Group.|16-MAY-23
9375|Keepera Group|Identifying features|This new group is defined to include the Black Stump Arkose, Wonnadinna Dolomite and Oorabra Arkose of the Mt Whelan, Hay River, Tobermory, Huckitta and probably Alcoota 1:250 000 Sheet areas. The name is derived from the Keepera Ridges, Tobermory 1:250 000 Sheet area. The formations are grouped because they comprise a distinct tectosome bounded by unconformities. (Walter)|16-MAY-23
9375|Keepera Group|Age reasons|Upper of two late Neoproterozoic glacigene units; correlated with Marinoan glaciation in Adelaide Rift (de Keyser 1972, Preiss et al 1978, Haines et al 1991). Shergold (1985) correlated Sun Hill Arkose with Black Stump Arkose on the basis of lithological similarity.|16-MAY-23
9375|Keepera Group|Correlations|Olympic Formation and Pioneer Sandstone of Amadeus Basin, Mount Doreen Formation of Ngalia Basin.|16-MAY-23
9375|Keepera Group|Comments|The Keepera Group is here expanded beyond the original Black Stump Arkose, Wonnadinna Dolostone and Oorabra Arkose in the conception of Walter (1980), to include units subsequently correlated or erected.|16-MAY-23
9375|Keepera Group|First Reference|81/22263|16-MAY-23
9375|Keepera Group|State(s)|NT|16-MAY-23
9383|Keilambete Tonalite|Name source|Keilambete pastoral holding and homestead at 8451-607070.  The grid reference is based on the AGD66 datum.|16-MAY-23
9383|Keilambete Tonalite|Geomorphic expression|The pluton is characterised by low relief and gently undulating terrain that contrasts with the surrounding metamorphic rocks. Outcrop is sparse and occurs as isolated boulder-sized exposures.   The Keilambete Tonalite is delineated on the Landsat 5 TM (1-4-7 BGR) image by cleared areas that have a yellowish hue. It has moderate to strong magnetic anomalies, but very low K, U and Th responses.|16-MAY-23
9383|Keilambete Tonalite|Type section locality|At 8451-647094.  The grid reference is based on the AGD66 datum.|16-MAY-23
9383|Keilambete Tonalite|Description at type locality|Dark grey, fine to coarse-grained, porphyritic biotite-hornblende tonalite.|16-MAY-23
9383|Keilambete Tonalite|Extent|An oval body, 45 km2 in area, centred about 2-3 km northeast of Mount Leura homestead.|16-MAY-23
9383|Keilambete Tonalite|Lithology|Dark grey to grey, locally foliated, fine to coarse-grained, subequigranular to porphyritic biotite-hornblende tonalite.|16-MAY-23
9383|Keilambete Tonalite|Relationships and boundaries|Intrudes the Anakie Metamorphic Group, Gem Park Granite, and possibly the Mount Newsome Granodiorite.|16-MAY-23
9383|Keilambete Tonalite|Age reasons|A Devonian age has been assigned because of the similarities of the unit to other components of the Retreat Batholith, for which Middle Devonian ages have been determined.|16-MAY-23
33722|Kenewah Granodiorite|Name source|The Kenewah Granodiorite was named after Kenewah property which is situated on the western side of Cooyar Creek.|16-MAY-23
33722|Kenewah Granodiorite|Unit history|This is a new name for a granodiorite body originally mapped as part of the Woolshed Mountain Granodiorite by Cranfield and Schwarzboch (1974).  The RTP magnetic image shows the Kenewah Granodiorite to be a separate body from the main Woolshed Mountain Granodiorite.  On the basis of this substantially different magnetic response a new unit is proposed.|16-MAY-23
33722|Kenewah Granodiorite|Geomorphic expression|The Kenewah Granodiorite forms hilly country on the drainage divide between Granite and Oaky Creeks on the western margin of the Blackbutt Range.  Deeply weathered Tertiary sediments and volcanics, which form the cuesta-like Blackbutt Range, obscure the majority of the unit.|16-MAY-23
33722|Kenewah Granodiorite|Type section locality|A type area for the Kenewah Granodiorite is the valley containing the headwaters of the eastern branch of Granite Creek.  In this valley scattered tors of light grey medium to coarse-grained granodiorite occur adjacent to the road.  Examples of the granite can also be found beside the road in the headwaters of the eastern branch of Oaky Creek.|16-MAY-23
33722|Kenewah Granodiorite|Extent|The Kenewah Granodiorite is located in the southeastern bottom corner of KINGAROY in the headwaters of the eastern branch of Oaky Creek and eastern branch of Granite Creek.  The two areas of exposure are separated by Tertiary cover and have a combined area of out approximately 8km2.  Elevations in this unit range from about 440m to 500m above sea level.|16-MAY-23
33722|Kenewah Granodiorite|Lithology|The Kenewah Granodiorite is composed of medium grained light to dark grey and pink, even to moderately porphyritic, biotite hornblende granodiorite and lesser grey-pink medium grained sparsely porphyritic biotite granite.  The sparsely porphyritic granite contains alkali feldspar phenocrysts to 20mm although the most common size is about 5mm.|16-MAY-23
33722|Kenewah Granodiorite|Relationships and boundaries|The Kenewah Granodiorite intrudes the Devonian to Carboniferous Sugarloaf Metamorphics and hornfelses that unit along its contact.  Sediments of the Triassic Tarong Basin, and sediments and volcanics of Tertiary age, overlie the Kenewah Granodiorite.  Small Tertiary rhyolitic? plugs intrude the Kenewah Granodiorite near its south-western margin.|16-MAY-23
33722|Kenewah Granodiorite|Age reasons|No age dating of this unit has been attempted though it is probably of Permo-Triassic age.|16-MAY-23
33722|Kenewah Granodiorite|Geophysical Expression|Magnetic response was used to distinguish the Kenewah Granodiorite from the Woolshed Mountain Granodiorite on the RTP magnetic image.  The moderate magnetic response shown by the Kenewah Granodiorite contrasts sharply with the very low response of the Woolshed Mountain Granodiorite.  The subsurface body is approximately 19km2 in area and is elongated in a south-westerly direction.  Contrast on the RGBI (total count as intensity layer) radiometric image is also substantial with the Kenewah Granodiorite giving a `hot¿ (white) response whereas the Woolshed Mountain Granodiorite has a reddish signature.|16-MAY-23
33722|Kenewah Granodiorite|References|CRANFIELD, L.C. & SCHWARZBOCH, H.,1974, New and revised stratigraphic names for the Ipswich 1:250 000 Sheet area. Queensland Government Mining Journal, 75, 322-323. Regional Geology.|16-MAY-23
28642|Kerosene Creek Member|Name source|Kerosene Creek; GR 300,700E, 7,382,250N, Gladstone 1:100 000 topographic sheet.|16-MAY-23
28642|Kerosene Creek Member|Unit history|Part of the Narrows Beds (Kirkegaard et al, 1970) and part of the Rundle Formation (Henstridge and Missen, 1982).|16-MAY-23
28642|Kerosene Creek Member|Type section locality|43 m of oil shale with minor interbeds of claystone and carbonaceous shale; from 120.6 to 163.3 m in drill hole RDD66 (GR 299,441E 7, 382,121N, Gladstone 1:100 000 topographic sheet), which is part of the type section of the Rundle Formation. The dark yellowish-brown to olive-brown oil shale contains two major greyish-green claystone beds (from 127.5 to 127.9 m and 141.9 to 142.5 m in the type section) and two carbonaceous shale beds (from 144.3 to 145.8 m and 153.9 to 154.9 m in the type section). Cyclicity of lithologies is a feature, with oil shale grading upwards through clayey oil shale to claystone, commonly overlain by carbonaceous material.|16-MAY-23
28642|Kerosene Creek Member|Extent|Subcrops in an area of about 12 km2 in The Narrows Graben, N.W. of Gladstone, Queensland. Sparse, weathered outcrops are recorded. The member has been identified from drill hole core.|16-MAY-23
28642|Kerosene Creek Member|Thickness range|43 m (estimated true thickness 42.9 m corrected for an apparent dip of 4o in RDD66) in type section. Range of true thickness of the member as intersected in drill holes is 42.9 m to 58.4 m.|16-MAY-23
28642|Kerosene Creek Member|Lithology|Oil shale, dark yellowish-brown to olive-brown; calcareous in part, carbonaceous and clayey cyclicity; very thinly to very thickly bedded (up to 2m); laminated, brecciated in part. Minor interbeds of greyish-green claystone and very dark grey carbonaceous shale; rare discontinuous thin dolomite concentrations. Claystone beds often show bioturbation features and rare cross laminations where more arenaceous. Ostracode tests are abundant with minor gastropods, vertebrate remains (crocodile, turtle), fish fragments and coprolites. Plant remains (including Azolla) in the more carbonaceous material. To the northwest in the Narrows Graben, the lower of the two claystone beds thickens, ranging up to 10 m.|16-MAY-23
28642|Kerosene Creek Member|Relationships and boundaries|The member is conformable with the underlying Telegraph Creek Member and is the contact between oil shale and claystone. The upper boundary is conformable with the Curlew Formation and is the contact between oil shale and carbonaceous shale. The member is faulted against Devonian to Carboniferous rocks of the Curtis Island Group along the western edge of The Narrows Graben.|16-MAY-23
28642|Kerosene Creek Member|Age reasons|Mid to late Eocene - as for the Rundle Formation.|16-MAY-23
28642|Kerosene Creek Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
28642|Kerosene Creek Member|Comments|Note: Drill-core from RDD66 is stored at Southern Pacific Petroleum's Research and Core Storage Facility located in Gladstone, Queensland.|16-MAY-23
28642|Kerosene Creek Member|Reserved? Yes/No|Henstridge D.A., Coshell L.|16-MAY-23
79128|Kidgell Andesite Member|Name source|After Kidgell Street which crosses the andesite unit about 1.5 km south of Gympie Railway Station.|16-MAY-23
79128|Kidgell Andesite Member|Unit history|This unit was described informally as the Hall andesite by Gympie Eldorado Gold Mines at Monkland Mine. Equates to Dunstan's (1911) Second Volcanic (Greenstone) Group (2V), together with Mary Basalt.  Termed 'hard greenstone' or 'Gympie greenstone' by Rands (1889).|16-MAY-23
79128|Kidgell Andesite Member|Type section locality|Well exposed at the lower end of Deep Creek on the Bruce Highway (River Road) near the Normanby Bridge (MGA 467255mE, 7101510mN. Lat: -26°12'20"  Long: 152°40'20".).  Being on a busy highway inspection of this locality requires great care.  A reference section at the Zillmere core library, Brisbane is GEGM drill hole G215, 13.7-98.4 m (MGA 467424mE; 7101493mN. Lat: -26°12'21"  Long: 152°40'26").|16-MAY-23
79128|Kidgell Andesite Member|Extent|At depth in Monkland Mine, rising northwards to surface at North Inglewood where it was encountered in the upper levels of several shafts to the east of the reference section. These workings included Union Extended (0-116 m), Ellen Harkins (0-90 m), Ellen Harkins and St Kilda (0-120 m), South Ellen Harkins and Wilmot andWalton Extended. GEGM drill holes in the vicinity included G250 and G256. The unit continues northwards into the Phoenix Block where it was termed 'hard greenstone' or 'Gympie greenstone' by Rands (1889). Here it reaches a maximum thickness on Calton Hill then thins out northwards to Myall Street. West of the Laing Fault this andesite was recorded below Mary Basalt in the Dawn Block and occurs beneath the Curra Break in West Phoenix and Sovereign blocks. A probable separate flow occurs north of the Dawn Mine.|16-MAY-23
79128|Kidgell Andesite Member|Thickness range|About 100-120 m, both at Monkland and at West Phoenix below Curra Break.|16-MAY-23
79128|Kidgell Andesite Member|Lithology|Type section is a road cutting of massive andesite, intruded by a couple of quartz veins on a Gympie Vein trend.  The andesite consists of 2-3 mm zoned feldspar phenocrysts, lesser hornblende, accessory titano-magnetite, part altered to leucoxene, and no quartz.  Like the Calton Andesite, which it resembles, ghosting of the white plagioclase in altered examples makes textures difficult to see.|16-MAY-23
79128|Kidgell Andesite Member|Relationships and boundaries|Located either within the Hall Clastics Member or immediately underlying Mary Basalt.  Houston (in Houston and others, 2003) interpreted the unit in part as 'dome facies volcanics with blocky proximal breccias containing high proportions of non-vesicular, juvenile material.  More coherent bodies may be subvolcanic'.|16-MAY-23
79128|Kidgell Andesite Member|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie, 12-JAN-2017.|16-MAY-23
79128|Kidgell Andesite Member|References|Dunstan, B., 1911: Geology map of Gympie and environs. GSQ Publ. No. 221b.  **Rands, W.H. 1899: Geological Map of part of Gympie Goldfield.  Geological Survey of Queensland.  **Houston, M, McQuitty B., Beckton, J and Groves, S, 2003: Exploration Permit for Minerals 6031. Annual report for the year ending 6th September 2003. GEGM report to DNR&M. Report number VIII 16.|16-MAY-23
9563|Kilmarnock Granodiorite|Name source|Kilmarnock homestead at 8351-494494.   The grid reference is based on the AGD66 datum.|16-MAY-23
9563|Kilmarnock Granodiorite|Geomorphic expression|The granodiorite forms gentle to moderately undulating terrain with numerous rock platforms and boulder-sized outcrops, although large areas of the granodiorite are obscured by Cainozoic gravel. On the Landsat 5 TM (1-4-7 BGR), the Kilmarnock Granodiorite is represented by a light brown colour in the west which changes to a magenta hue east of the Clermont-Rubyvale Road.  Moderate magnetic anomalies occur over most of this unit, with stronger anomalies along the northern and eastern margins. Magnetic response is significantly decreased along abundant northwest, east-northeast and northerly lineaments. An area of lower magnetisation also occurs around Tomahawk Creek. The unit has generally strong K, moderate to strong Th, and generally low U responses.|16-MAY-23
9563|Kilmarnock Granodiorite|Type section locality|At 8451-534315, 2 km southeast of Bald Hills.   The grid reference is based on the AGD66 datum.|16-MAY-23
9563|Kilmarnock Granodiorite|Description at type locality|Light grey, fine to coarse-grained, subequigranular hornblende-biotite granodiorite is exposed.|16-MAY-23
9563|Kilmarnock Granodiorite|Extent|A large pluton, 900km2 in area, from Old Peak Vale homestead in the north to Mount Ball in the south.|16-MAY-23
9563|Kilmarnock Granodiorite|Lithology|Grey, fine to coarse-grained, equigranular to porphyritic, hornblende-biotite granodiorite. Metasedimentary xenoliths are common in the west but decrease towards the east.|16-MAY-23
9563|Kilmarnock Granodiorite|Relationships and boundaries|Intrudes the Anakie Metamorphic Group, but relationships with adjacent plutons are unknown. Similarities in petrography, geochemistry and age suggest a common genesis and time of emplacement. It is partly faulted against the Karmoo Quartz Diorite, Mount Observatory Granite and Mount Newsome Granodiorite along the Kettle Creek fault.  Numerous small basalt plugs of the Hoy Basalt intrude the Kilmarnock Granodiorite. Many plugs are located along the boundaries with the Annmore Quartz Monzodiorite and the Mount Observatory Granite.|16-MAY-23
9563|Kilmarnock Granodiorite|Age reasons|Webb & others (1963) obtained two K-Ar biotite ages corrected to 352 Ma and 355 Ma, and two K-Ar hornblende ages corrected to 363 Ma and 365 Ma. Webb & McDougall (1968) reported one K-Ar biotite age corrected to 370 Ma, and one hornblende age corrected to 360 Ma. An age of 375 Ma (Middle Devonian) has been obtained from Rb-Sr dating of a biotite-whole rock pair.|16-MAY-23
9563|Kilmarnock Granodiorite|References|WEBB, A.W., COOPER, J.A. & RICHARDS, J.R., 1963: K-Ar ages on some Central Queensland granites. Journal of the Geological Society of Australia, 10, 317-324.|16-MAY-23
9570|Kimbala Granodiorite|Name source|Kimbala homestead, GR 5483 6901, Gympie 1:250 000 Sheet area SG56-10. Name published informally by Brooks (1971).|16-MAY-23
9570|Kimbala Granodiorite|Type section locality|The area west of Monsildale Creek at GR 5450 6960|16-MAY-23
9570|Kimbala Granodiorite|Extent|The unit covers 40 km2 in the southern central portion of the Gympie 1:250 000 Sheet area between Yulburn Creek and Mount Monsildale.|16-MAY-23
9570|Kimbala Granodiorite|Lithology|Coarse-grained, hornblende-biotite granodiorite.|16-MAY-23
9570|Kimbala Granodiorite|Relationships and boundaries|Intrudes the Lower Permian Marumba Beds.|16-MAY-23
9570|Kimbala Granodiorite|Age reasons|It is probably related to the adjacent Monsildale Granodiorite and is thus assigned a Permo-Triassic age.|16-MAY-23
9570|Kimbala Granodiorite|Proposed publication|Report of the Geological Survey of Queensland|16-MAY-23
9570|Kimbala Granodiorite|Status|1|16-MAY-23
9606|Kingaham Creek Granodiorite|Name source|Kingaham Creek, GR 5550 7050.|16-MAY-23
9606|Kingaham Creek Granodiorite|Unit history|The unit includes the "Manumbar Granodiorite" of Lewis (1967) and the "Kingaham granodiorite" of McNaughton (1973).|16-MAY-23
9606|Kingaham Creek Granodiorite|Type section locality|Between Kingaham homestead, GR 550 7030, and near the Central Burnett Highway at GR 5510 7000.|16-MAY-23
9606|Kingaham Creek Granodiorite|Extent|The unit crops out as a northwest trending, elongate body covering an area of 250 km2 from 6 km north of Jimna, GR 5590 6888, north to Gobongo Creek, GR 5371 7300.|16-MAY-23
9606|Kingaham Creek Granodiorite|Lithology|The rock is a homogeneous, grey, medium to coarse grained hornblende-biotite granodiorite.|16-MAY-23
9606|Kingaham Creek Granodiorite|Relationships and boundaries|Intrudes undifferentiated Palaeozoic metamorphics and serpentinite, Lower Permian Marumba Beds and is overlain by Lower to Middle Triassic Neara Volcanics. It is intruded by the Upper Carboniferous Gallangowan Granodiorite.|16-MAY-23
9606|Kingaham Creek Granodiorite|Age reasons|K/Ar radiometric ages of 215 m.y., 216 m.y. and 237 m.y. were obtained from this unit by Webb and McDougall (1967) and Murphy et al. (in prep.). The unit may be in part as old as Late Permian. A Permian-Triassic age is thus assigned to the intrusion.|16-MAY-23
9606|Kingaham Creek Granodiorite|Proposed publication|Report of the Geological Survey of Queensland|16-MAY-23
9606|Kingaham Creek Granodiorite|Name first published by|Geological Survey of Queensland, 1975|16-MAY-23
24344|Korenan Oil Shale Member|Name source|Korenan railway siding, GR 64900E 93500N Miriam Vale 1:100 000 Sheet area.|16-MAY-23
24344|Korenan Oil Shale Member|Unit history|Part of the Lowmead Beds of Cribb, 1960; Mack, 1972; and Ellis and Whitaker, 1976.|16-MAY-23
24344|Korenan Oil Shale Member|Type section locality|135.2 m (estimated true thickness 133.2 m) from 78.4 m to 213.6 m in LDD14 (GR 64906E 95222N Miriam Vale 1:000 000 Sheet area). The interval is within the type section of the Lowmead Formation. Dark to dusky yellow-brown kerogenous claystone (oil shale) is the dominant rock type (greater than 90%). Upper and lower boundaries are identified by the contact of brown oil shale with black carbonaceous oil shale of the Makowata Oil Shale Member and Wheatley Oil Shale Member, respectively.|16-MAY-23
24344|Korenan Oil Shale Member|Extent|Subcrops in an area of about 7 km2 north and east of Korenan railway siding. Sparse mostly weathered outcrops are known. The member has been identified from drill core.|16-MAY-23
24344|Korenan Oil Shale Member|Thickness range|135.2 m in type section. True thickness 133.2 m, corrected for a 10o dip of the strata in LDD14. The member ranges in thickness from 94.3 m to 149.7 m.|16-MAY-23
24344|Korenan Oil Shale Member|Lithology|There are two types of oil shale, identified by lithological changes and confirmed by comparison of assay histogram of oil yields. The boundary between the two types is determined from the assay histogram. The lower oil shale is hard, very thinly laminated dusky yellow-brown. There are sporadic carbonaceous oil shale beds up to 2 m thick. On an assay histogram of oil yield the average yield is above 50 litres of shale oil per tonne of oil shale at zero percent moisture (LTOM). The upper oil shale is moderately hard, massive to laminated and dark to dusky yellow-brown. There are sporadic thin (less than 30 cm) very hard sideritic argillite beds. Traces of bioturbation (annelid grazing tracks) are present. The average oil yield is below 50 LTOM.|16-MAY-23
24344|Korenan Oil Shale Member|Relationships and boundaries|The Korenan Oil Shale Member is conformably overlain by the Makowata Oil Shale Member and conformably overlies the Wheatley Oil Shale Member of the Lowmead Formation. It is faulted against igneous rocks of the Miriam Vale Granodiorite and Agnes Waters Volcanics (Ellis and Whitaker, 1976) along the boundaries of the Lowmead Graben.|16-MAY-23
24344|Korenan Oil Shale Member|Age reasons|Early Tertiary - as for the Lowmead Formation.|16-MAY-23
24344|Korenan Oil Shale Member|Defn author|McConochie M.J., Henstridge D.A., 1985. |16-MAY-23
24344|Korenan Oil Shale Member|Comments|Note: Drill core of LDD14 is stored at Southern Pacific Petroleum's Research and Core Storage Facility in Gladstone, Qld.|16-MAY-23
24344|Korenan Oil Shale Member|Defn Reference|86/25154 Described P211. Mention Table 1 as Korenan Member|16-MAY-23
9839|Koukandowie Formation|Name source|From Koukandowie Mountain (Trig Station), (MM 874.824, Grafton 1:100 000 sheet 9438) at the southern margin of the Clarence-Moreton Basin.|16-MAY-23
9839|Koukandowie Formation|Unit history|The unit name is derived from the Koukandowie 'Sandstone Member' of the 'Marburg Formation' as published by McElroy (1962). The Formation composes the younger of the two units of the Marburg Subgroup defined in this paper.|16-MAY-23
9839|Koukandowie Formation|Constituents|Two members, the Heifer Creek Sandstone Member and the Ma Ma Creek Member occur within the Koukandowie Formation. In many areas the members cannot be identified, and under the revised stratigraphic scheme the sequence is referred to as undivided Koukandowie Formation.|16-MAY-23
9839|Koukandowie Formation|Type section locality|Reference Section: No type section was given for the Koukandowie Sandstone Member by McElroy. Gray (1975) subsequently nominated the interval in GSQ Ipswich 18 from 203'5" (62.0 m) - 1368'4" (417.07 m) as the reference section for the interval equivalent to the Koukandowie Formation.  Type Section: The interval from 811.15 m to 1070.63 m in GSQ Ipswich 24 is here nominated as the type section, as it is considered that the reference section in GSQ Ipswich 18 is atypical and the boundaries with adjacent units are not readily defined.|16-MAY-23
9839|Koukandowie Formation|Description at type locality|In the type section in GSQ Ipswich 24 the Koukandowie Formation contains about 67% sandstone. The Ma Ma Creek Member contains 54% shale and siltstone whereas the undifferentiated Koukandowie Formation contain 80% sandstone. The sandstone in the undifferentiated upper part of the Koukandowie Formation is fine to coarse grained, commonly in stacked multistorey fining up sequences about 10 m thick in the upper part of the formation and up to 40 m thick in the lower part. The sandstone is mostly cross laminated and rippled. Thin pebble conglomerates occur at the base of channel sands. Interbedded mudstone intervals are 10-12 m thick with fine grained sandstone laminae, cross laminae and rootlets. In places the mudstone exhibits brecciated soil textures. The formation is 259.48 m thick in GSQ Ipswich 24. The description of the Ma Ma Creek Member in GSQ Ipswich 24 is detailed separately.|16-MAY-23
9839|Koukandowie Formation|Extent|The formation has been identified throughout the Clarence Moreton Basin, wherever the Marburg Subgroup is identified. The Koukandowie Formation has been identified in most deep well sections; in the southern Clarence-Moreton Basin it has been continuously cored in Pillar Valley DDH2 stratigraphic drill hole and corresponds to the 'Upper Marburg Formation' of Etheridge et al., (1985).|16-MAY-23
9839|Koukandowie Formation|Depositional environment|The upper part of the Heifer Creek Formation in GSQ Ipswich 24 was laid down as predominantly channel deposits, with flood plain siltstone interspersed with probable fining up crevasse splay sandstones. The lower part of the formation - the Ma Ma creek Member - was deposited in lacustrine conditions with deposition of mainly claystone and shale with chamositic oolite.|16-MAY-23
9839|Koukandowie Formation|Fossils|The formation contains plant fossils and fossil wood and palynomorphs.|16-MAY-23
9839|Koukandowie Formation|Relationships and boundaries|The boundaries of the formation with other units is conformable. The upper boundary of the Koukandowie Formation corresponds to the description of the change of sandstone composition described under the Marburg Subgroup. The lower boundary of the formation is defined as the change from predominantly mudrocks of the Ma Ma Creek Member to the multistory medium to very coarse grained, quartz-lithic to lithic sandstone bodies of the Gatton Sandstone. Where the Ma Ma Creek Member is not recognisable the boundary is the change from the variable sandstone/siltstone/shale sequence of the Koukandowie Formation to the uniform quartz-feldspathic-lithic sandstone and subordinate conglomerate of the Gatton Sandstone.|16-MAY-23
9839|Koukandowie Formation|Identifying features|The sandstone composition, lithological assemblages and associations, and stratigraphic position are the main methods for distinguishing the formation. The characteristics and sequences in the constituent members, where they are identifiable, can also be used to distinguish the formation. Most of the attributes of the formation are shown on the graphic log of GSQ Ipswich 24. The sandstones of the Koukandowie Formation are quartzose to quartz-lithic in composition with silty and clayey matrix and varying amounts of channel base conglomerate and overbank shale. The lithological sequence penetrated in GSQ Ipswich 24 is characteristic of the formation.|16-MAY-23
9839|Koukandowie Formation|Age reasons|The formation contains plant fossils, fossil wood, spores, pollen grains and sporadic acritarchs. The Koukandowie Formation contains palynofloras similar to those formed in the lower Eurombah Formation, Hutton Sandstone and the post-oolite ironstone section of the upper Evergreen Formation of the Surat Basin. The age of the palynoflora is late Toarcian to early Bajocian interpreted principally from McKallar (1974), and McKellor (1981).|16-MAY-23
9839|Koukandowie Formation|Correlations|The Koukandowie Formation is broadly correlated with the Hutton Sandstone of the Surat Basin sequence.|16-MAY-23
9839|Koukandowie Formation|Proposed publication|Wells A.T., O'Brien P.E., Willis I.L. and Cranfield L.C.  A new lithostratigraphic framework for the Early Jurassic units in the Bundamba Group, Clarence-Moreton Basin, Queensland and New South Wales. BMR Journal of Geology and Geophysics.|16-MAY-23
9839|Koukandowie Formation|References|The name Koukandowie 'Sandstone Member' was first proposed by McElroy (1962).|16-MAY-23
9919|Kuridala Group|Name source|The former township of Kuridala at GDA94 coordinates lat. -21.28406 and long. 140.50429, MALBON 1:100 000 Sheet area.|16-MAY-23
9919|Kuridala Group|Unit history|The unit was originally named the Kuridala Formation (White, 1957; Carter, 1959; Carter et al; 1961; Donchak et al., 1983; Blake, 1987; Betts et al., 2000; Giles et al., 2006) and was included in the Mary Kathleen Group by Derrick et al. (1977) and Blake (1987). Beardsmore et al., (1988) renamed the lower part of the unit as 'New Hope Arkose' (which was included in their Fullarton River Group) and assigned the rest of the formation to the Soldiers Cap Group, regarding the name 'Kuridala Formation' as obsolete. Foster & Austin (2008) reinstated the name and included it in the Soldiers Cap Group. Revised mapping by GSQ raised it to group status as Kuridala Group consisting of Starcross Formation, New Hope Sandstone and Hampden Slate (GSQ, 2011; Whitnall & Hutton, 2013) but did not formally define the units.|16-MAY-23
9919|Kuridala Group|Constituents|Starcross Formation (which includes the New Hope Sandstone Member) and Hampden Slate.|16-MAY-23
9919|Kuridala Group|Extent|The Kuridala Group is exposed as a belt of rocks that is up to 15km wide and 90km long with its northern extent in the Hampden Syncline near Kuridala, 65km south of Cloncurry. It is transected by the headwaters of the Cloncurry and Mort Rivers. The Kuridala Group has been dominantly mapped in south-eastern Malbon (7054) and the western parts of the Mount Angelay (7055), Selwyn (7054) and Toolebuc (7053) 1: 100 000 Sheet areas.|16-MAY-23
9919|Kuridala Group|Relationships and boundaries|Intruded by numerous sills of metadolerite and metagabbro and by the Mesoproterozoic granitoids of the Williams Supersuite. Faulted against the Staveley Formation along the Mount Dore Fault Zone.  Parent Unit: Beardsmore et al., (1988) assigned the Soldiers Cap Group -in which they included most of the 'Kuridala Formation' - and their Fullarton River Group to the Maronan Supergroup. Foster & Austin (2008)  and revised mapping by GSQ (GSQ, 2011) discontinued usage of the name Fullarton River Group and re-assigned the rocks to various units of the Soldiers Cap Group. It is proposed that the Maronan Supergroup continue to be used as a parent unit for the Kuridala Group and Soldiers Cap Group.|16-MAY-23
9919|Kuridala Group|Identifying features|Basal micaceous psammopelitic beds with common andalusite porphyroblasts (Starcross Formation), locally intercalated towards the top with repeated thick bedsets of coarse-grained sandstone (New Hope Sandstone Member); the upper part of the group consists of micaceous phyllitic schist and carbonaceous slate (Hampden Slate).|16-MAY-23
9919|Kuridala Group|Structure and Metamorphism|Complexly folded with a common bed-parallel foliation and crenulation cleavage; common andalusite porphyroblasts indicate upper greenschist to amphibolite facies metamorphism.|16-MAY-23
9919|Kuridala Group|Age reasons|Paleoproterozoic (Statherian). SHRIMP dating of detrital zircons indicates a maximum depositional age of ~1690 Ma for the Starcross Formation and New Hope Sandstone Member (Online Geochronology Delivery System; Withnall, in preparation). It was deformed by the 1600-1570 Isan Orogeny and later intruded by the Mesoproterozoic granitoids of the Williams Supersuite.|16-MAY-23
9919|Kuridala Group|Correlations|Correlates broadly with the Soldiers Cap Group.|16-MAY-23
9919|Kuridala Group|Defn author|Alexander P. Slade and Ian W. Withnall (Geological Survey of Queensland) 21-MAR-2018.|16-MAY-23
9919|Kuridala Group|Proposed publication|Queensland Geological Record|16-MAY-23
9919|Kuridala Group|References|Betts, P.G., Ailleres, L., Giles, D. and Hough, M., 2000. Deformation history of the Hampden Synform in the Eastern Fold Belt of the Mt Isa terrane. Australian Journal of Earth Sciences, 47(6), 1113-1125.  **Blake, D.H., 1987. Geology of the Mount Isa Inlier and Environs. Bureau of Mineral Resources, Australia, Bulletin 225.  **Carter, E.K., 1959. New stratigraphic units in the Precambrian of north-western Queensland. Queensland Government Mining Journal, 60(692), 437-431.  **Carter, E.K., Brooks, J.H. and Walker, K.R., 1961. The Precambrian mineral belt of north-western Queensland. Bureau of Mineral Resources, Australia, Bulletin 51.  **Derrick, G.M., Wilson, I.H. and Hill, R.M., 1977. Revision of stratigraphic nomenclature in the Precambrian of northwestern Queensland. VI. Mary Kathleen Group. Queensland Government Mining Journal, 78, 15-23. **Donchak, P.J.T., Blake, D.H., Noon, T.A. and Jaques, A.L., 1983. Kuridala Region, 1: 100 000 Geological Map Commentary. Bureau of Mineral Resources, Australia, Canberra.  **Foster, D.R.W., Austin, J.R., 2008. The 1800¿1610 Ma stratigraphic and magmatic history of the Eastern Succession, Mount Isa Inlier, and correlations with adjacent Paleoproterozoic terranes, Precambrian Research, 163, 7¿30 doi:10.1016/j.precamres.2007.08.010  **Giles, D., Betts, P.G., Ailleres, L., Hulscher, B., Hough, M. and Lister, G.S., 2006. Evolution of the Isan Orogeny at the southeastern margin of the Mt Isa Inlier. Australian Journal of Earth Sciences, 53(1), 91-108.  **GSQ, 2011. North-West Queensland Mineral and Energy Province Report. Department of Employment, Economic Development and Innovation. Queensland Government.  **White, W.C., 1957. Preliminary report on the geology of the Selwyn area of N.W. Queensland. Bureau of Mineral Resources, Canberra. Australian Record 1957/094.  **Withnall, I.W., in preparation. Review of zircon ages for the eastern Succession of the Mount Isa Province. Queensland Geological Record.  **Withnall, I.W., and Hutton, L.J., 2013. Chapter 2: North Australian Craton, in Jell, P. A., editor, Geology of Queensland. Brisbane, Geological Survey of Queensland, 23-112.|16-MAY-23
10002|Lady Loretta Formation|Name source|Lady Loretta mine, 35 km southwest of Mammoth mine at GR 971121 in the Mammoth Mines 1:100 000 Sheet area.|16-MAY-23
10002|Lady Loretta Formation|Unit history|The rocks now included in the Lady Loretta Formation were included in the Paradise Creek Formation and Ploughed Mountain Beds by Carter & others (1961).|16-MAY-23
10002|Lady Loretta Formation|Type section locality|Holostratotype: 10 km northeast of Thorntonia homestead between GR 923500 (base) and GR898500 in the Mount Oxide 1:100 000 Sheet area. The section lies due east of the Burketown-Camooweal road; its top is 2 km east of the road while its base is 500 m east of the Thornton River. The holostratotype comprises a basal sequence of ferruginous and altered laminated and stromatolitic dolomite, overlain by a less latered sequence of laminated and intraclast dolomite stromatolitic dolomite and possible tuff which in turn is overlain by a thin band of green and mauve indurated siltstone and shale. Interbedded laminated and intraclast dolomite overlain by medium bedded, flaggy, sporadically dolomitic sandstone complete the sequence in the holostratotype.  Hypostratotype: 5 km south of Lady Annie mine, northeasterly for 5 km to the Lady Loretta mine (953068 (base) to 975129 (top)) in the Mammoth Mines 1:100 000 Sheet area. The lithologies in this section are different to those in the Holostratotype and comprise variably pyritic, dolomitic and carbonaceous shale and siltstone with minor sandstone, quartzite, dolarenite, chert, barite, tuff and bedded silver-lead-zinc deposits.|16-MAY-23
10002|Lady Loretta Formation|Extent|The northernmost outcrops of the unit are in the cores of the Mount Caroline and Ploughed Mountain anticlines in the Mount Oscar Lawn Hill 1:100 000 Sheet areas. The unit is best exposed around the Kamaraga dome and in several anticlines and synclines in the Lawn Hill and Riversleigh 1:100 000 Sheet areas. It crops out as a long narrow, sometimes tightly folded, belt which extends through Riversleigh, Mount Oxide, Mammoth Mines and Undilla 1:100 000 Sheet areas and which includes the Lady Loretta syncline; and it forms isolated outcrops in the Mammoth Mines, Kennedy Gap and Yelvertoft 1:100 000 Sheet areas.|16-MAY-23
10002|Lady Loretta Formation|Thickness range|The formation is 1800 m thick in the holostratotype but less than 600 m in the hypostratotype. The thickest development is in the Lawn Hill 1:100 000 Sheet area where over 2000 m is exposed, and in general the unit thins southward.|16-MAY-23
10002|Lady Loretta Formation|Lithology|Apart from the area around the hypostratotype, the lithologies in the holostratotype are typical of those throughout the outcrop area. The ferruginous and cherty breccia at the base of the formation grades into a cyclic sequence of alternating high spire Conophyton beds and cream laminated dolomite and "cauliflower chert" beds.|16-MAY-23
10002|Lady Loretta Formation|Relationships and boundaries|The unit conformably overlies the Esperanza Formation and is conformably overlain by the Shady Bore Quartzite. The basal contact is sharp and is commonly marked by a ferruginous breccia overlying massive chert beds. The upper boundary is gradational and is placed where massive orthoquartzite beds form more than 25 per cent of the sequence.|16-MAY-23
10002|Lady Loretta Formation|Age reasons|Mid Proterozoic (Carpentarian).|16-MAY-23
10002|Lady Loretta Formation|Proposer|Hutton L.J., Cavaney R.J., Sweet I.P.|16-MAY-23
10047|Lake Galilee Sandstone|Name source|From ENL Lake Galilee 1 well; Latitude 22o11'30"S, Longitude 145o58'32"E. The type section is in this well.|16-MAY-23
10047|Lake Galilee Sandstone|Type section locality|In ENL Lake Galilee 1 from 2578 m (8458 ft) to 2841 m (9320 ft) K.B. Cuttings and cores from this interval are available at the Core Library, Redbank.|16-MAY-23
10047|Lake Galilee Sandstone|Extent|In the following wells - ENL Lake Galilee 1, FPN Koburra 1 and AOD Jericho 1; it has been continuously cored in GSQ Jericho 2.|16-MAY-23
10047|Lake Galilee Sandstone|Thickness range|263 m in the type section; 145m+ and 84 m thick, in GSQ Jericho 2 and AOD Jericho 1 respectively. The unit is present but its limits are not clearly defined in FPN Koburra 1.|16-MAY-23
10047|Lake Galilee Sandstone|Lithology|Silicified sandstone with minor amounts of mudstone in the upper part. Cores 31 to 35 inclusive were cut in the type section and are described in detail by Pemberton in Exoil N.L. (1965). Sandstone is light to medium grey, very fine to medium, generally well sorted and quartzose. It consists of subround to angular quartz grains in a quartz cement. Conglomeratic bands are present, containing rounded pebbles of quartz, quartzite, chert, and intraformational clasts. Mudstone is dark grey to black, fissile and locally interbedded with light to dark grey, argillaceous, siliceous siltstone; silicification is secondary.|16-MAY-23
10047|Lake Galilee Sandstone|Depositional environment|Probably fluviatile.|16-MAY-23
10047|Lake Galilee Sandstone|Relationships and boundaries|The Lake Galilee Sandstone is the basal unit of the Joe Joe Group. It overlies pre-Late Carboniferous strata unconformably; it is conformably overlain by the Jericho Formation.|16-MAY-23
10047|Lake Galilee Sandstone|Age reasons|Late Carboniferous to Early Permian.|16-MAY-23
10047|Lake Galilee Sandstone|Defn author|Geological Survey of Queensland, 1975|16-MAY-23
10047|Lake Galilee Sandstone|Name first published by|Gray A.R.G., Swarbrick C.F.J., 1975|16-MAY-23
32276|Lakes Creek Formation|Name source|The first reference to the Lakes Creek beds was by Smith (1887) detailing fossils within indurated, pyritic shale.|16-MAY-23
32276|Lakes Creek Formation|Unit history|A detailed study of the the Lakes Creek Quarry area covering approximately 3 km2 was conducted by East (1946), who defined an approximately 800 m sequence, as detailed in the previous section. Intrusive bodies of diorite, feldspar porphyry and quartz-feldspar porphyry were also found.East (1946) also described a NE trending fault which bisects the quarry area, the south block defined by westerly dipping beds, and the north block by a series of antiforms and synforms. These structures are consistent with observations during present mapping.Other references to the Lakes Creek beds include Jack and Etheridge (1892) who referred to Thozet¿s Creek beds overlying Lakes Creek beds, Whitehouse (1928a, 1928b, 1930), Reid & Morton (1928), Reid (1930), Bryan (1929), Crockford (1945), Bryan & Jones (1946), Maxwell (1960), Armstrong & others (1967), and Runnegar (1970).The Lakes Creek beds were included in the Berserker beds by the Geological Survey of Queensland in 1966 (Kirkegaard & others, 1966).|16-MAY-23
32276|Lakes Creek Formation|Geomorphic expression|The Lakes Creek Formation occupies generally flat, low areas although steeper terrain is common adjacent to the large rhyolite to dacite domes especially on the southern margin of the Berserker Range. The terrain is characterised by a widely spaced dendritic drainage pattern.|16-MAY-23
32276|Lakes Creek Formation|Type section locality|The type area of the Lakes Creek Formation is designated here as a 1 km2 area bounded by the Lakes Creek Quarry on the west and Nerimbera settlement to the east. In the type area, the unit is dominated by interbedded siltstone and sandstone with local fossiliferous beds. Calcareous sandstone to limestone is restricted to Lakes Creek Quarry.|16-MAY-23
32276|Lakes Creek Formation|Extent|North of the Fitzroy River, the Lakes Creek Formation crops out in the Mount Etna area, east of Mount Belmont, and north of Rockhampton. It is also SE of Rockhampton encompassing the type area near Lakes Creek, extending east to Nankin. South of the Fitzroy River, the Lakes Creek Formation forms outcrops in a belt about 7 km long west of the peak of Mount Larcom, and a larger outcrop SE of the Targinie Granite.|16-MAY-23
32276|Lakes Creek Formation|General description|The Lakes Creek Formation comprises grey, massive, interbedded siltstone and sandstone with local fossiliferous beds (Figure 4).|16-MAY-23
32276|Lakes Creek Formation|Thickness range|East (1946) interpreted the Lakes Creek Formation to be approximately 800 m thick at Lakes Creek based on structural evidence. However, near the peak of Mount Larcom the unit may be substantially thinner.|16-MAY-23
32276|Lakes Creek Formation|Lithology|The Lakes Creek Formation is a sequence of grey, massive, indurated siltstones and lithofeldspathic to quartzofeldspathic sandstones derived from felsic to intermediate volcanics. This sequence is composed of generally thin to medium beds of siltstone, fine to medium grained, well sorted sandstone, and chert, giving the rock a banded appearance. Less common moderate to poorly sorted, granule to pebbly sandstones are found locally, and contain angular to rounded clasts of fine grained sediments and volcanics.Sedimentary structures include local occurrences of soft sediment deformation features, and rhythmic bedding which was found near Nankin, consisting of thin planar siltstone beds and thin, planar to disrupted sandstone beds.Fossiliferous calcareous sandstone to limestone exists at Lakes Creek but is not apparent elsewhere within the sequence. Similar rocks have been found further south near Mount MacDonald,and 2 km NW of Mount Kilner, but are associated with volcanic beds indicative of the Chalmers Formation.Silicification resulting in induration is common throughout the area. Local hematitic and limonitic alteration is also present in association with felsic to intermediate intrusives.|16-MAY-23
32276|Lakes Creek Formation|Depositional environment|The presence of a wide variety of marine fossils, and the type of sediments and sedimentary structures suggest the Lakes Creek Formation formed in a shelf environment. Deposition below wave base is suggested by the common occurrence of fossils lacking effects of abrasion, including the presence of fine spines on brachiopods and of entire blastoid cups. The fauna of brachipods, molluscs, and bryozoans is considered to be typical of that found in water depths of around 30-50 m, and no deeper than 200 m.|16-MAY-23
32276|Lakes Creek Formation|Fossils|Marine fossils correlative with faunas of the Lower Permian Buffel Formation of the Bowen Basin have been collected from Lakes Creek Quarry, at Lakes Creek, Artillery Road, 8 km NNW of Cabbage Tree Hill and 6 km NNW of the peak of Mount Larcom. These include abundant fenestellid bryozoans, Echinalosia warwicki (Maxwell, 1954), Anidanthus sp , Taeniothaerus n. sp, Costatumulus farleyensis (Etheridge & Dun, 1909), and Sulciplica sp. (Figure 5).|16-MAY-23
32276|Lakes Creek Formation|Relationships and boundaries|The Lakes Creek Formation is probably laterally equivalent to the Chalmers Formation with the latter containing sediment similar to the Lakes Creek Formation interbedded with volcaniclastic rock (Figure 3). Shallowly dipping siltstone and sandstone beds of the Lakes Creek Formation overlie more steeply dipping volcaniclastic conglomerate of the Upper Devonian to Lower Carboniferous Mount Alma Formation 3 km east of Mount Etna. Structural measurements, fossil data and radiometric evidence suggests that gently to moderately folded fossiliferous Lakes Creek Formation overlies steeply dipping siltstone and mudstone beds of the Lower Carboniferous Rockhampton Group in an area 3 km west of the peak of Mount Larcom. An angular unconformity is inferred in these two areas. The angular unconformity between Lower Carboniferous Rockhampton Group and Lower Permian Berserker Group contrasts with a previous structural interpretation which defines a narrow fault bounded sliver of Carboniferous rocks 10 km NW of the peak of Mount Larcom, as described in Donchak & Holmes (1991).The Lakes Creek Formation is intruded by rhyolites and dacites of the Ellrott Rhyolite, andesite dykes and gabbro bodies. The contacts are sharp and steep, and metamorphism is weak.|16-MAY-23
32276|Lakes Creek Formation|Defn Reference|SOURCE OF INFORMATION --Crouch. S, Parfrey. S, and Taube. A  [DATE ?]. 'Geology, tectonic setting and metallogenesis of the Berserker Subprovince, northern New England Orogen'. Supplied by Ian Withnall (GSQ), September 2008.(Incomplete reference)|16-MAY-23
25986|Lakeview Dolerite|Name source|Lakeview mine (M.L. 5720, Cloncurry Mining District) 8 km southeast of Mary Kathleen, Latitude 20o50'S, Longitude 140o1'25"E (6956 985958) is approximately 200 m east of the largest dyke of this Dolerite.|16-MAY-23
25986|Lakeview Dolerite|Geomorphic expression|The Lakeview Dolerite forms elongate valleys containing deep soil, scattered well-rounded dolerite boulders and rare rock pavements. Country rocks adjacent to the dykes are in many places more elevated than the surrounding exposures of these rocks.|16-MAY-23
25986|Lakeview Dolerite|Type section locality|A boulder strewn pavement 500 m north of Lakeview mine exposes a typical section of the main dyke, which is 35 km long and up to 150 m thick.|16-MAY-23
25986|Lakeview Dolerite|Extent|Dolerite which shows no evidence of regional metamorphism and which occurs as east to northeast-trending dykes is assigned to the Lakeview Dolerite. Dykes of this dolerite occur in the Mary Kathleen and the western part of the Marraba 1:100 000 Sheet areas. Some dykes in the surrounding Sheet areas are probably of the same type and age but until more extensive radiometric dating is done on these bodies they have been mapped as undivided dolerite dykes. The main dyke extends from Ballara, 18 km south of Mary Kathleen, northeastwards for about 35 km towards Corella Park homestead.|16-MAY-23
25986|Lakeview Dolerite|Thickness range|The dykes of this dolerite range from approximately 10 to 50 m thick.|16-MAY-23
25986|Lakeview Dolerite|Lithology|The dolerite typically has fine-grained margins of intersertal textured dolerite and a medium to coarse-grained core of ophitic textured dolerite. The dolerite contains two pyroxenes, abundant hornblende and some biotite. Irregular patches of alteration to chlorite and serpentine are thought to have resulted from autometamorphism.|16-MAY-23
25986|Lakeview Dolerite|Relationships and boundaries|The Lakeview Dolerite intrudes the Corella Formation, the Lunch Creek Gabbro and the Burstall Granite. Because the Dolerite is virtually undeformed it is thought to have been intruded after the main period of folding in the layered Middle Proterozoic rocks.|16-MAY-23
25986|Lakeview Dolerite|Age reasons|Green (1975) obtained a potassium/argon biotite date on the Lakeview Dolerite of 1380 m.y. A rubidium/strontium age of 116+/-12 m.y. has been obtained by Page (1975, pers. comm.).|16-MAY-23
25986|Lakeview Dolerite|Comments|Discussion: This un;it has been shown by radiometric dating to be one of the youngest Precambrian units in northwestern Queensland. Dykes of this age are designated do6 on the 1:100 000 Preliminary Geological Maps. The Lakeview Dolerite was definitely post-tectonic and was intruded after cooling of the country rock.|16-MAY-23
25986|Lakeview Dolerite|Defn approved by|Queensland Sub-Committee|16-MAY-23
24353|Lane Creek Formation|Name source|Lane Creek, a tributary of Fiery Creek which it joins at GR 581075 (Forest Home 1:100 000 Sheet area).|16-MAY-23
24353|Lane Creek Formation|Geomorphic expression|The Lane Creek Formation forms relatively subdued relief, but bedding trends have been picked out by differential weathering and erosion in places. On coloured aerial photographs, the formation is characterised by a greyish tone due to the abundant carbonaceous rocks; calc-silicate rocks within the formation give rise to reddish soils.|16-MAY-23
24353|Lane Creek Formation|Type section locality|The holostratotype is along the Robertson River for about 2 km between the QWRC stream gauging station at GR484233 (base) and 471251 (top) (North Head 1:100 000 Sheet area). A maximum of 2500 m is exposed but the thickness is likely to be considerably less because of repetition by minor folds. Variably carbonaceous, cleaved mudstone, siltstone, and minor fine-grained sandstone are exposed. Withnall & Mackenzie (1980) designated this section as a reference section (hypostratotype) of the Robertson River Formation (now Subgroup). Reference section: more highly metamorphosed rocks are exposed along the Forsayth-Agate Creek road for about 17 km between GR 605232 and 636350 (North Head 1:100 000 Sheet area), and area designated as a parastratotype of the Lane Creek Formation. The rocks consist of mica schist, carbonaceous phyllite and schist, quartzite, and minor calc-silicate rocks.|16-MAY-23
24353|Lane Creek Formation|Extent|The main outcrop area is a broad sinuous belt extending northwest from the Ropewalk Range to near Huonfels homestead and then northeast to the Newcastle Range. Smaller areas occur in the North Head 1:100 000 Sheet area between Mount Clarke and Mount Johnstone, and near Malcolms Creek and Dry Pocket. The total area of the formation is about 2000 km2.|16-MAY-23
24353|Lane Creek Formation|Thickness range|The thickness of the Lane Creek Formation is indeterminate in most areas because of the complex deformation. However, in the western part of the area, where the structure is less complex, the formation is 1000 to 2000 m thick.|16-MAY-23
24353|Lane Creek Formation|Lithology|The Lane Creek Formation consists of cleaved, variably carbonaceous mudstone, siltstone and fine-grained sericitic to quartzose sandstone, and local calcareous siltstone and impure limestone; these grade eastwards into their metamorphic equivalents. The metamorphic grade ranges from greenschist to upper amphibolite facies.|16-MAY-23
24353|Lane Creek Formation|Relationships and boundaries|The Lane Creek Formation is the uppermost unit of the Robertson River Subgroup. It conformably overlies the Corbett Formation, from which it is distinguished by its abundant carbonaceous rocks. In some places (including the type section), resistant ridge-forming green mudstone occurs at the top of the Corbett Formation, and marks its upper boundary. The Lane Creek Formation is overlain conformably by the Townley Formation, and the boundary is recognised by the change from the predominant carbonaceous rocks to white and pale grey siltstone, and fine-grained quartzose sandstone. The Townley Formation is also topographically more prominent than the Lane Creek Formation, and has a lighter tone on aerial photographs. The Lane Creek Formation is intruded by sills of Cobbold Metadolerite as well as by various Proterozoic granitoid plutons, late Palaeozoic hypabyssal rocks, and the Permian Yataga Granodiorite. It is overlain unconformably by various late Palaeozoic volcanic units, and the Jurassic Hampstead Sandstone.|16-MAY-23
24353|Lane Creek Formation|Age reasons|The minimum age of 1570+/-20 Ma (mid-Proterozoic) obtained for the Etheridge Group, also applies to the Lane Creek Formation.|16-MAY-23
24353|Lane Creek Formation|Unit name|Lane Creek Formation (new name)|16-MAY-23
27818|Langdon River Mudstone|Type section locality|As per the definition for the Langdon River Siltstone: White designated the type area as the track between Forest Home and Candlow Dam along the eastern side of the valley of the Langdon River. We restrict the type section to that part of the track between GR 7560-11913288 and -11453390; a section in Candlow Creek about 0.5 km east, between -12653287 and 12703368 is better exposed and designated as a reference section.|16-MAY-23
27818|Langdon River Mudstone|Lithology|Variation: Withnall & Mackenzie (1980) redefined White's (1959) 'Langdon River Formation' as 'Langdon River Siltstone'. The rocks were incorrectly classified in the field as siltstone, and are in fact predominantly mudstone. We therefore propose that the name be varied to Langdon River Mudstone.|16-MAY-23
27818|Langdon River Mudstone|Proposed publication|Queensland Government Mining Journal|16-MAY-23
28247|Langlovale Group|Name source|Langlovale (also known as 'Langdon', and 'Langlo') homestead, now an outstation of 'Lake Carlo', GR 7561*-103600 near the Langdon River, 60 km WSW of Georgetown.|16-MAY-23
28247|Langlovale Group|Unit history|Rocks of the Langlovale Group were considered to be part of either the 'Langdon River Formation' or the 'Etheridge Formation' by White (1965).|16-MAY-23
28247|Langlovale Group|Constituents|Yarman Formation underlain by Malacura Sandstone (defined by Withnall & Mackenzie (1980)).|16-MAY-23
28247|Langlovale Group|Extent|Exposed along most of the valley of the Langdon River, from 7460*-070140 north to the Gilbert River; small outliers crop out on the northern side of the Gilbert River near 'Forest Home' homestead (around 7561*-135800) and near 'Boomerang Swamp', around 7461*-800025.|16-MAY-23
28247|Langlovale Group|Thickness range|Variable; up to at least 3200 m.|16-MAY-23
28247|Langlovale Group|Lithology|Dark grey (weathering to red-brown) shale, mudstone, and siltstone with 5-10% 10 mm to 1 m-thick interbeds of cross-laminated sandstone (Yarman Formation); fine to medium feldspathic, commonly micaceous sublithic to quartzose sandstone, siltstone, silty sandstone, sandy siltstone, and dark grey shale; minor carbonaceous quartzose mudstone and very coarse sublithic sandstone; sandstones predominant (Malacura Sandstone).|16-MAY-23
28247|Langlovale Group|Relationships and boundaries|Unconformably overlies Etheridge Group (Withnall & Mackenzie, 1980); in places unconformably overlain by, in others faulted against Croydon Volcanics; intruded by Esmeralda Granite and possibly by Forest Home Granodiorite; unconformably overlain by Mesozoic sandstones.    *1:100 0000 Sheet areas - see continuation card.|16-MAY-23
28247|Langlovale Group|Age reasons|Probably Middle Proterozoic; underlying rocks have been affected by deformation and metamorphism, dated at 1570+/-20 m.y. (Black & others, 1979), which do not affect the Langlovale Group; the Group is overlain by Croydon Volcanics dated at 1429+/-75 m.y. (Black, 1973).|16-MAY-23
28247|Langlovale Group|Proposer|Mackenzie D.E., Withnall I.W.|16-MAY-23
36349|Langton Dolerite|Name source|After Langton Road next to the West of Scotland shaft, Gympie.|16-MAY-23
36349|Langton Dolerite|Unit history|The term Langton Dolerite was first used informally by Gympie Eldorado Gold Mines at Monkland Mine.  It was formally registered with member status following publication by Sivell and McCulloch (2001).  It is also documented in Sivell and Arnold (1999) and Cranfield (1999). Herein raised to formation rank.|16-MAY-23
36349|Langton Dolerite|Type section locality|Although outcrop is very limited an exposure can be seen on the Heritage rail line about 100m NW of the Six Mile Oval at MGA 469445mE; 7098940mN (Lat: -26°13'44" Long: 152°41'39") .  This is a complex zone close to the Sovereign East Fault.  Access is from the east end of Laurenceson Road which downgrades to a dirt road across the rail line. Proceeding from this rail crossing, outcrop occurs in a low cutting along the west side of the line; from about 60-100m is weathered sandstone, from 100-200m is Langton Dolerite, then up to 250m is Glanmire Conglomerate containing flattened rounded cobbles, dipping about 30-40° east. Complete sections can be seen in drill holes G023, depth 31-73 (collar (MGA 468 180mE; 7100900mN , Lat:-26°12'40" Long: 152°40'53"); G135, depth 23-67m (MGA 468180mE; 7100885mN, Lat: -26°12'40", Long: 152°40'53"; G137: depth 206-272m (MGA 468390mE; 7100785mN, Lat: -26°12'44" Long: 152°41'01") and G224: depth 6-15m (MGA 469520mE; 7098880mN, Lat:-26°13'46" Long: 152°41'41"), all held in Zillmere storage facility, Brisbane.|16-MAY-23
36349|Langton Dolerite|Description at type locality|Outcrop is massive and amygdaloidal.|16-MAY-23
36349|Langton Dolerite|Extent|From Six Mile Block northwards through Monkland and Phoenix blocks to west of Bruce Highway in Pinewoods Block. Also at Partridge and Wylly prospects, Jones Hill and Dawn blocks. Commonly associated with thrust faulting.|16-MAY-23
36349|Langton Dolerite|Thickness range|Up to about 70m at Monkland, decreasing to about 10 m in the northern part of the Phoenix Block (Dugdale, 2004). Some 20 m is present in the Pinewoods Block, located immediately above a thrust fault and overlain by Glanmire Conglomerate. About 10-20 m thick in the Partridge graben.|16-MAY-23
36349|Langton Dolerite|Lithology|Typically a massive fine grained dolerite within which are numerous amygdaloidal zones.  However it is texturally variable due to alteration and structural deformation.  Composed of randomly interlocking, sometimes flow aligned laths of plagioclase which are albitised or completely altered to fine decussate sericite and rare chlorite.  Laths are about 0.1 x 0.5mm in size, some larger, and they constitute 25% to 50% of the rock.  The interstitial groundmass includes very fine quartz or albite, chlorite, clays, sericite and patches of carbonate. Mafic phenocrysts are rare, up to about 10%, replaced by fine chlorite, leucoxene, minor epidote and quartz.  The original minerals have been interpreted as both pyroxene and hornblende.  Fresh olivine dissected by skeletal magnetite was also observed. Characteristic are the presence of numerous irregular vesicles, 1-10mm in diameter, filled with calcite lined with chlorite, sericite-chlorite, microspherulitic quartz-chlorite, or chlorite alone.|16-MAY-23
36349|Langton Dolerite|Relationships and boundaries|This unit can be difficult to recognize on surface and was rarely noted by historic miners. Its origin was much debated, being described variously as basalt, andesite and dolerite.  The eventual consensus at the mine was an intrusive sill of fine amygdaloidal dolerite which is pre-veining and pre-mineralisation.  Because of its fine grain and amygdaloidal nature it must have been a high level intrusive. Its position in the stratigraphic column is enigmatic in that in places it occurs below the South Curra Limestone and in others it occurs below the Glanmire Conglomerate.  It is particularly associated with the Curra Thrust.  At Monkland Mine both contacts are closely associated with carbonaceous shears or breaks, termed the Top and Bottom breaks at the mine.  When in contact with the Curra thrust (Top break position), the dolerite is strongly sheared and its texture consists of dark green mafic lenses in a light green groundmass, resembling an ignimbrite.   Where the shearing intensifies, it becomes serpentinised, with yellow green or black soapy illitic clay which causes drilling problems. XRD tests identified the serpentine minerals as lizardite, amesite and berthierine (Paul Ashley, University of New England, 2001, in Houston & others, 2001).|16-MAY-23
36349|Langton Dolerite|Alteration and Mineralisation|See lithology.|16-MAY-23
36349|Langton Dolerite|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie, 12-JAN-2017.|16-MAY-23
36349|Langton Dolerite|References|Cranfield, L.C., 1999: Gympie Special Sheet 9445, Part 9545, Queensland 1:100,000 Geological Map Commentary. Queensland Department of Mines and Energy, Brisbane.  **Sivell, W.J. and Arnold, G.O. 1999: Geochemical and volcanic stratigraphy of a segment of an island arc - Gondwana rim accretion zone, Gympie Province, southeast Queensland.  IN Flood, P.G. (Editor): Regional Geology, Tectonics and Metallogenesis, New England Orogen, NEO '99 Conference, 255-266.  **Sivell, W.J. and McCulloch, M.T. 2001: Geochemical and Nd-isotopic systematics of the Permo-Triassic Gympie Group, southeast Queensland.  Australian Journal of Earth Sciences 48, 377-394.  **Houston, M., McQuitty, B. and Murray, A.	2001: Exploration Permits for Minerals 6031, 10578, 10843, 10844, 11122, 11123, 11552, 12298. Gympie Project.  Annual combined report for period ending 31st October 2001.|16-MAY-23
22167|Larramore Metabasalt Member|Name source|The member is named after Larramore Creek, a major tributary of the North Palmer River in southeastern LAURA.|16-MAY-23
22167|Larramore Metabasalt Member|Geomorphic expression|Chert lenses in the Larramore Metabasalt Member are resistant to erosion and tend to form steep-sided narrow ridges.  Deeply incised and rugged country is developed on the member in the north, where the local relief commonly exceeds 100 m.  A maximum relief of 400 m is attained in the Mount Hann area.  Mount Hann has an elevation of 712 m and Woods Peak, to the south, an elevation of 751 m and a local relief of about 200 m (Royal Australian Survey Corps, 1982).   The chert lenses generally show pale tones on aerial photographs.  Mafic volcanics crop out poorly and are characterised by dark tones.  Weathering of the volcanics has resulted in the extensive development of a thin red-brown ferruginous soil cover.|16-MAY-23
22167|Larramore Metabasalt Member|Type section locality|The designated type area is in and adjacent to the Palmer River upstream of its junction with Granite Creek (in MAYTOWN).  The river cuts across bedding trends at high angles and the sequence is well exposed.|16-MAY-23
22167|Larramore Metabasalt Member|Extent|The member forms a prominent northwest to northeast-trending belt, up to 3 km wide.  This belt extends from the upper reaches of Chinky Creek (in southern LAURA) 30 km south to the abandoned Cannibal Creek tin mine (in central-eastern MAYTOWN).  Farther to the southwest, in the Mount Madden - Stony Creek area, the member outlines a structural dome about 25 km in circumference.  The sequence is intensely deformed in this area and extensively disrupted.|16-MAY-23
22167|Larramore Metabasalt Member|Thickness range|The thickness of the member is uncertain because of extensive deformation and the likelihood of repetition of parts of the sequence by difficult-to-detect bed-parallel thrust faults.  The member has a maximum outcrop width of about 3000 m.|16-MAY-23
22167|Larramore Metabasalt Member|Lithology|The sequence exposed in the type area consists mainly of metabasalt lava flows with numerous interlayered chert lenses ranging from about 2 m to 20 m thick, and minor greywacke, mudstone, and tuffaceous(?) sediments.  In the North Palmer River, to the north, the eastern (oldest?) part of the member consists of a relatively thick sequence of metabasalt lava flows.  Chert lenses are concentrated in the western part of the unit; they are not as common as in the Palmer River section.  The western part of the North Palmer River section also contains some interlayered, strongly cleaved phyllitic mudstone and fine-grained greywacke, which is mapped as part of the undivided Hodgkinson Formation.  The metabasalts in the belt north of Cannibal Creek are dark grey to greenish grey and extensively recrystallised to fine to medium-grained aggregates of mainly tremolite/ actinolite, clinozoisite/epidote, and albite.  Minor and accessory minerals (not all present in every sample) include calcite, quartz (characterised by highly irregular grain boundaries and undulose extinction), sphene/leucoxene, sericite/muscovite, pyrite and chlorite (colourless or, rarely, very pale green).  The minerals show no obvious preferred orientation except in samples from or adjacent to major shear zones (e.g., at GR 2199 82322).  The metabasalts examined from this belt show only poorly preserved or, more rarely, no relict igneous textures.  Porphyritic textures are the most common.  Scarce, turbid, extensively altered groundmass grains (up to about 1.5 mm long) and phenocrysts (up to 6 mm long) of calcic plagioclase are present in many samples.  The plagioclase grains are replaced mainly by albite(?), sericite/muscovite, clinozoisite/epidote and calcite.  Metabasalt from the summit of Mount Bennett shows a relict porphyritic texture but is atypical compared with the other samples examined in that the calcite grains are relatively coarse (0.3 mm - 1.5 mm long) - most appear to be pseudomorphing clinopyroxene (as mainly subhedral, tabular grains).  The metabasalts are mainly massive but amygdaloidal zones are present locally (e.g., at GR 2205 82326, in the North Palmer River).  Very few, if any primary structures and textures are preserved in the mafic volcanics exposed in the structural dome southwest of Cannibal Creek, due to extensive deformation and recrystallisation.  The metabasalts are commonly cut by thin veinlets of quartz +/- clinozoisite/epidote (zoned) +/- chlorite, and of calcite +/- quartz +/- clinozoisite/epidote +/- chlorite +/- muscovite.  Vuggy quartz veins up to 30 cm thick also cut the sequence in Granite Creek.  The cherts are white, pale brown to dark red-brown, grey, olive green or black, and fine grained; the radiolarian probably originated from the deposition of primary siliceous oozes...The interlayered siliciclastic sediments consist mainly of pale brown, pale to dark grey, or black phyllitic mudstone and brown or grey, fine to medium-grained greywack|16-MAY-23
22167|Larramore Metabasalt Member|Relationships and boundaries|The Larramore Metabasalt Member forms a prominent marker unit in the Hodgkinson Formation in the eastern part of MAYTOWN and adjoining LAURA to the north.  Amos & de Keyser (1964), Lucas & de Keyser (1965), and de Keyser & Lucas (1968) included the rocks of the Larramore Metabasalt Member in the Hodgkinson Formation.  The member is concordant with the enclosing siliciclastic metasediments of the Hodgkinson Formation.  It is therefore tentatively interpreted to conformably overlie and to be conformably overlain by siliciclastic sediments of the Hodgkinson Formation.  Nevertheless the member is bounded and cut by prominent broken-formation zones in the north.  The member may be extensively disrupted internally by low-angle or bed-parallel thrust faults.  The member is cut by numerous thin (generally <3 cm thick) quartz veins and scattered dolerite dykes.|16-MAY-23
22167|Larramore Metabasalt Member|Structure and Metamorphism|The metabasalts commonly show a weak to prominent tectonic foliation.  The foliation is most intensely developed southwest of Cannibal Creek tin mine, in the Mount Madden - Stonyville area, where the rocks are generally characterised by a prominent platy fabric.  The sequence in this area outlines a broad structural dome about 25 km in circumference, but on a detailed scale the rocks are intensely folded and faulted.   The cherts are generally extensively deformed; mesoscopic folds are common north and south of Cannibal Creek tin mine and they generally show a well-developed foliation.  The foliation is most intensely developed in the Mount Madden - Stonyville area.  A cross-cutting crenulation cleavage is also commonly strongly developed in this area and foliation planes are generally characterised by a prominent down-dip mineral streaking/intersection lineation.   Farther north, in the North Palmer River, the cherts also show a well-developed foliation sub-parallel to bedding.  Stylolites are locally well developed at contacts between individual beds.  The associated fine-grained metasediments are generally strongly cleaved and in places show a well-developed cross-cutting crenulation cleavage.  The Larramore Metabasalt Member has been regionally metamorphosed to the lower greenschist facies.  Relict igneous textures are poorly preserved in the metabasalts, most of which contain abundant tremolite/actinolite and albite.  Fine metamorphic biotite is relatively common in the interlayered siliciclastic sediments.  The most extensively recrystallised and highest grade rocks occur in the structural dome southwest of Cannibal Creek tin mine.  This may indicate the presence of a granite (sensu lato) at relatively shallow depths.  Granite has been intersected in several holes drilled near the Keddy tungsten mine (abandoned) to the northeast (McConnell & Carver, 1984).  Furthermore, hornfelsed phyllitic rocks containing altered andalusite porphyroblasts are poorly exposed in the area around Buchanan's mine (McConnell & Carver, 1985).  Poorly exposed muscovite-schist containing scattered chlorite porphyroblasts was also found in the same area during the current survey.  The only other known occurrences of schist in the Hodgkinson Formation are in the metamorphic aureole surrounding the Cannibal Creek Granite.  McConnell & Carver (1985) also reported hornfelsed phyllite near Mount Madden.|16-MAY-23
22167|Larramore Metabasalt Member|Age reasons|No diagnostic fossils have been found in the member and its age is therefore uncertain.  It is thought to be most probably Devonian.|16-MAY-23
22167|Larramore Metabasalt Member|References|AMOS, B.J., & DE KEYSER, F., 1965:  Mossman, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes, SE/55-1. **DE KEYSER, F., & LUCAS, K.G., 1968:  Geology of the Hodgkinson and Laura Basins, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 84. **MCCONNELL, W.D., & CARVER, R.N., 1985:  Authority to Prospect 2181M, Cannibal Creek, north Queensland - report for six months ending 9th September, 1984.  Western Mining Corporation (unpublished - held as Company Report 13966). **ROYAL AUSTRALIAN SURVEY CORPS, 1982:  Maytown, Queensland - 1:100 000 topographic map - Series R631, Sheet 7765, Edition 1 - AAS.  Royal Australian Survey Corps, Canberra. **MCLEAN, D.S., 1982:  Cannibal Creek Authority to Prospect 2181M - half yearly report - 10th September, 1981 - 10th March, 1982.  Newmont Holdings Pty Ltd (unpublished - held as Company Report 10499).|16-MAY-23
34129|Larry Creek Complex|Name source|Larry Creek, a tributary of the Cape River.|16-MAY-23
34129|Larry Creek Complex|Unit history|This complex was mapped by Paine & others (1971) and Vine & Paine (1974) as unnamed Palaeozoic granite (Pzg).|16-MAY-23
34129|Larry Creek Complex|Type section locality|In a north draining gully at GR 3358 77265, where a pale grey porphyritic hornblende granodiorite crops out.  The grid reference is based on the AGD66 datum.|16-MAY-23
34129|Larry Creek Complex|Description at type locality|Pale grey porphyritic hornblende granodiorite in outcrop. Phenocrysts of hornblende and plagioclase up to 0.5 cm long are common and define a crude lineation. Rare mafic clots to 1cm diameter are present in the granodiorite.|16-MAY-23
34129|Larry Creek Complex|Extent|The Larry Creek Complex is 2km southeast of Pentland and crops out as a circular body of approximately 7 km2. Drilling to the south at GR 3351 77221 (Morrison, 1993) intersected hornblende-biotite granodiorite (11 holes), and drilling east of Glenhoughton homestead (McInnes & Collins, 1993) intersected similar rock types (predominantly quartz diorite), suggesting a more widespread distribution. Isolated outcrops of felsic granite/gabbro found at GR 3296 77251 and south of Elimeek at GR 3278 77255, may be similar to rocks in this complex.  The grid references are based on the AGD66 datum.|16-MAY-23
34129|Larry Creek Complex|Lithology|The unit is very poorly exposed and deeply weathered generating a coarse sandy soil mostly underlain by deeply weathered biotite granite. However, fresh outcrops at the type locality and drilling information (McInnes & Collins, 1993) indicate that grey to black, hornblende granodiorite to gabbro are also common rock types in the unit. Deeply weathered coarse grained biotite granite crops out along the road southeast of Pentland. Three small bodies of porphyritic hornblende granite south west of Pentland (adjacent to the Flinders Highway) may be part of this same suite of rocks.|16-MAY-23
34129|Larry Creek Complex|Relationships and boundaries|The Larry Creek Complex intrudes the Cape River Metamorphics and Fat Hen Creek Complex displaying sharp contacts. The unit is deeply weathered and overlain by Cainozoic sediments obscuring the relationships between the different rock types within the complex.|16-MAY-23
34129|Larry Creek Complex|Age reasons|The age of the Larry Creek Complex is uncertain. An age of Late Palaeozoic has been tentatively assigned, because of similarities to gabbro-granite complexes such as the Tuckers Igneous Complex in the Charters Towers area.|16-MAY-23
34129|Larry Creek Complex|Comments|Magnetic Susceptibility: At the type locality readings of 1531-2415 x 10[superscript]-5 SI units were obtained.|16-MAY-23
34129|Larry Creek Complex|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
10261|Lawn Hill Formation|Name source|The feature from which the name was derived is not known. Carter & others (1961) designated Lawn Hill Creek as the source.|16-MAY-23
10261|Lawn Hill Formation|Unit history|The name "Lawn Hills Greenstone" was first applied to these rocks by Ball (1931) and the name Lawn Hill Formation was formally defined by Carter & others (1961). In the Carrara Range region, the rocks now named as Lawn Hill Formation were previously mapped as the Bluff Range Beds by Smith & Roberts (1963).|16-MAY-23
10261|Lawn Hill Formation|Type section locality|Hypostratotype: Between 506064 (base) and 522055 (top) in the Lawn Hill 1:100 000 Sheet area. This section crosses the Lawn Hill-Riversleigh road at 521056, approximately 18 km by road north of Riversleigh homestead. The formation is subdivided into six subunits, two of which are formally defined as members in this paper, and four of which remain informal. The subunits are: Subunit 6: 80 m + green siltstone, shale and minor sandstone (top); Subunit 5 - Widdallion Sandstone Member: 550 m friable, reddish brown to cream lithic, feldspathic arenite; Subunit 4: 850 m tuff and siltstone with minor sandstone, shale, dolomite and acid volcanics; Subunit 3: Bulmung Sandstone Member: 40 m lithic sandstone and intraclast conglomerate; Subunit 2: 80 m thin to medium bedded green tuff, siltstone and minor sandstone and shale; Subunit 1: 220 m concretionary grey weathering shale and black carbonaceous shale.|16-MAY-23
10261|Lawn Hill Formation|Extent|The Lawn Hill Formation crops out from the Gregory River 6 km west of Riversleigh homestead to Accident Creek 20 km east of Bowthorn homestead. It extends eastward to Archie Creek and has been mapped in the Carrara-Mitchiebo area in the Northern Territory.|16-MAY-23
10261|Lawn Hill Formation|Thickness range|Approximately 1800 m of sediment are present in the hypostratotype of the Lawn Hill Formation, and a similar thickness is exposed in the Carrara Range region of the Northern Territory.|16-MAY-23
10261|Lawn Hill Formation|Lithology|The unit is characterised by the presence of a basal black shale overlain by a tuffaceous and silty sequence which is capped by the ferruginous friable sandstone of the Widdallion Sandstone Member. In the western part of the Lawn Hill Sheet area, a thin but prominent sandstone bed (Bulmung Sandstone Member) occurs in the lower part of the tuff and siltstone sequence and some siltstone and shale crop out above the Widdallion Sandstone Member.|16-MAY-23
10261|Lawn Hill Formation|Relationships and boundaries|The Lawn Hill Formation conformably overlies the Termite Range Formation in the Lawn Hill 1:100 000 Sheet area. In the Carrara and Mitchiebo 1:100 000 Sheet areas it conformably overlies the Musselbrook Formation. Throughout the outcrop area it is overlain unconformably by the Carpentarian South Nicholson Group or by the Cambrian limestones of the Georgina Basin.|16-MAY-23
10261|Lawn Hill Formation|Age reasons|Mid-Proterozoic (Carpentarian).|16-MAY-23
28675|Leichhardt Volcanics|Name source|Named after the Leichhardt River (Carter & others, 1961).|16-MAY-23
28675|Leichhardt Volcanics|Unit history|Mapped as part of the Leichhardt Metamorphics by Carter & Opik (1963).|16-MAY-23
28675|Leichhardt Volcanics|Type section locality|The type section for the Leichhardt Metamorphics is in the Prospector 1:100 000 Sheet area, Cloncurry 1:250 000 Sheet area, extending west from the Referee copper mine (GR 797531) for about 8 km to the gorge on Doughboy Creek (GR 718524): here metamorphosed felsic volcanics of the Leichhardt Metamorphics are extensively intruded by granite and dolerite dykes (Carter & others, 1961; Derrick & others, 1976). Reference Section:  Along the Dajarra/The Monument road E of Wills Creek, from GR 670840, 24 km ES of Dajarra, east for 7 km, to GR 740890, Dajarra 1:100 000 Sheet area, Duchess 1:250 000 Sheet area. In this section pink to grey felsic volcanics containing quartz and feldspar phenocrysts, the characteristic rock types of the unit, are exposed, together with a thin sandstone bed (in the W) and minor feldspar porphyry, and are seen to be intruded by leucocratic Wills Creek Granite (new name) and dolerite. The volcanics here form undulating terrain.|16-MAY-23
28675|Leichhardt Volcanics|Extent|In the Duchess 1:250 000 Sheet area the formation crops out in a series of N-trending belts up to 6 km wide extending from the northern border of the Duchess 1:100 000 Sheet area south to the southern border of the Dajarra 1:100 000 Sheet area. It also crops out extensively in sheet areas to the north where it has been mapped as Leichhardt Metamorphics (Carter & others, 1961; Derrick & others, 1976).|16-MAY-23
28675|Leichhardt Volcanics|Thickness range|Unknown, but probably more than 1000 m.|16-MAY-23
28675|Leichhardt Volcanics|Lithology|As mapped in the Duchess 1:250 000 Sheet area the Leichhardt Volcanics consist mainly of massive rhyolitic volcanics containing quartz and feldspar phenocrysts enclosed in a very fine-grained groundmass commonly showing primary igneous textures; most of the volcanics appear to be ignimbrites, but some flow-banded lavas are also present; minor rock types present locally include feldspar porphyry, volcaniclastic sandstone, bedded tuff, and altered basaltic volcanics; at only a few localities are the volcanic rocks regionally metamorphosed to form foliated and schistose rocks.|16-MAY-23
28675|Leichhardt Volcanics|Relationships and boundaries|The formation, Leichhardt Volcanics, is overlain disconformably by Magna Lynn Metabasalt and unconformably by Makbat Sandstone and Stanbroke Sandstone (new name). It overlies One Tree Granite and is intruded by Wills Creek, Birds Well and Woonigan Granite (all new names) and mafic dykes. Its relationship to adjacent Kalkadoon Granite and gneissic metavolcanics mapped as undivided Tewinga Group is uncertain.|16-MAY-23
28675|Leichhardt Volcanics|Identifying features|Definition: Revision of Leichhardt Metamorphics (Carter & others, 1961; Derrick & others, 1976) - change in lithologic designation for this formation in the Duchess 1:250 000 Sheet area.|16-MAY-23
28675|Leichhardt Volcanics|Age reasons|Early Proterozoic; samples from the Duchess 1:250 000 Sheet area have been isotopically dated at 1870-1880 m.y. by R W Page (personal communication, 1980) using the U-Pb zircon method. This age is similar to the 1865+/-3 m.y. age given by the Leichhardt Metamorphics to the north (Page, 1978).|16-MAY-23
28675|Leichhardt Volcanics|Comments|Remarks:  The Leichhardt Volcanics is equivalent to all or most of the Leichhardt Metamorphics mapped in sheet areas to the north, hence is part of the Tewinga Group of Derrick & others (1976). In the Duchess 1:250 000 Sheet area, the unit consists predominantly of readily recognisable felsic volcanic rocks, not metamorphic rocks. To designate the formation 'metamorphics' is misleading, in that almost all other stratigraphic un;its in the southern part of the Mount Isa Inlier are either equally metamorphic or more so. Also, a term such as 'metamorphics' conceals the essential volcanic nature of the unit. Clearly, the name Leichhardt Volcanics is more informative than Leichhardt Metamorphics and is an accurate lithologic description for the formation in the Duchess 1:250 000 Sheet area. Outcrop belts containing extensively recrystallised and gneissic felsic volcanics to the west in the Duchess 1:250 000 Sheet area, previously mapped as Leichhardt Metamorphics (Carter & Opik, 1963) but now mapped as undivided Tewinga Group, may include metamorphosed equivalents of the Leichhardt Volcanics.|16-MAY-23
28675|Leichhardt Volcanics|Defn Reference|82/22920|16-MAY-23
10337|Lena Quartzite Member|Name source|Lena Creek, which flows eastwards and joins the West Leichhardt River 2 km south of Mount Isa, Latitude 20o45'30"S, Longitude 139o29'E.|16-MAY-23
10337|Lena Quartzite Member|Type section locality|The type section of the Eastern Creek Volcanics east of Mount Isa (Carter et al., 1961) does not include a representative section of the Lena Quartzite member. A good type and reference section for the Quartzite is near the Counter uranium prospect, 17 km northeast of Mount Isa, Latitude 20o38'S, Longitude 139o37'E, from 6856 565171 to 6856 565175. It contains 300 m of feldspathic quartzite and orthoquartzite.|16-MAY-23
10337|Lena Quartzite Member|Extent|As for the Eastern Creek Volcanics, in a north-trending belt (centred on Mount Isa) 300 km long and up to 40 km wide, mainly in the Cloncurry and Dobbyn 1:250 000 Sheet areas.|16-MAY-23
10337|Lena Quartzite Member|Thickness range|From 170 to 1000 m; an average thickness is about 500 m.|16-MAY-23
10337|Lena Quartzite Member|Lithology|Feldspathic quartzite, orthoquartzite, minor siltstone.|16-MAY-23
10337|Lena Quartzite Member|Relationships and boundaries|The Lena Quartzite member is underlain conformably by the Cromwell Metabasalt Member and overlain conformably by the Pickwick Metabasalt Member.|16-MAY-23
10337|Lena Quartzite Member|Age reasons|Carpentarian, between about 1700 and 1650 m.y. (Plumb & Derrick, 1975).|16-MAY-23
10337|Lena Quartzite Member|Comments|Remarks: The name Lena Quartzite was used by Robinson (1968), and was given member status by Smith (1969), although no formal definition or type area were given.|16-MAY-23
10337|Lena Quartzite Member|Status|1|16-MAY-23
10392|Lighthouse Granite|Name source|Lighthouse Creek which joins Dalroy Creek (a tributary of the Etheridge River) at GR 726710 (Georgetown 1:100 000 Sheet area).|16-MAY-23
10392|Lighthouse Granite|Unit history|Previously mapped as Forsayth Granite (White, 1962c).|16-MAY-23
10392|Lighthouse Granite|Type section locality|In Lighthouse Creek at GR 721 696 about 6 km southeast of Georgetown near the track between "Roseglen" Homestead and the yards on Pinchers Creek. Here the granite consists mainly of biotite leucogranite, usually well-foliated with some muscovite leucogranite, biotite pegmatite and muscovite pegmatite; garnet is a common accessory in the pegmatites.|16-MAY-23
10392|Lighthouse Granite|Extent|A sinuous belt between 1 and 2 km wide extending north for about 13 km from GR 725664 on Lighthouse Creek. Other small bodies of leucogranite elsewhere in the Georgetown 1:100 000 Sheet area may also be Lighthouse Granite.|16-MAY-23
10392|Lighthouse Granite|Lithology|Medium even grained biotite-bearing leucogranite; locally contains biotite-rich bands and muscovite which is mostly secondary.|16-MAY-23
10392|Lighthouse Granite|Relationships and boundaries|Intrudes the Proterozoic Robertson River Metamorphics and Einasleigh Metamorphics; in the latter it predates the second folding episode. Intruded by the Proterozoic Forsayth Granite.|16-MAY-23
10392|Lighthouse Granite|Age reasons|Proterozoic; as indicated by the above cited relationships.|16-MAY-23
10392|Lighthouse Granite|References|01/31334|16-MAY-23
24358|Lily Creek Sandstone Member|Name source|Lily Creek (140o17'30"E, 22o00'S), a tributary of the Mort River, Boulia 1:250 000.|16-MAY-23
24358|Lily Creek Sandstone Member|Type section locality|Upper 12 m of type section of the Chatsworth Limestone at Lily Creek, essentially the interval 278 m - 300 m in section GEO201 between 272622 (149o17'45"E, 22o02'40"S and 269618 (140o17'30"E, 22o02'55"S). The base is defined as the incoming of sandstone beds above a thick siltstone horizon, the top is a thick cross-bedded sandstone.|16-MAY-23
24358|Lily Creek Sandstone Member|Extent|The unit is exposed in small areas over a 90 km belt, from Chatsworth in the north to Dribbling Bore in the south, on the Boulia 1:250 000 Sheet area.|16-MAY-23
24358|Lily Creek Sandstone Member|Thickness range|Range 12 m-40 m.|16-MAY-23
24358|Lily Creek Sandstone Member|Lithology|White to light red very fine calcareous sandstone, cross-bedded with foresets of an angle of 5o-15o. Interbeds of intraclastic limestone (with abundant fine sand and some skeletal fragments) and minor calcareous siltstone.|16-MAY-23
24358|Lily Creek Sandstone Member|Relationships and boundaries|The member forms the upper, relatively sandy, part of the Chatsworth Limestone. It is conformably overlain by limestones (often dolomitized) of the Unbunmaroo Member of the Ninmaroo Formation in the Black Mountain area. No clear relationships are seen in the Lily Creek area but the Ninmaroo Formation is probably unconformable on the Liky Creek Member, in the Lily Creek to Chatsworth Homestead area. The base of the member is marked by the incoming of abundant fine sand in the Chatsworth limestone and the top by the change to dolomitized peloidal and intraclastic limestone of the Unbunmaroo Member (Ninmaroo Formation).|16-MAY-23
24358|Lily Creek Sandstone Member|Age reasons|At Lily Creek the trilobite fauna is pre Payntonian (Late Cambrian) fauna B of Jones, Shergold & Druce, 1971). At Black Mountain the trilobites represent the assemblage zone of Neoagnostus quasibilobus and Tsinania nomas (see Shergold, 1975, p.235) and is Late Cambrian (Early Payntonian) and is younger than at Lily Creek.|16-MAY-23
24358|Lily Creek Sandstone Member|Proposed publication|BMR publication, BMR 1:100 000 special - the Southern Burke River Structural Belt.|16-MAY-23
24358|Lily Creek Sandstone Member|First Reference|81/21484|16-MAY-23
24358|Lily Creek Sandstone Member|Proposer|Druce E.C., Radke B.M., Shergold J.H.|16-MAY-23
10415|Lime Creek Metabasalt Member|Name source|Lime Creek Limestone quarry 17 km north-northeast of Mary Kathleen township, Latitude 20o38'S, longitude 140o01'20"E (6956 981180).|16-MAY-23
10415|Lime Creek Metabasalt Member|Geomorphic expression|The metabasalts form low rocky hills and ridges.|16-MAY-23
10415|Lime Creek Metabasalt Member|Type section locality|A section along Cameron River extending 1 km downstream from a point 1.2 km southeast of Lime Creek mine (6956 992174 to 6956 001179). In the type section the base is defined by the contact between calcareous metasediments and a basaltic flow. Pillow structures are common in zones up to 50 m thick towards the base of the member and are well exposed in pavements in Cameron River; amygdaloidal metabasalt is also common in this section. The top of the unit is marked byh the change from metabasalt to calcareous metasediments. The east-facing jof the unit has been determined from the pillow structures.|16-MAY-23
10415|Lime Creek Metabasalt Member|Extent|This member forms a continuous belt 1 km wide extending 20 km northwards from a point 4 km north of the Mary Kathleen open cut mine. It is mapped only in the Marraba 1:100 000 Sheet area, but may occur in the Quamby Sheet area to the north.|16-MAY-23
10415|Lime Creek Metabasalt Member|Thickness range|The member is about 800 m thick but thins to both the north and the south.|16-MAY-23
10415|Lime Creek Metabasalt Member|Lithology|Fine grained metabasalt, locally porphyritic and with pillow structures near the base; amphibolite and amygdaloidal metabasalt.|16-MAY-23
10415|Lime Creek Metabasalt Member|Relationships and boundaries|This member occurs just above thin quartzites of the middle Corella Formation, about 800 m from the base of the formation; it is conformably overlain by calcareous metasediments which are extensively intruded by dolerite. It is cut by calcite veinlets and thin sheets of tourmaline pegmatite related to the Burstell Granite.|16-MAY-23
24360|Littleton Dacite Member|Name source|The name is derived from 'Littleton' Holding, Parishes of Dirie, Guela and Awring, County of Langlo, covering much of the drainage areas of Rosella, Twenty :Mile, and Maitland Creeks, and Little River.|16-MAY-23
24360|Littleton Dacite Member|Unit history|The Littleton Dacite Member was previously an undifferentiated part of the Croydon Volcanics of Branch (1966); it was informally named 'Littleton dacite member' and described by Mackenzie (1983).|16-MAY-23
24360|Littleton Dacite Member|Geomorphic expression|The Littleton Dacite Member has characteristically formed relatively low, subdued to flat topography, with a slightly darker soil colour and slightly denser vegetation cover than the adjoining Carron and Idalia Rhyolites.|16-MAY-23
24360|Littleton Dacite Member|Type section locality|The type section extends from GR 7461-735027 (base), along a tributary of Little River to -720025 (top), and consists of dark green-grey, fine to coarse-grained, crystal-poor to crystal-lithic-rich dacitic ignimbrite about 150 m thick. Its base is a conformable contact with medium to dark grey, fine-grained, crystal poor rhyolitic ignimbrite (Carron Rhyolite), and the top is marked by a conformable(?) contact with massive, green-grey, medium-grained, moderately crystal-rich rhyolitic ignimbrite (Idalia Rhyolite).|16-MAY-23
24360|Littleton Dacite Member|Extent|The unit crops out in two main areas: one is a belt about 10 km long and up to 1 km wide extending northwestward from Poleycow Creek (about GR 7461-750020); the other is an irregularly shaped inlier, about 5 km2, at the head of Ross Creek, 3 km west of Dinner Camp Waterhole (Little River; GR 7461-860650). An area of outcrop too small to show at 1:100 000 or 1:250 000 scale is located near Mount Angus, 3 km northeast of Croydon.|16-MAY-23
24360|Littleton Dacite Member|Thickness range|Dacitic rocks in the Poleycow Creek area are arrpximately 150-200 m thick, but there is abundant evidence of faulting at the upper contact and within the sequence, so this may not be a true thickness. It was not possible to estimate thickness at other localities.|16-MAY-23
24360|Littleton Dacite Member|Lithology|Rocks in the Poleycow Creek area are dark greenish-grey, intensely altered (chlorite, sericite, epidote, 'leucoxene', calcite) dacitic ignimbrites, ranging from fine-grained and crystal-poor to coarse-grained (up to several cm) crystal-lithic-rich types, and a moderately crystal-rich dacitic pyroclastic rock, possibly a tuff. Outcrop in the Ross Creek area is altered, fine-grained, sparsely porphyritic, biotite hornblende dacite or microgranodiorite intrusive. The outcrop near Mount Angus is an altered, crystal-poor, dacitic ignimbrite.|16-MAY-23
24360|Littleton Dacite Member|Relationships and boundaries|The unit is a Member of the Carron Rhyolite, and occurs sporadically at the top of this formation, conformably(?) overlain by the Idalia Rhyolite. It is unconformably overlain by Late Cretaceous to Tertiary Bulimba Formation at Poleycow Creek.|16-MAY-23
24360|Littleton Dacite Member|Age reasons|Middle Proterozoic, as for the remainder of the Croydon Volcanic Group.|16-MAY-23
24360|Littleton Dacite Member|Defn author|Mackenzie D.E., Henderson G.A.M., Warnick J.V., Bain J.H.C., 1985|16-MAY-23
24360|Littleton Dacite Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24360|Littleton Dacite Member|Defn Reference|86/25125 Mention Map legend.|16-MAY-23
24360|Littleton Dacite Member|Proposer|Mackenzie D.E., Warnick J.V., Henderson G.A.M.|16-MAY-23
23733|Llandillo Granite|Name source|Parish of Llandillo, Rubyvale 1:100 000 cadastral map.|16-MAY-23
23733|Llandillo Granite|Geomorphic expression|The granite forms moderate relief. It is well exposed with numerous scattered platforms or boulder-sized outcrops.   On the Landsat 5 TM (1-4-7 BGR) image, the Llandillo Granite can be distinguished from the adjacent Annmore Quartz Monzodiorite and Kilmarnock Granodiorite by its bluish white colour. In the magnetic data, it is readily distinguished from the surrounding Kilmarnock Granodiorite as a circular magnetic low. However, it is radiometrically indistinguishable from the Kilmarnock Granodiorite, which in this area, has similar high K and Th and moderate U responses.|16-MAY-23
23733|Llandillo Granite|Type section locality|In Cattle Creek at 8451-626340, 4 km southeast of Llandillo pinnacle.  The grid reference is based on the AGD66 datum.|16-MAY-23
23733|Llandillo Granite|Description at type locality|Typical light grey, fine to medium-grained, equigranular biotite granite crops out.|16-MAY-23
23733|Llandillo Granite|Extent|A circular body, 4 km in diameter, about 4 km southeast of Llandillo pinnacle at 8451-601378.  The grid reference is based on the AGD66 datum.|16-MAY-23
23733|Llandillo Granite|Lithology|Light grey, fine to medium-grained, equigranular biotite granite containing minor hornblende locally.|16-MAY-23
23733|Llandillo Granite|Relationships and boundaries|Lies along the boundary between the Annmore Quartz Monzodiorite and the Kilmarnock Granodiorite, and probably intruded these plutons. Surrounding the Llandillo Granite are small bodies (up to 1 km2) of similar rock type that appear to intrude the Annmore Quartz Monzodiorite and Kilmarnock Granodiorite.|16-MAY-23
23733|Llandillo Granite|Age reasons|The precise age is unknown. A Devonian age has been assigned because of the similarities to other components of the Retreat Batholith, such as the Mount Observatory Granite, for which Middle Devonian ages have been determined.|16-MAY-23
25171|Llewellyn Creek Formation|Name source|Llewellyn Creek, 29 km southeast of Cloncurry, latitude 25o54'S, longitude 140o42'E (7056-680880).|16-MAY-23
25171|Llewellyn Creek Formation|Geomorphic expression|The more siliceous strata in this formation form high ranges of rounded hills, which in places are capped by mesas of lateritized Mesozoic sediments; rugged silicified ridges occur along faults and shear zones. The major drainage pattern appears to be superimposed whereas the minor tributaries are mostly subsequent.|16-MAY-23
25171|Llewellyn Creek Formation|Type section locality|The proposed type section is the western end of the section which was used by Carter et al. (1961) in defining the Soldiers Cap Formation. It is about 30 km southeast of Cloncurry and extends for 4.5 km from the core of a major anticline near Snake Creek (East Branch) at latitude 20o56'40"S, longitude 140o39'50"E (7056 651842) to a point 800 m southeast of the Mountain Home (Mount Norna) mine at latitude 20o55'20"S, longitude 140o42'10"E (7056 690862). This section contains approximately 2000 m of the formation but does not expose its base; lower stratigraphic levels of this formation are not known. The section contains from west to east, i.e. from oldest to youngest, 1000 m of arenaceous and pelitic garnet-andalusite schist; two meta-dolerite sills separated by about 200 m of garnet schist; and about 700 m of garnet-staurolite schist, pelitic and arenaceous schist, containing at least two thin intercalations of amphibolitic metabasalt.|16-MAY-23
25171|Llewellyn Creek Formation|Extent|The Llewellyn Creek Formation is exposed in a belt up to 30 km wide that extends for 100 km in a south-southeasterly direction from a point about 20 km southeast of Cloncurry. The formation has been mapped in detail in the Cloncurry 1:100 000 Sheet area (Glikson & Derrick, 1970) where it covers about 125 km2, and occupies anticlinal cores near Snake Creek, and the Williams River 13 km to the east. It continues south into the Mount Angelay 1:100 000 Sheet area and probably extends into the Selwyn 1:100 000 Sheet area.|16-MAY-23
25171|Llewellyn Creek Formation|Thickness range|The formation is at least 2000 m thick. Glikson & Derrick (1970) record a thickness of 2200 in the headwaters of Sandy Creek, i.e. near latitude 21oS, longitude 140o43'E.|16-MAY-23
25171|Llewellyn Creek Formation|Lithology|Well-bedded, graded and laminated phyllite, pelitic schist, metagreywacke, metasiltstone and minor pebbly beds. The metamorphic minerals developed include almandine, sillimanite, anthophyllite, andalusite, staurolite, biotite and muscovite (Glikson, 1972).|16-MAY-23
25171|Llewellyn Creek Formation|Relationships and boundaries|The base of the Llewellyn Creek Formation is not exposed and no older rocks are known in this part of the Cloncurry Complex. The formation is overlain conformably by the Mount Norna Quartzite and is overlain unconformably by the Corella Formation and Mesozoic sediments. The Llewellyn Creek Formation is intruded by large dolerite sills and dykes, and by the Williams Granite.|16-MAY-23
25171|Llewellyn Creek Formation|Age reasons|?Lower Proterozoic to Carpentarian.|16-MAY-23
25171|Llewellyn Creek Formation|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1977|16-MAY-23
25171|Llewellyn Creek Formation|Proposed publication|Queensland Government Mining Journal 1976|16-MAY-23
25171|Llewellyn Creek Formation|Comments|Remarks: Honman (1939) referred to these rocks as the Lower or Schist stage of the Soldiers Cap series. Glikson (1972) used an informal stratigraphic term, the Snake Creek metaturbidites, for this unit. This name is invalid because the geographic term Snake Creek was pre-empted by Snake Creek Mudstone Member - a Triassic unit validly defined by Hogetoorn (1970). The Llewellyn Creek Formation may be a time equivalent of the mainly acid volcanic Argylla Formation to the west.|16-MAY-23
25171|Llewellyn Creek Formation|Name first published by|Glikson A.Y., Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
24361|Loafers Granodiorite|Name source|Loafers Creek which joins the Gilbert River at GR 014 626 (Gilberton 1:100 000 Sheet area).|16-MAY-23
24361|Loafers Granodiorite|Unit history|Previously mapped as Dumbano Granite (White, 1962).|16-MAY-23
24361|Loafers Granodiorite|Type section locality|Outcrops at GR 100 570, near the junction of the track from cattle yards on the Gilbert River at GR 107 566 and the tracks to Glenmore homestead and Yard Soak. Outcrops ar epinkish grey to light grey, medium grained equigranular biotite-hornblende granodiorite.|16-MAY-23
24361|Loafers Granodiorite|Extent|Elongate intrusion about 10 km2 in area, cropping out south of the Bagstowe Ring Dyke Complex mainly in the headwaters of Loafers Creek, Horse Creek and their tributaries; it has an irregular embayed margin and contains some large roof pendants of Einasleigh Metamorphics.|16-MAY-23
24361|Loafers Granodiorite|Lithology|As at the type locality; locally slightly porphyritic with sparse pink K-feldspar megacrysts; a very weak foliation is locally present but generally the rocks appear to be unfoliated.|16-MAY-23
24361|Loafers Granodiorite|Relationships and boundaries|Intrudes the Proterozoic Einasleigh Metamorphics and intruded by a micro-granodiorite ring dyke which is part of the Carboniferous Bagstowe Ring Dyke Complex. In contact with the Dumbano Granite and Anning Granite but its relationship with these units is not known because of poor exposure.|16-MAY-23
24361|Loafers Granodiorite|Age reasons|Age is uncertain. It probably post-dates the second deformation in the area as it is only weakly foliated. Probably late Proterozoic or Silurian-Devonian like the Dumbano Granite, Anning Granite and Robin Hood Granodiorite, but a Carboniferous age is also possible as it shows some similarities to the Culba Granodiorite.|16-MAY-23
24361|Loafers Granodiorite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24361|Loafers Granodiorite|Proposer|Withnall I.W., Bain J.H.C.|16-MAY-23
10558|Lochness Formation|Name source|Lochness mineral lease, 90 km north-northeast of Mount Isa, latitude 19o52'S, longitude 139o38'E, Dobbyn 1:250 000 Sheet area (M.L. 6852, Cloncurry :Mining District).|16-MAY-23
10558|Lochness Formation|Type section locality|Near Paroo Creek, 13 km southwest of Julius dam, on the Prospector 1:100 000 Sheet area, from 6857-598626 to 6857 598628, (latitude 20o14'15"S, longitude 139o39'30"E to latitude 20o14'10"S, longitude 139o39"30"E. 1000 metres of ferruginous sandstone and siltstone are traversed by a Mount Isa-Julius dam survey track.|16-MAY-23
10558|Lochness Formation|Extent|The formation is more restricted in its distribution than other units in the Myally Subgroup. It forms a north-trending belt 80 km long by 15 km between Police Creek in the south and Dynamite Creek in the north, in an area 40 to 120 km north of Mount Isa.|16-MAY-23
10558|Lochness Formation|Thickness range|400 to 1200 m.|16-MAY-23
10558|Lochness Formation|Lithology|Valley-forming ferruginous feldspathic sandstone, ferruginous purple brown siltstone, calcareous sandstone, oolitic and arenaceous dolomite; ripple marking, mud cracks, load casting and sandstone dykes common. Mottled grey-pink siltstone and minor rhyolitic tuff at top of formation are known as the Police Creek Siltstone Member.|16-MAY-23
10558|Lochness Formation|Relationships and boundaries|Conformably or disconformably overlain by quartzite of Surprise Creek Beds; overlies Whitworth Quartzite conformably.|16-MAY-23
10558|Lochness Formation|Age reasons|Carpentarian: minimum age about 1650 m.y. set by Sybella Granite intrusive into time equivalent units west of Mount Isa.|16-MAY-23
10558|Lochness Formation|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
10558|Lochness Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
10558|Lochness Formation|Comments|Remarks: Ripple marks, oolites, and mudcracks in siltstone and dolomite suggest a shallow shelf and tidal flat environment. This formation was formerly an undifferentiated part of the Myally Beds (Carter et al., 1961); it is now the topmost formation in the redefined Myally Subgroup of the Haslingden Group.|16-MAY-23
10558|Lochness Formation|Name first published by|Glikson A.Y., Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
23736|Lomandra Limestone|Name source|Lomandra Creek which joins Dosey Creek at 7859-603423. The grid reference is based on the AGD66 datum.|16-MAY-23
23736|Lomandra Limestone|Unit history|The unit was previously mapped as part of the Broken River Formation (now Group) (White, 1959, 1962, 1965) (parts of 'F' and 'G' lenses of White (1965)).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
23736|Lomandra Limestone|Geomorphic expression|Generally forms low ridges of limestone outcrops and rubble, and locally low bluffs with karst features.|16-MAY-23
23736|Lomandra Limestone|Type section locality|Lomandra Creek between 7859-613407 (base) and 609409 (top).  The section is 390 m thick, and is part of section SD170 of Mawson & Talent (in press).  The grid references are based on the AGD66 datum.  REFERENCE SECTION::  Broken River between 7859-611441 (base) and 610442 (top).  The outcrop is only about 130 m wide, and is complexly folded, but is the most easily accessible exposure of the unit|16-MAY-23
23736|Lomandra Limestone|Description at type locality|).  The lower 140 m consists of thin to medium-bedded calcilutite and calcarenite with lesser calcirudite.  The calcilutites are mainly wackestone or mudstone, and the calcarenite and calcirudite are mainly wackestone and packstone.  The next 120 m is coarser and consists of medium to thick-bedded calcarenite and calcirudite (mainly packstone and wackestone) with minor calcilutite.  The uppermost 130 m is mainly calcarenite and calcirudite (packstone and wackestone and crinoidal grainstone), most of which contain sandy and muddy terrigenous material.  See Withnall & others (1988, figure 28 and pages 68-69) for more details|16-MAY-23
23736|Lomandra Limestone|Thickness range|Up to 400 m.|16-MAY-23
23736|Lomandra Limestone|Lithology|Mainly bioclastic limestone (calcarenite, calcirudite, and calcilutite) represented mainly by packstone, grainstone, and wackestone, with mudstone more dominant in the lower part of the sequence; minor calcareous siltstone, arenite, and polymictic conglomerate.|16-MAY-23
23736|Lomandra Limestone|Fossils|The unit contains crinoids, corals, stromatoporoids, and rare brachiopods, gastropods, conodonts, algae and fish fragments.  It contains the Phillipsastrea fauna, the lowermost fauna of the Chinaman Creek Limestone (Wyatt & Jell, 1967).|16-MAY-23
23736|Lomandra Limestone|Relationships and boundaries|The Lomandra Limestone is part of the Wando Vale Subgroup of the Broken River Group.  It conformably overlies the Bracteata Mudstone and is conformably overlain by the Storm Hill Sandstone.  Where the latter lenses out north of the type section, it is directly overlain by the Dosey Limestone.  North of the Broken River, it passes laterally into the Burges Formation, which consists mainly of mudstone, arenite, and polymictic conglomerate.|16-MAY-23
23736|Lomandra Limestone|Age reasons|Conodonts indicate a late Emsian to early Eifelian age (Mawson & Talent, in press).|16-MAY-23
23736|Lomandra Limestone|References|*MAWSON, R., & TALENT, J.A., in press:  Late Emsian-Givetian stratigraphy and conodont biofacies - carbonate slope and offshore shoal to sheltered lagoon and nearshore carbonate ramp - Broken River, north Queensland.  Courier Forschungs-Institute Senckenburg.WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.    *WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of 	Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes.    *WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.    *WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
22213|Long Gully Granite|Name source|The unit is named after Long Gully, a tributary of the Walsh River to the east of Chillagoe Creek (in CHILLAGOE).|16-MAY-23
22213|Long Gully Granite|Unit history|Previously mapped as Elizabeth Creek Granite by Best (1962) and de Keyser & Lucas (1968), and as Bungabilly Adamellite by Richards (1981).|16-MAY-23
22213|Long Gully Granite|Geomorphic expression|The unit forms undulating country with scattered large rounded boulders and bouldery outcrops.  It is characterised by medium to dark tones on aerial photographs.|16-MAY-23
22213|Long Gully Granite|Type section locality|The designated type area is about 150 m west-southwest of Walsh's hut, at GR 2331 81150. The grid reference is based on the AGD66 datum.|16-MAY-23
22213|Long Gully Granite|Description at type locality|The adamellite crops out as large rounded boulders in this area.|16-MAY-23
22213|Long Gully Granite|Extent|The unit crops out over an area of ~8 km2, north and south of the Walsh River.  It occurs mainly as an irregular, elongate, northwesterly-trending pluton.|16-MAY-23
22213|Long Gully Granite|General description|STRUCTURE AND METAMORPHISM:: The Long Gully Granite is essentially massive and unmetamorphosed.  Quartz grains commonly show slightly undulose extinction, indicating some post-crystallisation deformation.|16-MAY-23
22213|Long Gully Granite|Lithology|The Long Gully Granite is typically a pale grey to pale pink, medium-grained hornblende-biotite adamellite.  Scattered rounded aggregates of quartz grains up to 1 cm in diameter impart a distinctive 'porphyritic' texture to the rocks.  Locally, the adamellite contains scarce interstitial grains of pyrite.  Rounded mafic enclaves up to 30 cm in diameter are common.  In several places (e.g., at GR 2331 81150, GR 2309 81182) net-veined complexes of adamellite and diorite are exposed.  The irregular, crenulate and embayed outlines of many of the diorite inclusions (up to 2 m in diameter) and the abundant net-veining by adamellite strongly suggests that magma mixing has taken place (Blake & others, 1965). This granite has a hypidiomorphic granular texture and consists mainly of quartz, plagioclase, and K-feldspar, together with minor biotite and hornblende, and accessory and secondary minerals.  Quartz forms anhedral, interstitial grains, 1 to 5 mm across, and scattered rounded aggregates of grains.  Most grains show slightly undulose extinction and some quartz aggregates are rimmed by fine biotite flakes.  Plagioclase grains range from 1 mm to 1 cm in length.  They are mainly subhedral and many show well-developed oscillatory zoning.  K-feldspar generally forms irregular, anhedral grains (0.1 to 2 mm long), most of which crystallised relatively late.  Hornblendes are pleochroic from dark green or blue-green to pale yellow.  They show two distinct habits - euhedral to subhedral laths, 1 to 2 mm long, and small (0.1 - 0.5 mm), more irregular interstitial grains.  Biotite forms scattered subhedral to euhedral flakes, up to 4 mm in length, and much smaller interstitial grains, pleochroic from dark brown to straw-yellow.  Some of the larger flakes show fairly pronounced undulose extinction. The granite contains traces of allanite, opaque oxide, zircon, apatite, and primary sphene, mainly as small (0.2 - 0.5 mm) interstitial grains.  They are generally fairly fresh, but locally show slight alteration.  Myrmekitic intergrowths are present in marginal zones of some plagioclase grains in contact with grains of K-feldspar.  Mafic inclusions ('diorite' and 'quartz diorite'; commonly extensively altered) are common and, in places (e.g., at GR 2331 81150 and GR 2309 81182) the adamellite forms a net-veined complex with 'diorite' or 'quartz diorite'.  The grid references are based on the AGD66 datum.|16-MAY-23
22213|Long Gully Granite|Age reasons|The Long Gully Granite has not been isotopically dated, but is most probably Late Carboniferous.|16-MAY-23
22213|Long Gully Granite|Comments|The Long Gully Granite forms part of the Doolan Creek Ring Complex of Branch (1966), and the Northern Tate Batholith of Richards (1981).  Richards included the unit in his Bungabilly Adamellite, but it is more mafic and enclave rich and contains hornblende, as well as late-stage, largely interstitial K-feldspar (orthoclase?) rather than large subhedral to anhedral grains of orthoclase microperthite.Modal analyses of three samples of Long Gully Granite plot in the adamellite field on a QKP diagram (as modified by Chappell, 1978).  The one sample apparently collected from this unit by Richards (1981) also plots in the adamellite field.The widespread occurrence of relatively large, rounded, composite.|16-MAY-23
22213|Long Gully Granite|References|BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.BRANCH, C.D., 1966:  Volcanic cauldrons, ring complexes, and associated granites of the Georgetown Inlier, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 76.CHAPPELL, B.W., 1978:  Granitoids from the Moonbi district, New England Batholith, eastern Australia.  Journal of the Geological Society of Australia, 25, 267-283.DE KEYSER, F., & LUCAS, K.G., 1968:  Geology of the Hodgkinson and Laura Basins, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 84.|16-MAY-23
10823|Lowmead Formation|Name source|Lowmead township, GR 74000E 86300N Rosedale 1:100 000 Sheet area.|16-MAY-23
10823|Lowmead Formation|Unit history|The Lowmead Beds of Cribb, 1960; Mack, 1972; and Ellis and Whitaker, 1976.|16-MAY-23
10823|Lowmead Formation|Type section locality|A composite section of 591.1 m (estimated true thickness of 589.8 m), from 14 to 286.2 m in LDD7 (65665E 97292N Miriam Vale 1:100 000 Sheet area) 35.1 m to 246.5 m LDD14 (64906E 95222N Miriam Vale 1:100 000 Sheet area), 56 m to 147 m in LDD1 (67628E 93690N Miriam Vale 1:100 000 Sheet area) and 25.7 m to 47.2 m in LDD16 (69066E 94908N Miriam Vale 1:100 000 Sheet area. LDD14 is located 2.2 km SSW of LDD7. LDD1 is located 4.1 km S of LDD7. LDD16 is located 4.1 km SE of LDD7. The formation is an interbedded sequence of claystone, kerogenous claystone (oil shale, kerogen-rich carbonaceous shale and coal (carbonaceous oil shale), and minor sandstone, siltstone and sandy claystone with beds ranging from 0.05 m to 32 m thick. The formation unconformably overlies igneous rock and is unconformably overlain by unconsolidated Quaternary sediment. The Lowmead Formation has been sub-divided into six conformable members. In order of decreasing age they are the Hobble Creek, Harpur Creek, Wheatley Oil Shale, Korenan Oil Shale, Makowata Oil Shale, and Sonoma Members. Correlation between drill holes is on the basis of lithology, confirmed (where available) by comparison of assay histograms of oil yield from oil shale beds. Between drill holes LDD7 and LDD14 the correlation is based on the boundaries of the Makowata Oil Shale Member, the top of which occurs at 286.2 m in LDD7 and 35.1 m in LDD14. Between drill holes LDD4 and LDD1 the top of the Wheatley Oil Shale Member has been used, which occurs at 213.6 m in LDD14 and 25.8 m in LDD1. Correlation of LDD16 to LD1 is made using the top of the Hobble Creek Member which occurs at 147 m in LDD1 and 25.7 m in LDD16.|16-MAY-23
10823|Lowmead Formation|Extent|Subcrops in an area of about 65 km2 between Lowmead township and Coongoola homestead within the Lowmead Graben. Outcrop is present, but weathering renders it unsuitable for stratigraphic correlation. Two relatively fresh exposures of oil shale are found in road quarries at grid references 66550E 94150N and 64000E 94600N Miriam Vale 1:100 000 Sheet area. The formation has been identified from drill core.|16-MAY-23
10823|Lowmead Formation|Thickness range|596.1 m in the type section (estimated true thickness 589.8 m corrected for dip of strata in drill holes). This is the maximum known thickness of the formation.|16-MAY-23
10823|Lowmead Formation|Lithology|Claystone is dusky yellow-green to olive-grey, ranging from very thick to lamina beds and is soft (puggy) to hard. It is calcareous in part. Oil shale is dark to dusky yellow-brown, hard, well laminated and calcareous in part. Carbonaceous oil shale is brownish-block, well laminataed (shaly) and hard. Sandstone beds are fine to coarse grained, massive, with sand grains poorly sorted, subangular and of low sphericity. There are interbeds of sandy claystone to clayey sandstone. Red sandy claystone (clayey sandstone and sandstone in part) occur at the base of the formation (Hobble Creek Member).|16-MAY-23
10823|Lowmead Formation|Relationships and boundaries|The Lowmead Formation unconformably overlies Palaeozoic and Mesozoic igneous rocks of the Miriam Vale Granodiorite and the Agnes Waters Volcanics (Ellis and Whitaker, 1976). The top of the formation is eroded. It is in part unconformably overlain by Quaternary overburden. The formation is faulted against igneous rocks of the Miriam Vale Granodiorite and the Agnes Waters Volcanics and is contained within the Lowmead Graben.|16-MAY-23
10823|Lowmead Formation|Age reasons|An Early Tertiary age is indicated using microfloral and macrofloral and faunal evidence (Ball, 1916; Beasley, 1945). Correlation with other Tertiary oil shale deposits in central Queensland (Rundle & Stuart - Hendstridge and Missen 1982, and Yaamba) and with the Redbank Plains Formation (Cranfield et al, 1976) would restrict the Lowmead Formation to the middle to Late Eocene.|16-MAY-23
10823|Lowmead Formation|Comments|Note: Drill core of LDD1, LDD7, LDD14 and LDD16, is stored at Southern Pacific Petroleum's Research and Core Storage facility in Gladstone, Queensland.|16-MAY-23
23743|Lugano Metamorphics|Lithology|Biotite gneiss, mica schist, quartzite, leucogneiss, laminated amphibolite and minor marble; quartzite (locally contains kyanite); amphibolite - local relict pillow lavas; biotite gneiss and schist grading to nebulitic and agmatitic migmatite, foliated biotite granite containing abundant xenoliths and schlieren, local tourmaline-muscovite pegmatite veins|16-MAY-23
25185|Lunch Creek Gabbro|Name source|Lunch Creek, which flows east just to the south of the main mass of the unit, 9 km east of Mary Kathleen, latitude 20o47'24"S, longitude 140o3'45"E (6956 025007).|16-MAY-23
25185|Lunch Creek Gabbro|Geomorphic expression|Well-grassed, high bouldery hills cut by creeks which expose many fresh rock pavements.|16-MAY-23
25185|Lunch Creek Gabbro|Type section locality|Along an unnamed east flowing stream from 3 to 5 km west-northwest of Timberu Homestead, I.e. latitude 20o45'15"S, longitude 140o4'30"E (6956 037046) to latitude 20o45'10"S, longitude 140o3'10"E (6956 014048). Extensive rock pavements provide excellent exposure of the various gabbros, diorites and pegmatite.|16-MAY-23
25185|Lunch Creek Gabbro|Extent|The main mass of Lunch Creek Gabbro is a 2 km wide belt that extends northward from just north of Lunch Creek 9 km east of Mary Kathleen. A smaller mass of the Gabbro has been mapped 7 to 9 km further to the east, east of the Corella River and north of the Barkly Highway.|16-MAY-23
25185|Lunch Creek Gabbro|Thickness range|The Gabbro is about 500 m thick.|16-MAY-23
25185|Lunch Creek Gabbro|Lithology|Mostly olivine-pyroxene gabbro, with biotite diorite, biotite gabbro, hybrid diorite, tonalite, and minor hornblende-feldspar pegmatite. Some small-scale layering from a mafic-rich base to a felsic-rich top occurs locally in the gabbros. The unit is described by Derrick et al. (1971).|16-MAY-23
25185|Lunch Creek Gabbro|Relationships and boundaries|The Lunch Creek Gabbro intrudes the Corella Formation and is intruded by the Burstall Granite and related acid porphyry dykes, fine-grained basic dykes, and dykes of the Lakeview Dolerite.|16-MAY-23
25185|Lunch Creek Gabbro|Age reasons|Page (1975, pers. comm.) considers that a rubidium/strontium age of 1466+/-78 m.y. is a reliable minimum estimate for the time of emplacement of the Lunch Creek Gabbro.|16-MAY-23
25185|Lunch Creek Gabbro|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1978|16-MAY-23
25185|Lunch Creek Gabbro|Proposed publication|Queensland Government Mining Journal, 79 (1978).|16-MAY-23
25185|Lunch Creek Gabbro|Defn approved by|Queensland Sub-Committee|16-MAY-23
25185|Lunch Creek Gabbro|Name first published by|Duff B.A., Embleton B.J.J., 1976|16-MAY-23
27293|Lyall Formation|Name source|Parish of Lyall, County of Clarke.|16-MAY-23
27293|Lyall Formation|Unit history|Previously part of the Clarke River Formation (now Group) (White, 1959).|16-MAY-23
27293|Lyall Formation|Geomorphic expression|The Lyall Formation generally forms moderately hilly country. An irregular pattern of ridges is typical of the coarse sandstone and conglomerate, whereas low, continuous ridges outlining bedding trends are more characteristic of areas where finer sedimentary rocks are interbedded with the coarser rock types. Except for the Meath Rhyolite Member, vegetation on the Lyall Formation is generally less dense than on the Venetia Formation.|16-MAY-23
27293|Lyall Formation|Type section locality|A composite type section comprising three separate sections is proposed for the Lyall Formation. The lower section is approximately 400 m thick and extends from GR961517 (top of the Venetia Formation which is recognised by its lack of volcanic detritus) to GR 949515 (base of the Meath Rhyolite Member); this includes the type section (holostratotype) of the Furry Hoop Member (approximately 320 m thick) between GR 960516 (base) and 951515 (top, see separate definition). The second section is the type section of the Meath Rhyolite Member (approximately 75 m thick) which crops out along the Clarke River from GR 948504 (base) to 946404 (top). The third section (approximately 290 m thick) is through the volcanolithic rocks overlying the Meath Rhyolite Member, along a tributary of Keppel Creek South between GR 944568 (top) of Meath Rhyolite Member and 930550 (synclinal hinge).|16-MAY-23
27293|Lyall Formation|Extent|The Lyall Formation crops out in the central and western parts of the Clarke River Basin, about 40 km southeast of Greenvale, adjacent to and west of the range of hills which form the Venetia Formation. It is obscured by Tertiary laterite to the north, and by Cainozoic basalt to the southeast. An outlier also occurs about 10 km east of Niall homestead.|16-MAY-23
27293|Lyall Formation|Thickness range|Probably up to 850 m, although structural complexities prevent an accurate estimate of the thickness in many places. The original thickness is unknown because of erosion of the top of the formation.|16-MAY-23
27293|Lyall Formation|Lithology|The Lyall Formation can be informably divided into lower and upper subunits, separated by the ignimbrite of the Meath Rhyolite Member. The lower subunit consists largely of volcanolithic sandstone (sporadically pebbly) pebble to boulder conglomerate, red-green siltstone to fine-grained sandstone and tuff. The rocks of the lower subunit are typically calcareous with a large volcanic component. The upper subunit has a basal sequence of calcareous siltstone, tuffaceous sandstone and sporadic dirty limestone overlain by coarse green volcanolithic sandstone and boulder to cobble conglomerate.|16-MAY-23
27293|Lyall Formation|Relationships and boundaries|The Lyall Formation conformably (with possible local angular unconformity) overlies the Venetia Formation, from which it is distinguished by its large acid volcanic component. The contact could be a disconformity. The Furry Hoop Member occurs in the lower part of the formation. A resistant, ridge-forming ignimbrite, the Meath Rhyolite Member, marks the middle of the formation separating the informal upper and lower subunits. The Lyall Formation is intruded to about the level of the Meath Rhyolite Member by quartz porphyry bosses and stocks. It is also intruded by the Oweenee Granite in the outlier to the southwest (on Spring Park Station). To the north the Lyall Formation is overlain by Tertiary laterite, and to the south by Cainozoic basalt.|16-MAY-23
27293|Lyall Formation|Age reasons|The Lyall Formation is late Visean to Late Carboniferous, possibly extending into the Early Permian (a hiatus is likely within the sequence) (Jell & Playford, in press).|16-MAY-23
27293|Lyall Formation|Defn author|Coote S.M., 1986|16-MAY-23
27293|Lyall Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
27293|Lyall Formation|Defn Reference|86/25587 Mention Table 4A.|16-MAY-23
27293|Lyall Formation|Proposer|Scott M|16-MAY-23
10907|Ma Ma Creek Member|Name source|The name is derived from Ma Ma Creek in the Laidley Valley, southeast Queensland.|16-MAY-23
10907|Ma Ma Creek Member|Unit history|The name of the unit was first proposed by McTaggart (1963) and published as Ma Ma Creek 'Sandstone' Member.|16-MAY-23
10907|Ma Ma Creek Member|Geomorphic expression|Not characteristic; mostly weathers recessively, and generally obscured by alluvium.|16-MAY-23
10907|Ma Ma Creek Member|Type section locality|Reference Section: McTaggart (1963) did not nominate a type section and Gray (1975) designated the interval 1030'3" (314.02 m) to 1368'4" (417.07 m) in GSQ Ipswich 18 as a reference section. Type Section: The type section for the Ma Ma Creek Member is nominated as the interval 971.1 m - 1073.52 m in GSQ Ipswich 24.|16-MAY-23
10907|Ma Ma Creek Member|Description at type locality|The graphic log of GSQ Ipswich 24 (Fig. 10) shows the lithological sequence in the member. The depositional environment is considered to be lacustrine. The member is characterised by the presence of a chamositic oolite in the siltstone.|16-MAY-23
10907|Ma Ma Creek Member|Extent|The member is recognised chiefly in the Laidley Valley area. Identification of the member elsewhere is difficult although it is possibly present in parts of the southern Clarence-Moreton Basin. It is not present at many localities, and in many well sections. Identified outcrops of the Ma Ma Creek Member are confined to the northern part of the basin and the finer grained shale and siltstone are poorly exposed and difficult to identify. Poor outcrops doubtfully referred to as the Ma Ma Creek Member are found as far south as sections on the western flank of the basin where they are cut by the Bruxner and Gwydir Highways.|16-MAY-23
10907|Ma Ma Creek Member|Depositional environment|The most characteristic rock type is a fine grained, grey shale/siltstone sequence which in drill core commonly contains 2-10 cm beds of chamositic oolite. The depositional environment is considered to be lacustrine.|16-MAY-23
10907|Ma Ma Creek Member|Fossils|Plant and wood fossils and spores, pollen grains and sporadic acritarchs.|16-MAY-23
10907|Ma Ma Creek Member|Relationships and boundaries|The base is generally taken as a sharp boundary between dark grey siltstone and shale of the Ma Ma Creek Member with quartzose, lithic and feldspathic, cross-bedded sandstone, fine to coarse and very coarse grained sandstone of the underlying Gatton Sandstone. The upper boundary is less well defined because many sections of the Ma Ma Creek Member, such as those present in GSQ Ipswich 18 and 24, show a high proportion of sandstone in the upper part of the member. The upper boundary is therefore taken as the first appearance of coarse to very coarse grained sandstone, the base of which is commonly marked by a thin granule and pebble conglomerate. This boundary is interpreted as the base of the first stacked multistorey, fining up, channel sand. The underlying, upper part of the Ma Ma Creek Member is commonly cross-laminated to ripple cross laminated, uniform, fine and medium grained sandstone with interbedded mudstone intervals. This sandstone commonly forms 2-5 m cliff faces in the creeks around the Lockyer Valley.|16-MAY-23
10907|Ma Ma Creek Member|Identifying features|See NSW for card|16-MAY-23
10907|Ma Ma Creek Member|Age reasons|The member is late Early Jurassic in age and contains the upper limit of palynological assemblage D (de Jersey, 1971, 1976; McKellar, 1981b) which lies in the interval 1035.29 m to 1034.19 m, of GSQ Ipswich 18. It is also associated with the succeeding interval J2 (Toarcian) in JM Urbenville 1. The palynofloras are equivalent to those recovered from beds adjacent to the oolitic ironstone sequence in the upper Evergreen Formation, and the basal Hutton Sandstone of the Surat Basin. The age is Toarcian according to McKellar (1974 and 1981).|16-MAY-23
10907|Ma Ma Creek Member|Correlations|The Ma Ma Creek Member is broadly correlated with the Evergreen Formation in the Surat Basin sequence.|16-MAY-23
10907|Ma Ma Creek Member|Resdate|01-MAR-1988|16-MAY-23
23746|Macauley Creek Granite|Name source|From Macauley Creek.|16-MAY-23
23746|Macauley Creek Granite|Unit history|This granite was previously mapped as Oweenee Granite by Wyatt & others (1970).|16-MAY-23
23746|Macauley Creek Granite|Geomorphic expression|The granite forms relatively subdued sandy downs with sparse outcrop in the south and this contrasts with the more rugged, hilly topography of the Spinifex Creek Granite. However, to the north of Macauley Creek from which the unit takes its name, the granite also forms hilly topography with local relief up to 100 m, and is more difficult to distinguish from the Spinifex Creek Granite on aerial photographs.  The boundary has been located by using subtle differences in composite radiometric images processed from the AGSO airborne data, followed up by ground traversing using a hand-held spectrometer.|16-MAY-23
23746|Macauley Creek Granite|Type section locality|The type locality is a small tor of pink, coarse-grained, equigranular biotite granite at 8059-865694 on the western side of the Ewan-Laroona road, just south of the Lassies Creek crossing.   The grid reference is based on the AGD66 datum.|16-MAY-23
23746|Macauley Creek Granite|Extent|The Macauley Creek Granite crops out immediately to the east of the Sybil Graben and forms an elongate west-northwest trending body up to 9km wide extending about 30km from the Star River to the Burdekin River. To the northeast it is bounded by the Spinifex Creek Granite and to the northwest and south by the Running River Metamorphics and Argentine Metamorphics respectively.|16-MAY-23
23746|Macauley Creek Granite|Lithology|The Macauley Creek Granite is relatively uniform in appearance and consists generally of pink to white or cream, medium to coarse-grained, equigranular to seriate, biotite granite.|16-MAY-23
23746|Macauley Creek Granite|Relationships and boundaries|The Macauley Creek Granite intrudes the Proterozoic(?) Running River and Argentine Metamorphics and a small screen of Early Carboniferous Ewan Formation. It is inferred to be intruded by the Spinifex Creek Granite because of the shape of the contact. It is also intruded by swarms of rhyolite and granophyric microgranite dykes and minor porphyritic dolerite dykes, particularly to the north of Spring Creek. It is faulted against and thought to be older than the Late Carboniferous Sybil Group. A sample of Macauley Creek Granite was included in the Rb-Sr isochron for the 'Oweenee Granite' which produced an age of 342±7 Ma* (Wyatt & others, 1970). This may be a mixed isochron, but an Early Carboniferous age for the `Oweenee Granite' has been verified by the 330±4 Ma (Early Carboniferous) crystallisation age for the Kallanda Granite (Appendix 1). Samples from the Kallanda Granite were also included in the Rb-Sr isochron for the 'Oweenee Granite'.|16-MAY-23
23746|Macauley Creek Granite|Age reasons|See Relationship details (above) for age analysis.|16-MAY-23
23746|Macauley Creek Granite|Comments|The Macauley Creek Granite generally shows lower values in the Total Count, K, U and Th channels than the Spinifex Creek Granite, and is a slightly deeper pink on the composite images. East of Mount Julia, a screen of Ewan Formation partly separates the units. More resistant rhyolite and microgranite dykes are more common here and may have 'buttressed' the granite.|16-MAY-23
23746|Macauley Creek Granite|References|WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127.|16-MAY-23
27185|Magna Lynn Metabasalt|Name source|The Magna Lynn copper mine, 28 km north-northwest of Mary Kathleen, latitude 22o33'S, longitude 139o52'E (6856 812275).|16-MAY-23
27185|Magna Lynn Metabasalt|Geomorphic expression|The Magna Lynn Metabasalt generally forms a broad undulating valley between two units of predominantly acid vaolcanics, and is especially useful in the identification of different acid volcanic formations in fault zones. The unit has previously been mapped as "db" on the Cloncurry and Duchess 4-mile Geological Sheets and described as "altered dolerite dykes and basalt" and "metadolerite and metabasalt" in the respective map references. In Carter et al. (1961, p.133), "db" is described as "intrusive metadolerite (mainly anastomosing dykes) in the Leichhardt Metamorphics and Argylla Formation. Outcrops are large, branched, and elongated north-south". The anastomosing pattern results from fault repetition within the Tewinga Group, and intrsion of the basalt by sills of porphyritic rhyolite comagmatic with Argylla Formation lavas. The unit is described in detail in Derrick et al. (1974), and Wilson et al. (in prep). A general description can be found in Plumb & Derrick (1975).|16-MAY-23
27185|Magna Lynn Metabasalt|Type section locality|Along the north bank of an unnamed creek, 10 km south-southwest of the Referee copper mine, 3.2 km north of the Lillimay copper mine, latitude 20o24'25"S, longitude 139o50"E. The base of the section is 0.4 km east-southeast of a water hole which is accessible by a track from the old Mount Isa-Kajabbi road. The top of the section is at the foot of a high northwest-trending ridge 1.5 km east-southeast of the water hole. At the type locality the basal unit of the Magna Lynn Metabasalt rests conformably on a ridge of creamy grey fine-grained rhyolite of the Leichhardt Metamorphics. Dips are from 40o to 60o to the northeast. All rocks in the formation show evidence of upper greenschist facies metamorphism. The basal 200 m of the Magna Lynn Metabasalt section consists of several flows of fine-grained altered basalt with amygdaloidal and brecciated flow tops, and some minor intercalations of greenish brown thin-bedded fine-grained epidotized quartzite. A dyke of porphyritic rhyolite trends north-northeast through this part of the section, where there is also a similarly oriented fault with a sinistral displacement of about 50 m. Towards the middle of the section a sequence of up to 150 m of metamorphosed thin-bedded ferruginous calcareous sandstone, lamintead siltstone and basic tuff is intercalated with basaltic flows and fine-grained epidote-rich sandstone and siltstone containing basaltic blocks. This sequence is overlain by about 200 m of predominantly basaltic rocks in which at least 10 flows with amygdaloidal tops can be recognised; minor basalt/sediment mixes, basic tuff, and thin lenticular grey to brown fine-grained quartzite are intercalated with these flows. Near the top of the type section two fairly continuous quartzite units up to 20 m thick are separated by about 50 m of amygdaloidal basalt and minor grey porphyritic andesite. A thin amygdaloidal basalt overlies the upper quartzite and is conformably overlain by grey porphyritic dacite that marks the base of the Argylla Formation. The total thickness in the type section is about 520 m.|16-MAY-23
27185|Magna Lynn Metabasalt|Extent|The Magna Lynn Metabasalt is exposed to the east of longitude 139o45'E in a north-trending belt, 5 km wide and 120 km long, which extends from about 12 km northwest of Duchess northwards to Kajabbi. It also occurs in a fault block between 10 and 25 km northwest of Mary Kathleen. The formation has been mapped in the Mary Kathleen and Prospector 1:100 000 Sheet areas and is known to occur in the Alsace and Duchess 1:100 000 Sheet areas. Future mapping may show that this formation extends to the north of Kajabbi and to the west and southwest of Duchess.|16-MAY-23
27185|Magna Lynn Metabasalt|Thickness range|Thickness ranges from 200 to 700 m. Metasedimentary intercalations are mostly 5 to 25 m thick but are up to 360 m thick near the East Leichhardt Dam.|16-MAY-23
27185|Magna Lynn Metabasalt|Lithology|Massive metabasalt; amygdaloidal metabasalt with amygdales of quartz, calcite, chlorite and/or epidote; flow-top breccia; metabasalt/metasediment mixes; calcareous, epidote-rich and feldspathic quartzites; agglomerate; and basic tuff. Biotite, chlorite and actinolite schists occur in shear zones, together with secondary vein calcite and siderite.|16-MAY-23
27185|Magna Lynn Metabasalt|Relationships and boundaries|The Magna Lynn Metabasalt appears to conformably overlie the Leichhardt Metamorphics and it is conformably overlain by the Argylla Formation. The lower contact is abrupt: pale rhyolite of the Leichhardt Metamorphics is overlain by dark metabasalt. The upper contact is gradational, metabasalt flows and grey porphyritic lavas being intercalated in the upper 50 m. The top of the Magna Lynn Metabasalt is placed at the top of the highest metabasalt lava. The unit is intruded by porphyritic acid dykes (possibly comagmatic with lavas of Argylla Formation), dolerite dykes of at least two ages, and granite (50 km north and 30 km southwest of MaryKathleen; the former is Wonga Granite, the latter is shown as Kalkadoon Granite on the Duchess 4-mile Geological Sheet but is probably also Wonga Granite). Relations with Kalkadoon Granite are not clear but current work west of Duchess suggests Kalkadoon Granite predates the Magna Lynn Metabasalt.|16-MAY-23
27185|Magna Lynn Metabasalt|Age reasons|Precambrian, probably Carpentarian (Middle Proterozoic). The Sybella Granite, dated in part as 1656 m.y. old, intrudes rocks younger than the Magna Lynn Metabasalt and provides a minimum age for the formation (see Plumb & Derrick, 1975).|16-MAY-23
27185|Magna Lynn Metabasalt|Defn author|Krosch N.J., Sawers J.D., 1974|16-MAY-23
27185|Magna Lynn Metabasalt|Proposed publication|Queensland Government Mining Journal|16-MAY-23
23748|Magpie Creek Limestone Member|Name source|Magpie Creek, a tributary of Gray Creek, which it joins at 7859 779725.  The grid reference is based on the AGD66 datum.|16-MAY-23
23748|Magpie Creek Limestone Member|Unit history|The unit was previously mapped as an unnamed member of the Graveyard Creek Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
23748|Magpie Creek Limestone Member|Geomorphic expression|The limestone generally forms a low-ridge, but a prominent bluff with typical karst features occurs at the western end where the unit is thickest.  The larger limestone outcrops and bluffs are clearly discernible on the aerial photographs.|16-MAY-23
23748|Magpie Creek Limestone Member|Type section locality|About 300 m of limestone as described below, and minor mudstone is exposed between 7859 723657 (base) and 726655 (top), in a tributary of Turtle Creek, where it cuts through a limestone bluff.  The grid reference is based on the AGD66 datum.|16-MAY-23
23748|Magpie Creek Limestone Member|Extent|A large limestone lens about 5 km long, in the headwaters of Magpie and Turtle Creeks.|16-MAY-23
23748|Magpie Creek Limestone Member|Thickness range|300-500 m.|16-MAY-23
23748|Magpie Creek Limestone Member|Lithology|Massive, commonly unbedded calcilutite and fine pelloidal calcarenite (packstone and wackestone), and mudstone,  locally brecciated. Generally unbedded and massive.|16-MAY-23
23748|Magpie Creek Limestone Member|Fossils|The limestone contains a rich coral fauna not yet studied in detail, but which is probably of Late Silurian (Ludlow and possibly Pridoli) age (J.S. Jell, personal communication).|16-MAY-23
23748|Magpie Creek Limestone Member|Relationships and boundaries|A member towards the top of the Quinton Formation.|16-MAY-23
23748|Magpie Creek Limestone Member|Age reasons|Probably of Late Silurian (Ludlow and possibly Pridoli) age (J.S. Jell, personal communication) - based on fossils (see above).|16-MAY-23
23748|Magpie Creek Limestone Member|References|WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4. Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. ***WHITE, D.A., 1962:  Clarke River 1.250 000 Geological series.  Bureau of Mineral Resources, Australia, Explanatory Notes, E/55-13. ***WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. ***WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
24369|Mairindi Creek Granite|Name source|Named after Mairindi Creek, which drains the country adjacent to the SE margin of the granite, 7 km NW of Duchess, Duchess 1:100 000 Sheet area (Duchess 1:250 000 Sheet area).|16-MAY-23
24369|Mairindi Creek Granite|Unit history|Previously ;mapped as Kalkadoon Granite (Carter & Opik, 1963). However, the Kalkadoon Granite is now known to be significantly older than the Argylla Formation (Page, 1978).|16-MAY-23
24369|Mairindi Creek Granite|Type section locality|0.5 km to 4.5 km E of main Duchess-Mount Isa road, from GR 725390 to GR 753400. Here the unit consists mainly of foliated, medium to coarse-grained, patchily and sparsely porphyritic biotite granite, cut by aplite and quartz veins and numerous metadolerite dykes.|16-MAY-23
24369|Mairindi Creek Granite|Extent|The granite crops out over about 20 sq km, 9 km northwest of Duchess.|16-MAY-23
24369|Mairindi Creek Granite|Lithology|Medium to coarse-grained, foliated, biotite granite containing scattered phenocrysts of pink microcline, quartz and rare plagioclase, and traces of muscovite, hornblende, opaque oxide, allanite and fluorite; minor aplite (as veins). The granite is cut by thin quartz veins. The well-developed, steeply dipping to vertical, NW-trending foliation is defined mainly by the parallel alignment of biotite flakes and aggregates, and is crenulated in places.|16-MAY-23
24369|Mairindi Creek Granite|Relationships and boundaries|The granite intrudes Magna Lynn Metabasalt and Argylla Formation, and is cut by numerous mainly NW-trending metadolerite dykes.|16-MAY-23
24369|Mairindi Creek Granite|Age reasons|Proterozoic|16-MAY-23
24369|Mairindi Creek Granite|Proposed publication|Blake & others, in preparation.|16-MAY-23
24369|Mairindi Creek Granite|Comments|Remarks: The Mairindi Creek Granite forms a small discrete pluton. The presence of fluorite in the granite may indicate a correlation with the Burstall and Sybella Granites.|16-MAY-23
24369|Mairindi Creek Granite|Defn Reference|82/22920|16-MAY-23
24369|Mairindi Creek Granite|First Reference|82/22710  82/22663|16-MAY-23
24369|Mairindi Creek Granite|Proposer|Bultitude R.J.|16-MAY-23
24370|Makowata Oil Shale Member|Name source|Makowata railway siding, GR 63300E 96750N Miriam Vale 1:100 000 Sheet area.|16-MAY-23
24370|Makowata Oil Shale Member|Unit history|Part of the Lowmead Beds of Cribb, 1960; Mack, 1972; and Ellis and Whitaker, 1976.|16-MAY-23
24370|Makowata Oil Shale Member|Type section locality|43.3 m (estimated true thickness 42.6 m) from 35.1 m to 78.4 m in LDD14 (GR 64906E 95222N Miriam Vale 1:100 000 Sheet area). The interval is within the type section of the Lowmead Formation. Carbonaceous oil shale is the dominant rock type. There is minor interbedded claystone. Upper and lower boundaries of the member are identified by the contact of carbonaceous oil shale with oil shale of the Sonoma Member and Korenan Oil Shale Member, respectively.|16-MAY-23
24370|Makowata Oil Shale Member|Extent|Subcrops in an area of about 3 km2 east of Makowata railway siding. Sparse highly weathered outcrop is known. The member has been identified from drill core.|16-MAY-23
24370|Makowata Oil Shale Member|Thickness range|43.3 m in the type section; true thickness 42.6 m corrected for a 10o dip of the strata in LDD14. The member ranges from 18.4 m to 73.5 m thick.|16-MAY-23
24370|Makowata Oil Shale Member|Lithology|Carbonaceous oil shale is brownish-black and hard. It is composed of alternating clay, kerogenous and carbonaceous to coaly thin laminae in beds up to 28.5 m thick. Fragments of plant leaves and stems are abundant. The carbonaceous oil shale beds are separated by massive olive-grey claystone beds from 0.70 m to 3.25 m thick.|16-MAY-23
24370|Makowata Oil Shale Member|Relationships and boundaries|The Makowata Oil Shale Member is conformably overlain by the Sonoma Member and conformably overlies the Korenan Oil Shale Member of the Lowmead Formation. It is faulted against igneous rocks of the Miriam Vale Granodiorite and the Agnes Waters Volcanics (Ellis and Whitaker, 1976) along the boundaries of the Lowmead Graben.|16-MAY-23
24370|Makowata Oil Shale Member|Age reasons|Early Tertiary - as for the Lowmead Formation.|16-MAY-23
24370|Makowata Oil Shale Member|Defn author|McConnochie M.J., Henstridge D.A., 1985  Br descr. P211 as M. oil shale.|16-MAY-23
24370|Makowata Oil Shale Member|Comments|Note: Drill core of LDD14 is stored at Southern Pacific Petroleum's Research and Core Storage facility in Gladstone, Qld.|16-MAY-23
24370|Makowata Oil Shale Member|Defn Reference|86/25154 Mention p212 & Fig. 4. Mention Table 1 as Makowata Member.|16-MAY-23
24370|Makowata Oil Shale Member|Resdate|04-OCT-1982|16-MAY-23
24371|Malacura Sandstone|Name source|"Malacura" pastoral holding, Langdon River area, centred on about 143o00'E, 18o30'S; in Parish of Malacura, County of Lang.|16-MAY-23
24371|Malacura Sandstone|Unit history|Previously mapped as part of the 'Etheridge Formation' or of the Langdon River Formation of White (1959; 1962, 1965). The 'Etheridge Formation', now redefined as a Group containing Robertson River, Townley, Heliman, Candlow, Langdon River (and other) Formations, unconformably underlies the Malacura Sandstone.|16-MAY-23
24371|Malacura Sandstone|Geomorphic expression|Generally very subdued topography except where hornfelsed; prominent trend lines, and pale brown to red-brown tones on airphotographs; medium cover of low scrub.|16-MAY-23
24371|Malacura Sandstone|Type section locality|Unnamed tributary of the upper Langdon River on the eastern bank of which is located Red Bull Bore, between 7460-09352285 and 7460-08402185, and thence along a small tributary of that stream to 7460-07682140.|16-MAY-23
24371|Malacura Sandstone|Description at type locality|The rocks exposed consist of about 1300 m of medium to fine-grained feldspar-bearing, commonly micaceous sublithic sandstone or grit.|16-MAY-23
24371|Malacura Sandstone|Extent|Exposed along most of the valley of the Langdon River, from GR 7460-070140 north to the Gilbert River, along the eastern edge of Esmeralda and Gilbert River 1:100 000 Sheets (7460 and 7461), in the northwestern corner of North Head (7560), and along the western edge of Forest Home (7561) to GR 7561-135800, where small outliers crop out on the northern side of Gilbert River near Forest Home homestead.|16-MAY-23
24371|Malacura Sandstone|Thickness range|About 1300 to 1450 m in the south; probably thicker in the north, but top and base obscured.|16-MAY-23
24371|Malacura Sandstone|Lithology|Generally as in type section; sandstones more dominant in the north.|16-MAY-23
24371|Malacura Sandstone|Relationships and boundaries|Unconformably overlies Langdon River Siltstone (phyllitic siltstone) and Candlow Formation (phyllitic siltstone and sandstone). Angular relationship can be seen in places in the south, but clearer on airphotographs than on the ground. Clasts of underlying units and of granitic rocks recognisable in some sandstones. Conformable boundary with overlying 'Yarman Formation', which consists predominantly of shale and siltstone that are maroon or red-brown in outcrop. Unconformably overlain by or faulted against Croydon Volcanics and/or unconformably overlain by Mesozoic sandstones; intruded by Esmeralda Granite.|16-MAY-23
24371|Malacura Sandstone|Age reasons|Early upper Proterozoic. Underlying rocks have been affected by deformation and metamorphism, dated at 1570+/-30 m.y. (Black et al., in press), which do not affect the Malacura Sandstone. Both the Malacura Sandstone and the overlying 'Yarman Formation' are unconformably overlain by Croydon Volcanics, dated at 1429+/-75 m.y. (Oversby et al., 1976).|16-MAY-23
24371|Malacura Sandstone|Proposed publication|Queensland Govrnment Mining Journal|16-MAY-23
24371|Malacura Sandstone|Proposer|Mackenzie D.E.|16-MAY-23
27187|Malbon Group|Name source|Township of Malbon, latitude 21o4'30"S, longitude 140o18'E.|16-MAY-23
27187|Malbon Group|Constituents|The Malbon Group consists of the Marraba Volcanics and the Mitakoodi Quartzite.|16-MAY-23
27187|Malbon Group|Geomorphic expression|The metabasalt and labile sediments form valleys with low boulder- and scree-covered hills and ridges. The quartzite forms rugged ridges and plateaux.|16-MAY-23
27187|Malbon Group|Extent|The constituent formations of the group were mapped in the Cloncurry and Duchess 4-mile Sheet areas (Carter et al., 1961). Recent mapping in the Marraba 1:100 000 Sheet area has shown that several quartzite bodies to the west and northwest of Cloncurry, that were previously mapped as Corella Formation, are correlatives of the Mitakoodi Quartzite (Derrick et al., 1971).|16-MAY-23
27187|Malbon Group|Thickness range|The group ranges in thickness from about 3500 m in the east to about 1000 m in the northwest.|16-MAY-23
27187|Malbon Group|Lithology|Characterised by metamorphosed basic lava flows with sedimentary intercalations that are more abundant towards the top of the group, culminating in the Mitakoodi Quartzite. The sediments are predominantly fine- to medium-grained quartzofeldspathic clastics, and minor shale and calcareous rocks.|16-MAY-23
27187|Malbon Group|Relationships and boundaries|The Malbon Group conformably overlies the Tewinga Group, and is overlain unconformably or conformably by the Mary Kathleen Group (Derrick et al., 1971; Derrick et al., in prep.). It correlates broadly with the middle to upper parts of Haslingden Group in the western succession, and the upper parts of the Soldiers Gap Group to the east.|16-MAY-23
27187|Malbon Group|Age reasons|Precambrian, probably Carpentarian (Middle Proterozoic). The Wimberu Granite intrudes the Malbon Group, and is dated at 1530 m.y. (Richards, 1966). From the correlation with the Haslingden Group noted above, the minimum age of the Malbon Group may be about 1650 m.y., and a maximum age about 1700 m.y. (Plumb & Derrick, 1975).|16-MAY-23
27187|Malbon Group|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
27187|Malbon Group|Proposed publication|Queensland Government Mining Journal, 1976|16-MAY-23
27187|Malbon Group|Comments|Remarks: Further field work is necessary to determine whether or not the Overhang Jaspilite, currently the basal formation in the Mary Kathleen Group, is more properly the topmost unit in the Malbon Group. The Cone Creek and Wakeful Metabasalt Members of the Group are host rocks to small vein-type copper deposits, particularly where the metabasalt is intruded by dolerite dykes.|16-MAY-23
26312|Malmesbury Microgranite|Name source|The name is derived from the Parish of Malmesbury, County of O'Connell, Clarke River, 1:250 000 Series cadastral sheet.|16-MAY-23
26312|Malmesbury Microgranite|Unit history|Included originally by White (1959) and Wyatt & others (1970) in the Oweenee Granite. This unit was expanded (Wyatt & others, 1970) to include granites which form the Coane Range northeast of the Sybil Graben. The type area of the Oweenee  Granite was remapped in 1986 as ignimbrite and consequently the name was changed to Oweenee Rhyolite. The name Malmesbury Microgranite is given to porphyritic microgranite south of the Sybil Graben formerly mapped as Oweenee Granite.|16-MAY-23
26312|Malmesbury Microgranite|Geomorphic expression|The Malmesbury Microgranite is clearly distinguishable on aerial photographs from the associated Oweenee Rhyolite because it forms the lower, less rugged topography.|16-MAY-23
26312|Malmesbury Microgranite|Type section locality|A section along the Gregory Developmental Road between 8059-542602 and 8059528618 is proposed.|16-MAY-23
26312|Malmesbury Microgranite|Extent|The Malmesbury Microgranite crops out, southwest of the Sybil Graben, from the Gregory Developmental road to the Daintree tin mine. It covers an area of approximately 280 km2.|16-MAY-23
26312|Malmesbury Microgranite|Lithology|Pink to grey-pink, extensively chloritised, porphyritic microgranite. Phenocrysts of quartz occur locally and large potassium-feldspar phenocrysts commonly are albite-rimmed.|16-MAY-23
26312|Malmesbury Microgranite|Relationships and boundaries|The granite is not foliated, either tectonically or by magmatic processes. Joint orientations taken from the granite have strong northeast, north-northeast and northwesterly orientations. Faulting is most apparent in the area of Gin Mill where north-northwest and northwest trending faults offset blocks of Oweenee Rhyolite within the granite. The Malmesbury Microgranite intrudes the Oweenee Rhyolite. This can be seen near Silver Spray mine where porphyritic microgranite dykes cut the ignimbrite. The relationship between granites previously known as Oweenee Granite, largely cropping out north of the Sybil Graben (Whatt & others, 1970) and the Malmesbury Microgranite has not been determined.|16-MAY-23
26312|Malmesbury Microgranite|Age reasons|A Rb/Sr isochron of 341+/-7 m.y. was obtained by Webb (1969) from granite south of the Sybil Graben. This age fits in well with the suggestions that the Oweenee Rhyolite is co-magmatic with the Malmesbury Microgranite and is an equivalent of the Middle Carboniferous Meath Rhyolite Member of the Clarke River Basin.|16-MAY-23
26312|Malmesbury Microgranite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
26312|Malmesbury Microgranite|Proposer|Scott M.|16-MAY-23
26312|Malmesbury Microgranite|Resdate|31-AUG-1988|16-MAY-23
26312|Malmesbury Microgranite|Reserved? Yes/No|Yes updated|16-MAY-23
11255|Marburg Subgroup|Name source|The name is derived from the town of Marburg in the Ipswich 1:250 000 Sheet area, Queensland.|16-MAY-23
11255|Marburg Subgroup|Unit history|The unit is redefined from Marburg Formation and upgraded to the Marburg Subgroup. The name was originally used by Reid (1921) as Marburg Stage of the Wolloon Coal Measures and finally evolved to the Marburg Formatioon of McTaggart (1963).|16-MAY-23
11255|Marburg Subgroup|Constituents|The basic two fold sub-division of the Marburg Subgroup comprises the Koukandowie Formation and the underlying Gatton Sandstone and their respective members. The names Koukandowie and Gatton were formerly applied to members, but as it has been demonstrated that they extend basinwide as mappable units, they are redefined as formations. The Marburg 'Formation', of which they were a part, is therefore upgraded to Marburg Subgroup.|16-MAY-23
11255|Marburg Subgroup|Geomorphic expression|See description of constituent formations and members. The cleaner quartzose conglomeratic sandstone intervals form prominent benches and cliffs. The lithic and silty sandstones form rounded hills and slopes and the siltstone and mudrocks weather recessively.|16-MAY-23
11255|Marburg Subgroup|Type section locality|Reference section: Outcrops of most units are incomplete and deeply weathered and thus a reference section was nominated by Grey (1975) in GSQ Ipswich 18 stratigraphic drill hole over the interval 203'5" (620 m) to 2874.0' (876 m).  Type Section: The type section of the Marburg Subgroup is described under the two constituent formations - the Koukandowie Formation (GSQ Ipswich 24), and the Gatton Sandstone (GSQ Ipswich 18). GSQ Ipswich 24 and Ipswich 18 were originally logged and described by officers of the Geological Survey of Queenlsand (Gray, 1975; Cranfield, 1981) and subsequently relogged by A.T. Wells and P.LLE. O'Brien of the Bureau of Mineral Resources.|16-MAY-23
11255|Marburg Subgroup|Description at type locality|The Marburg Subgroup comprises the Koukandowie Formation and the underlying Gatton Sandstone and their respective component members, and as such are described under each of the members. The Marburg Subgroup is conformably overlain by the Walloon Coal Measures in GSQ Ipswich 18 and 24 and conformably overlies the Woogaroo Subgroup in GSQ Ipswich 18. The base of the Subgroup was not reached in GSQ Ipswich 24. The Ma Ma Creek Member of the Koukandowie Formation is differentiated in GSQ Ipswich 18 and 24 but no members of the Gatton Sandstone are apparent in either well section.|16-MAY-23
11255|Marburg Subgroup|Extent|Throughout the Clarence Moreton Basin.|16-MAY-23
11255|Marburg Subgroup|Lithology|The Marburg Subgroup contains labile quartzose-lithic and feldspathic sandstones whereas the underlying Ripley Road Sandstone is predominantly clean quartzose sandstone that is very resistant to weathering. The sandstones in the overlying Walloon Coal Measures are volcanolithic and very friable.|16-MAY-23
11255|Marburg Subgroup|Relationships and boundaries|In all outcrops where the upper contact is visible (there are very few) it is conformably overlain by the Walloon Coal Measures. The lower contact is an unconformity over wide areas particularly on the western margin of the basin where the Subgroup overlaps Late Triassic sediments, and Palaeozoic basement rocks. In the southern part of the Clarence-Moreton Basin notably in the Coast Range, Glenreagh and Nymboida areas, an angular unconformity occurs at the contact with the underlying Woogaroo Subgroup. Elsewhere the Marburg and Woogaroo Subgroups are apparently conformable. McElroy (1962) used the base of the lowest fossil wood horizon as the base of his Marburg 'Formation'. The top was taken as the first pebble band below the Walloon Coal Measures or alternatively at the base of the coal bearing sequence of dark shales, claystones and friable sandstone of the Walloon Coal Measures. These boundary criteria have proved to be unsatisfactory and it is proposed that sandstone composition is the most reliable method of distinguishing the Marburg Subgroup from bounding sequences. The Marburg Subgroup contains labile quartzose-lithic and feldspathic sandstones whereas the underlying Ripley Road Sandstone is predominantly clean quartzose sandstone that is very resistant to weathering. The sandstones in the overlying Walloon Coal Measures are volcanolithic and very friable.|16-MAY-23
11255|Marburg Subgroup|Identifying features|See NSW for def.|16-MAY-23
11255|Marburg Subgroup|Age reasons|Palynofloral assemblages in the Marburg Subgroup indicate an Early Jurassic age (Rhaetian to possibly basal Bajocian) (Cranfield et al., 1976; McKellar, 1981). Details of the ages of each formation and member of the Subgroup are described later in this report.|16-MAY-23
11255|Marburg Subgroup|Proposed publication|Wells A.T., et al. BMR Journal of Geology and Geophysics|16-MAY-23
11255|Marburg Subgroup|State(s)|NSW and QLD|16-MAY-23
11343|Maronghi Creek beds|Unit history|Early workers referred to the Maronghi Creek beds as Neranleigh-Fernvale beds equivalents because of their lithological similarities to that unit (Cranfield & Schwarzbock, 1974).  They were initially defined on the IPSWICH 1:250 000 Sheet area by Cranfield &  Schwarzbock (1973).  The unit was mapped further by Cranfield & others (1976) and extended north onto the GYMPIE 1:250 000 Sheet by Murphy & others (1976).  The unit stretches along the eastern margin of the Yarraman Subprovince, as far north as Murgon, and includes the "Wondai Series" of Reid (1925).  Willey (1998) studied the Maronghi Creek beds in the southern part of NANANGO and northern part of ESK and divided it informally into three broad lithological and structural groups - Elements A to C.Aeromagnetic and radiometric images, and ground observations have been used during the current mapping phase to delineate eight sub-units of the Maronghi Creek beds (see Table 2 below)Table 2: units of the Maronghi Creek beds:-Sub-unit	Generalised Description DCm Undifferentiated sediments and minor volcanics DCmh Hornfelsed DCmv Volcanic DCmd Intruded by numerous microdiorite dykes DCmmc Thinly bedded mudstone and chert DCmsSchist DCma Amphibolite DCmws Weathered and silicified metaarenite, mudstone.|16-MAY-23
11343|Maronghi Creek beds|Geomorphic expression|The unit forms a range of landscapes, from low, rolling grassy hills to rugged heavily timbered country.  As a result the unit exhibits a variety of airphoto patterns, ranging from featureless, evenly drained country in the south to more linear, ridge-dominated patterns in the north.|16-MAY-23
11343|Maronghi Creek beds|Extent|The Maronghi Creek beds occur as a north-north-west trending linear belt forming the eastern margin of the Palaeozoic basement block comprising the Yarraman Subprovince.  The linear belt extends for over 100km from south-west of Toogoolawah on ESK to Murgon on MURGON, and ranges in width from 5 to 20km.  The total area of exposure is over 1000km2.  A brief description of the distribution of the various sub-units follows:-A roof pendant (~4.5km2) of hornfelsed Maronghi Creek beds (DCmh) is present within the Taromeo Igneous Complex approximately 7km north of Blackbutt.  An area (5km2) hornfelsed by the southern part of the Memerambi Granite is present in the south-east corner of MURGON and north-east corner of KINGAROY.  Another area of hornfelsing (8km2) is located between Barker and Meandu Creeks west of Nanango.  Other, smaller areas of hornfelsing (not identified on the map), are present adjacent to intrusive contacts in other parts of NANANGO, ESK and MURGON.A body (~2.5km2 in area) of the volcanic sub-unit (DCmv) occurs approximately 8km north of Nanango.  Two other small areas of around 1km2 are exposed close to the Esk Trough, 16km and 12km respectively, south-east of Nanango. Exposure of the Maronghi Creek beds locally contains significant areas of microdiorite intrusions that could not be mapped out at the scale of this project.  These zones (DCmd) form two linear belts on the eastern margin of the Yarraman Subprovince.  The southern belt (totalling ~45km2) is separated into two parts by a down-faulted block of Permian sediments (Cranfield & others, 1998; Willey, 1998), and extends from Emu Creek to 0.5km north of the D'Aguilar Highway, east of Benarkin.  The northern belt, of approximately 20km2, extends from 8km north of Benarkin to 10km south-east of Nanango.  A mudstone/chert-dominated sequence (DCmmc) forms an elongate body (~28km2) up to 4km wide located in the north-east corner of KINGAROY.  Several small areas of schist (DCms) are present south-east of Nanango as roof pendants in the Taromeo Igneous complex.|16-MAY-23
11343|Maronghi Creek beds|Thickness range|A reliable estimate of the original thickness of the unit is difficult to make due to structural repetition during subduction.  The unit may have originally been as little as a few hundred metres thick.|16-MAY-23
11343|Maronghi Creek beds|Lithology|Reid (1925) and Derrington (1954) described the lithology of this unit in the Murgon area and later Fardon (1960) described it in the Cooyar area.  The Maronghi Creek beds were first defined by Cranfield & Schwarzbock (1974) as a sequence of interbedded chert, jasper, mudstone, arenite and metavolcanics.  Cranfield & others (1976) summarised the unit in the Ipswich 1:250 000 Sheet area as being composed of interbedded chert, jasper, shale, arenite and metavocanics.  Transposition structures showing deformed quartz veins were noted in thin section.  Maronghi Creek beds in southern part of NANANGO and northern part of ESK -  divided into 3 broad groups, Elements A to C, based on structural character (Willey 1998).  Willey reported, although chert and jasper, were present , they were not as extensive as indicated by previous authors. He also suggested that arenite is most dominant lithology and considered the silica-rich lithologies did not have chert, jasper, vein quartz or quartzite as their protolith.The undifferentiated Maronghi Creek beds (DCm) include most of `Element A¿ as described by Willey (1998).  In general, rocks of this unit DCm comprise interbedded massive to poorly sorted quartz lithic to lithic arenites, siltstones and mudstones with rare thin deeply weathered spilitic volcanics.  In some areas, most notably south of Emu Creek and in a gully draining into Nukinenda Creek (AMG 419000 7014200), they may show  melange or 'broken formation' - features that are consistent with those described by Raymond (1984) for deformed sediments in melange terrains (Willey, 1998, p52).  Within the arenites numerous irregular sub-planar zones show soft sediment grain alignment and/or up to 3 generations of quartz vein healed brittle fractures (Willey, 1998).  Dense quartz veining + alteration often gives appearance of chert in  hand specimens.  Bedding, where preserved, is often complexly folded, faulted, boudinaged or sheared.  In the central west and north-western part of NANANGO the undifferentiated Maronghi Creek beds include areas of phyllitic mudstone and siltstone intruded by dykes ranging in composition from basalt to rhyolite....Hornfelsed Maronghi Creek beds (DCmh) occur in a number of areas adjacent to intrusive bodies.  A roof pendant is present within Taromeo Igneous Complex north of Blackbutt - composed of hard dark grey to black hornfelsed and semi-hornfelsed quartzose and lithic arenites. The volcanic sub-unit (DCmv) makes up only a small percentage of overall Maronghi Creek beds and is composed primarily of altered basaltic rocks...... Sub-unit DCmd is a composed of fine-grained arenaceous lithologies similar to the main body of the unit but has been extensively intruded by microdiorite dykes and irregular intrusions...........The sub-unit DCmmc, mapped in the northeastern part of KINGAROY, is composed of thinly bedded (generally 1-2 cm) mudstone and red chert......Sub-unit DCma comprises basic meta-volcanics + amphibolite|16-MAY-23
11343|Maronghi Creek beds|Depositional environment|The unit is thought to represent mainly fine-grained sediments and mafic sea-floor lavas deposited in deep marine conditions before being incorporated into the eastern Australian margin as a subduction complex.  The sediments were derived from the eastern Australian continental margin.  The dominance of poorly sorted arenite, composed of angular grains and showing no bedding, indicate a density current origin.|16-MAY-23
11343|Maronghi Creek beds|Relationships and boundaries|The Maronghi Creek beds are unconformably overlain by or faulted against the Triassic Esk Formation along the western margin of the Esk Trough.  The unit is faulted against probable Permian unnamed sediments south-east of Blackbutt, and the Middle Carboniferous Bjelke Petersen beds east of Murgon. The Maronghi Creek beds grade laterally into the Devonian to Carboniferous Sugarloaf Metamorphics and are overlain unconformably by the Permian Gilla Volcanics, Triassic Neara Volcanics and Tarong beds, the Triassic to Jurassic Woogaroo Subgroup, the Jurassic Marburg Formation, the Tertiary Main Range Volcanics and associated sediments.The Memerambi Granite, the Boondooma and Taromeo Igneous Complexes, the Kenewah Granodiorite, and the Woolshed Mountain Granodiorite intrude the unit.  A number of smaller unnamed bodies also intrude the unit in different areas including the Permian microdiorites, porphyries and gabbro/diorites south of Blackbutt described by Willey (1998,1999).|16-MAY-23
11343|Maronghi Creek beds|Age reasons|No identifiable fossils have been found within the unit.  A minimum age of Latest Carboniferous-Early Permian is indicated by Early Permian (291, 296Ma) dates for pyritic microdiorites (Willey, 1998), that intrude the Maronghi Creek beds south of Emu Creek, south-south-west of Blackbutt.  A Devonian-Carboniferous age is inferred for the unit because its lithological and structural style is similar to accretionary wedge rocks of that age elsewhere in the northern New England Orogen.|16-MAY-23
11343|Maronghi Creek beds|Correlations|The unit is thought to correlate with accretionary wedge rocks of similar age within the northern New England Orogen.  Probable correlatives in the nearby North and South D'Aguilar Sub-provinces include the Mount Clara beds (around Kilkivan), the Amamoor beds (west of Gympie), the Booloumba beds (south-west of Kenilworth), and the Neranleigh Fernvale beds (north and south of Brisbane).  To the north, the unit is thought to correlate with elements of the Curtis Island Group (the Wandilla and Doonside Formations.|16-MAY-23
11343|Maronghi Creek beds|Comments|GEOPHYSICAL EXPRESSION::  On AIRDATA K-Th-U (RGB) ternary radiometric images, the majority of the unit has a characteristic medium-toned, mottled pink/brown/green combination.  Sub-unit DCmd has a distinctive dark tone on the image caused by numerous small dioritic dykes or intrusions.  Deeply weathered areas of Maronghi Creek beds have elevated relative thorium and uranium levels and have a deeper green-blue signature on the ternary radiometric image.All parts of the unit show a uniformly low response on aeromagnetic images.STRUCTURE:: Bedding and the sub-parallel slaty cleavage within the Maronghi Creek beds dip either steeply to the west or east.  The unit is assumed to be structurally thickened by imbricate thrusting during the Devonian-Carboniferous subduction process.  This process may have also produced the small-scale tight to isoclinal, sub-horizontally-plunging folds locally visible in some thin-bedded rocks.|16-MAY-23
11343|Maronghi Creek beds|References|CAMPBELL, L.M., HOLCOMBE, R.J. & FIELDING, C.R.,1999,The Esk Basin - a Triassic foreland basin within the northern New England Orogen.,In: Flood, P.G. (Editor) New England Orogen : regional geology, tectonics and metallogenesis : papers presented at a conference held at the University of New England, Armidale, 1-3 February 1999.  Earth Sciences, University of  New England, 1999,Regional Geology.CRANFIELD, L.C. & SCHWARZBOCK, H., 1974, New and revised stratigraphic names for the Ipswich 1:250 000 Sheet area.,"Queensland Government Mining Journal, 75, 322-323.CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.",1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional Geology.DERRINGTON, S.S,1954,The geology of the Murgon-Windera district. Unpublished Bsc Honours Thesis, Department of Geology, University of Queensland. Regional Geology,Murgon.FARDON, R.S.H.,1960, The geology of the Cooyar area. Unpublished Honours Thesis, Department of Geology, University of Queensland. Regional Geology.MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.REID, J.H., 1925, The Murgon-Goomeri Districts. Queensland Government Mining Journal. 26, 87-91WILLEY, E.C., 1998, The Maronghi Creek beds: A preliminary appraisal. Queensland Government Mining Journal. 99 (No. 1161), 49-56.WILLEY, E.C., 1999, Intrusives in the southern outcrop of the Maronghi Creek beds (SE Qld). Regional Geology. Tectonics and Metallogenesis. New England Orogen.  Papers presented at a conference held at The University of New England, Armidale. 1-3 February 1999.|16-MAY-23
11361|Marraba Volcanics|General description|Detailed regional mapping has shown that lower boundary of the Marraba Volcanics as defined by Carter et al. (1961) requires redefinition. The previous definition placed this boundary below a pink-brown, well-bedded to massive, fine-grained quartzite but Carter et al. (1961, p.72) note that this quartzite is similar in appearance to the uppermost quartzite in the underlying Argylla Formation. In mapping the Marraba 1:100 000 Sheet area, Derrick et al. (1971) restricted the Marraba Volcanics to the sequence of mainly basic volcanics, and placed the former basal quartzite in the Argylla Formation. This results in a more readily mappable lower boundary of the Marraba Volcanics, which are now separated from a sequence of acid volcanics and intercalated fine-grained quartzites. The quartzite which formerly was in the Marraba Volcanics is about 100 m thick in the west and up to 1000 m thick in the east, and is probably time equivalent to the Mount Guide Quartzite (Derrick et al., 1976b). The remaining sequence of Marraba Volcanics was subdivided by Derrick et al. (1971) into three conformable members, namely the Cone Creek Metabasalt Member, the Mount Start Member, and the Timberoo Member. They are defined elsewhere (see relevant cards for details).|16-MAY-23
11361|Marraba Volcanics|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
11361|Marraba Volcanics|Proposed publication|Queensland Government Mining Journal, 1976|16-MAY-23
11387|Martins Well Limestone Member|Name source|Martins Well at 7859 682684.  The grid reference is based on the AGD66 datum.|16-MAY-23
11387|Martins Well Limestone Member|Unit history|White (1965) referred to the unit as 'B' lens of the Broken River Formation.  It was originally defined by Jell (1968) as a member of the Broken River Formation, but with the introduction of the name Shield Creek Formation by Wyatt & Jell (1980), it became a member of that formation.|16-MAY-23
11387|Martins Well Limestone Member|Geomorphic expression|The unit forms a low strike ridge, readily discernible on airphotos.  The outcrop is rubbly due to its well bedded nature, and does not form prominent bluffs.|16-MAY-23
11387|Martins Well Limestone Member|Type section locality|Jell (1968) described a type section 85 m thick, cropping out 225 m NW of Martins Well between 7859 682684 (base) and 683683 (top).   The grid reference is based on the AGD66 datum.|16-MAY-23
11387|Martins Well Limestone Member|Description at type locality|The section consists of three lithological units.  The lowermost unit consists of 15 m of bioclastic calcarenite with sporadic shale interbeds and autochthonous coralline limestone.  The middle unit is 44 m thick, and consists of well-bedded muddy calcarenite, calcilutite, and mudstone.  The uppermost 26 m consists of bioclastic calcarenite with minor thin mudstone beds.|16-MAY-23
11387|Martins Well Limestone Member|Extent|A narrow folded belt from near Martins Well to the headwaters of Magpie Creek.|16-MAY-23
11387|Martins Well Limestone Member|Thickness range|Up to 150 m.|16-MAY-23
11387|Martins Well Limestone Member|Lithology|Well bedded (medium to thick) bioclastic calcarenite with thin shale interbeds.|16-MAY-23
11387|Martins Well Limestone Member|Fossils|The member contains a rich fauna of corals (tabulate and rugose) and stromatoporoids, as well as brachiopods, bivalves, crinoids, sponges, nautiloids, trilobites, ostracods, and conodonts; algae are also common.|16-MAY-23
11387|Martins Well Limestone Member|Relationships and boundaries|A member of the Shield Creek Formation.|16-MAY-23
11387|Martins Well Limestone Member|Age reasons|The conodonts indicate a Lochkovian to Pragian age (Telford, 1975).|16-MAY-23
11387|Martins Well Limestone Member|References|JELL, J.S., 1968:  New Devonian rock units of the Broken River Embayment, north Queensland.  Queensland Government Mining Journal, 69, 6-8.  **TELFORD, P.G., 1975:  Lower and Middle Devonian conodonts from the Broken River Embayment, north Queensland, Australia.  Special Papers in Palaeontology, 15.  **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River 	area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.  **WYATT, D.H. & JELL, J.S., 1980:  Devonian and Carboniferous stratigraphy of the northern Tasman Orogenic Zone in the 	Townsville hinterland; in Henderson, R.A. & Stephenson, P.J. (editors), The Geology and Geophysics of Northeastern Australia.  Geological Society of Australia, Queensland Division, Brisbane, 201-228.|16-MAY-23
79119|Mary Basalt|Name source|After Mary River which meanders through Gympie.|16-MAY-23
79119|Mary Basalt|Unit history|This unit was first used informally as Mary volcanics by Gympie Eldorado Gold Mines at Monkland Mine and was subsequently referred to by Cranfield (1999), Sivell & Arnold (1999), Sivell & McCulloch (2001), Li & others (2015). Equivalent to Dunstan's (1911) Second Volcanic (Greenstone) Group (2V).|16-MAY-23
79119|Mary Basalt|Constituents|Tozer Basalt Member.|16-MAY-23
79119|Mary Basalt|Type section locality|Two drillholes held in the Zillmere storage facility represent the Mary Basalt: BHP drill hole G023, depth 227-307m near Monkland Mine collared at MGA 468180mE; 7100900mN (Lat: -26°12'40"  Long: 152°40'53"  ) and GEGM dril hole G227, depth 222-322m collared 800m east of the municipal quarry at MGA 469895mE; 7098795mN (Lat: -26°13'48" Long: 152°41'55"  ).  Surface exposure can be seen in the Municipal quarry located west off Laurenceson Road  at MGA 469055mE; 7098890mN (Lat: -26°13'45" Long: 152°41'25" where it occurs on the upper two benches of the quarry and in the face of the lowest bench.  The latter is dissected by shears, some of which contain very narrow seams of actinolite asbestos. Permission is required to enter the quarry.|16-MAY-23
79119|Mary Basalt|Extent|From Dawn Block and Six Mile Block northwards through Monkland Block and Jones Hill. Thins northwards in the Phoenix Block but was identified at 251-371 m in Freeport drill hole G002 in the Great Northern Block and at 361-509 m in Freeport drill hole G005 in the Two Mile Block.|16-MAY-23
79119|Mary Basalt|General description|At Monkland Mine the Mary Basalt is notably hematitic and is regarded as shallow water to emergent, subaerial deposit. It is underlain by the Tozer basalt which is not hematitic and is interpreted partly as deeper marine flow deposit and partly as forming intrusive dykes or sills. Both appear to be fed from the same source via dykes which have cut through the underlying Dawn Formation. Away from Monkland Mine, some basalts mapped as Mary Basalt may have closer affinities with Tozer.|16-MAY-23
79119|Mary Basalt|Thickness range|100 m to 300 m at Monkland, 150 m at Kenna prospect in the Sovereign Block, over 150 m at Inglewood Horst. At the municipal quarry within Six Mile Block and in the Dawn Block thicknesses are considerable but unknown.|16-MAY-23
79119|Mary Basalt|Lithology|At Monkland  consists of numerous, successive coherent basalt flows, each one terminated by an oxidised flow top.  Arnold (1996) estimated an average flow thickness of about 10m.  The lavas contain varying proportions of plagioclase (5-35%), clinopyroxene (1-20%) and olivine (1-5%) in a fine groundmass of albitised plagioclase microlites and low grade alteration products (sericite, chlorite, epidote, carbonate, leucoxene).  The saussuritised plagioclase phenocrysts are commonly 1-2mm long. Pyroxenes are larger, to 4mm, varying from fresh to totally altered.  Olivines form cellular boxworks infilled with carbonate, chlorite and minor quartz.   Many lavas are vesicular, containing trains of circular, elliptical or amoeboid shaped amygdules.  Rare re-deposited debris flows and ash beds have been recorded.  Flow tops vary in thickness from less than a metre to 25m and are scoriaceous, brecciated (tuff-breccias) and very hematitic.  They may also have higher concentrations of close-packed feldspar phenocrysts than the underlying lava.  The numerous vesicles are filled with chlorite-epidote-carbonate.|16-MAY-23
79119|Mary Basalt|Relationships and boundaries|In  both reference drillholes and elsewhere is overlain by hematitic conglomerate and sandstone of the Eldorado Clastics Member; In G023 the basalt terminates against the Inglewood Fault structure and in G227 ends in a swarm of dolerite dykes.  In the municipal quarry the Mary Basalt is underlain by Tozer Basalt on the lowest bench in a possible intrusive contact.  Where Tozer Basalt is absent it is underlain by Hall Clastics, Dawn Formation.|16-MAY-23
79119|Mary Basalt|Alteration and Mineralisation|Some autobrecciated lavas have fracture controlled liesegang or 'onion-ring' alteration in which relict cores of fresher basalt are surrounded by very epidotised rock impregnated with rings of densely concentrated fine hematite. These liesegang textures are attributed to palaeoweathering by Sivell and McCulloch (2001).|16-MAY-23
79119|Mary Basalt|Geochemistry|Regarded as volcanic arc tholeiitic basalts by Sivell & McCulloch (2001).|16-MAY-23
79119|Mary Basalt|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie, 12-JAN-2017.|16-MAY-23
79119|Mary Basalt|References|Dunstan, B., 1911: Geology map of Gympie and environs. GSQ Publ. No. 221b.  **Arnold, G.O., 1996. Geology of the Southern Gympie Goldfield from core logging, and implications for mineralisation.  Unpublished report to Gympie Eldorado Gold Mines Pty Ltd.  **Cranfield, L.C., 1999:Gympie Special Sheet 9445, Part 9545, Queensland 1:100,000 Geological Map Commentary. Queensland Department of Mines and Energy, Brisbane.  **Sivell, W.J. and Arnold, G.O. 1999: Geochemical and volcanic stratigraphy of a segment of an island arc - Gondwana rim accretion zone, Gympie Province, southeast Queensland.  In Flood, P.G. (Editor): Regional Geology, Tectonics and Metallogenesis, New England Orogen, NEO ¿99 Conference, 255-266.  **Sivell, W.J. and McCulloch, M.T. 2001: Geochemical and Nd-isotopic systematics of the Permo-Triassic Gympie Group, southeast Queensland.  Australian Journal of Earth Sciences 48, 377-394.  **Li, P., Rosenbaum, G., Yang, J-H. and Hoy, D. 2015	Australian-derived detrital zircons in the Permian-Triassic Gympie terrane (eastern Australia): Evidence for an autochthonous origin. Tectonics, 34, 858-874.|16-MAY-23
26018|Mary Kathleen Group|Name source|Township of Mary Kathleen, latitude 20o46'40"S, longitude 139o58'45"E.|16-MAY-23
26018|Mary Kathleen Group|Constituents|The Mary Kathleen Group consists of the Ballara Quartzite, Overhang Jaspilite, Chumvale Breccia, Corella Formation, Mount Philp Agglomerate, Marimo Slate, Answer Slate, Staveley Formation and Kuridala Formation.|16-MAY-23
26018|Mary Kathleen Group|Extent|The constituents of the group were mapped on the Dobbyn, Cloncurry and Duchess 4-mile Geological Sheets (Carter et al., 1961) and on the Boulia 1:250 000 Sheet area (Casey, 1968).|16-MAY-23
26018|Mary Kathleen Group|Thickness range|The group ranges in thickness from about 1700 m on the eastern edge of the Kalkadoon-Leichhardt basement, where it consists of only the Ballara Quartzite and the Corella Formation, to about 4000 m in a section north of Duck Creek Anticline where it consists of Overhang Jaspilite and Corella Formation. Greater thicknesses may occur in some sections which include the slate formations further south.|16-MAY-23
26018|Mary Kathleen Group|Lithology|Characterised by metamorphosed fine-grained sediments, shale, siltstone, marl, banded iron formation and limestone with minor fine to medium sandstone and basic tuff and basalt.|16-MAY-23
26018|Mary Kathleen Group|Relationships and boundaries|The Mary Kathleen Group conformably or disconformably overlies the Malbon Group and unconformably overlies the Tewinga Group and the Soldiers Cap Group. It is unconformably overlain by the Mount Albert Group and Quamby Conglomerate. It is intruded by dolerite of at least three ages, the Lunch Creek Gabbro, the Tommy Creek Microgranite, the Burstall Granite, the Hardway Granite, and phases of the Naraku Granite and Wonga Granite.|16-MAY-23
26018|Mary Kathleen Group|Age reasons|Probably between about 1780 and 1550 m.y; the age of the Argylla Formation, about 1780 m.y. minimum (McDougall et al., 1965) provides a maximum age for the unconformably overlying Mary Kathleen Group. An age of about 1650 m.y. on Sybella Granite (Plumb and Derrick, 1975), which is thought to unconformably underlie Mary Kathleen Group equivalents, may also set an older limit to the age of the Group. Granites intrusive into the Mary Kathleen Group include the Wonga Granite, dated at 1665+/-16 and 1738+/-20 m.y. (Page and Derrick, 1973); Page, pers. comm.), the Burstall Granite, dated at 1630+/-50 m.y. and 1448+/-46 m.y. (R W Page, pers. comm.), and the Wimberu Granite 1540 m.y. (Richards, 1966). The Group is also intruded by the Lunch Creek Gabbro, whose minimum age is 1498+/-78 m.y. (Page, pers. comm.). Ar40/Ar39 dating suggests that the Corella Formation was being metamorphosed between about 1570 m.y. and 1450 m.y. (Green, 1975).|16-MAY-23
26018|Mary Kathleen Group|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1977|16-MAY-23
26018|Mary Kathleen Group|Proposed publication|Queensland Government Mining Journal|16-MAY-23
11533|McCord Granite|Name source|The unit is named after McCord Creek which drains the northwestern part of the unit.|16-MAY-23
11533|McCord Granite|Unit history|Previously mapped as Elizabeth Creek Granite (Best, 1962;  de Keyser & Wolff, 1964;  de Keyser & Lucas, 1968).|16-MAY-23
11533|McCord Granite|Geomorphic expression|The granite forms rough hilly country with numerous bouldery outcrops and scattered pavements.  The country underlain by the unit has an open drainage pattern and is characterised by medium tones on aerial photographs.|16-MAY-23
11533|McCord Granite|Type section locality|The designated type locality is at GR 2268 80734, ~4 km southwest of Crystal Brook homestead, on the northern side of the track to the Tate Tin Field and the site of the abandoned settlement of Fischerton. The grid reference is based on the AGD66 datum.|16-MAY-23
11533|McCord Granite|Description at type locality|The granite (sensu lato) forms prominent bouldery outcrops and pavements in this area.|16-MAY-23
11533|McCord Granite|Extent|The unit forms an irregular body with a northwesterly elongation north and south of the Tate River, ~30 km southwest of Chillagoe.  The unit extends over an area of ~220 km2|16-MAY-23
11533|McCord Granite|General description|STRUCTURE AND METAMORPHISM:: The unit forms massive, non-foliated outcrops.MINERALISATION:: Extensive tin mineralisation in the Tate River area is intimately associated with the McCord Granite, in particular the late-stage microgranites.  The elevated Sn and Nb, as well as F, Rb, U, Th, Zr, Ga and Li abundances which characterise the McCord Granite (especially the late-stage microgranites) resulted mainly from extensive crystal fractionation (Champion, 1991).|16-MAY-23
11533|McCord Granite|Lithology|The McCord Granite consists mainly of pale pink to cream, medium-grained, even-grained to slightly porphyritic adamellite.  K-feldspar grains are pink, euhedral to subhedral and commonly perthitic.  Albite rims are common.  Plagioclase ranges in composition from oligoclase to albite.  Most grains are only slightly to moderately zoned.  Biotite occurs as well-formed to ragged grains, pleochroic from pale yellow to dark greenish brown or red-brown and appears to have crystallised relatively late.  Fluorite is a conspicuous accessory mineral in many samples.  Miarolitic cavities and irregular pegmatitic zones are relatively common.  The pegmatitic zones consist mainly of quartz and pink K-feldspar; minor tourmaline and fluorite are commonly also present.  Quartz, tourmaline, and fluorite infill or partly infill many of the miarolitic cavities.The adamellite is intruded by pods and dykes of more highly fractionated, late-stage microgranite.  The microgranites are similar mineralogically to the early, main granite, but are of finer grainsize and are generally more strongly porphyritic.  Plagioclase is relatively sodic and typically unzoned or only slightly zoned.  Biotite flakes are mainly interstitial.The McCord Granite shows widespread alteration of plagioclase, K-feldspar, and biotite and extensive growth of secondary minerals such as chlorite, secondary biotite, muscovite, albite and fluorite (see Witt, 1987, 1988;  Pollard, 1988; and Taylor & Pollard, 1988 for more details).  The unit is extensively jointed, and the most intense alteration is commonly shown by adamellite adjacent to the joints.|16-MAY-23
11533|McCord Granite|Relationships and boundaries|The McCord Granite intrudes the McDevitt and Dargalong Metamorphics (Proterozoic), biotite adamellite of Proterozoic or Early Silurian age (mapped as part of the Forsayth Granite by Best, 1962) and the Blackman Gap Complex of Proterozoic and Early Silurian age.  It is cut by intrusive rhyolite and fine to medium-grained granodiorite(?), quartz monzodiorite and adamellite forming the Crystalbrook Volcanic Neck of Best (1962), and by numerous quartz veins and linear greisen zones;  the latter appear to be localised along joints.  It is also inferred to be intruded by units Cgd6 and Cg3 (Cranfield, 1992) of the Ootann Supersuite of Champion (1991).|16-MAY-23
11533|McCord Granite|Age reasons|The McCord Granite has yielded isotopic ages of 309 Ma (K-Ar; Richards & others, 1966) and 321 Ma (Rb-Sr biotite, with an assumed initial ratio of 0.710; Black, 1978).  The unit is therefore regarded as Late Carboniferous.|16-MAY-23
11533|McCord Granite|Comments|The McCord Granite is similar to the Elizabeth Creek Granite in the Elizabeth Creek area north of Mount Surprise.  Both are members of the O'Briens Creek Supersuite of Champion (1991).  They are distinguished by their anomalously high Th, F, and, to a lesser extent, U, Ga, Y and K contents compared with granites of the Almaden and Ootann Supersuites in the region (Champion & Chappell, 1992).  The McCord also forms a prominent anomaly on airborne radiometric maps of the region.|16-MAY-23
11533|McCord Granite|References|BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.BLACK, L.P., 1978:  Isotopic ages of rocks from the Georgetown-Mount Garnet-Herberton area, north Queensland.  Bureau of Mineral Resources, Australia, Report 200 (BMR Microform MF28).CHAMPION, D.C., 1991:  Petrogenesis of the felsic granitoids of far north Queensland.  Ph.D. Thesis, Australian National University, Canberra (unpublished). CHAMPION, D.C., & CHAPPELL, B.W., 1992:  Petrogenesis of felsic I-type granites:  an example from northern Queensland.  Transections of the Royal Society of Edinburgh:  Earth Sciences, 83, 115-126.DE KEYSER, F., & LUCAS, K.G., 1968:  Geology of the Hodgkinson and Laura Basins, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 84.DE KEYSER, F., & WOLFF, K.W., 1964:  The geology and mineral resources of the Chillagoe area.  Bureau of Mineral Resources, Australia, Bulletin 70.POLLARD, P.J., 1988:  Petrogenesis of tin-bearing granites of the Emuford district, Herberton tinfield, Australia.  Australian Journal of Earth Sciences, 35, 39-57.RICHARDS, J.R., WHITE, D.A., WEBB, A.W., & BRANCH, C.D., 1966:  Isotopic ages of acid igneous rocks in the Cairns hinterland, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 88.TAYLOR, R.G., & POLLARD, P.J., 1988:  Pervasive hydrothermal alteration in tin-bearing granites and implications for the evolution of ore-bearing magmatic fluids;  in Taylor, R.P., & Strong, D.F. (editors) - Recent advances in the geology of granite-related mineral deposits - Proceedings of the CIM conference on granite-related mineral deposits, September 1985.  Canadian Institute of Mining & Metallurgy, Special Volume 39, 86-95.WITT, W.K., 1987:  Fracture-controlled feldspathic alteration in granites associated with tin mineralization in the Irvinebank-Emuford area, northeast Queensland.  Australian Journal of Earth Sciences, 34, 447-462.|16-MAY-23
11575|McNamara Group|Name source|Jack McNamara's Mine on the Mount Oxide 1:100 000 Sheet at 000567, and from McNamaras Highway, a major access road.|16-MAY-23
11575|McNamara Group|Unit history|The sequences now included in the McNamara Group have previously been mapped as part of the now discarded Mammoth Formation (Cavaney, 1975a) and as Gunpowder Creek Formation, Paradise Creek Formation, Ploughed Mountain Beds, Mingera Beds and Philpah Sandstone (Carter & others, 1961). The name was first published by Cavaney (1975b).|16-MAY-23
11575|McNamara Group|Constituents|Lawn Hill Formation (top); Termite Range Formation; Riversleigh Siltstone; Shade Bore Quartzite; Lady Loretta Formation; Esperanza Formation; Paradise Creek Formation; Gunpowder Creek Formation; Torpedo Creek Quartzite (base).|16-MAY-23
11575|McNamara Group|Extent|The group crops out extensively from the Nicholson River in the northern part of the Lawn Hill 1:250 000 Sheet area to the Templeton River in the south of the Mount Isa 1:250 000 Sheet area. It is bounded to the east by the Mount Gordon fault zone and is overlain to the west by Cambrian rocks of the Georgina Basin and in the Carrara and Mitcheibo 1:100 000 Sheet areas in the Northern Territory.|16-MAY-23
11575|McNamara Group|Thickness range|The greatest thickness of McNamara Group preserved in any one section is 8500 m in the Lawn Hill 1:100 000 Sheet area. This is the only section where a complete sequence is preserved.|16-MAY-23
11575|McNamara Group|Lithology|Three broad subdivisions can be recognised in the group: 1. A lower, mainly clastic subdivision which contains coarse sandstone and conglomerate (Torpedo Creek Quartzite), overlain by a thicker sequence of siltstone, sandstone, shale and dolomite (Gunpowder Creek Formation).  2. A middle dolomitic subdivision comprising lower and upper components of dolomite, stromatolitic dolomite, siltstone and sandstone (Paradise Creek Formation and Lady Loretta Formation) separated by massive stromatolitic chert, sandstone and siltstone (Esperanza Formation).  3. An upper clastic subdivision comprising basal orthoquartzite (Shade Bore Quartzite) overlain by siltstone, sandstone and dolomite (Riversleigh Siltstone), massive greywacke, siltstone and sandstone (Termite Range Formation) and tuff, siltstone, sandstone and shale (Lawn Hill Formation) at the top.|16-MAY-23
11575|McNamara Group|Relationships and boundaries|The McNamara Group rests with slight angular unconformity on the Surprise Creek Formation. In the Lawn Hill Sheet area, the group lies unconformably on a basement of Kamarga Volcanics and Yeldham Granite while in the Kennedy Gap and Mammoth Mines Sheet areas, it overlies Surprise Creek Formation, Carters Bore Rhyolite, Myally Subgroup, Eastern Creek Volcanics, Judenan Beds and Leander Quartzite. The McNamara Group is overlain with angular unconformity by sandstone of the Carpentarian South Nicholson Group and by Cambrian limestones of the Georgina Basin.|16-MAY-23
11575|McNamara Group|Identifying features|The definition of the McNamara Group, as published by Hutton, Cavaney & Sweet (1981), is hereby varied to include two new units which have been recognised in the Carrara Range Region, Northern Territory. Names of new constituent formations: Musselbrook Formation and Plain Creek Formation.  Reasons for including the new formations in the McNamara Group: In its type area, in the Lawn Hill 1:100 0000 Sheet area, th McNamara Group consists of nine formations totalling some 8500 m. Hutton and others (1981) descriabe three broad lithological subdivisions within the group: a lower, mainly clastic sequence, a middle carbonate-rich sequence, and an upper clastic sequence. During recent mapping in the Carrara Range Region in the eastern Northern Territory the Carrara Range Formation and Bluff Range beds of Smith & Roberts (1963) were subdivided into six formations. The three upper formations are a conformable sequence from Musselbrook Formation (oldest), through Plain Creek Formation, to Lawn Hill Formation (youngest). This sequence is included in the McNamara Group for the following reasons: (1) The Lawn Hill Formation, a constituent formation of the Group in its type area, has been recognised in the Carrara Range Region; and (2) the same broad threefold subdivision, described by Hutton & others (1981), is recognisable. Although the threefold subdivision is recognisable individual formations are not. The Musselbrook Formation includes the two lower subdivisions, but has not been subdivided for reasons given elsewhere (see definition of Musselbrook Formation). The Plain Creek and Lawn Hill Formations together represent the upper clastic subdivision in the Carrara Range Region.|16-MAY-23
11575|McNamara Group|Age reasons|Mid Proterozoic (Carpentarian). It unconformably overlies the Carters Bore Rhyolite which has been dated at 1678 m.y. (Page, 1978). The upper age limit is 1270-1390 m.y. (McDougall & others, 1965) for the Roper Group, a correlative of the South Nicholson Group which unconformably overlies the McNamara Group. Tuff beds in the MOunt Isa Group which are correlatead with those in the McNamara Group have been dated by U-Pb (Zircon) as about 1670 m.y. (Page, in press).|16-MAY-23
11575|McNamara Group|Proposed publication|Queensland Government Mining Journal|16-MAY-23
11575|McNamara Group|Proposed publication|Already published, redefn in Rept. 242|16-MAY-23
11575|McNamara Group|Apprdate|12-MAR-1982|16-MAY-23
11575|McNamara Group|Apprdate|24-JUL-1981|16-MAY-23
11575|McNamara Group|Defn approved by|Brakel A.T.|16-MAY-23
11575|McNamara Group|Defn approved by|Whitaker W.|16-MAY-23
11575|McNamara Group|Name first published by|Glikson A.Y., Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
11575|McNamara Group|Proposer|Hutton L.J., Cavaney R.J., Sweet I.P.|16-MAY-23
11575|McNamara Group|Proposer|Sweet I.|16-MAY-23
11575|McNamara Group|State(s)|QLD & NT|16-MAY-23
11575|McNamara Group|State(s)|NT|16-MAY-23
11575|McNamara Group|Status|1|16-MAY-23
24376|Meath Rhyolite Member|Name source|Parish of Meath, County of Clarke.|16-MAY-23
24376|Meath Rhyolite Member|Unit history|Previously part of the Clarke River Formation (now Group) (White, 1959).|16-MAY-23
24376|Meath Rhyolite Member|Geomorphic expression|The Meath Rhyolite Member forms relatively narrow, continuous ridges, which are heavily wooded and have dark tones on the aerial photographs.|16-MAY-23
24376|Meath Rhyolite Member|Type section locality|The holostratotype of the Meath Rhyolite Member (approximately 75 m thick) is along the Clarke River from GR 948504 (base) to 946505 (top), where heavily jointed, pink-buff, massive ignimbrite containing phenocrysts of quartz and biotite, crop out.|16-MAY-23
24376|Meath Rhyolite Member|Extent|The Meath Rhyolite Member is a useful marker in the middle of the Lyall Formation. It crops out around a domal structure in the centre of the Clarke River Basin, north of the junction of the Clarke River and Keppell Creek South, and also in windows within the Tertiary laterite further to the north. It also has been mapped in the west of the basin near the Broken River.|16-MAY-23
24376|Meath Rhyolite Member|Thickness range|In the type section the member is approximately 75 m thick, but it thins around the northern margin of the dome.|16-MAY-23
24376|Meath Rhyolite Member|Lithology|Around the dome the Meath Rhyolite Member mainly consists of several sheets of brown-pink-orange ignimbrite which contains pumice fragments and roughly aligned fiamme. Euhedral biotite and embayed beta-quartz phenocrysts are characteristic. Minor volcanolithic sandstone and conglomerate (locally containing plant remains) are interbedded with the ignimbrite. Also, Mouthier & Rippert (1980) have described a massive, vitric, crystal ashfall-tuff, from windows in the Tertiary laterite, in the northern portion of the Clarke River Basin.|16-MAY-23
24376|Meath Rhyolite Member|Relationships and boundaries|The Meath Rhyolite Member forms a distinctive marker unit in the Lyall Formation, dividing the formation into two informal subunits. Microfossil evidence suggests a possible hiatus at or near the onset of the volcanism (Jell & Playford, in press). Quartz porphyry bosses and stocks intrude the Clarke River Group to the level of the Meath Rhyolite Member, and may represent feeders.|16-MAY-23
24376|Meath Rhyolite Member|Age reasons|A hiatus between the Late Visean and Late Carboniferous is suggested from palynological evidence at or near the onset of volcanism represented by the Meath Rhyolite Member (Jell & Playford, in press). Late Visean spores were described by Playford (1983) stratigraphically above what is interpreted as an equivalent of the Meath Rhyolite Member in the southwestern corner of the basin. This suggests that the member is Late Visean in age.|16-MAY-23
24376|Meath Rhyolite Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24376|Meath Rhyolite Member|Proposer|Scott M.|16-MAY-23
26026|Melon Creek Tonalite|Unit history|The Melon Creek Tonalite  was not recognised by previous mapping (Wyatt & others, 1970).|16-MAY-23
26026|Melon Creek Tonalite|Type section locality|The best known outcrops are around 8159-190629 in Melon Creek which is therefore designated as the type locality. Grey, medium-grained, equigranular biotite tonalite crops out at this locality. The grid reference is based on the AGD66 datum.|16-MAY-23
26026|Melon Creek Tonalite|Extent|The Melon Creek Tonalite occurs to the east and northeast of Star homestead along Yarraman and Melon Creeks downstream to their junction with the Little Star River. It has an area of about 16 squared km.  It crops out very poorly and forms undulating sandy downs, generally more subdued and less dissected than the topography on the Argentine Metamorphics.  Outcrop is mostly restricted to very weathered material in gullies, but some fresher outcrops occur in the larger creeks, and rare boulders have been observed on the interfluves.|16-MAY-23
26026|Melon Creek Tonalite|Lithology|The Melon Creek Tonalite consists of grey, medium-grained, equigranular to seriate, biotite tonalite. The tonalite is weakly foliated, but insufficient outcrops were studied to determine a predominant trend; the foliation is defined by aligned quartz and biotite, and a mortar texture around aligned plagioclase laths is locally developed. No xenoliths were observed.  In thin section the tonalite contains aggregates up to 5 mm across of slightly strained quartz (20-25%); the subgrains are subequant with straight to curved interlocking margins. Plagioclase (60%) is Na-andesine, and forms subhedral laths, generally 1-2 mm long, but some up to 5 mm; they are generally unzoned, but some grains show weak oscillatory zoning; the twin lamellae are locally weakly deformed. K-feldspar is rare and interstitial. Biotite (10-20%) forms clumps of yellow-brown flakes up to 2 mm across, commonly containing pleochroic haloes and apatite inclusions; partial alteration to epidote and minor chlorite is present.|16-MAY-23
26026|Melon Creek Tonalite|Relationships and boundaries|The Melon Creek Tonalite intrudes the Argentine Metamorphics (subunits PLa[subscript]m and PLa[subscript]sa). It is overlain to the west by the Late Devonian to Carboniferous Keelbottom Group (formerly Star beds). To the north, it is overlain by the Carboniferous Tareela Volcanics; the contact is obscured by alluvium along the Little Star River, but is probably faulted.|16-MAY-23
26026|Melon Creek Tonalite|Age reasons|No isotopic data are available on the tonalite and its age is therefore uncertain. However, it is likely to be in the range Ordovician to Early Devonian like most of the components of the Ravenswood and Lolworth Batholiths in the southern part of the province (Hutton & others, 1990b).|16-MAY-23
37120|Melrose Igneous Complex|Name source|The unit is named after Melrose homestead, which is situated about 2km to the west of the complex.|16-MAY-23
37120|Melrose Igneous Complex|Unit history|The Melrose Igneous Complex comprises intermingled felsic to mafic coarse-grained intrusives and metamophics that was previously included within the Boondooma Igneous Complex by Murphy & others (1976).|16-MAY-23
37120|Melrose Igneous Complex|Geomorphic expression|The unit forms sparsely wooded low ridges and undulating hills ranging from 340m to 380m in elevation.|16-MAY-23
37120|Melrose Igneous Complex|Type section locality|The type area is designated as between AMG 366000 7091300 and 367200 7092000 near the intersection of Galbraith Creek and the Stuart River.  The grid reference is based on the AGD66 datum.|16-MAY-23
37120|Melrose Igneous Complex|Extent|The Melrose Igneous Complex forms a narrow belt extending south-east for about 8km from a position around 2km east of Melrose homestead, 14km south-south-east of Proston. The unit flanks the northeastern margin of the Stuart River Granite, covering an area of approximately 4km2.|16-MAY-23
37120|Melrose Igneous Complex|Lithology|The unit contains a variety of mostly mafic rock types, along with scattered granite phases and meta-sedimentary rafts.  The most typical mafic rock type is fine to medium grained, dark grey hornblende diorite which ranges in texture from equigranular to coarsely porphyritic (or megacrystic) in feldspar.  This rock type locally grades into microgranodiorite or more rarely dolerite.  The granitic component of the unit is lithologically similar to the Hivesville Granite, ranging from equigranular to coarsely megacrystic, in a quenched-fined grained matrix.  The metasedimentary rafts are mainly laminated siliceous or biotite gneiss, probably representing fragments of the nearby Fifer Creek Metamorphics.Near the Galbraith Creek-Stuart River confluence the unit is cut by north-west-trending steeply dipping mylonitic shear zones with a sinistral sense of shear.|16-MAY-23
37120|Melrose Igneous Complex|Relationships and boundaries|The complex intrudes the Fifer Creek Metamorphics and is .is intruded by Triassic diorite (Rgd), granodiorite (Rg3), and granite (Rg2) bodies, and probably also by the Permo-Triassic Stuart River Granite. The unit has an uncertain relationship with the Hivesville Granite and may be close to the same age.  The common occurrence of feldspar megacrysts (or porphyroblasts) in both units and the range of mafic to felsic compositions in the Melrose Igneous Complex suggest that the latter results from the admixture of mafic magmas with Hivesville Granite magmas along the western margin of the granite pluton.|16-MAY-23
37120|Melrose Igneous Complex|Age reasons|No radiometric dating of the unit has been undertaken, but parts of the unit have lithological similarities to the adjacent Hivesville Granite.  Consequently the Melrose Igneous Complex is thought to range from Permian to Triassic in age.|16-MAY-23
37120|Melrose Igneous Complex|Comments|GEOPHYSICAL EXPRESSION:: The unit has a low magnetic response on AIRDATA aeromagnetic images and occurs as dark mottled brown tones on AIRDATA RGB radiometric images.|16-MAY-23
37120|Melrose Igneous Complex|References|MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.|16-MAY-23
33428|Memerambi Granite|Name source|The unit is named after the township of Memerambi that is situated 5km to the west of the intrusion.|16-MAY-23
33428|Memerambi Granite|Unit history|Murphy and others (1976) mapped the unit as part of the Boondooma Igneous Complex.|16-MAY-23
33428|Memerambi Granite|Geomorphic expression|The unit forms sandy plains with occasional outcropping tors or low hills.|16-MAY-23
33428|Memerambi Granite|Type section locality|The type area is designated to be around AMG 395500 7073100, 13km east of Memerambi.|16-MAY-23
33428|Memerambi Granite|Extent|The unit occurs 15km NE of Kingaroy where it forms a roughly circular pluton covering around 130km2.|16-MAY-23
33428|Memerambi Granite|Lithology|The unit consists of cream to pale grey, medium to locally fine grained, inequigranular biotite - hornblende granite. In thin section, micrographic intergrowth textures are locally developed.  The mafic minerals occur as scattered fine clots making up to 4% of the rock except in the southern margin of the body where the mafic content ranges up to 7%. The granite contains sparse rounded fine-grained mafic xenoliths averaging 10cm across.  In the southern part of the unit it is deeply weathered medium grained biotite micrgranite with local mariolitic cavities.  Pits for sand extraction and decomposed granite pits are developed in the unit at AMG 394021 7070027, 394492 7069424 and 395737 7066488 respectively.  The unit is locally deeply weathered and at AMG 388663 7054760 the outcrop comprises strongly mottled microgranite and minor ferricrete.  The grid references are based on the AGD66 datum.|16-MAY-23
33428|Memerambi Granite|Relationships and boundaries|The Late Triassic Tarong beds, and Tertiary basalts of the Main Range Volcanics unconformably overlie the unit.  Extensive areas of Tertiary duricrust up to 10m thick are also developed on the granite.|16-MAY-23
33428|Memerambi Granite|Age reasons|No age dating of the pluton has been carried out.  The unit is thought to be Triassic in age, older than the overlying Late Triassic Tarong beds.|16-MAY-23
33428|Memerambi Granite|Comments|GEOPHYSICAL EXPRESSION: The unit has a moderately high magnetic response on RTP aeromagnetic images and displays strong pink tones on ternary radiometric images. MINERALISATION: According to local anecdotal communications, a small gold occurrence (the Wondi mine) is thought to occur within the granite on the west side of the Charlestown road at AMG 390860 7078650.  No record of production is known from the mine.  The grid references are based on the AGD66 datum.|16-MAY-23
33428|Memerambi Granite|References|MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.|16-MAY-23
24378|Meringa Basalt|Name source|Meringa railway station (GR 696115, Bartle Frere 1:100 000 Sheet area, 8063), 18 km south of Cairns, Queensland.|16-MAY-23
24378|Meringa Basalt|Unit history|Previously included in the Atherton Basalt by Best (1960) and de Keyser (1964).|16-MAY-23
24378|Meringa Basalt|Type section locality|Basalts of this unit crop out poorly and are highly to extremely weathered. Less weathered olivine basalt appears to be restricted to the southern flanks of the Green Hill cone (GR 733150, Bartle Frere 1:100 000 Sheet area) which is designated the type locality.|16-MAY-23
24378|Meringa Basalt|Extent|Green Hill volcanic cone (GR 731154, Bartle Frere 1:100 000 Sheet area, 8063) and its flanks, and in small deeply weathered inlier (GR 689119, Bartle Frere 1:100 000 Sheet area, 8063) near Meringa, which is possibly continuous to Green Hill. The total area of surface exposure is about 7 km2; the subsurface extent about 26 km2.|16-MAY-23
24378|Meringa Basalt|Lithology|The olivine basalt is fine-grained and porphyritic with small phenocrysts (2 mm) of olivine and subordinate augite; basaltic fragments or ejecta are distinguished by their finer texture and less altered olivine microphenocrysts. The steep sided Green Hill cone is composed of basaltic scoria. Flow structures are occasionally seen. Elsewhere, rocks of the unit are deeply weathered and have developed dark red to red-brown soils. In the Meringa area, the only surface evidence of the basalt is the presence of these dark soils and the slightly higher relief above the surrounding alluvial plain.|16-MAY-23
24378|Meringa Basalt|Relationships and boundaries|The Meringa Basalt is considered to represent one of the most recent phases of volcanic activity in the Atherton Volcanic Province. The Green Hill vent is the most obvious source for the basalt, but a second subsidiary vent is suggested by drillhole sections (Muller, 1978) near Meringa. Pleistocene alluvial deposits on basement rocks comprising metasediments of the Hodgkinson Formation and the Bellenden Ker Granite are unconformably overlain by the Meringa Basalt. Local erosion preceded subsequent sediment deposition by the Mulgrave River; the overlying sediments have a maximum thickness of 35 m (Muller, 1978).|16-MAY-23
24378|Meringa Basalt|Age reasons|A whole rock isotopic date on basalt (DA 1) from Green Hill resulted in a date of 0.986 x 106 m.y. (Pleistocene; Muller & Henry, 1982).|16-MAY-23
24378|Meringa Basalt|Proposed publication|1:100 000 Geological Map Commentary, Cairns Region, Queensland. Geological Survey of Queensland.|16-MAY-23
24378|Meringa Basalt|Category|2|16-MAY-23
11776|Mick Creek Sandstone Member|Name source|Little Mick Creek in the southwest corner of the Cloncurry 1:100 000 Sheet area, latitude 20o59'10"S, longitude 140o36'E (7056 585785).|16-MAY-23
11776|Mick Creek Sandstone Member|Geomorphic expression|The member forms moderately high ridges and plateaux.|16-MAY-23
11776|Mick Creek Sandstone Member|Type section locality|Near Robur mine, 27 km south-southeast of Cloncurry, from latitude 20o57'24"S, longitude 140o33'E (base), to latitude 20o56'48"S, longitude 140o33'48"E (7056 537828 to 7056 544838). The base is defined by contact with underlying black to grey slate, but the top is placed in the core of a small syncline; contacts with overlying units are not present in the type section, which contains a minimum thickness of 500 m of mainly fine-grained feldspathic sandstone.|16-MAY-23
11776|Mick Creek Sandstone Member|Extent|The member outcrops in a northwest-trending belt about 20 km long and 3 km wide about 25 km south of Cloncurry; the main outcrops are in the southwest corner of the Cloncurry 1:100 000 Sheet area, and it extends into the Marraba 1:100 000 Sheet to the west, and into the northwest corner of the Mount Angelay 1:100 000 Sheet area to the south.|16-MAY-23
11776|Mick Creek Sandstone Member|Thickness range|The thickness is difficult to determine because of the structural complexity, but a minimum thickness is about 500 m.|16-MAY-23
11776|Mick Creek Sandstone Member|Lithology|Flaggy to blocky fine to medium sandstone and quartzite; heavy-mineral banding, ripple marking and cross-bedding are common; minor pebble conglomerate, friable ferruginous sandstone and limestone.|16-MAY-23
11776|Mick Creek Sandstone Member|Relationships and boundaries|This member appears to be a conformable lens at the top of the Marimo Slate; it conformably overlies black slate of the lower part of the Marimo Slate and is unconformably overlain locally by breccia of the Corella Formation.|16-MAY-23
11776|Mick Creek Sandstone Member|Unit name|Mick Creek Sandstone Member of the Marimo Salte|16-MAY-23
25235|Middle Creek Sandstone Member|Type section locality|Lawn Hill 4-mile sheet - E54/9. Along the watercourse of Middle Creek at lat. 18° 15'10" S, long. 138° 14'10" E, for distance of one third of a mile.|16-MAY-23
25235|Middle Creek Sandstone Member|Defn author|E.K. Carter & D.C. Zimmerman, 1960. Constance Range iron deposits, north-western Queensland. BMR Record 1960/75, p10-15.|16-MAY-23
11912|Mingoom Granite|Name source|Name derived from Mingoom Hill, a peak about 7km west of south-west of Thronton Gap in ROLLINGSTONE.|16-MAY-23
11912|Mingoom Granite|Unit history|The unit was previously part of Wyatt & others (1970) unnamed CPg unit. They noted that 'drusy, chloritised leucocratic granite and microgranite formed Mingoom Hill and extended several miles west across Keelbottom Creek'. Mingoom Hill, from which the name is derived, is a peak about 7km west south-west of Thornton Gap in ROLLINGSTONE.|16-MAY-23
11912|Mingoom Granite|Geomorphic expression|The topography is rugged and sides of the hills are very steep. On top of the ridges, bouldery outcrop and tors are prevalent.|16-MAY-23
11912|Mingoom Granite|Type section locality|The type area is 2km west of Glen Haven Homestead (8159-385559) on the eastern side of the pluton.  The grid reference is based on the AGD66 datum.|16-MAY-23
11912|Mingoom Granite|Description at type locality|Pink, medium-grained equigranular biotite granite is exposed in this area.|16-MAY-23
11912|Mingoom Granite|Extent|The Mingoom Granite lies to the north and north-east of Ben Lomond East and forms an elongate, east-trending body, 12km long, up to 3.5km wide and approximately 25km2 in area. It is a resistant unit rising up to 335m above the surrounding area.|16-MAY-23
11912|Mingoom Granite|Lithology|The Mingoom Granite is a pink, predominantly medium-grained, equigranular biotite granite.|16-MAY-23
11912|Mingoom Granite|Relationships and boundaries|The Mingoom Granite intrudes the Tareela Volcanics, Saint Giles Volcanics and the Speed Creek Granite. On its southern boundary it is faulted against the Insolvency Gully Formation, the Watershed North Rhyolite and a mafic unit of the Tareela Volcanics. Along most of its northern boundary it has been intruded by rhyolite.|16-MAY-23
11912|Mingoom Granite|Age reasons|A U-Pb zircon (SHRIMP) age of 283 ± 4 on a sample from the Speed Creek Granite (Appendix 1) suggests that the Mingoom Granite is also Early Permian.|16-MAY-23
11912|Mingoom Granite|References|WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127|16-MAY-23
27198|Mistletoe Granite|Name source|"Mistletoe" Homestead, 7.5 km northeast of Georgetown at GR 736 816 (Georgetown 1:100 000 Sheet area).|16-MAY-23
27198|Mistletoe Granite|Unit history|Previously mapped as Forsayth Granite (White, 1962c).|16-MAY-23
27198|Mistletoe Granite|Type section locality|Georgetown-Ironhurst road for about 3 km south from Quartz Blow Creek. Typical "gneissic", medium even grained muscovite-biotite granite with abundant biotite schlieren and xenoliths of schist, gneiss, leucogranite and quartz is exposed at GR 691 812 about 200 m south of Boggy Creek and 100 m east of the road.|16-MAY-23
27198|Mistletoe Granite|Extent|Numerous small irregular bodies on Mistletoe Holding between Georgetown and the outstation on Fiery Creek (GR 802 919). Similar rocks are found further south between the Etheridge River and Lighthouse Creek.|16-MAY-23
27198|Mistletoe Granite|Lithology|Medium even grained muscovite-biotite granite grading into granodiorite; characterised by the presence of biotite-rich schlieren and numerous xenoliths of quartzite, amphibolite, quartz and leucogranite; commonly foliated.|16-MAY-23
27198|Mistletoe Granite|Relationships and boundaries|Intrusive into the Proterozoic Robertson River Metamorphics and Einasleigh Metamorphics. Intruded by the Proterozoic Forsayth Granite and Talbot Creek Granodiorite.|16-MAY-23
27198|Mistletoe Granite|Age reasons|Proterozoic; as indicated by above cited relationships.|16-MAY-23
27198|Mistletoe Granite|References|01/31334|16-MAY-23
25245|Mitakoodi Quartzite|General description|In the Marraba 1:100 000 Sheet area, Derrick et al. (1971) delineated three units within the Mitakoodi Quartzite as defined by Carter et al. (1961). The basal unit is a thick sequence of feldspathic quartzite, and the top unit consists of fine sandstone, siltstone and slate. At and near the top of the basal unit, several minor sequences of basic lava are present; the topmost and most prominent of these is defined as the Wakeful Metabasalt Member of the Mitakoodi Quartzite. The other sequences are not formally named.|16-MAY-23
25245|Mitakoodi Quartzite|Relationships and boundaries|The relation between the Mitakoodi Quartzite and younger formations also needs revision as a result of the detailed mapping. Carter et al. (1961) state that the Mitakoodi Quartzite is overlain conformably by the Marimo Slate (p.77) and the Answer Slate (p.82) in the east, and is overlain apparently conformably, by the Corella Formation (p.77) in the north. The Mitakoodi Quartzite was considered to be overlain, apparently conformably, by the Overhang Jaspilite (Derrick et al., 1971) which has been mapped as part of the Mary Kathleen Group in the Marraba and Mary Kathleen sheet areas, and is known to extend into adjoining Sheet areas to the south. The upper contact of the Overhang Jaspilite is currently being studied in more detail.|16-MAY-23
25245|Mitakoodi Quartzite|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1977. Approved H.R.E. Staines 5-JUL-1976.|16-MAY-23
25245|Mitakoodi Quartzite|Proposed publication|Queensland Government Mining Journal, 1976.|16-MAY-23
25245|Mitakoodi Quartzite|References|Carter, E.K., Brooks, J.H., Walker, K.R., 1961. The Precambrian mineral belt of north-western Queensland. Bureau of Mineral Resources, Bulletin 51. **Derrick, G.M., Wilson, I.H., Hill, R.M., Mitchell, J.E., 1971. Geology of Marraba 1:100 000 sheet area, Qld. Bureau of Mineral Resources, Record 1971/56. **Derrick, G.M., Wilson, I.H., Hill, in prep [1976] Revision of stratigraphic nomenclature in the Precambrian of northwestern Queensland. IV: Malbon Group.|16-MAY-23
25245|Mitakoodi Quartzite|Status|1|16-MAY-23
11980|Mitchell River Volcanics|Lithology|Slightly to moderately porphyritic rhyolite and dacite (commonly flow-banded); welded rhyolitic ignimbrite; slightly to moderately porphyritic andesite; mainly massive, fine-grained moderately to highly porphyritic basalt to andesite; laminated to thick-bedded rhyolitic tuff, lapilli tuff and volcanic claystone, siltstone, sandstone and conglomerate;|16-MAY-23
12115|Monsildale Granodiorite|Name source|Monsildate Creek (GR 5510 6850), Gympie 1:250 000 Sheet area, SG 56-10. The name was first published by Brooks (1971).|16-MAY-23
12115|Monsildale Granodiorite|Type section locality|Between Monsildale Homestead, GR 5520 6845 and the western edge of the intrusion where Monsildate Creek enters the outcrop area at GR 5502 6850.|16-MAY-23
12115|Monsildale Granodiorite|Extent|The unit covers 15 km2 in the southern centralpart of the Gympie 1:250 000 Sheet area SG 56-10.|16-MAY-23
12115|Monsildale Granodiorite|Lithology|Medium-grained, grey, hornblende-biotite granodiorite, and olivine gabbro varying to hornblende diorite to granodiorite. Orbicular gabbro is also present.|16-MAY-23
12115|Monsildale Granodiorite|Relationships and boundaries|The unit intrudes the Lower Permian Marumba Beds.|16-MAY-23
12115|Monsildale Granodiorite|Age reasons|A K/Ar radiometric age of 248 m.y. was obtained from the unit. A Permo-Triassic age is assigned to the intrusion.|16-MAY-23
12115|Monsildale Granodiorite|Proposed publication|Report of the Geological Survey of Queensland|16-MAY-23
24385|Monte Christo Member|Name source|Monte Christo Creek; GR 306,000E, 7,387,000N, Gladstone 1:100 000 topographic sheet.|16-MAY-23
24385|Monte Christo Member|Unit history|Part of The Narrows Beds (Kirkegaard et al, 1970) and part of the Rundle Formation (Henstridge and Missen, 1982).|16-MAY-23
24385|Monte Christo Member|Type section locality|224 m of claystone and oil shale with minor sandstone, impure dolomite and coaly bands; from 323.8 to 548 m in drill hole GSQ Rockhampton 2 (Noon, 1981), which is part of the type section of the  Rundle Formation. GSQ Rockhampton 2 is locatead at GR 313,210E, 7,363,665N, Gladstone 1:100 000 topographic sheet. The Monte Christo Member contains two major oil shale sections (from 382 to 454 m and from 488 to 538 m in type section) where the oil shale is interbedded with claystone. The basal part of the member contains minor siltstone and sandstone beds.|16-MAY-23
24385|Monte Christo Member|Extent|Subcrops in an area of about 110 km2 in The Narrows Graben, N.W. of Gladstone, Queensland. Sparse, weathered outcrops are recorded. The member has been identified from drill hole core.|16-MAY-23
24385|Monte Christo Member|Thickness range|224.2 m (estimated true thickness 220.1 m corrected for an apparent dip of 11o in GSQ Rockhampton 2 in type section   ?????  2 is the only drill hole to have intersected the Monte Christo Member.       |16-MAY-23
24385|Monte Christo Member|Lithology|Oil shale and claystone; the oil shale is dark to moderate yellowish-brown with olive gradations. Claystone beds are light olive-grey to greenish-grey and in places can be silty or sandy. Part of the member is very calcareous and in places there are discontinuous impure dolomite beds (up to 1.1 m thick) and very thin coaly bands. Cyclicity of rock types within the member is common; breccias and peloids are abundant. In places the member is richly fossiliferous; with mainly ostracode tests, occasional gastropods, fish elements and other rare vertebrate macrofossils. Claystone and brecciated clayey oil shale beds arae often bioturbated, showing well-preserved burrows in places. Desiccation features are common with current bedding being recorded in sandy units. To the east within The Narrows Graben, sandy beds within the member increase in number and thickness and there are interbeds of red haematitic claystone.|16-MAY-23
24385|Monte Christo Member|Relationships and boundaries|The member is conformable with the underlying Worthington formation and is the contact between oil shale and claystone. The upper contact is the conformable contact between claystone and oil shale of the Teningie Creek Member. The member is faulted against Devonian to Carboniferous rocks of the Curtis Island along the western edge of The Narrows Graben.|16-MAY-23
24385|Monte Christo Member|Age reasons|Mid to late Eocene - as for the Rundle Formation.|16-MAY-23
24385|Monte Christo Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24385|Monte Christo Member|Comments|Note: Drill-core from GSQ Rockhampton 2 is stored at the Queensland Department of Mines Core Library located in Brisbane, Queensland.|16-MAY-23
24385|Monte Christo Member|Proposer|Henstridge D.A., Coshell L.|16-MAY-23
24385|Monte Christo Member|Resdate|15-DEC-1983|16-MAY-23
12129|Monteagle Quartzite|Name source|Monteagle Holding (Monteagle 1:100 000 Cadastral Series map).|16-MAY-23
12129|Monteagle Quartzite|Unit history|Previously mapped as Anakie Metamorphics (Malone & others, 1964; Veevers & others, 1964a, b) and now part of the Anakie Metamorphic Group  .|16-MAY-23
12129|Monteagle Quartzite|Geomorphic expression|The Monteagle Quartzite is distinguishable on Landsat 5 TM bands 1-4-7 (BGR) images by a green colour which contrasts with the purplish colour of the Rolfe Creek Schist. A dark green tone is in part due to the relatively dense vegetation, which is characteristic of the unit and also a useful distinguishing feature on aerial photographs. Strike ridges outlining the gross bedding trends are also common, because of the resistance of the quartzite beds.   On the geophysical radiometric images, the Monteagle Quartzite is generally lower in K and Th than the adjacent Rolfe Creek Schist and Wynyard Metamorphics. It has a very low magnetic response.|16-MAY-23
12129|Monteagle Quartzite|Type section locality|Along the Clermont-Laglan road from 8352-381919 (the boundary with the Rolfe Creek Schist) to 361937, and thence along the boundary fence between Monteagle and Moorlands Stations from 338930 to 328850.   The grid references are based on the AGD66 datum.|16-MAY-23
12129|Monteagle Quartzite|Description at type locality|Phyllite and meta-arenite, correlated with the Wynyard Metamorphics, crops out 1 km farther south, but the boundary with the Monteagle Quartzite is obscured by a belt of Cainozoic cover.|16-MAY-23
12129|Monteagle Quartzite|Extent|Crops out in the western part of the Clermont area as a sinuous belt up to 8 km wide. The belt extends from the northern edge of MONTEAGLE for about 90 km south to the Zig Zag Range, where it is truncated by the Retreat Batholith. Another belt surrounded by Rolfe Creek Schist, north of Karmoo homestead, is tentatively assigned to the Monteagle Quartzite. To the north of MONTEAGLE, the unit is overlain by Cainozoic deposits. Outliers of quartzite in FRANKFIELD may be correlatives of the Monteagle Quartzite.|16-MAY-23
12129|Monteagle Quartzite|Lithology|Characterised by abundant outcrop of quartzite, although because of the relative resistance of quartzite to weathering compared with the interbedded schist, its actual abundance overall may be less than 50% of the total unit. The quartzite is white to pale greyish brown in outcrop, fine to very coarse-grained, and medium to very thick-bedded. Mica schist forms thin to thick interlayers with the quartzite. Metamorphic grade ranges from greenschist (biotite zone) to lower amphibolite facies.|16-MAY-23
12129|Monteagle Quartzite|Relationships and boundaries|The Monteagle Quartzite structurally overlies the Rolfe Creek Schist to the east, and is structurally overlain by the Wynyard Metamorphics to the west, although it is uncertain whether the boundaries are actually stratigraphic. Quartzite and schist cropping out west of the Wynyard Metamorphics to the south of the Barcaldine powerline are tentatively correlated with the Monteagle Quartzite, although there is little data available in this area. If these rocks are Monteagle Quartzite, they may have been repeated by thrusting or folding, or alternatively, the Wynyard Metamorphics may represent a more labile member within the quartzite-rich lithofacies represented by the Monteagle Quartzite.   The Monteagle Quartzite is intruded by the various plutons of the Devonian Retreat Batholith and is overlain unconformably by the Devonian-Carboniferous Silver Hills Volcanics and various Cainozoic deposits.|16-MAY-23
12129|Monteagle Quartzite|Age reasons|The original age is still uncertain, but is probably Early Cambrian or Neoproterozoic.|16-MAY-23
12129|Monteagle Quartzite|References|MALONE, E.J., CORBETT, D.P.W., & JENSEN, A.R., 1964: Geology of the Mount Coolon 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 64.VEEVERS, J.J., RANDAL, M.A., MOLLAN, R.G., & PATEN, R.J., 1964a: The geology of the Clermont 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report, 66.VEEVERS, J.J., MOLLAN, R.G., OLGERS, F., & KIRKEGAARD, A.G., 1964b: The geology of the Emerald 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 68.|16-MAY-23
12136|Montgomery Range Igneous Complex|Name source|Montgomery Range, which is part of the Great Dividing Range southwest of 'Pandanus Creek'.|16-MAY-23
12136|Montgomery Range Igneous Complex|Unit history|Branch (1966) and White (1959, 1962, 1965) mapped the rocks as the Montgomery Range Rhyolite Porphyry.  Because of the wide range of rock types, the name was changed to Montgomery Range Igneous Complex by Withnall & others (1988).  It was decided not to give separate names to the plutons, because of a shortage of available names in the area, and the lack of detailed studies.  It would be possible to separately name some of the larger plutons with more detailed work.|16-MAY-23
12136|Montgomery Range Igneous Complex|Geomorphic expression|The rocks generally form rugged, boulder-strewn hills with up to 150 m of relief.|16-MAY-23
12136|Montgomery Range Igneous Complex|Type section locality|White (1959) gave the type area as Montgomery Range, which is the northeastern half of the belt. This includes most of the range of the rock types, as well as the Bundock Creek Group, which is intruded by them.|16-MAY-23
12136|Montgomery Range Igneous Complex|Extent|Numerous intrusions from 'Pandanus Creek' southwest to 'Blackbraes' in a belt 50 km long and 20 km wide.|16-MAY-23
12136|Montgomery Range Igneous Complex|Lithology|Fine to medium-grained, equigranular to porphyritic, biotite granite, biotite-hornblende granite and granodiorite, microgranite, and granophyre.  These form stocks up to 40 km2 in area.  Numerous sills of rhyolite and some microgranite up to 100 m thick, and dykes of rhyolite and less common dacite, are also included in the Complex.|16-MAY-23
12136|Montgomery Range Igneous Complex|Age reasons|The sills are probably of Early Carboniferous age, because they intrude the Teddy Mount Formation, and were folded by the main mid(?) Carboniferous folding event.  The later plutons are probably Late Carboniferous or Permian.|16-MAY-23
12136|Montgomery Range Igneous Complex|References|BRANCH, C.D., 1966:  Volcanic cauldrons, ring complexes, and associated granites of the Georgetown Inlier, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 76.WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.WHITE, D.A., 1962:  Clarke River - Qld E/55-13.  Bureau of Mineral 	Resources, Australia 1:250 000 Geological Series Explanatory Notes.WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.D., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
23805|Mooramin Granite|Name source|Mooramin homestead at 8452-879058.   The grid reference is based on the AGD66 datum.|16-MAY-23
23805|Mooramin Granite|Geomorphic expression|The unit forms undulating terrain with incised gullies and scattered pavement outcrops affording the best exposures. The unit is typically highly jointed and moderately weathered. It has pale yellow to pinkish hues on the Landsat 5 TM (1-4-7 BGR) image. The highly sheared portion in the northwest quadrant, however, forms hilly, dissected topography, and has darker tones on the Landsat images due to denser vegetation.|16-MAY-23
23805|Mooramin Granite|Type section locality|Track crossing of a gully at Wildhorse Springs at 8452-961085.  The grid reference is based on the AGD66 datum.|16-MAY-23
23805|Mooramin Granite|Description at type locality|At type location, grey, fine to medium-grained foliated and locally sheared biotite-muscovite granite contains numerous biotite schist and quartz xenoliths.|16-MAY-23
23805|Mooramin Granite|Lithology|Grey to brown-grey, fine to medium-grained foliated and locally mylonitised cordierite-bearing muscovite-biotite granite. The granite hosts numerous biotite-rich schlieren and metasedimentary xenoliths of dominantly biotite schist and quartzite as well as quartz. The northwestern quarter of the unit, as mapped, is highly sheared and has been converted to mica schist. It also includes migmatitic phases.|16-MAY-23
23805|Mooramin Granite|Relationships and boundaries|The Mooramin Granite forms the core of the uplifted Fletchers Awl Dome. Shallow marine sediments and predominantly subaerial, intermediate lavas and volcaniclastic rocks of the Greybank Volcanics unconformably overlie the Mooramin Granite on all sides. One large (0.75 km2) and two smaller (<0.1 km2) serpentinised ultramafic bodies are hosted by the granite.  At one locality, a dyke of granite appears to intrude the serpentinite, and therefore the ultramafic bodies are thought to represent roof pendants/rafts of country rock. However, the possibility of them being later and emplaced along a structural weakness has not been entirely excluded.|16-MAY-23
23805|Mooramin Granite|Age reasons|The age is uncertain. Fossils in the basal sedimentary sequence of the overlying Greybank Volcanics are Late Devonian. Being an S-type granite, it could have been sourced from the Anakie Metamorphic Group during the Middle to Late Cambrian deformation and metamorphism.|16-MAY-23
24386|Moorooloo Mudstone Member|Name source|The name is derived from Moorooloo Station, located 18 km east of Springsure, Springsure 1:250 000 Sheet area.|16-MAY-23
24386|Moorooloo Mudstone Member|Unit history|The Moorooloo Mudstone Member was formally referred to as the Middle Mudstone Member of the Cattle Creek Formation by Power (1966). Mollan & others (1969) included the unit in the Stanleigh Formation of Phillips (1960).|16-MAY-23
24386|Moorooloo Mudstone Member|Type section locality|The type section (holostratotype) of the Moorooloo Mudstone Member is taken as the fully cored interval between 296 m and 394 m in stratigraphic bore GSQ Springsure 16, located at 24o02'36"S, 148o13'30"E. The lowermost 35 m of the type section consist of dark grey mudstone. It is laminated and even-grained near the base and slightly siltier higher up, with rare thin siltstone beds near the top. About 40 m above the bottom of the unit rounded masses of brown calcareous mudstone, some with crystalline calcite cores, are common. Higher in the section mudstone becomes gradually more silty and lighter coloured, and the proportion of siltstone increases. The coarser material is commonly calcareous. In the top half of the unit siltstone is the dominant lithology, withy mid to dark grey silty mudstone less common. The siltstone and silty mudstone are both pyritic. The sediments are bioturbated in part, and well-preserved burrows are common. Near the top, siltstone grades in places to light grey sandstone, which is fine to medium grained, fairly to poorly sorted, sublabile to labile, and has an argillaceous matrix.  Reference section: The composite cored section obtained by overlap in stratigraphic bores GSQ Springsure 7 (located at 24o16'S; 148o14'E) from 213 m to 457 m (total depth) and GSQ Springsure 8 (located at 24o16'S; 148o13'E) from 144 m to 150 m (Gray, 1976) is nominatead as a reference section (hypostratotype) for the Moorooloo Mudstone Member. This section is considerably thicker than the type section. The lowermost 193 m of the reference section comprises dark grey to black shale and siltstone (partly sandy), and minor mudstone. Limestone fragments, calcareous fossil remains, and scattered quartz pebbles occur throughout. Beds of brown-grey, iron-rich siltstone, and beds rich in pyrite occur in the lowermost 110 m. The uppermost 57 m of the unit comprise approximately equal amounts of fine, labile to sublabile sandstone and laminated, mid to dark grey shale and siltstone. Carbonaceous plant remains occur throughout.|16-MAY-23
24386|Moorooloo Mudstone Member|Extent|Surface: The unit crops out very poorly. Weathered discontinuous outcrop occurs in Springsure Creek on Mostyndale. In Little Oaky Creek, on Moorooloo station, it is represented by a section of no outcrop stratigraphically below the outcropping Staircase  Sandstone Member.  Sub-surface: The Moorooloo Mudstone Member was intersected in stratigaraphic bores GSQ Springsure 7 and 8, drilled on Orion Creek about 20 km southeast of Springsure (Gray, 1976) and in GSQ Springsure 16 drilled 16 km northeaast of Springsure (Balfe, 1982). The unit was intersected in the petroleum exploration wells HOM Fernless 1, AFO Arcturus 1, and AFO Inderi 1. In AOE 1 (Reids Dome) and AOE 2 (Reids Dome), sandstone occurs in a position stratigraphically similar to the Riverstone Sandstone Member, but the continuity of these sandstone intervals has not been demonstrated and their equivalence is not proven. The Moorooloo Mudstone Member is therefore only tentatively identified in Reids Dome. South of Reids Dome, east of the Arcturus Anticline, and in the Consuelo Anticline, the Moorooloo Mudstone Member cannot be differentiated from the underlying Mostyndale Mudstone Member, since the Riverstone Sandstone Member is absent.|16-MAY-23
24386|Moorooloo Mudstone Member|Thickness range|Thickness of the Moorooloo Mudstone Member ranges from a maximum of 250 m in GSQ Springsure 7 and 8, to a minimum of 46 in HOM Fernless 1. The type section is 98 m thick. The unit is 99 m thick in AFO Arcturus 1 and 104 m thick in AFO Inderi 1.|16-MAY-23
24386|Moorooloo Mudstone Member|Lithology|The Moorooloo Mudstone Member consists mainly of dark grey mudstone which grades upward into siltstone and fine grained sandstone. At outcrop, the mid to dark grey mudstone contains large silty, calcareous concretions, and some beds of brown, fine-grained sandstone occur.|16-MAY-23
24386|Moorooloo Mudstone Member|Fossils|Marine fossils occur throughout the unit, but in the type section are most common towards the base. The fauna is dominated by brachiopods, with some bivalves, bryozoans, large foraminifera, and crinoid fragments. In GSQ Springsure 7, large foraminifera are common towards the top of the unit. As in the Mostyndale Mudstone Member, the range of these unusual fossils is apparently restricted to the siltier parts of the unit. The observed fauna is consistent with an Early Permian age.|16-MAY-23
24386|Moorooloo Mudstone Member|Relationships and boundaries|The Moorooloo Mudstone Member conformably overlies the Riverstone Sandstone Member, and is conformably overlain by the Staircase Sandstone Member of the Cattle Creek formation. The lower boundary of the type section is taken at the base of the monotonous dark grey mudstone, which directly overlies a 3 m thick, sandy, bioturbated transitional bed. The upper boundary is placed immediately below the first thick sandstone bed above the predominantly silty section.|16-MAY-23
24386|Moorooloo Mudstone Member|Identifying features|Wireline logs: The gamma-ray log shows many high frequency, low amplitude variations, and a response which gradually decreases upwards as a result of grain size increase. The resistivity log has a particularly distinctive 'wine glass' shape which also reflects the gradual upward increase in grain size.|16-MAY-23
24386|Moorooloo Mudstone Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24386|Moorooloo Mudstone Member|Proposer|Balfe P.E.|16-MAY-23
12305|Mopunga Group|Name source|From Mopunga Range in western HUCKITTA.|16-MAY-23
12305|Mopunga Group|Unit history|Approximately equivalent to Mopunja beds and Mopunja series of Tindale (1931). Group name coined by Noakes (1956) without constituent formations. Redefined by Smith (1964) to include Elyuah Formation (with Oorabra Arkose Member), Grant Bluff Formation (equivalent to present Grant Bluff Formation and Elkera Formation) and Mount Baldwin Formation as then understood (equivalent to present Mount Baldwin Formation, Red Heart Dolostone and possible Thorntonia Limestone). Further redefined by Walter (1980) to include all above listed constituent units other than Andagera Formation. Andagera Formation is added following its correlation by Haines et al (1991) with Central Mount Stuart Formation.|16-MAY-23
12305|Mopunga Group|Constituents|Gnallan-a-Gea Arkose, Elyuah Formation, Grant Bluff Formation, Elkera Formation, Central Mount Stuart Formation, Andagera Formation.|16-MAY-23
12305|Mopunga Group|Extent|MOUNT PEAKE, NAPPERBY, BARROW CREEK, ALCOOTA, HUCKITTA, TOBERMORY, HAY RIVER, MOUNT WHELAN.|16-MAY-23
12305|Mopunga Group|Relationships and boundaries|Overlies Wonnadinnna Dolostone with inferred disconformity, and Oorabra Arkose (both of Keepera Group) with disconformity or slight angular unconformity; where these are absent, unconformable on Palaeoproterozoic rocks. Disconformably overlain by Mount Baldwin Formation and Octy Formation or where these are absent, Red Heart Dolostone (all of Shadow Group) or Thorntonia Limestone and Gum Ridge Formation (both of Narpa Group).|16-MAY-23
12305|Mopunga Group|Age reasons|Stratigraphic position above Marinoan-equivalent glacigene units and below fossiliferous Cambrian units indicates terminal Neoproterozoic age. Ediacara fauna in Central Mount Stuart Fomation and ichnofossil fauna of simple horizontal trails in Grant Bluff, Elkera and Central Mount Stuart Fomations are consistent with this age assignment.|16-MAY-23
12305|Mopunga Group|Correlations|Pertatataka Formation, Julie Formation and Arumbera Sandstone I and II of Amadeus Basin, Yuendumu Sandstone I of Ngalia Basin.|16-MAY-23
12305|Mopunga Group|Comments|(Orig. Defn) The Mopunga Group of Noakes (1957) as redefined by Smith (1964) is here redefined. In Smith's definition it comprised the Elyuah, Grant Bluff and Mt Baldwin Formations. Major unconformities are now recognised between the  Elyuah Formation sensu stricto and its former member, the Oorabra Arkose, and between the Elkera Formation (former upper Grant Bluff Formation) and the Mount Baldwin Formation. The name Mopunga Group is here applied to the unconformity-bounded tectosome comprised of the following formations: Gnallan-a-gea Arkose, Elyuah Formation, Grant Bluff Formation, Elkera Formation and Central Mount Stuart Formation (excluding the basal diamictite). This definition retains the name for the bulk of the units previously included, and extends its use laterally from the Huckitta Sheet onto the Tobermory, Hay River, Mt Whelan, Alcoota Barrow Creek and Mt Peake 1:250 000 Sheet area.|16-MAY-23
12305|Mopunga Group|State(s)|NT|16-MAY-23
12359|Mort Member|Name source|From Mort River (140o10'E, 22o05'S) Boulia 1:250 000 Sheet area.|16-MAY-23
12359|Mort Member|Unit history|Generally equates with Unit 4 of Casey (1968), The Breccia Member of Jones et al (1971) and Member (iii) of Druce (1976).|16-MAY-23
12359|Mort Member|Type section locality|Black Mountain (140o17'E, 22o32'S), the interval between 371 m and 500 m within the Ninmaroo Formation from 257090 (140o16'35"E, 22o31'30"S) to 251094 (140o16'15"E, 22o31'15"S).|16-MAY-23
12359|Mort Member|Extent|The unit is exposed in a 95 km belt from Mt Datson in the south to the Swift Hills in the north, Boulia 1:250 000 Sheet area.|16-MAY-23
12359|Mort Member|Thickness range|130m at Black Mountain; 104 m+ at N. end of Swift Hills, 60 m at Digby Peaks; 40 m at Mt Datson; 120 m at Mt Ninmaroo.|16-MAY-23
12359|Mort Member|Lithology|Dominantly thin bedded, flat-pebble limestone conglomerates also called clast grainstone (Dunham, 1962), and intraformational breccia, peloidal (pellet-like) ooid and peloidal clast grainstone; micrite, peloidal grainstone, stromatolitic biostromes. Clast grainstones are formed from exfoliation of algal mounds and the breakup of 'hard ground' during high energy periods.|16-MAY-23
12359|Mort Member|Relationships and boundaries|The unit conformably overlies the Jiggamore Member and is conformably overlain by the Corrie Member. The unit is characterised by the preponderance of flat-pebble limestone conglomerates (intraclast grainstones).|16-MAY-23
12359|Mort Member|Age reasons|The unit contains conodonts and nautiloids: the conodonts indicate an Early Ordovician (early Warendian) age (Druce & Jones, 1971).|16-MAY-23
12359|Mort Member|Defn author|Druce E.C., 1978|16-MAY-23
12359|Mort Member|Proposed publication|BMR Publication, BMR 1:100 000 Special - The Southern Burke River Structural Belt|16-MAY-23
24387|Mostyndale Mudstone Member|Name source|The name is derived from Mostyndale Holding, 13 km north-northeast of Springsure, on the Springsure 1:250 000 Sheet area.|16-MAY-23
24387|Mostyndale Mudstone Member|Unit history|The Mostyndale Mudstone Member was informally referred to as the Lower Mudstone Member of the Cattle Creek Formation by Power (1966). Mollan & other (1969) included the unit in the Stanleigh Formation on Phillips (1960).|16-MAY-23
24387|Mostyndale Mudstone Member|Type section locality|The type section (holostratotype) of the Mostyndale Mudstone Member is defined as a composite section from the cored stratigraphic bores GSQ Springsure 8 and 9. These holes were drilled on Orion Creek at 24o16'S; 148o13'E and 24o16'; 148o12'E respectively (Gray, 1976). The lowermost 178 m of the unit is represented by the interval 32 to 210 m in GSQ Springsure 9, and the uppermost 71 m by the interval 273 to 344 m in GSQ Springsure 8. Total thickness of the type section is 249 m. The lowermost 78 m of the type section comprise sandstone (53 percent) interbedded with shale, mudstone, and siltstone (47 percent). The sandstone is light grey, very fine to fine grained and in part silty, and is labile with an argillaceous and calcareous matrix. Bedding is commonly destroyed by bioturbation. The sandstone contains shell fossils and plant remains. Mudstone clasts and calcite veining are common. Shale, mudstone and siltstone are grey to black and sandy, with carbonised plant fragments, fossil shells, and pyritic nodules. The upper 171 m of the type section comprise dark grey to black mudstone and shale with minor siltstone. Fossil shells, pyritic nodules, limestone fragments, and iron-rich, ?sideritic siltstone beds (up to 0.3 m thick) occur throughout. Reference section: Two reference sections (hypostratotypes), one a composite cored section, and the other a reasonably well-exposed outcrop section, are nominated for the Mostyndale Mudstone Member. 1. The cored section in GSQ Springsure 15 (located at 24o02'54"S; 148o11'15"E) from surface to 266 m, and in GSQ Springsure 16 (located at 24o02'36"S; 148o13'30"E) from 584 to 897 m (total depth) provide a complete, overlapping section of the Mostyndale Mudstone Member. Because the overlap occurs in a monotonous shaly sequence, precise correlation between these two bores is more difficult to establish than in the type section. The only major lithological difference between this reference section and the type section occurs in the lower part of the unit, which in the reference section is composed mostly of silty mudstone, with two isolated sandstone intervals. In the type section, the corresponding interval is considerably more sandy.  2. The outcrop reference section is located in Springsure Creek, on Mostyndale, between GR 637006 and 638007 on the Springsure 1:250 000 Sheet. The section, which comprises several individual outcrops with intervening intervals of no exposure, is dominated by blue-grey silty mudstone, in part ferruginised, with beds of burrowed, sandy siltstone. Fine, calcareous grains occur in both siltstone and mudstone. Scattered granules and pebbles occur at some levels, and sandstone stringers are common. Red-brown concretions up to 0.5 m in diameter occur in one outcrop. Gypsum, probably of pedogenic origin, occurs in sheet-like beds up to 15 mm thick.|16-MAY-23
24387|Mostyndale Mudstone Member|Extent|Surface: Crops out very poorly, with exposures generally discontinuous and deeply weathered. Incomplete exposures occur in Springsure Creek on Mostyndale; in a small, southerly flowing gully 2 km northeast of Stanleigh homestead; and in a tributary of Minerva Creek, approximately 2.5 km east of Crystal Plains homestead. Subsurface: The Mostyndale Mudstone Member was intersected in stratigraphic bores GSQ Springsure 8 and 9, (Orion Creek; Gray, 1976), and GSQ Springsure 15 and 16 (Arcturus Road; Balfe, 1982). Also intersected in petroleum exploration wells AFO Arcturus 1, AFO Inderi 1, and HOM Fernlees 1. In AOE 1 (Reids Dome) and AOE 2 (Reids Dome), sandstone occurs in a position stratigraphically ;similar to the Riverstone Sandstone Member, but the continuity of these sandstone intervals has not been demonstrated, and their equivalence is not proven. The Mostyndale Mudstone Member is therefore only tentatively identified in Reids Dome. South of Reids Dome and in the Consuelo Anticline to the east, the Mostyndale Mudstone Member cannot be differentiated from the Moorooloo Mudstone Member, since the Riverstone Sandstone Member is absent.|16-MAY-23
24387|Mostyndale Mudstone Member|Thickness range|The thickness of the Mostyndale Mudstone Member ranges from a maximum of 425 m in the composite reference section from GSQ Springsure 15 and 16 to a minimum of 244 m in AFO Inderi 1. The type section is 249 m thick, and in HOM Fernless 1 the unit is 276 m thick.|16-MAY-23
24387|Mostyndale Mudstone Member|Lithology|The Mostyndale Mudstone Member is composed mainly of dark grey mudstone. The proportion of silty material in the mudstone increases towards the top of the un;it. A variable amount of very fine, light grey sandstone is present in the lower part of the unit. At outcrop, the unit generally shows a blue-grey colour, and ferruginised concretions occur.|16-MAY-23
24387|Mostyndale Mudstone Member|Fossils|The type section contains marine shell fossils, mainly brachiopods, which are scattered throughout the unit but are particularly abundant toward the bottom. The cored reference section in GSQ Springsure 15 and 16 contains bivalves, brachiopods, gastropods, crinoids, bryozoans, and very large foraminifera, some of which are more than 10 mm long. The large foraminifera appear to be strongly facies controlled, being confined to the more silty intervals. Large foraminifera and fish scales are present in the outcrop reference section in Springsure Creek. The fauna observed is consistent with an Early Permian age.|16-MAY-23
24387|Mostyndale Mudstone Member|Relationships and boundaries|The Mostyndale Mudstone Member conformably overlies the Reids Dome Beds, and is conformably overlain by the Riverstone Sandstone Member of the Cattle Creek Formation. The lower boundary is taken at the base of the first bed of bioturbated, marine mudstone above the Reids Dome Beds. The upper boundary is placed at the top of the monotonous marine mudstone, beneath the first thick bed of sandstone.|16-MAY-23
24387|Mostyndale Mudstone Member|Identifying features|Wireline logs: Wireline logs of the Mostyndale Mudstone Member exhibit the following characteristics: 1. A clearly defined lower boundary on both gamma-ray and resistivity logs. 2. Strong log differentiation between sandstone and mudstone in the lower part of the unit, particularly on the resistivity log. 3. A gradual upward increase in resistivity and decrease in gamma-ray intensity reflecting the gradual increase in average grain size from mud to silt.|16-MAY-23
24387|Mostyndale Mudstone Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24387|Mostyndale Mudstone Member|Proposer|Balfe P.E.|16-MAY-23
12441|Mount Albert Group|Name source|Mount Albert mine (M.L. 8486, Cloncurry Mining District), 15 km west-northwest of Mary Kathleen town, latitude 21o42'35"S, longitude 139o51'30"E (6856 810096).|16-MAY-23
12441|Mount Albert Group|Constituents|The Mount Albert Group consists of the Deighton Quartzite, White Blow Formation, Roxmere Quartzite and Knapdale Quartzite.|16-MAY-23
12441|Mount Albert Group|Extent|The formations of this Group are exposed discontinuously in the area bounded by 20o12'S and 21o6'S latitude and 139o47'E and 140o36'E longitude. The Deighton Quartzite and White Blow Formation occur in a north-trending strip 15 km wide at the west of this area, the Roxmere Quartzite occurs in the southeast and the Knapdale Quartzite occurs in the northeast.|16-MAY-23
12441|Mount Albert Group|Thickness range|The Deighton Quaratzite and White Blow Formation have a total thickness of up to 3700 m. The Roxmere Quartzite is at least 1500 m thick and the Knapdale Quartzite is at least 2000 m thick.|16-MAY-23
12441|Mount Albert Group|Lithology|The Quartzites contain sublabile quartzite, pebbly quartzite, minor conglomerate, calcareous sandstone, micaceous sandstone and minor siltstone and shale and phyllite. The White Blow Formation contains micaceous siltstone, limestone, calcareous rocks, slate, phyllite, schist and minor quartzite.|16-MAY-23
12441|Mount Albert Group|Relationships and boundaries|The Group contains discontinuous remnants of the youngest sedimentary cycle recognised in the Middle Proterozoic sequence of the eastern succession. The three Quartzite Formations overlie the Corella Formation with apparent conformity in most areas, but locally the Deighton Quartzite shows angular relationships with older rocks. Because of their similar stratigraphic position, similar lithologies, and similar air-photo pattern they are considered to be equivalent. The Group is possibly a correlative of units A to D in the Surprise Creek Beds (Wilson et al., in prep.), and to parts of the Mammoth Formation (Cavaney, 1975) west of the Kalkadoon-Leichhardt basement block. The Deighton Quartzite grades abruptly upwards into a finer grained sequence and a similar transition occurs near the top of the Knapdale Quartzite, where minor stratabound copper mineralisation is located. Both of these Quartzites overlie sulphide-bearing shales towards the top of the Corella Formation.|16-MAY-23
12441|Mount Albert Group|Age reasons|Precambrian, probably Carpentarian (Middle Proterozoic).|16-MAY-23
12441|Mount Albert Group|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1977|16-MAY-23
12441|Mount Albert Group|Proposed publication|Queensland Government Mining Journal|16-MAY-23
12441|Mount Albert Group|Name first published by|Glikson A.Y., Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
24390|Mount Angelay Granite|Name source|Named after Mount Angelay, a prominent mesa at GR 763535, situated 7.5 km to E of the granite, Mount Angelay 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24390|Mount Angelay Granite|Unit history|Like all other granites in the eastern part of the Duchess 1:250 000 Sheet area, the Mount Angelay Granite was mapped as Williams Granite by Carter & Opik (1963).|16-MAY-23
24390|Mount Angelay Granite|Type section locality|Hilly terrain in the vicinity of GR 635555, 2.5 km NE of Eureka homestead, Mount Angelay 1:100 000 Sheet area. Here there are extensive exposures of partly foliated, pink hornblende-biotite granite and minor biotite-rich granite and pegmatite.|16-MAY-23
24390|Mount Angelay Granite|Extent|The granite forms an elongate body 28 km long, trending NNW and covering about 200 km2, west of the Cloncurry Fault in the centralpart of Mount Angelay 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24390|Mount Angelay Granite|Lithology|Consists of pinkish, locally foliated, medium to coarse-grained, mainly even-grained but locally porphyritic granite containing hornblende and/or biotite and/or clinopyroxene, and minor leucogranite, porphyritic microgranite, contaminated grey mafic-rich granite, aplite and pegmatite.|16-MAY-23
24390|Mount Angelay Granite|Relationships and boundaries|The granite intrudes Doherty Formation and Soldiers Cap Group, is cut by E-trending dolerite dykes, and is overlain by flat-lying Mesozoic sediments. Intrusive contacts with the Doherty Formation are locally highly irregular and in places the granite cannot easily be distinguished from calc-silicate rocks.|16-MAY-23
24390|Mount Angelay Granite|Age reasons|Proterozoic|16-MAY-23
24390|Mount Angelay Granite|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
24390|Mount Angelay Granite|Comments|Remarks: The granite forms a large, mostly well-defined and hence readily mappable, intrusive body geographically separated from, but probably related to, the petrographically similar Saxby Granite to NE and the Squirrel Hills Granite to S. It forms part of the Williams Batholith (new structural term).|16-MAY-23
24390|Mount Angelay Granite|Defn Reference|82/22920|16-MAY-23
24390|Mount Angelay Granite|Proposer|Donchak P.J.T.|16-MAY-23
24393|Mount Cobalt Granite|Name source|Mount Cobalt mine, GR 475957, Mount Merlin 1:100 000 Sheet area, Duchess 1:250 000 Sheet area. This mine is situated 5 km SW of the granite.|16-MAY-23
24393|Mount Cobalt Granite|Type section locality|Central part of the outcrop area, in the vicinity of GR 508002, 5 km NE of Mount Cobalt mine and 19 km S of Selwyn, Selwyn 1:100 000 Sheet area. Here pink, mainly medium-grained granite is well exposed as tors and spheroidal boulders.|16-MAY-23
24393|Mount Cobalt Granite|Extent|The granite forms an isolated oval intrusive body about 1 km long from N to S, centred at GR 508002, in the W of the Selwyn 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24393|Mount Cobalt Granite|Lithology|The unit consists of massive (non-foliated), pink, medium to fine-grained biotite granite and minor aplite.|16-MAY-23
24393|Mount Cobalt Granite|Relationships and boundaries|The granite intrudes Kuridala Formation and metadolerite.|16-MAY-23
24393|Mount Cobalt Granite|Age reasons|Proterozoic|16-MAY-23
24393|Mount Cobalt Granite|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
24393|Mount Cobalt Granite|Comments|Remarks: The granite is given a separate name as it forms a well-defined though small intrusive body geographically separated from other granites in the area. It is probably closely related to the petrographically similar Mount Dore and Yellow Waterhole Granites (new names) to the N and S respectively, and forms part of the Williams Batholith (new structural term). It is distinctive in being surrounded by a metamorphic aureole about 1 km wide).|16-MAY-23
24393|Mount Cobalt Granite|Defn Reference|82/22920|16-MAY-23
26050|Mount Darcy Microgranodiorite|Name source|Mount Darcy, a small but prominent conical hill at GR 7561-407816 (Forest Home 1:100 000 Sheet area), 7 km northeast of Prestwood homestead. "Mount Darcy" here conforms with local usage; most topographic maps show "Mount Darcy" incorrectly as the highest (but relatively inconspicuous) point on a mesa of Mesozoic sandstone 3 km to the northeast.|16-MAY-23
26050|Mount Darcy Microgranodiorite|Unit history|Mapped (in part) as part of the Prestwood Microgranite, and in part included in "Forsayth Granite" by White (1959) and Branch (1966).|16-MAY-23
26050|Mount Darcy Microgranodiorite|Type section locality|A small tor 1 km southeast of Mount Darcy (GR 7561-416811). Two phases of intrusive rock are present; both are porphyritic microgranodiorite, containing phenocrysts of quartz, plagioclase, and biotite, but lacking hornblende. The younger, light grey porphyry contains large xenoliths of the older phase, a darker rock with a finer-grained groundmass and less abundant phenocrysts. The younger phase contains about 30 percent by volume phenocrysts including prominent ellipsoidal quartz phenocrysts, a characteristic of the Mount Darcy Microgranodiorite. The older phase contains slightly rounded bipyramidal B-quartz phenocrysts; it may have been intruded originally as a dyke swarm. Xenoliths of Forsayth Granite are also abundant in the Microgranodiorite.|16-MAY-23
26050|Mount Darcy Microgranodiorite|Extent|Numerous small intrusive bodies in the Mount Darcy-upper Crooked Creek-upper Dismal Creek area; larger bodies to the south in the Somerset Creek area, on both sides of the Gulf Developmental Highway, where there are also numerous roof pendants and inclusions of Forsayth Granite; small bodies crop out between Mount Darcy and Mount Turner.|16-MAY-23
26050|Mount Darcy Microgranodiorite|Lithology|The unit consists predominantly of the younger phase described above; it contains between 20 and 80 percent (by volume) phenocrysts. In the area either side of the highway between Somerset Creek and Crooked Creek, porphyritic hornblende-biotite microgranodiorite is intimately mixed with, and appears to intrude the biotite microgranodiorite, but could not be mapped out separately at 1:100 000 scale. Apart from a tendency for its quartz phenocrysts to be bipyramidal rather than ellipsoidal, the hornblende-bearing rock is difficult to distinguish from the biotite microgranodiorite in outcrop. A further, still younger phase occurs as narrow dykes cutting both the biotite and hornblende-biotite microgranodiorites in the Somerset Creek area. It is a green hornblende microgranodiorite containing about 20 percent by volume of hornblende and plagioclase phenocrysts; quartz phenocrysts are not common. Mount Darcy Microgranodiorite is commonly associatead with areas of brecciation, and of intense quartz-sericite (and, locally, potassic) alteration as affecting both porphyry and country rocks. At Mount Darcy itself, intensely sericitised porphyry surrounds a small breccia pipe. The "Phyllis May" and Mount Turner Cu-Mo prospects are associated with Mount Darcy Microgranodiorite.|16-MAY-23
26050|Mount Darcy Microgranodiorite|Relationships and boundaries|Intrudes Proterozoic Aurora, Delaney, and Forsayth Granites. Occurs as small irregularly-shaped plutons ranging from several hundred metres to several kilometres across. Some of these "plutons" may be dyke swarms, but if so, the screens of granitic country rock rarely crop out. Mount Darcy Microgranodiorite intrudes Dismal Creek Volcanics, and is probably intruded by Prestwood Microgranite. The hornblende-bearing "phases" may, at least in part, be equivalent to Mount Sircom Microgranodiorite.|16-MAY-23
26050|Mount Darcy Microgranodiorite|Age reasons|Probably Carboniferous. Intrudes Dismal Creek Volcanics, which are probably mid-Carboniferous, but is probably comagmatic with at least part of the Volcanics. At Mount Turner cuts rhyolite dykes that are related to the mid-Carboniferous Newcastle Range Volcanics (Black, 1973) or the time-equivalent(?) Maureen Volcanics.|16-MAY-23
26050|Mount Darcy Microgranodiorite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
26050|Mount Darcy Microgranodiorite|Unit name|Mount Darcy Microgranodiorite (new name)|16-MAY-23
24396|Mount Dore Granite|Name source|Named after Mount Dore copper mine, GR 474043, Mount Merlin 1:100 000 Sheet area, which is near the southwestern margin of the granite body. Duchess 1:250 000 Sheet area.|16-MAY-23
24396|Mount Dore Granite|Unit history|Like all other granites in the eastern part of the Duchess 1:250 000 Sheet area, it was mapped as Williams Granite by Carter & Opik (1963).|16-MAY-23
24396|Mount Dore Granite|Type section locality|From a point 2.7 km N of Mount Dore mine, at GR 473070, where the granite intrudes black slate of the Kuridala Formation, east for 2 km, in the Mount Merlin and Selwyn 1:100 000 Sheet areas. Spheroidal boulders, tors, and mesas capped by weathered bedrock here are formed of pink, medium to coarse, even-grained to slightly porphyritic granite cut by some irregular aplite veins, and a few thin sheet-like veins of coarse hematite.|16-MAY-23
24396|Mount Dore Granite|Extent|The granite crops out south and southeast of Selwyn, covering an area 14 km long from SW to NE and up to 7 km wide in NW Selwyn and NE Mount Merlin 1:100 000 Sheet areas, Duchess 1:250 000 Sheet area.|16-MAY-23
24396|Mount Dore Granite|Lithology|The unit consists of massive (non-foliated), even-grained to slightly porphyritic medium to coarse biotite and hornblende-biotite granite, and minor fine-grained granite, aplite, pegmatite, and greisen.|16-MAY-23
24396|Mount Dore Granite|Relationships and boundaries|Intrudes Kuridala Formation and is overlain by flat-lying Mesozoic sediments.|16-MAY-23
24396|Mount Dore Granite|Age reasons|Proterozoic|16-MAY-23
24396|Mount Dore Granite|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
24396|Mount Dore Granite|Comments|Remarks: The unit is a homogeneous body of granite forming a well-defined, mappable intrusion which is separated geographically from other granites in the area. It is probably closely related to thepetrographically similar Mount Cobalt, Squirrel Hills and Yellow Waterhose Granites (new names), and forms part of the Williams Batholith (new structural term).|16-MAY-23
24396|Mount Dore Granite|Defn Reference|82/22920|16-MAY-23
24396|Mount Dore Granite|Proposer|Blake D.H.|16-MAY-23
29478|Mount Elvan Granite|Name source|Mount Elvan, north of the Cape River and east of Gorge Creek at about GR 3115 77450 (Figure 1). The feature is not named on current topographic maps but is shown on maps of the Upper Cape River goldfield published by Daintree (1868).  The grid reference is based on the AGD66 datum.|16-MAY-23
29478|Mount Elvan Granite|Unit history|The Mount Elvan Granite was not recognised on the Hughenden 1:250 000 geological map (Paine & others, 1971), the rocks being mapped as the undivided unit, ODn.|16-MAY-23
29478|Mount Elvan Granite|Type section locality|In Gorge Creek, north of the Cape River at GR 3110 77546. Here, a grey to white, fine grained, locally garnetiferous biotite granite crops out.  The grid reference is based on the AGD66 datum.|16-MAY-23
29478|Mount Elvan Granite|Description at type locality|This granite comprises quartz, albite, oligoclase, microcline in granophyric intergrowths with quartz, red/brown biotite and minor muscovite. Large garnet phenocrysts(?) occur in patches near the type locality.|16-MAY-23
29478|Mount Elvan Granite|Extent|The Mount Elvan Granite crops out over about 9km2 parallel to the Cape River and east and west of Gorge Creek (Figure 2). It appears to form a large sheet intruding granitoids of the Fat Hen Creek Complex and Gorge Creek Granite.|16-MAY-23
29478|Mount Elvan Granite|Lithology|The rock type at the type locality occurs throughout the area of outcrop of the unit. However, large garnet phenocrysts(?) up to 1cm which occur in bands at the type locality are not common elsewhere in the unit.The granite appears to form a large sheet which intrudes the Fat Hen Creek Complex and Gorge Creek Granite both east and west of Gorge creek. A foliation, interpreted as an igneous foliation, is present in some rocks beside the track along Gorge Creek.|16-MAY-23
29478|Mount Elvan Granite|Relationships and boundaries|The Mount Elvan Granite intrudes the Mesoproterozoic Fat Hen Creek Complex and the Gorge Creek Granite.|16-MAY-23
29478|Mount Elvan Granite|Age reasons|The age of the Mount Elvan Granite is not known. An age of Silurian to Devonian is assigned on the basis of lack of deformation features in the granite.|16-MAY-23
29478|Mount Elvan Granite|Comments|The Mount Elvan Granite is non-magnetic at the type locality and throughout the unit.|16-MAY-23
29478|Mount Elvan Granite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
24398|Mount Erle Igneous Complex|Name source|Named after Mount Erle, GR 825296, Duchess 1:100 000 Sheet area, Duchess 1:250 000 Sheet area. Mount Erle lies within the outcrop area of the Mount Erle Igneous Complex.|16-MAY-23
24398|Mount Erle Igneous Complex|Type section locality|Railway cutting 300 m west-northwest of Duchess post office, at GR 818378, Duchess 1:100 000 Sheet area. Here there are exposures of granite, dolerite, and some hybrid rocks.|16-MAY-23
24398|Mount Erle Igneous Complex|Extent|The unit crops out over a northerly trending area of about 30 km2 extending from 2 km N to 12 km S of Duchess, in the Duchess 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24398|Mount Erle Igneous Complex|Lithology|The unit consists of pink granite which is commonly foliated, dolerite, gabbro, heterogeneous dioritic hybrid rocks, and minor aplite, feldspar porphyry, quartz-feldspar pegmatite, and calc-silicate rocks. The mafic rocks occur as large masses and as smaller angular fragments and rounded pillow-like bodies enclosed in and veined by granite.|16-MAY-23
24398|Mount Erle Igneous Complex|Relationships and boundaries|The unit intrudes the Corella Formation, which surrounds it.|16-MAY-23
24398|Mount Erle Igneous Complex|Age reasons|Proterozoic|16-MAY-23
24398|Mount Erle Igneous Complex|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
24398|Mount Erle Igneous Complex|Comments|Remarks: Exposures of the unit near Duchess were mapped as unnamed granite by Carter & Opik (1963).|16-MAY-23
24398|Mount Erle Igneous Complex|Defn Reference|82/22920|16-MAY-23
24398|Mount Erle Igneous Complex|First Reference|81/21497|16-MAY-23
24398|Mount Erle Igneous Complex|Proposer|Blake D.H.|16-MAY-23
24398|Mount Erle Igneous Complex|Resdate|08-MAR-1978, 02-MAY-1978|16-MAY-23
12714|Mount Formartine Granite|Name source|Mount Formartine, adjacent to the coastline north of Cairns (GR 520515, Cairns 1:100 000 Sheet).|16-MAY-23
12714|Mount Formartine Granite|Unit history|Two plutons previously included within the Mareeba Granite.|16-MAY-23
12714|Mount Formartine Granite|Type section locality|Road cuttings and gullies adjacent to the Captain Cook Highway immediately north of the settlement at Ellis Beach (GR 545515, Cairns 1:100 000 Sheet and adjacent vicinity), which show strongly foliated and sheared, dark grey, medium-grained muscovite-biotite granite at the edge of a pluton. The degree of shearing appears to decrease uphill (west) away from the contact.|16-MAY-23
12714|Mount Formartine Granite|Extent|Several small elongate plutons and dyke-like bodies in a northwesterly trending belt between the southern suburbs of Cairns and the Mowbray River, south of Port Douglas. Total known area of exposure is about 60 km2.|16-MAY-23
12714|Mount Formartine Granite|Lithology|Dark grey to black, medium-grained, even grained, muscovite-biotite granite; muscovite predominates in places. Invariably foliated to some extent, the foliation resulting from shearing. Strong shearing evident near margins of bodies and throughout small bodies. Small dark xenoliths to 3 cm common. Slices of country rock common near margins.|16-MAY-23
12714|Mount Formartine Granite|Relationships and boundaries|Intrudes sheared 'broken formation' of the Hodgkinson Formation, which it has hornfelsed. Appears to have been intruded during a shearing event.|16-MAY-23
12714|Mount Formartine Granite|Age reasons|Latest Permian-earliest Triassic based on K-Ar age of 247 million years (sample DA 36) on ample from intrusion at Trinity Beach.|16-MAY-23
12714|Mount Formartine Granite|Proposed publication|1:100 000 Geological Map Commentary, Cairns region, Queensland, Geological Survey of Queensland.|16-MAY-23
12714|Mount Formartine Granite|Category|2|16-MAY-23
22420|Mount Glengalder Granite|Name source|Mount Glengalder, at GR 3625 77557, located 5km north of the Flinders Highway and 12km west of Thalanga station in the Homestead 1:100 000 Sheet area. The grid reference is based on the AGD66 datum.|16-MAY-23
22420|Mount Glengalder Granite|Unit history|The Mount Glengalder Granite was mapped as ODa (felsic phase of the Ravenswood Granodiorite Complex by Wyatt & others (1971), Clarke & Paine (1970)).|16-MAY-23
22420|Mount Glengalder Granite|Type section locality|On the western flanks of Mount Glengalder at GR 3625 77559 in the Homestead 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
22420|Mount Glengalder Granite|Description at type locality|A white, medium grained, altered biotite granite is well exposed on the mountain. The rock comprises quartz, microperthitic K-feldspar, plagioclase with altered cores, and recrystallised biotite.|16-MAY-23
22420|Mount Glengalder Granite|Extent|The Mount Glengalder Granite crops out over about 3km2 around Mount Glengalder.|16-MAY-23
22420|Mount Glengalder Granite|Lithology|The rock type at the type locality is representative of the unit. Southeast of the type locality, a sample comprises quartz, turbid K-feldspar, plagioclase, biotite/chlorite, opaques and minor altered hornblende. Alteration is variable ranging from intense to minor throughout the unit. The granite is strained as evidenced by the blue 'pearly' appearance of the quartz grains.|16-MAY-23
22420|Mount Glengalder Granite|Relationships and boundaries|The Mount Glengalder Granite appears to intrude the Seventy Mile Range Group. Its relationship to the Shovel Creek Complex is not known.|16-MAY-23
22420|Mount Glengalder Granite|Age reasons|The age of the Mount Glengalder Granite is not known precisely. An age of Middle Ordovician is assigned on the basis of lithological similarity to Middle Ordovician granites in the Ravenswood BatholithThe age of the Mount Glengalder Granite is not known precisely. An age of Middle Ordovician is assigned on the basis of lithological similarity to Middle Ordovician granites in the Ravenswood Batholith.|16-MAY-23
22420|Mount Glengalder Granite|Comments|MAGNETIC SUSCEPTIBILITY::  Magnetic susceptibilities at the type locality are in the range 303-534 x 10[superscript]-5 SI units. Throughout the outcrop area, susceptibilities are in the range 61-671 (average 255) x 10[superscript]-5 SI units with the lower values in the more altered samples.|16-MAY-23
26315|Mount Helpman Member|Name source|Mount Helpman (GR 769213 - Forsayth 1:100 000 Sheet area) on the south side of the Robertson River, 10.5 km northwest of Robin Hood homestead, Georgetown area, north Queensland.|16-MAY-23
26315|Mount Helpman Member|Unit history|The unit was previously shown as an unnamed member of the Robertson River Metamorphics on the Forsayth and Georgetown 1:100 000 Preliminary Geological maps (Bain & others, 1976; Oversby & others, 1978).|16-MAY-23
26315|Mount Helpman Member|Geomorphic expression|The unit forms gently to moderately hilly terrain and is commonly topographically more prominent than adjacent parts of the Robertson River Formation. Differential weathering and erosion have picked out well-defined bedding trends in some areas.|16-MAY-23
26315|Mount Helpman Member|Type section locality|In Bull Creek from GR 723132 downstream to 714147 (inferred to be the base and top of the unit respectively). Within this section small isoclinal folds are common, indicating that multiple repetition of the unit has occurred; the thickness represented by this section is therefore not known. The maximum thickness (if no repetition had occurred) is about 1200 m. However the sectionspecified is typical of the unit as presently mapped. The most accessible outcrops in the type section are in Bull Creek, near where it is crossed by the track between Robin Hood and the Forsayth-Agate Creek road, and are characteristic of the unit; they consist of alternating quartz-mica schist and micaceous quartzite layers from several centimetres to a metre thick. In some of the quartzite layers flattened ellipsoids containing calc-silicate minerals are present.|16-MAY-23
26315|Mount Helpman Member|Extent|In the Forsayth 1:100 000 Sheet area, the unit has been mapped as a sinuous belt extending northwest from the site of Old Robin Hood homestead, along the Little Robertson River to near its junction with the Robertson River, and thence east-northeast towards the Newcastle Range, mainly on the southern side of the Robertson River, but extending north of it in the Quartz Blow Creek area. Two areas of outcrop have been assigned to the member in the Georgetown 1:100 000 Sheet area. One is a crudely triangular area extending south from the abandoned City of Glasgow gold mine to an easterly line from Lornevale homestead to the Newcastle Range. The other is an area 7.5 km by 6 km in the headwaters of Daniel Creek. In the Gilberton 1:100 0000 Sheet area the unit has not been mapped out, but its eqivalents have been recognised in several sections of the lower part of the Robertson River Formation which have been examined in detail: (a) in a reference section of the lower part of the Robertson River Formation along the Percy River (Withnall & Mackenzie, 1980);  (b) near the Eight Mile Waterhole on the Gilbert River;  and (c) along the Gilbert River for several kilometres upstream of its junction with Six Mile Creek.|16-MAY-23
26315|Mount Helpman Member|Thickness range|The thickness of the unit as mapped cannot be determined because of the repetition by complex isoclinal folding. However the equivalent rocks in the Gilberton area are only of the order of several hundred metres thick.|16-MAY-23
26315|Mount Helpman Member|Lithology|Quartz-mica schist and micaceous quartzite as in the type section are the main rock-types in the unit as presently mapped. Quartzite constitutes up to 30 percent of the unit. Spots of calc-silicate minerals are locally present in quartzite. The rocks are all metamorphosed in the amphibole facies. In the Gilberton area, the equivalents of the Mount Helpman Member are much lower in metamorphic grade and less deformed. They consist of cleaved shale and siltstone with prominent thick, laminated and trough cross-laminated sub-labile to quartzose sandstone beds, commonly containing ellipsoidal calcareous concretions up to 1 m across. Some of the beds are also calcareous.|16-MAY-23
26315|Mount Helpman Member|Relationships and boundaries|The unit is a member of the lower part of the Robertson River Formation which is part of the Etheridge Group (Withnall & Mackenzie, 1980). The equivalents in the Gilberton area occupy a position midway between the base of the formation and the Dead Horse Metabasalt Member. A similar position is inferred in the Forsayth area. Amphibolite containing relict amygdales crops out in Bull Creek downstream from the type section. The Mount Helpman Member is recognised by a marked increase in the abundance of quartzite relative to schist, compared with the rest of the Robertson River Formation.|16-MAY-23
26315|Mount Helpman Member|Age reasons|A minimum age of 1570+/-20 m.y. (mid-Proterozoic) was obtained for the Etheridge Group by dating the earliest deformational-metamorphic event in the Einasleigh Metamorphics (Black & others, 1979).|16-MAY-23
26315|Mount Helpman Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
26315|Mount Helpman Member|Proposer|Withnall I.W.|16-MAY-23
26315|Mount Helpman Member|Unit name|Mount Helpman Member (of the Robertson River Formation)|16-MAY-23
24400|Mount Hogan Granite|Name source|Mount Hogan homestead at GR 976 791 (Gilberton 1:100 000 Sheet area); also the old Mount Hogan gold mines centred around GR 948 765 occur within the granite.|16-MAY-23
24400|Mount Hogan Granite|Unit history|Previously mapped as Robin Hood Granite (White, 1962).|16-MAY-23
24400|Mount Hogan Granite|Type section locality|Group of tors around GR 942 778, 2.5 km southwest of Mount Hogan homestead and 1.5 km northwest of the main group of gold mines. Cream to grey and pink medium to coarse equigranular biotite granite crops out.|16-MAY-23
24400|Mount Hogan Granite|Extent|A roughly semi-circular pluton 7 km in diameter and 30 km2 in area centred at about GR 950 800 (Gilberton 1:100 000 Sheet area).|16-MAY-23
24400|Mount Hogan Granite|Lithology|Mainly medium to coarse equigranular to slightly porphyritic biotite granite, grey when fresh but commonly pink or reddish brown, due to mild alteration. Aplite or fine grained pink leucogranite veins occur in the northern part of the pluton. Around the southeastern and southern margins the granite contains shallowly dipping zones of intense chlorite-sericite alteration which host gold-silver-uranium mineralisation in quartz veins.A characteristic feature of the granite is its high radiometric background (3 to 5 times as high as that in the metamorphics).|16-MAY-23
24400|Mount Hogan Granite|Relationships and boundaries|Intrudes the Proterozoic Robertson River and Bernecker Creek Formations and also metadolerite sills within the former. Intruded by late Palaeozoic andesite, rhyolite and microdiorite dykes.|16-MAY-23
24400|Mount Hogan Granite|Age reasons|Probably late Proterozoic. The pluton truncates and therefore post-dates large-scale folds outlined in the country rocks by metadolerite sills; mapping has demonstrated that these structures also fold the slaty cleavage produced by the first deformation in the area, and are therefore probably second or possibly third generation folds. The second and third deformations have been dated at about 1470 and 970 m.y. respectively (Black & others, 1979). An imprecise Rb/Sr total rock isochron on a sample of Mount Hogan Granite indicates the unit is more likely to be Precambrian than Palaeozoic in age (L.P. Black, pers. comm.).|16-MAY-23
24400|Mount Hogan Granite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24400|Mount Hogan Granite|Proposer|Bain J.H.C., Withnall I.W.|16-MAY-23
12822|Mount Isa Group|Name source|The city of Mount Isa, latitude 20o44'S, longitude 139o29'E.|16-MAY-23
12822|Mount Isa Group|Constituents|Magazine Shale: 210 m, calcareous shale, locally pyritic. Kennedy Siltstone: 310 m, dolomitic siltstone, feldspathic quartzite. Spear Siltstone: 170 m, dolomitic siltstone, shale, albite-dolomite marker bed. Urquhart Shale: 910 m, ferruginous pyritic shale, tuff, siliceous dolomitic breccia; includes Pb-Zn and Cu orebodies. Native Bee Siltstone: 800 m, dolomitic siltstone, minor tuff. Breakaway Shale: 1040 m, grey shale, minor siltstone. Moondarra Siltstone: 1220+, dolomitic siltstone, shale. Warrina Park Quartzite: 35-150 m, orthoquartzite, feldspathic quartzite, conglomerate. Total of approximately 4800 m.|16-MAY-23
12822|Mount Isa Group|Geomorphic expression|Most formations of the group form valleys; however, the Breakaway Shale forms a series of prominent hills and ridges, the Urquhart Shale is generally exposed as discontinuous, iron-stained ridges; and the Warrina Park Quartzite forms prominent silicified ridges and hogbacks.|16-MAY-23
12822|Mount Isa Group|Type section locality|The upper seven formations in the Mount Isa Group were first described by Bennett (1965), but the location of their type sections have not been published. The following type sections are based on an unpublished report for Mount Isa Mines Ltd (Battey, 1962); metric grid references have been added. Magazine Shale: North of King Gully, from 6756-407172 to 6756-405172.  Kennedy Siltstone: North of King Gully, from 6756-410104 to 6756-407104. Spear Siltstone: At Spear Creek, from 6756-412145 to 6756-409145. Urquhart Shale: King Gully, from 6756-425107 to 6756-413103. Native Bee Siltstone: East of the Mount Isa Golf Course, from 6756-427030 to 6756-421030. Breakaway Shale: East of the Leichhardt River crossing on the Mount Isa-Lake Moondarra road, from 6856-444120 to 6756-433120. Moondarra Siltstone: Southeast of Lake Moondarra, from 6856-505195 to 6856-495201. These formations and the Warrina Park Quartzite are all present in an east-west reference section near Depot Creek and King Gully, 3.5 km north of Mount Isa Post Office.|16-MAY-23
12822|Mount Isa Group|Extent|In a north-trending belt, 1 to 10 km wide, from a point 30 km south of Mount Isa to near the Leander Range, 48 km north of Mount Isa. An outlier of the Group was mapped by Carter et al. (1961) 80 km south of Mount Isa, and there is another outlier in the Crystal Creek area, 80 km north of Mount Isa.|16-MAY-23
12822|Mount Isa Group|Relationships and boundaries|The Mount Isa Group overlies Myally Subgroup and Eastern Creek Volcanics unconformably, and 'Mammoth Formation' correlatives either conformably or unconformably. It is intruded by a few dolerite and diorite dykes.|16-MAY-23
12822|Mount Isa Group|Age reasons|The Group is probably younger than 1570+/-12 m.y., the age of the Sybella Granite, which is overlain by rocks probably equivalent to the Mount Isa Group (Plumb & Derrick, 1975). Ages determined from lead in the Urquharat Shale range between 1500 and 1600 m.y. (Richards, 1963); Ostic et al., 1967; Cooper et al., 1969).|16-MAY-23
12822|Mount Isa Group|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
12822|Mount Isa Group|Proposed publication|Queensland Government Mining Journal|16-MAY-23
12822|Mount Isa Group|Comments|Remarks: The Mount Isa Group is redefined to include the Warrina Park Quartzite as the basal formation in the Group.|16-MAY-23
24401|Mount Juliet Granite|Name source|Mount Juliet at GR 016519 (Einasleigh 1:100 000 Sheet area.|16-MAY-23
24401|Mount Juliet Granite|Unit history|Previously mapped as Forsayth Granite (White, 1962).|16-MAY-23
24401|Mount Juliet Granite|Type section locality|Outcrops in Ellendale Creek at GR 020541 (Mount Surprise 1:100 000 Sheet area) consist of coarse-grained porphyritic biotite-muscovite granite with abundant muscovite 'books' up to 1 cm across and sub-equant K-feldspar phenocrysts generally 1 to 2 cm, but up to 6 cm in size.|16-MAY-23
24401|Mount Juliet Granite|Extent|A roughly circular pluton about 16 km2 in area, situated about 9 km east-northeast of Einasleigh.|16-MAY-23
24401|Mount Juliet Granite|Lithology|Whitish-grey to pink, medium to coarse-grained equigranular to slightly porphyritic biotite-muscovite granite to granodiorite. Muscovite flakes are up to 1 cm across. Sparse white to pink K-feldspar megacrysts are found in places and are generally 1 to 2 cm in size (rarely up to 6 cm). Locally a foliation is present.|16-MAY-23
24401|Mount Juliet Granite|Relationships and boundaries|The granite intrudes the Proterozoic Einasleigh Metamorphics. The eastern edge of the pluton is in contact with the Mount Webster Granodiorite; however, no contact relationships have been observed.|16-MAY-23
24401|Mount Juliet Granite|Age reasons|The granite is probably Middle Proterozoic in age, because it is locally foliated. However, some known Siluro-Devonian granitoids, such as the Dumbano Granite, are weakly foliated, so that a Siluro-Devonian age is a possibility for the Mount Juliet Granite.|16-MAY-23
24401|Mount Juliet Granite|Proposer|Warnick J.V.|16-MAY-23
12886|Mount Les Siltstone|Name source|From Mount Les, a small hill at grid ref. 857230, in the southwestern Hedleys Creek 1:100 000 Sheet area. The name is best known as applied to the Mt Les Prospect near Gorge Creek 0.5 km south of Mount Les.|16-MAY-23
12886|Mount Les Siltstone|Unit history|Included by Carter (1959) in the Wollogorang Formation, a name now restricted to an older formation in the Tawallah Group in the McArthur Basin. Roberts et al. (1963) included Mount Les Siltstone in the Fickling Beds, which now become the Fickling Group.|16-MAY-23
12886|Mount Les Siltstone|Type section locality|About 90 m of finely laminated shale and siltstone, with some dolomite interbeds. The base is at grid reference 906243, abut 5 km east-northeast of the Mt Les prospect; the section runs 450 m in a southeasterly direction along a mining company track.|16-MAY-23
12886|Mount Les Siltstone|Extent|Exposed over 30 km in the southwestern Hedleys Creek 1:100 000 Sheet area, Queensland, and the eastern part of the adjacent Seigal Sheet area, Northern Territory.|16-MAY-23
12886|Mount Les Siltstone|Thickness range|55-90 m|16-MAY-23
12886|Mount Les Siltstone|Lithology|Black dolomitic siltstone and black and white shale; interbeds of pink and brown dolomite in western outcrops.|16-MAY-23
12886|Mount Les Siltstone|Relationships and boundaries|Conformably overlies Walford Dolomite; boundary is sharp in most areas because the upper layers of the Walford Dolomite have been altered to chert. The boundary is gradational in places, as interbeds of dolomite occur in Mount Les Siltstone. The upper contact is a disconformity in most places, and around grid reference 135255 in the eastern Seigal Sheet area the Mount Les Siltstone has been completely eroded, and Doomadgee Formation lies unconformably on Walford Dolomite.|16-MAY-23
12886|Mount Les Siltstone|Age reasons|Proterozoic-Carpentarian. Correlation of part of the underlying Peters Creek Volcanics with the Hobblechain Rhyolite Member of the Masterton Formation in the McArthur Basin suggest an age of less than 1575 m.y. (age of the Hobblechain Rhyolite Mbr). Younger age limit provided by 1280 m.y. old dolerites which intrude equivalents of the South Nicholson Group, which unconformably overlies Mount Les Siltstone.|16-MAY-23
12886|Mount Les Siltstone|Defn author|Ian Sweet, 1976.|16-MAY-23
12886|Mount Les Siltstone|Proposed publication|BMR Bulletin - Precambrian geology of the Westmoreland region, Northern Australia.|16-MAY-23
12886|Mount Les Siltstone|Defn Reference|82/22568|16-MAY-23
23827|Mount Newsome Granodiorite|Name source|Mount Newsome at 8351-483159. The grid reference is based on the AGD66 datum.|16-MAY-23
23827|Mount Newsome Granodiorite|Geomorphic expression|The granodiorite forms gentle to moderately undulating terrain with sporadic boulder-sized and rarer platform outcrop. The central part of the pluton is poorly exposed and unweathered outcrop is very rare.   The Mount Newsome Granodiorite is similar in character on Landsat TM images to the eastern area of the Kilmarnock Granodiorite, although the former does exhibit a brownish hue to the west where there is abundant Cainozoic wash. Moderate magnetic anomalies (lower than for the Kilmarnock Granodiorite) are associated with this unit. Significant decreases in magnetisation occur along and proximal to northwest and north trending lineaments. Radiometrically, the Mount Newsome Granodiorite contrasts strongly with the Kilmarnock Granodiorite. It has weak to moderate K and very low Th and U responses.|16-MAY-23
23827|Mount Newsome Granodiorite|Type section locality|At 8351-505251 in the northwest of the pluton, 3 km west of Mount. The grid reference is based on the AGD66 datum.|16-MAY-23
23827|Mount Newsome Granodiorite|Description at type locality|Grey, fine to coarse-grained, porphyritic biotite-hornblende granodiorite.|16-MAY-23
23827|Mount Newsome Granodiorite|Extent|A large subequant pluton, 380 km2 in area, from Mount Mica homestead in the north to Silver Hills homestead in the south.|16-MAY-23
23827|Mount Newsome Granodiorite|Lithology|Dominantly a grey, fine to coarse-grained, equigranular to porphyritic biotite-hornblende granodiorite.|16-MAY-23
23827|Mount Newsome Granodiorite|Relationships and boundaries|Intrudes the Anakie Metamorphic Group, the Gem Park Granite and Whitdale Granodiorite, and is probably intruded by the Keilambete Tonalite. An east-trending line of small, leucocratic, tourmaline-bearing granite bodies intrude the unit north of Mount Leura. The unit is unconformably overlain by the Late Devonian to Early Carboniferous Silver Hills Volcanics and sedimentary rocks of the Drummond Basin, and belts of Cainozoic sediments including gravels and silcrete, along and adjacent to Tomahawk Creek. Numerous small basalt plugs of the Hoy Basalt intrude the unit.  Local outcrop, up to 3 km2 in area, of light grey, fine-grained biotite granite similar to the Central Creek Granodiorite are also present. The origin of these granite outcrops is uncertain. They could later intrusions related to the Central Creek Granodiorite, or may be derived from the granodiorite by fractionation, or represent assimilation of metasedimentary rock like the Mount Observatory Granite.  South of Whitdale, cream to pink, fine to coarse-grained, equigranular garnet-muscovite-biotite granite dykes, and associated veins of aplite and pegmatite (up to 30 cm wide), intrude the Mount Newsome Granodiorite. The origin of the dykes and veins is uncertain. They could be a product of partial melting of metasedimentary country rocks by the granodiorite, or the intrusion of late-stage fractionated material.|16-MAY-23
23827|Mount Newsome Granodiorite|Age reasons|Webb & McDougall (1968) obtained a K-Ar biotite age corrected to 370 Ma. Rb-Sr dating of several biotite-whole rock samples by P. Carr (unpublished data) gave an age range of 372 to 382 Ma (Middle Devonian).|16-MAY-23
23827|Mount Newsome Granodiorite|References|WEBB, A.W. & MCDOUGALL, I., 1968: The geochronology of the igneous rocks of Eastern Queensland. Journal of the Geological Society of Australia, 15, 313-346.|16-MAY-23
12978|Mount Norna Quartzite|Name source|Mount Norna, 30 km southeast of Cloncurry, latitude 20o55'10"S, longitude 140o42'E, (7056 685867). Mount Norna is plotted incorrectly on the Cloncurry 1:250 000 topographic map (SF 54-2 edition 1) and on the Cloncurry 1:100 000 topographic map (7056) but it is shown in its correct position on the 1:39 600 topographic map in Honman (1939). The Mount Norna mine (otherwise known as the Mountain Home or Mount Norma mine) occurs on the northeast slopes of the mountain.|16-MAY-23
12978|Mount Norna Quartzite|Geomorphic expression|This formation is generally ridge forming and has a rugged to gently rounded surface. The metabasalt and dolerite are mostly expressed as valleys.|16-MAY-23
12978|Mount Norna Quartzite|Type section locality|The middle portion of the type section that was used by Carter et al. (1961) to define the Soldiers Cap Formation is the proposed type section of the Mount Norna Quartzite. It commences at a point 800 m southeast of the Mountain Home (Mount Norna) mine at latitude 20o55'20"S, longitude 140o42'10"E (7056 690862) and exteands for 2.5 km in an east-northeasterly direction to a point at latitude 20o54'40"S, longitude 140o43'30"E (7056 713875). This section contains from west to east, 650 m of cross-bedded quartzite, meta-siltstone and phyllite, 150 m of metabasalt with thin quartzite intercalations, and about 1500 m of cross-bedded quartzite, phyllite, chert and silicified siltstone.|16-MAY-23
12978|Mount Norna Quartzite|Extent|The Mount Norna Quartzite occurs in a complex tightly folded zone and crops out discontinuously between 8 km north and 120 km southeast of Cloncurry. Outcrop in the Cloncurry 1:100 000 Sheet area has been mapped in detail by Glikson & Derrick (1970); exposures in the Mount Angelay & Selwyn 1:100 000 Sheet areas have been delineated by private company work and air-photo interpretation.|16-MAY-23
12978|Mount Norna Quartzite|Thickness range|The thickness of this formation ranges from 1300 m in the north to 2700 m in the south.|16-MAY-23
12978|Mount Norna Quartzite|Lithology|Metamorphosed cross-bedded sandstone, feldspathic sandstone, siliceous siltstone and phyllite, with numerous intercalations of metabasalt and amphibolites. Skarn, quartzofeldspathic gneiss and gahnite quartzite are associated with zinc mineralisation in a belt extending from the Fullarton River south to the McKinlay River.|16-MAY-23
12978|Mount Norna Quartzite|Relationships and boundaries|The Mount Norna Quartzite overlies the Llewellyn Creek Formation conformably, and is overlain conformably by the Toole Creek Volcanics and unconformably by the Corella Formation, Roxmere Quartzite and Mesozoic sediments. The Mount Norna Quartzite is intruded by dolerite dykes and sills, and by the Naraku and Williams Granites.|16-MAY-23
12978|Mount Norna Quartzite|Age reasons|Precambrian, probably Carpentarian.|16-MAY-23
12978|Mount Norna Quartzite|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1977|16-MAY-23
12978|Mount Norna Quartzite|Proposed publication|Queensland Government Mining Journal 1976|16-MAY-23
12978|Mount Norna Quartzite|Comments|Remarks: Honman (1939) included this unit in his Upper or Volcanic stage of the Soldiers Cap series. Carter et al. (1961) described this succession as "interbedded metabasalts and medium-grained quartzite (with subordinate pelites)", but did not formally define it as a subdivision of the Soldiers Cap Formation. Glikson & Derrick (1970) used the name Weatherly Creek Quartzite for these rocks in an unpublished BMR Record but Glikson (1972) later published the informal stratigraphic term Mount Norna Quartzite. In Plumb & Derrick (1975) the unit is called the Weatherly Creek Quartzite. The publication by Glikson (1972) of the geographic term Mount Norna has precedence over the alternative term, Weatherly Creek. The Mount Norna Quartzite appears to be host to stratabound zinc mineralisation of the Broken Hill type.B43|16-MAY-23
23828|Mount Observatory Granite|Name source|Mount Observatory at 8351-433399. The grid reference is based on the AGD66 datum.|16-MAY-23
23828|Mount Observatory Granite|Geomorphic expression|The granite forms gentle to moderately undulating terrain, with local tors, such as at Mount Observatory in the northwest where extensive rocky platforms cover about 1 km2. Such exposures are rare, the granite mostly forming isolated boulder-sized outcrop.  On the Landsat 5 TM (1-4-7 BGR) image, the Mount Observatory Granite is represented by a diffuse bluish hue. It has a weak to moderate magnetic response, but has very strong Th and strong K and U responses.|16-MAY-23
23828|Mount Observatory Granite|Type section locality|Mount Observatory, a prominent tor at 8351-433399.  The grid reference is based on the AGD66 datum.|16-MAY-23
23828|Mount Observatory Granite|Description at type locality|Typical light grey, fine to medium-grained biotite granite crops out.|16-MAY-23
23828|Mount Observatory Granite|Extent|A northwest trending body approximately 15 km long and 6 km wide, with a centre 7 km northeast of Peak Vale homestead.|16-MAY-23
23828|Mount Observatory Granite|Lithology|Grey to light grey, fine to medium-grained biotite granite with common metasedimentary xenoliths up to 1 m and sparse quartz eyes. Biotite clots or glomercrystic intergrowths up to 4 mm across are also a characteristic feature.|16-MAY-23
23828|Mount Observatory Granite|Relationships and boundaries|Intrudes the Monteagle Quartzite of the Anakie Metamorphic Group. It is faulted against the Kilmarnock Granodiorite along the Kettle Creek Fault, but the intrusive relationships with that unit are unknown.  Numerous small basalt plugs of the Hoy Basalt were intruded along the faulted boundary between the Mount Observatory Granite and Kilmarnock Granodiorite.|16-MAY-23
23828|Mount Observatory Granite|Age reasons|Webb & McDougall (1968) obtained a K-Ar biotite age corrected to 373 Ma. The age is therefore probably Middle Devonian.|16-MAY-23
23828|Mount Observatory Granite|References|WEBB, A.W. & MCDOUGALL, I., 1968: The geochronology of the igneous rocks of Eastern Queensland. Journal of the Geological Society of Australia, 15, 313-346.|16-MAY-23
25735|Mount Oxide Chert Member|Name source|Mount Oxide mine, 24 km north of Mammoth mine at 310453 on the Mount Oxide 1:100 000 Sheet area.|16-MAY-23
25735|Mount Oxide Chert Member|Unit history|The rocks now included in the Mount Oxide Chert Member were mapped as part of the Paradise Creek Formation by Carater & others (1961). Cavaney (1975) proposed to name these rocks "Oxide Chert Member".|16-MAY-23
25735|Mount Oxide Chert Member|Type section locality|Holostratotype: The holostratotype of the Mount Oxide Chert Member forms the basal part of the holostratotype of the Paradise Creek Formation. It crops out as a 2 m band of thinly bedded chert at GR 195146 in the Mammoth Mines 1:100 000 Sheet area, about 1.5 km along Paradise Creek from its junction with Gunpowder Creek.|16-MAY-23
25735|Mount Oxide Chert Member|Extent|The unit crops out as a thin band from th Kennedy Gap 1:100 000 Sheet area in the south to the Gregory Downs 1:100 000 Sheet area in the north. It is almost always present at the base of the Paradise Creek Formation except in the Lawn hill 1:100 000 Sheet area.|16-MAY-23
25735|Mount Oxide Chert Member|Thickness range|The unit ranges from less than 1 m to 10 m in thickness.|16-MAY-23
25735|Mount Oxide Chert Member|Lithology|The unit everywhere comprises thin bedded to laminated chert, rarely interbedded with siltstone.|16-MAY-23
25735|Mount Oxide Chert Member|Relationships and boundaries|The unit is a member at the base of the Paradise Creek Formation. It conformably overlies the Gunpowder Creek Formation. It is recognised as a thinly bedded chert overlying carbonaceous shale and underlying siltstone and dolomite.|16-MAY-23
25735|Mount Oxide Chert Member|Age reasons|Mid Proterozoic (Carpentarian).|16-MAY-23
25735|Mount Oxide Chert Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
13029|Mount Philp Breccia|Name source|Revision of Mount Philp Agglomerate defined by Carter & others (1961) and revised by Derrick, Wilson & Hill (1977). Derivation: Named after Mount Phillp in S of Mary Kathleen 1:100 000 Sheet area, Cloncurry 1:250 000 Sheet area (Carter & others, 1961).|16-MAY-23
13029|Mount Philp Breccia|Unit history|Mount Philp Agglomerate (Carter & others, 1961; Carter & Opik, 1963; Derrick & others, 1977).|16-MAY-23
13029|Mount Philp Breccia|Type section locality|As selected by Carter & others (1961) the type section for the Mount Philp Agglomerate is from the edge of the unit, southeast of Ballara, to the waterhole at Latitude 20o58'25"S, Longitude 139o59'20"E. Derrick & others (1977), in their revision of the unit, stated that the type section extends 2.5 km SE from the edge of the outcrop of the formation about 0.5 km SE of the abandoned township of Ballara to a large waterhole on Read Creek. However, the waterhole referred to by Carter & others is probably Pelican Waterhole rather than one on Reid Creek some 2 km to the north. Pelican Waterhole is at about Latitude 20o59'00"S, Longitude 139o58'20"E, GR 932792, Mary Kathleen 1:100 000 Sheet area. The best exposures of the unit are rock plataforms at Pelican Waterholeand for about 200 m upstream to the west, and it is proposed that these exposures be considered the type area for the Mount Philp Breccia. Here the unit consists of angular to slightly rounded fragments mostly of amphibolitic metabasalt, calc-silicate rocks and pegmatite, enclosed in a bright pink, fine-grained igneous-textured rock containing small euhedral amphibole and magnetite phenocrysts.|16-MAY-23
13029|Mount Philp Breccia|Extent|The main outcrop of the un;it covers about 15 km2 in SE corner of Mary Kathleen and NE corner of Duchess 1:100 000 Sheet areas, and other outcrops are present to the S, in the E part of the Duchess 1:100 000 Sheet area, Cloncurry and Duchess 1:250 000 Sheet areas.|16-MAY-23
13029|Mount Philp Breccia|Lithology|The unit consists of breccia formed of disoriented and mainly angular fragments, some several metres across, of various rock types - metabasalt, amphibolite, banded and massive calc-silicate granofels, quartzite, micaceous schist, albitite, quartz-feldspar pegmatite - enclosed in a pink to red igneous-textured groundmass formed of small euhedral amphibole and magnetite phenocrysts and fine-grained subhedral albite laths. Most of the rock types present as fragments in the breccia can be matched with rock types present in adjacent Corella Formation.|16-MAY-23
13029|Mount Philp Breccia|Relationships and boundaries|The breccia cuts banded calc-silicate rocks mapped as Corella Formation and is intruded by meta-dolerite.|16-MAY-23
13029|Mount Philp Breccia|Age reasons|Proterozoic.|16-MAY-23
13029|Mount Philp Breccia|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
13029|Mount Philp Breccia|Comments|Remarks: Fragments in the breccia are mostly derived from the adjacent Corella Formation, and were metamorphosed before being incorporated in the breccia. The unit is therefore much younger than the Corella Formation, and is no longer regarded as part of the Mary Kathleen Group. Textures and field relationships indicate an intrusive rather than an extrusive origin;. For these reasons the name of the unit is changed from Mount Philp Agglomerate (which implies a volcanic origin) to Mount Philp Breccia (a descriptive, rathern than genetic, lithological designation).|16-MAY-23
13029|Mount Philp Breccia|Defn Reference|82/22920|16-MAY-23
13029|Mount Philp Breccia|Status|1|16-MAY-23
24404|Mount Sircom Microgranodiorite|Name source|Mount Sircom pastoral holding, within which the southern parts of the microgranodiorite crop out; Mount Sircom, a prominent, solitary group of hills, at GR 7561-433578, however the unit is not exposed at this locality.|16-MAY-23
24404|Mount Sircom Microgranodiorite|Unit history|Interpreted by White (1959) and Branch (1966) as part of the Prestwood Microgranite, which is a biotite microgranite rather than a biotite-hornblende microgranodiorite.|16-MAY-23
24404|Mount Sircom Microgranodiorite|Geomorphic expression|Forms subdued rolling grasslands with areas of alluvium or boggy black soil, and low knolls covered with rounded boulders mostly about 30 to 60 cm in diameter.|16-MAY-23
24404|Mount Sircom Microgranodiorite|Type section locality|Hills just north of McDonald Creek, about GR 7561-498667; this area is representatiave of the most common, more biotite-rich variant of the microgranodiorite.|16-MAY-23
24404|Mount Sircom Microgranodiorite|Extent|Crops out over an area of about 15 km2 between the Gilbert River and the Cumberland Range (lower to middle reaches of McDonald Creek, and two unnamed creeks joining the Gilbert River to the south) in a hook-like shape. Extremities are at GR 7561-510680, -490607, -444610, and 453656, with the 3 km-deep embayment of the "hook" in the southeast.|16-MAY-23
24404|Mount Sircom Microgranodiorite|Lithology|Strongly porphyritic biotite-hornblende microgranodiorite,* with large phenocrysts of quartz, plagioclase and alkali feldspar, and smaller phenocrysts of altered hornblende and biotite. The rock is commonly pink or grey in hand specimen, with pink alkali feldspar and green plagioclase phenocrysts. Richer in hornblende and poorer in biotite in places (e.g. central western portion).|16-MAY-23
24404|Mount Sircom Microgranodiorite|Relationships and boundaries|Intrudes Robertson River and Townley Formations, without noticeable contact effects. In one place there is indisputable evidence that it intrudes part of the Cumberland Range Volcanics, which are similar to and correlated with (in time, at least) some of the Newcastle Range Volcanics, dated by Black (1973) at 318+/-5 m.y.  The Mount Sircom Microgranodiorite is therefore considered to be mid-Carboniferous.  Somewhat similar rocks, which may in part be equivalent, occur in the Mount Darcy Microgranodiorite.|16-MAY-23
24404|Mount Sircom Microgranodiorite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24404|Mount Sircom Microgranodiorite|Proposer|Mackenzie D.E.|16-MAY-23
26058|Mount Start Member|Name source|Mount Start, latitude 20o59'S, longitude 140o17'E, 38 km southwest of Cloncurry, in the Marraba 1:100 000 Sheet area.|16-MAY-23
26058|Mount Start Member|Geomorphic expression|Low rounded ridges and hills, e.g.,  Mounts Start, Finish, Connor, Brownie and Sheaffe.|16-MAY-23
26058|Mount Start Member|Type section locality|A section from west to east across Mount Start, latitude 20o59'S, longitude 140o17'E. This section consists of 90 m of intricately folded laminated fine-grained calcareous sandstone and siliceous shale.|16-MAY-23
26058|Mount Start Member|Extent|In the Marraba 1:100 000 Sheet area this member forms a nearly continuous thin band in the Duck Creek and Bulonga anticlines. It probably extends south into the Malbon 1:100 000 Sheet area.|16-MAY-23
26058|Mount Start Member|Thickness range|Thickness ranges from about 120 m in the east to about 10 m in the west.|16-MAY-23
26058|Mount Start Member|Lithology|Laminated fine-grained calcareous sandstone, quartzite, crenulated siliceous shale, friable decalcified sandstone. Some of the crenulated bedding may be of algal origin. Leaching and silicification are restricted to the elevated parts of the member.|16-MAY-23
26058|Mount Start Member|Relationships and boundaries|The Mount Start Member is underlain conformably by the Cone Creek Metabasalt Member, and overlain conformably by the Timberoo Member of the Marraba Volcanics.|16-MAY-23
26058|Mount Start Member|Comments|Remarks: The Mount Start Member is present as a narrow, low ridge in the vicinity of the Marraba Volcanics type section (I.e., near latitude 20o53'S, longitude 150o14'E (Carter et al., 1961) but this outcrop is not wide enough to be shown on the Marraba 1:100 000 Geological Sheet. The member has been delineated 11 km along strike to the southwest of the type section and in areas to the north and east.|16-MAY-23
24405|Mount Webster Granodiorite|Name source|Mount Webster, 22.5 km south of Mount Surprise at GR 134689 (Mount Surprise 1:100 000 Sheet area).|16-MAY-23
24405|Mount Webster Granodiorite|Unit history|Previously mapped as Forsayth Granite (White, 1962).|16-MAY-23
24405|Mount Webster Granodiorite|Type section locality|Along the north-south trending fence-line, about 2 km west of Sandy Creek, from where it meets another fence at GR 152666 (Mount Surprise 1:100 000 Sheet area) south to where it turns east at GR 147610. Outcrops consist of pale pinkish-grey medium-grained, equigranular, muscovite-biotite granodiorite, which is slightly foliated in places and locally cut by pegmatitic veins.|16-MAY-23
24405|Mount Webster Granodiorite|Description at type locality|GR 123450 (Einasleigh 1:100 000 Sheet area), where pinkish-grey fine to medium-grained equigranular biotite granodiorite containing minor muscovite is exposed. The granodiorite in this area is characterised by a strong, locally intense, steeply plunging lineation defined by elongate quartz and mica grains.|16-MAY-23
24405|Mount Webster Granodiorite|Extent|An elongate batholith, about 200 km2 in araea, in the southern part of the Mount Surprise 1:100 000 Sheet area and extending into the Einasleigh Sheet area. The batholith has several large screens or roof pendants of metamorphics; and there is a northeast-trending 'hook'-shaped extension at its southern end.|16-MAY-23
24405|Mount Webster Granodiorite|Lithology|As described at the type area and reference locality: pinkish-grey, fine to medium-grained, equigranular muscovite-biotite granodiorite, locally grading into granite. The rocks are weakly to strongly foliated and in thin section a mortar texture is commonly developed. Towards the southern end of the batholith a strong lineation defined by elongate quartz grains and mica aggregates is present. Enclaves of Einasleigh Metamorphics are locally abundant and large screens or roof pendants up to several kilometres long have been mapped.|16-MAY-23
24405|Mount Webster Granodiorite|Relationships and boundaries|The unit intrudes the Proterozoic Einasleigh Metamorphics. On its western edge it is in contact with the Mount Juliet Granite but the intrusive relationship is not known. It is intruded by numerous uralitised dolerite dykes of probable late Palaeozoic age.|16-MAY-23
24405|Mount Webster Granodiorite|Age reasons|Probably Middle Proterozoic, because of the local strong deformation evidenced by the lineation and mortar texture. A Siluro-Devonian age is a possibility, although nearby Siluro-Devonian granitoids such as the Puppy Camp Granodiorite do not show such intense deformation.|16-MAY-23
24405|Mount Webster Granodiorite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24405|Mount Webster Granodiorite|Proposer|Warnick J.V.|16-MAY-23
33436|Mountefontein Metamorphics|Name source|The unit is named after Mountefontein homestead that is situated almost on the centre of the outcrop.|16-MAY-23
33436|Mountefontein Metamorphics|Unit history|Murphy & others (1976) included this unit in a sequence of undifferentiated Palaeozoic metamorphics (unit Pz).  The unit is meta-sedimentary in character, and clearly of a different lithology to the surrounding Chahpingah Meta-Igneous Complex from which it is herein separated.|16-MAY-23
33436|Mountefontein Metamorphics|Geomorphic expression|The unit is exposed as elevated ridges and hills covering an area of around 12 km2.  The outcrop area has been mostly cleared for grazing, although small patches dense woodland still remain. Exposure is generally poor and limited mostly to creeks and gullies.|16-MAY-23
33436|Mountefontein Metamorphics|Extent|The unit occurs about 30km due west of Kingaroy, occupying a roughly rectangular area of around 12 km2.|16-MAY-23
33436|Mountefontein Metamorphics|Lithology|The unit consists mainly of thinly interlayered biotite gneiss and fine schist, intruded by scattered biotite leucogranite sills and migmatitic veins. Thick horizons of thinly banded haematitic meta-chert occur sporadically throughout the unit.  Layering within the unit trends west-south-west parallel to the layering in the enclosing Chahpingah Meta-Igneous Complex.|16-MAY-23
33436|Mountefontein Metamorphics|Relationships and boundaries|The unit has a concordant relationship with the Chahpingah Meta-Igneous Complex: Both units are intruded by various phases of the Boondooma Igneous Complex.|16-MAY-23
33436|Mountefontein Metamorphics|Age reasons|The grossly concordant relationship, similar metamorphic grade, and presence of granitic sills suggest that the Mountefontein Metamorphics and Chahpingah Meta-Igneous Complex share a similar tectonic history and age (i.e. late Carboniferous).|16-MAY-23
33436|Mountefontein Metamorphics|Correlations|See AGE REASONS above section for correlative comment.|16-MAY-23
33436|Mountefontein Metamorphics|Comments|GEOPHYSICAL EXPRESSION:: The unit has a uniformly low magnetic response on geophysical images, but has characterisitic mauve to purple colour on the Ternary K-Th-U (RGB) radiometric image.STRUCTURE:: The major metamorphic layering in the unit dips at moderate to steep angles to the north-north-west. No significant internal folding was noted.|16-MAY-23
33436|Mountefontein Metamorphics|References|MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.|16-MAY-23
13391|Mullera Formation|Name source|Unit name derived from Mullera parish (approximately 18°33'00"S 138°06'00"E)  in the county of Mueller, Queensland, in the west LAWN HILL 1:250 000 mapsheet (Carter, 1959).|
13391|Mullera Formation|Unit history|Unit was originally mapped as the “Mullera Formation” by Carter (1959). Name has not been revised since.|
13391|Mullera Formation|Constituents|The Mullera Formation comprises two formal subdivisions (members) and three informal subdivisions. They are, in ascending stratigraphic order: LPsm1: “lower mudstone member” - Mainly shale and siltstone, with numerous thin sandstone and ironstone beds. In places, thin to medium beds of indurated, white fine-grained sandstone occur in background of laminated siltstone and shale. Lenticular beds and gutter casts common, decrease in abundance up section. Some thicker sandstone beds near the contact with the overlying Train Range Ironstone Member have been termed LPsm1s (Sweet, 2017).  Train Range Ironstone Member: Comprises a series of ferruginous sandstone and ironstone beds that are laterally gradational. Ironstones at depth consist of hematite, chamosite and siderite, have oolitic texture, and are mainly hematitic or limonitic at the surface. Unit consists of coarsening-upwards cycles, with sandstones/ironstones displaying wavy bedding and hummocky cross-stratification, and rare intraclast conglomerate (Sweet, 2017).  LPsm2: “middle mudstone member” - Similar lithologies to LPsm1, but with a higher proportion of shale. Predominantly grey-green shale with minor siltstone in outcrop. Sandstones occur toward top of unit in some places, indicating gradational contact with Middle Creek Member in some locations and a sharp contact in others (Sweet, 2017). Middle Creek Member: Predominantly a series of resistant quartz-rich sandstone units separated by laminated and thin-bedded mudstone, with some speckles of possible hematite after chamosite or glauconite in the sandstone. Sandstone beds display medium- to large-scale trough cross-bedding, and bed tops in upper sections of unit display wave/interference ripple marks. Overall, the unit displays coarsening upwards cycles (Sweet, 2017). LPsm3:”upper mudstone member” – Similar facies to LPsm1 and LPsm2. Basinal mudstones punctuated by fine-grained sandstones (Sweet, 2017).|
13391|Mullera Formation|Geomorphic expression|The unit is predominantly recessive, except for the more resistant Train Range Ironstone and Middle Creek Sandstone members (Rawlings et al, 2008). The informal fine-grained units are poorly exposed, forming rubble-strewn slopes, with the best exposures in gullies (Sweet, 2017).|
13391|Mullera Formation|Type section locality|Type section nominated by Carter (1959), starting from approximately (pre-AGD66) 18°32’15”S 138°06’30”E, extending for approximately 6.25 miles (about 10 km) on true bearing of 128°, in the LAWN HILL 1:250 000 mapsheet in Queensland.|
13391|Mullera Formation|Type section locality|Lawn Hill 4-mile sheet - E54/9. From lat. 18deg32'15" S, long. 138deg06'30" E on true bearing 128deg for a distance of 6.25 miles.|16-MAY-23
13391|Mullera Formation|Extent|The Mullera Formation outcrops on the LAWN HILL 1:250 000 mapsheet in Queensland, and the MOUNT DRUMMOND and CALVERT HILLS 1:250 000 mapsheets in the Northern Territory (Rawlings et al, 2008).|
13391|Mullera Formation|Thickness range|Thickness not recorded at type section. Unit thickness varies considerably, up to a maximum thickness of approximately 2130 m (Carter et al, 1961), but is more typically approximately 1100 to 2130 m (Carter et al, 1961). Individual subdivision thicknesses: LPsm1: “lower mudstone member”: 300 to 700 m-thick (Sweet, 2017). Train Range Ironstone Member: 40 to 150 m-thick (Sweet, 2017).  LPsm2: “middle mudstone member”: 210 to 690 m-thick (Sweet, 2017). Middle Creek Member: up to 150 m-thick (Sweet, 2017). LPsm3:”upper mudstone member”: 180 to 500 m-thick (Sweet, 2017).|
13391|Mullera Formation|Lithology|Essentially well-bedded siltstone, shale and fine-grained sandstone. Several quartzitic sandstone sequences, one including oolitic, and another ironstone (Carter, 1959).|
13391|Mullera Formation|Depositional environment|The Mullera Formation as a whole is interpreted as a marine shelf, partly above storm wave-base (tempestite facies), and partly below (organic-rich and shale-rich facies). Periodic shallowing above fair weather wave-base is represented by thickly-bedded, shoreface to intertidal sandstone of the Middle Creek Sandstone Member, which is interpreted as resulting from repeated shallowing events (Rawlings et al, 2008). The Train Range Ironstone Member displays abundant hummocky cross-stratification (Sweet, 2017), which supports a similar depositional environment interpretation to the Middle Creek Sandstone Member.|
13391|Mullera Formation|Relationships and boundaries|In the MOUNT DRUMMOND and CALVERT HILLS 1:250 000 mapsheets, the Mullera Formation lies conformably on the Elizabeth Formation and the Constance Sandstone, respectively, and is unconformably overlain by Georgina Basin units (Rawlings et al, 2008). On the LAWN HILL 1:250 000 mapsheet, the Mullera Formation conformably overlies the Elizabeth Sandstone, and conformably underlies the Tidna Sandstone (Sweet, 2017).|
13391|Mullera Formation|Identifying features|The oolitic ironstone of the Train Range Ironstone Member, bracketed above and below by recessive, fine-grained units, is distinct in outcrop.|
13391|Mullera Formation|Structure and Metamorphism|The variable thickness of the Mullera Formation may be due to possible diachroneity in deposition or the development of local depocentres in the lower parts of the formation (Rawlings et al, 2008). The Mullera Formation is known to outcrop across a series of structural basins (Sweet, 2017).|
13391|Mullera Formation|Age reasons|Maximum depositional ages derived from U-Pb SHRIMP dating of detrital zircons: Bukalara Sandstone (stratigraphically overlies Mullera Formation): GA sample 2777481 – 1316 ± 27 Ma (Kositcin et al, 2020). Constance Sandstone (stratigraphically underlies Mullera Formation): GA sample 2678595 – 1591 ± 18 Ma (Anderson et al, 2019). Constance Sandstone (stratigraphically underlies Mullera Formation): GA sample 1987412 – 1599 ± 19 Ma (Anderson et al, 2019). Constance Sandstone (stratigraphically underlies Mullera Formation): GA sample 2678593 – 1578 ± 53 Ma (Anderson et al, 2019). Constance Sandstone (stratigraphically underlies Mullera Formation): GA sample 2678591 – 1569 ± 37 Ma (Anderson et al, 2019). Constance Sandstone (stratigraphically underlies Mullera Formation): GA sample 2678383 – 1468 ± 36 Ma (Kositcin et al, 2020). Schultz Sandstone Member (stratigraphically underlies Mullera Formation): GA Sample 1990594 - 1577 ± 21 Ma (Carson et al, 2011). Therefore, the potential depositional age range for the Mullera Formation can be considered to extend from ca. 1578 ± 53 Ma to 1316 ± 27 Ma.|
13391|Mullera Formation|Correlations|Based on U-Pb SHRIMP maximum depositional age estimates for the Constance Sandstone (Anderson et al, 2019), the Mullera Formation may be correlative with units of the Favenc package or possibly the overlying Wilton package (Rawlings, 1999) of the McArthur Basin.|
13391|Mullera Formation|Alteration and Mineralisation|Considerable Fe mineralisation, mostly in the form of oolitic hematite, chamosite and siderite at depth, and hematite and limonite at surface due to oxidation and weathering (Carter and Zimmerman, 1960; Carter et al, 1961; Rawlings et al, 2008; Sweet, 2017).|
13391|Mullera Formation|Geophysical Expression|Moderate to high magnetic response, likely due to ironstones and ferruginous sandstones.|
13391|Mullera Formation|Geochemistry|see Carson CJ, Jarrett AJM, Anderson JR, Champion DC and Henson PA, 2020. Exploring for the Future – Whole rock geochemistry data release of sedimentary and igneous rocks from the South Nicholson region, Northern Territory and Queensland. Geoscience Australia, Record 2020/02.|
13391|Mullera Formation|Defn author|E.K. Carter & D.C. Zimmerman, 1960. Constance Range iron deposits, north-western Queensland. BMR Record 1960/75, p10-15.|16-MAY-23
13391|Mullera Formation|Defn author|Elliot Foley, Jack Simmons, Ben Williams, Charles Verdel (Northern Territory Geological Survey), Chris Carson (Geoscience Australia) 07-DEC-2022.|
13391|Mullera Formation|Comments|Standard series 1: 100 000 and 1: 250 000 mapsheet names are shown in uppercase.|
13391|Mullera Formation|References|Anderson JR, Lewis CJ, Jarrett AJM, Carr LK, Henson P, Carson CJ, Southby C and Munson TJ, 2019. New SHRIMP U–Pb zircon ages from the South Nicholson Basin, Mount Isa Province and Georgina Basin, Northern Territory and Queensland. Geoscience Australia, Record 2019/10. 
 **Carson CJ, Hutton LJ, Withnall IW, Perkins WG, Donchak PJT, Parsons A, Blake PR, Sweet IP, Neumann NL and Lambeck A, 2011. Summary of results: Joint GSQ-GA geochronology project Mount Isa region, 2009-2010. Geological Survey of Queensland, Record 2011/03.  **Carson, C. J., Kositcin, N., Anderson, J. R., and Henson, P. A. in prep. A revised Proterozoic tectono-stratigraphy of the South Nicholson region, Northern Territory, Australia - insights from SHRIMP U-Pb detrital zircon geochronology. Australian Journal of Earth Sciences.  **Carter EK, 1959. New stratigraphic units in the Precambrian of north-western Queensland. Queensland Government Mining Journal 60(92), 437–431.  **Carter EK, Brooks JH and Walker KR, 1961. The Precambrian mineral belt of northwestern Queensland. Bureau of Mineral Resources, Bulletin 51.  **Carter EK and Zimmerman DO, 1960. Constance Range iron deposits, northwestern Queensland. Bureau of Mineral Resources, Record 75.  **Kositcin N, Carson CJ, Anderson JR, Doublier MP and Murr J, 2020. Exploring for the Future - New SHRIMP geochronology constraints on the basin evolution of the South Nicholson region. Geoscience Australia, Record 2020/25.  **Rawlings DJ, 1999. Stratigraphic resolution of a multiphase intracratonic basin system: the McArthur Basin, northern Australia. Australian Journal of Earth Sciences 46(5), 703-723.  **Rawlings DJ, Sweet IP and Kruse PD, 2008. Mount Drummond, NT (Second Edition). 1:250 000 Geological Map Series Explanatory Notes, Sheet SE 53-12. Northern Territory Geological Survey, Darwin, Northern Territory.  **Simmons JM, Williams B, Carson, C and Verdel C, 2023a. Mount Drummond, Northern Territory 1:250 000 Geological Map, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.  **Simmons JM, Williams B, Carson, C and Verdel C, 2023b. Mount Drummond, Northern Territory 1:250 000 Geological Map Explanatory Notes, Sheet SE 53-12 (Third Edition). Northern Territory Geological Survey, Darwin, Northern Territory.  **Sweet IP, 2017. The geology of the South Nicholson Group, northwest Queensland. Queensland Geological Record 2017/07.|
13449|Munduran Creek Member|Name source|Munduran Creek; GR 299,800E, 7,379,000N, Gladstone 1:100 000 topographic sheet.|16-MAY-23
13449|Munduran Creek Member|Unit history|Part of The Narrows Beds (Kirkegaard et al, 1970) and part of the Rundle Formation (Henstridge and Missen, 1982).|16-MAY-23
13449|Munduran Creek Member|Type section locality|36 m of oil shale with minor interbeds of claystone and rare impersistent dolomite; from 83.8 to 120.3 m in drill hole ERD 169 (GR 300,999E, 7,380,998N Gladstone 1:100 000 topographic sheet). The dark yellowish-brown to olive brown oil shale contains two major greyish-green claystone beds (from 99.0 to 102.0 m and 111.2 to 115.9 m in type section). Minor clayey oil shale occurs interlayered with the claystone. Other claystone to clayey oil shale beds are recorded from 93.2 to 94.1 m and 96.1 to 97.0 m in type section. A rare yellowish-grey impure dolomite concentration is contained within the type section from 113.8 to 114.0 m. Cyclicity of lithologies is a feature, with oil shale grading upwards through clayey oil shale to claystone, commonly overlain by minor carbonaceous material. Cyclic alternation of lithologies occurs more frequently in the upper oil shale unit.|16-MAY-23
13449|Munduran Creek Member|Extent|Subcrops in an area of about 36 km2 in The Narrows Graben, NW of Gladstone, Queensland. Spase weathered outcrops are recorded. The member has been identified from drill hole core.|16-MAY-23
13449|Munduran Creek Member|Thickness range|36.5 m (estimated true thickness 35.9 m corrected for an apparent dip of 9o in ERD 169) in type section. Range of true thickness of the member as intersected in drill holes is 24.1 m to 52.0 m.|16-MAY-23
13449|Munduran Creek Member|Lithology|Oil shale, dark yellowish-brown to olive brown; calcareous, carbonaceous and clayey cyclicity; very thinly to very thickly bedded (up to 5 m); laminated, brecciated and peloidal in part. Minor interbeds of greyish-green claystone; rare discontinuous yellowish-grey impure dolomite concentrations and very rare dark grey carbonaceous shale. Oil shale beds attenuate towards the east in The Narrows Graben with a corresponding increase in the commonly silty to sandy claystone. Claystone and brecciated clayey oil shale beds often show bioturbation features. Ostracode tests are abundant with minor gastropods, vertebrate remains (crocodile, turtle), fish elements and coprolites.|16-MAY-23
13449|Munduran Creek Member|Relationships and boundaries|The member is conformable with the underlying Humpy Creek Member and is the generally sharp contact between calcareous oil shale and claystone. The upper boundary is conformable with the Telegraph Creek Member and is the contact between oil shale and claystone or, in places, the sharp contact between oil shale and dolomite. The member is faulted against Devonian to Carboniferous rocks of the Curtis Island Group along the western edge of The Narrows Graben.|16-MAY-23
13449|Munduran Creek Member|Age reasons|Mid to late Eocene - as for the Rundle Formation.|16-MAY-23
13449|Munduran Creek Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
13449|Munduran Creek Member|Comments|Note: Drill-core from ERD 169 is stored at Southern Pacific Petroleum's Research and Core Storage Facility located in Gladstone, Queensland.|16-MAY-23
13635|Myally Subgroup|Name source|(For original definition see Carter, et al., 1961, p.97).  From Myally Creek, 185 km north of Mount Isa.|16-MAY-23
13635|Myally Subgroup|Type section locality|The old type section of Myally Beds near Myally Creek is incomplete and faulted (Carter et al. 1961). A new type section of the subgroup cannot be specified because of slight variation in the distribution of the type sections of the constituent formations. However, two excellent reference sections can be noted; one, between Paroo and Conglomerate Creeks along the Mount Isa-Julius dam road, contains all type sections of the constituent formations, but not the type section of the Police Creek Siltstone Member, which is nevertheless present in the reference section. The centre of the section is 16 km southwest of Julius dam or 56 km north-northeast of Mount Isa, latitude 20o15'S, 139o37'E, and its thickness is 3770 metres. A second reference section is located along a line trending due west for 4 km from the Lochness mineral lease, 32 km northwest of Julius dam and 90 km north of Mt Isa. It contains all the constituent formations, and is about 3000 m thick.|16-MAY-23
13635|Myally Subgroup|Extent|The subgroup extends from near Mount Isa up to 200 km north to the Myally Creek-Gregory Downs area. The belt is up to 70 km wide in the north, but narrows to an average width of 20 km in the south. Total extent of the subgroup is near 4000 km2.|16-MAY-23
13635|Myally Subgroup|Thickness range|From top to bottom, the constituent formations and their thickness range are as follows: Lochness Formation - siltstone, sandstone, dolomite 400-1200 m.  Police Creek Siltstone Member - siltstone, rhyolite 0-400 m. Whitworth Quartzite - feldspathic quartzite 650-2000 m. Bortala Formation - quartzite, siltstone 80-700 m. Alsace Quartzite - quartzite 70-600 m.|16-MAY-23
13635|Myally Subgroup|Lithology|The subgroup is a sandstone-siltstone sequence.|16-MAY-23
13635|Myally Subgroup|Relationships and boundaries|The subgroup forms part of the Haslingden Group. It conformably overlies the Eastern Creek Volcanics, and is overlain unconformably by the Mount Isa Group, and conformably or disconformably by the Surprise Creek Beds. The Judenan Beds are probable equivalents of the Myally Subgroup, but until they are redefined, they are excluded from it.|16-MAY-23
13635|Myally Subgroup|Age reasons|Carpentarian: minimum age of about 1650 m.y. set by Sybella Granite intrusive into the time equivalent units west of Mount Isa. Maximum age possibly near 1700 m.y. (Plumb & Derrick, 1975).|16-MAY-23
13635|Myally Subgroup|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
13635|Myally Subgroup|Proposed publication|Queensland Government Mining Journal|16-MAY-23
13635|Myally Subgroup|Comments|Remarks: The name Myally Subgroup refers to those rocks formerly termed the Myally Beds, except for thick sequences of acid lavas and agglomerate which were formerly part of the Myally Beds, but are now thought to be unconformable above the Myally Subgroup (R.J. Cavaney, pers. comm., 1975). Some areas of the Myally Beds are now mapped as Surprise Creek Beds.|16-MAY-23
22494|Myola Granite|Name source|Myola station at GR 3447 77830 in the Homestead 1:100 000 Sheet area. The grid reference is based on the AGD66 datum.|16-MAY-23
22494|Myola Granite|Unit history|The Myola Granite was previously included in the Lolworth Igneous Complex by Wyatt & others (1971), Clarke & Paine (1970) and Paine & others, (1971).|16-MAY-23
22494|Myola Granite|Type section locality|A small knoll at GR 3397 77795 south of the Myola to Lolworth road and north of Horseshoe Lagoon in the Lolworth 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
22494|Myola Granite|Description at type locality|Here a cream to pink, medium grained, biotite-muscovite granite forms a low knoll. The rock is non-magnetic and comprises quartz, K-feldspar, altered plagioclase, muscovite minor biotite and opaques.|16-MAY-23
22494|Myola Granite|Extent|The Myola Granite crops out over about 6km2 in the northwest of the Homestead 1:100 000 Sheet area and the northeast of the Lolworth 1:100 000 Sheet area. Southwest of Myola, the granite forms low hills across the Myola to Lolworth road.|16-MAY-23
22494|Myola Granite|Lithology|Only a few outcrops of the Myola Granite have been examined. All are leucocratic biotite granites similar to that at the type locality.|16-MAY-23
22494|Myola Granite|Relationships and boundaries|The Myola Granite is a leucocratic granite similar to the Grasstree Suite. However, it is geochemically more like the Amarra Suite with which it is included.|16-MAY-23
22494|Myola Granite|Age reasons|The Myola Granite is Late Silurian to Early Devonian in age. A K-Ar age of 398 +/- 12 Ma was recorded by Webb (1971), from a sample from near the type locality.|16-MAY-23
22494|Myola Granite|Comments|The Myola granite is non-magnetic|16-MAY-23
22494|Myola Granite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
13663|Mytton Formation|Name source|Parish of Mytton, County of Philp.|16-MAY-23
13663|Mytton Formation|Unit history|The unit was previously mapped as part of the Broken River Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
13663|Mytton Formation|Geomorphic expression|Because of the abundant resistant sandstone beds, the unit generally forms hilly topography with well-defined strike ridges.|16-MAY-23
13663|Mytton Formation|Type section locality|In the Broken River between 7859-589449 (base) and 578447 (top).  The grid reference is based on the AGD66 datum.   REFERENCE SECTION: (1) Gorge Creek between 7859-668513 (base) and 632517 (top) - the section is complexly folded, but is at least 940 m thick; (2) GSQ Clarke River 2 borehole from 139 m to 389.89 m (Law, 1986).|16-MAY-23
13663|Mytton Formation|Description at type locality|The section consists of 450 m of alternating mudstone and mainly fine-grained, medium to thick-bedded sublithic arenite.  See Withnall & others (1988, figure 31, and pages 64-66).|16-MAY-23
13663|Mytton Formation|Extent|A sinuous folded belt from the hinge of the Atherton Anticlinorium at about 7859-580550 around the hinge of the Broken River Anticlinorium to about 7858-670380 near 'Craigie'.  It also occurs in a narrow belt about 10 km long west of 'Pandanus Creek'.  The grid reference is based on the AGD66 datum.|16-MAY-23
13663|Mytton Formation|Thickness range|450m at type section.|16-MAY-23
13663|Mytton Formation|Lithology|Grey mudstone and very fine to coarse-grained sublithic arenite, and lesser granule to pebble conglomerate, oncolitic/oolitic conglomerate, and oolitic and bioclastic limestone.  The mudstones are massive and bioturbated or laminated, ripple cross-laminated with wave and current ripple marks.  Arenites are typically massive, graded, or laminated with dish structures, hummocky cross-stratification, flutes, and ripple marks.|16-MAY-23
13663|Mytton Formation|Fossils|The Mytton Formation mainly contains lycopod fragments, and also minor tabulate corals, crinoid ossicles, brachiopods, bivalves, bryozoans, and rare stromatoporoids, trilobites and fish fragments.  In the Broken River-Gorge Creek area, the unit is nearly barren of fossils.|16-MAY-23
13663|Mytton Formation|Relationships and boundaries|The Mytton Formation is the uppermost part of the Broken River Group.  It apparently conformably overlies the Papilio Mudstone, and is overlain with a slight angular unconformity by the Bulgeri Formation of the Bundock Creek Group.  It contains the Stanley Limestone Member. Near 'Pandanus Creek', it apparently conformably overlies the Chinaman Creek Limestone.|16-MAY-23
13663|Mytton Formation|Age reasons|The age is late Givetian and possibly Frasnian (Mawson & Talent, unpublished data) based on fossil evidence.|16-MAY-23
13663|Mytton Formation|References|LAW, S.R., 1986:  GSQ Clarke River 2 - preliminary lithological log and composite log.  Geological Survey of Queensland, Record 1986/7 (unpublished). **WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. **WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of 	Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes. **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River 	area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
24415|Myubee Igneous Complex|Name source|Named after Myubee railway siding on the Mount Isa-Townsville railway line, about 13.5 km NW of Duchess, Duchess 1:100 000 Sheet area (Duchess 1:250 000 Sheet area).|16-MAY-23
24415|Myubee Igneous Complex|Unit history|Mapped as dolerite and Wonga Granite by Carter & Opik (1963).|16-MAY-23
24415|Myubee Igneous Complex|Type section locality|About 16.5 km N of Duchess, from GR 775546 to GR 798535. Here the complex consists of an outer zone of foliated, medium-grained biotite-hornblende granite with some aplite, leucogranite and pegmatite (mainly as veins), and an inner zone of gabbro; the lithologies are described below.|16-MAY-23
24415|Myubee Igneous Complex|Extent|The complex forms a small circular outcrop about 1.5 to 2 km in diameter, 9 km NE of Myubee railway siding.|16-MAY-23
24415|Myubee Igneous Complex|Lithology|The complex consists of a gabbro plug or stock, partly encircled by granite similar to the Revenue and Overlander Granites. The gabbro contains olivine, orthopyroxene, clinopyroxene, hornblende, plagioclase, primary biotite and opaque minerals, and locally, large inclusions of calc-silicate rocks. It is differentiated from olivine-rich norite through pyroxene gabbro, hornblende gabbro and hornblende leucogabbro containing small segregations of pegmatoidal diorite rich in coarse green hornblende and white feldspar grains, to pegmatoidal hornblende diorite. The gabbro is converted locally to medium-grained amphibolite around the margins where it is in contact with the granite, and is cut by veins of aplite, biotite leucogranite, foliated biotite granite, and pegmatite. The granite associated with the gabbro is porphyritic (in feldspar) to even-grained, medium-grained, generally strongly foliated and, locally, relatively rich in hornblende and especially biotite. It contains rare inclusions of coarse-grained granite and large pendants of calc-silicate rocks.|16-MAY-23
24415|Myubee Igneous Complex|Relationships and boundaries|The Myubee Igneous Complex intrudes the Corella Formation and is cut by an apparently unmetamorphosed dolerite dyke.|16-MAY-23
24415|Myubee Igneous Complex|Age reasons|Proterozoic.|16-MAY-23
24415|Myubee Igneous Complex|Proposed publication|Blake & others, in preparation.|16-MAY-23
24415|Myubee Igneous Complex|Comments|Remarks: The gabbro of the complex may be correlated with the dolerite of the Mount Erle Igneous Complex to the south, and with the Lunch Creek Gabbro in the Marraba 1:100 000 Sheet area to the northeast (Derrick, 1980). The potassic granite may be a correlative of the Revenue and Overlander Granites. The gabbro forms a net-veined complex with the granite. An analogous relationship exists to the south where the dolerite of the Mount Erle Igneous Complex is interpreted to be younger than the associated granite, and to the northeast where Derrick (1980) regarded the Lunch Creek Gabbro to be probably older than the closely associated Burstall Granite.|16-MAY-23
24415|Myubee Igneous Complex|Defn Reference|82/22920|16-MAY-23
24415|Myubee Igneous Complex|First Reference|81/21497|16-MAY-23
24415|Myubee Igneous Complex|Proposer|Bultitude R.J.|16-MAY-23
24415|Myubee Igneous Complex|Resdate|21-FEB-1980|16-MAY-23
24416|Mywyn Granite|Name source|Mywyn homestead situated at GR 191190 (Einasleigh 1:100 000 Sheet area).|16-MAY-23
24416|Mywyn Granite|Unit history|Previously mapped as McKinnons Creek Granite by White (1962).|16-MAY-23
24416|Mywyn Granite|Type section locality|A group of hills within grid square 3215 (Einasleigh 1:100 000 Sheet area). Grey, strongly foliated porphyritic biotite granite is exposed. The foliation is defined by aligned K-feldspar megacrysts up to 3 cm long and by flattened and aligned quartz grains. Some pegmatite veins and xenoliths of biotite gneiss occur in places.|16-MAY-23
24416|Mywyn Granite|Extent|A small irregularly shaped pluton with maximum dimensions of 12 by 5 km, centred about 10 km east-southeast of Mywyn homestead; it has a strongly embayed margin and numerous roof pendants.|16-MAY-23
24416|Mywyn Granite|Lithology|Grey to pink, generally strongly foliated, porphyritic biotite granite as described for the type area. K-feldspar megacrysts constitute almost 50 percent of the rock in some places. Where the foliation is weaker, the megacrysts are randomly orientated.|16-MAY-23
24416|Mywyn Granite|Relationships and boundaries|The Mywyn Granite intrudes the Einasleigh Metamorphics.|16-MAY-23
24416|Mywyn Granite|Age reasons|Probably Middle Proterozoic because of the strong foliation which mainly trends northeast to southeast. Foliation in the Siluro-Devonian granitoids, where present, is weaker and generally trends north to north-northeast.|16-MAY-23
24416|Mywyn Granite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24416|Mywyn Granite|Proposer|Withnall I.W.|16-MAY-23
27295|Nancy Lee Sandstone Member|Name source|Nancy Lee mine, one of the abandoned mines of the Golden Gate group, GR 7361-270930.|16-MAY-23
27295|Nancy Lee Sandstone Member|Unit history|Branch (1966) regarded the sandstone as an inlier of subvolcanic basement. Mackenzie (1983) informally named and described the 'Nancy Lee sandstone member').|16-MAY-23
27295|Nancy Lee Sandstone Member|Geomorphic expression|The sandstone occurs in area of gentle slopes at the foot of rugged volcanic terrain farther to the east.|16-MAY-23
27295|Nancy Lee Sandstone Member|Type section locality|The type section is the discontinuous creek-bed exposures of medium to coarse quartzofeldspathic, micaceous feldspathic, and, near the top, silicified quartzose sandstone between GR 7361-269934 (base) and -273935 (top). The section is about 140 m thick, based on an average dip of 20o.|16-MAY-23
27295|Nancy Lee Sandstone Member|Extent|Outcrop is limited to an area about 3 km long and 0.5 km wide straddling Golden Gate Creek immediately east of the Golden Gate group of mines.|16-MAY-23
27295|Nancy Lee Sandstone Member|Thickness range|The maximim thickness of the unit is estimated to be about 150 m based on an average dip of 20o; however, dip may be up to 30o, and maximum thickness 200 m. The unit lenses out less than 2 km north of Golden Gate Creek.|16-MAY-23
27295|Nancy Lee Sandstone Member|Lithology|The unit consists of thinly bedded yellow-brown to purplish-brown medium to coarse quartzofeldspathic sandstone, banded pinkish-buff micaceous feldspathic sandstone, and silicified sandstone close to upper contact. A few silty layers up to 1 cm thick are present in places.|16-MAY-23
27295|Nancy Lee Sandstone Member|Relationships and boundaries|Contacts with adjacent formations are not exposed, but the easterly dip of bedding indicates that the sandstone overlies the Parrot Camp Rhyolite to the west and is overlain by the Carron Rhyolite to the east. Spoil of Esmeralda Granite from the mines immediately to the west of the sandstone outcrop indicates that the sandstone is probably intruded by the granite.|16-MAY-23
27295|Nancy Lee Sandstone Member|Age reasons|The age is Middle Proterozoic as for the rest of the Croydon Volcanic Group.|16-MAY-23
27295|Nancy Lee Sandstone Member|Defn author|Mackenzie D.E., Henderson G.A.M., Warnick J.V., Bain J.H.C., 1985 Mention Map legend|16-MAY-23
27295|Nancy Lee Sandstone Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
27295|Nancy Lee Sandstone Member|References|B076|16-MAY-23
27295|Nancy Lee Sandstone Member|Defn Reference|86/25125|16-MAY-23
27295|Nancy Lee Sandstone Member|Proposer|Mackenzie D.E., Warnick J.V., Henderson G.A.M.|16-MAY-23
79129|Nash Clastics Member|Name source|Named after Nash Street and Nash Gully near the centre of Gympie, both of which pay tribute to James Nash, the discoverer of gold in Gympie.|16-MAY-23
79129|Nash Clastics Member|Unit history|The Nash Clastics Member was formally registered in 2002 after Cranfield (1999). Equated with the lower part of Dunstan's (1911) First Slate Group (1MC, 1C, 1LC, 1LS).  This unit first used informally as Upper Nash Clastics by Gympie Eldorado Gold Mines at Monkland Mine.  Subsequently referred to by Cranfield (1999), Sivell & Arnold (1999), Sivell & McCulloch (2001), Li & others (2015).|16-MAY-23
79129|Nash Clastics Member|Type section locality|GEGM Drill Hole G137, depth 360-399m  near Monkland Mine, collar 468390mE; 7100785mN, Lat: -26°12'44"  Long: 152°41'01",  held at Zillmere storage facility, Brisbane.  Reference sections: BHP drill hole G023: 131-134 m at north end of Monkland Mine. GEGM drill hole G135: 135-142 m near the Aurelia shoot, Monkland Mine, core also held at Zillmere core library. In the Phoenix Block typical sandstone can be seen at the rear of Madill Motors in Mellor Street, close to Nash Gully at QFG8349, MGA 466770mE; 7103370mN.|16-MAY-23
79129|Nash Clastics Member|Description at type locality|In GEGM drillhole G137 consists of feldspathic sandstone, grit and conglomerate, fining upwards plus shelly grit at the base.  In general consists of massive or thick-bedded, homogeneous volcaniclastic sandstone, generally medium to coarse grained with occasional interbeds of siltstone and pebbly conglomerate. In places upward fining cycles are present, with conglomerate at base, coarse to fine sandstone above.  Historically known as 'crystalline greywacke', it is composed of rounded to subangular crystal and lithic grains and clasts derived from underlying basaltic, andesitic and dacitic units, with the underlying Calton Andesite contributing detrital feldspars, particularly near the base.|16-MAY-23
79129|Nash Clastics Member|Extent|Widely distributed from north of the Two Mile Block to Dawn Block though apparently faulted out by the Curra Thrust in the Six Mile Block.|16-MAY-23
79129|Nash Clastics Member|Thickness range|Ranges from a few metres to about 50 m at Monkland, increasing in thickness in the northern part of the Phoenix Block and the Two Mile Blockto as much as 160m. About 15-25 m at Partridge and Inglewood Horst.|16-MAY-23
79129|Nash Clastics Member|Lithology|In the Monkland Block, consists of massive or thick-bedded, homogeneous volcanoclastic sandstone, generally medium- to coarse-grained with occasional interbeds of siltstone and pebbly conglomerate (Photograph 10). In places upward fining cycles are present, with conglomerate at base, coarse to fine sandstone above. Historically known as 'crystalline greywacke', it is composed of rounded to subangular crystal and lithic grains and clasts derived from underlying basaltic, andesitic and dacitic units, with the Calton Andesite contributing detrital feldspars, particularly near the base. All grains are variably altered to fine sericite, leucoxene, hematite/limonite and carbonate. Some are silicified. The sandstone can be rich in heavy minerals especially magnetite or leucoxene. In the Phoenix Block the early miners discovered two thin, fissile, carbonaceous shale beds within the sandstone unit, about 3-6 m thick and 30 m vertically apart (Rands, 1889). The uppermost shale, which they termed the 'First Bed of Slate', is located within the upper sandstones; the lower shale, termed the 'Second Bed of Slate' is at the base of the lower sandstone (Eldorado Clastics). They do not appear to extend south into the Monkland Block.|16-MAY-23
79129|Nash Clastics Member|Fossils|Etheridge (1872) collected species from the 'green fossiliferous sandstone', its position shown in the map by Rands (1899), now within the Nash Clastics Member.  Waterhouse and Balfe (1987) allocated them to their Notospirifer strzeleckii fauna. In 2015 a spirifer cast was observed by von Gnielinski at QFG8349 in a loose rock on the Madrill Motors outcrop (Photograph 11) but no further identification seemed possible.|16-MAY-23
79129|Nash Clastics Member|Relationships and boundaries|Conformably overlain by Pengelly carbonaceous siltstone [Pengelly Siltstone Member], underlain by Calton Andesite [Member].|16-MAY-23
79129|Nash Clastics Member|Structure and Metamorphism|All grains are variably altered to fine sericite, leucoxene, hematite/limonite and carbonate.  Some are silicified.|16-MAY-23
79129|Nash Clastics Member|Age reasons|Waterhouse and Balfe (1987) believe the fauna are of late Asselian age in the Lower Permian.|16-MAY-23
79129|Nash Clastics Member|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie, 12-JAN-2017.|16-MAY-23
79129|Nash Clastics Member|References|Dunstan, B., 1911: Geology map of Gympie and environs. GSQ Publ. No. 221bEtheridge, R. Snr, 1872:  Description of  the Palaeozoic and Mesozoic fossils of Queensland. Quarterly Journal of the Geological Society of London, 28, 317-350. **Waterhouse, J.B. and Balfe, P.,1987: Stratigraphic and faunal subdivisions of the Permian rocks at Gympie. IN Murray, C.G. & Waterhouse, J.B. (Eds). 1987 Field Conference, Gympie District.  Geol. Soc. Australia, Queensland Division, Brisbane, 20-29.  **Cranfield, L.C., 1999: Gympie Special Sheet 9445, Part 9545, Queensland 1:100,000 Geological Map Commentary. Queensland Department of Mines and Energy, Brisbane. **Sivell, W.J. and Arnold, G.O. 1999: Geochemical and volcanic stratigraphy of a segment of an island arc - Gondwana rim accretion zone, Gympie Province, southeast Queensland.  IN Flood, P.G. (Editor): Regional Geology, Tectonics and Metallogenesis, New England Orogen, NEO '99 Conference, 255-266.  **Sivell, W.J. and McCulloch, M.T. 2001: Geochemical and Nd-isotopic systematics of the Permo-Triassic Gympie Group, southeast Queensland.  Australian Journal of Earth Sciences 48, 377-394. **Li, P., Rosenbaum, G., Yang, J-H. and Hoy, D. 2015. Australian-derived detrital zircons in the Permian-Triassic Gympie terrane (eastern Australia): Evidence for an autochthonous origin. Tectonics, 34, 858-874.|16-MAY-23
14032|Netherwood Tonalite|Name source|Netherwood Block on Wando Vale Holding (Clarke River 4-Mile Cadastral Map).|16-MAY-23
14032|Netherwood Tonalite|Unit history|The tonalite was previously mapped as Craigie Granodiorite (White, 1962, 1965).  The name was first published by Withnall & others (1988), and described briefly, but was not formally defined.|16-MAY-23
14032|Netherwood Tonalite|Geomorphic expression|The unit is generally expressed as hilly topography, because it has only recently been exhumed from beneath Tertiary basalt cover.  On aerial photographs, it is difficult to distinguish from surrounding units  although it has slightly paler tones.|16-MAY-23
14032|Netherwood Tonalite|Type section locality|Broken River, between 7859 675443 and 679442, where  medium-grained, equigranular biotite-hornblende tonalite crops out.  The grid references are based on the AGD66 datum.|16-MAY-23
14032|Netherwood Tonalite|Extent|Two small plutons, partly dismembered by faulting, and totalling 5 km2 in the Broken River area.|16-MAY-23
14032|Netherwood Tonalite|Lithology|Medium grained, equigranular biotite hornblende tonalite to quartz diorite.|16-MAY-23
14032|Netherwood Tonalite|Relationships and boundaries|The Netherwood Tonalite intrudes the Judea Formation, and is nonconformably overlain by the Poley Cow Formation.|16-MAY-23
14032|Netherwood Tonalite|Age reasons|Ordovician to Early Silurian (interpreted from relationships).|16-MAY-23
14032|Netherwood Tonalite|References|WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4. Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. **WHITE, D.A., 1962:  Clarke River 1.250 000 Geological series. Bureau of Mineral Resources, Australia, Explanatory Notes, E/55-13. **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
80509|New Hope Sandstone Member|Name source|The small New Hope copper mine at GDA coordinates lat. -21.716877 and long. 140.483512 in the MOUNT MERLIN (6954) 1:100 000 Sheet area.|16-MAY-23
80509|New Hope Sandstone Member|Unit history|The name 'New Hope Arkose' was published by Beardsmore et al. (1988) for a lenticular area of feldspathic sandstone south of Mount Dore and considered by them to be the lower part of the Kuridala Formation. However, no definition or detailed description was given. Revised GSQ mapping showed the unit was more extensive but interpreted to occur within the middle of the Kuridala Group between the Starcross Formation and Hampden Slate and it was renamed as New Hope Sandstone (GSQ, 2011; Withnall & Hutton, 2013). New mapping has shown that typical Starcross Formation rock types also occur above the New Hope Sandstone in places, so the unit is downgraded in status to a member of the Starcross Formation.|16-MAY-23
80509|New Hope Sandstone Member|Type section locality|The name `New Hope Arkose¿ was published by Beardsmore et al. (1988) for a lenticular area of feldspathic sandstone south of Mount Dore and considered by them to be the lower part of the Kuridala Formation. However, no definition or detailed description was given. Revised GSQ mapping showed the unit was more extensive but interpreted to occur within the middle of the Kuridala Group between the Starcross Formation and Hampden Slate and it was renamed as New Hope Sandstone (GSQ, 2011; Withnall & Hutton, 2013). New mapping has shown that typical Starcross Formation rock types also occur above the New Hope Sandstone in places, so the unit is downgraded in status to a member of the Starcross Formation.|16-MAY-23
80509|New Hope Sandstone Member|Extent|Occurs in discrete mappable horizons throughout the Starcross Formation, generally towards the top of the formation. The Starcross Formation is exposed in a belt that is 10 km wide and 90 km long with its northern extent in the Hampden Syncline, 65 km due south of Cloncurry.|16-MAY-23
80509|New Hope Sandstone Member|General description|Very thick to thick beds of very coarse to coarse-grained quartz (at times feldspathic) sandstone which is occasionally interbedded with micaceous pelitic schist. Locally exhibits normal grading associated with flat lamination and rare ripple cross-lamination.|16-MAY-23
80509|New Hope Sandstone Member|Thickness range|~1000 m. The thickness commonly cannot be evaluated accurately because of the complex folding and possible thrusting.|16-MAY-23
80509|New Hope Sandstone Member|Lithology|Very thick to thick beds of very coarse to coarse grained quartz (commonly feldspathic) sandstone which is locally interbedded with micaceous pelitic schist. In places, it exhibits normal grading associated with flat lamination and rare ripple cross-lamination.|16-MAY-23
80509|New Hope Sandstone Member|Depositional environment|The outcrop lithology of the New Hope Sandstone is laterally discontinuous along and across strike; its bedsets of amalgamated medium to coarse, poorly sorted, and mostly structureless sandstones indicate higher hydrodynamic activity during their deposition than the typical Starcross Formation turbiditic bedsets. These bedsets in the New Hope Sandstone Member are interpreted to represent avulsed turbidite channel fills within a turbidite fan.|16-MAY-23
80509|New Hope Sandstone Member|Relationships and boundaries|Lies conformably within the Starcross Formation. A basal progressive gradational contact can be observed on the eastern limb of the Mort River Anticline located at lat. -21.634412 and long. 140.618227. An upper progressive gradational contact can be observed on the western limb of the Mort River Anticline at lat. -21.707058 and long. 140.510638.|16-MAY-23
80509|New Hope Sandstone Member|Identifying features|Common amalgamated bedsets of coarse-grained quartzose to feldspathic sandstone.|16-MAY-23
80509|New Hope Sandstone Member|Structure and Metamorphism|The New Hope Sandstone Member was complexly folded within the Starcross Formation during the 1600¿1570 Isan Orogeny. Metamorphic assemblages within the Starcross Formation indicate upper greenschist to amphibolite facies metamorphism. The type section on the western limb of the Mort River Anticline is overturned with a bed-parallel to slightly oblique schistosity within interlayed pelitic schist.|16-MAY-23
80509|New Hope Sandstone Member|Age reasons|Paleoproterozoic (Statherian). A maximum depositional age of 1662 ± 22 Ma has been determined by Lewis et al. (2018, this record), but other samples in the Geoscience Australia Online Geochronology Delivery System collected from the unit (although assigned to the `Kuridala Formation¿) give maximum depositional ages of 1691 ± 9 Ma, 1676 ± 4 Ma and 1671 ± 16 Ma (Withnall, in preparation). It was deformed by the 1600¿1570 Isan Orogeny.|16-MAY-23
80509|New Hope Sandstone Member|Correlations|Possibly correlates with the Mount Norna Quartzite in the Soldiers Cap Group, although the latter is generally finer grained.|16-MAY-23
80509|New Hope Sandstone Member|Defn author|Alexander P. Slade, Allan Parsons and Ian W. Withnall, Geological Survey of Queensland, 19/03/2018.|16-MAY-23
80509|New Hope Sandstone Member|Proposed publication|Queensland Geological Record|16-MAY-23
80509|New Hope Sandstone Member|References|Beardsmore, T.J., Newbery, S.P. and Laing, W.P., 1988. The Maronan Supergroup: an inferred early volcanosedimentary rift sequence in the Mount Isa Inlier, and its implications for ensialic rifting in the Middle Proterozoic of northwest Queensland. Precambrian Research, 40, 487-507. **GSQ, 2011. North-West Queensland Mineral and Energy Province Report. Department of Employment, Economic Development and Innovation. Queensland Government. **Lewis, C.J, Hutton, L.H., Withnall, I.W., Slade, A.P., Sargeant, S., 2018. Summary of results Joint GSQ-GA geochronology project: Mount Isa region, 2016-2017. Queensland geological Record. **Withnall, I.W., in preparation. Review of zircon ages for the eastern Succession of the Mount Isa Province. Queensland Geological Record. **Withnall, I.W., and Hutton, L.J., 2013. Chapter 2: North Australian Craton, in Jell, P. A., editor, Geology of Queensland. Brisbane, Geological Survey of Queensland, 23-112.|16-MAY-23
28097|Newirie Formation|Lithology|Grey to purple thin-bedded slate, sandy slate and green metasandstone with rippled bedding; quartzite in southeast; locally tourmaline-mica schist, garnet, andalusite, chloritoid, staurolite; Muscovite-quartz phyllite, thin to thick beds of quartzite, with garnet; grades into garnet-muscovite schist; flaggy fine-grained biotite-muscovite-quartz schist|16-MAY-23
24432|Nonda Granite|Name source|Nonda Creek joins Nunda Creek at GR 7360-557380|16-MAY-23
24432|Nonda Granite|Unit history|The Nonda Granite was previously included in the Esmeralda Granite (White, 1959; Branch, 1966); it was informally named 'Nonda granite' and described by Mackenzie (1983).|16-MAY-23
24432|Nonda Granite|Type section locality|2.5 km northeast of where Nonda Creek crosses the road from Croydon to Esmeralda homestead (about GR 7460-675493); outcrops consist of grey, fine-grained porphyritic biotite granite with sporadic graphitic and mafic inclusions.|16-MAY-23
24432|Nonda Granite|Extent|Irregular stocks and apophyses ranging from a few hundred metres to several kilometres across crop out in the following areas: the Mount Cassiterite area (southeast Croydon); east of Stanhills Battery, and in the area surrounding Brennans Knob (southwest Gilbert River); on either side of the road to Esmeralda homestead, from Nonda Creek southward to Six Mile Waterhole (northwest Esmeralda); and about 18 km west-northwest of Glenora homestead (southeast Esmeralda).|16-MAY-23
24432|Nonda Granite|Lithology|Grey, fine to medium, slightly porphyritic biotite granite to microgranite which typically outcrops as subangular to subrounded boulders less than 0.5 m across. The rock commonly contains graphite and/or lithic inclusions and tends to be quite dark in colour even though it generally has low mafic content and in some cases is actually leucocratic; dark colour may be due to disseminated graphite. Alteration is extensive; biotite is commonly chloritised and plagioclase is almost invariably seriticised. Graphic intergrowths of quartz and K-feldspar are common.|16-MAY-23
24432|Nonda Granite|Relationships and boundaries|The Nonda Granite is considered to be a chilled marginal (roof) phase of the Esmeralda Granite, although a contact relationship has not been observed. It intrudes the Proterozoic Croydon Volcanic Group (specifically the Idalia Rhyolite, including the Democrat Rhyolite Member, and Carron Rhyolite), and is unconformably overlain by the Jurassic Hampstead Sandstone and Loth Formation, and the Jurassic-Cretaceous Gilbert River Formation.|16-MAY-23
24432|Nonda Granite|Age reasons|The Nonda Granite is probably mid-Proterozoic in age; as mentioned above it is considered to be a marginal variant of the Esmeralda Granite which has a Rb-Sr muscovite age of 1444 Ma* (Black, 1973).   *Corrected using the 87Rb decay constant of 1.42 x 10-11yr-1 recommended by Steiger and Jager (1977).|16-MAY-23
24432|Nonda Granite|Defn author|Mackenzie D.E., Henderson G.A.M., Warnick J.V., Bain J.H.C., 1985 |16-MAY-23
24432|Nonda Granite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24432|Nonda Granite|References|73/050; B076|16-MAY-23
24432|Nonda Granite|Defn Reference|86/25125 Mention Map legend.|16-MAY-23
24432|Nonda Granite|Proposer|Mackenzie D.E., Warnick J.V., Henderson G.A.M.|16-MAY-23
14246|Normanby Formation|Lithology|Fine to coarse-grained quartzose sandstone; pebble to cobble polymictic conglomerate; aphyric to slightly porphyritic rhyolite; rhyolitic ignimbrite; andesite and andesitic tuff; subordinate basalt, rhyolitic tuff, lapilli tuff, volcanic breccia, sandstone, siltstone and mudstone; minor coal, carbonaceous mudstone, impure limestone|16-MAY-23
14388|Nundah Granodiorite|Name source|The formation is named after Nundah Creek which rises in and traverses a large area of granite country in the northwestern part of MUNGANA.|16-MAY-23
14388|Nundah Granodiorite|Unit history|It was previously mapped as part of the Dargalong Metamorphics (Best, 1962;  de Keyser & Wolff, 1964;  de Keyser & Lucas, 1968) apart from the large pluton exposed about 9 km southwest of Chillagoe, which was tentatively assigned to the Forsayth Granite (Best, 1962).  The granitic rocks in the Cardross to Butterfly Spring area were informally referred to as Nundah Granite by Goudie (1976, 1978).|16-MAY-23
14388|Nundah Granodiorite|Geomorphic expression|Hilly to gently undulating country with coarse gravelly soils and scattered rounded boulders and bouldery outcrops is extensively developed on the unit.  The granodiorite shows mainly as pale tones on aerial photographs.  Locally, medium tones predominate and in these areas the granodiorite is commonly very difficult to distinguish from Dargalong Metamorphics on aerial photographs.Subunit LP gnp forms low hilly country with scattered boulders and is characterised by pale tones on aerial photographs.|16-MAY-23
14388|Nundah Granodiorite|Type section locality|The designated type locality is at GR 1935 81013, about 0.5 km southwest of Butterfly Spring, on the northern side of the track and east of a northerly trending tributary of Poison Creek, MUNGANA.|16-MAY-23
14388|Nundah Granodiorite|Description at type locality|The formation is well exposed in this general area.  At Butterfly Spring it is unconformably overlain by an outlier of Mesozoic sandstone (Gilbert River Formation of the Carpentaria Basin sequence) and to the south it intrudes schist, gneiss and amphibolite of the Dargalong Metamorphics.|16-MAY-23
14388|Nundah Granodiorite|Extent|The granodiorite crops out over ~510 km2 in northern MUNGANA and southern BELLEVUE.The granodiorite has two distinct modes of occurrence:(1)	as large discrete plutons whose contacts with the Dargalong Metamorphics are fairly sharp and discordant, and readily delineated on aerial photographs, and(2)	as irregular to elongate stocks containing numerous inclusions of metamorphic rocks (particularly in marginal zones) and as thin lenses and dykes oriented mainly parallel to the foliation in the metamorphics.  These units commonly form migmatitic complexes with quartzofeldspathic gneisses of the Dargalong Metamorphics and they are generally difficult to distinguish from the metamorphics on aerial photographs.SubunitLP gnp crops out over <5 km2, north of Muldiva Creek and about 13 km west of Mungana.|16-MAY-23
14388|Nundah Granodiorite|General description|The granodiorite is cut by numerous faults and shear zones, particularly in the area between Butterfly Spring and Cardross dam.  A metamorphic foliation or, more rarely, a schistosity is commonly developed in the sheared granite (sensu lato) which tends to form ridges that are difficult to distinguish from rhyolite dykes on aerial photographs.  Some relatively long narrow zones of quartz-muscovite schist, interpreted as extensively sheared and altered granodiorite, have also been mapped.The Nundah Granodiorite shows abundant evidence (e.g., recrystallisation of grains - in particular quartz grains, undulose extinction in quartz and muscovite grains, bent muscovite and biotite flakes) of extensive deformation.  Most outcrops show a tectonic foliation defined mainly by the alignment of mica flakes.  Locally quartz grains in the granodiorite have recrystallised to elongate 'ribbons' which 'wrap around' large feldspar grains.MINERALISATION:  Fluorspar veins and small deposits of copper minerals are common along fractures and in shear zones which cut the Nundah Granodiorite.  Minor copper mineralisation has been found in the Nundah Granodiorite in the Dargalong - Mount Delaney area, southwest of Chillagoe.  The deposits are in veins filling fractures in the granodiorite and the lodes consist mainly of gossany chalcedony or vuggy quartz.  Gold has been mined at Mount Wandoo where the host rock is hydrothermally altered Nundah Granodiorite.  Books of muscovite, up to 30 cm square, in pegmatite veins and segregations have been reported from several localities.  The most productive mines were in the Mount Kitchen area, but reserves are low.  Rutile is patchily distributed throughout aplite and minor pegmatite of subunitLP gnp.  Minor deposits of antimony, arsenic, lead, tin, tungsten and zinc minerals have also been reported; most, if not all of these, are fracture controlled.|16-MAY-23
14388|Nundah Granodiorite|Lithology|The formation in the type locality consists of white to pale grey, medium-grained biotite-muscovite granodiorite containing euhedral white potassium feldspar phenocrysts and coarse muscovite flakes.  Elsewhere the granodiorite is mainly medium to coarse grained, although pegmatitic and fine-grained variants also occur.  Textures range from megacrystic to equigranular;  porphyritic and seriate textures are common.  The granodiorite is locally heterogeneous, both texturally and compositionally, particularly adjacent to contacts with the gneissic country rocks of the Dargalong Metamorphics - granodiorite exposed near contacts with the Dargalong Metamorphics commonly contain biotite-rich schlieren and large (up to ~2 m x 1 m) inclusions of mica schist, gneiss and amphibolite.  The unit also contains minor pegmatite, as dykes and segregations and rare aplite (as pods).Quartz occurs mainly as anhedral, irregular grains which show highly undulose extinction.  Plagioclase (mainly oligoclase) is the dominant mineral in most outcrops.  Champion (1991) reported plagioclase compositions ranging from An16 to An27 in granites of the Blackman Gap Complex.................Biotite (pleochroic from dark red-brown or dark brown to pale yellow) forms mainly anhedral, ragged flakes, as well as scattered euhedral grains.  It occurs as discrete grains and small aggregates of flakes (commonly with minor muscovite)..............Muscovite is the most abundant mica in most outcrops. It occurs as small flakes scattered throughout the groundmass, as coarse flakes and megacrysts (up to 3 cm across), and as a partial replacement of plagioclase..............Accessory and secondary minerals include ilmenite, apatite, zircon, garnet, sphene, sericite, muscovite (secondary), chlorite, epidote and calcite.  Garnet is relatively common in some muscovite-rich leucogranites (sensu lato).............SubunitLP gnp consists of white to pink, fine to medium-grained, rutile-bearing aplite, together with minor pegmatite (as small irregular pods and segregations), muscovite leucogranodiorite and quartzofeldspathic gneiss................ALTERATION:  The granodiorite has undergone extensive hydrothermal alteration in several places, involving mainly sericitisation and silicification.  The alteration appears to be mainly fracture controlled and is probably related to the emplaced nearby of Late Palaeozoic rhyolite dykes and pods of porphyritic microgranite (sensu lato).|16-MAY-23
14388|Nundah Granodiorite|Relationships and boundaries|The Nundah Granodiorite intrudes the Dargalong Metamorphics and is cut by numerous dykes of rhyolite (commonly flow banded) and dolerite (locally amygdaloidal) of probable Late Carboniferous age.|16-MAY-23
14388|Nundah Granodiorite|Age reasons|The Nundah Granodiorite (as well as the granite of the Blackman Gap Complex - the other member of the Blackman Gap Supersuite) had, until recently, been interpreted to be Proterozoic.  A specimen collected from the pluton exposed east of the Dargalong group of mines reportedly yielded a K-Ar isotopic age (adjusted) of 1072 Ma (Table    ; Richards & others, 1966).  Subsequently, Silurian-Devonian ages were obtained on biotites from this specimen using Rb-Sr and K-Ar isotopic dating techniques (Black, 1973).  Black (1973) interpreted the relatively young ages to have most probably resulted from extensive resetting of both K-Ar and Rb-Sr mineral ages during a regional heating event at ~400 Ma.U-Pb zircon ion microprobe (SHRIMP) ages of ~430 Ma and 426 ± 7 Ma have recently been obtained on samples of the Nundah Granodiorite and Blackman Gap Complex, respectively (Table  ).  These indicate the Blackman Gap Supersuite was indeed emplaced in the Early Silurian and not the Proterozoic as previously thought.  The ages are similar to that (431 + 10- 21 Ma) obtained for the Dido Tonalite, in the Georgetown Province to the south (Black & McCulloch, 1990).|16-MAY-23
14388|Nundah Granodiorite|Comments|The Nundah Granodiorite is characterised by relatively high Na2O, Sr, and Ba contents, and low K2O contents (Champion, 1991).  These characteristics indicate the granodiorite is infracrustal in origin (i.e., an I-type) despite its relatively high ASI (cf. White & others, 1986) and normative corundum contents.|16-MAY-23
14388|Nundah Granodiorite|References|BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.BLACK, L.P., 1973:  Tables of isotopic ages from the Georgetown Inlier, north Queensland.  Bureau of Mineral Resources, Australia, Record 1973/50.CHAMPION, D.C., 1991:  Petrogenesis of the felsic granitoids of far north Queensland.  Ph.D. Thesis, Australian National University, Canberra (unpublished).DE KEYSER, F., & LUCAS, K.G., 1968:  Geology of the Hodgkinson and Laura Basins, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 84.GOUDIE, J.C., 1976a:  The Split Rock Copper Prospect near Cardross, in the Chillagoe district.  M.Sc. Thesis, James Cook University of North Queensland, Townsville (unpublished)..DE KEYSER, F., & WOLFF, K.W., 1964:  The geology and mineral resources of the Chillagoe area.  Bureau of Mineral Resources, Australia, Bulletin 70.RICHARDS, J.R., WHITE, D.A., WEBB, A.W., & BRANCH, C.D., 1966:  Isotopic ages of acid igneous rocks in the Cairns hinterland, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 88.|16-MAY-23
14458|Oak River Granodiorite|Name source|Oak River, a tributary of the Copperfield River which it joins at GR 952 302 (Einasleigh 1:100 000 Sheet area). Also Oak River Holding.|16-MAY-23
14458|Oak River Granodiorite|Unit history|Previously defined by Withnall & others (1976).|16-MAY-23
14458|Oak River Granodiorite|Unit history|Included in the Forsayth Granite by White (1959; 1962a; b; 1965).|16-MAY-23
14458|Oak River Granodiorite|Type section locality|Along the track from the Einasleigh-Kidston road near Edmonds Creek to "Duck Hole" yards at GR 112 093 (Forsayth 1:100 000 Sheet area) on the Oak River. Grey medium grained porphyritic biotite granodiorite crops out.|16-MAY-23
14458|Oak River Granodiorite|Type section locality|The type area as previously published (Withnall & others, 1976) is along the track from the Einasleigh-Kidston road near Edmonds Creek (GR 868040, Einasleigh 1:100 000 Sheet area). Between the yards and about GR 852050 medium-grained porphyritic biotite granodiorite crops out; from here to the Einasleigh-Kidston road, equigranular hornblende-biotite tonalite predominates; outcrops of calc-silicate gneiss are common along the first kilometre of the track, and leucogranite crops out between GR 848063 and GR 848057.|16-MAY-23
14458|Oak River Granodiorite|Description at type locality|Medium-grained equigranular hornblende-biotite tonalite is well exposed at GR 025158 (Einasleigh 1:100 000) Sheet area) in the Copperfield River where it is crossed by the road to Kidston, and is herein designated as a reference locality.|16-MAY-23
14458|Oak River Granodiorite|Extent|From the Newcastle Range in the Forsayth 1:100 000 Sheet area northeast to the Einasleigh River in the Einasleigh 1:100 000 Sheet area and extending to near Mount Blacktop (GR 214435). The batholith crops out over a total area of about 850 km2.|16-MAY-23
14458|Oak River Granodiorite|Extent|East of the Newcastle Range in the Oak River catchment area in the Forsayth 1:100 000 Sheet area. Its extent to the east on the Einasleigh 1:100 0000 Sheet area is unknown at present although similar rocks occur in the Copperfield River near "The Oaks" Homestead.|16-MAY-23
14458|Oak River Granodiorite|Lithology|Grey medium grained biotite granodiorite with pink K-feldspar megacrysts; locally foliated. Subordinate grey foliated hornblende-biotite tonalite.|16-MAY-23
14458|Oak River Granodiorite|Lithology|The unit consists of two main lithologies; a grey medium-grained porphyritic biotite granodiorite and an equigranular, locally hornblende-bearing, biotite tonalite. The porphyritic biotite granodiorite contains locally abundant, pink microcline megacrysts which are zoned, subsequent to lath-shaped crystals generally a few centrimetres long but up to 6 cm in places. Weak alignment of the megacrysts locally defines a foliation in the granodiorite. The equigranular hornblende-biotite tonalite which is most common in the eastern half of the batholith is characterised by ellipsoidal to spheroidal quartz grains up to 1 cm long and common mafic segregations, generally 2-3 cm long. The tonalite commonly has a foliation defined by biotite and the elongate quartz grains. A mortar texture is commonly developed.|16-MAY-23
14458|Oak River Granodiorite|Relationships and boundaries|Intrudes the Proterozoic Einasleigh Metamorphics. Intruded by the Proterozoic Digger Creek Granite (new name) and late Palaeozoic rhyolite dykes. Unconformably overlain by the Carboniferous Newcastle Range Volcanics and Jurassic-Cretaceous sandstone.|16-MAY-23
14458|Oak River Granodiorite|Relationships and boundaries|The unit intrudes the Proterozoic Einasleigh Metamorphics and associated leucogranitoid bodies. It is in contact with Proterozoic of Siluro-Devonian Eleven-B Granite and Quinine Spring Granite but the intrusive relationships are not known. Intruded by the Beverly Hills Granite and other leucogranitoids containing biotite and/or muscovite as well as mica-poor varieties. Intruded by numerous late Palaeozoic microgranite and rhyolite dykes. Unconformably overlain by the Carboniferous Newcastle Range Volcanics, Jurassic-Cretaceous sandstone and Cainozoic basalt.|16-MAY-23
14458|Oak River Granodiorite|Age reasons|The age of the Oak River Granodiorite is uncertain. It is intruded by the Beverly Hills Granite, a muscovite granite previously assigned to the Digger Creek Granite by Bain & others (1976) and Withnall & others (1976). The Digger Creek Granite is Precambrian in its type area and the Oak River Granodiorite was therefore also thought to be Precambrian. Four biotite/total rock pairs from the Oak River Granodiorite give Early Devonian Rb/Sr ages between 388 and 400 Ma (Black & Holmes, in preparation). Most samples of Oak River Granodiorite show thin section evidence of deformation and it is difficult to tell whether these are primary ages or have been reset. However, the whole rock 87Sr/86Sr ratios are dissimilar to known Precambrian granitoids from the area and are almost identical to those for the Siluro-Devonian Robin Hood Granodiorite, suggesting that the Oak River Granodiorite is also of Siluro-Devonian age.|16-MAY-23
14458|Oak River Granodiorite|Age reasons|Proterozoic; intruded by the Proterozoic Digger Creek Granite (new name).|16-MAY-23
14458|Oak River Granodiorite|References|98/29026; ? 01/31335; B071|16-MAY-23
14458|Oak River Granodiorite|Apprdate|19-DEC-1975|16-MAY-23
14458|Oak River Granodiorite|Defn approved by|Staines H.R.E.|16-MAY-23
14458|Oak River Granodiorite|Proposer|Bain J.H.C., Oversby B.S., Withnall I.W.|16-MAY-23
14470|Oakleigh Siltstone Member|Name source|From Oakleigh grazing homestead, the property on which GSQ Jericho 2 stratigraphic bore was drilled. The co-ordinates of the bore are: Latitude 23o37'S; Longitude 146o33'E.|16-MAY-23
14470|Oakleigh Siltstone Member|Type section locality|In ENL Lake Galilee 1 from 2036 m (6680 ft) to 2190 m (7185 ft) K.B.  Cuttings and cores of this interval are stored at the Core Library, Redbank.|16-MAY-23
14470|Oakleigh Siltstone Member|Extent|Present in wells in the Koburra Trough. Thins northwestward from AOD Jericho 1 to BPO Coreena 1. Represented in continuous core by the interval 492 to 628 m in GSQ Jericho 2 and probably 205 to 268 m in GSQ Springsure 13.|16-MAY-23
14470|Oakleigh Siltstone Member|Thickness range|154 m in the type section. Thins from 107 m in AOD Jericho 1 to possibly 39 m in BPO Coreena 1. 136 m and 63 m in GSQ Jericho 2 and Springsure 13 respectively.|16-MAY-23
14470|Oakleigh Siltstone Member|Lithology|The Oakleigh Siltstone Member consists mainly of interbedded siltstone, mudstone and shale. Cores 25 and 26 were cut in the type section and are described in detail by Pemberton in Exoil N.L. (1965). Siltstone, mudstone and shale are dark grey and green, very hard, strongly banded, possibly varved. Few poorly preserved plant impressions occur on the bedding.|16-MAY-23
14470|Oakleigh Siltstone Member|Depositional environment|Calm water, lacustrine with a glacial influence.|16-MAY-23
14470|Oakleigh Siltstone Member|Relationships and boundaries|Conformable unit within the Jericho Formation in deeper parts of the basin. Contains significant amounts of interbedded sandstone in FPN Koburra 1l.|16-MAY-23
14470|Oakleigh Siltstone Member|Age reasons|Late Carboniferous to Early Permian. Spore assemblages characteristic of Stage 1 of Evans (1969) were obtained from the cores in the type section.|16-MAY-23
14470|Oakleigh Siltstone Member|Defn author|Gray A.R.G., Swarbrick C.F.J., 1975|16-MAY-23
14470|Oakleigh Siltstone Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
14470|Oakleigh Siltstone Member|Name first published by|Geological Survey of Queensland, 1975.|16-MAY-23
14590|One Tree Granite|Name source|Named after One Tree Tank, which is situated within the outcrop area of the unit 16 km SE of Stanbroke Homestead, at GR 760010, Dajarra 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
14590|One Tree Granite|Unit history|Previously mapped as Kalkadoon Granite (Carter & Opik, 1963).|16-MAY-23
14590|One Tree Granite|Type section locality|In vicinity of GR 733037, about 1 km W of station track, 12 km SSE of Stanbroke homestead, and 3 km NW of One Tree Tank, Dajarra 1:100 000 Sheet area. Here a southerly draining creek, a tributary of Boundary Creek, marks an approximate contact between the two main rock types of the unit: pink medium to coarse biotite granite, which forms tors and boulder-strewn hills to the west, and grey finer grained biotite-rich granite forming more subdued terrain to the east.|16-MAY-23
14590|One Tree Granite|Extent|The unit crops out in a broad band 40 km long and up to 10 km wide trending N to NNW in the central part of Dajarra 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
14590|One Tree Granite|Lithology|Consists mainly of grey, foliated, medium to fine-grained biotite-rich granite which commonly contains small feldspar phenocrysts, and massive to locally foliated commonly porphyritic coarser biotite granite; both are commonly xenolithic. Some microgranite, aplite, and pegmatite are also present.|16-MAY-23
14590|One Tree Granite|Relationships and boundaries|The granite is inferred to intrude Plum Mountain Gneiss (new name) and may also intrude undivided Tewinga Group. It is intruded by mafic and porphyritic felsic dykes, and probably by Wills Creek Granite (new name), and is overlain by Leichhardt Volcanics and Cambarian sediments.|16-MAY-23
14590|One Tree Granite|Age reasons|Early Proterozoic; it pre-dates overlying Leichhardt Volcanics, which are isotopically dated at about 1880 m.y. (R.W. Page, personal communication, 1980).|16-MAY-23
14590|One Tree Granite|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
14590|One Tree Granite|Comments|Remarks: One Tree Granite is petrographically similar to parts of the Kalkadoon Granite. However, it forms a large, well defined, separate intrusion consisting of two main rock types, and is a distinctive, readily mappable unit, hence it is mapped separately from other granite bodies mapped as Kalkadoon Granite.|16-MAY-23
14590|One Tree Granite|References|98/29253|16-MAY-23
14590|One Tree Granite|Defn Reference|82/22920|16-MAY-23
14590|One Tree Granite|Proposer|Blake D.H. (in Blake & others, in prep.)|16-MAY-23
24445|Oroopo Metabasalt|Name source|Named after Oroopo Waterhole (GR 319893) on Sulieman Creek, Ardmore 1:100 000 Sheet area, Urandangi 1:250 000 Sheet area.|16-MAY-23
24445|Oroopo Metabasalt|Unit history|Mapped as Eastern Creek Volcanics and Sybella Granite by Noakes & others (1959).|16-MAY-23
24445|Oroopo Metabasalt|Type section locality|From GR 158792 to GR 124747, in the SW of the Ardmore 1:100 000 Sheet area. The section extends from about 2 km S of the track extending west from Rufus Tank in a SW direction to a major unnamed tributary of Quita Creek. A complete section from the base to the top of the formation has not been found. The type section consists mainly of amygdaloidal and massive metabasalt and interlayered lenses of meta-arenite and quartzite. It also contains some flow-margin breccia and scoriaceous metabasalt.|16-MAY-23
24445|Oroopo Metabasalt|Extent|Exposed mainly in the SW of the Ardmore 1:100 000 Sheet area, and extends S into the Glenormiston 1:250 000 Sheet area. Some small outcrops in the central-north of the Ardmore Sheet area are also tentatively regarded as forming part of this unit.|16-MAY-23
24445|Oroopo Metabasalt|Thickness range|Unknown; probably at least 1300 m. A complete section has not been found and there is a general absence of facing evidence and a lack of useful marker beds.|16-MAY-23
24445|Oroopo Metabasalt|Lithology|The rocks are generally as in the type section. The formation also contains beds of recrystallised limestone, calcareous meta-arenite, ?dolomite, and metasiltstone.|16-MAY-23
24445|Oroopo Metabasalt|Relationships and boundaries|The unit appears to concordantly overlie Saint Ronans Metamorphics; however, the contact is poorly exposed. It is cut by metadolerite dykes, and by rare veins of pegmatite and non-foliated to foliated, porphyritic to non-porphyritic biotite granite similar to the Sybella Granite elsewhere in the Ardmore Sheet area. The Oroopo Metabasalt is unconformably overlain by Cambrian sedimentary rocks of the Georgina Basin succession.|16-MAY-23
24445|Oroopo Metabasalt|Age reasons|Precambrian, probably Proterozoic.|16-MAY-23
24445|Oroopo Metabasalt|Proposed publication|Blake & others, in preparation|16-MAY-23
24445|Oroopo Metabasalt|Comments|Remarks: The Oroopo Metabasalt is confined to within, and W of, the Rufus Fault Zone, which forms part of a major right-lateral fracture system extending to the SW and NNE (the Gorge Creek-Mount Remarkable Fault of Derrick & others, 1980). The Oroopo Metabasalt closely resembles the Eastern Creek Volcanics in the E part of the Ardmore 1:100 000 Sheet area. However, one of the noteworthy differences is the presence in the Eastern Creek Volcanics of abundant conglomerate and conglomeratic sediments containing clasts of felsic volcanics. Also, the Eastern Creek Volcanics apparently conformably overlie the Mount Guide Quartzite, a thick sequence of quartzose, feldspathic, and sericitic meta-arenite, whereas the Oroopo Metabasalt appears to be concordant on a sequence of mainly argillaceous metasediments and felsic and mafic metavolcanics (Saint Ronans Metamorphics). Such differences may be the result of facies variations from east to west, or they may indicate that the two formations are not equivalent.|16-MAY-23
24445|Oroopo Metabasalt|References|JO503/04|16-MAY-23
24445|Oroopo Metabasalt|Defn Reference|82/22920|16-MAY-23
24445|Oroopo Metabasalt|Resdate|05-NOV-1980|16-MAY-23
26091|Overhang Jaspilite|Name source|The Overhang manganese mine, 33 km south-southwest of Cloncurry, latitude 20o49'19"S, longitude 140o23'16"E (6956 365793).|16-MAY-23
26091|Overhang Jaspilite|Geomorphic expression|The formation crops out as low, dark, strike ridges of jaspilite and calcareous metasediments, separated by valleys underlain by shale and siltstone. The formation has a soft, dark grey tone on black-and-white air photographs, and a distinctive dark blue-grey coloration on colour air photographs.|16-MAY-23
26091|Overhang Jaspilite|Type section locality|Extending northeast for about 500 m from a point 17 km west southwest of Cloncurry, 4 km south of the Barkly Highway, latitude 20o45'20"S, longitude 140o21'5"E (6956 324049). The base of the section is 0.5 km north of a track joining Butcher Bore and the Malbon road. At the type locality the pale buff and greenish siltstone at the top of the Mitakoodi Quartzite grade into calcareous siltstone of the Overhang Jaspilite. Dips are from 45o to 50o to the northeast. The calcareous siltstone contains sporadic resistant laminae of ferruginous quartzite or chert, and is overlain by dark manganese-stained limestone with quaratzite laminae, tightly cross-folded jaspilite in laminated limestone, and dark green pyritic siltstone. In nearby outcrops this part of the sequence contains stromatolitic domes up to 2 m in diameter and one metre high. They are overlain by a recessive unit of greenish grey, laminated, slightly pyritic shale, which is overlain by another sequence of limestone and jaspilite. These sediments are overlain by varve-like shales with minor jaspilite beds and limestone, both of which become less common higher in the sequence. The top of the formation is not exposed in the type section due to folding, and elsewhere the top of the formation is generally obscured by minor faulting. However, the sections examined in detail are believed to be almost complete. A good reference section is located at Overhang Mine; in this section a thin quaratzite is exposed at the top of the section and is separated from the overlying Corella Formation by minor faulting. Barite veins are a characteristic feature of parts of the Overhang Jaspilite.|16-MAY-23
26091|Overhang Jaspilite|Extent|The main exposures of the Overhang Jaspilite are in the Duck Creek and Bulonga Anticlines and in the Fox Mountain Dome (Fig. 3). It has been mapped in the Marraba and Mary Kathleen 1:100 000 1:100 000 Sheet areas and is known to occur in the Duchess and Malbon 1:100 000 Sheet areas. Jaspilitic rocks at the top of the Soldiers Cap Group on the Cloncurry 1:100 000 Sheet area may also belong to the Overhang Jaspilite.|16-MAY-23
26091|Overhang Jaspilite|Thickness range|In the type section almost 200 metres of section is exposed; in the reference section about 500 metres of section is present but sections up to 850 m have been measured in other parts of the formation (Derrick et al., 1971).|16-MAY-23
26091|Overhang Jaspilite|Relationships and boundaries|The Overhang Jaspilite conformably overlies the Mitakoodi Quartzite, except possibly in the south of the Bulonga Anticline, where the contact appears disconformable. The relationship of the Overhang Jaspilite with overlying units is uncertain as most boundaries are locally faulted or concealed. It appears to be conformably or disconformably overlain by the Corella Formation; the Chumvale Breccia contains jaspilitic fragments and appears to be derived from the Overhang Jaspilite by a process of brecciation, decalcification, and silicification.|16-MAY-23
26091|Overhang Jaspilite|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1977|16-MAY-23
26091|Overhang Jaspilite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
26091|Overhang Jaspilite|Comments|The relationships between the Overhang Jaspilite and the overlying Corella Formation has not been completely clarified by the detailed mapping. The evidence avalable at present favours a conformable relationship. However, regional considerations, such as the unconformities between the Mary Kathleen Group and Tewinga Group in the west of the basin, and between the Mary Kathleen Group and the Soldiers Cap Group (part of which is equivalent to the Malbon Group) in the east of the basin, and in unconformity of similar age in the western succession, indicate the possibility of an unconformity between the Overhang Jaspilite and the Corella Formation. Also, in several localities a thin conglomeratic quartzite is present at the base of the Corella Formation, overlying the Overhang Jaspilite. If further work substantiates this unconformity the Overhang Jaspilite will need to be redefined as part of the Malbon Group.|16-MAY-23
26091|Overhang Jaspilite|References|71/056|16-MAY-23
26091|Overhang Jaspilite|Name first published by|Glikson A.Y., Derrick G.M., Wilson I.H., Hill R.M., 1976 - J0102/04, Brooks 1975|16-MAY-23
24446|Overlander Granite|Name source|Named after the Overlander group of prospects and small mines in NE Duchess 1:100 000 Sheet area (Duchess 1:250 000 Sheet area).|16-MAY-23
24446|Overlander Granite|Unit history|Mapped as Wonga Granite by Carter & Opik (1963).|16-MAY-23
24446|Overlander Granite|Type section locality|From about GR 850745 to GR 859743, where the granite is very well exposed in the gorge cut by the Malbon River. Here the unit consists mainly of medium-grained foliated biotite leucogranite commonly showing well-developed joints. The granite contains scattered, sparse, small feldspar phenocrysts away from contacts with country rocks.|16-MAY-23
24446|Overlander Granite|Extent|The granite forms several discrete elongate plutons in NE of the Duchess 1:100 000 Sheet area, the largest of which has an area of about 10 sq. km.|16-MAY-23
24446|Overlander Granite|Lithology|The Overlander Granite is white, pink or grey, leucocratic, medium to coarse-grined, even-grained to slightly porphyritic, massive to foliated, and commonly partly recrystallised. The main mafic minerals are biotite and hornblende. Swarms of tourmaline-bearing, graphic, quartz-pink feldspar pegmatite dykes in the adjacent Corella Formation ar thought to be related to the Overlander Granite, because, although some pegmatite veins cut the plutons and were obviously intruded after the granite was emplaced, a few appear to be marginal facies of the granite and merge into it.|16-MAY-23
24446|Overlander Granite|Relationships and boundaries|The Overlander Granite intrudes the Corella Formation and some amphibolitic metadolerite bodies. It is cut by an apparently unmetamorphosed dolerite dyke.|16-MAY-23
24446|Overlander Granite|Age reasons|Proterozoic|16-MAY-23
24446|Overlander Granite|Defn author|Donchak, Bultitude & Blake 1981|16-MAY-23
24446|Overlander Granite|Proposed publication|Blake & others, in preparation.|16-MAY-23
24446|Overlander Granite|Comments|The Overlander Granite may be equivalent to the Burstall Granite to the north, and to the Revenue Granite to the south. It may also be a correlative of the granite of the Myubee and Mount Erle Igneous Complexes.|16-MAY-23
24446|Overlander Granite|References|98/29253|16-MAY-23
24446|Overlander Granite|Defn Reference|82/22920|16-MAY-23
24446|Overlander Granite|First Reference|82/22710,  82/22663|16-MAY-23
24446|Overlander Granite|Name first published by|Blake, Bultitude & Donchak 1981|16-MAY-23
24446|Overlander Granite|Proposer|Bultitude R.J.|16-MAY-23
24447|Oweenee Rhyolite|Name source|The name is derived from Mount Oweenee, at GR 8059-452604.|16-MAY-23
24447|Oweenee Rhyolite|Unit history|Originally defined as the Oweenee Granite by White (1959) and referred to as such by Wyatt & others (1970).|16-MAY-23
24447|Oweenee Rhyolite|Geomorphic expression|The Oweenee Rhyolite is clearly identifiable on aerial photographs, forming higher, more rugged hills compared to the lower hills of the Malmesbury Microgranite and Silurian-Devonian sedimentary rocks of the Broken River Province.|16-MAY-23
24447|Oweenee Rhyolite|Type section locality|The type area for the Oweenee Granite by White (1959) was a 'good section along the telegraph line, 14 miles (23 km) south of Blue Range Station in Stenhouse Gap'. White's type area stands as the type area for the Oweenee Rhyolite. However, because the section in Stenhouse Gap is roughly parallel to strike and is topographically low, it probably does not contain a significant vertical section through the unit. Therefore several reference sections are also designated. Reference section: The base of the Oweenee Rhyolite is well exposed at GR 7959-380545 in a gully on the western slopes of Mount Mackay, and the section from there to the summit of Mount Mackay at 7959-389542 is designated a reference section. At the base, 5 m of buff to pale grey, moderately crystal-rich rhyolitic ignimbrite, overlies purple, medium to very coarse-grained, thick-bedded lithic sandstone (probably volcaniclastic) of the Lyall Formation. The sandstone dips east at about 20o. The remainder of the section (approximately 600 m) consists of dark grey to pink, generally crystal-rich rhyolitic ignimbrite. Another reference section is along the Kidston power line at 8059-449650 where the basal parat of the unit is exposed. At the base, 5 to 10 m of pink to green crystal-rich rhyolitic ignimbrite containing common flamme up to 10 cm long is inferred to unconformably overlie the Greenvale Formation, although the actual contact does not crop out. This unit is overlain by 5 to 10 m of buff, moderately crystal-rich ignimbrite with smaller fiamme. The uppermost unit is dark grey, moderately crystal-rich to crystal-rich ignimbrite with smaller fiamme, although a eutaxitic foliation is etched out on weathered surfaces. The total thickness of this upper unit has not been determined. Gowrie Creek from GR 8059-438589 to 8059-425612 is the third proposed reference section. In this section, coarse, recrystallised, crystal-rich, biotite rhyolitic ignimbrite are exposed. Variations include the presence of clasts of sedimentary rocks and/or intrusive rocks. Dykes of porphyritic microgranite intrude the ignimbrite.|16-MAY-23
24447|Oweenee Rhyolite|Extent|The Oweenee Rhyolite covers approximately 260 km2 and is restricted to the area south of the Sybil Graben, from near Spring Park homestead in the south, to at least as far north as the Gregory Developmental Road.|16-MAY-23
24447|Oweenee Rhyolite|Thickness range|The thickness is difficult to determine because of the lack of dip information. At least 600 m is exposed in the section at Mount Mackay where the sequence dips 20o east. Assuming a constant easterly dip of 20o, the thickness exposed between the western contact and the topographic high on the east side of Stenhouse Gap, is 1000 m. The total thickness must therefore, be considerably greater.|16-MAY-23
24447|Oweenee Rhyolite|Lithology|Crystal-rich rhyolitic ignimbrite, commonly recrystallised.|16-MAY-23
24447|Oweenee Rhyolite|Relationships and boundaries|The Oweenee Rhyolite is intruded by, but is probably co-magmatic with the Malmesbury Microgranite. This is postulated largely on the basis of their close spatial association rather than geochemical or petrographic evidence. After eruption, the Oweenee Rhyolite was intruded by the remaining magma (i.e. the Malmesbury Microgranite) possibly by a stoping mechanism in which blocks of the overlying ignimbrite fell into the underlying magma. The relationships between the Malmesbury Microgranite and the Oweenee Rhyolite can be seen in the Silver Spray mine area where ignimbrite is intruded by porphyritic microgranite dykes. Similar relationships occur 4 km southeast of Mount George, where dykes of porphyritic microgranite cut the ignimbrite, adjacent to the contact with the Malmesbury Microgranite. Along its northwestern margin the Oweenee Rhyolite unconformably overlies the Silurian Greenvale Formation of the Broken River Province. In Sandy Creek and gullies west of Spring Park Homestead and north to near Mount Mackay the ignimbrite overlies (apparently conformably) sedimentary and volcanic rocks of the Lyall Formation of the Clarke River Group (Scott and Withnall, 1987). The Meath Rhyolite Member, a significant unit in the middle of the Lyall Formation could be a distal equivalent of the Oweenee Rhyolite. It consists of approximately 40 m of biotite bearing, moderately crystal-rich ignimbrite and some sandstone. However, alternative sources for the Meath Rhyolite Member may be some of the rhyolitic plugs within the Clarke Rivr Basin. If so, some of the airfall tuffs in the sequence may be distal equivalents of the Oweenee Rhyolite.|16-MAY-23
24447|Oweenee Rhyolite|Identifying features|The Oweenee Granite was defined by White (1959). He described it as "coarse, pink, porphyritic granite to microgranite, frequently containing zoned feldspars and xenoliths of quartz-biotite hornfels. Grades marginally into a grey, flow banded rhyolite". It was described in more detail by Wyatt & others (1970) who extended the name to include granite which forms the Coane Range to the northeast of the Sybil Graben. Mapping by the Mines Department Officers during the 1986 field season, mainly to the south of the Sybil Graben, has led to a redefinition of the Oweenee Granite as defined by White (1959). Three main lithologies were delineated. These are: (1) crystal-rich rhyolitic ignimbrites; (2) porphyritic microgranite; and (3) an equigranular to rarely porphyritic, coarse biotite granite. Remapping of the type area of White (1959) has shown it to be rhyolitic ignimbrite. Branch (1966) recognised that the Oweenee Granite included some ignimbrite, at least along its western margin, but did not know its full extent. The ignimbrite is now known to be extensive and also includes Mount Oweenee, the feature after which the Oweenee Granite was named. It is therefore proposed that the rhyolitic ignimbrite be named the Oweenee Rhyolite, and that the porphyritic microgranite, which makes up the remainder of the area of White's "Oweenee Granite" to the southeast of the Sybil Graben be named the Malmesbury Microgranite. The equigranular to rarely porphyritic biotite granite, and other granitoids north of the Sybil Graben, all of which were included in Oweenee Granite by Wyatt & others (1970), will not be renamed until further work has been done.|16-MAY-23
24447|Oweenee Rhyolite|Structure and Metamorphism|South of the Daintree mine eutaxitic layering, destroyed in most other places by recrystallisation, indicates a local dip of 8o southwest. Along the Kidston power line dips of 15o south-southeast are indicated by large fiamme. In the Mount Mackay area, a basal ignimbrite rests apparently conformably on sandstone of the Lyall Formation which dips 20o east. A similar relationship occurs in the Spring Park area, where the sedimentary rocks dip 15o southeast. The Oweenee Rhyolite is strongly jointed, most common orientations being northwest and northeast.|16-MAY-23
24447|Oweenee Rhyolite|Age reasons|The age of the Oweenee Rhyolite is not known exactly. However, as suggested above, the Oweenee Rhyolite may be co-magmatic with the Malmesbury Microgranite. Webb (1969) suggested a Middle Carboniferous age (342+/-7 Ma) for the granite on the basis of a Rb/Sr isochron. This age would be consistent with the correlation of the Oweenee Rhyolite with the Meath Rhyolite Member and/or other tuffs in the Lyall Formation. The Lyall Formation is a volcaniclastic unit and is largely Visean in age (Scott, 1985; Playford and Jell, 1985).|16-MAY-23
24447|Oweenee Rhyolite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24447|Oweenee Rhyolite|Comments|Revision of previously published name|16-MAY-23
24447|Oweenee Rhyolite|References|B076; B088; 87/25858; 79/05443; 99/29928; B071; 59;114; R217|16-MAY-23
25377|Pall Mall Granite|Name source|Pall Mall Spring hut and yards, from which the unit is named, are located near the centre of the granite pluton at 8158-139413.  The grid reference is based on the AGD66 datum.|16-MAY-23
25377|Pall Mall Granite|Unit history|The original name for this unit, the "Pall Mall Adamellite", was first published by Wyatt & Jell (1967) but was not formally defined. The unit was also described by Wyatt & others (1970). The name has been changed to Pall Mall Granite to conform with IUGS recommendations (Le Maitre, 1989).|16-MAY-23
25377|Pall Mall Granite|Geomorphic expression|The granite is well exposed and forms large boulders and tors. Residual sand and gravel, as well as minor Tertiary basalt cover a small part of the pluton.|16-MAY-23
25377|Pall Mall Granite|Type section locality|The type locality is beside the Hervey Range Road at 8159-128438 just east of the Dotswood Homestead turnoff.  The grid reference is based on the AGD66 datum.|16-MAY-23
25377|Pall Mall Granite|Description at type locality|Boulders and a few low tors of mottled cream and pink, medium to coarse-grained, moderately porphyritic biotite granite occur at this locality.|16-MAY-23
25377|Pall Mall Granite|Extent|The Pall Mall Granite is an oval-shaped pluton in the southern part of ROLLINGSTONE extending into the northern part of DOTSWOOD. It is roughly 16km long, 10km wide and covers an area of approximately 155km2. It lies 4 to 10km west of Keelbottom Creek and is dissected by Brinagee (Brummagy) Creek.|16-MAY-23
25377|Pall Mall Granite|Lithology|The Pall Mall Granite is a mottled cream and pink, medium to coarse grained, moderately to abundantly porphyritic biotite granite. The Pall Mall Granite has sparse, dark grey, fine-grained, rounded, dioritic xenoliths up to 15cm long.|16-MAY-23
25377|Pall Mall Granite|Relationships and boundaries|The Pall Mall Granite intrudes the Proterozoic(?) Argentine Metamorphics, sedimentary rocks of the Late Devonian Dotswood Group, and the Ravenswood Granodiorite Complex. A small portion of the pluton is overlain by Tertiary-Quaternary sediments and Tertiary basalt.|16-MAY-23
25377|Pall Mall Granite|Age reasons|Webb (1969) determined a K-Ar biotite age of 289 Ma for the Pall Mall Granite, close to the Carboniferous - Permian boundary.|16-MAY-23
25377|Pall Mall Granite|References|Le MAITRE, R.W., 1989: A Classification of Igneous Rocks and Glossary of Terms. Blackwell, London.WEBB, A.W., 1969: Metallogenic epochs in eastern Queensland.  Proceedings of the Australasian Institute of Mining and Metallurgy, 230, 27 39.WYATT, D.H. & JELL, J.S., 1967: Devonian of the Townsville hinterland, Queensland, Australia; in Oswald, D.H. (Editor): International Symposium of the Devonian System, Volume 2. Alberta Society of Petroleum Geologists, Calgary, 99 105.WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127.|16-MAY-23
23891|Paluma Rhyolite|Name source|The unit is named after the Paluma Range and also the township of Paluma.|16-MAY-23
23891|Paluma Rhyolite|Unit history|Wyatt & others (1970) previously termed these rocks the "Unnamed Dark Grey Volcanics" (Cuy). Our mapping has not greatly altered the unit's boundaries in the northern part of ROLLINGSTONE, but rocks in the southeast portion of the sheet that were previously mapped as Cuy are not included in the Paluma Rhyolite.|16-MAY-23
23891|Paluma Rhyolite|Type section locality|A road cutting on the Paluma Ewan Road (8159 107969) about 6km west of Paluma township provides good exposure.  The grid reference is based on the AGD66 datum.|16-MAY-23
23891|Paluma Rhyolite|Description at type locality|Dark grey, very crystal-rich rhyolitic ignimbrite.|16-MAY-23
23891|Paluma Rhyolite|Thickness range|The thickness of the Paluma Rhyolite cannot be accurately measured. Orientation of fiamme indicate that the unit is relatively flat lying. It crops out from near sea level to the top of the Paluma Range, suggesting that the unit is up to 900m thick.|16-MAY-23
23891|Paluma Rhyolite|Lithology|The Paluma Rhyolite is predominantly a dark grey, crystal-rich to very crystal-rich rhyolitic ignimbrite. Crystal content is generally over 50% consisting of quartz (25-30%), K-feldspar (15 20%), plagioclase (10-15%) and mafic minerals (<5%). The ignimbrite contains sparse fiamme (<5%) up to 2cm long and rare andesitic or dacitic lithic clasts up to 1.5cm.|16-MAY-23
23891|Paluma Rhyolite|Relationships and boundaries|Spatial relationship and dips measured in the Blue Gum Creek area suggest that the Paluma Rhyolite unconformably overlies the Saint Giles Volcanics. To the west it is intruded by the Coane Range Granite Complex and to the east it has been intruded by the Clemant Microgranite. Geochemical data suggest the Paluma Rhyolite is co-magmatic with the Clemant Microgranite (Gunther & Withnall, 1992) and is part of a suite that includes most of the Early Carboniferous granites in the region. M. Fanning (Appendix 1) obtained a U-Pb zircon (SHRIMP) age of 337±6 Ma for the Clemant Microgranite|16-MAY-23
23891|Paluma Rhyolite|Age reasons|Based on relationships detailed above, the Paluma Rhyolite is therefore inferred to be Early Carboniferous.|16-MAY-23
23891|Paluma Rhyolite|References|GUNTHER, M.C. & WITHNALL, I.W., 1992: Late Palaeozoic igneous rocks of the Rollingstone and Ewan 1:100 000 Sheet areas. Queensland Resource Industries Record 1992/17WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127.|16-MAY-23
14851|Papilio Mudstone|Name source|Papilio Creek which joins Bracteata Creek at 7858-574392.  The grid reference is based on the AGD66 datum.|16-MAY-23
14851|Papilio Mudstone|Unit history|The Papilio Mudstone was previously mapped as part of the Broken River Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
14851|Papilio Mudstone|Geomorphic expression|Generally recessive topography, and commonly poorly grassed, being represented by light tones on airphotos.|16-MAY-23
14851|Papilio Mudstone|Type section locality|In a gully flowing into Bracteata Creek between 7858-574403 (boundary with the Dosey Limestone) and 575402 (boundary with Mytton Formation).   The grid references are based on the AGD66 datum.  REFERENCE SECTIONS:  (1) Between 7858-595402 (base) in an unnamed gully and 595402 (top) on the left flank of Dosey Creek (part of section SD146 of Mawson & Talent, in press); (2) 295 m between 7858-606412 in Lomandra Creek (boundary with Dosey Limestone) and 604414 (boundary with Mytton Formation) in a small gully east of Lomandra Creek (Withnall & others, 1988, figure 28).|16-MAY-23
14851|Papilio Mudstone|Description at type locality|The section consists of 200 m of calcareous mudstone with minor fine-grained calcareous sandstone and nodular limestone (packstone and wackestone).  It is part of section SD196 of Mawson & Talent (in press).|16-MAY-23
14851|Papilio Mudstone|Extent|A narrow southwest-trending belt from near Jessey Springs at about 7859-675517 to the Broken River.  South of the Broken River, it is intricately folded with other units of the Broken River Group from the headwaters of Dosey Creek to about 2 km west of Spanner Hill.|16-MAY-23
14851|Papilio Mudstone|Thickness range|200m at type section.|16-MAY-23
14851|Papilio Mudstone|Lithology|Calcareous mudstone and generally minor fine-grained calcareous sandstone and nodular limestone.  The proportion of sandstone increases to the southwest.  A thick unit of limestone southwest from Pages Creek to Spanner Hill is assigned to the Spanner Limestone Member.  Limestone is also well developed south of the Broken River between 7859-580436 and 591449, and is also assigned to this member.|16-MAY-23
14851|Papilio Mudstone|Fossils|The unit contains common to locally abundant brachiopods, solitary rugose and tabulate corals, stromatoporoids, bivalves, gastropods, crinoids, conodonts, and plant fragments.|16-MAY-23
14851|Papilio Mudstone|Relationships and boundaries|The Papilio Mudstone is the uppermost formation in the Wando Vale Subgroup of the Broken River Group.  South of the Broken River it conformably overlies the Dosey Limestone, whereas to the north, between the river and Jessey Springs it conformably overlies the Burges Formation.  Thin mudstone intervals overlying the Lockup Well and Dip Creek Limestones are also equated with the Papilio Mudstone, but are mostly too thin to map out.  The unit contains the Spanner Limestone Member between Pages Creek and Spanner Hill.  The Papilio Mudstone is conformably overlain by the Mytton Formation.|16-MAY-23
14851|Papilio Mudstone|Age reasons|A latest Eifelian to late Givetian age is indicated (Mawson & Talent, in press).|16-MAY-23
14851|Papilio Mudstone|References|MAWSON, R., & TALENT, J.A., in press:  Late Emsian-Givetian stratigraphy and conodont biofacies - carbonate slope and offshore shoal to sheltered lagoon and nearshore carbonate ramp - Broken River, north Queensland.  Courier Forschungs-Institute Senckenburg. **WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. **WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of 	Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes. **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River 	area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
14857|Paradise Creek Formation|Name source|Paradise Creek which joins Gunpowder Creek at 6758-210135.|16-MAY-23
14857|Paradise Creek Formation|Unit history|The rocks now included in the redefined Paradise Creek Formation were previously part of the Paradise Creek Formation of de Keyser (1958). In the Lawn Hill and northern part of the Camooweal 4-mile Geological Sheets they were included in the Ploughed Mountain Beds by Carter & others (1961). Cavaney (1975) proposed to name these rocks "Paradise Formation".|16-MAY-23
14857|Paradise Creek Formation|Type section locality|Holostratotype: Along Paradise Creek from 195146 (base) to 137170 (top) in the Mammoth Mines 1:100 000 Sheet area.The base of the holostratotype is about 1.5 km along Paradise Creek from its junction with Gunpowder Creek. The Paradise Creek Formation in the type section has been subdivided into four subunits, the lowermost of which is defined as the Mount Oxide Chert Member; the other three subunits remain informal. The four subunits are, from top to bottom: Subunit 4: Approximately 350 m of dolomite, stromatolitic dolomite and intraclast dolomite containing "cauliflower chert" structures (replacements after anhydrite) and minor chert nodules.  Subunit 3: Middle stromatolite marker (informal); stromatolitic chert and sandstone.  Subunit 2: Approximately 1000 m of interbedded dolomite and siltstone, stromatolitic dolomite, intraclast dolomite, chert and minor sandstone.  Subunit 1: Mount Oxide Chert Member: Two metre thick bed of laminated to thinly bedded chert. It forms the base of the Paradise Creek Formation.|16-MAY-23
14857|Paradise Creek Formation|Extent|The unit crops out extensively in the eastern parts of the Lawn Hill and Riversleigh 1:100 000 Sheet areas. It is best exposed along the western margin of the Mount Oxide 1:100 000 Sheet area, and also crops out extensively in the Mammoth Mines, Kennedy Gap and Yelvertoft 1:100 000 Sheet areas.|16-MAY-23
14857|Paradise Creek Formation|Thickness range|The maximum thickness recorded is 850 m in the type section. In the Lawn Hill 1:100 000 Sheet area, the thickness is 500 m. It is thickest in the western part of the Mammoth Mines 1:100 000 Sheet area where it is 1400 m thick.|16-MAY-23
14857|Paradise Creek Formation|Lithology|The lithology of the Unit throughout the region differs little from the type section. The Mount Oxide Chert Member is present everywhere except in the northernmost outcrops. The middle stromatolite marker is not always present and may be a facies equivalent of the massive quartz sandstone which occurs at about this stratigraphic level in the Kennedy Gap, Mount Oxide and western part of the Mammoth Mines Sheet areas.|16-MAY-23
14857|Paradise Creek Formation|Relationships and boundaries|The Paradise Creek Formation conformably overlies the Gunpowder Creek Formation. This boundary is placed at the base of the Mount Oxide Chert Member which occurs in most basal sequences and is easily recognised as it forms a low but persistent ridge. The Paradise Creek Formation is conformably overlain by the Esperanza Formation. This boundary is placed at the base of the lowermost of a series of massive stromatolitic cherts.|16-MAY-23
14857|Paradise Creek Formation|Age reasons|Mid Proterozoic (Carpentarian).|16-MAY-23
14857|Paradise Creek Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
14857|Paradise Creek Formation|References|58/100|16-MAY-23
24451|Parrot Camp Rhyolite|Name source|Parrot Camp dam; GR 7361-425027.|16-MAY-23
24451|Parrot Camp Rhyolite|Unit history|The rhyolite is a previously undifferentiated part of the Croydon Volcanics (Branch, 1966). Mackenzie (1983) informally named and described the 'Parrot Camp rhyolite'.|16-MAY-23
24451|Parrot Camp Rhyolite|Geomorphic expression|The unit occurs in areas of moderate to gentle relief with relatively sparse tree cover compared to surrounding units. Bouldery outcrops are common.|16-MAY-23
24451|Parrot Camp Rhyolite|Type section locality|The type section extends from GR 7361-412065 (base) south to -416048, thence southwest to -404025. It is made up of about 300 m of dark grey to greenish-grey, medium-coarse-grained, moderately crystal-rich rhyolitic ignimbrite overlain by about 10 m of very dark-grey, medium to fine-grained, crystal-rich dacitic ignimbrite. The base of the section is a conformable (?) contact with very dark grey, medium to coarse-grained, crystal-poor, intensely recrystallised rhyodacitic ignimbrite (B Creek Rhyolite), and the top of the section is an abarupt, concordant, possibly paraconformable transition into massive, medium to dark-grey, fine-grained, crystal-poor rhyolitic ignimbrite (Carron Rhyolite).|16-MAY-23
24451|Parrot Camp Rhyolite|Extent|The unit crops out in a belt extending from west and northwest of Parrot Camp dam to about 3 km east of the Near Carron River, and also to the south and southwest of the dam around the head of Dead Horse Creek. Similar rocks, which occupy the same stratigaraphic position and are therefore correlated with the unit, occur in a small area near Golden Gate Creek, 8 km northwest of Croydon.|16-MAY-23
24451|Parrot Camp Rhyolite|Thickness range|The thickness ranges up to possibly 200 or 300 m, but is difficult to estimate because of the generally massive nature of the formation. The topographic relief in the type area indicates a minimum thickness there of about 60 m. The unit lenses out completely to the east of the Near Carron River.|16-MAY-23
24451|Parrot Camp Rhyolite|Lithology|The rock is a dark-grey to green-grey, coarse, moderately crystal-rich rhyolitic ignimbrite with abundant crystals (up to 4 mm) of quartz, pale greenish altered plagioclase, and white K-feldspar; pellets (up to 1 cm across) of graphite are common. The rock is commonly massive, but in some places has an irregular eutaxitic structure consisting of alternating lenses of paler and darker rock (e.g. outcrop at GR 420039, 1.3 km northwest of Parrot Camp Dam). The rock is very similar in appearance, mineralogy and composition to another unit in the Croydon Volcanic Group, the Idalia Rhyolite.|16-MAY-23
24451|Parrot Camp Rhyolite|Relationships and boundaries|The unit is interpreted as overlying the B Creek Rhyolite from its geographical distribution between this rhyolite and the overlying Carron Rhyolite. The relationship with the Carron Rhyolite is indicated to the south and southwest of Parrot Camp Dam, where the Carron Rhyolite forms ridges and in some places cliffs above the Parrot Camp Rhyolite in the valleys below, and where the contacts tend to follow contours levels.|16-MAY-23
24451|Parrot Camp Rhyolite|Age reasons|The age is Middle Proterozoic as for the rest of the Croydon Volcanic Group.|16-MAY-23
24451|Parrot Camp Rhyolite|Defn author|Mackenzie D.E., Henderson G.A.M., Warnick J.V., Bain J.H.C., 1985|16-MAY-23
24451|Parrot Camp Rhyolite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24451|Parrot Camp Rhyolite|References|B076|16-MAY-23
24451|Parrot Camp Rhyolite|Defn Reference|86/25125 Mention Map legend|16-MAY-23
24451|Parrot Camp Rhyolite|Proposer|Mackenzie D.E., Warnick J.V., Henderson G.A.M.|16-MAY-23
23894|Peak Vale Granodiorite|Name source|Peak Vale homestead at 8351-360356.  The grid reference is based on the AGD66 datum.|16-MAY-23
23894|Peak Vale Granodiorite|Geomorphic expression|Relief is low compared with the surrounding metamorphic rocks, and the area is gently undulating. Outcrop is good in Theresa Creek, forming platforms up to tens of metres across, but is poor elsewhere because of a thick weathering profile and extensive deposits of alluvial gravels, especially in the north.  The Peak Vale Granodiorite is delineated on the Landsat 5 TM (1-4-7 BGR) image by cleared areas that have a yellowish hue. The unit exhibits complex magnetic anomalies with strongest responses along the northern and southern margins, and very low anomalies in the central portion. K, Th and U responses are strongest in the south and central area of outcrop, but are generally low elsewhere.|16-MAY-23
23894|Peak Vale Granodiorite|Type section locality|At 8351-326347, 3 km west of Peak Vale Homestead.  The grid reference is based on the AGD66 datum.|16-MAY-23
23894|Peak Vale Granodiorite|Description at type locality|Two rock types, representative of the unit, are exposed; a biotite-hornblende granodiorite and biotite-hornblende quartz diorite or monzodiorite.|16-MAY-23
23894|Peak Vale Granodiorite|Extent|An east-west trending oval pluton, 8 km by 5 km, on the central-west margin of the Retreat Batholith.|16-MAY-23
23894|Peak Vale Granodiorite|Lithology|Two main rock-types make up the Peak Vale Granodiorite - grey, fine to coarse-grained, subequigranular to porphyritic pyroxene-biotite-hornblende granodiorite, and subordinate quartz monzodiorite of similar texture and composition. The quartz monzodiorite is found only in the southern half of the pluton.|16-MAY-23
23894|Peak Vale Granodiorite|Relationships and boundaries|Largely surrounded by and intrudes the Anakie Metamorphic Group. To the east, it probably intrudes the Kilmarnock Granodiorite.|16-MAY-23
23894|Peak Vale Granodiorite|Age reasons|Ages of 369 Ma and 376 Ma were obtained from Rb-Sr dating of biotite-whole rock pairs from the granodiorite and quartz monzodiorite respectively. The age is therefore Middle Devonian and similar to ages from the Kilmarnock Granodiorite.|16-MAY-23
15032|Pemberton Grange Basalt|Name source|The name is derived from the locality of Pemberton Grange approximately 10 km east of Bundaberg on the Bundaberg-Elliott Heads road. Pemberton Grange is located at GR 442488 Bundaberg 1:100 000 Sheet area (latitude 24o52'26"S, longitude 152o26'46"E, Bundaberg 1:250 000 Sheet SG 56-2). The basalt cropping out at the surface at Pemberton Grange is Hummock Basalt but it is in this area that the maximum thickness of subsurface basaltic lava has been intersected in water bores in the Bundaberg Trough.|16-MAY-23
15032|Pemberton Grange Basalt|Type section locality|The type section of the Pemberton Grange Basalt is taken as the 45 m of cored volcanics extending from 69 m to 114 m in Fairymead NS1 drillhole drilled 4.2 km north of Fairymead Sugar Mill at GR 353619 Bundaberg 1:100 000 Sheet area. The top is defined by red clay, the decomposition product vesicular basalt. The base is defined by weathered vesicular basalt. The material designated as the type section is stored at the Queensland Mines Department core storage library at Redbank under the designation Fairymead NS1. The hole was drilled by the Drilling Branch of the Mines Department at the request of the Geological Survey of Queensland.|16-MAY-23
15032|Pemberton Grange Basalt|Extent|The unit is not exposed at the surface. It is known to occur over a distance of more than 40 km extending from Moore Park to south of the Elliott River in the Bundaberg Trough, and that its subsurface extent on land probably exceeds 80 km2.|16-MAY-23
15032|Pemberton Grange Basalt|Thickness range|The maximum thickness intersected is 45 m in Fairymead NS1.|16-MAY-23
15032|Pemberton Grange Basalt|Lithology|Microporphyritic olivine basalt occurring as both the massive and vesicular varieties and varying in colour from black to grey black when unweathered. The upper part of the unit has been altered to a red clay to a depth of approximately 4.6 m. In thin section, olivine (10 percent) occurs as altered euhedral to subhedral microphenocrysts of up to 2 mm diameter set in a fine-grained groundmass of labradorite feldspar (50 percent), augite (15 percent), glass (20 percent) and opaques (5 percent).The euhedral to subhedral labaradorite laths average 0.3 mm in length, but may attain a length up to 1.2 mm while the subophitic grains of augite rarely exceed 0.5 mm in diameter partly enclosing as well as interstitial to plagioclase.|16-MAY-23
15032|Pemberton Grange Basalt|Relationships and boundaries|Basalt unconformably overlies the Cretaceous Burrum Coal Measures and is unconformably overlain by late Early Eocene sediments (informally named Fairymead beds). The base of the unit is taken as the change from sediments of the Burrum Coal Measures to volcanic material. The upper boundary is fixed by the change from basalt or its weathering products to sediments.|16-MAY-23
15032|Pemberton Grange Basalt|Identifying features|Geophysical characteristics: No geophysical investigations have been conducted on the unit.|16-MAY-23
15032|Pemberton Grange Basalt|Age reasons|The basalt unconformably overlies the Burrum Coal Measures of late Aptian to Albian age (Ellis & Whitaker, 1976) and is nonconformably overlain by late Early Eocene sediments. Based on stratigraphic and tectonic evidence for the formation of the Bundaberg Trough, the age of the Pemberton Grange Basalt is tentatively given as Paleocene to Early Eocene. Isotopic data are not available.|16-MAY-23
15032|Pemberton Grange Basalt|References|79/01354|16-MAY-23
15032|Pemberton Grange Basalt|Defn Reference|79/20398|16-MAY-23
79130|Pengelly Siltstone Member|Name source|Named after the Pengelly Bridge which crosses the old fossicking area on Deep Creek on the Tin Can Bay Road.|16-MAY-23
79130|Pengelly Siltstone Member|Unit history|Termed the 'Phoenix slates' and the 'Monkland slates' by the early miners as described by Rands (1889).  One of these terms could have taken preference in nomenclature but the correlation was not well established in the early years of GEGM mining when the informal term Pengelly siltstone was introduced.  Equivalent to Dunstan's (1911) First Slate Group (1TS, 1TC, 1MS). Formally registered as  Pengelly Siltstone Member after Cranfield (1999) and referred to by Sivell & Arnold (1999) and Sivell & McCulloch (2001), Li & others (2015).|16-MAY-23
79130|Pengelly Siltstone Member|Type section locality|BHP Drill hole G023, depth 82-130m, at north end of Monkland Mine, collar 468180mE; 7100900mN, Lat: -26°12'40"  Long: 152°40'53",  held in Zillmere storage facility, Brisbane. Outcrop is almost non-existent but small appearances might be found in Deep Creek below the Pengelly Bridge and to the east of the Dawn Mine. Reference sections in other holes: GEGM drill hole G135: 77-135 m near the Aurelia shoot, Monkland Mine. GEGM drill hole G137: 272-360 m at Monkland Mine. GEGM drill hole L015B: 0-108 m drilled from 12 Level, Monkland Mine (MGA 468910mE; 7100250mN).  Core hld in Zillmere core library.|16-MAY-23
79130|Pengelly Siltstone Member|Description at type locality|Predominantly dark grey to black, variably carbonaceous siltstone and shale, also finely sericitised and chloritised siltstone alternating with concentrated lenses of finely dispersed carbonaceous material .  Carbonaceous beds are mostly fairly massive with poor wispy bedding, occasionally laminated.  They are prone to shearing parallel to bedding, producing a distorted and disrupted schistose mass of coarse clays and foliae of graphitic material with pyrite.  Mostly non calcareous in places weakly so. Pyrite is common, both euhedral and framboidal varieties.|16-MAY-23
79130|Pengelly Siltstone Member|Extent|Best developed in the Phoenix, Monkland and Dawn blocks. Maximum thickness is about 70 m in the Monkland Block, up to 60 m in the Phoenix Block where Rands (1889) records thin conglomerate and sandstone beds within the shale beds, and 30-80 m thick east of the Dawn Mine. It is also preserved in down-faulted wedges at Partridge (25-40 m thick) and at the Wylly prospect but has not been located in the Six Mile Block.|16-MAY-23
79130|Pengelly Siltstone Member|Thickness range|25 to 70m, wedging out to the north.|16-MAY-23
79130|Pengelly Siltstone Member|Lithology|Consists predominantly of dark grey to black, variably carbonaceous siltstone and shale (Photograph 8), also finely sericitised and chloritised siltstone alternating with concentrated lenses of finely dispersed carbonaceous material (GG073). Carbonaceous beds are mostly fairly massive with poor wispy bedding, occasionally laminated. They are prone to shearing parallel to bedding, producing a distorted and disrupted schistose mass of coarse clays and foliae of graphitic material with pyrite. Is mostly non-calcareous at Monkland, in places weakly so. Waterhouse & Balfe (1987) describe it as 'very rich in fossils'. Miethke (2000) and Gray (1999) found that the dominant minerals are fine detrital quartz and feldspar along with chlorite, albite and calcite, and occasional volcanic fragments. Pyrite is common, both euhedral and framboidal varieties. The geochemistry of these sediments has been studied in detail by Gray (1999).|16-MAY-23
79130|Pengelly Siltstone Member|Fossils|This unit in the Monkland Block rarely contains shell fragments whereas futher north in the Phoenix Block (city centre of Gympie) Rands (1889) found it to be fossiliferous. Waterhouse & Balfe (1987) describe a faunal assemblage they assign to their ?Cancrinelloides fauna which they identify as probable early Sakmarian age within the Lower Permian.|16-MAY-23
79130|Pengelly Siltstone Member|Relationships and boundaries|At Monkland the carbonaceous unit occurs above volcanoclastic sandstone of the Nash Clastics and below the Langton Dolerite, separated from it by a fissile and slaty graphitic break. Some sandstone also may occur above the Pengelly Siltstone. This is the most economically important unit on the field, being host to the high grade historically mined (particularly between 1870 and 1925) Gympie Veins as well as the sheeted veins, termed Stockworks, mined in recent times. Reference GEGM drill hole L015B shows narrow sheeted auriferous quartz veins in Pengelly Siltstone, part of the 6A Stockwork ore body.|16-MAY-23
79130|Pengelly Siltstone Member|Age reasons|Waterhouse and Balfe (1987) describe a faunal assemblage they assign to their ?Cancrinelloides fauna which they identify as probable early Sakmarian age in the Lower Permian.|16-MAY-23
79130|Pengelly Siltstone Member|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie 12-JAN-2017.|16-MAY-23
79130|Pengelly Siltstone Member|References|Rands, W.H. 1889: Gympie Goldfield. Publs. Geol. Surv. Qld 52.  **Dunstan, B., 1911: Geology map of Gympie and environs. GSQ Publ. No. 221b.  Waterhouse, J.B. and Balfe, P.1987: Stratigraphic and faunal subdivisions of the Permian rocks at Gympie. IN Murray, C.G. & Waterhouse, J.B. (Eds). 1987 Field Conference, Gympie District.  Geol. Soc. Australia, Queensland.  **Cranfield, L.C., 1999:Gympie Special Sheet 9445, Part 9545, Queensland 1:100,000 Geological Map Commentary.Queensland Department of Mines and Energy, Brisbane.  **Sivell, W.J. and Arnold, G.O. 1999:Geochemical and volcanic stratigraphy of a segment of an island arc - Gondwana rim accretion zone, Gympie Province, southeast Queensland.  In Flood, P.G. (Editor): Regional Geology, Tectonics and Metallogenesis, New England Orogen, NEO '99 Conference, 255-266.  ** Sivell, W.J. and McCulloch, M.T. 2001: Geochemical and Nd-isotopic systematics of the Permo-Triassic Gympie Group, southeast Queensland.  Australian Journal of Earth Sciences 48, 377-394.  **Li, P., Rosenbaum, G., Yang, J-H. and Hoy, D. 2015	Australian-derived detrital zircons in the Permian-Triassic Gympie terrane (eastern Australia): Evidence for an autochthonous origin. Tectonics, 34, 858-874.|16-MAY-23
15163|Pickwick Metabasalt Member|Name source|Pickwick' pastoral blocks of the Whitworth holding 56 km north of Mount Isa situated between 20o2'S latitude and 20o23'S latitude and between 139o27'E longitude and the Leichhardt River. The name "Pickwick Beds" was introduced as an informal name by Robinson (1968); since this unit is generally well exposed, and its relationships to other units is readily determined, it is proposed that the unit become a formal member.|16-MAY-23
15163|Pickwick Metabasalt Member|Type section locality|No type section was nominated by Robinson (1968) but an area 48 km north-northeast of Mount Isa, between Paroo and Conglomerate Creek would be suitable. It is 19 km south-southwest of Julius dam, and is traversed by the Mt Isa-Julius dam pipeline road; GR 581565 in the Prospector 1:100 000 Sheet area, latitude 20o27'20"S, longitude 139o38'E to latitude 20o16'45"S, longitude 139o38'45"E. The type section contains 750 m of massive and amygdaloidal breccia, basalt, and white to dark grey quartzite. At least three quartzite interbeds are present - a 10 m to 60 m thick white quartzite, a 3 m and a 5 m thick dark grey quartzite, 130 m, 315 m and 600 m from the base of the member, respectively. Other complete sections of the Pickwick Metabasalt Member occur 10 to 15 km northeast of Mount Isa.|16-MAY-23
15163|Pickwick Metabasalt Member|Extent|As for the Eastern Creek Volcanics, in a north-trending belt (centred on Mount Isa) 300 km long and up to 40 km wide, mainly in the Cloncurry & Dobbyn 1:250 000 Sheets. The member is not mapped west of the Mount Isa Fault zone.|16-MAY-23
15163|Pickwick Metabasalt Member|Thickness range|About 750 m.|16-MAY-23
15163|Pickwick Metabasalt Member|Lithology|Metabasalt, amygdaloidal metabasalt, flow-top breccia, quartzite, tuffaceous beds, purple siltstone.|16-MAY-23
15163|Pickwick Metabasalt Member|Relationships and boundaries|Underlain conformably by the Lena Quartzite Member; overlain conformably by the Myally Subgroup, and unconformably by the Mount Isa Group. From the Leander Range area north to Mt Oxide the proportion of sedmentary intercalations relative to metabasalt appears to increase.|16-MAY-23
15163|Pickwick Metabasalt Member|Age reasons|As for the Haslingden Group, between 1700 m.y. and 1650 m.y.|16-MAY-23
15163|Pickwick Metabasalt Member|References|99/29866|16-MAY-23
22657|Pinchgut Granite|Name source|The unit was named by Richards (1981) after Pinchgut Pinnacle, a prominent knoll of granite about 12.5 km east-northeast of Chillagoe.|16-MAY-23
22657|Pinchgut Granite|Unit history|Formerly mapped as part of the Almaden Granite (Best, 1962;  de Keyser & Wolff, 1964;  de Keyser & Lucas, 1968).|16-MAY-23
22657|Pinchgut Granite|Extent|The granite forms a roughly ovoid, northeasterly trending pluton of 2 km2 east of Pinchgut Creek.  The small pod of granite 1.5 km to the south is tentatively mapped as Pinchgut Granite.|16-MAY-23
22657|Pinchgut Granite|Lithology|(after Richards, 1981;  Mouthier & Schumacher, 1981):  The unit consists mainly of coarse-grained biotite leucogranite characterised by a relatively high K feldspar content.Quartz forms large irregular, locally composite grains up to 8 mm across.  K-feldspar is orthoclase microperthite or microcline microperthite and forms simply twinned grains up to 10 mm long.  Granophyric intergrowths are reportedly present in parts of the pluton.  Plagioclases are mainly subhedral laths, up to 8 mm long, with sericitised cores of andesine (~An42) mantled mainly by normally zoned oligoclase (~An20-An14).  Oscillatory zoning is rare and, where present, weakly developed.  Some plagioclase grains lack andesine cores.  Plagioclases in contact with K-feldspar commonly have an outer rim of albite either in optical continuity with the enclosed plagioclase grains or as aggregates of small (0.5 to 1 mm across) grains.  Albite is also reported to form coarse perthitic lamellae, and is commonly associated with quartz in myrmekitic intergrowths.Biotite, pleochroic from straw yellow to brown, forms subhedral grains up to 4 mm long.The main accessory minerals are apatite, zircon, and magnetite containing ilmenite lamellae.The Pinchgut Granite has undergone some hydrothermal alteration.  Feldspars are commonly clouded and calcic plagioclase cores and biotite grains are commonly partly replaced by sericite and chlorite, respectively.  Less common secondary minerals reported are muscovite, calcite, fluorite, and iron oxides (commonly forming aggregates of small grains).Enclaves are small (average diameter about 1.5 cm) and rare, and consist of granular aggregates of anhedral plagioclase, quartz and biotite grains in about the same abundance, and subordinate K feldspar.  Accessory minerals are scarce.|16-MAY-23
22657|Pinchgut Granite|Relationships and boundaries|The granite intrudes the Ruddygore Granodiorite.  The pluton tentatively assigned to this formation south of Pinchgut Pinnacle may also intrude the Featherbed Volcanics.|16-MAY-23
22657|Pinchgut Granite|Structure and Metamorphism|The Pinchgut Granite is cut by several faults and by numerous joints and small-scale fractures.  Mouthier & Schumacher (1981) reported that the northern pluton is cut by an easterly trending mylonite zone, about 4 m wide.|16-MAY-23
22657|Pinchgut Granite|Age reasons|The granite is most probably Late Carboniferous.  It has not been isotopically dated.|16-MAY-23
22657|Pinchgut Granite|Alteration and Mineralisation|MINERALISATION::  Minor uranium mineralisation has been reported from several places in the northern pluton (Mouthier & Schumacher, 1981).  According to Mouthier & Schumacher (1981) the anomalous zone is 1.5 km long and 1 km wide and the main areas of mineralisation are located along an easterly trending mylonite zone.  The principal uranium mineral identified is novacekite, a yellow hydrated magnesium uranyl arsenate [Mg(UO2)2 (AsO4)2.9H2O].  A green radioactive mineral (torbenite?) is also present in places.  The uranium minerals are generally associated with pyrite and psilomelane, and occur mainly along joints and fractures in the granite.  In 1981, AFMECO Pty Ltd drilled 36 shallow (3 m) percussion holes in the two main radiometric anomalies.  The drilling indicated that yellow and pale green secondary uranium-bearing minerals persisted in the granite to depths of at least 3 m.|16-MAY-23
22657|Pinchgut Granite|Comments|The Pinchgut Granite is a member of the Ootann Supersuite.  The common occurrence of exsolved albite in the K-feldspar grains, the presence of granophyric intergrowths and the narrow contact metamorphic aureole indicate that the Pinchgut Granite was emplaced at relatively high crustal levels, possibly to within 6 to 3 km of the surface (Richards, 1981).  It is a subvolcanic granite using the classification of White & others (1964).|16-MAY-23
22657|Pinchgut Granite|References|BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.DE KEYSER, F., & LUCAS, K.G., 1968:  Geology of the Hodgkinson and Laura Basins, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 84.DE KEYSER, F., & WOLFF, K.W., 1964:  The geology and mineral resources of the Chillagoe area.  Bureau of Mineral Resources, Australia, Bulletin 70.MOUTHIER, B., & SCHUMACHER, F., 1981:  A.P. 2782M, 2933M, 2783M, 2934M.  Featherbed. AFMECO Pty Ltd Annual Report for 1981.  Report No. TW81.12 (held as CR 11100).RICHARDS, D.N.G., 1981:  Granitoids of the northern Tate batholith, Chillagoe, north Queensland.  Ph.D. Thesis, James Cook University of North Queensland, Townsville (unpublished).|16-MAY-23
26320|Pindari Formation|Name source|'Pindari Hills' located approximately 1 km west of the Taroom-Cracow road between Cracow homestead and Cracow township, GR 263910-GR 269950 Cracow 1:100 000 Sheet 8947.|16-MAY-23
26320|Pindari Formation|Unit history|Wass (1965) and subsequent workers included this sequence in the Buffel or Oxtrack Formations.|16-MAY-23
26320|Pindari Formation|Type section locality|Section normal to the strike 1.8 km NW of Cracow homestead from GR 265913 to 262913, Cracow 1:100 000 Sheet area 8947. The section commences on the eastern flank of Pindari Hills, traverses the ridge line and continues down the dip stope on the western side of the ridge. The lower 50 m is obscured by scree and the upper 50 m consists of tuffs up to several metres thick, tuffaceous sandstone, and shales.|16-MAY-23
26320|Pindari Formation|Extent|The unit crops out in an elongate NW-SE trending belt from southwest of Cracow homestead for 7 km to the vicinity of GR 265966. Similar rocks occur in the core of the syncline to the SW of Buffel Hill. The unit may be represented in the lower section of GSQ drill hole Banana NS1 where a thick sequence of tuffaceous and tuff-derived sediments occurs below 213 m.|16-MAY-23
26320|Pindari Formation|Thickness range|100 m in type section but the unit thins rapidly northwards.|16-MAY-23
26320|Pindari Formation|Lithology|Primarily a bedded sequence of reworked siliceous tuffs and interbedded grey shales. Individual tuff beds range in thickness from a few metre to several metres.|16-MAY-23
26320|Pindari Formation|Fossils|Fauna: Brachiopods (unidentifiable), sponge spicules and brachiopod spines, and plant remains.|16-MAY-23
26320|Pindari Formation|Relationships and boundaries|The base of the unit is not seen but is likely to be conformable on Buffel Formation. Conformably overlain by the Brae Formation.|16-MAY-23
26320|Pindari Formation|Age reasons|The age of the unit can be determined from the ages of the underlying and overlying units i.e. between Sakmarian to Baigendzinian, possibly Sarginian (Early Permian).|16-MAY-23
26320|Pindari Formation|References|98/29407|16-MAY-23
26320|Pindari Formation|Proposer|Flood P.G., Jell J.S., Waterhouse J.B.|16-MAY-23
15253|Pinecliff Formation|Name source|Campbell (1952) derived the name from Pinecliff Ridge, a prominent geomorphic feature about 3 km south of Mount Deongwar.|16-MAY-23
15253|Pinecliff Formation|Unit history|Campbell (1952) recognised a three-fold subdivision of the formation. He named the volcanic middle part the Kipper Creek Andesites.  These have not been identified during the current mapping as separate units|16-MAY-23
15253|Pinecliff Formation|Geomorphic expression|The unit occupies a rugged, thickly forested area of 78 km2 south of Oakey Creek, at an average elevation of about 450m above sea level.|16-MAY-23
15253|Pinecliff Formation|Type section locality|Type section designated along Cressbrook and Oakey Creeks (Cranfield & others, 1976).|16-MAY-23
15253|Pinecliff Formation|Extent|The unit crops out along Cressbrook and Oakey Creeks, and its type section was designated along the creek (Cranfield & others, 1976).|16-MAY-23
15253|Pinecliff Formation|Thickness range|To the south of Mount Sugarloaf the unit is approximately 1500 m thick.  Cranfield & others (1976) did not consider this as the maximum thickness of the unit as the base is truncated by the Sugarloaf Fault.|16-MAY-23
15253|Pinecliff Formation|Lithology|The formation consists of chert and silicified mudstone, with less common volcanics, arenite, and conglomerate.  The lower part consists of green and grey chert, quartzite, and minor altered bluish conglomerate and shale.  These sediments are overlain by about 150 m of basaltic flows and agglomerate. The volcanic flows are spilitic in composition and exhibit well-formed pillow structures.  Agglomerate occurs at the base and the top of these volcanics.  The basal agglomerate consists of clasts of porphyritic andesite in an andesitic groundmass whereas the top agglomerate consists of fragments of pink fluidal rhyolite in a tuffaceous andesitic groundmass.  Chert, conglomerate, and minor coarse feldspathic arenite overlie the volcanics.  The chert immediately above the volcanics is greenish and well banded, but becomes more massive higher in the sequence.  Conglomerate is present as small, discrete lenticular bodies.|16-MAY-23
15253|Pinecliff Formation|Depositional environment|Pillow structures in the volcanic interbeds, together with the association of coarse-grained feldspathic arenite and chert, suggest marine deposition in an unstable shelf environment. O¿Shea (1975) located a 4cm band of crinoid fossils in a mudstone bed at AMG 424700 6981500.  Rose (1986) located a dark banded lithic arenite containing fossiliferous carbonaceous material at AMG 424530 6981780.  This material was a thin stem-like material lying parallel to the bedding plane and was estimated to make up to 15% of the rock in thin section.PROVENANCE::  The unit appears to have been derived from a marine source due to the presence of spilitic volcanics.  No geochemistry has been undertaken on the unit to determine its tectonic affinities.|16-MAY-23
15253|Pinecliff Formation|Relationships and boundaries|The unit is conformably overlain by the Hampton Road Rhyolite and faulted against younger formations within the group in the north.  The unit is faulted against the Sugarloaf Metamorphics along the Sugarloaf Fault, and intruded by units of the Eskdale Granodiorite to the west.  The Woogaroo Sub-Group unconformably overlies the formation to the south-west.|16-MAY-23
15253|Pinecliff Formation|Age reasons|In the absence of definitive fossils in the unit, the age of the unit is tentatively equated with that of the overlying Biarraville Formation, which has well developed mid-Permian fossils, however if the unit is on stratigraphic correlation grounds the unit may be older (?Early Pemian).|16-MAY-23
15253|Pinecliff Formation|Correlations|The unit may be a correlative of Early Permian altered basic volcanics mapped to the east in the Cambroon and Northbrook Subprovinces.  It may also be a correlative of some parts of the Highbury Volcanics of the Gympie Province in the Gympie area.|16-MAY-23
15253|Pinecliff Formation|Comments|GEOPHYSICAL EXPRESSION::  The unit has a non-distinctive mauve and light grey response on the K-Th-U ternary radiometric image.  The signature can not be distinguished from rocks of the Sugarloaf Metamorphics to the north and west.  The unit has an underlying high magnetic signature.STRUCTURE::  The Pinecliff Formation is folded in a broad east-south-east plunging anticline, which is defined by outcrops of the Kipper Creek Andesite Member (Campbell, 1952).  Dips range from about 400 to 800.  South of the Sugarloaf Fault and north of the Esk - Hampton Road, the unit is affected by faulting and dips between 700 to the south-south-east and vertical.  To the west the Eskdale Granodiorite intrudes the lower part of the formation.  Rose (1986) identified mylonites developed at the contact with Sugarloaf Metamorphics along the Sugarloaf Fault, south-west of Cressbrook Creek.|16-MAY-23
15253|Pinecliff Formation|References|CAMPBELL, K.S.W.,1952,The geology of the Cressbrook-Buaraba area,"University of Queensland.  Department of Geology Papers (New series), Regional Geology.**CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.,1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional Geology.**O'SHEA, P.D.,1975,The geology of the 'sugarloaf' - West Kipper Creek area, southern Queensland, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.**ROSE, P.,1986,The Geology of the Sugarloaf Fault - Cressbrook Creek Contact, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.|16-MAY-23
24459|Plum Mountain Gneiss|Name source|Named after Plum Mountain, GR 750239, Duchess 1:100 000 Sheet area.|16-MAY-23
24459|Plum Mountain Gneiss|Unit history|Previously mapped as Kalkadoon Granite with metamorphic remnants (Carter & Opik, 1963).|16-MAY-23
24459|Plum Mountain Gneiss|Type section locality|Low hills and ridges and undulating terrain on S side of track from Stanbroke homestead east to Twin Tank, from GR 692140 to GR 755130, Dajarra 1:100 000 Sheet area, Duchess 1:250 000 Sheet area. The characteristic rock types of the unit, massive to banded quartzofeldspathic gneiss and augen gneiss, together with irregular bodies of weakly to strongly foliated granite, are well exposed, though somewhat weathered in this area.|16-MAY-23
24459|Plum Mountain Gneiss|Extent|The unit crops out in a band up to 9 km wide extending NNE from SE part of Dajarra 1:100 000 Sheet area into S central part of Duchess 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24459|Plum Mountain Gneiss|Thickness range|Unknown, but probably several thousand metres.|16-MAY-23
24459|Plum Mountain Gneiss|Lithology|The unit consists mainly of massive to banded leucocratic to mafic quartzo-feldspathic gneiss and augen gneiss, but also includes micaceous, arkosic and quartzitic meta-arenites, mica schist, calc-silicate gneiss, amphibolite, metabasalt, and numerous irregular bodies of weakly to strongly foliated granite.|16-MAY-23
24459|Plum Mountain Gneiss|Relationships and boundaries|Plum Mountain Gneiss is intruded by One Tree, Birds Well? And Saint Mungo Granites and by basic dykes. It has concordant contacts with metasediments mapped as Corella Formation to the east (e.g. 2 km NW of the Saint Mungo copper mine) and is overlain unconformably by flat-lying Cambrian sediments in the south.|16-MAY-23
24459|Plum Mountain Gneiss|Age reasons|Probably older than 1870-1880 m.y. old Leichhardt Volcanics, which overlie One Tree Granite.|16-MAY-23
24459|Plum Mountain Gneiss|Comments|Plum Mountain Gneiss is a complex metamorphic unit forming a readily mappable coherent unit bounded by faults, granites, and Corella Formation. It is probably a correlative of some similar gneissic rocks mapped as undivided Tewinga Group further west in the Duchess 1:250 000 Sheet area.|16-MAY-23
24459|Plum Mountain Gneiss|References|R233; 98/29253|16-MAY-23
24459|Plum Mountain Gneiss|Proposer|Donchak P.J.T., Blake D.H.|16-MAY-23
23914|Poley Cow Formation|Name source|Poley Cow Creek, which joins the Broken River at 7859 754445.  The grid reference is based on the AGD66 datum.|16-MAY-23
23914|Poley Cow Formation|Unit history|The unit was previously mapped as part of the Graveyard Creek Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
23914|Poley Cow Formation|Geomorphic expression|The unit generally forms relatively subdued topography, except in areas recently exhumed from beneath Tertiary cover.  Some of the conglomerates form slightly more elevated topography, and locally outline trends.|16-MAY-23
23914|Poley Cow Formation|Type section locality|Broken River between 7859 662442 (base) and 660453 (top).  About 550 m of lithic to lithofeldspathic arenite, polymictic conglomerate, and mudstone are exposed.  See Withnall & others (1988, figure 27 and page 43) for more details.|16-MAY-23
23914|Poley Cow Formation|Extent|A belt about 5 km wide and 20 km long, trending southwest from the large laterite plateau in central BURGES to Dosey Creek, and folded with Judea, Jack, and Shield Creek Formations.|16-MAY-23
23914|Poley Cow Formation|Thickness range|550 m in the type section, wedging out to the south in the Dosey Creek area, and also to the north in the area east of Jessey Springs.|16-MAY-23
23914|Poley Cow Formation|Lithology|Lithic to lithofeldspathic arenite, polymictic conglomerate, and mudstone with rare limestone.  Arenites are thin to very thick-bedded and have erosive bases, rip up clasts, horizontal stratification, ripple cross laminae, soft sediment deformation, and rare hummocky cross stratification. Trace fossils are locally abundant.  A muddy storm-dominated shelf environment is likely.|16-MAY-23
23914|Poley Cow Formation|Fossils|The fauna consists of graptolites and rare brachiopods, trilobites, and conodonts, indicating an Early Silurian (Llandovery) age for the lower part, possibly extending to Ludlow towards the top.  See Withnall & others (1988) for more details.|16-MAY-23
23914|Poley Cow Formation|Relationships and boundaries|The unit is part of the Graveyard Creek Group, and unconformably overlies the Judea Formation, and in places the Netherwood Tonalite. Arenites are more lithic than those in the Judea Formation, and conglomerates are common.  It is conformably (or disconformably?) overlain by the Jack Formation, which contains large limestone lenses in the type section and adjacent area. Arenites in the Jack Formation are generally very micaceous, and discontinuous lenses of quartzose arenite at its base mark the boundary where the limestones are absent.  The Poley Cow Formation is faulted against the Clarke River Group along the Poley Cow Fault.|16-MAY-23
23914|Poley Cow Formation|Age reasons|Fossil fauna indicates an Early Silurian (Llandovery) age for the lower part, possibly extending to Ludlow towards the top.  See Withnall & others (1988) for more details.|16-MAY-23
23914|Poley Cow Formation|References|WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4. Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. **WHITE, D.A., 1962:  Clarke River 1.250 000 Geological series.  Bureau of Mineral Resources, Australia, Explanatory Notes, E/55-13.  **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J..A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.J., 1988:  tratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
15400|Police Creek Siltstone Member|Name source|Police Creek, a tributary of the Leichhardt River, 45 km north-northeast of Mount Isa, latitude 20o25'S, longitude 139o40'E on the Cloncurry 1:250 000 Sheet area.|16-MAY-23
15400|Police Creek Siltstone Member|Type section locality|300 m of mottled, purple-grey phyllite and siltstone and thin-bedded waterlain rhyolitic tuff 27 km south of Julius dam, and 48 km north-northeast of Mount Isa. It extends approximately 750 m north from GR 653454 on the Prospector 1:100 000 Sheet area, near latitude 20o23'10"S, longitude 139o42'30"E.|16-MAY-23
15400|Police Creek Siltstone Member|Extent|The member is a thin, discontinuous unit at the top of the Lochness Formation, and exteands from the Police Creek area 90 km northwards to near Dynamite Creek.|16-MAY-23
15400|Police Creek Siltstone Member|Thickness range|0 to 400 m|16-MAY-23
15400|Police Creek Siltstone Member|Lithology|Massive earthy siltstone and phyllite, with blotchy pale purple to grey coloration; minor fine-grained sandstone and green-grey rhyolitic tuff.|16-MAY-23
15400|Police Creek Siltstone Member|Relationships and boundaries|The member forms a lenticular unit with discontinuous distribution at the top of the Lochness Formation. The lack of bedding and mottled, earthy appearance of much of the member suggests it may have been weathered before burial and that the contact with the overlying Surprise Creek Beds may be a disconformity. The presence of rhyolitic tuff indicates some degree of crustal disturbance at this time also.|16-MAY-23
15400|Police Creek Siltstone Member|Age reasons|Carpentarian; minimum age about 1650 m.y. set by Sybella Granite intrusive into approximate time equivalents west of Mount Isa.|16-MAY-23
15400|Police Creek Siltstone Member|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
30137|Ponto Basalt Member|Name source|The name is derived from Ponto hut and yards in the middle of the outcrop area at 8159-244870.  The grid reference is based on the AGD66 datum.|16-MAY-23
30137|Ponto Basalt Member|Geomorphic expression|The Ponto Basalt Member forms predominantly subdued areas with substantial dark soil cover. Vegetation consists of good grass cover and scattered narrow-leaf ironbarks.|16-MAY-23
30137|Ponto Basalt Member|Type section locality|The type section is between 8159-197786 and 182787 along a vehicle track that heads west off the Taravale-Star track some 10km north of Ponto Hut. The section is up the side of a ridge, climbing some 200m in elevation, and the total thickness exposed is approximately 1000 m.|16-MAY-23
30137|Ponto Basalt Member|Description at type locality|At the base of the section, dark grey, slightly porphyritic, moderately amygdaloidal andesite about 200m thick, is faulted to the east against the Devonian to Carboniferous Keelbottom Group. This andesite is overlain by about 150m of dark grey, crystal-poor, lithic-rich, andesitic lapilli breccia and this is overlain by about 150m of andesitic breccia. The uppermost, approximately 500m of the section is massive, dark grey, moderately porphyritic, basaltic andesite.|16-MAY-23
30137|Ponto Basalt Member|Extent|The Ponto Basalt Member crops out between the Little Star River and Star River on the limbs of the syncline, and south of Little Star River in the anticline. The total area is about 50km2.|16-MAY-23
30137|Ponto Basalt Member|Thickness range|On the western limb of the syncline between Little Star River and Star River, the Ponto Basalt Member is 1000m thick.|16-MAY-23
30137|Ponto Basalt Member|Lithology|The Ponto Basalt Member comprises dark grey, slightly to moderately porphyritic basalt to andesite, andesitic breccia, amygdaloidal basalt and basaltic andesite, andesitic lapilli breccia and aphyric basalt to andesite.|16-MAY-23
30137|Ponto Basalt Member|Relationships and boundaries|The Ponto Basalt Member is part of the Tareela Volcanics. In its outcrop area, is probably the lowermost part of the sequence. It is faulted against the Devonian to Early Carboniferous Keelbottom Group. As for the rest of the Tareela Volcanics, it is probably Early Carboniferous|16-MAY-23
30137|Ponto Basalt Member|Age reasons|..........probably Early Carboniferous (see Relationships, etc....)|16-MAY-23
83550|Porcupine Gorge Formation|Name source|A previously unrecognised stratigraphic unit discovered in this study is here defined as the Porcupine Gorge Formation. The name for the unit is derived from the Porcupine Gorge in which the unit was discovered, and in which the type section is described.|16-MAY-23
83550|Porcupine Gorge Formation|Unit history|The Porcupine Gorge Formation replaces 18 m of strata that had been previously assigned to the
overlying Warang Sandstone. However, the distinct lithology of this unit, coupled with the erosional
unconformity above and the distinct difference in mean paleocurrent vectors (southwest for Porcupine Gorge Formation, south for Warang Sandstone), is sufficient to determine it as a separate
lithostratigraphic unit.|16-MAY-23
83550|Porcupine Gorge Formation|Type section locality|The type locality is defined as an 18.4 m thick interval of sedimentary rock, accessible on the eastern
cliff-face ~1.8 km north of the base of the Pyramid Trail, itself 300 m north of the Pyramid, in Porcupine Gorge National Park, ~63 km northeast of the town of Hughenden in northern Queensland, Australia (WGS84 20deg20'6.91"S 144deg28'8.48"E). An additional 18.2 m thick interval of the Porcupine Gorge Formation was observed in the GSQ Hughenden 6 stratigraphic drill core (~184.6?202.8 m), which is housed in the Department of Minerals and Energy Exploration Data Centre in Zillmere, Brisbane, Queensland.
|16-MAY-23
83550|Porcupine Gorge Formation|Extent|The Porcupine Gorge Formation is confined in its extent to Porcupine Gorge and to the GSQ Hughenden 6 stratigraphic drill core, located ~1.2 km west of the gorge. The Warang Sandstone is poorly preserved in GSQ Hughenden 5 and so it is not possible to ascertain whether the Porcupine Gorge Formation extends to this bore location.|16-MAY-23
83550|Porcupine Gorge Formation|Lithology|The 18.4 m thick formation consists of four main lithologies. The basal 2.9 m (15.8% of the formation) contains a yellow to red, poorly to moderately sorted, polymictic pebble conglomerate, with subrounded to rounded clasts. Clast types are dominated by quartz and rhyolite with lesser
intraformational mudstones and cherts. Above the conglomerate is a 2.2 m covered interval where
lithology is indeterminable. This is followed by a 3.8 m thick very pale yellow quartzose, cross-bedded sandstone (20.7% of the formation). The sandstone fines upwards from medium- to fine-grained, is typically subangular to subrounded and moderately to well sorted. Overlying this unit is 2.2 m of localised bluish grey carbonaceous siltstone interbedded with minor claystones and fine-grained sandstone (12.0%). The siltstone is typically thinly laminated but may also contain small ripple cross-stratification. Carbonaceous leaf and wood fragments are common within the laminations, with less abundant conchostracan and Planolites trace fossils occurring. Capping the formation is a distinctive, 6.7 m thick, mottled paleosol succession, with minor interbedded fine-grained sandstones and numerous slickensides (40%). A very thin sandstone (<10 cm) is interbedded with the paleosol at the very top.|16-MAY-23
83550|Porcupine Gorge Formation|Relationships and boundaries|In the type section in Porcupine Gorge, the Porcupine Gorge Formation overlies the medium-to very
coarse-grained sandstones of the Betts Creek beds at a disconformable surface. The white, medium-grained, cross-bedded sandstone Warang Sandstone then overlies the paleosol of the Porcupine Gorge Formation at a paraconformity. These same relationships are observed in the GSQ Hughenden 6 drill core.|16-MAY-23
83550|Porcupine Gorge Formation|Identifying features|The distinct lithology of this unit, coupled with the erosional unconformity above and the distinct difference in mean paleocurrent vectors (southwest for Porcupine Gorge Formation, south for Warang Sandstone), is sufficient to determine it as a separate lithostratigraphic unit.|16-MAY-23
83550|Porcupine Gorge Formation|Age reasons|Using U-Pb detrital zircon geochronology through LA-ICP-MS, a robust maximum depositional age of the Porcupine Gorge Formation was determined at 238.7 +/- 3 Ma from the core. A second age was calculated from outcrop at 229.4 +/- 3.6 Ma from outcrop and is considered to have been taken higher in the unit (see main text for discussion). This indicates that deposition of the Porcupine Gorge Formation occurred from the Ladinian until at least the late Carnian. Palynology conducted on the mudstone unit returned an Anisian to Carnian age for the unit, which is consistent with the detrital zircon ages. Further, based on this age, this unit cannot be either the Rewan or Clematis group, which overlie the Betts Creek beds in more southerly exposures of the Galilee Basin.|16-MAY-23
83550|Porcupine Gorge Formation|Defn author|Todd et al. (2022).|16-MAY-23
27682|Prestwood Microgranite|Geomorphic expression|Topography: Generally forms steep-sided, elevated, very rocky areas with a cover of brown grasses (mainly "speargrass") and scattered bushes. Large boulders and tors are common, especially in the type area.|16-MAY-23
27682|Prestwood Microgranite|Type section locality|Along a track which runs between the Georgetown-Croydon highway and the Gilbert River, in an area known as "The Pillars", between GR 7561-403757 and -391734.|16-MAY-23
27682|Prestwood Microgranite|Extent|The Prestwood Microgranite crops out as a composite ring-dyke in the area between the Cumberland Mine and Riverview Homestead, on Forest Home 1:100 000 Sheet area. A central, irregularly shaped ring-like intrusion has its northern, eastern, southern and western extremities at GR 7561-395759, -460705, 415687 and 0337777. There are small "outliers" at -366757 and -337765, and dykes at -441752and -4507055. An outer arcuate dyke crops out through Quaternary cover in the Riverview area (GR 7561-307770) and thence south and southeast to -320633, where it narrows and becomes finer-grained (rhyolitic), and thence east to -351617 where it splays into a number of small rhyolite dykes. A small but prominent "outlier" on the northern side of the Gilbert River, opposite Riverview has also been mapped as part of this dyke.|16-MAY-23
27682|Prestwood Microgranite|Lithology|Pink or grey generally strongly porphyritic biotite microgranite, with large phenocrysts of quartz, orthoclase or sanidine, sodic plagioclase and small phenocrysts of chloritized biotite in a fine-grained mosaic of quartz, alkali feldspar, plagioclase, and other (minor) phases. The feldspars are generally partly to heavily sericitised.|16-MAY-23
27682|Prestwood Microgranite|Relationships and boundaries|Intrudes Robertson River, Townley, and Heliman Formations, Forsayth Granite, and Aurora Granite and probably Mount Darcy Microgranodiorite. Does not appear to have undergone significant metamorphism or structural disturbance. |16-MAY-23
27682|Prestwood Microgranite|Identifying features|Original definition: The term "Prestwood Microgranite" was first used by White (1959), who gave as its type locality an area "one mile [1.6 km] northeast of Prestwood Homestead on the northern side of the Georgetown-Croydon highway".  The problem: We have inspected and sampled a location 800 m north of the highway and 500 m east of Crooked Creek (GR 7561-364783) corresponding to White's (1959) type area, and found there a grey porphyritic microgranodiorite containing phenocrysts of quartz, plagioclase, hornblende, and biotite. White's description of the lithology of the Prestwood Microgranite is "light grey porphyritic microgranite with phenocrysts of quartz, orthoclase and biotite". His distribution corresponds with ours, but includes the Mount Sircom Microgranodiorite. Branch (1966) described the Prestwood Microgranite as a pink porphyritic biotite adamellite, stressing that biotite was the sole ferromagnesian mineral, and mentioned a locality 5 km southeast of Prestwood Homestead. We have confirmed that the porphyritic intrusive rocks south and southeast of Prestwood homestead are biotite microgranite (or "microadamellite", an obsolete term), but many other porphyritic intrusive bodies assigned by White (1959) and Branch (1966) to the Prestwood Microgranite belong to other units (Mount Darcy Microgranodiorite or Mount Sircom Microgranodiorite.|16-MAY-23
27682|Prestwood Microgranite|Age reasons|Probably Carboniferous; probably a late-stage intrusive related to the Cumberland Range Volcanics (Branch, 1966) which are closely similar to the mid-Carboniferous Newcastle Range Volcanics (Black, 1973).|16-MAY-23
27682|Prestwood Microgranite|Comments|Both original authors of the name "Prestwood Microgranite", D A White and C D Branch, have been contacted and have agreed to our proposal that the type area be changed.|16-MAY-23
27682|Prestwood Microgranite|References|73/050; B076; 98/29525|16-MAY-23
24464|Puppy Camp Granodiorite|Name source|Pummp Camp Creek, which joins Telegraph Creek at GR 931732 (Mount Surprise 1:100 000 Sheet area).|16-MAY-23
24464|Puppy Camp Granodiorite|Unit history|Previously mapped as Forsayth Granite (White, 1962).|16-MAY-23
24464|Puppy Camp Granodiorite|Type section locality|In Telegraph Creek and its tributaries from the railway bridge at GR 980693 downstream to GR 964700 (Mount Surprise 1:100 000 Sheet area), where whitish-grey medium-grained equigranular to slightly porphyritic biotite granodiorite crops out.|16-MAY-23
24464|Puppy Camp Granodiorite|Extent|The Puppy Camp Granodiorite crops out in the southwestern part of the Mount Surprise 1:100 000 Sheet area as an oblong-shaped pluton with a northeasterly trending axis. It is exposed over an area of about 150 km2.|16-MAY-23
24464|Puppy Camp Granodiorite|Lithology|Whitish-grey, massive medium-grained, equigranular to slightly porphyritic muscovite-biotite and biotite granodiorite with sparse white K-feldspar megacrysts which are generally 2 to 4 cm long and rarely up to 8 cm. Biotite 'clots', generally 1 to 3 cm long, are present locally. Pinkish-white muscovite leucogranite veins are common throughout the granodiorite. Muscovite-biotite granodiorite crops out mainly in the southwestern half of the batholith.|16-MAY-23
24464|Puppy Camp Granodiorite|Relationships and boundaries|The unit intrudes the Proterozoic Einasleigh Metamorphics and small unassigned leucogranite bodies. It is overlain by the Carboniferous Newcastle Range Volcanics and locally intruded by large Palaeozoic microgranite dykes. It is overlain by Cainozoic basalt.|16-MAY-23
24464|Puppy Camp Granodiorite|Age reasons|Probably Silurian to Devonian; the unit has a massive unfoliated character and is petrographically similar to the White Springs Granodiorite (Withnall & others, 1976), which is now known to be of Siluro-Devonian age (Black & Holmes, in preparation).|16-MAY-23
24464|Puppy Camp Granodiorite|References|? R200; 01/31335; 79/04763|16-MAY-23
24464|Puppy Camp Granodiorite|Proposer|Warnick J.V.|16-MAY-23
25420|Purkin Granite|Name source|Parish of Purkin, County of Percy.|16-MAY-23
25420|Purkin Granite|Unit history|White (1962) mapped the rocks as unassigned late Palaeozoic granite. Branch (1966 p.99) equated them with the Elizabeth Creek Granite which they resemble. Smart (1973) used the name Purkin Igneous Complex for the outer part of the stock, the core being interpreted as Dumbano Ganite. He did not define the unit, however. Our mapping has shown the "complex" to be relatively uniform and that the stock and batholith are not significantly different in character. Therefore the name is changed to Purkin Granite and applied to the rocks of both the batholith and stock.|16-MAY-23
25420|Purkin Granite|Type section locality|Between GR 137481 and 138451 in Goat Gorge, formed where the Gilbert River cuts through the granite in the batholith. Grey to pink, medium grained, equigranular biotite granite, and some porphyritic and coarse grained varieties locally cut by aplite veins, crop out in the gorge.|16-MAY-23
25420|Purkin Granite|Extent|Crops out in a batholith and a large stock along the northern edge of the Gilberton Plateau. The batholith is irregular in outline and has an area of 300 km2. The stock, which is roughly circular in Outline, 10 to 12 km in diameter and about 100 km2 in area, occurs to the west of the batholith, south of the old Gorge Creek Outstation, and centred at about GR 890 420 (Gilberton 1:100 000 Sheet area).|16-MAY-23
25420|Purkin Granite|Lithology|As for the type area; porphyritic varieties are mainly restricted to the batholith where some grey to dark grey and very coarse grained varieties are also present.|16-MAY-23
25420|Purkin Granite|Relationships and boundaries|Intrudes the Proterozoic Einasleigh Metamorphics and various leucogranite phases associated with them. Partly overlain by Mesozoic sediments of the Eulo Queen Group and Gilbert River Formation.|16-MAY-23
25420|Purkin Granite|Age reasons|Carboniferous; Richards & others (1966) obtained a K-Ar biotite age of 350 m.y. on a sample of the granite.|16-MAY-23
25420|Purkin Granite|References|B076; 98/29234; 02/32158; 02/32159|16-MAY-23
23929|Quadroy Conglomerate|Name source|The unit forms a discontinuous belt along the western margin of the Hodgkinson Province.  Early workers in the region mapped the rocks as part of either the Proterozoic(?) Dargalong Metamorphics or the Silurian-Devonian Chillagoe Formation (Amos & de Keyser, 1964;  de Keyser & Lucas, 1968).  Subsequently, Fawckner (1981), who carried out the first detailed mapping of the western part of the Hodgkinson Province between the Palmer and Mitchell Rivers, delineated the distinctive arkosic/conglomeratic sequence as the Quadroy Conglomerate, of probable Late Devonian age.|16-MAY-23
23929|Quadroy Conglomerate|Geomorphic expression|The unit mainly forms low undulating country characterised by pale to medium tones on aerial photographs.|16-MAY-23
23929|Quadroy Conglomerate|Type section locality|The designated type section is along Quadroy Creek, about 10 km south-southeast of Palmerville homestead (Fawckner, 1981).  The formation attains its maximum thickness of 700 m in this area (Fawckner, 1981).|16-MAY-23
23929|Quadroy Conglomerate|Extent|The formation crops out as a narrow, north-trending belt east of the Palmerville Fault.  The belt has an average width of 150 m, with a maximum width of about 700 m.  It extends discontinuously adjacent to the Palmerville Fault for ~150 km, from northwest of Chillagoe almost to the Palmer River.|16-MAY-23
23929|Quadroy Conglomerate|Thickness range|The thickness of the formation ranges from <100 m west-southwest of Mungana to ~700 m in the Quadroy Creek area.|16-MAY-23
23929|Quadroy Conglomerate|Lithology|The formation consists mainly of clast-supported, poorly sorted, cobble and boulder conglomerate and interbedded arkose and conglomeratic arkose.  Some breccia and matrix-supported conglomerate are present locally.  Outcrops are mainly massive with little or no obvious internal stratification.  Fawckner (1981) reported possible west-younging cross beds at one locality south of Quadroy Creek.  The arkosic sediments are generally extensively weathered.   Clasts consist predominantly of foliated, medium-grained to pegmatitic, porphyritic muscovite-biotite granite (sensu lato), together with subordinate quartz mylonite, amphibolite, schist, quartzofeldspathic gneiss, quartzite, quartz, and rare quartzose arenite and limestone.  Clast size coarsens noticeably towards the west (towards the postulated top of the formation) in the far north.   The characteristic rock type south and north of the Mitchell River is pink to pale brown, massive, medium-grained arkose.  The arkose consists mainly of quartz, K-feldspar, muscovite and biotite.  Scattered rounded clasts of foliated muscovite-biotite granite and granitic gneiss occur locally within the arkose, together with rare, more angular fragments of schist, amphibolite, and quartz mylonite.  The arkose is well exposed in the bed of the Mitchell River at Boomers Crossing (GR 1905 81745).   Lenses of clast-supported conglomerate containing granite clasts up to coarse boulder size are very common north of Mount Mulgrave.  The boulders of foliated granite commonly protrude (like tors) above the ground surface which is littered with coarse quartz and feldspar grains.  Exposures superficially resemble those typically found in granitic terrains but the granitic debris between the boulders actually represents extensively disaggregated arkosic matrix.  The size and abundance of the clasts generally decreases to the east where the conglomeratic character of the deposit is more obvious.   In the Quadroy Creek area, the arkosic sediments are white, grey or pink, mainly coarse grained, and massive.  They resemble the porphyritic muscovite-biotite granite forming the dominant clast type in most outcrops.  The arkoses contain scattered pink K-feldspar grains up to 3 cm long and smaller quartz grains and muscovite and biotite flakes.  Rare, poorly developed cross beds are present locally.  The sediments are commonly difficult to distinguish from weathered granite, especially in poorly exposed outcrops.  The sequence shows secondary iron oxide staining in a few places.   The sequence locally contains lenses of extensively ferruginised dark red-brown breccia (at GR 1898 82190 and GR 1892 82171) consisting mainly of angular to subrounded clasts up to about 30cm across (generally <10cm) of dark grey, fine-grained quartzite (commonly foliated), phyllite (only observed at GR 1898 2190), quartz, amphibolite (very common at GR 1892 82171), together with minor banded migmatite gneiss, mylonite, and muscovite-rich granite............|16-MAY-23
23929|Quadroy Conglomerate|Depositional environment|The immaturity of the arkoses and the large size of the granite clasts within the conglomerates indicate a proximal, high-relief source made up mainly of granitic rocks and, to a lesser degree, gneissic and schistose metamorphic rocks.  These clasts were derived from a terrain similar to that exposed west of the Palmerville Fault.  The sequence was probably deposited adjacent to an active fault scarp (Fawckner, 1981).  The common occurrence of angular mylonite fragments, apparently identical to mylonites in and adjacent to the Palmerville Fault zone, supports this interpretation.  The massive, immature character, both texturally and compositionally, of the sediments, the almost complete lack of sedimentary structures including bedding, and the coarse character of the sediments implies extremely rapid deposition under high energy conditions, probably in a proximal fan environment.  Furthermore, a non-marine or marginal-marine environment is suggested by the characteristic red-brown or brick-red colour of many of the metamorphic fragments.  Deposition took place subaqueously, at least in part, as indicated by poorly developed cross beds and grading locally (Fawckner, 1981). The occurrence of amphibolite and other high-grade metamorphic detritus in the conglomeratic sediments implies that deep erosion of the terrain to the west had already taken place prior to the deposition of the Quadroy Conglomerate.|16-MAY-23
23929|Quadroy Conglomerate|Fossils|The formation contains clasts of fossiliferous limestone, one of which has yielded Early Devonian conodonts (B.G. Fordham, personal communication, 1988), ~12 km northwest of Chillagoe (at GR 2271 81024).|16-MAY-23
23929|Quadroy Conglomerate|Structure and Metamorphism|Where bedding is discernible moderately steep to steep easterly dips are the most common.  The few younging directions determined are all to the west.  A weak foliation is commonly developed, but adjacent to the Palmerville Fault the sequence is strongly foliated and locally brecciated.  According to Fawckner (1981) the Palmerville Fault in Quadroy Creek is marked by a zone 1-2 m wide of intensely deformed and locally brecciated, chlorite?-rich mylonite.  The transition is abrupt with a marked colour contrast between the pink conglomerate and the grey or greyish green mylonitic rocks.  Fawckner (1981) also reported a lens (30 m x 10 m) of relatively undeformed conglomerate enveloped by greyish green mylonite/breccia at one locality in Quadroy Creek.  The faulted western contact appears to be sub-vertical in most places.|16-MAY-23
23929|Quadroy Conglomerate|Age reasons|The age of the formation is uncertain.  The formation contains clasts of fossiliferous limestone, one of which has yielded Early Devonian conodonts (B.G. Fordham, personal communication, 1988), ~12 km northwest of Chillagoe (at GR 2271 81024).  Furthermore, the basal part of the Quadroy Conglomerate in the south locally (at GR 2269 81025) contains numerous clasts of quartzose arenite identical to that in the adjacent Mulgrave Formation.  These factors combined with the interpretation of the formation as a thrust-nose or fault-scarp deposit generated during the first major deformational event (regional D1 - cover) to affect the entire province (Fawckner, 1981) imply that the formation is most probably Late Devonian or Early Carboniferous.|16-MAY-23
23929|Quadroy Conglomerate|Comments|Fawckner (1981) and Shaw & others (1987) interpreted the Quadroy Conglomerate as a synorogenic deposit eroded from the nose of an advancing thrust sheet that developed during the first major deformation (D1 - cover) to affect the western Hodgkinson Province.  We interpret the lack of a well-developed foliation in the formation away from the bounding faults (particularly the Palmerville Fault) to indicate that the sequence was most probably deposited during the waning stages of the D1 (cover) deformation.|16-MAY-23
23929|Quadroy Conglomerate|References|AMOS, B.J., & DE KEYSER, F., 1965:  Mossman, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes, SE/55-1. **DE KEYSER, F., & LUCAS, K.G., 1968:  Geology of the Hodgkinson and Laura Basins, north Queensland.  Bureau of Mineral Resources, Australia, Bulletin 84. **FAWCKNER, J.F., 1981:  Structural and stratigraphic relations and a tectonic interpretation of the western Hodgkinson Province, northeastern Australia.  Ph.D. Thesis, James Cook University of North Queensland, Townsville (unpublished). **SHAW, R.D., FAWCKNER, J.F., & BULTITUDE, R.J., 1987:  The Palmerville fault system:  A major imbricate thrust system in the Northern Tasmanides, North Queensland.  Australian Journal of Earth Sciences, 34, 69-93.|16-MAY-23
29321|Quaker Granite|Name source|The unit is named after Quaker Creek which drains the northern part of the adamellite.|16-MAY-23
29321|Quaker Granite|Unit history|Previously mapped as Elizabeth Creek Granite (Best, 1962;  de Keyser & Wolff, 1964).|16-MAY-23
29321|Quaker Granite|Type section locality|The proposed type locality is at GR 2407 80916 on the eastern side of Quaker Creek.  The locality is ~11 km south-southeast of Chillagoe and on the southern side of a station track extending west from Quaker Bore.|16-MAY-23
29321|Quaker Granite|Description at type locality|The adamellite forms undulating and dissected hilly country with numerous scattered boulders, bouldery outcrops and rock pavements.  It is characterised by medium tones on aerial photographs.|16-MAY-23
29321|Quaker Granite|Extent|The Quaker Granite forms an ovoid, northerly trending pluton of ~40 km2, about 15 km south-southeast of Chillagoe.|16-MAY-23
29321|Quaker Granite|General description|STRUCTURE AND METAMORPHISM:: The Quaker Granite forms a massive, discordant pluton.  Despite its massive appearance the adamellite displays petrographic evidence of slight to moderate deformation.  Most quartz phenocrysts are characterised by undulose extinction, and many of the larger biotite flakes also locally show undulose extinction|16-MAY-23
29321|Quaker Granite|Lithology|The unit consists mainly of pale grey, fine-grained, slightly to moderately porphyritic (hornblende ) biotite adamellite.  Plagioclase is the most abundant phenocryst - as euhedral to subhedral grains up to 2 cm long.  Oscillatory zoning is common in the plagioclase phenocrysts, some of which have narrow rims of normally zoned albite(?).  Small inclusions of quartz, hornblende and biotite occur in the phenocrysts.  Quartz forms rounded phenocrysts, 1-5 mm across.The fine-grained groundmass consists mainly of quartz, plagioclase, and K-feldspar.  Biotite is the dominant mafic mineral and has two modes of occurrence:  1) as scattered well-formed, relatively large (0.5 - 1.5 mm) discrete flakes and, 2) as aggregates up to ~1 cm across, of relatively small flakes.  Some of the larger clots also contain traces of hornblende.Hornblende is scarce and is absent from some specimens.  It has been extensively replaced by biotite and, less commonly, by actinolite.  Zircon, opaque oxide, and allanite are the most common accessory minerals.  Most samples show slight to moderate alteration; sericite, chlorite, epidote/clinozoisite, sphene, muscovite, and calcite are the most abundant and widespread secondary minerals.The adamellite contains scattered rounded mafic enclaves up to ~75 cm across|16-MAY-23
29321|Quaker Granite|Relationships and boundaries|The unit intrudes the Chillagoe Formation and Ootann Granite, and probably also the Muldiva Quartz Monzodiorite (with which it locally forms net-veined complexes).  It is cut by the Carrs Granite.  The adamellite appears to be truncated by the Palmerville Fault.|16-MAY-23
29321|Quaker Granite|Age reasons|The adamellite has not been isotopically dated.  It is most probably Late Carboniferous and about the same age (~300 Ma) as the other granites of the Ootann Supersuite.|16-MAY-23
29321|Quaker Granite|Comments|The Quaker Granite is a member of the Ootann Supersuite of Champion (1991).|16-MAY-23
29321|Quaker Granite|References|BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.DE KEYSER, F., & WOLFF, K.W., 1964:  The geology and mineral resources of the Chillagoe area.  Bureau of Mineral Resources, Australia, Bulletin 70.CHAMPION, D.C., 1991:  Petrogenesis of the felsic granitoids of far north Queensland.  Ph.D. Thesis, Australian National University, Canberra (unpublished).|16-MAY-23
15764|Quilalar Formation|Name source|Parish of Quilalar, which surrounds Kajabbi Township, near 20o2'S latitude, 140o00'E longitude, 6857-953845*. The Quilalar Fault truncates the Quilalar Formation near 20o11'S latitude, 139o00'E longitude, 6857-710677.|16-MAY-23
15764|Quilalar Formation|Geomorphic expression|Quartzite and sandstone in the Quilalar Formation form a distinctive series of about three close-spaced ridges; the silty, dolomitic and ferruginous upper part of the formation is recessive, forming low hills and valleys between the major quartzite units.|16-MAY-23
15764|Quilalar Formation|Type section locality|In Prospector, about 55 km north-northeast to Mount Isa, and 5 km north-northwest of old Glenroy homestead, near the Junction of Conglomerate Creek and the Leichhardt River. The base of the section is at latitude 20o17'25"S, longitude 139o42'00"E (6857-644558); the top of the section is 2.5 km to the northeast, at latitude 20o16'35"S, longitude 139o43'10"E (6857-644573). The type section (holostratotype) exposes, from top to base: 120 m of purple siltstone, friable fine-grained feldspathic sandstone, calcareous siltstone, and laminaated shale (Pqx).  500 m of orthoquartzite and massive medium-grained feldspathic quartzite, with minor siltstone partings - the unnamed orthoquartzite member (Pqx).  335 m of dolomitic siltstone and sandstone, dolomite, stromatolitic dolomite, brown feldspathic sandstone, purple shale and siltstone (Pqx).  360 m of massive brown to white feldspathic and clayey sandstone with pebbly beds and minor siltstone (Pqx). This section is overlain disconformably by pebbly beds of the Fiery Creek Volcanics, and underlain by ferruginous sandstone and siltstone of the Lochness Formation of the Myally Subgroup.  Reference Sections (hypostratotypes) are necessary to illustrate the facies variations within the Quilalar Formation. In Mount Oxide, a reference section is located 3 km west-southwest of Alhambra homestead overlying Myally Subgroup rocks. From the base at 6759-308798, 500 m of feldspathic quartzose and dolomitic sandstone are overlain to the north by at least 300 m of dolomite, dolomitic and ferruginous siltstone and sandstone with halite casts; this dolomitic sequence is capped by 50 m of orthoquartzite, the top of which terminates the reference section at 6759-296819. The basal sandstone contains a 50 m-thick trachybasalt unit, the unnamed volcanic member of the Quilalar Formation; the orthoquartzite at the top of the section is probably equivalent to the unnamed orthoquartzite member in the type section. The second reference section is located 17 km west-southwest of Dobbyn, in Alsace from 6858-807028 (base) northwest for 2 km to 6858-795042. Here, 600 m of feldspathic sandstone with basal arkose disconformably overlie acid volcanics of the Argylla Formation; the sandstone is overlain by 450 m of ferruginous sandstone and siltstone, and dolomitic siltstone with thin interbeds of rhyolitic tuff or ashstone. It is overlain unconformably by pebbly sandstone of the Fiery Creek Volcanics.|16-MAY-23
15764|Quilalar Formation|Extent|In open to moderately tight anticlines and synclines north, west and southwest of Alhambra (MOUNT OXIDE, GREGORY DOWNS); in a tight to isoclinal 2 to 6 km wide synclinal fold belt extending for about 80 km along the western edge of the Ewen Block; and in tight to moderately tight synclines separated by an anticline in a north-trending belt 10 to15 km wide and 60 km long between the Ewen and Kalkadoon-Leichhardt basement blocks (MYALLY, ALSACE, PROSPECTOR). These two latter fold belts are faulted together south of the Ewen Block, and terminate against the Quilalar and Mount Remarkable Faults. Some Quilalar Formation is present in MARY KATHLEEN, where it is shown as Surprise Creek Beds south of the Gorge Creek-Mount Remarkable Fault, mainly 15 to 20 km southeast of Mount Isa. This belt also extends southwards onto DUCHESS.|16-MAY-23
15764|Quilalar Formation|Thickness range|500 to 1500 m; the basal sandstone unit varies from almost zero thickness along the eastern side of the Ewen Block, to 600 m; the dolomitic unit, exclusive of the orthoquartzite member, ranges from 100 to 520 m; the orthoquartzite member varies from 30 m in the northwest to 750 m near Julius Dam, in Prospector.|16-MAY-23
15764|Quilalar Formation|Lithology|The basal part of the formation consists of white, grey or bff, medium to coarse-grained feldspathic quartzite, orthoquartzite, fine-grained feldspathic sandstone, clayey sandstone and minor siltstone, shale, conglomerate and trachybasalt; in areas near the Ewen Block the basal rocks include arkose and grit, pyritic sandstone and minor acid tuff and basalt. The upper part is mainly stromatolitic dolomite, brown dolomitic sandstone and siltstone, ferruginous sandstone and siltstone, purple-grey siltstone, siltstone with fine-grained sandstone lenses, orthoquartzite, shale-clast conglomerate and minor green to grey rhyolitic tuff or ashstone. Calc-silicate rocks occur in Pqx in the aureole of the Weberra Granite in Mount Oxide.|16-MAY-23
15764|Quilalar Formation|Relationships and boundaries|The Quilalar Formation conformably overlies the Lochness Formation of the Myally Subgroup, and undivided Myally Subgroup; Wilson & others (1977) suggest this contact may also be disconformable, since the underlying Lochness Formation is locally a massive, structureless and mottled siltstone, possibly a palaeosol. The Quilalar Formation overlies basement rocks unconformably. In Alsace, Quilalar Formation quartzite with basal arkosic grit and pebble conglomerate directly overlies ?Leichhardt Metamorphics at Hendersons Soak (6858-720946) and elsewhere along the eastern edge of the Ewen Block; in Prospector, Quilalar Formation arkose and quartzite overlie small inliers of ?Leichhardt Metamorphics unconformably at 6857-7209762, and also overlie Kalkadoon Granite unconformably at Sunday Gully (6857-730573), where cleaved conglomeratic siltstone is also present in the sequence. In Alsace, the formation rests disconformably on acid volcanics of the Argylla Formation, in a series of north-plunging anticlines 15 to 25 km southwest of Dobbyn, and along the eastern edge of the Ewen Block at Mistake Creek (6858-743316). The Quilalar Formation is overlain unconformably by pale pink to purple conglomeratic sandstone of the Fiery Creek Volcanics; this contact is an angular unconformity in many areas of Mount Oxide, west of and just east of Alhambra, but is a disconformity throughout Alsace and Prospector. Where the Fiery Creek Volcanics are absent, basal conglomeratic quartzite of the Surprise Creek Formation overlies the silty and dolomitic sequence of the Quilalar Formation unconformably or disconformably. Weberra Granite intrudes dolomitic rocks of Quilalar Formation in Mount Oxide, a few kilometres west-northwest of Alhambra.|16-MAY-23
15764|Quilalar Formation|Age reasons|Between 1780 m.y. (Argylla Formation) and 1680 m.y. (Carters Bore Rhyolite, a probable correlative of the Fiery Creek Volcanics) (Page, 1978).|16-MAY-23
15764|Quilalar Formation|Correlations|Probably equivalent to the Ballara Quartzite and Corella Formation of the Mary Kathleen Group; possibly equivalent to Stanbroke beds and Makbat Sandstone.|16-MAY-23
15764|Quilalar Formation|Proposed publication|J0503/04|16-MAY-23
24467|Quinine Spring Granite|Name source|Quinine Spring is located about 5 km south of Rosella Plains homestead at GR 324562 (Mount Surprise 1:100 000 Sheet area).|16-MAY-23
24467|Quinine Spring Granite|Unit history|Previously mapped as Forsayth Granite (White, 1962).|16-MAY-23
24467|Quinine Spring Granite|Type section locality|Outcrops of medium-grained equigranular to porphyritic biotite-muscovite granite along Four Mile Creek from GR 249523 (Einasleigh 1:100 000 Sheet area) downstream to a fence-line at GR 271558 (Mount Surprise 1:100 000 Sheet area).|16-MAY-23
24467|Quinine Spring Granite|Description at type locality|Reference locality: At GR 276425 (Einasleigh 1:100 000 Sheet area), medium to coarse-grained porphyritic biotite-muscovite granite, with coarse muscovite 'books' 1 to 2 cm across and subsequent K-feldspar megacrysts up to 3 cm in size, crops out.|16-MAY-23
24467|Quinine Spring Granite|Extent|The unit crops out in two main areas. The largest is an irregularly shaped batholith about 140 km2 in area which extends from approximately 2 km southwest of Rosella Plains homestead to about 15 km northeast of Carpentaria Downs homestead. The other main outcrop area extends along the western side of the Einasleigh River, northwest of Twelve Mile Swamp, from GR 010410 (Einasleigh 1:100 000 Sheet area) in a southeasterly direction to near Washpool Lagoon (GR 092350).|16-MAY-23
24467|Quinine Spring Granite|Lithology|Medium to coarse-grained equigranular to porphyritic biotite-muscovite granite. The granite is pegmatitic in places, and locally a foliation is present. Muscovite 'books', in places up to 2 cm across, are common, particularly in the southern part of the main outcrop area, for example in the reference locality. The porphyritic variety contains pink K-feldspar megacrysts up to 3 cm across. In the northern part of the main outcrop area the unit is most commonly equigranular.|16-MAY-23
24467|Quinine Spring Granite|Relationships and boundaries|The granite intrudes the Proterozoic Einasleigh Metamorphics and is in contact with the Oak River Granodiorite; however, no intrusive relationship has been observed. It is overlain by Cainozoic basalt.|16-MAY-23
24467|Quinine Spring Granite|Age reasons|Uncertain; Middle Proterozoic or Siluro-Devonian. The porphyritic granite bears some resemblance to the Siluro-Devonian Dumbano and McKinnons Creek Granites to the south. These granites are locally weakly foliated.|16-MAY-23
24467|Quinine Spring Granite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24467|Quinine Spring Granite|References|01/31335|16-MAY-23
24467|Quinine Spring Granite|Proposer|Warnick J.V.|16-MAY-23
23931|Quinton Formation|Name source|Parish of Quinton, County of Lyndhurst (Clarke River 1:250 000 Cadastral map).|16-MAY-23
23931|Quinton Formation|Unit history|The unit was previously mapped as part of the Graveyard Creek Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and fully described by Withnall & others (1988), but was not formally defined.|16-MAY-23
23931|Quinton Formation|Geomorphic expression|The unit generally subdued topography, especially where mudstone is dominant.  Strike lines are better developed in the Chinaman Creek area in the west, where arenite is dominant.|16-MAY-23
23931|Quinton Formation|Type section locality|Chinaman Creek (shown on some maps as Graveyard Creek), between 7859 665696 (base) and 610696 (top).  See Withnall & others (1988, figure 26 and page 40) for more details.|16-MAY-23
23931|Quinton Formation|Description at type locality|About 5000 m of lithofeldspathic arenite, mudstone, and conglomerate are exposed, with no obvious repetition by folding.  The arenites are generally coarse-grained and thick to very thick-bedded (relatively proximal turbidite facies).  See Withnall & others (1988, figure 26 and page 40) for more details|16-MAY-23
23931|Quinton Formation|Extent|From 'Pandanus Creek' in the west to Tomcat creek in the east, and from the head of Graveyard Creek in the north to the large laterite plateau in central part of BURGES   a total area of approximately 300 km2.|16-MAY-23
23931|Quinton Formation|Thickness range|The unit is about 5000 m thick in the type section, but it thins eastwards and is probably less than 2000 m in the Top Hut-Tomcat Creek area.|16-MAY-23
23931|Quinton Formation|Lithology|Lithofeldspathic arenite and mudstone, local conglomerate and limestone. Arenites are thin to very thick bedded, commonly graded, with erosive bases, planar and ripple cross laminae, and soft sediment folds (Bouma cycles).  Rocks become more distal in aspect (i.e. thin-bedded and finer grained) east of Martins Well.  Minor volcaniclastic rocks occur in the area south and east of Top Hut Yards.  Further brief notes on lithology included in Relationshipsboundaries section....|16-MAY-23
23931|Quinton Formation|Fossils|Llandovery graptolites, corals, trilobites, and conodonts have been found in the lower part, and Ludlow to Pridoli corals and conodonts occur in the Magpie Creek Limestone Member.  See Withnall & others (1988) for more details.|16-MAY-23
23931|Quinton Formation|Relationships and boundaries|The Quinton Formation conformably overlies the Crooked Creek Conglomerate, and locally unconformably overlies the Judea Formation.  It is overlain possibly disconformably by the Shield Creek Formation which is predominantly feldspathic arenite.  The distal facies of the Quinton Formation is easily distinguished from the latter by being generally thin-bedded arenite and mudstone.  The proximal facies is more difficult to distinguish, but arenites in the Quinton Formation are more lithic.  Polymictic conglomerate is less abundant than in the Crooked Creek Conglomerate.|16-MAY-23
23931|Quinton Formation|Age reasons|Llandovery graptolites, corals, trilobites, and conodonts have been found in the lower part, and Ludlow to Pridoli corals and conodonts occur in the Magpie Creek Limestone Member.  See Withnall & others (1988) for more details.|16-MAY-23
23931|Quinton Formation|References|WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4. Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. **WHITE, D.A., 1962:  Clarke River 1.250 000 Geological series. Bureau of Mineral Resources, Australia, Explanatory Notes, E/55-13.  **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
15817|Rammutt Formation|Unit history|Runnegar & Ferguson (1969) describe the Rammutt Formation in three main sections: a)The lower section is along the Bruce Highway near Bell's Bridge and along Fisherman's Pocket No 1 Road west of Chatsworth. This part of the formation is described as green and grey-green shale, siltstone and argillite. In GEGM mapping these rocks were correlated with the 'Alma unit'. b) The middle section is exposed in cuttings on River Road (Bruce Highway), just north of Normanby Bridge. These outcrops accord with their andesitic lavas. GEGM mapped these as 'Hall andesite'. c) The upper section is the type locality on Rammutt Road, described as subgreywacke and shale overlain by volcanic conglomerate. In Monkland Mine terminology, the upper part is interpreted as 'Top Conglomerate', underlain by 'Alma shale', the two separated by the Laing Fault.|16-MAY-23
15817|Rammutt Formation|Constituents|In this report (GSQ Record 2016/05)  the approach of Cranfield (1999) is adopted, retaining Rammutt as a formation but with five members not four. These members are Glanmire Conglomerate (= 'Top conglomerate'), Pengelly Siltstone, Nash Clastics, Calton Andesite, and a new member, Eldorado Clastics, to replace the 'Lower Nash clastics'.|16-MAY-23
15817|Rammutt Formation|Type section locality|The type section was established along Rammutt Road, east of Chatsworth, to the north of Gympie.|16-MAY-23
15817|Rammutt Formation|Lithology|The dominant lithology is massive volcanoclastic sandstone with intermittent conglomerate beds, capped by massive conglomerate (Glanmire Conglomerate). Below this conglomerate Pengelly Siltstone is a prominent member through the Phoenix, Monkland and Dawn blocks. South of the Great Northern Block the sandstone is segregated into two parts by the Calton Andesite Member, one above (Nash Clastics =GEGM¿s Upper Nash clastics) the other below (Eldorado Clastics = GEGM¿s Lower Nash clastics).|16-MAY-23
28949|Ramsay Crossing Member|Name source|Ramsay Crossing (a low-water ford of The Narrows channel); GR 303,000E, 7,784,500N, Gladstone 1:100 000 topographic sheet.|16-MAY-23
28949|Ramsay Crossing Member|Unit history|Part of The Narrows Beds (Kirkegaard et al, 1970) and part of the Rundle Formation (Henstridge and Missen, 1982).|16-MAY-23
28949|Ramsay Crossing Member|Type section locality|69 m of oil shale with lesser interbeds of claystone and minor impure dolomite; from 266.3 to 335.1 m in drill hole ERD 169 (GR 300,999E, 7,380,998N Gladstone 1:100 000 topographic sheet). The dark yellowish-brown to olive-brown oil shale contains two major greenish-grey claystone beds (from 266.3 to 272.0 m and 390.1 to 299.2 m in the type section). Lesser moderately thick to very thick claystone and clayey oil shale beds occur interbedded within the upper and basal oil shale units (from 274.9 to 278.6 m, 282.7 to 283.8 m, 286.2 to 287.2 m and 310.0 to 310.5 m, 313.0 to 314.3 m, 325.0 to 326.0 m in the type section respectively). A yellowish-grey impure dolomite concentration is contained within the type section from 274.5 to 274.9 m. Cyclicity of lithologies is a feature with oil shale grading upwards through clayey oil shale to claystone, commonly overlain by minor carbonaceous material.|16-MAY-23
28949|Ramsay Crossing Member|Extent|Subcrops in an area of about 73 km2 in The Narrows Graben, NW of Gladstone, Queensland. Part of the unit is exposed in a shallow excavation (slot cut) located between 7,380,611N to 7,380,592N and 303,847E to 304,242E. Very sparse weathered outcrops are recorded. The member has been identified from drill hole core.|16-MAY-23
28949|Ramsay Crossing Member|Thickness range|68.8 m (estimated true thickness 67.8 m corrected for an apparent dip of 9o in ERD 169) in type section. Range of true thickness of the member as intersected in drill holes is 30.1 m to 81.2 m.|16-MAY-23
28949|Ramsay Crossing Member|Lithology|Oil shale, dark yellowish-brown to olive-brown; brecciated and peloidal, well laminated to poorly laminated in part; very thinly to very thickly bedded (up to 2 m); calcareous, clayey and carbonaceous cyclicity. Major and minor interbeds of calcareous greyish-green claystone, rare discontinuous yellowish-grey impure dolomite concentrations and traces of very dark grey carbonaceous shale. Dolomite concentrations tend to be very thick (up to 2.5 m) and are in greater abundance to the northwest and east in The Narrows Graben. Along the southeastern margin of the graben the oil shale beds become attenuated and there is also an associated thickening of the commonly silty to sandy claystone. Claystone and brecciated clayey oil shale generally show bioturbation features. Ostracode tests are abundant with mino gastropods, vertebrate remains (crocodile, turtle), fish fragments and coprolites. Plant remains in the more carbonaceous material include reedy monocots.|16-MAY-23
28949|Ramsay Crossing Member|Relationships and boundaries|The member is conformable with the underlying Teningie Creek Member and is the contact between oil shale and claystone. The upper boundary is the conformable contact between claystone and oil shale of the Brick Kiln Member. The member is faulted against Devonian to Carboniferous rocks of the Curtis Island Group along the western edge of The Narrows Graben.|16-MAY-23
28949|Ramsay Crossing Member|Age reasons|Mid to late Eocene - as for the Rundle Formation.|16-MAY-23
28949|Ramsay Crossing Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
28949|Ramsay Crossing Member|Comments|Note: Drill-core from ERD 169 is stored at Southern Pacific Petroleum's Research and Core Storage Facility located in Gladstone, Queensland.|16-MAY-23
28949|Ramsay Crossing Member|References|79/02402|16-MAY-23
15955|Red Mountain Formation|Name source|Red Mountain, which lies 2 km north of Rubyvale (723114 m, Rubyvale 1:100 000 Sheet area).|16-MAY-23
15955|Red Mountain Formation|Unit history|No other names have been applied to the unit. Robertson (1974) described them under the name Red Mountain Beds in an unpublished report and the name "Red Mountain Beds" appears on a map in Siemon (1977).|16-MAY-23
15955|Red Mountain Formation|Type section locality|The western scarp of Red Mountain (723114 m, Rubyvale 1:100 000) where 13 m of lateritised poorly sorted pebbly sandstone and claystone overlie 1 m of massive silcrete and the Devonian Retreat Granite. The top of the mountain is a flat, partly stripped lateritised poorly sorted pebbly sandstone and claystone overlie 1 m of massive silcrete and the Devonian Retreat Granite. The top of the mountain is a flat, partly stripped lateritised planation surface and could approximate the final depositional surface of the unit.|16-MAY-23
15955|Red Mountain Formation|Extent|Isolated mesas extending northeast and north from Red Mountain on the Rubyvale 1:100 000 Sheet area. About 15 km2 in all.|16-MAY-23
15955|Red Mountain Formation|Thickness range|The maximum measured thickness is 15 m, however the unit may exceed 30 m in places, where its base is concealed by colluvial cover.|16-MAY-23
15955|Red Mountain Formation|Lithology|In the type area Robertson (1974) records under the name Red Mountain Beds a sequence of coarse, angular, consolidated gravels with a silty clayey matrix. The pebbles include angular fragments of metamorphics, highly weathered volcanics, granite, and rounded pebbles and boulders of billy (silcrete) and of 'Kettle beds' (now though to be Permian). However, the dominant lithology in most areas is a ferruginised or mottled, ill-sorted pebbly sandy mudstone. The angular pebbles and poor sorting are diagnostic in distinguishing the unit from Permian sediments which occur in the area. The deposits are probably of fluvial origin and derived from local sources.|16-MAY-23
15955|Red Mountain Formation|Relationships and boundaries|The Red Mountain Formation is flat lying and overlies a silicified surface or is unconformable on Palaeozoic granites and on the Permian "Kettle Conglomerate member" of the Aldebaran Sandstone. The top of the formation is a lateritised surface of low relief. The relationship between the formation and Tertiary basalts or the Emerald Beds is not known. Robertson (1974) thought that the "Red Mountain Beds" might be younger than the "sapphire wash" of this area, but this seems unlikely in view of its position in the landscape and the well developed laterite.|16-MAY-23
15955|Red Mountain Formation|Age reasons|No fossils have been found. The unit is tentatively regarded as mid Tertiary as it overlies a silcrete bed and predates a lateritised surface. The laterites of this region would seem to be of mid to late Tertiary age, from their relationships to dated basalts, and silcretes overlie an early Tertiary unit further to the north (cf Grimes, in press). The relationship between the formation and the basalt flows and plugs in the area or to the Emerald Beds (both of which are of mid Tertiary age) is unfortunately not known.|16-MAY-23
15955|Red Mountain Formation|References|79/03959; 82/22417|16-MAY-23
22743|Redlands Granite|Name source|Redlands station north of the Flinders Highway at GR 3807 77620 in the Homestead 1:100 000 Sheet area. The grid reference is based on the AGD66 datum.|16-MAY-23
22743|Redlands Granite|Unit history|The Redlands Granite was previously mapped as Lolworth Igneous Complex by Wyatt & others (1971), Clarke & Paine (1970).|16-MAY-23
22743|Redlands Granite|Type section locality|On the northern flanks of Mount Oweenee at GR 3716 77694.  The grid reference is based on the AGD66 datum.|16-MAY-23
22743|Redlands Granite|Description at type locality|Here a pink to cream, muscovite leucogranite comprises quartz, poikilitic K-feldspar, lath-shaped plagioclase, muscovite and minor garnet.|16-MAY-23
22743|Redlands Granite|Extent|Crops out over about 8km2 around Mount Oweenee which is north of Balfe Creek about 12km west of Balfes Creek township.|16-MAY-23
22743|Redlands Granite|Lithology|The rocks at the type locality are typical of the unit. No layered granite/pegmatite/aplite dykes were observed in the Redlands Granite in the present study. Petrographically, the Redlands Granite has large poikilitic K-feldspar grains, a feature of granites in the Amarra Suite, and it is included as a fractionated member of that suite.|16-MAY-23
22743|Redlands Granite|Relationships and boundaries|The Redlands Granite is surrounded by Tertiary sediments and its relationship to adjacent rocks is not known.|16-MAY-23
22743|Redlands Granite|Age reasons|The age of the Redlands Granite is not known precisely. A Late Silurian to Early Devonian age is assigned because of lithological similarity to other rock types in the Lolworth Batholith.|16-MAY-23
22743|Redlands Granite|Comments|The Redlands Granite is non-magnetic.|16-MAY-23
22743|Redlands Granite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
22746|Reedybed Granite|Name source|Reedybed Creek, which joins Hann Creek at GR 3540 77784.  The grid reference is based on the AGD66 datum.|16-MAY-23
22746|Reedybed Granite|Unit history|The Reedybed Granite was included in the Lolworth Igneous Complex by Wyatt & others (1971), Clarke & Paine (1970).|16-MAY-23
22746|Reedybed Granite|Type section locality|Beside the track near the junction of Reedybed and Hann Creeks at GR 3540 77783 in the Homestead 1:100 000 Sheet area.|16-MAY-23
22746|Reedybed Granite|Description at type locality|Here, a white to pink, medium grained, muscovite-biotite granite is interlayered with layered leucogranite. The rock comprises quartz, poikilitic K-feldspar, plagioclase, muscovite and biotite with traces of epidote and zircon.|16-MAY-23
22746|Reedybed Granite|Extent|The Reedybed Granite crops out over 90-100km2 north and south of Barrington station.  Most of the outcrop area is deeply weathered making determination of the distribution of the Reedybed Granite difficult. Medium grained granite cropping out along Emu Creek and in the upper parts of Gardiner Creek south of Barrington station are also included in the Reedybed Granite.|16-MAY-23
22746|Reedybed Granite|Lithology|Only a few fresh outcrops of the Reedybed Granite are known as much of the unit is deeply weathered. Fresh outcrop is restricted to bands between layered leucogranite sheets of the Grasstree Leucogranite which intrudes the Reedybed Granite. All outcrop, both fresh and weathered, is medium grained, muscovite-biotite granite with rare biotite clots. South of Barrington station, some fresher outcrops of medium grained biotite granite have been assigned to the Reedybed Granite.|16-MAY-23
22746|Reedybed Granite|Relationships and boundaries|The Reedybed Granite is intruded by the Late Silurian to Early Devonian Grasstree Leucogranite . Its relationships to adjacent granitoids such as the Hodgon Granodiorite and Amarra Granite are uncertain.|16-MAY-23
22746|Reedybed Granite|Age reasons|The age of the Reedybed Granite is not known precisely. An age of Late Silurian to Early Devonian is assigned due to its similarity to other Amarra Suite granites of this age in the Lolworth Batholith.|16-MAY-23
22746|Reedybed Granite|Comments|MAGNETIC SUSCEPTIBILITY::  Magnetic susceptibilities at the type locality are 368-567 x 10[superscript]-5 SI units. Throughout the outcrop area, magnetic susceptibilities are 0-723 10[superscript]-5 SI units. The lower values correspond to more deeply weathered outcrops.|16-MAY-23
22746|Reedybed Granite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
22751|Retchford Granite|Name source|The unit is named after the Retchford gold mine located ~300 m south of the pluton (Richards, 1981).|16-MAY-23
22751|Retchford Granite|Unit history|The pluton was previously included in the Almaden Granite (Best, 1962;  de Keyser & Wolff, 1964;  Branch, 1966).|16-MAY-23
22751|Retchford Granite|Geomorphic expression|The Retchford Granite forms undulating to hilly terrain with scattered boulders and bouldery outcrops.  It is characterised by pale to medium tones on aerial photographs.|16-MAY-23
22751|Retchford Granite|Extent|The Retchford Granite forms several small elongate plutons exposed over an area of ~2 km2, 4 km east-northeast and north of Fluorspar.|16-MAY-23
22751|Retchford Granite|General description|STRUCTURE AND METAMORPHISM:: The Retchford Granite forms an essentially unmetamorphosed, massive, discordant pluton.MINERALISATION:: No mineral deposits are known in the adamellite.|16-MAY-23
22751|Retchford Granite|Lithology|Fine to medium-grained, pale pink (hornblende-) biotite adamellite is the main rock type.  Minor aplite as small pods and dykes is also present.The main minerals present in the adamellite are quartz, plagioclase, and K-feldspar, together with minor biotite, opaque oxide(s) and pyrite.  The one thin section of a sample from this pluton examined also contained traces of hornblende (mainly as small inclusions in large plagioclase grains), but according to Richards (1981) much of the pluton is devoid of amphibole.  Most grains are between 0.5 and 1 mm in length, but quartz and plagioclase grains range up to 3 mm across.  Granophyric intergrowths are common.  Quartz grains show undulose extinction.  Plagioclases form subhedral laths with cores of andesine (~An40; Richards, 1981), commonly mantled by rims of zoned, more sodic plagioclase.  The designated type locality is at GR 2495 80917, ~700 m northeast of the Retchford gold mine (abandoned).Plagioclase grains in contact with K-feldspar are locally rimmed by a thin selvage of more sodic plagioclase (albite).  A similar feature was described in samples of Ootann Granite by Richards (1981) who determined the composition of the selvage to be ~An7.  A few of the larger plagioclase grains contain subhedral grains (0.2 mm long) of hornblende, pleochroic from dark green to pale yellowish green.  The cores of relatively calcic plagioclase are commonly partly to extensively replaced by sericite, locally accompanied by rare epidote/clinozoisite.K-feldspar is mainly orthoclase microperthite which forms euhedral to anhedral grains up to 2 mm long and relatively small, anhedral grains granophyrically intergrown with quartz.Biotite forms subhedral grains, typically 0.5 to 1 mm in length.  The grains are pleochroic from very dark brown to pale yellowish brown (straw), contain sparse small inclusions of opaque oxide, and are commonly partly replaced by chlorite and secondary muscovite.  Aggregates of smaller, ragged biotite grains similar to those found, for example, in the Ruddygore and Almaden Granodiorites were not observed in the thin section examined.Scattered grains of pyrite, commonly altered to secondary iron oxides are fairly common.|16-MAY-23
22751|Retchford Granite|Relationships and boundaries|The adamellite intrudes the Redcap Dacite (Volcanics) and Almaden Granodiorite.  Its relationship with the Hiker Granodiorite is unknown.  The pluton is cut by dykes and small pods of aplite.|16-MAY-23
22751|Retchford Granite|Age reasons|The unit is most probably Late Carboniferous.  The adamellite has not been isotopically dated, but it post-dates the Almaden Granodiorite which has yielded Rb/Sr isotopic ages ranging between 301 Ma and 302 Ma (Richards, 1981).|16-MAY-23
22751|Retchford Granite|Comments|The Retchford Granite forms a small heterogeneous pluton and is a member of the Ootann Supersuite.  According to Richards (1981) it is similar mineralogically to the Ootann Granite exposed farther south.|16-MAY-23
22751|Retchford Granite|References|BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.BRANCH, C.D., 1966:  Volcanic cauldrons, ring complexes, and associated granites of the Georgetown Inlier, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 76.DE KEYSER, F., & WOLFF, K.W., 1964:  The geology and mineral resources of the Chillagoe area.  Bureau of Mineral Resources, Australia, Bulletin 70.RICHARDS, D.N.G., 1981:  Granitoids of the northern Tate batholith, Chillagoe, north Queensland.  Ph.D. Thesis, James Cook University of North Queensland, Townsville (unpublished).|16-MAY-23
24471|Revenue Granite|Name source|The granite is named after the Revenue group of mines and prospects, about 8-9 k, NNW of Duchess, Duchess 1:100 000 Sheet area (Duchess 1:250 000 Sheet area).|16-MAY-23
24471|Revenue Granite|Unit history|Previously mapped was Wonga Granite (Carter & Opik, 1963).|16-MAY-23
24471|Revenue Granite|Type section locality|About 11.5 km N of Duchess, from GR 813496 to GR 823496, drained by unnamed tributaries of the Little Burke River. Here the granite consists mainly of medium to coarse-grained, foliated biotite leucogranite together with some non-foliated aplite and pegmatite (mainly around the margins).|16-MAY-23
24471|Revenue Granite|Extent|The granite crops out mainly as an elongate pluton, up to 3.5 km wide, about 6 to 18 km N of Duchess. The small pod of granite mapped as part of this unit about 4 km NW of Duchess may be part of the main body displaced along the Saint Andrews Fault.|16-MAY-23
24471|Revenue Granite|Lithology|Mainly medium to coarse-grained, even-grained to slightly porphyritic, foliated, commonly partly recrystallised biotite leucogranite. In places, for example, at GR 793456, the marginal zone of the granite consists of pink, fine to medium-grained, even-grained, non-foliated aplite which grades towards the centre of the pluton into pink medium-grained, even-grained, non-foliated aplite which grades towards the centre of the pluton into pink medium-grained, even-grained biotite leucogranite with a primary flow foliation. The granite contains sparse mafic xenoliths and large inclusions and pendants of mainly calc-silicate rocks probably derived from the enclosing Corella Formation. A gneissic foliation developed in the granite NE of the Revenue group of mines shows crenulations with wave lengths of about 30 cem and amplitudes of about 15 cm. The assertions by Joplin & Walker (1961) that this crenulated gneissic granite represents metasomatised calc-silicate rocks seems unlikely, because contacts between calc-silicates of the Corella Formation and crenulated granite are sharp (resolvable within 1 to 2 cm) and appear cross-cutting. Swarms of tourmaline-bearing, graphic quartz-feldspar pegmatite dykes in the adjacent Corella Formation hav ebeen mapped as part of the Revenue Granite.|16-MAY-23
24471|Revenue Granite|Relationships and boundaries|The Revenue Granite intrudes the Corellla Formation and some amphibolitic metadolerite bodies.|16-MAY-23
24471|Revenue Granite|Age reasons|Proterozoic|16-MAY-23
24471|Revenue Granite|Proposed publication|Blake & others, in preparation (R233)|16-MAY-23
24471|Revenue Granite|Comments|The Revenue Granite may be a correlative of the Burstall and Overlander Granites and of the granites of the Myubee and Mount Erle Igneous Complexes. Calc-silicates of the Corella Formation adjacent to the granite SE of Green Creek Tank (GR 795521) have been extensively metasomatised and converted to skarns.|16-MAY-23
24471|Revenue Granite|References|R233;   98/29253|16-MAY-23
24471|Revenue Granite|Proposer|Bultitude R.J.|16-MAY-23
24472|Riversleigh Siltstone|Name source|From Riversleigh station; the homestead is located 2 km southwest of the junction of the Gregory and O'Shannassy Rivers at 6659-620941.|16-MAY-23
24472|Riversleigh Siltstone|Unit history|The rocks now mapped as Riversleigh Siltstone were previously assigned to the Ploughed Mountain Beds, Pradise Creek Formation and Pilpah Sandstone by Carter & others (1961).|16-MAY-23
24472|Riversleigh Siltstone|Type section locality|Holostratotype: A composite type section comprising a holostratotype covering the upper 2400 m and a parastratotype covering the basal 800 m is defined. The holostratotype is situated 13 km due north of Riversleigh homestead and extends from 604073 (base) to 576070 (top) in the Lawn Hill 1:100 000 Sheet area. It can be subdivided into four informal subunits:  200 m - fine clayey siltstone (top).  400 m - leached carbonaceous shale.  300 m - fine to coarse grained gritty sandstone.  1500 m - laminated siltstone, thinly interbedded with coarse siliceous siltstone and minor dolomite (base).  Parastratotype: The parastratotype is situated 8 km south of the holostratotype and extends from 6660-1012 (base) to 6660-624007 (top). It is 800 m thick and comprises coarse quartz siltstone with three fine grained clayey dolomitic sandstone beds each between 100 and 150 m thick.|16-MAY-23
24472|Riversleigh Siltstone|Extent|Discontinuously as a long narrow belt of broadly folded rocks from Musselbrook Creek in the Bowthorn 1:100 000 Sheet area, through the Mount Oscar, Lawn Hill, Riversleigh, Mount Oxide, Mammoth Mines, Kennedy Gap and Undilla 1:100 000 Sheet areas to the Yelvertoft 1:100 000 Sheet area in the south. It is best exposed in the southern part of the Lawn Hill and Riversleigh Sheet areas where it crops out in the cores of numerous basins and domes.|16-MAY-23
24472|Riversleigh Siltstone|Thickness range|The unit is 3200 m thick in the combined type sections but is only 800 m thick in the Ploughed Mountain anticline. A minimum of 300 to 400 m is present between the southern part of the Riversleigh Sheet area and the northern part of the Undilla Sheet area.|16-MAY-23
24472|Riversleigh Siltstone|Lithology|South of the type sections, only the lower part of the Riversleigh Siltstone crops out. These rocks mainly comprise coarse quartz siltstone and fine to medium clayey sandstone. To the north of the type sections in the Ploughed Mountain anticline, about 800 m of laminatead siltstone, fine sandstone and carbonaceous shale crop out.|16-MAY-23
24472|Riversleigh Siltstone|Relationships and boundaries|The unit conformably overlies the Shady Bore Quartzite. Usually the boundary is sharp but in places siltstone of the Riversleigh Siltstone intertongues with orthoquartzite of the Shady Bore Quartzite. Conformably overlying the Riversleigh Siltstone is massive arenite of the Termite Range Formation. In the type section this boundary is sharp but intertonguing of the two units occurs to the north. South of the Gregory River, the Riversleigh Siltstone is the youngest outcropping formation in the McNamara Group. Here it is unconformably overlain by Cambrian sediments.|16-MAY-23
24472|Riversleigh Siltstone|Age reasons|Mid Proterozoic (Carpentarian)|16-MAY-23
24472|Riversleigh Siltstone|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24472|Riversleigh Siltstone|References|B051|16-MAY-23
24472|Riversleigh Siltstone|Proposer|Hutton L.J., Cavaney R.J., Sweet I.P.|16-MAY-23
25745|Robertson River Subgroup|Name source|The Robertson River, a major tributary of the Gilbert River.|16-MAY-23
25745|Robertson River Subgroup|Unit history|Robertson River Metamorphics (White, 1959, 1965) and Robertson River Formation (Withnall & Mackenzie, 1980) as outlined in the Introduction.|16-MAY-23
25745|Robertson River Subgroup|Constituents|The constituent formations of the Robertson River Subgroup are, in ascending stratigraphic order, the Daniel Creek Formation, Dead Horse Metabasalt, Corbett Formation, and Lane Creek Formation.|16-MAY-23
25745|Robertson River Subgroup|Extent|Crops out as a broad belt, 50 km wide and 150 km long, extending from around Gilberton homestead to near Dagworth homestead, and mostly between the Gilbert River and the Newcastle Range. The total area is about 5000 km2.|16-MAY-23
25745|Robertson River Subgroup|Thickness range|The thickness of the subgroup is difficult to determine because of the intense multiple deformation which has affected much of its outcrop area. A composite section made up of the type and reference sections of its constituent formations is about 4000 m thick. This is only a rough order of magnitude because the constituent units range considerably in thickness. For example, the Dead Horse Metabasalt, which is up to 1000 m thick, pinches out entirely in the northern half of the outcrop area.|16-MAY-23
25745|Robertson River Subgroup|Lithology|Mainly cleaved mudstone, siltstone, fine-grained sandstone, and metabasalt grading eastwards into mica schist, quartzite and amphibolite. The sedimentary rocks are locally calcareous and the finer grained rocks are locally variably carbonaceous.|16-MAY-23
25745|Robertson River Subgroup|Relationships and boundaries|The Robertson River Subgroup, which is part of the Etheridge Group, conformably overlies the Bernecker Creek Formation, and is overlain conformably by the Townley Formation. Criteria for recognising these boundaries are included in the definitions of the Daniel and Lane Creek Formations, respectively. The subgroup is intruded by the Proterozoic Cobbold Metadolerite, by a variety of Proterozoic and Siluro-Devonian granitoids, and by various late Palaeozoic igneous rocks. It is overlain unconformably by various late Palaeozoic volcanic units and the Jurassic Hampstead Sandstone.|16-MAY-23
25745|Robertson River Subgroup|Age reasons|The minimum age of 1570+/-30 Ma (mid-Proterozoic) obtained by dating the earliest deformational-metamorphic event in the Etheridge Group (Black & others, 1979), also applies to the Robertson River Subgroup and its constituent formations.|16-MAY-23
25745|Robertson River Subgroup|Proposed publication|Queensland Government Mining Journal|16-MAY-23
25745|Robertson River Subgroup|Comments|White (1959, 1965) gave the name Robertson River Metamorphics to an area of metamorphic rocks in the Robertson River area. Subsequent work by the joint BMR-GSQ party and James Cook University staff and students demonstrated that these graded westwards into low-grade metasedimentary correlatives. Having established the stratigraphic position of these low-grade correlatives in the Etheridge Group, Withnall & Mackenzie (1980) changed the name of the unit to Robertson River Formation, and redefined it to include both the low and high-grade metamorphic rocks. They informally divided it into upper and lower subunits. The lower subunit was effectively subdivided into two more metasedimentary subunits by the Dead Horse Metabasalt Member. Each of these three metasedimentary subunits is lithologically distinct and it is now considered desirable to name them as formations. The Dead Horse Metabasalt Member is also redefined as a formation. The Robertson River Formation is redefined as a subgroup. The name is retained because, although the formations are readily distinguished in their low-grade parts, the distinctions become less apparent at higher grades. Consequently some workers may find it useful to have an overall term for the high-grade metamorphic rocks. Field work was completed in the higher grade parts of the subgroup before the detailed stratigraphy was established in the low-grade rocks. The boundaries can be extrapolated into the high-grade areas, but have not been mapped in detail. Criteria which could be applied by subsequent field workers to locate the boundaries more accurately, are given with definitions of the individual formations.|16-MAY-23
25745|Robertson River Subgroup|References|80/20677; 98/29026; B071; 80/20650|16-MAY-23
16185|Robin Hood Granodiorite|Name source|"Robin Hood" Homestead at GR 853 146 (Forsayth 1:100 000 Sheet area).|16-MAY-23
16185|Robin Hood Granodiorite|Unit history|Robin Hood Granite (White 1959; 1962b, c; 1965).|16-MAY-23
16185|Robin Hood Granodiorite|Type section locality|The type area given by White (1959) was "one mile (1.6 km) west of Robin Hood Homestead on the Forsayth track". However as this point lies within the Robertson River Metamorphics it is suggested that a more appropriate type area should be given. Excellent exposures of grey hornblende-biotite granodiorite with quartz phenocrysts crop out along the Robin Hood-Fish Hole track between GR 861 151 and 865 220; this is designated the new type area.|16-MAY-23
16185|Robin Hood Granodiorite|Extent|Crops out in a belt 50 km long and up to 20 km wide between "Robin Hood" and "Percyvale" Homesteads.|16-MAY-23
16185|Robin Hood Granodiorite|Lithology|Pink to grey, massive, hornblende-biotite granodiorite with quartz phenocrysts. The unit is remarkably uniform over the whole outcrop area.|16-MAY-23
16185|Robin Hood Granodiorite|Relationships and boundaries|Intrudes the Proterozoic Einasleigh Metamorphics, Robertson River Metamorphics and Digger Creek Granite (new name). Unconformably overlain by the Carboniferous Newcastle Range Volcanics, Permian Agate Creek Volcanics and Jurassic-Cretaceous sandstone.|16-MAY-23
16185|Robin Hood Granodiorite|Age reasons|Probably Silurian or Devonian. Rb/Sr dating on a biotite sample gave a minimum age of 426 million years (Black, 1973).|16-MAY-23
16185|Robin Hood Granodiorite|Comments|Discussion: White (1959) defined the Robin Hood Granite as "a hornblende-biotite granite". Petrographic studies show that the unit is a hornblende-biotite granodiorite rather than a granite. Granodiorite is therefore considered a more appropriate lithological term and the name of the unit is changed to Robin Hood Granodiorite. Areas of muscovite leucogranite and pegmatite were included in the Robin Hood Granite on the Georgetown and Gilberton 1:250 000 Geological Series Maps (White, 1962b, c) although this lithology was not mentioned in either the map legend or the explanatory notes. Recent mapping (Bain et al. in prep), isotopic dating (Black, 1973) and geochemical studies (Sheraton and Labonne, in press) show that the muscovite leucogranite is easily mappable as a unit, separate from the hornblende-biotite granodiorite, that it is probably much older and that it is probably derived from a different magma to that of the granodiorite.|16-MAY-23
16185|Robin Hood Granodiorite|References|76/004; 73/050; B169; 98/29026; -; 01/31334; B071|16-MAY-23
16201|Rockfields Member|Name source|Parish of Rockfields, County of Clarke (Clarke River 1:250 000 Cadastral map).|16-MAY-23
16201|Rockfields Member|Unit history|The member was previously mapped as part of the Bundock Creek Formation (now Group) (White, 1959, 1962, 1965).  The name was first published by Withnall & others (1988), and described in full but not formally defined.|16-MAY-23
16201|Rockfields Member|Geomorphic expression|The unit forms a series of low strike ridges, sparsely vegetated with stunted silver leaf ironbark and quinine bush.  Individual bands of white and brownish tones on the aerial photos correspond with tuffs and redbeds, respectively.|16-MAY-23
16201|Rockfields Member|Type section locality|In the type section of the Bulgeri Formation in the Broken River between 7859 578447 (base) and 560444 (top).  The grid reference is based on the Agd66d datum.|16-MAY-23
16201|Rockfields Member|Description at type locality|The section is 795 m thick, and begins with a polymictic, pebble to cobble conglomerate overlain by red and drab, fine to medium-grained lithofeldspathic sandstone, grey mudstone, variegated and greyish red fine-grained redbeds, thin, reworked, fine-grained tuff beds, and minor rip-up-clast conglomerate.  See Withnall & others (1988, figure 52 and page 81) and Lang (1985, 1986a) for more details.|16-MAY-23
16201|Rockfields Member|Extent|A sinuous folded belt from about 7858-485335 near Pages Dam in the south to about 7859-585545 in the hinge of the Atherton Creek Anticlinorium.  The grid reference is based on the AGD datum.|16-MAY-23
16201|Rockfields Member|Thickness range|795 m in the type section, thinning progressively to the northeast until it wedges out near the hinge of the Atherton Creek Anticlinorium at about 7859-587545.  The grid reference is based on the AGD66 datum.|16-MAY-23
16201|Rockfields Member|Lithology|Fine to medium-grained lithofeldspathic sandstone, mudstone, fine-grained redbeds, reworked tuff, and rip-up-clast conglomerate as in the type section.  Polymictic conglomerate also occurs at the base of the unit.  Towards the Clarke River Fault in the south, the unit becomes coarser grained until it contains lithofacies assemblages indistinguishable from the rest of the Bulgeri Formation.|16-MAY-23
16201|Rockfields Member|Fossils|Rare Cyrtospirifer sp. and bivalves have been found near the base in both outcrop and in GSQ Clarke River 2 (Lang, 1985, 1986a; Law, 1986).  Rare plant remains, usually indeterminate but including some lycopod casts, are present.  Non-marine fish remains occur sporadically throughout the unit, in both the fine-grained redbeds and foresets and channel lags in the sandstone.|16-MAY-23
16201|Rockfields Member|Relationships and boundaries|The Rockfields Member forms the basal part of Bulgeri Formation, overlying the Mytton Formation of the Broken River Group with slight angular unconformity (a few degrees) to disconformity. The base is generally marked by a pebble conglomerate containing abundant quartz and quartzite clasts.  The sandstones are less lithic than those in the underlying Mytton Formation and are commonly interbedded with redbeds.  The member is distinguished from the rest of the Bulgeri Formation by being generally finer grained and containing abundant soft-sediment deformation.  The unit is generally overlain by white, pebble conglomerate and very coarse sandstone of the undivided Bulgeri Formation. However, between the north branch of Gorge Creek at 7859-641537 and where it wedges out in the hinge of the Atherton Anticlinorium, it is conformably overlain by the Stopem Blockem Conglomerate Member.|16-MAY-23
16201|Rockfields Member|Age reasons|The unit is most likely of Late Devonian (Famennian) age because of Cyrtospirifer, although it could be as old as Frasnian.|16-MAY-23
16201|Rockfields Member|References|LANG, S.C., 1985:  Devonian-Carboniferous stratigraphy of the 	southeastern Bundock Basin, Broken River area, north Queensland. B.Sc. (Hons) Thesis, University of Queensland (unpublished) LANG, S.C., 1986a:  Devonian-Carboniferous stratigraphy of the 	southeastern Bundock Basin, Broken River area, north Queensland. Geological Survey of Queensland, Record 1986/5 (unpublished).LAW, S.R., 1986:  GSQ Clarke River 2 - preliminary lithological log and composite log.  Geological Survey of Queensland, Record 1986/53 (unpublished).WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.WHITE, D.A., 1962:  Clarke River - Qld E/55-13.  Bureau of Mineral 	Resources, Australia 1:250 000 Geological Series Explanatory Notes.WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River 	area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.D., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
23942|Rolfe Creek Schist|Name source|Rolfe Creek, which joins Oaky Creek at 8352-479761.|16-MAY-23
23942|Rolfe Creek Schist|Unit history|Previously mapped as Anakie Metamorphics (Malone & others, 1964; Veevers & others, 1964a, b) and now part of the Anakie Metamorphic Group.|16-MAY-23
23942|Rolfe Creek Schist|Geomorphic expression|The Rolfe Creek Schist is distinguishable on Landsat 5 TM bands 1-4-7 (BGR) images by a reddish purple colour which contrasts with the bluish greens of the adjacent units. On coloured aerial photographs it has a slightly reddish tint. The Monteagle Quartzite is also generally more densely vegetated. The Rolfe Creek Schist commonly has a dense midstorey of small Acacia species, and larger trees are sparser than in the Bathampton Metamorphics. It also appears to be more prominent topographically than the Bathampton Metamorphics and is better exposed, the soil commonly being littered with small reddish schist fragments.   On the geophysical images, it is slightly more magnetic than adjacent units, possibly reflecting the local magnetite porphyroblasts. It also stands out on radiometric images, being overall richer in K and Th than the adjacent quartzite-bearing units.|16-MAY-23
23942|Rolfe Creek Schist|Type section locality|In the Slaty Creek - Expedition Creek area, in particular between 8352-461816 (the contact with the Bathampton Metamorphics) and 429804 (the contact with the Monteagle Quartzite).  The grid references are based on the AGD66 datum.|16-MAY-23
23942|Rolfe Creek Schist|Description at type locality|In this area, the homogeneous fine-grained, grey to green, mica schist or phyllite of the Rolfe Creek Schist is easily distinguished from the quartzite-bearing Bathampton Metamorphics and Monteagle Quartzite.|16-MAY-23
23942|Rolfe Creek Schist|Extent|The Rolfe Creek Schist forms a belt, 2 to 5 km wide, from the northern edge of MONTEAGLE in the headwaters of Western Creek and its tributaries for about 30 km to Oaky Creek. From there, the unit is folded around the Oaky Creek antiformal dome and is generally narrower (1 to 2 km wide). To the south of the dome (west of Sunny Park homestead), the foliation flattens and the unit is up to 3 km wide, surrounding a core, about 4 km across, of rocks tentatively assigned to the Monteagle Quartzite. Farther south, the unit is truncated by the Retreat Batholith. It has not been recognised south of the batholith in the Rubyvale area.|16-MAY-23
23942|Rolfe Creek Schist|Lithology|Generally greenish grey, weathering to reddish brown, fine-grained mica schist grading to phyllite. Metamorphic grade is greenschist facies (biotite zone).|16-MAY-23
23942|Rolfe Creek Schist|Relationships and boundaries|The Rolfe Creek Schist contrasts with the Bathampton Metamorphics and Monteagle Quartzite by being a homogeneous pelitic unit lacking quartzite and greenstone. It consistently occupies a position between the Bathampton Metamorphics and the Monteagle Quartzite around the Oaky Creek antiformal dome and northwest to the Western Creek area. It is uncertain whether the contacts are stratigraphic or tectonic, but this consistent relationship lends support to a stratigraphic relationship, at least in part.   The unit is intruded by the Devonian Sunny Park Granodiorite and Kilmarnock Granodiorite. It is faulted against the Silver Hills Volcanics near Sunny Park homestead and overlain by various Cainozoic deposits.|16-MAY-23
23942|Rolfe Creek Schist|Age reasons|The original age is still uncertain, but is probably Early Cambrian or Neoproterozoic.|16-MAY-23
23942|Rolfe Creek Schist|References|MALONE, E.J., CORBETT, D.P.W., & JENSEN, A.R., 1964: Geology of the Mount Coolon 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 64.VEEVERS, J.J., RANDAL, M.A., MOLLAN, R.G., & PATEN, R.J., 1964a: The geology of the Clermont 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report, 66.VEEVERS, J.J., MOLLAN, R.G., OLGERS, F., & KIRKEGAARD, A.G., 1964b: The geology of the Emerald 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 68.|16-MAY-23
23943|Rollingstone Granite|Name source|Named for the township of Rollingstone.|16-MAY-23
23943|Rollingstone Granite|Unit history|Wyatt & others (1970) included the Rollingstone Granite in an unnamed granitoid unit, C-Pg, which contained granite, adamellite and some granodiorite.|16-MAY-23
23943|Rollingstone Granite|Geomorphic expression|The granite generally forms part of the steep, rugged coastal scarp. Areas of outcrop are very rocky, consisting of abundant large boulders and tors.|16-MAY-23
23943|Rollingstone Granite|Type section locality|A hill at (8159-357934), just west of Rollingstone township.  The grid reference is based on the AGD66 datum.|16-MAY-23
23943|Rollingstone Granite|Description at type locality|Composed of mottled, cream and pink, fine-grained, slightly to moderately porphyritic, biotite granite.|16-MAY-23
23943|Rollingstone Granite|Extent|The Rollingstone Granite crops out as several irregularly shaped bodies in the north of ROLLINGSTONE. One body, 7km2 in area, crops out on the eastern side of the Paluma Range between the townships of Kinduro and Rollingstone (from which the name is derived). Three small bodies (each up to 1km2) lie just to the south of Rollingstone. A larger body (approximately 9km2) crops out in the Little Crystal Creek National Park area and extends north of ROLLINGSTONE. In addition, an area of some 3km2 has been interpreted from aerial photography and company report data (C.R. 6852) in dense tropical rainforest near the headwaters of Blue Gum Creek.|16-MAY-23
23943|Rollingstone Granite|Lithology|The Rollingstone Granite is a mottled cream and pink, fine to medium-grained, slightly to abundantly porphyritic, biotite granite. Phenocrysts are quartz, K-feldspar, plagioclase up to 2cm.|16-MAY-23
23943|Rollingstone Granite|Relationships and boundaries|The Rollingstone Granite intrudes both the Paluma Rhyolite and Clemant Microgranite.|16-MAY-23
23943|Rollingstone Granite|Age reasons|A sample from the Rollingstone Granite was included in the Rb/Sr isochron of Webb (1969) and Wyatt & others (1970) that suggested an Early Carboniferous age (342±7 Ma) for the "Oweenee Granite". Although this age is probably not reliable because of the mixing of samples from different units, an Early Carboniferous age is consistent with the relationships. However, it may be as young as Early Permian.|16-MAY-23
23943|Rollingstone Granite|References|WEBB, A.W., 1969: Metallogenic epochs in eastern Queensland.  Proceedings of the Australasian Institute of Mining and Metallurgy, 230, 27 39. **WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127.|16-MAY-23
23948|Ruddygore Granodiorite|Name source|The unit was named by Richards (1981) after Ruddygore copper mine, which is located in the granodiorite about 3 km northeast of Chillagoe.|16-MAY-23
23948|Ruddygore Granodiorite|Unit history|Previously mapped as part of the Almaden Granite by Best (1962), de Keyser & Wolff (1964), and Branch (1966).|16-MAY-23
23948|Ruddygore Granodiorite|Geomorphic expression|The unit forms mainly gently undulating terrain with scattered boulders and bouldery hills.  Prominent bouldery hills of black weathering granodiorite occur north of Chillagoe and are known locally as 'metal hills' because of the metallic ring produced when the boulders are struck with a hammer.  Most areas underlain by the granodiorite are characterised by open drainage patterns and pale to medium tones on aerial photographs.|16-MAY-23
23948|Ruddygore Granodiorite|Type section locality|The proposed type area is Coonbeta Hill, around GR 2380 81028.  The unit is well exposed in this area and readily accessible from Chillagoe.|16-MAY-23
23948|Ruddygore Granodiorite|Extent|The granodiorite forms an ovoid pluton of about 350 km2 (Richards, 1981).  It extends from about 2.5 km north of Calcifer (abandoned site) to north of the Walsh River.|16-MAY-23
23948|Ruddygore Granodiorite|General description|Alteration:  Most, if not all, of the Ruddygore Granodiorite has undergone slight to extensive hydrothermal alteration.  The most common secondary minerals are sericite, muscovite, chlorite, epidote/clinozoisite, actinolite and sphene.  Calcic plagioclase grains are extensively replaced by sericite, generally accompanied by epidote/clinozoisite and rare muscovite and sphene, whereas rims of more sodic plagioclase are little altered.  Biotite grains are commonly partly replaced by secondary muscovite and partly to completely replaced by chlorite, generally accompanied by some epidote/clinozoisite and/or sphene.  Hornblende grains are partly to extensively replaced by actinolite or chlorite, commonly with some associated sphene and epidote/clinozoisite. Scattered secondary iron oxide-stained patches are present locally in the granodiorite.  The secondary iron oxides have probably replaced sulphide minerals.  The alteration is reported to display a crude zonation in places (Broadhurst, 1949;  Richards, 1981).  According to Richards the first indication of alteration in the outer zone is a change from brown to red-brown in the colour of biotite grains.  This is followed by conversion of biotite to chlorite, epidote/clinozoisite and sphene.  Orthoclase, plagioclase and hornblende remain virtually unaffected.  In more extensively altered rocks, such as those exposed in the Ruddygore mine area, the mafic minerals are generally completely altered and feldspar grains are cloudy or replaced by sericite.  Chlorite grains commonly have a bleached appearance (Stillwell, 1947).  ENDOSKARNS::  consist mainly of metasomatically altered granodiorite which formed adjacent to contacts with calcareous units of the Chillagoe Formation, are not as extensively developed in the Ruddygore Granodiorite as in the Almaden Granodiorite to the south.  Several small outcrops of extensively modified granodiorite occur in the Zillmanton area.STRUCTURE AND METAMORPHISM::  The Ruddygore Granodiorite is an essentially massive, unmetamorphosed, discordant pluton.  Richards (1981) reported a vertical foliation in the granodiorite near the Walsh River, at about GR 2405 81109.MINERALISATION:: The Ruddygore Granodiorite contains the Ruddygore copper deposit and the Metal Creek copper prospect, both of which represent examples of porphyry copper-type mineralisation.  Jensen (1941) reported that traces of alluvial gold, and a thin gold-bearing quartz veins had been found in the granodiorite southwest of the Ruddygore mine.|16-MAY-23
23948|Ruddygore Granodiorite|Lithology|Grey, medium-grained, slightly porphyritic hornblende-biotite granodiorite is the dominant rock type.  Rounded inclusions of mafic granodiorite or diorite, up to 2 m in diameter (generally <15 cm) are locally abundant. The granodiorite consists mainly of a network of euhedral to subhedral plagioclase, biotite and hornblende grains which are partly enveloped by and poikilitically enclosed in irregular quartz and K-feldspar grains. Plagioclases range from 1 mm to 1.5 cm in length, and generally show well-developed polysynthetic twinning. Quartz grains commonly show slightly undulose extinction, and some K-feldspar grains contain inclusions of microperthitic albite(?). Hornblendes range from 0.5 to 8 mm in length, are commonly twinned, contain scattered small inclusions of plagioclase, quartz, opaque oxide and apatite, and are pleochroic from yellow-green to dark green or, more rarely, blue-green.  Some of the larger grains are partly rimmed and replaced by biotite.  Accessory minerals include apatite, zircon, opaque minerals, sphene, dark brown allanite, and tourmaline (as small needles in quartz and orthoclase).  The opaque oxide is mainly magnetite with exsolution lamellae of ilmenite; discrete ilmenite grains are rare (Richards, 1981).  The opaque oxides are commonly associated with the mafic minerals, particularly biotite.  Locally, e.g., at GR 2340 81117 and in the Ruddygore mine area, the Ruddygore Granodiorite contain miarolitic cavities up to 15 cm long and 8 cm wide.  At GR 2340 81117 some are filled with an outer layer of pale pink potassium feldspar and an inner zone of quartz, whereas in the Ruddygore mine area the cavities are filled or partly filled mainly with quartz crystals, commonly with minor associated calcite and malachite.  Vuggy quartz veins are also common in the granodiorite exposed in the Ruddygore mine area. ENCLAVES:: Xenoliths are of variable composition, but mafic granodiorite, diorite, or quartz diorite are by far the most common.  These have the same mineralogy as the host but the minerals are of finer grainsize and are present in different proportions.  Average grainsize ranges from 1 mm up to about 2 mm.  Plagioclases and mafic minerals tend to form a mesh of euhedral to subhedral grains poikilitically enclosed by relatively large, highly irregular quartz and K-feldspar grains.  Irregular quartz and K-feldspar grains also fill interstices.  Plagioclase and hornblende predominate in inclusions with relatively low quartz contents.  The mafic minerals occur mainly as discrete grains, rarely as aggregates of grains.  Accessory apatite, as fine needles, is relatively common, but zircon is reported to be rare (Richards, 1981).  Minor myrmekite is also present in some xenoliths.  Plagioclase grains are commonly partly replaced by sericite and minor muscovite, and biotite flakes by chlorite.|16-MAY-23
23948|Ruddygore Granodiorite|Relationships and boundaries|The granodiorite truncates the Chillagoe and Hodgkinson Formations, the Doolan Creek Rhyolite, the Redcap Dacite (Redcap Volcanics on the preliminary map), and Late Carboniferous units in the Featherbed Volcanics Group.  A knife-sharp intrusive contact between the Ruddygore Granodiorite and Jamtin Rhyolite (Featherbed Volcanic Group) is well exposed in the bed of Chillagoe Creek at Chillagoe.  Contacts between the granodiorite and the Early Permian Fisherman Rhyolite (Featherbed Volcanics Group) are faulted.  The granodiorite intrudes several unnamed stocks of mafic granodiorite or diorite (exposed mainly in the north) and is inferred to intrude the Almaden Granodiorite.  It is cut by the Bungabilly Granite, Pinchgut Granite, fine-grained porphyritic felsic intrusives of the Doolan Creek Ring Complex, by several unnamed stocks and dykes of aplite, leucogranite and leucoadamellite(?), by numerous rhyolite dykes, and by rare dykes and pods of dolerite (at least some of which is probably Cainozoic).  Small felsic intrusions are relatively common north and south of the Walsh River.|16-MAY-23
23948|Ruddygore Granodiorite|Age reasons|The Ruddygore Granodiorite has yielded isotopic (Rb-Sr biotite) ages ranging between 301 Ma and 302 Ma (Richards, 1981).|16-MAY-23
23948|Ruddygore Granodiorite|Comments|The Ruddygore Granodiorite closely resembles the Almaden Granodiorite and is one of the major units of the northern Tate batholith of Richards (1981).  According to Richards (1981) it is the most complex pluton in the batholith.|16-MAY-23
23948|Ruddygore Granodiorite|References|BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.BRANCH, C.D., 1966:  Volcanic cauldrons, ring complexes, and associated granites of the Georgetown Inlier, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 76.CHAPPELL, B.W., 1978:  Granitoids from the Moonbi district, New England Batholith, eastern Australia.  Journal of the Geological Society of Australia, 25, 267-283.DE KEYSER, F., & WOLFF, K.W., 1964:  The geology and mineral resources of the Chillagoe area.  Bureau of Mineral Resources, Australia, Bulletin 70.RICHARDS, D.N.G., 1981:  Granitoids of the northern Tate batholith, Chillagoe, north Queensland.  Ph.D. Thesis, James Cook University of North Queensland, Townsville (unpublished).|16-MAY-23
24481|Rundle Formation|Name source|Rundle Range; GR 296 000E 7 380 000N Gladstone 1:100 000 Sheet area.|16-MAY-23
24481|Rundle Formation|Unit history|Part of the Narrows Beds of Kirkegaard and others (1970).|16-MAY-23
24481|Rundle Formation|Type section locality|A composite section from 121 m to 254 m in RDD66 (GR 299 441E, 7 382 121N Gladstone 1:100 000 Sheet) and 90 m to 548 m in GSQ Rockhampton 2 (GR 313 210E, 7 363 665N Gladstone 1:100 000 Sheet area). GSQ Rockhampton 2 is located 23 km SE of RDD66. Correlation between drill holes is on the basis of lithology - confirmed by comparison of assay histograms for oil yield from oil shale beds.|16-MAY-23
24481|Rundle Formation|Extent|Subcrop in an area of about 150 km2 in The Narrows Graben, NW of Gladstone, Qld. Very sparse (mostly weathered) outcrops are present. It has been identified from drill hole core.|16-MAY-23
24481|Rundle Formation|Thickness range|591 m in type section (estimated true thickness 582 m with 10o dip of strata).|16-MAY-23
24481|Rundle Formation|Lithology|A kerogen-rich sequence of claystone that has been informally subdivided into six kerogenous seams and a claystone unit. There are minor limestone and carbonaceous to coaly shale beds. All six oil shale seams contain varying amounts of interbedded claystone, but the unit is dominantly claystone. The oil shale ranges from dark yellowish-brown through moderate yellowish-brown to olive-grey. It is moderately hard, sectile, silty in part and ranges from massive to shaly. It is sporadically calcareous. The claystone is dominantly dark greenish-grey to greyish blue, green, massive, and ranges from soft (puggy) to moderately hard. It is calcareous in part.|16-MAY-23
24481|Rundle Formation|Relationships and boundaries|Conformable with the informally named Worthington beds (below) and the Curlew Formation (above). The lower boundary of the Rundle Formation is the base of the lowermost oil shale bed in the type section. The upper boundary is gradational. The oil shale grades into carbonaceous oil shale over a stratigraphic interval up to 5 m thick at the base of a thick interbedded carbonaceous shale and grey claystone bed of the overlying Curlew Formation. The formation is faulted against Palaeozoic rocks (basement) at the western margin of The Narrows Graben.|16-MAY-23
24481|Rundle Formation|Age reasons|The Rundle Formation on megaspore evidence is middle to late Eocene (Foster and Harris, 1981). Olivine dolerite intruding the Rundle Formation has been dated at 26.8 m.y.|16-MAY-23
24481|Rundle Formation|Proposed publication|Bulletin of the American Association of Petroleum Geologists|16-MAY-23
24481|Rundle Formation|Comments|The drill core from RDD66 is currently stored in Southern Pacific Petroleum's core shed at Rundle. To be transferred at a later date to Southern Pacific Petroleum's core shed located in Gladstone, Qld.|16-MAY-23
24481|Rundle Formation|References|82/22438; 79/02402|16-MAY-23
24481|Rundle Formation|First Reference|82/22486|16-MAY-23
24481|Rundle Formation|Proposer|Henstridge D.A., Missen D.D.|16-MAY-23
26129|Saddington Tonalite|Name source|Saddington Block of Shield Creek Holding (Clarke River 4-Mile Cadastral Map).|16-MAY-23
26129|Saddington Tonalite|Unit history|The tonalite was previously mapped as part of the Gray Creek Complex (White, 1962, 1965; Arnold & Rubenach, 1976).  The name was first published by Withnall & others (1988) and described briefly, but not formally defined.|16-MAY-23
26129|Saddington Tonalite|Geomorphic expression|The unit crops out poorly, forming undulating topography with low relief.  It is difficult to distinguish from the surrounding Gray Creek Complex and Donaldsons Well Volcanic Member, except for exhibiting slightly paler tones on aerial photographs.|16-MAY-23
26129|Saddington Tonalite|Type section locality|At 7859 780770, at the head of a small tributary of Horse Creek, where grey, medium, equigranular hornblende tonalite crops out.  The grid reference is based on the AGD66 datum.|16-MAY-23
26129|Saddington Tonalite|Extent|Between Crooked and Horse Creeks straddling the Greenvale Broken River road about 20 km2 in area.|16-MAY-23
26129|Saddington Tonalite|Lithology|Grey, medium grained, equigranular hornblende tonalite, quartz diorite, and diorite.|16-MAY-23
26129|Saddington Tonalite|Relationships and boundaries|The Saddington Tonalite intrudes the Gray Creek Complex and Donaldsons Well Volcanic Member, and is intruded by numerous mafic dykes.|16-MAY-23
26129|Saddington Tonalite|Age reasons|Ordovician to Early Silurian from relationships.|16-MAY-23
26129|Saddington Tonalite|References|ARNOLD, G.O. & RUBENACH, M.J., 1976:  Mafic-ultramafic complexes of the Greenvale area, north Queensland.  Devonian intrusions or Precambrian metamorphics?  Journal of the Geological Society of Australia, 23, 119-139. **WHITE, D.A., 1962:  Clarke River 1.250 000 Geological series.  Bureau of Mineral Resources, Australia, Explanatory Notes, E/55-13. **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5|16-MAY-23
23953|Saint Giles Volcanics|Name source|The name is derived from the Parish of Saint Giles, County of Wilkie Gray.|16-MAY-23
23953|Saint Giles Volcanics|Unit history|Rocks of the Saint Giles Volcanics were previously included in the "Unnamed Acid Volcanics" (Cuv) of Wyatt & others (1970). Curent mapping has assigned other parts of this unit to the Tareela Volcanics, Carboniferous to Permian intrusive rhyolites and the Watershed North Rhyolite|16-MAY-23
23953|Saint Giles Volcanics|Type section locality|The type area is in the headwaters of the Little Star River upstream from 8159-247784 on the North Branch and 8159-271772 on the South Branch.  The grid reference is based on the AGD66 datum.|16-MAY-23
23953|Saint Giles Volcanics|Description at type locality|Outcrop in this area consists of moderately crystal-rich to crystal-rich, moderately lithic-rich rhyolitic ignimbrite and tuff and minor slightly porphyritic rhyolite.|16-MAY-23
23953|Saint Giles Volcanics|Extent|The Saint Giles Volcanics crop out along the Paluma Range from just north of Thornton Gap to Mount Halifax, about 27km to the north. The area also includes various plutons which have intruded the volcanic rocks. Scattered outcrop also occurs to the northwest, arcing across the upper reaches of the Star River.|16-MAY-23
23953|Saint Giles Volcanics|Thickness range|The thickness of the Saint Giles Volcanics is very difficult to determine because of lack of information due to inaccessibility and dense rainforest cover. Dips measured in the headwaters of Little Star and Star Rivers suggest that the unit comprises moderately dipping sheets. This information and the fact that the unit crops out from near sea level to the top of the Paluma Range puts its thickness at over 1000m and possibly up to 3500 m.|16-MAY-23
23953|Saint Giles Volcanics|Lithology|The Saint Giles Volcanics consist of grey to dark grey, crystal-poor to crystal-rich, lithic-poor to moderately lithic-rich dacitic to rhyolitic ignimbrite and minor lapilli breccia and flow-banded, spherulitic, slightly to moderately porphyritic rhyolite. The rhyolites are probably equivalent to some of the felsic intrusions which have been mapped throughout the area. Because of poor access and thick forest cover, boundaries of the felsic intrusions could not be delineated, and these rocks were included in the Saint Giles Volcanics.  The dominant rock type of this unit is a dacitic to rhyolitic ignimbrite. Crystal and lithic content covers a wide range. Given the diverse range of crystal, lithic and fiamme content the unit undoubtedly comprises different ignimbrite sheets. However, due to poor access and thick rainforest cover these sheets have not been delineated. Overall the Saint Giles Volcanics contain more lithics and less crystals than the Paluma Rhyolite.|16-MAY-23
23953|Saint Giles Volcanics|Relationships and boundaries|The Saint Giles Volcanics are intruded by numerous Carboniferous to Permian granite and rhyolite bodies including the Clemant Microgranite (337±6 Ma) and unnamed granite. They are faulted against and unconformably overlie Proterozoic and early Palaeozoic metamorphics and granitoids. Rocks in the Bog Hollow Pocket area may be equivalent to upper subunits of the Tareela Volcanics. Dips in the Blue Gum Creek area suggest that the unit is overlain by the Paluma Rhyolite.|16-MAY-23
23953|Saint Giles Volcanics|Age reasons|The stratigraphic position and intrusive relationships of the Saint Giles Volcanics suggest an Early Carboniferous age.|16-MAY-23
23953|Saint Giles Volcanics|References|WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127.|16-MAY-23
27230|Saint James Volcanics|Unit history|The name "Saint James Volcanics" was first used by Wyatt & others (1970).  The Saint James Volcanics were included in the Glenrock Group by Hutton & others (1994).|16-MAY-23
27230|Saint James Volcanics|Constituents|Our mapping has subdivided the Saint James Volcanics into five unassigned units (Cs1, Cs2, Cs3, Cs4, Cs5) that crop out in the north-west corner of the Parish of Saint James.|16-MAY-23
27230|Saint James Volcanics|Type section locality|Wyatt & others (1970) did not give a type section for the Saint James Volcanics. A type section is herein designated across the western limb of the syncline between 8159-253536 and 268540, and thence along a gully, which trends approximately in the same direction as the fold hinge, to its headwaters at the boundary with the Watershed Rhyolite at 282547.  The grid references are based on the AGD66 datum.|16-MAY-23
27230|Saint James Volcanics|Description at type locality|From the base upwards the section consists of the following informal units: - about 50m of dark grey, mainly aphyric basalt (porphyritic at the base) (Cs1); - about 50m of coarse to pebbly, volcaniclastic sandstone (Cs2); - about 200m of cream, rhyolitic breccia (Cs3); - about 200m of dark grey, aphyric, amygdaloidal basalt and basaltic breccia (Cs4); - about 1000m of pale green, moderately crystal and lithic-rich rhyolitic ignimbrite, aphyric and spherulitic flow-banded rhyolite and dark green, crystal and lithic-rich rhyolitic lapilli breccia (Cs5).|16-MAY-23
27230|Saint James Volcanics|Extent|The two basaltic units, Cs1 and Cs4, are recessive forming low dark soil country, vegetated by good grass cover and narrow leaf ironbarks. The felsic units are more resistant, particularly the breccia unit (Cs3) which forms a low ridge along the western limb of the syncline. Vegetation cover is poor consisting of less grass than over the basic units and stunted, broad-leaf ironbarks.|16-MAY-23
27230|Saint James Volcanics|Thickness range|The Saint James Volcanics are estimated to be approximately 1500m thick in the type section. The constituent units vary considerably in thickness along strike.|16-MAY-23
27230|Saint James Volcanics|Lithology|Five informal units have been recognised in the Saint James Volcanics as described in the type section. The lowest unit Cs1 is composed of a dark grey, mainly aphyric basalt, that is locally porphyritic, particularly at the base.  Cs2 consists of grey to pale green coarse to pebbly volcaniclastic sandstone, chert and rhyolitic breccia. The volcaniclastic sandstone contains felsic volcanic pebbles which tend to be fissile and are commonly imbricated. Local very thin to thin internal bedding has been noted but overall bedding is thick to very thick.  Unit Cs3 is a cream to pale pink, rhyolitic breccia.   Cs4 comprises dark grey, aphyric to abundantly porphyritic basalt and basaltic autobreccia. The aphyric basalt is locally amydaloidal.  The uppermost unit (Cs5) consists predominantly of pale green to grey, moderately crystal-rich to crystal-rich and lithic-rich rhyolitic lapilli breccia and ignimbrite. Minor porphyritic, spherulitic, flow-banded rhyolite and felsic volcanic breccia are also present.|16-MAY-23
27230|Saint James Volcanics|Relationships and boundaries|On their western margin the Saint James Volcanics disconformably overlie the Devonian to Early Carboniferous Keelbottom Group. Along the eastern and southern margins the formation has been intruded by Carboniferous to Permian rhyolite, whereas to the north it is unconformably overlain by the Watershed Rhyolite of probable Carboniferous age.|16-MAY-23
27230|Saint James Volcanics|Age reasons|Because of their stratigraphic position and lithological similarities to other known Early Carboniferous volcanics in the Townsville hinterland, the Saint James Volcanics have been assigned to the Early Carboniferous.|16-MAY-23
27230|Saint James Volcanics|References|*HUTTON, L.J., DRAPER, J.J., GUNTHER, M.C., WITHNALL, I.W. & LOCKHART, D.A., 1994: Glenrock Group; in DRAPER, J.J. & LANG, S.C. (Editors), Geology of the Devonian to Carboniferous Burdekin Basin. Queensland Geological Record 1994/9.    *WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127|16-MAY-23
24485|Saint Mungo Granite|Name source|Named after Saint Mungo copper mine, GR 808080. Dajarra 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24485|Saint Mungo Granite|Unit history|Previously mapped as part of the Kalkadoon Granite (Carter & Opik, 1963).|16-MAY-23
24485|Saint Mungo Granite|Type section locality|The vicinity of Saint Mungo mine, GR 808080, Dajarra 1:100 000 Sheet area. Here pinkish richly porphyritic gneissic granite forms rocky hills, tors, and spheroidal boulders.|16-MAY-23
24485|Saint Mungo Granite|Extent|Outcrops trend NNW and cover about 90 km2 in the vicinity of The Monument and to the N, in E part of Dajarra 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24485|Saint Mungo Granite|Lithology|Consists mainly of weakly to strongly foliated, medium to coarse-grained, hornblende-biotite granite crowded with pink equant megacrysts of microcline up to 3 cm across. Also includes minor foliated porphyritic biotite granite, aplite, and quartz-feldspar pegmatite.|16-MAY-23
24485|Saint Mungo Granite|Relationships and boundaries|The granite is inferred to intrude Plum Mountain Gneiss and Corella Formation. It is cut by mafic dykes and overlain by flat-lying Cambrian sediments.|16-MAY-23
24485|Saint Mungo Granite|Age reasons|Proterozoic|16-MAY-23
24485|Saint Mungo Granite|Proposed publication|R233|16-MAY-23
24485|Saint Mungo Granite|Comments|Saint Mungo Granite is geographically separated and petrographically different from other named granites in Dajarra 1:100 000 Sheet area. It may be related to part of the Bushy Park Gneiss of Duchess 1:100 000 Sheet area.|16-MAY-23
24485|Saint Mungo Granite|References|R233; 98/29253|16-MAY-23
24485|Saint Mungo Granite|Proposer|Blake D.H., Donchak P.J.T.|16-MAY-23
24486|Saint Ronans Metamorphics|Name source|Named after Saint Ronans Creek whose tributaries drain much of the outcrop area in the Ardmore 1:100 000 Sheet area, Urandangi 1:250 000 Sheet area.|16-MAY-23
24486|Saint Ronans Metamorphics|Unit history|Mapped as Eastern Creek Volcanics by Noakes & others (1959).|16-MAY-23
24486|Saint Ronans Metamorphics|Type section locality|From GR 170860 to GR 209857, at the head of Saint Ronans Creek-Wet Branch, about 9.5-13 km W of Steeles Tank. In this area the unit consists mainly of extensively recrystallised felsic metavolcanics, fine-grained schistose metabasalt, fine-grained quartz + muscovite (or sericite) +/- biotite schist, and quartz + biotite + feldspar + muscovite gneiss. Minor rock types present include quartzite, epidotic quartzite, and quartzose and sericitic meta-arenite.|16-MAY-23
24486|Saint Ronans Metamorphics|Extent|The metamorphics are most extensively exposed in the central part of the Ardmore 1:100 000 Sheet area, S and E of Ardmore homestead. A small outcrop in the far N of the sheet area has also been tentatively assigned to this unit. The metamorphics are confined to the area W of the Rufus Fault Zone, which forms part of a major right-lateral fracture system extending to the SW and NNE (the Gorge Creek-Mount Remarkable Fault of Derrick & others, 1980).|16-MAY-23
24486|Saint Ronans Metamorphics|Lithology|The rocks are generally as in the type area. Locally andalusite porphyroblasts are common in the schistose meta-argillites. Minor rock types present elsewhere include biotite schist, quartz-biotite schist locally containing small scattered muscovite porphyroblasts, muscovite quartzite, para-amphibolite, chlorite schist, and schistose micaceous metasiltstone. Small-scale cross-beds and ripple laminations are preserved in some meta-arenite units. The Saint Ronans Metamorphics have a generally steeply dipping foliation trending mainly N to NW, more or less parallel to the lithological layering; small crenulations and kink bands are common, but few major folds have been positively identified. In the S, about 6 km NNW of Rufus Tank (GR 202786), foliation and rare bedding have easterly trends, dip generally steeply southwards, and are cut by a prominent N-trending cleavage.|16-MAY-23
24486|Saint Ronans Metamorphics|Relationships and boundaries|The metamorphics are intruded by veins, pods, and larger bodies of granite and pegmatitic granite and by swarms of pegmatite dykes, interpreted as part of the Sybella Granite batholith. They are also cut by numerous non-schistose to schistose amphibolitic metadolerite dykes and ?sills, some of which are cut by granite and pegmatite veins. The relationship between the Saint Ronans Metamorphics and Oroopo Metabasalt is uncertain, due largely to poor exposures. The two formations appear concordant and no major break has been recognised between them. Cross-beds in a S-dipping meta-arenite unit in the Oroopo Metabasalt at GR 126763 indicate that the beds are right way up and younging southwards. Rare cross-beds in the Saint Ronans Metamorphics adjacent to the contact indicate that this sequence is also right way up, and underlies the Oroopo Metabasalt.|16-MAY-23
24486|Saint Ronans Metamorphics|Age reasons|Precambrian, probably Proterozoic.|16-MAY-23
24486|Saint Ronans Metamorphics|Proposed publication|R233|16-MAY-23
24486|Saint Ronans Metamorphics|Comments|The general obliteration of bedding, the widespread development of schistose rocks, the presence of andalusite porphyroblasts in some meta-argillites, and the extensive recrystallisation of the felsic and mafic volcanic rocks are interpreted as indicating mainly upper greenschist to possible middle amphibolite grades of regional metamorphism. Metamorphic grade appears to decrease to the south.|16-MAY-23
24486|Saint Ronans Metamorphics|References|R233; J0503/04|16-MAY-23
24488|Sawpit Granodiorite|Name source|Sawpit Creek (also known as Styx River) which joins the Gilbert River at GR 071 688 (Gilberton 1:100 000 Sheet area). The name Sawpit has been used as part of a lithostratigraphic name in New South Wales ("Sawpit Gully Member, Thompson, 1976). The New South Wales unit was clearly meant to be an informal one.|16-MAY-23
24488|Sawpit Granodiorite|Unit history|Previously included in the Dumbano Granite by White (1962).|16-MAY-23
24488|Sawpit Granodiorite|Type section locality|On Christmas Hill (also known as Duffer) Creek at GR 088 778 about 7.5 km west-northwest of Bagstowe homestead. There the unit is a well foliated biotite granodiorite containing biotite rich bands about 1 cm wide and over 5 m long, as well as wider (about 10 cm) more leucocratic layers and streaks; discordant leucocratic veins cut across the layering and the abundant xenoliths of gneiss. Tight folds which deform the foliation in the xenoliths also deform the layering in the granodiorite and the discordant veins. Outcrops of grey biotite granodiorite containing abundant xenoliths of calc-silicate gneiss at GR 073 686 in the Gilbert River can be regarded as a reference locality.|16-MAY-23
24488|Sawpit Granodiorite|Extent|Crops out over an area of about 15 km2 in two main areas; one is centred near the junction of Sawpit and Christmas Hill (or Duffer) Creeks (grid square 0975) and the other extends for about a kilometre upstream along the Gilbert River from its junction with Sawpit Creek.|16-MAY-23
24488|Sawpit Granodiorite|Lithology|Grey equigranular, medium grained, foliated biotite granodiorite, tonalite and quartz diorite. Commonly banded as well as foliated, as described at the type locality. Enclaves of Einasleigh Metamorphics ranging from a few centimetres to hundreds of metres are common.|16-MAY-23
24488|Sawpit Granodiorite|Relationships and boundaries|Intrudes the Proterozoic Einasleigh Metamorphics. Intruded by white leucogranite equated with the Anning Granite and muscovite granite equated with the Digger Creek Granite, as well as ring dykes and cone sheets which form part of the Carboniferous Bagstowe Ring Dyke Complex.|16-MAY-23
24488|Sawpit Granodiorite|Age reasons|Mid-Proterozoic; strongly foliated and deformed during the second major deformation in the area which has been dated at about 1470 m.y. (Black & others, 1979).|16-MAY-23
24488|Sawpit Granodiorite|Proposed publication|80/20649|16-MAY-23
24488|Sawpit Granodiorite|References|80/20677; 79/04313;|16-MAY-23
24488|Sawpit Granodiorite|Proposer|Bain J.H.C., Withnall I.W.|16-MAY-23
26324|Saxby Granite|Name source|Named after Saxby Waterholes on the Williams River at GR 789691, Mount Angelay 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
26324|Saxby Granite|Unit history|Like all other granites in the eastern part of the Duchess 1:250 000 Sheet area, the Saxby Granite was mapped as part of the Williams Granite by Carter & Opik (1963).|16-MAY-23
26324|Saxby Granite|Type section locality|Vicinity of Saxby Waterholes on the Williams River, GR 789691, Mount Angelay 1:100 000 Sheet area, Duchess 1:250 000 Sheet area. Here there are extensive exposures - rocky hills, tors and spheroidal boulders - of pink, medium to coarse, porphyritic biotite granite.|16-MAY-23
26324|Saxby Granite|Extent|The main outcrops of this unit are in the northern part of Mount Angelay 1:100 000 Sheet area, mainly in the catchment area of the Williams River east of the Cloncurry Fault, where they cover a total area of about 180 km2. The unit is also taken to include small outcrops of petrographically similar granite east of the Cloncurry Faualt to the south, between the Fullarton River and Boorama Creek, Mount Angelay 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
26324|Saxby Granite|Lithology|The unit consists mainly of medium to coarse, porphyritic and even-grained granite containing biotite and/or hornblende (and clinopyroxene near contacts with calc-silicate rocks). It also includes minor leucogranite, granodiorite, diorite, monzonite, aplite and pegmatite.|16-MAY-23
26324|Saxby Granite|Relationships and boundaries|Saxby Granite intrudes the Soldiers Cap Group and Doherty Formation, and is cut by E-trending dolerite dykes. It is overlain unconformably by Mesozoic sediments.|16-MAY-23
26324|Saxby Granite|Age reasons|Proterozoic|16-MAY-23
26324|Saxby Granite|Proposed publication|R233|16-MAY-23
26324|Saxby Granite|Comments|The granite forms a group of closely spaced intrusives separated geographically from other named granites in the area by the Cloncurry Fault zone. It forms part of the Williams Batholith (new structural term), and is probably related to the petrographically similar Mount Angelay Granite and Squirarel Hills Granite.|16-MAY-23
26324|Saxby Granite|References|98/29253, R233|16-MAY-23
26324|Saxby Granite|Proposer|Donchak P.J.T.|16-MAY-23
37737|Schultz Sandstone Member|Name source|From Schultz Creek, whose confluence with the Nicholson River is at latitude longitude , in WESTMORELAND.|16-MAY-23
37737|Schultz Sandstone Member|Unit history|Previously undifferentiated from the remainder of the Constance Sandstone on the first editions of LAWN HILL (Carter & Öpik 1959), WESTMORELAND (Carter 1959), CALVERT HILLS (Roberts et al 1963), and MOUNT DRUMMOND (Smith and Roberts 1963). Distinguished as  LP sc3, and LP sc4 on the second editions of LAWN HILL  - Hutton & Grimes (1983), WESTMORELAND  - Grimes & Sweet (1979), and CALVERT HILLS  -  Ahmad & Wygralak (1989), following the scheme of Sweet et al (1981), who designated the undifferentiated sandstones of the Constance Sandstone LP sc1, LP sc2, LP sc3, and LP sc4, during mapping of the Seigal and Hedleys Creek 1:100 000 sheet areas. The Bowthorn Siltstone Member, which was identified as LP sc3 by Sweet et al (1981) is now obsolete, as it has been absorbed into the Schultz Sandstone Member.|16-MAY-23
37737|Schultz Sandstone Member|Geomorphic expression|In areas of low dip forms extensive rocky plateaux, commonly with pseudokarstic weathering surfaces; in rarer steeply dipping outcrops forms a banded rocky ridge. The basal beds are massive, and form striking bare rocky platforms cut by deeply eroded joints.|16-MAY-23
37737|Schultz Sandstone Member|Type section locality|South of Bowthorn homestead, in northwestern LAWN HILL. Base of section is accessed from a station track leading south from Accident Creek. Base is at Latitude 18deg9' 7"S Longitude 138deg21' E (219620E 7990970N), thence 5.9 km to the top of a siltstone interbed at Latitude 18deg8' 39" S Longitude 138deg17' 43" E (213820E 7991770N), then a further 9.9 km to the top, at Latitude 18deg9' 55"S Longitude 138deg12' 16"E (204230E 7989270N)South of Bowthorn homestead, in northwestern LAWN HILL. Base of section is accessed from a station track leading south from Accident Creek. Base is at Latitude 18deg9' 7"S Longitude 138deg21' E (219620E 7990970N), thence 5.9 km to the top of a siltstone interbed at Latitude 18deg8' 39"S Longitude 138deg17'43"E (213820E 7991770N), then a further 9.9 km to the top, at Latitude 18deg9' 55"S Longitude 138deg12' 16"E (204230E 7989270N). REFERENCE SECTION: Adjacent to but southwest of Gorge Creek, from 190600E 8012800N (base) to 190700E 8012050 (top), in southwestern WESTMORELAND. The uppermost beds are faulted out, but the section provides a geographically compact section of most of the Member.|16-MAY-23
37737|Schultz Sandstone Member|Extent|Crops out north of Elizabeth Creek in northern LAWN HILL, and south of Hedleys Creek, in southwestern WESTMORELAND, and in adjacent parts of southeastern CALVERT HILLS and northeast and northern MOUNT DRUMMOND.|16-MAY-23
37737|Schultz Sandstone Member|Thickness range|140-300 m in the type section, depending on the dip assumed (actual dips range from 1-5 degrees); at least 500 m thick in the reference section.|16-MAY-23
37737|Schultz Sandstone Member|Lithology|Basal beds are massive outcrop of yellow to white, subfriable medium- to coarse-grained, well-sorted quartz sandstone; some granule layers present. Sandstone becomes medium-grained up-section. Very pure medium-grained quartz sandstone with siliceous cement continues virtually to top of formation. Cross-bedded throughout.|16-MAY-23
37737|Schultz Sandstone Member|Depositional environment|Marine shelf, ranging from very shallow, intertidal for the sandstone members, to deeper, storm-dominated shelf for the siltstone members.|16-MAY-23
37737|Schultz Sandstone Member|Relationships and boundaries|The lower boundary, with the Wallis Siltstone Member, is sharp but apparently conformable, and the upper contact, with the Mullera Formation, is sharp but conformable. In northern Mount Drummond the Member truncates the Wallis Siltstone Member to lie disconformably or with subtle angular unconformity on the Burangoo Sandstone Member.|16-MAY-23
37737|Schultz Sandstone Member|Age reasons|The interpreted age range for the whole South Nicholson Group, of 1500 1400 Ma, is based on its correlation with the Roper Group of the southern McArthur Basin (Dunn et al 1966) with which it makes up the Roper Superbasin (Jackson et al 1999, Abbott and Sweet 2000, Abbott et al 2001). Ages of 1492±4 and 1493±4 Ma for tuffaceous material from the lower Roper Group (Jackson et al 1999) provides the most reliable estimate for the age of that Group, and hence for the South Nicholson Group. The age of the Schultz Sandstone Member is judged to lie near the middle of this age range.|16-MAY-23
37737|Schultz Sandstone Member|Correlations|None known, but it is likely that a sandstone unit/s in the middle Renner Group (Hussey et al 2001) and the Roper Group (Jackson et al 1999) are in part correlative, given the overall correlation between these groups.|16-MAY-23
37737|Schultz Sandstone Member|Defn author|Ian Sweet, May 2006|16-MAY-23
37737|Schultz Sandstone Member|Comments|The Schultz Sandstone Member incorporates the now obsolete Bowthorn Siltstone Member of Sweet (1981). The obsolete member consisted of at least two thin lenses within the newly defined (Schultz) member in its type area and further north, in WESTMORELAND. Because these 'siltstones' include a substantial proportion of very fine-grained sandstone and several coarser sandstone interbeds, and because the new Schultz Sandstone Member consists entirely of sandstone in most of its outcrops, the lithology term 'sandstone' is incorporated into the name.|16-MAY-23
37737|Schultz Sandstone Member|References|**ABBOTT S.T. and Sweet I.P. 2000. Tectonic control on third-order sequences in a siliciclastic ramp-style basin: an example from the Roper Superbasin (Mesoproterozoic), northern Australia. Australian Journal of Earth Sciences, 47, 637-657.  **ABBOTT S.T., Sweet I.P., Plumb K.A., Young D.N., Cutovinos A., Ferenczi P.A., Brakel A. and Pietsch B.A., 2001. Roper region: Urapunga and Roper River special, Northern Territory (Second Edition); 1:250 000 Geological Map Series, sheets SD53-10,11. Northern Territory Geological Survey-Australian Geological Survey Organisation (NGMA), Map and Explanatory Notes.  **AHMAD M. and Wygralak A.S., 1989. Calvert Hills, Northern Territory (First Edition); 1:250 000 Metallogenic Map Series, sheet SE53-8. Northern Territory Geological Survey, Map and Explanatory Notes.  **CARTER E.K., 1959. Westmoreland, Queensland (First Edition); 1:250 000 Geological Series, sheet SE54-5. Bureau of Mineral Resources, Geology and Geophysics, Map and Explanatory Notes.  **CARTER E.K. and Öpik A.A., 1959. Lawn Hill, Queensland (First Edition); 1:250 000 geological series, sheet SE54-9. Bureau of Mineral Resources, Geology and Geophysics, Map and Explanatory Notes.  **DUNN P.R., Plumb K.A. and Roberts H.G. 1966. A proposal for time-stratigraphic subdivision of the Australian Precambrian. Journal of the Geological Society of Australia, 13, 593-608.  **GRIMES K.G. & Sweet I.P. 1979. Westmoreland, Queensland (Second Edition); 1:250 000 Geological Map Series, sheet SE54-5. Bureau of Mineral Resources, Geology and Geophysics, Map and Explanatory Notes.  **HUSSEY K.J., Beier P.R., Crispe A.J., Donnellan N. and Kruse P.D. 2001. Helen Springs, Northern Territory (Second Edition); 1:250 000 geological series, sheet SE53-10.  **HUTTON L.J. & Grimes K.G. 1983. Lawn Hill, Queensland (Second Edition); 1:250 000 geological series, sheet SE54-9. Geological Survey of Queensland, Geological Map.  **JACKSON M.J., Sweet I.P., Page R.W. and Bradshaw B.E., 1999. The South Nicholson and Roper Groups: evidence for the early Proterozoic Roper Superbasin. In: Bradshaw B.E. and Scott D.L. (Eds.), Integrated basin analysis of the Isa Superbasin using seismic, well-log and geopotential data: an evaluation of the economic potential of the northern Lawn Hill Platform. Australian Geological Survey Organisation, Record 1999/19 (unpaginated).  **ROBERTS H.G., Rhodes J.M. and Yates K.R., 1963. Calvert Hills, N.T. (First Edition); 1:250,000 geological series, sheet SE53-8. Bureau of Mineral Resources, Geology and Geophysics, Map and Explanatory Notes.  **SMITH J.W. and Roberts H.G., 1963. Mount Drummond, N.T. (First Edition); 1:250,000 geological series, sheet SE53-12. Bureau of Mineral Resources, Geology and Geophysics, Map and Explanatory Notes.  **SWEET I.P., 1981. Definitions of new stratigraphic units in the Seigal and Hedleys Creek 1:100 000 Sheet areas, Northern Territory and Queensland. Bureau of Mineral Resources, Geology and Geophysics, Report 225; BMR Microform MF150.|16-MAY-23
37737|Schultz Sandstone Member|Parent|Constance Sandstone, Accident Subgroup, South Nicholson Group.|16-MAY-23
23960|Scurvy Creek Meta-arenite|Name source|Scurvy Creek, which joins Sandy Creek at 8352-488865.|16-MAY-23
23960|Scurvy Creek Meta-arenite|Unit history|Previously mapped as Anakie Metamorphics (Malone & others, 1964; Veevers & others, 1964a, b) and now part of the Anakie Metamorphic Group.|16-MAY-23
23960|Scurvy Creek Meta-arenite|Geomorphic expression|The Scurvy Creek Meta-arenite forms undulating topography which tends to be slightly more recessive and less densely wooded than the adjacent quartzite dominated Bathampton Metamorphics and Hurleys Metamorphics. In places it has a slightly reddish colour on aerial photographs and a pinkish colour on the images from Landsat 5 TM bands 1-4-7 (BGR). This probably reflects a more Fe-rich chemistry, manifest by the greater abundance of chlorite in the rocks.    The rocks have a low magnetic response similar to most of the other metasedimentary units. The radiometric response is not particularly distinctive with respect to the surrounding units, although it has a slightly lower total count than the Bathampton Metamorphics .|16-MAY-23
23960|Scurvy Creek Meta-arenite|Type section locality|Along the Blair Athol road from 8452-581869 to 540873.  The grid references are based on the AGD66 datum.|16-MAY-23
23960|Scurvy Creek Meta-arenite|Description at type locality|Greenish to purple or brown, labile meta-arenite, commonly showing a strong differentiated layering and tight folds is the dominant rock type. Minor more pelitic rocks (phyllite) are also present. The unit is bounded at both ends of the section by rocks assigned to the Hurleys Metamorphics from which they are distinguished by the dominance of the labile meta-arenite rather than more quartzose meta-arenite (quartzite) and phyllite. The nature of the boundaries is uncertain, but it is possible that at least one, if not both, is tectonic.|16-MAY-23
23960|Scurvy Creek Meta-arenite|Extent|Crops out as two parallel belts, each up to 4 km wide and separated by a belt of Hurleys Metamorphics up to 5 km wide. The unit has been traced for about 25 km from the Brigalow Creek area near the northern edge of MONTEAGLE, southeast to the Laglan and Blair Athol roads.|16-MAY-23
23960|Scurvy Creek Meta-arenite|Lithology|Dominated by schistose, relatively labile meta-arenite and subordinate phyllite or fine-grained mica schist. The meta-arenite is pale green when fresh, weathering to pale purple or brown. It is generally very fine to medium-grained, and only rarely coarse-grained. The metamorphic grade is greenschist facies (chlorite to biotite zone).|16-MAY-23
23960|Scurvy Creek Meta-arenite|Relationships and boundaries|The Bathampton Metamorphics structurally overlie the Scurvy Creek Meta-arenite to the west. The nature of this contact is uncertain, but could be a thrust, particularly if the Scurvy Creek Meta-arenite is equivalent to the Wynyard Metamorphics. The Hurleys Metamorphics structurally underlie the Scurvy Creek Meta-arenite to the east, the same relationship as between the Wynyard Metamorphics and Monteagle Quartzite. However, another belt of Scurvy Creek Meta-arenite lies to the east of the Hurleys Metamorphics, apparently underlying them structurally. This could be due to thrust repetition or an overturned F2 antiform, of which the Hurleys Metamorphics represent the core. The Hurleys Metamorphics crop out farther east of the second belt, again due to either thrust repetition or an F2 synform.   The Scurvy Creek Meta-arenite is unconformably overlain by Permian sedimentary rocks of the Moorlands and Blair Athol Basins, Tertiary basalt, and unassigned Cainozoic superficial deposits.|16-MAY-23
23960|Scurvy Creek Meta-arenite|Age reasons|The original age is still uncertain, but is probably Early Cambrian or Neoproterozoic.|16-MAY-23
23960|Scurvy Creek Meta-arenite|References|MALONE, E.J., CORBETT, D.P.W., & JENSEN, A.R., 1964: Geology of the Mount Coolon 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 64. **VEEVERS, J.J., RANDAL, M.A., MOLLAN, R.G., & PATEN, R.J., 1964a: The geology of the Clermont 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report, 66. **VEEVERS, J.J., MOLLAN, R.G., OLGERS, F., & KIRKEGAARD, A.G., 1964b: The geology of the Emerald 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 68.|16-MAY-23
22830|Sentinel Range Igneous Complex|Name source|The unit forms the northern part of the Sentinel Range, a series of northwesterly-trending low hills ~12 - 23 km northwest of Chillagoe.|16-MAY-23
22830|Sentinel Range Igneous Complex|Unit history|The complex was previously mapped as Elizabeth Creek Granite (Best, 1962;  de Keyser & Wolff, 1964).|16-MAY-23
22830|Sentinel Range Igneous Complex|Geomorphic expression|The unit forms bouldery hilly terrain which has pale to medium tones on aerial photographs.|16-MAY-23
22830|Sentinel Range Igneous Complex|Type section locality|The proposed type area is from ~GR 2180 81172 to ~GR 2297 81173.  Most of the variants are exposed in this area.  The grid reference is based on the AGD66 datum.|16-MAY-23
22830|Sentinel Range Igneous Complex|Extent|The complex crops out as an elongate, northwest-trending body of ~2 km2, extending 4 - 7 km northwest of the abandoned mining centre of Mungana.|16-MAY-23
22830|Sentinel Range Igneous Complex|General description|ALTERATION: The micro-adamellite has been extensively altered locally (e.g., south of Red Hill) and epidote/clinozoisite is common along joints.  MINBERALISATION: No mineralisation was observed, apart from traces of pyrite or altered pyrite(?).  The complex may have been responsible for the metasomatic, skarn-type, Cu-Sn mineralisation in the calcareous sediments of the adjacent Chillagoe Formation at Red Hill.  The mineralised rocks consist mainly of magnetite/hematite/jarosite, chalcedony and vuggy quartz.  Banding is commonly well developed and quartz grains show comb structures indicating that they grew in open spaces.  Chalcedony pseudomorph after zoned garnet megacrysts are present locally, but the relict structures and textures are generally poorly preserved adjacent to the complex.  The host rocks, probably mainly magnetite-garnet-diopside skarn, appear to have been extensively brecciated.  The brecciation may have been produced by supergene weatherin.|16-MAY-23
22830|Sentinel Range Igneous Complex|Lithology|The complex consists of white to pale pink porphyritic micro-adamellite, even-grained to porphyritic quartz diorite, heterogeneous hybrid rocks, and minor medium to coarse-grained porphyritic adamellite, aplite, and pegmatite.  The felsic granitic rocks which make up most of the complex show considerable textural and compositional variation.  Euhedral to subhedral phenocrysts make up to ~40% of the porphyritic/micro-adamellite.  They consist of quartz, plagioclase, K-feldspar, and minor biotite, hornblende, allanite, opaque oxide, and zircon.  Quartz and feldspar phenocrysts tend to form glomeroporphyritic aggregates.  Quartz phenocrysts are up to 6 mm across.  They show slightly undulose extinction and some have embayed margins.  Plagioclase is generally the most abundant phenocryst present.  The laths, up to 6 mm long, commonly show well-developed compositional zoning.  Cores contain inclusions of hornblende, biotite and quartz, and cloudy zones or patches due to incipient preferential alteration.  Some grains are partly replaced by sericite but the degree of alteration is generally only slight.  K-feldspar phenocrysts are up to 12 mm long and appear mainly unaltered.  Some of the larger grains contain inclusions of plagioclase and show slight zoning.  Biotite makes up to ~5% of the micro-adamellite, but is irregularly distributed throughout the felsic rocks of the complex.  Hornblende forms euhedral to subhedral grains, up to about 0.5 mm across, and small aggregates of subhedral to anhedral grains.  It is generally subordinate to biotite and is absent in some specimens. Accessory minerals are mainly opaque oxide, allanite, and zircon.  More felsic, microgranitic variants in the complex contain few (<5%) or no phenocrysts and tend to be concentrated in marginal zones.  The mafic rocks occur as small pods and also as irregular, angular to rounded fragments, ranging from <2 cm to 1 m across, enclosed in and veined by adamellite.|16-MAY-23
22830|Sentinel Range Igneous Complex|Relationships and boundaries|The complex intrudes the Chillagoe Formation and Dargalong Metamorphics.  It also truncates the Palmerville Fault.|16-MAY-23
22830|Sentinel Range Igneous Complex|Age reasons|The unit is Late Carboniferous.  Biotite from a sample of porphyritic micro-adamellite has yielded an isotopic age of 303 ± 2 Ma using the K-Ar method (Amdel report GS 4840/83).|16-MAY-23
22830|Sentinel Range Igneous Complex|Comments|The striking textural and compositional variations shown by the rocks of the complex appear to have resulted mainly from the mingling of mafic and felsic magmas.  Much of the complex consists of porphyritic micro-adamellite with a very fine-grained groundmass and microgranophyric intergrowths, implying emplacement at relatively high levels in the crust.  The age of the complex indicates that the last major movement on the Palmerville Fault in the Mungana area must have taken place before the Late Carboniferous.|16-MAY-23
22830|Sentinel Range Igneous Complex|References|*BEST, J.G., 1962:  Atherton, Qld - 1:250 000 Geological Series.  Bureau of Mineral Resources, Australia, Explanatory Notes SE/55-5.    *DE KEYSER, F., & WOLFF, K.W., 1964:  The geology and mineral resources of the Chillagoe area.  Bureau of Mineral Resources, Australia, Bulletin 70.|16-MAY-23
16787|Shady Bore Quartzite|Name source|Shady Bore on the Thornton River, 10 km northeast of Thorntonia at 947460 in the Mount Oxide 1:100 000 Sheet area.|16-MAY-23
16787|Shady Bore Quartzite|Unit history|The rocks now defined as Shady Bore Quartzite were previously included in the Ploughed Mountain Beds in the north, in the Pilpah Sandstone in the southwest, and in other areas in the Paradise Creek Formation by Carter & others (1961). Cavaney (1975) originally named this unit the "Carrier Quartzite" but this name was invalid due to prior usage.|16-MAY-23
16787|Shady Bore Quartzite|Type section locality|Holostratotype: Along the south bank of a creek adjacent to the track from Thorntonia to Shady Bore from 911439 (base) to 906439 (top) in the Mount Oxide 1:100 000 Sheet area. The section comprises 250 m of massive, medium grained white orthoquartzite with poorly outcropping interbeds of friable sandstone, siltstone and dolomite.|16-MAY-23
16787|Shady Bore Quartzite|Extent|Best exposed as broadly folded outcrops in the Lawn Hill and Riversleigh Sheet areas, as a narrow band along the boundary between the Riversleigh and Mount Oxide and Undilla and Mammoth Mines sheet areas, and in the Yelvertoft and Kennedy Gap Sheet areas.|16-MAY-23
16787|Shady Bore Quartzite|Thickness range|The unit is 250 m thick in the holostratotype. Elsewhere, the thickness varies from a maximum of 500 m in the centre of the Riversleigh 1:100 000 Sheet area and in the southwest of the Kennedy Gap 1:100 000 Sheet area to a minimum of 50 m on the Riversleigh Sheet area.|16-MAY-23
16787|Shady Bore Quartzite|Lithology|White, flaggy to massive medium grained white orthoquartzite, with siltstone and dolomite interbeds. It varies along strike depending on the number of massive orthoquartzite beds present.|16-MAY-23
16787|Shady Bore Quartzite|Relationships and boundaries|The unit conformably overlies the Lady Loretta Formation and is conformably overlain by the Riversleigh Siltstone. The basal contact is gradational and is placed where orthoquartzite beds make up more than 25 percent of the sequence. The upper contact is placed at the top of the uppermost massive orthoquartzite bed.|16-MAY-23
16787|Shady Bore Quartzite|Age reasons|Mid Proterozoic (Carpentarian)|16-MAY-23
16787|Shady Bore Quartzite|Proposed publication|81/22260|16-MAY-23
16787|Shady Bore Quartzite|References|B051|16-MAY-23
16787|Shady Bore Quartzite|Proposer|Hutton L.J., Cavaney R.J., Sweet I.P.|16-MAY-23
27653|Shield Creek Formation|Name source|Shield Creek, the name for the upper reaches of Gray Creek   also Shield Creek Holding (Clarke River 1.250 000 Cadastral map).|24-JUN-23
27653|Shield Creek Formation|Unit history|The unit was originally mapped as part of the Broken River Formation (White, 1959, 1962, 1965).  Wyatt & Jell (1980), separated the unit from the Broken River Formation, but did not formally define it.|24-JUN-23
27653|Shield Creek Formation|Geomorphic expression|The unit generally forms low to recessive topography, but locally slightly more elevated than the adjacent units.  It has a light tone on the airphotos due to the abundant feldspathic arenite, and supports a low cover of quinine bush and locally spinifex.|24-JUN-23
27653|Shield Creek Formation|Type section locality|A composite section is designated. The basal part is in a small tributary of Turtle Creek from 7859 702665 (base) to 694661 (base of Martins Well Limestone Member). The middle part is the type section of the Martins Well Limestone Member, between 7859 682684 (base) and 683683 (top). The top part is in a gully between 7859-680640 (top of the member) to 679635 (base of Dip Creek Limestone). The grid reference is based on the AGD66 datum.|24-JUN-23
27653|Shield Creek Formation|Description at type locality|The basal part consists of 300 m of generally coarse-grained feldspathic arenite with minor fine-grained silty arenite, siltstone and mudstone.    The middle part is the type section of the Martins Well Limestone Member, between 7859 682684 (base) and 683683 (top), and consists of 85 m of bioclastic calcarenite with thin shale interbeds, as originally defined by Jell (1968).   The top part is in a gully between 7859-680640 (top of the member) to 679635 (base of Dip Creek Limestone) in which about 450 m of mainly feldspathic arenite, locally calcareous crops out.  The grid references are based on the AGD66 datum.|24-JUN-23
27653|Shield Creek Formation|Extent|The unit crops out as a continuous folded belt from near 'Pandanus Creek' to the head of Magpie Creek, north of the large laterite plateau in central BURGES.  It extends from the southern edge of the plateau to Dosey Creek and in several synclinal cores between Storm Dam and the Broken River.|24-JUN-23
27653|Shield Creek Formation|Thickness range|The unit is up to 900 m in the Martins Well area, but it is locally thin to absent as along the Broken River where it is only 20 m thick.|24-JUN-23
27653|Shield Creek Formation|Lithology|Feldspathic sandstone, conglomerate, and limestone. Minor siltstone and mudstone. Thick to very thick bedded, with local medium scale, trough cross bedding.|24-JUN-23
27653|Shield Creek Formation|Fossils|A rich fauna of corals (tabulate and rugose) as well as crinoids, sponges, brachiopods, and nautiloids occurs in the limestone members.  Brachiopods and trilobites occur in the siliciclastics.  Conodonts occur in the limestone members.|24-JUN-23
27653|Shield Creek Formation|Relationships and boundaries|The Shield Creek Formation disconformably(?) overlies the Jack and Quinton Formations, and is disconformably(?) overlain by the Broken River Group. It is  distinguished from all these units by consisting predominantly of coarse-grained feldspathic arenite.  The boundary is usually poorly exposed, but in the Broken River at 7859-612441, it appears to be gradational with mudstone of the Bracteata Mudstone.    The unit contains the Martins Well Limestone Member, which was originally defined by Jell (1968) as part of the Broken River Formation, and also a new member near Jessey Springs, the Arch Creek Limestone Member, which is equivalent in age to the Martins Well Limestone Member.|24-JUN-23
27653|Shield Creek Formation|Age reasons|A rich fauna of corals (tabulate and rugose) as well as crinoids, sponges, brachiopods, and nautiloids occurs in the limestone members.  Brachiopods and trilobites occur in the siliciclastics.  Conodonts in the limestone members indicate a Lochkovian to Pragian age (Telford, 1975;  Mawson & Talent, unpublished data), but the upper siliciclastics could extend into the Emsian.  See Withnall & others (1988) for more details.|24-JUN-23
27653|Shield Creek Formation|Comments|With the raising of the Broken River Formation to group status, we have considered reinstating the Shield Creek Formation as part of the Broken River Group.  An alternative is to include it in the underlying Graveyard Creek Group.  However, the units may be separated by significant disconformities.  Conodont studies indicate a significant hiatus represented by three to four conodont zones in the Pragian and early Emsian between the limestone in the Shield Creek Formation and the lowermost carbonates of the Broken River Group (Mawson & Talent, unpublished data; Withnall & others, 1988).  It is worth noting, however, that this break is represented, at least in part, by a palaeontologically barren siliciclastic sequence, which in some places appears to have a gradational contact with the Broken River Group.  Lithologically and sedimentologically, the Shield Creek Formation possibly has more in common with the siliciclastic parts of the underlying Jack Formation of the Graveyard Creek Group, except for being predominantly feldspathic rather than quartzose.  However, conodonts indicate that a hiatus in the mid Lochkovian (again represented at least partly by a siliciclastic interval) also occurs between the Shield Creek Formation and the Jack Formation.  The hiatus was possibly of shorter duration (two to three zones), but may have been more significant tectonically.  On the time-scale of Harland & others (1982), it corresponds with widespread resetting of isotopic ages in the adjacent Georgetown Province at about 400 Ma, which may correspond with granitoid emplacement and uplift, and a corresponding lowering of relative sea-level, before the extensive transgression.  The flood of feldspathic sand may reflect such uplift of the plutonic and high-grade metamorphic rocks in the Georgetown and Lolworth-Ravenswood Provinces.Therefore, because of the uncertain relationships with the adjacent units, and its possible tectonic significance, the Shield Creek Formation is not included in either of the Groups which bound it.|24-JUN-23
27653|Shield Creek Formation|References|HARLAND, W.B., COX, A., LLEWELLYN, P.G., PICKTON, C.A.G., SMITH, 	A.G., & WALTERS, R., 1982: A Geologic Time Scale.  Cambridge University Press.  **JELL, J.S., 1968:  New Devonian rock units of the Broken River Embayment, north Queensland.  Queensland Government Mining Journal, 69, 6-8.  **TELFORD, P.G., 1975:  Lower and Middle Devonian conodonts from the Broken River Embayment, north Queensland, Australia.  Special Papers in Palaeontology, 15.  **WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.  **WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes.  **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.  **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|24-JUN-23
22844|Shovel Creek Complex|Name source|Shovel Creek, a tributary of Travers Creek (and eventually Balfe Creek) which it joins at GR 3809 77500 in the Homestead 1:100 000 Sheet area.|16-MAY-23
22844|Shovel Creek Complex|Unit history|The Shovel Creek Complex was mapped as undivided Ravenswood Granodiorite Complex by Clarke & Paine (1970).|16-MAY-23
22844|Shovel Creek Complex|Type section locality|The type locality of the Shovel Creek Complex is near the Barrington/Thalanga boundary fence at GR 3622 77588 in the Homestead 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
22844|Shovel Creek Complex|Description at type locality|Here a foliated, grey to green, granodiorite is extensively intruded by layered leucogranite dykes of the Grasstree Suite. The rock comprises quartz, plagioclase, K-feldspar, biotite and opaques with minor sphene, epidote, allanite and zircon.|16-MAY-23
22844|Shovel Creek Complex|Extent|The Shovel Creek Complex crops out over about 17km2 along Puddler and Shovel Creeks extending toward Lemon Tree Mill on Allandale.|16-MAY-23
22844|Shovel Creek Complex|Lithology|The Shovel Creek Complex is lithologically variable, probably representing different magmatic pulses. The rocks, however are foliated and intruded by aplite/leucogranite/pegmatite dykes making identification of the individual intrusions difficult. Rocks in the complex range from gabbro to granite.Samples of gabbro/diorite from GR 3589 77598 and GR 3596 77606 in the Homestead 1:100 000 Sheet area, comprise hornblende, chlorite, plagioclase and minor quartz. A quartz diorite from 3589 77591 is strongly foliated and comprises quartz, plagioclase, biotite, hornblende with minor epidote, allanite, opaques and sphene. Near Puddler Mill on Puddler Creek, a less deformed diorite contains quartz, plagioclase, augite and possible orthopyroxene. A sample from of amphibole/plagioclase rock also from Puddler Creek is interpreted as metamorphic basement.  The rgid references are based on the AGD66 datum.|16-MAY-23
22844|Shovel Creek Complex|Relationships and boundaries|The Shovel Creek Complex is intruded by leucogranite dykes of the Grasstree Suite. Its relationship to the Mount Glengaldler Granite is not known, but the greater degree of deformation in the Shovel Creek Complex suggests it may be older.|16-MAY-23
22844|Shovel Creek Complex|Age reasons|The age of the Shovel Creek Complex is not known. An age of Cambrian to Early Ordovician is tentatively assigned on the basis of the assumed older relationship to the possible Middle Ordovician age for the Mount Glengaldler Granite.|16-MAY-23
22844|Shovel Creek Complex|Comments|MAGNETIC SUSCEPTIBILITY::  The magnetic susceptibility of the Shovel Creek Complex at the type locality is in the range 612-1254 x 10[superscript]-5 SI units. Throughout the unit susceptibilities are highly variable ranging from 0-1254 10[superscript]-5 SI units. This is consistent with the lithological variability of the unit.|16-MAY-23
22844|Shovel Creek Complex|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
40138|Sleipner Member|Name source|The name was derived from the township of Sleipner.|16-MAY-23
40138|Sleipner Member|Geomorphic expression|The Sleipner Member forms moderate to steep terrain as exemplified at Mount Chalmers and Mount MacDonald, with generally rocky terrain and a wide to closely spaced dendritic pattern of drainage.|16-MAY-23
40138|Sleipner Member|Type section locality|The type area of the Sleipner Member is situated on the southern side of Mount MacDonald. The area is dominated by relatively flat lying, very thick bedded, dark green-grey, massive, poorly sorted, matrix supported, monomictic and lesser polymictic, granule to boulder breccia and minor conglomerate. Interbedded with these rocks are thick bedded, grey, fine to coarse, well sorted, feldspatholithic sandstone and minor siltstone.|16-MAY-23
40138|Sleipner Member|Extent|The Sleipner Member is found at Mount Belmont, Mount Chalmers, Mount MacDonald, and Mount Kilner. It is absent south of the Fitzroy River.|16-MAY-23
40138|Sleipner Member|General description|The Sleipner Member was previously defined as the Sleipner Andesite Tuff by Taube (1979). Taube describes the unit as consisting of dark green lithic tuff with green to purple andesitic fragments 0.2 to 2 cm across, set in a lighter green chlorite-epidote rich matrix. At some localities the fragments are both andesitic and rhyolitic in character, the latter generally being larger, commonly 20 to 30 cm across.|16-MAY-23
40138|Sleipner Member|Thickness range|The thickest section observed for the Sleipner Member is 360 m at Mount MacDonald.|16-MAY-23
40138|Sleipner Member|Lithology|The Sleipner Member is dominated by dark green-grey, massive, poorly sorted, matrix supported to clast supported, monomictic and lesser polymictic, granule to boulder breccia and minor conglomerate (Figure 13). Interbedded with the breccia and conglomerate are grey to green-grey, fine to coarse grained, well sorted, feldspatholithic sandstone and minor siltstone. Porphyritic andesite to rhyolite, either massive or flow-banded, are the most common clasts and are characteristic components of a distinctive green-grey, monomictic rock within the unit. Grey to dark grey, massive, featureless clasts are also found in this rock and in polymictic varieties. These massive clasts could be either an aphyric volcanic, siltstone, or chert.Silicification, chloritisation and clay alteration are observed in hand specimen and thin section. Saussurite alteration is seen in thin section.|16-MAY-23
40138|Sleipner Member|Depositional environment|The Sleipner Member is interpreted to be a marine mass flow deposit being poorly sorted, massive and having a sharp contact with underlying beds. Near Mount Chalmers and Mount MacDonald it immediately overlies sediments rich in marine macrofossils. Because the Sleipner Member is spatially restricted, it suggests local areas of instability, probably proximal to volcanic centres defined by the Ellrott Rhyolite.|16-MAY-23
40138|Sleipner Member|Relationships and boundaries|The Sleipner Member is part of the Chalmers Formation. The contact is preserved within the Mount Chalmers area, both in outcrop and drill holes. Stratigraphic contacts with the Ellrott Rhyolite have not been observed but all occurrences are close to the Rhyolite. Four kilometres south of Mount Chalmers, the Ellrott Rhyolite intrudes the Sleipner Member.The three dimensional extent of the Sleipner Member is unclear and must be gleaned from scattered outcrops and subsurface intersections. Both outcrop and drill hole sections contain more than one interval of the Member and it appears that the Member consists of multiple bodies. These bodies are considered to represent aprons formed by erosion of volcanic domes of the Ellrott Rhyolite. The U-Pb zircon dates (within error) obtained from the Ellrott Rhyolite coincide with the appearance of the Sleipner Member within the Chalmers Formation.The Sleipner Member appears to be restricted to the upper half of the Chalmers Formation (Figure 3). Subsurface sections intersected the Member stratigraphically no deeper than 100 m below the fossiliferous sandstone bed situated in the middle to upper part of the Chalmers Formation.In the North Star area, 4 km south of the Mount Chalmers mine, the geology is represented by large blocks of Sleipner Member within pyroclastic rocks. The blocks are predominantly massive although some do show bedding. This bedding is randomly orientated. This suggests the area was probably a sequence of Chalmers Formation dominated by Sleipner Member which was brecciated on a large scale during a volcanic eruption. The cause of the eruption was probably due to a subsurface body of Ellrott Rhyolite.|16-MAY-23
40138|Sleipner Member|Age reasons|Because of the association of the Sleipner Member with the Chalmers Formation an Early Permian age has been assigned to this unit.|16-MAY-23
40138|Sleipner Member|Defn Reference|SOURCE OF INFORMATION --Crouch. S, Parfrey. S, and Taube. A  [DATE ?]. 'Geology, tectonic setting and metallogenesis of the Berserker Subprovince, northern New England Orogen'. Supplied by Ian Withnall (GSQ), September 2008.(Incomplete reference)|16-MAY-23
40138|Sleipner Member|Parent|The Sleipner Member is found in the upper half of the Chalmers Formation (Figure 3), and extends down to no more than 100 m below the fossiliferous beds. It is characterised by monomictic to polymictic breccia and lesser sandstone and siltstone.|16-MAY-23
26144|Soldiers Cap Group|Name source|Soldiers Cap is a mesa capped with flat-lying Mesozoic sediments, 40 km southeast of Cloncurry, latitude 20o59'35"S, longitude 140o44'15"E (7056 727786).|16-MAY-23
26144|Soldiers Cap Group|Constituents|Llewellyn Creek Formation, Mount Norna Quartzite and Toole Creek Volcanics. The Group was previously defined as the Soldiers Cap Formation (Carter et al., 1961).|16-MAY-23
26144|Soldiers Cap Group|Geomorphic expression|The Group is expressed as rugged ridges in the central part, near Mount Norna and Soldiers Cap, and the topography becomes more mature with rounded hills of lower relief to the north, south and east.|16-MAY-23
26144|Soldiers Cap Group|Type section locality|The type section of the Soldiers Cap Formation as defined by Carter et al. (1961) is approximately 11.5 km long and extends from latitude 20o56'40"S, longitude 140o39'50"E (7056 651842) to latitude 20o53'40"S, longitude 140o45'30"E (7056 750895). The type section of the constituent formations in the Group have been defined along this section.|16-MAY-23
26144|Soldiers Cap Group|Extent|The Soldiers Cap Group has a total outcrop area of 2000 km2. Its distribution is essentially the same as that of the Soldiers Cap Formation as shown on the Cloncurry and Duchess 4-mile Geological Sheets (Carter et al., 1961). It occurs in the Cloncurry, Mount Angelay and Selwyn 1:100 000 Sheet areas.|16-MAY-23
26144|Soldiers Cap Group|Thickness range|The Group is at least 6000 m thick and in some sections it lmay be more than 7500 m thick.|16-MAY-23
26144|Soldiers Cap Group|Lithology|Phyllite, pelitic schist, metagreywacke, metasiltstone, lmetasandstone, metabasalt, amphibolite, chert, jaspilite, and calcareous shale.|16-MAY-23
26144|Soldiers Cap Group|Relationships and boundaries|The base of the Soldiers Cap Group is not exposed; the Group is overlain unconformably by the Mary Kathleen Group (mainly the Corella Formation). Correlations with other Groups to the west are indirect; basalts in the Toole Creek Volcanics, Marraba Volcanics and Eastern Creek Volcanics are thought to represent contemporaneous basic volcanicity over a large area of the Cloncurry Complex. On this basis, the Soldiers Cap Group is broadly equivalent to the Malbon Group (Derrick et al., 1976d) and the Haslingden Group (Derrick et al., 1976b). Since the Toole Creek Volcanics appear to be equivalent to all of the Malbon Group, it follows that the Mount Norna Quartzite and Llewellyn Creek Formation may be time equivalent to the Argylla Formation (part of the Tewinga Group), which underlies the Malbon Group. This implies a facies change from a mainly acid volcanic-sandstone sequence in the west to a siltstone-sandstone sequence in the east. Alternatively, the Tewinga Group may be older than all of the Soldiers Cap Group.|16-MAY-23
26144|Soldiers Cap Group|Age reasons|Precambrian, probably Carpentarian to possibly Lower Proterozoic. McDougall et al. (1965) dated the Ewen Granite at 1780+/-20 m.y., and Carter et al. (1961) stated that the Ewen Granite is intrusive into the Argylla Formation. A minimum age of about 1780 m.y. is thus indicated for the Argylla Formation. Since the Argylla Formation underlies or is equivalent to the lower part of the Soldiers Cap Group, a maximum age of the latter is also about 1780 m.y.|16-MAY-23
26144|Soldiers Cap Group|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1977.|16-MAY-23
26144|Soldiers Cap Group|Proposed publication|Queensland Government Mining Journal 1976|16-MAY-23
26144|Soldiers Cap Group|Comments|Remarks: Near Naraku siding, 60 km north-northwest of Cloncurry, a thick sequence of feldspathic quartzite with amphibolite interbeds, assigned to the Corella Formation by Carter, Brooks and Walker (1961), is thought by some workers to be part of the Soldiers Cap Group.|16-MAY-23
26144|Soldiers Cap Group|References|B051; 79/01220.|16-MAY-23
26144|Soldiers Cap Group|Reserved? Yes/No|N|16-MAY-23
24498|Sonoma Member|Name source|Sonoma homestead, GR 64800E 96300N Miriam Vale 1:100 000 Sheet area.|16-MAY-23
24498|Sonoma Member|Unit history|Part of the Lowmead Beds of Cribb, 1960; Mack, 1972; and Ellis and Whitaker, 1976.|16-MAY-23
24498|Sonoma Member|Type section locality|272.2 m (estimated true thickness 269.6 m) from 14 m to 286.2 m in LDD7 (GR 65665E, 97292N Miriam Vale 1:100 000 Sheet area). The interval is located within the type section of the Lowmead Formation. Claystone is the dominant rock type with interbedded kerogenous carbonaceous shale (carbonaceous oil shale) and kerogenous claystone (oil shale). There is minor sandstone and sandy claystone. Beds within the member range in thickness from 0.2 m to 20 m. The upper boundary of the member is an unconformity with unconsolidated Quaternary sediment. The lower boundary is defined at the contact between oil shale of the Sonoma Member and carbonaceous oil shale of the Makowata Oil Shale Member. |16-MAY-23
24498|Sonoma Member|Description at type locality|Rock Types: Claystone beds are olive grey, moderately hard, massive and in part sandy and weakly kerogenous. Carbonaceous oil shale is brownish-black, moderately hard to hard and thinly bedded. Fragmentary plant remains are abundant. Oil shale is dusky yellow brown, hard and laminated. It is diffusely to strongly carbonaceous in part. Sandstone is dominantly fine to medium grained, with sand grains which are well sorted, sub-rounded, of moderate sphericity and friable. It contains dominantly (over 80%) quartz in a clay matrix.|16-MAY-23
24498|Sonoma Member|Extent|Subcrops over an area of 14 km2 in the vicinity of Sonoma homestead. Sparse, highly weathered outcrop is present. The member has been identified from drill core.|16-MAY-23
24498|Sonoma Member|Thickness range|272.2 m in type section. True thickness 269.6 m, corrected for an 8o dip of the strata in LDD7. This is the maximum known thickness of the member.|16-MAY-23
24498|Sonoma Member|Relationships and boundaries|The Sonoma Member conformably overlies the Makowata Oil Shale Member of the Lowmead Formation. The top of the Sonoma Member is eroded and is in part unconformably overlain by Quaternary overburden. It is faulted against igneous rocks of the Miriam Vale Granodiorite and the Agnes Water Volcanics (Ellis and Whitaker, 1976).|16-MAY-23
24498|Sonoma Member|Age reasons|Early Tertiary - as for the Lowmead Formation.|16-MAY-23
24498|Sonoma Member|Comments|Note: Drill core of LDD7 is stored at Southern Pacific Petroleum's Research and Core Sortage facility in Gladstone, Queensland.|16-MAY-23
24498|Sonoma Member|References|79/01354|16-MAY-23
24498|Sonoma Member|Reserved? Yes/No|Y|16-MAY-23
39585|South Buaraba Microdiorite|Name source|REVISION OF NAME:: The name has been modified to 'South Buaraba Microdiorite' to better reflect the interpretation of it as an intrusive body.|16-MAY-23
39585|South Buaraba Microdiorite|Unit history|This unit was first mapped and described by Campbell (1949, 1952).  Other workers who studied the unit were Houtgraaf (1974), Vonhoff (1975), Reimers (1977) and Tudor (1985) from the University of Southern Queensland and Hegarty (1981), McCabe (1982) and Slijderink 1988 from the Queensland University of Technology.Campbell informally called the unit the 'South Buaraba Feldspar Porphyrite' and considered it as an intrusive.  Campbell's mapping was accepted in the production of the Ipswich 1:250 00 map (Cranfield and Schwarzbock, 1973).  The microdiorite was generally considered younger than the Champion Hills Diorite because Campbell (1949) mapped porphyrite dykes in the diorite 'behind Buaraba Post Office' (approximately AMG. 432100 6973600), and older than the Buaraba Granodiorite, as the microdiorite was intruded by a granodiorite dyke at AMG. 424500 6968000 (Campbell, 1952).  The grid reference is based on the AGD66 datum.|16-MAY-23
39585|South Buaraba Microdiorite|Geomorphic expression|Topography ranges from 200m in Buaraba Creek to a maximum of 500m elevation to the west of the creek.  Selective clearing has been carried out on the less steep slopes.|16-MAY-23
39585|South Buaraba Microdiorite|Type section locality|The type area of the unit defined in this report is the area of outcrop of the unit centred on South Buaraba Creek around AMG.424000 6970000.The grid reference is based on the AGD66 datum.|16-MAY-23
39585|South Buaraba Microdiorite|Extent|The outcrop occupies about 14 km2 west of Box Gully, centred on the south branch of Buaraba Creek.  The Buaraba Granodiorite separates two small outcrops less than 0.25 km2 from the main body on the south-east edge.  Campbell (1952) attributed dykes adjacent to the Buaraba Post Office to the South Buaraba Microdiorite.  During current mapping other small outcrops that may be related to the unit were located north of Buaraba Creek at grid references AMG 424100 6974800, 423900 6975100 and 423600 6975800.  The grid references are based on the AGD66 datum.|16-MAY-23
39585|South Buaraba Microdiorite|Lithology|In hand specimen the rock is dark grey and aphanitic to porphyritic with phenocrysts of feldspar and locally hornblende.  Thin section descriptions by Campbell (1952) and Cranfield & others (1976) indicate major constituents are plagioclase (andesine), hornblende and secondary chlorite.  Minor constituents are quartz, biotite, K feldspar with accessory minerals magnetite, apatite, zircon and epidote, and a high percentage of groundmass that is often cryptocrystaline and microcrystaline|16-MAY-23
39585|South Buaraba Microdiorite|Relationships and boundaries|The South Buaraba Microdiorite is intruded by the Buaraba Granodiorite and intrudes the Champion Hills Diorite and Cressbrook Creek Group as described by Campbell (1952).  The Woogaroo Sub-Group unconformably overlies the unit.|16-MAY-23
39585|South Buaraba Microdiorite|Age reasons|The Buaraba Granodiorite indicates a minimum age of Middle Triassic as it intrudes the South Buaraba Microdiorite.  Porphyry dykes intruding the Champion Hills Diorite, adjacent to the Buaraba Post Office indicate a maximum age for the unit.  All of these units intrude the Permian age Cressbrook Creek Group.  The South Buaraba Microdiorite has been assigned early to mid Triassic age.|16-MAY-23
39585|South Buaraba Microdiorite|Comments|GEOPHYSICAL EXPRESSION::  A combined K-Th-U ternary false colour radiometric image has a variable response but defines the South Buaraba Microdiorite reasonably well.  The unit has a low to moderate potassium response in contrast to the higher response of the nearby Cressbrook Creek Group and lower response of the Woogaroo Sub-group to the west.  However there is little contrast on the radiometric with the Woogaroo Sub-group to the south.  A low thorium response over most of the unit gives good contrast with surrounding units, except on the northern contact where a higher Th response in the body is similar to that of the Cressbrook Creek Group.The magnetic response of the unit is variable.  High magnetic responses correlate reasonably well with the low thorium responses at both the east and west sides of the body.  Over the remainder of the body there is a lower magnetic response, generally slightly lower than surrounding rocks, similar to that of the `Buaraba Granodiorite¿.  The body has an oval shape elongate north-east-south-west.  The body may occur near the surface up to 400m west of the interpreted geological boundary, beneath the overlying Woogaroo Sub Group.STRUCTURE::  Dr E.C.Willey (personal communication, April 1999) speculates that the microdiorite represents a caldera infill structure that has been intruded by a later ring dyke structure after caldera collapse.  The surrounding portion of the Buaraba Granodiorite represents the ring dyke system.  It seems likely that the structure also has associated small intrusions, represented by dykes described by Cambell (1952) and possibly also the small outcrops to the north of Buaraba Creek.|16-MAY-23
39585|South Buaraba Microdiorite|References|CAMPBELL, K.S.W.,1952,The geology of the Cressbrook-Buaraba area,"University of Queensland.  Department of Geology Papers (New series), Regional Geology.CRANFIELD, L.C. & SCHWARZBOCK, H., 1973, Ipswich 1:250 000 Geological Map,Queensland Department of Mines.HEGARTY, R.A.,1981,Geology of the Buaraba District, Southeast Queensland, Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology.HOUTEGRAFF, M.J., 1974,The geology of east of the north- and south branch Buaraba Creeks South Eastern Queensland. Unpublished Thesis, Department of Geology, Darling Downs Institute of Advanced Education.REIMERS, D.W.,1977,The geology of the North Buaraba - Oaky Creek area, Buaraba district, South east Queensland.  Unpublished Thesis, Department of Geology, Darling Downs Institute of Advanced Education.SLIDJERINK, P.,1988, Geology of the Buaraba Creek-North Branch project area, Unpublished Bsc honours thesis, Department of Geology, Queensland University of Technology.VONHOFF, J.D.,1975, The geology of the North and South Branch Buaraba Creeks, South Eastern Queensland, Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.|16-MAY-23
26145|South Curra Limestone|Name source|After Curra Siding, 15 km northwest of Gympie.|16-MAY-23
26145|South Curra Limestone|Unit history|Limestone group U.L. of Dunstan (1911). This unit was defined and described by Runnegar & Ferguson (1969) based on mapping to the north and east of Gympie, particularly in the vicinity of Curra and Tamaree railway stations. Brodie (1991) re-examined the outcrop at Curra quarry and Tamaree, and, in addition, made a detailed study of drill core from several underground drill holes at Monkland Mine.|16-MAY-23
26145|South Curra Limestone|Type section locality|Defined in a road cutting 2 km north of Bells Bridge, 13 km northwest of Gympie by Runnegar & Ferguson (1969). The cutting is exposed for about 100 m on both sides of the Bruce Highway (Photographs 2a, 2b) (QFG6799 & QFG8344; MGA 457495mE; 7112565mN). The beds dip northeast to east-northeast at variable angles between 40° and 65°, with localised recumbent folding (Photograph 2b). At the southern end of the cutting the limestone is separated from underlying siltstones by an apparent thrust fault which dips northeast at about 40°. This cutting is dangerous to inspect and an alternative site is just to the east along Greenhalgh Road where bedding dips vary from 25 to 40° northeast (QFG8343). More limestone is exposed in a cutting on the east side of the Bruce Highway south of the Gympie Golf Course (QFG8343; MGA 464885mE; 7104520mN). Archived drill core at Zillmere core library, Brisbane: GEGM drill hole G227: 23¿186 m at South Inglewood (MGA 469895mN; 7098795mN).|16-MAY-23
26145|South Curra Limestone|Extent|Extends as a discontinuous ridge from Keefton in the south around the eastern side of the town to Curra in the north, offset in a number of places by mainly easterly trending faults. Also occurs along the Mary River, within a series of fault blocks west of the Laing Fault, emplaced by east to west thrust faults. An isolated outcrop occurs as a small structural dome near Tamaree railway station.|16-MAY-23
26145|South Curra Limestone|Thickness range|In the type section the unit is 130 m thick. Underground at Monkland the limestone averages about 80¿120 m thick. Above the Curra Thrust at West Phoenix the limestone is 80 m thick and in a similar position overlying the Partridge graben it is 60¿75 m thick.|16-MAY-23
26145|South Curra Limestone|Lithology|Runnegar & Ferguson (1969) recognised two main rock types, a calcareous siltstone at the base of the formation, grading upwards into dominant coarser grained bioclastic calcarenite. Brodie¿s (1991) work identified numerous lithofacies, including calcarenite, biosparite and biomicrite, each with a range of variations depending bedding, from thick calcarenite to thinner calcilutite, and from coarse fossil debris to fossil-free limestone. Interbedded siltstones are also present. Colours range from dark grey to steel blue, cream coloured or grey. At Monkland Mine, Brodie (1991) analysed 130 m of core from BHP drill hole P001A (MGA 469405mE; 7099820mN) on 15 Level (750 m below surface). The basal 100 m contained graded beds of dark grey to black feldspathic calcarenites which became finer and more calcareous towards the top. They are carbonaceous,pyritic, and are interbedded with thin bioturbated siltstones. The upper 30 m consists of siliceous biosparite beds with interbedded calcilutite. Limestones at Monkland are more arenaceous than the more micritic and sparry limestones north of Gympie. Both primary and secondary porosity throughout the limestone has been destroyed; Brodie (1991) found that all pore space has been filled with calcite and silica cements. Numerous drill holes through limestone at Monkland and throughout the field failed to locate any voids.|16-MAY-23
26145|South Curra Limestone|Depositional environment|Brodie (1991) concludes that faunal assemblages reflect a low energy, restricted circulation environment affected by periods of turbulence, indicative of a shallow water shelf or lagoonal setting.|16-MAY-23
26145|South Curra Limestone|Relationships and boundaries|The upper contact of the limestone with the overlying Tamaree Formation, is regarded by Runnegar & Ferguson (1969), Brodie (1991) and geologists at Monkland Mine as conformable. The lower contact is mostly bounded by the Curra thrust fault. Where unaffected by the thrust it is in contact with underlying Glanmire Conglomerate and appears to be conformable, grading up from poorly sorted conglomerate into finer lithic arenite into basal calcarenite.|16-MAY-23
26145|South Curra Limestone|Age reasons|The Middle Permian fauna in the South Curra Limestone is discussed in great detail by Runnegar & Ferguson (1969), Waterhouse & Balfe (1987), and Brodie (1991). Bryozoan and Atomadesma filaments are common to all facies, and crinoid and brachiopod debris are widespread. Atomadesma is particularly evident in the basal facies at Curra quarry and throughout the limestone at Monkland Mine. Shelly fauna are more evident at the base of the formation and bryozoa, crinoids and corals are more abundant at the top. Li et al. (2015) obtained U-Pb ages from zircons in their sample GY1302, described as collected from 'an interstratified tuff layer within the South Curra Limestone' and with prominent cleavage. Its locality puts it at the southern end of the type section on the Bruce Highway. This could be contentious as this contact appears faulted and the sample appears to be from an adjacent unit rather than interstratified within the limestone. Zircon analyses for this sample yielded an age range of ~268-242 Ma and 40 zircons gave a weighted mean age of 258.3 +/- 2.6 Ma. They concluded deposition took place in the middle Permian up to this mean age.|16-MAY-23
26145|South Curra Limestone|Defn author|Details from Stidolph et al. (2015) GSQ Record 2015/05 p17-20.|16-MAY-23
27570|Spanner Limestone Member|Name source|Spanner Hill at 7858-523361.  The grid reference is based on the AGD66 datum.|16-MAY-23
27570|Spanner Limestone Member|Unit history|The unit was previously mapped as part of the Broken River Formation (now Group) (White, 1959, 1962, 1965) (most of 'I' lens of White (1965)).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
27570|Spanner Limestone Member|Geomorphic expression|Generally forms low ridges of limestone outcrops and rubble.|16-MAY-23
27570|Spanner Limestone Member|Type section locality|West of Spanner Hill, between 7858-513369 (base) and 513366 (top).   The grid reference is based on the AGD66 datum.|16-MAY-23
27570|Spanner Limestone Member|Description at type locality| The section consists of 156 m of calcarenite and calcirudite (coralline and stromatoporoid packstone, wackestone, and grainstone).|16-MAY-23
27570|Spanner Limestone Member|Thickness range|Up to 200 m.|16-MAY-23
27570|Spanner Limestone Member|Lithology|Mainly bioclastic limestone.|16-MAY-23
27570|Spanner Limestone Member|Fossils|Stromatoporoids (including Amphipora), corals, crinoid ossicles, brachiopods, gastropods, and conodonts.|16-MAY-23
27570|Spanner Limestone Member|Relationships and boundaries|The unit is a member within the Papilio Mudstone, which is part of the Wando Vale Subgroup of the Broken River Group.|16-MAY-23
27570|Spanner Limestone Member|Age reasons|The latter [conodonts?] indicate a Givetian age (Mawson & Talent, in press).|16-MAY-23
27570|Spanner Limestone Member|References|MAWSON, R., & TALENT, J.A., in press:  Late Emsian-Givetian 	stratigraphy and conodont biofacies - carbonate slope and offshore shoal to sheltered lagoon and nearshore carbonate ramp - Broken River, north Queensland.  Courier Forschungs-Institute Senckenburg.WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 	2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of 	Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes.WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River 	area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
17149|Speed Creek Granite|Name source|Name derived from Speed Creek.|16-MAY-23
17149|Speed Creek Granite|Unit history|Wyatt & others (1970) described these rocks as granodiorites and assigned them to two unnamed units, C-Pg and C-Pb. Our mapping has assigned them to one unit and found that they are dominantly granite.|16-MAY-23
17149|Speed Creek Granite|Geomorphic expression|The unit forms recessive, low lying topography broken by prominent bouldery outcrops and tors|16-MAY-23
17149|Speed Creek Granite|Type section locality|The type locality (8159-367513) is 800m north of the Hervey Range Road beside the track to the Ben Lomond uranium deposit.  The grid reference is based on the AGD66 datum.|16-MAY-23
17149|Speed Creek Granite|Description at type locality|Outcrop consists of cream, medium to coarse-grained equigranular biotite granite that contains minor hornblende.|16-MAY-23
17149|Speed Creek Granite|Extent|The Speed Creek Granite crops out as an irregularly shaped body trending north-east over an area of approximately 75km2. Outcrop area is largely along Speed Creek and its tributaries. Speed Creek is a tributary of Keelbottom Creek. Small areas of outcrop (0.3-2km2) also occur in the headwaters of Black Creek.|16-MAY-23
17149|Speed Creek Granite|Lithology|Speed Creek Granite is a cream to grey, fine to coarse-grained, predominantly equigranular hornblende-biotite granite.  It is locally slightly porphyritic.  Near Thorntons Gap at 8159-43178612, the granite has been foliated or sheared. Locally, the Speed Creek Granite contains abundant, subrounded to rounded xenoliths of diorite up to 15cm across.|16-MAY-23
17149|Speed Creek Granite|Relationships and boundaries|The Speed Creek Granite intrudes the Proterozoic(?) Argentine Metamorphics, Devonian sedimentary rocks of the Burdekin Basin, and Early Carboniferous Watershed North Rhyolite and Saint Giles Volcanics. A belt of hornfelsed sedimentary rocks surrounded largely by the granite is most probably Late Devonian Julia Formation. The unit has been intruded by Mingoom Granite, mafic and felsic high-level unnamed intrusive rocks, and an unnamed granite complex.|16-MAY-23
17149|Speed Creek Granite|Age reasons|Webb (1969) determined a K-Ar around biotite and hornblende age of 284-296 Ma for the Speed Creek Granite, which is close to Carboniferous-Permian boundary. An Early Permian U-Pb zircon (SHRIMP) age of 283±4 Ma on a sample from the Speed Creek Granite is reported in Appendix 1.|16-MAY-23
17149|Speed Creek Granite|References|WEBB, A.W., 1969: Metallogenic epochs in eastern Queensland.  Proceedings of the Australasian Institute of Mining and Metallurgy, 230, 27 39.|16-MAY-23
27057|Spinifex Creek Granite|Name source|From Spinifex Creek.|16-MAY-23
27057|Spinifex Creek Granite|Unit history|This granite was previously mapped as Oweenee Granite by Wyatt & others (1970).|16-MAY-23
27057|Spinifex Creek Granite|Geomorphic expression|The Spinifex Creek Granite crops out well, forming rugged, boulder-strewn, hilly topography with local relief of up to 250 m. Access is extremely difficult except along the Laroona-Ewan road and tracks constructed by tin miners during the early 1980's. Stream valleys define conspicuous lineaments trending mainly east and southeast. Spinifex Creek from which the unit takes its name defines a prominent north-trending lineament. The Coane Range Granite Complex to the north forms similar topography and the boundary is difficult to interpret on the aerial photographs. However, the southern part of the Coane Range Granite Complex appears to lack the prominent lineaments.|16-MAY-23
27057|Spinifex Creek Granite|Extent|The Spinifex Creek Granite is an elongate east-trending body about 35km long extending from the Star River to the Running River near Ewan townsite. It is about 15km wide in the east narrowing to about 7km in the west. It is bounded to the south by the Macauley Creek Granite and to the north by the Coane Range Granite Complex.|16-MAY-23
27057|Spinifex Creek Granite|Lithology|The Spinifex Creek Granite is relatively uniform in appearance and is mainly pink, medium to coarse-grained, seriate, biotite granite. Porphyritic granite appears to be more common in the east. In the western half of the pluton, the granite is only rarely porphyritic. However, porphyritic granite was observed along an old tin miners' road between 8059-890815 and 876801. In addition, an area of fine-grained, porphyritic biotite granite or microgranite has been mapped in the extreme northwest of the unit.  The grid Reference is based on the AGD66 datum. Overall, the granite is generally not as coarse-grained as the Macauley Creek Granite. It also commonly contains pegmatitic segregations and pods up to 1m across, aplite veins and miarolitic cavities; these features are rare in the Macauley Creek Granite.|16-MAY-23
27057|Spinifex Creek Granite|Relationships and boundaries|The Spinifex Creek Granite forms part of the Oweenee Batholith. The exact relationships to the other granite units is not certain, but the arcuate outlines of the contacts on a gross scale suggest that the Spinifex Creek Granite intrudes the Macauley Creek Granite and is intruded by the Coane Range Complex. A small screen of hornfelsed Ewan Formation about 2km2 in area and centred on 8059-780800, occurs between the Macauley Creek Granite and Spinifex Creek Granite. The Spinifex Creek Granite also intrudes the Running River and Argentine Metamorphics, the Late Devonian to Early Carboniferous Keelbottom Group, and the Carboniferous Paluma Rhyolite.|16-MAY-23
27057|Spinifex Creek Granite|Age reasons|No isotopic dating has been attempted, but the unit is probably Early Carboniferous like the rest of the batholith.|16-MAY-23
27057|Spinifex Creek Granite|Comments|The main distinguishing feature is that the Coane Range Granite Complex is significantly more radioactive -[than the Spinifex Creek Granite], and the boundary is clearly outlined on composite images processed from the AGSO airborne radiometric data. The Coane Range Granite complex is almost white on such images due to high K, U and Th, whereas the Spinifex Creek Granite shows pinkish tints. The Spinifex Creek Granite can also be distinguished from the Macauley Creek Granite by being generally more radioactive.|16-MAY-23
27057|Spinifex Creek Granite|References|WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127.|16-MAY-23
24501|Squirrel Hills Granite|Name source|Named after Squirrel Hills homestead, GR 765920, Selwyn 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24501|Squirrel Hills Granite|Unit history|Like all other graniteas of the eastern part of the Duchess 1:250 000 Sheet area, it was mapped as part of the Williams Granite by Carter & Opik (1963).|16-MAY-23
24501|Squirrel Hills Granite|Type section locality|Granite hills 0.8 km ESE of Squirrel Hills homestead, at GR 770915, Selwyn 1:100 000 Sheet area. Spheroidal bouldery exposures here are of medium-grained pinkish granite, most of which contains abundant feldspar phenocrysts, some more than 2 cm across.|16-MAY-23
24501|Squirrel Hills Granite|Extent|The unit has an outcrop area about 100 km long and up to 25 km wide extending NNW across Selwyn, SW part of Mount Angelay and SE part of Malbon 1:100 000 Sheet areas, Duchess 1:250 000 Sheet area.|16-MAY-23
24501|Squirrel Hills Granite|Lithology|The unit consists of massive, mainly pink, medium to coarse-grained, porphyritic and subordinate non-porphyritic granite, minor porphyritic microgranite and aplite, and rare pegmatite. The granite typically contains 5 to 15 percent biotite and/or hornblende and/or clinopyroxene and 2 percent or more of sphene and magnetite.|16-MAY-23
24501|Squirrel Hills Granite|Relationships and boundaries|Squirrel Hills Granite intrudes the Soldiers Cap Group, Corella Formation, Kuridala Formation, and metadolerite, and is also inferred to intrude Cowie Granite. It is cut by E-trending dolerite dykes and is overlain by flat-lying Mesozoic sediments.|16-MAY-23
24501|Squirrel Hills Granite|Age reasons|Proterozoic|16-MAY-23
24501|Squirrel Hills Granite|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
24501|Squirrel Hills Granite|Comments|Remarks: The granite forms a large, well-defined and probably composite body. It is probably closely related to the petrographically similar Wimberu, Mount Dore, Mount Cobalt, Yellow Waterhole, Mount Angelay, and Saxby Granites (new names), from which it is separated geographically, and forms part of the Williams Batholith (new structural term).|16-MAY-23
24501|Squirrel Hills Granite|References|R233; 98/29253.|16-MAY-23
24501|Squirrel Hills Granite|Defn Reference|R233   ?[82/22920]|16-MAY-23
24501|Squirrel Hills Granite|Reserved? Yes/No|Y|16-MAY-23
24501|Squirrel Hills Granite|Unit name|Squirrel Hills Granite (new name)|16-MAY-23
17256|Stanbroke Sandstone|Name source|Named after Stanbroke homestead, 25 km NE of Dajarra, at GR 676145, Dajarra 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
17256|Stanbroke Sandstone|Unit history|Previously mapped as part of the Argylla Formation (Carter & Opik, 1963).|16-MAY-23
17256|Stanbroke Sandstone|Type section locality|Across W limb of syncline from GR 660143 to GR 667143, 1 km WSW of Stanbroke homestead, Dajarra 1:100 000 Sheet area, Duchess 1:250 000 Sheet area. Here ridge-forming cross-bedded and ripple-marked quartz arenite and feldspathic arenite about 200 m thick, dipping east at about 30o and overlying Magna Lynn Metabasalt, are overlain by 100 m of mainly greywacke, siltstone, calcareous arenite, and limestone.|16-MAY-23
17256|Stanbroke Sandstone|Extent|Crops out in narrow N-trending synclinal and down-faulted zones in the Duchess and Dajarra 1:100 000 Sheet areas, Duchess 1:250 000 Sheet area. |16-MAY-23
17256|Stanbroke Sandstone|Thickness range|Maximum about 300 m, in type section.|16-MAY-23
17256|Stanbroke Sandstone|Lithology|Consists of quartz arenite, feldspathic arenite, and calcareous arenite, mainly in lower part, and micaceous greywacke, limestone dolomite, and siltstone, mainly in upper part: a basal conglomerate containing acid volcanic clasts is present locally, as also is arkose.|16-MAY-23
17256|Stanbroke Sandstone|Relationships and boundaries|Stanbroke Sandstone unconformably overlies Leichhardt Volcanics, Magna Lynn Metabasalt, Argylla Formation, undivided Tewinga Group, and probably Wills Creek Granite.|16-MAY-23
17256|Stanbroke Sandstone|Age reasons|Proterozoic; younger than the Argylla Formation which is isotopically dated at about 1780 m.y.|16-MAY-23
17256|Stanbroke Sandstone|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
17256|Stanbroke Sandstone|Comments|Remarks: It may be a correlative of Makbat Sandstone to S and Ballara Quartzite to N, but is separated geographically from these two units, and differs from them in generally containing interbedded calcareous and dolomitic sediments in its lower and upper parts.|16-MAY-23
17256|Stanbroke Sandstone|References|R233; 98/29253.|16-MAY-23
17256|Stanbroke Sandstone|Defn Reference|R233   ?[82/22920]|16-MAY-23
17256|Stanbroke Sandstone|First Reference|80/21252|16-MAY-23
17256|Stanbroke Sandstone|Proposer|Blake D.H.|16-MAY-23
17256|Stanbroke Sandstone|Reserved? Yes/No|Y|16-MAY-23
29214|Stanley Limestone Member|Name source|Stanley Block of Wando Vale Holding (Clarke River 4-Mile Cadastral map.|16-MAY-23
29214|Stanley Limestone Member|Unit history|The unit was previously mapped as part of the Broken River Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
29214|Stanley Limestone Member|Geomorphic expression|Crops out mainly on the northwest side of Page Creek, extending 8 km from 7859-561430 to 7858-505378.  The grid reference is based on the AGD66 datum.|16-MAY-23
29214|Stanley Limestone Member|Type section locality|Unnamed gully on the north side of Page Creek at 7858-543414.  The grid reference is based on the AGD66 datum.|16-MAY-23
29214|Stanley Limestone Member|Description at type locality|Consists of 65 m of oolitic to oncolitic calcarenite and calcirudite (grainstone and packstone) passing up into thick-bedded bioclastic calcarenite and calcirudite (packstone, wackestone, grainstone, and boundstone).|16-MAY-23
29214|Stanley Limestone Member|Thickness range|65m at type section.|16-MAY-23
29214|Stanley Limestone Member|Lithology|Bioclastic limestone (calcirudite, calcarenite, and calcilutite, represented by packstone and lesser grainstone), and minor calcareous siltstone and fine-grained sandstone.  Two thin oolitic/oncolitic grainstone intervals occur at the base of the member.  A laterally continuous stromatoporoid boundstone occurs at the top of the member.|16-MAY-23
29214|Stanley Limestone Member|Fossils|The limestone contains stromatoporoids, corals, crinoid ossicles, brachiopods, fish fragments, algae, and conodonts.|16-MAY-23
29214|Stanley Limestone Member|Relationships and boundaries|The unit is a member of the Mytton Formation of the Broken River Group.|16-MAY-23
29214|Stanley Limestone Member|Age reasons|The age is early Frasnian (Mawson & Talent, unpublished data).|16-MAY-23
29214|Stanley Limestone Member|References|MAWSON, R., & TALENT, J.A., in press:  Late Emsian-Givetian stratigraphy and conodont biofacies - carbonate slope and offshore shoal to sheltered lagoon and nearshore carbonate ramp - Broken River, north Queensland.  Courier Forschungs-Institute Senckenburg. ***WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. ***WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of  Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes. ***WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. ***WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
74793|Starcross Formation|Name source|The "Starcross" property surrounding the former Selwyn township. GDA94 coordinates lat. -21.52679 and long. 140.50287, SELWYN 1: 100 000 Sheet area.|16-MAY-23
74793|Starcross Formation|Unit history|The rocks were previously mapped as Kuridala Formation (White, 1957; Carter, 1959; Carter et al., 1961; Donchak et al., 1983; Blake, 1987; Betts et al., 2000; Giles et al., 2006), but they were assigned to the Llewellyn Creek Formation of the Soldiers Cap Group by Beardsmore et al, (1988). They were later assigned to a new unit, the Starcross Formation, by GSQ (2011), Carson et al, (2011) and Whitnall and Hutton (2013) but not formally defined.|16-MAY-23
74793|Starcross Formation|Constituents|New Hope Sandstone Member|16-MAY-23
74793|Starcross Formation|Type section locality|The proposed type-section is on the eastern limb of the Mort River Anticline in the SELWYN (7054) 1:100 000 Sheet area, trending E-W along two upper tributaries of Mort River, and Sand Creek. The section begins at lat. -21.719379 and long. 140.571859 in the west and ends at lat. -21.721308 and long. 140.606938. The thickness of the formation along this section cannot be evaluated due to its structural complexity and the absence of an observed basal contact. However, regionally representative examples of the main rock types of the Starcross Formation are present along this section. Boundary reference-section: A basal contact has not been observed. The upper contact is conformable with the Hampden Slate, with a gradational contact on the western limb of the Hampden Synform at lat. - 21.273089 and long. 140.495581.|16-MAY-23
74793|Starcross Formation|Extent|The Starcross Formation is exposed in a belt of rocks that is 10km wide and 90km long with its northern extent in the Hampden Syncline, 65km due south of Cloncurry. It is transected by the head waters of the Cloncurry and Mort Rivers. The formation has been mapped in the western parts of the MOUNT ANGELAY (7055), SELWYN (7054) and TOOLEBUC (7053) 1:100 000 Sheet areas.|16-MAY-23
74793|Starcross Formation|General description|Psammopelitic, typically consisting of grey, thick bedded, medium grained, lithic sandstone intercalated with micaceous schist.|16-MAY-23
74793|Starcross Formation|Thickness range|The thickness cannot be evaluated accurately because of the complex folding and possible thrusting, but it may be of the order of ~4000-5000m.|16-MAY-23
74793|Starcross Formation|Lithology|Very thick to medium-bedded, coarse to medium-grained, micaceous, lithic sandstone (locally feldspathic) with sporadic normal grading and flat lamination sedimentary structures interbedded with thick to thin bedded micaceous phyllitic schist (locally crenulated) with rare trough and ripple cross-lamination. Metamorphic minerals include common andalusite and uncommon staurolite, garnet and biotite.|16-MAY-23
74793|Starcross Formation|Depositional environment|The sedimentology of the Starcross Formation is suggestive of a turbidite fan succession.|16-MAY-23
74793|Starcross Formation|Relationships and boundaries|A basal contact has not been observed and is probably not exposed. It is conformably overlain by the Hampden Slate, with a gradational contact on the western limb of the Hampden Synform at lat. -21.273089 and long. 140.495581. Compared with the psammopelitic Starcross Formation, the Hampden Slate is distinguished by the dominance of pelitic rocks that are commonly carbonaceous. Intruded by numerous sills of metadolerite and metagabbro and by the Mesoproterozoic granitoids of the Williams Supersuite.|16-MAY-23
74793|Starcross Formation|Identifying features|Psammopelitc, typically consisting of grey, thick bedded, medium grained, lithic sandstone intercalated with micaceous andalusite schist.|16-MAY-23
74793|Starcross Formation|Structure and Metamorphism|Complexly folded with a common bed-parallel foliation and crenulation cleavage; common andalusite porphyroblasts indicate upper greenschist to amphibolite facies metamorphism.|16-MAY-23
74793|Starcross Formation|Age reasons|Paleoproterozoic (Statherian). A maximum depositional age of 1653 +/- 18 Ma was given by (Carson et al, 2011), but this data has been reinterpreted at 1692 +/- 12 Ma (Withnall, in preparation); 1716 +/- 9 Ma, 1679 +/- 11 Ma (Lewis et al., 2018, this record). It was deformed by the 1600-1570 Isan Orogeny. It is intruded by granitoids of the Mesoproterozoic Williams Supersuite which are in the range ~1520-1530 Ma (Withnall & Hutton, 2013, table 2.2.)|16-MAY-23
74793|Starcross Formation|Correlations|Llewellyn Creek Formation of the Soldiers Cap Group, based on similar lithological characteristics and detrital zircon age spectra.|16-MAY-23
74793|Starcross Formation|Alteration and Mineralisation|Kulthos and Osborne iron-oxide-copper-gold and Pegmont lead-zinc mineral deposits.|16-MAY-23
74793|Starcross Formation|Defn author|Alexander P. Slade, Allan Parsons and Ian W. Withnall, Geological Survey of Queensland.|16-MAY-23
74793|Starcross Formation|References|Beardsmore, T.J., Newbery, S.P. and Laing, W.P., 1988. The Maronan Supergroup: an inferred early volcanosedimentary rift sequence in the Mount Isa Inlier, and its implications for ensialic rifting in the Middle Proterozoic of northwest Queensland. Precambrian Research, 40, 487-507. **Betts, P.G., Ailleres, L., Giles, D. and Hough, M., 2000. Deformation history of the Hampden Synform in the Eastern Fold Belt of the Mt Isa terrane. Australian Journal of Earth Sciences, 47(6), 1113-1125. **Carson, C.J., Hutton, L.J., Withnall, I.W., Perkins, W.G., Donchak, P.J.T., Parsons, A., Blake, P.R., Sweet, I.P., Neumann, N.L. and Lambeck, A., 2011: Summary of results: Joint GSQ-GA NGA geochronology project, Mount Isa region, 2009¿2010. Queensland Geological Record 2011/03. **Carter, E.K., 1959. New stratigraphic units in the Precambrian of north-western Queensland. Queensland Government Mining Journal, 60(692), 437-431. **Carter, E.K., Brooks, J.H. and Walker, K.R., 1961. The Precambrian mineral belt of north-western Queensland. Bureau of Mineral Resources, Australia, Bulletin 51. **Donchak, P.J.T., Blake, D.H., Noon, T.A. and Jaques, A.L., 1983. Kuridala Region, 1: 100 000 Geological Map Commentary. Bureau of Mineral Resources, Canberra.  **Giles, D., Betts, P.G., Ailleres, L., Hulscher, B., Hough, M. and Lister, G.S., 2006. Evolution of the Isan Orogeny at the southeastern margin of the Mt Isa Inlier. Australian Journal of Earth Sciences, 53(1), 91-108. **GSQ, 2011. North-West Queensland Mineral and Energy Province Report. Department of Employment, Economic Development and Innovation. Queensland Government. **Lewis, C.J, Hutton, L.H., Withnall, I.W., Slade, A.P., Sargeant, S., 2018. Summary of results Joint GSQ-GA geochronology project: Mount Isa region, 2016-2017. Queensland geological Record. **White, W.C., 1957. Preliminary report on the geology of the Selwyn area of N.W. Queensland. Bureau of Mineral Resources, Canberra. Australian Record 1957/094. **Withnall, I.W., in preparation. Review of zircon ages for the eastern Succession of the Mount Isa Province. Queensland Geological Record. **Withnall, I.W., and Hutton, L.J., 2013. Chapter 2: North Australian Craton, in Jell, P. A., editor, Geology of Queensland. Brisbane, Geological Survey of Queensland, 23-112.|16-MAY-23
17306|Staveley Formation|Name source|Named after the Parish of Staveley, in which much of the outcrop area of the formation lies, in the Duchess 1:250 000 Sheet area.|16-MAY-23
17306|Staveley Formation|Unit history|The Staveley Formation, as defined here, is similar to the Staveley Formation of Carter & others except that it is more extensive in outcrop, does not include the Agate Downs Siltstone, and may overlie, rather than be overlain by, the Kuridala Formation.|16-MAY-23
17306|Staveley Formation|Type section locality|The type section given by Carter & others (1961) extends from a point 1.6 km north of the Tip-top mine (from GR 434234) west for a distance of about 6.4 km, Malbon 1:100 000 Sheet area, Duchess 1:250 000 Sheet area. However the western part of this type section is the type section for the Agate Downs Siltstone, now defined as a formation rather than as a member of the Staveley Formation. The type section has therefore been revised to extend from GR 434324 (1.6 km north of the Tip-top mine) west for 4.6 km (to GR 388324). From east to west this section passes across strike from a contact with ridge-forming schist of the Kuridala Formation in the east through the following map units - Pks of the Staveley Formation, 100 m; Pksbr of the Staveley Formation, 450 m; Pks, 600 m; alluvium, 400 m; Pks, 600 m; metadolerite, 700 m; Pks, 400 m; ridge-forming siltstone and slate mapped as Kuridala Formation, 250 m; Pks, 150 m; Pksbr, 400 m; metadolerite, 200 m; and Pksbr, 500 m; to ridge-forming Agate Downs Siltstone. Unit Pks forms gently undulating terrain and consists of interbedded, variably calcareous, ferruginous, feldspathic, micaceous and siliceous fine-grained sandstone, siltstone, and phyllite, and impure limestone, which are mainly shades of grey, brown, or red-brown. Unit Pksbr is more upstanding and commonly forms bouldery exposures; it consists of breccia formed of mainly angular fragments of Pks rocks enclosed in a sandy to silty matrix which is generally calcareous and ferruginous.|16-MAY-23
17306|Staveley Formation|Extent|As mapped by Blake & others (in prep. b) and Donchak & others (in prep.), the Staveley Formation crops out in a belt up to 14 km wide extending from 2 km north of Gin Creek Bore (from GR 380018, Mount Merlin 1:100 000 Sheet area) northwards for at least 75 km, to the northern edge of the Malbon and Mount Angelay 1:100 000 Sheet areas, Duchess 1:250 000 Sheet area. This belt contains most of the outcrops mapped as Staveley Formation by Carter & others (1961) and Carter & Opik (1963), and also includes outcrops in the north which they ;mapped as Corella Formation.|16-MAY-23
17306|Staveley Formation|Thickness range|The formation  may have a maximum thickness of more than 2000 m, but this is uncertain because of tight to isoclinal folding.|16-MAY-23
17306|Staveley Formation|Lithology|The formation consists of interbedded, variably calcareous, ferruginous, feldspathic, micaceous, and siliceous sandstone, siltstone, and phyllite, impure limestone (marble), and lenses of breccia, as exposed in the type section, together with schist and banded calc-silicate rocks (mainly near granite), and minor basalt lava, conglomerate, and banded quartz + hematite +/- magnetite rock. Sedimentary structures commonly present, in many cases outlined by heavy mineral laminae, include convolute to recumbent bedding, cross-bedding, graded bedding, and ripple marks; halite casts are present locally.|16-MAY-23
17306|Staveley Formation|Relationships and boundaries|The Staveley Formation has concordant contacts with Kuridala Formation, Answer Slate, and Overhang Jaspilite, which it may overlie disconformably, and with Agate Downs Siltstone, Marimo Slate, Roxmere Quartzite, Mick Creek Sandstone, and Toby Barty Sandstone, which overlie it, apparently conformably. The Agate Downs Siltstone and part of the Marimo Slate may be stratigraphic equivalents of part of the Staveley Formation. The formation is faulted against Double Crossing Metamorphics in the south and against Doherty Formation in the north. It is intruded by Gin Creek Granite, Wimberu Granite, Squirrel Hills Granite, unnamed granite, metadolerite, and feldspar porphyry, and overlain unconformably by flat-lying Mesozoic sediments.|16-MAY-23
17306|Staveley Formation|Age reasons|Proterozoic|16-MAY-23
17306|Staveley Formation|Proposed publication|Blake & others, in prep. a  - see References|16-MAY-23
17306|Staveley Formation|Comments|Revision of the definition originally proposed by Carter & others (1961).Remarks: Blake & others (in prep. B) and Donchak & others (in prep.) regard the Staveley Formation as part of the Marimo Slate sequence, which may have been laid down unconformably in the north on cherty and ferruginous breccia, representing a fossil regolith, mapped as part of the Overhang Jaspilite. To the south the formation possibly overlaps onto Answer Slate; the contact could be a low-angle unconformity rendered apparently concordant by subsequent isoclinal folding.|16-MAY-23
17306|Staveley Formation|References|88/26226; B051; 98/29253; 84/24381|16-MAY-23
17306|Staveley Formation|Defn Reference|R233    ?[82/22920]|16-MAY-23
17326|Stevenson Quartz Monzodiorite|Name source|Parish of Stevenson.|16-MAY-23
17326|Stevenson Quartz Monzodiorite|Geomorphic expression|Exposure is characterised by common boulder-sized outcrop and very rare tors, which rise above a gentle to moderately undulating terrain.  The Stevenson Quartz Monzodiorite has a yellowish-brown hue on the Landsat 5 TM (1-4-7 BGR) image. The magnetic response is moderate to strong, and the K, Th and U responses are moderate, low to moderate, and low respectively.|16-MAY-23
17326|Stevenson Quartz Monzodiorite|Type section locality|At the head of Tea Tree Creek at 8451-591553.  The grid reference is based on the AGD66 datum.|16-MAY-23
17326|Stevenson Quartz Monzodiorite|Description at type locality|Boulder-sized outcrop of fine to coarse-grained, subequigranular biotite-hornblende quartz monzonite.|16-MAY-23
17326|Stevenson Quartz Monzodiorite|Extent|An equant body 90 km2 in area, south of the Theresa Creek Dam, between the Iron Hut Quartz Monzonite to the north and the Kilmarnock Granodiorite and Annmore Quartz Monzodiorite to the south.|16-MAY-23
17326|Stevenson Quartz Monzodiorite|Lithology|Dark to light grey, fine to coarse-grained, and equigranular to subequigranular, ranging from biotite-hornblende quartz monzonite to biotite-hornblende quartz diorite.|16-MAY-23
17326|Stevenson Quartz Monzodiorite|Relationships and boundaries|Intrudes the Anakie Metamorphic Group and is unconformably overlain by the Late Devonian to Early Carboniferous Silver Hills Volcanics. The relationship with Kilmarnock Granodiorite and Iron Hut Quartz Monzonite is unknown.|16-MAY-23
17326|Stevenson Quartz Monzodiorite|Age reasons|Webb & McDougall (1968) obtained a K-Ar biotite age corrected to 379 Ma. An age of 382 Ma has been obtained from Rb-Sr dating of a biotite-whole rock pair (P. Carr, unpublished data). The age is therefore probably Middle Devonian.|16-MAY-23
17326|Stevenson Quartz Monzodiorite|References|WEBB, A.W. & MCDOUGALL, I., 1968: The geochronology of the igneous rocks of Eastern Queensland. Journal of the Geological Society of Australia, 15, 313-346.|16-MAY-23
17351|Stockyard Creek Mudstone Member|Type section locality|Originally given a type area of 'Headwaters of Stockyard Creek' by White (1959). Redefined as: In Stockyard Creek, about 2.5 km SSW from Stockyard Dam; GR 7560-282o291o (bottom) to -28252892 (top). The type section of the Candlow Formation (between GR 7560-23689 and -216377) also contains a representative section of the Stockyard Creek Siltstone.|16-MAY-23
17351|Stockyard Creek Mudstone Member|Identifying features|Variation:  The 'Stockyard Creek Siltstone Member' was defined by White (1959) and redefined by Withnall & Mackenzie (1980). The classification of the rocks as siltstone is incorrect; they are predominantly carbonaceous mudstone. We therefore propose that the name be varied to Stockyard Creek Mudstone Member.|16-MAY-23
17351|Stockyard Creek Mudstone Member|Proposed publication|Queensland Government Mining Journal.|16-MAY-23
17351|Stockyard Creek Mudstone Member|References|98/29026; 80/20650.|16-MAY-23
17351|Stockyard Creek Mudstone Member|References|White, D.A. 1959. White, D.A. 1959. New stratigraphic units in north Queensland geology. Queensland Government Mining Journal 60 (692 ), p444|16-MAY-23
29023|Stopem Blockem Conglomerate Member|Name source|Stopem Blockem Range, approximately 40 km west-northwest of Wando Vale homestead.|16-MAY-23
29023|Stopem Blockem Conglomerate Member|Unit history|The member was previously mapped as part of the Bundock Creek Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
29023|Stopem Blockem Conglomerate Member|Geomorphic expression|The member forms a range of steep hills with relief of about 100 m, and locally known as the Red Range, between Pages Creek and Gorge Creek.  It has a distinctive dark brown tone on aerial photographs, and is easily photo-interpreted even where it is not so topographically prominent.|16-MAY-23
29023|Stopem Blockem Conglomerate Member|Type section locality|Red Range Gorge on the Broken River from 7859 559448 (base) to 558449 (top).  The grid reference is based on the AGD66 datum.|16-MAY-23
29023|Stopem Blockem Conglomerate Member|Description at type locality|The member consists of 239 m of reddish grey to purple sandstone and conglomerate, with interbedded siltstone and grey sandstone.  See Withnall & others (1988, figure 53 and page 85) and Lang (1985, 1986a) for more details.|16-MAY-23
29023|Stopem Blockem Conglomerate Member|Extent|A narrow belt about 35 km long from near Pages Creek at 7858 508402 around the Rockfields Syncline to 7859 589547 near the hinge of the Atherton Anticlinorium.|16-MAY-23
29023|Stopem Blockem Conglomerate Member|Thickness range|Up to 300 m between the south branch of Gorge Creek and the Pandanus Creek-Jessie Springs track.  Progressively thins on the northwestern limb of the Rockfields Syncline, and lenses out near the hinge of the Atherton Creek Anticlinorium.|16-MAY-23
29023|Stopem Blockem Conglomerate Member|Lithology|Greyish red to purple lithic sandstone, polymictic conglomerate, and minor fine-grained redbeds; local calcirudite.  Pebbly sandstone is predominant over conglomerate, but the latter is distinctive and contains clasts of red jasper, and reddish brown quartzose arenite and siltstone.  The sandstone and conglomerate contain trough and low-angle trough and tabular cross-beds, ripple cross laminae, rip-up clasts, erosive structures with pebble lags, pebble imbrication, and horizontal planar laminae.|16-MAY-23
29023|Stopem Blockem Conglomerate Member|Fossils|The only fossils are moulds and casts of Leptophloeum australe and indeterminate root casts.|16-MAY-23
29023|Stopem Blockem Conglomerate Member|Relationships and boundaries|A member of the Bulgeri Formation. The base is marked by the first reddish purple polymictic conglomerate above the base of the Bulgeri Formation.  Northeast of the north branch of Gorge Creek, the member lies directly on the Rockfields Member, but to the southwest the members are up to 200 m apart.  The unit is overlain by normal drab sandstone and conglomerate.  Other reddish purple conglomerates do occur above the member, but these are presently unnamed.|16-MAY-23
29023|Stopem Blockem Conglomerate Member|Age reasons|The unit is probably Frasnian or Famennian in age based on its stratigraphic position.|16-MAY-23
29023|Stopem Blockem Conglomerate Member|References|LANG, S.C., 1985:  Devonian-Carboniferous stratigraphy of the southeastern Bundock Basin, Broken River area, north Queensland. B.Sc. (Hons) Thesis, University of Queensland (unpublished). **LANG, S.C., 1986a:  Devonian-Carboniferous stratigraphy of the southeastern Bundock Basin, Broken River area, north Queensland. Geological Survey of Queensland, Record 1986/5 (unpublished). **WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. **WHITE, D.A., 1962:  Clarke River - Qld E/55-13.  Bureau of Mineral 	Resources, Australia 1:250 000 eological Series Explanatory Notes. **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.D., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
17386|Storm Hill Sandstone|Name source|Storm Hill, a prominent bluff at 7858-550389.  The grid reference is based on the AGD66 datum.|16-MAY-23
17386|Storm Hill Sandstone|Unit history|The unit was previously mapped as part of the Broken River Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
17386|Storm Hill Sandstone|Geomorphic expression|The unit generally forms low ridges, but where it is thickest, it forms ridges with relief of up to 100 m.|16-MAY-23
17386|Storm Hill Sandstone|Type section locality|In Lomandra Creek between 7858-613407 (boundary with the underlying Lomandra Limestone) and 609409 (boundary with the Dosey Limestone).  The grid reference is based on the AGD 66 datum. REFERENCE SECTION::  In the north arm of Papilio Creek between 567400 (anticlinal hinge) and 566401 (boundary with the overlying relatively thin Dosey Limestone), consisting of about 100 m of coarse to very coarse quartzose to feldspathic sandstone.|16-MAY-23
17386|Storm Hill Sandstone|Description at type locality|About 50 m of coarse to very coarse quartzose sandstone and oligomictic pebble conglomerate is exposed.|16-MAY-23
17386|Storm Hill Sandstone|Extent|Intricately folded with other units of the Broken River Group, south of the Broken River.  The thickest development is in the southwest, particularly to the north and west of Storm Dam.  It lenses out north of Lomandra Creek.|16-MAY-23
17386|Storm Hill Sandstone|Thickness range|Up to 100 m at least.  It may be thicker in the area north and west of Storm Hill, but folding there prevents an accurate determination of thickness.|16-MAY-23
17386|Storm Hill Sandstone|Lithology|Coarse to very coarse-grained quartzose to feldspathic sandstone and lesser oligomictic conglomerate.|16-MAY-23
17386|Storm Hill Sandstone|Fossils|The unit is generally unfossiliferous, but poorly preserved corals, crinoids, brachiopods, and bivalves occur in a few places.|16-MAY-23
17386|Storm Hill Sandstone|Relationships and boundaries|The unit is part of the Wando Vale Subgroup of the Broken River Group.  It conformably overlies the Lomandra Limestone and is conformably overlain by the Dosey Limestone in much of its outcrop area, but lenses out to the northeast and east.  East of Storm Hill, the limestones lens out and the Storm Hill Sandstone directly overlies the Bracteata Mudstone and is overlain by the Papilio Mudstone.  At Storm Hill it directly overlies the Jack Formation, and to the northwest it unconformably overlies the Judea Formation.  In the northwest near the Broken River, it passes laterally into the Burges Formation.|16-MAY-23
17386|Storm Hill Sandstone|Age reasons|The age inferred from stratigraphic relationships is Emsian to late Eifelian.|16-MAY-23
17386|Storm Hill Sandstone|References|WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 	2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of 	Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes.WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River 	area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
33432|Stuart River Granite|Name source|The unit is named after the Stuart River, which flows through the centre of the pluton.|16-MAY-23
33432|Stuart River Granite|Unit history|The unit was previously mapped by Murphy & others (1976) and included as part of their Boondooma Igneous Complex.|16-MAY-23
33432|Stuart River Granite|Geomorphic expression|The unit forms an area of low bouldery hills that average 420m in elevation|16-MAY-23
33432|Stuart River Granite|Type section locality|The type area of the unit is designated as in the Stuart River around AMG 366300 7089500.  The grid references are based on the AGD datum.|16-MAY-23
33432|Stuart River Granite|Extent|The unit forms a north-north-west trending teardrop shaped pluton 15km in length and up to 4km wide, located about 18km due west of the township of Wondai.|16-MAY-23
33432|Stuart River Granite|Lithology|The granite is fine to medium (or rarely coarse) grained and cream in colour, with local areas of metasomatic? pinkening (of matrix feldspar) being common throughout the pluton. The granite is equigranular and leucocratic with the mafic minerals (fine biotite as scattered clots) making up only around 1% of the rock, associated with relatively coarse accessory sphene grains. Accessory opaques are very low or absent from the rock, which is consistent with its low magnetic response on geophysical images. In thin section, the granite is commonly extensively recrystallised with scattered anhedral, mainly alkali feldspar grains and aggregates surrounded by anastomosing zones of strained, dynamically recrystallised, finer grained quartz aggregates. The southernmost part of the granite (subunit PRgtf), is relatively homogeneously fine grained, leucocratic, and penetratively foliated.The western contact with the Fifer Creek Metamorphics is characterised by numerous quartz blows and silica flooding of the meta-sediments.|16-MAY-23
33432|Stuart River Granite|Relationships and boundaries|The unit intrudes the Fifer Creek Metamorphics and is intruded by a small granite body mapped as unit Rg2. The relationship with surrounding intrusive units (unit Rg5, the Melrose Igneous Complex and the Hivesville Granite) is unknown although the regular geometry of the pluton suggests that it may have intruded these units.  The granite is intruded by aplite and rhyolite dykes of unknown age.|16-MAY-23
33432|Stuart River Granite|Structure and Metamorphism|DEFORMATION::  The granite is commonly cut by networks of anastomosing mylonitic shears and brittle fractures, which account for the widespread partial recrystallisation throughout the pluton.  In a few places, (especially in subunit PRgtf) biotite alignment defines a penetrative, steeply dipping, north-west to north-north-west trending foliation visible at outcrop scale. At one locality (AMG 366351 7084851) a north-west plunging down-dip lineation is visible. The most intensely deformed rocks appear to be in the south where the granite contains mylonitic meta-sedimentary rafts of country rock, and within the more intensely foliated PRgtf subunit.|16-MAY-23
33432|Stuart River Granite|Age reasons|No age dating of the pluton has been carried out. The unit is thought to be in the Permian to Triassic age range.|16-MAY-23
33432|Stuart River Granite|Geophysical Expression|The unit has a low magnetic response on AIRDATA aeromagnetic images and a distinctive bright pink tone (potassic-rich signature) on the ternary K-Th-U radiometric image.|16-MAY-23
33432|Stuart River Granite|References|MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.WEBB, A.W. & MCDOUGALL, I.1968, The geochronology of the igneous rocks of eastern Queensland. ,"Journal of the Geological Society of Australia., 15, 313-346.|16-MAY-23
17500|Sugarloaf Metamorphics|Unit history|Campbell (1952) first used the name Sugarloaf Metamorphics for the rocks of probable Palaeozoic age that crop out east of Crow's Nest on the Ipswich 1:250 000 Sheet.  Fardon (1960) also described rocks from this area.  Cranfield and others (1976) included the rocks near Woolshed Mountain within this unit.  They were also included in this unit on the southern part of the Gympie 1:250 000 Sheet area by Murphy and others (1976).   The unit is named after The Sugarloaf, a prominent hill adjacent to Cressbrook Creek in the type area.|16-MAY-23
17500|Sugarloaf Metamorphics|Geomorphic expression|This unit has a variety of topographic expressions from cleared rolling hills to thickly forested rugged country.  For the northern part of the unit the air photo patterns show strong north-north-west linear trends which correspond to the dominant foliation.|16-MAY-23
17500|Sugarloaf Metamorphics|Type section locality|The type area was defined by Cranfield & others (1976) as lying along Cressbrook Creek between AMG 422000 6983530 and AMG 424680 6983180 on the Ipswich 1:250 000 Sheet.|16-MAY-23
17500|Sugarloaf Metamorphics|Extent|The Sugarloaf Metamorphics form a belt of rocks extending from 3km north of the Esk-Hampton Road in the south to approximately 1.5km south of Yarraman in the north and has a maximum width of approximately 15km.  A smaller area (~10km2) of north-west-trending metamorphosed sediments approximately 11km south of Kumbia have been tentatively assigned to this unit.|16-MAY-23
17500|Sugarloaf Metamorphics|Thickness range|A reliable estimate of the original thickness of the unit is difficult to make due to structural repetition and folding during subduction and thrusting.  The unit may have originally been as little as a few hundred metres thick.|16-MAY-23
17500|Sugarloaf Metamorphics|Lithology|Campbell (1952) noted three distinct rock types within the Sugarloaf Metamorphics on ESK, thin-bedded fine-grained sandstone, black slates and contorted phyllites.  He reported that sandstone was the most abundant of the three and occurs practically over the whole unit.  Forbes (1974) described the Sugarloaf Metamorphics, in the Mount Woolshed-Emu Creek area, as low-grade regional metamorphosed rocks, contact metamorphosed in places to produce some hornfels and schists.  Localised very tight isoclinal folding was also observed.  In hand specimen it was noted that fine quartz veins follow an axial plane cleavage.  Murphy and others (1976) identified only two rock types in the unit on the Gympie 1:250 000 Sheet area, slate and quartz-mica schist.  Typically the slate is light to dark grey with a well-developed cleavage and blocky jointing.  Spotted slate occurs in some areas.  On KINGAROY and NANANGO, shale, sandstone, phyllitic mudstone, phyllite, and mica schist have been identified within the unit.  East of Cooyar Creek (AMG 402381 7024427) dark grey hornfelsed mudstone occurs close to outcropping Taromeo Igneous Compex intrusives.  Strongly cleaved, quartz veined, cream to brown phyllitic shales are exposed in a small quarry beside a forestry track at AMG 404261 7017317.  Elsewhere, light brown cleaved phyllites are prevalant, commonly containing abundant quartz veining.  Spotted hornfelsed schist is common close to the contact of the Woolshed Mountain Granodiorite.  Mica schist is the dominant rock type in the isolated body of the unit west of the main body on KINGAROY.  On the road above Barkers Creek (AMG 368150 7035060) the rock is composed of cream-grey mica schist displaying a strong foliation defined by alternating quartz and mica.  Abundant fold closures, and common quartz veining along the major cleavage are also presentA thin zone of amphibolite and metavolcanics (DCov) forms a distinct unit within the Sugarloaf Metamorphics north of Anduramba along the eastern margin of Salty Waterhole Creek.  Jones (1955) referred to rocks in this unit as amphibolite whereas McLeod (1972) referred to the rock type as a hornblende schist.  The rocks are pale to dark green and display a well-developed schistosity.  The rocks exhibit contact metamorphism at the margin of the unit and the schistose nature of the unit is replaced by an indurated massive hornfelsed texture.............Mineralogically the non-hornfelsed part of the unit comprises pale to dark green pleochroic amphibole (hornblende) porphyroblasts (to 2mm) in a groundmass of fibrous amphibole (hornblende), quartz and feldspar minor magnetite and haematite opaques and accessory sphene.  The hornfelsed part of the unit contains brown-green pleochroic hornblende porphyroblasts in a groundmass of subhedral plagioclase (altered to Kaolin and sericite), deep brown biotite (with alteration to epidote), accessory sphene and zircon.  lenses of recrystallised quartz are common in hornfelsed zone|16-MAY-23
17500|Sugarloaf Metamorphics|Depositional environment|The unit is thought to represent mainly fine-grained sediments deposited in deep marine conditions before being incorporated into the eastern Australian margin as a subduction complex.  The sediments were derived from the eastern Australian continental margin.  The dominance of poorly sorted arenite composed of angular grains and showing no bedding indicates a density current origin for this unit.|16-MAY-23
17500|Sugarloaf Metamorphics|Relationships and boundaries|The Sugarloaf Metamorphics are interpreted to be faulted against the Maronghi Creek beds to the east.  The Sugarloaf Metamorphics are unconformably overlain by the Tarong beds and the Woogaroo Subgroup and outliers of the Main Range Volcanics --  basalt and sediments on ESK and NANAGO.  Unit is faulted against Permian Pinecliffe Formation on its south-eastern margin.The unit is intruded by the units of the Eskdale Granodiorite, Crows Nest Granite, Djuan Tonalite and the Woolshed Mountain Granodiorite and unit Pgo, and by the Boondooma Igneous Complex on KINGAROY.|16-MAY-23
17500|Sugarloaf Metamorphics|Age reasons|No fossils have been found within the unit. The unit is pre-Permian in age as the Woolshed Mountain Granodiorite intrudes it.  Minimum radiometric ages of Early Triassic (248 ± 0.8) and Cretaceous (137.4 ± 1.1 Ma) were generated through Ar/Ar dating of muscovite from samples of mica schist for this report (see age dating).  This former age is similar to that of the western part of the adjacent Eskdale Granodiorite, and has probably been reset by intrusion of this unit.  Alternatively, the Earliest Triassic age may represents an exhumation age of the unit during the Hunter Bowen Orogeny (see Geological and Tectonic History).  The younger Cretaceous age may represent resetting of muscovite due to a Cretaceous extension event.  This age is identical to Jurassic to Cretaceous intrusive rocks in the Maryborough 1:250 000 Sheet area and at Mount Williams on ESK immediately to the east of this area.|16-MAY-23
17500|Sugarloaf Metamorphics|Correlations|The unit is thought to be a deep crustal correlative of the Maronghi Creek beds.  The unit may be structurally correlative to lower plate accretionary wedge rocks of similar metamorphic grade in the nearby North and South D'Aguilar Subprovinces (e.g. the Murdering Creek Metamorphics, the Andersen Creek Phyllite, the Bunya Phyllite and the Kurwongbah beds).|16-MAY-23
17500|Sugarloaf Metamorphics|Comments|GEOPHYSICAL EXPRESSION::  The Sugarloaf Metamorphics have a moderately high mottled white, red green signature on the AIRDATA K-Th-U ternary (RGB) radiometric image.  This unit has a similar signature to that of the aronghi Creek beds and adjacent Boondooma Igneous Complex and Taromeo Igneous Complex.The unit is also like the Maronghi Creek beds in its magnetic response as it shows a very low response on the reduced to pole magnetic image.STRUCTURE::  Bedding and the subparallel slaty cleavage within the Sugarloaf Metamorphics dip either steeply to the west or east.  Locally, thicker beds of arenite show well developed grading and are only weakly deformed.  In general the unit has a well-defined primary cleavage with broad scale outcrop folds.  Along the western margin of the unit bedding is parallel to an enhanced cleavage, and this composite surface is strongly deformed by small-scale tight to isoclinal, sub-horizontally-plunging folds that are locally visible in some thin-bedded rocks.|16-MAY-23
17500|Sugarloaf Metamorphics|References|CAMPBELL, K.S.W.,1952,The geology of the Cressbrook-Buaraba area,"University of Queensland.  Department of Geology Papers (New series), Regional Geology.CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.",1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report,95. Regional Geology.FARDON, R.S.H.,1960, The geology of the Cooyar area. Unpublished Honours Thesis, Department of Geology, University of Queensland. Regional Geology.FORBES, ?, 1974.......................JONES, J.B.,1955, The petrology and economic potentialities of the Eskdale Complex, Unpublished honours thesis, Department of Geology, University of Queensland.MCLEOD, R.L.,1972,The geology of the northern extent of the Sugarloaf Metamorphics, Crows Nest Queensland. Unpublished undergraduate project, Department of Geology, Darling Downs Institute of Advanced Education.MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.|16-MAY-23
24510|Sulieman Gneiss|Name source|Named after Sulieman Creek, whose tributaries drain much of the area in which the unit is exposed, Ardmore 1:100 000 Sheet area (Urandangi 1:250 000 Sheet area).|16-MAY-23
24510|Sulieman Gneiss|Unit history|Previously mapped mainly as Eastern Creek Volcanics, and partly as Sybella Granite (Noakes & others, 1959).|16-MAY-23
24510|Sulieman Gneiss|Type section locality|From GR 196702 to GR 223696, about 39 km SW of Dajarra, Ardmore 1:100 000 Sheet area. The type area extends E and W of the track between Rufus Tank and The Pinnacles Dam and is drained by Spring Creek and its tributaries. The main lithologies present in the type area are interlayered medium-grained quartz + biotite + microcline + plagioclase +/- garnet +/- muscovite gneiss and augen gneiss, hornblende schist and amphibolite, and reacrystallised, medium to coarse-grained glassy quartzite and muscovite quartzite. Minor rock types present include banded garnetiferous calc-silicate gneiss and granofels, para-amphibolite, quaratz-mica schist, quartz-feldspar pegmatite, and feldspar metaporphyry. Trends are mainly northerly and dips are fairly steep to vertical. Foliation and lithological layering commonly show small-scale folds and crenulations.|16-MAY-23
24510|Sulieman Gneiss|Extent|The unit forms a narrow N-trending belt in the central part of the Ardmore 1:100 000 Sheet area, and extends S into the Glenormiston 1:250 000 Sheet area.|16-MAY-23
24510|Sulieman Gneiss|Thickness range|The thickness of the unit is unknown. The unit has been complexly folded, and its base is apparently not exposed. Bedding is very poorly preserved.|16-MAY-23
24510|Sulieman Gneiss|Lithology|The rocks are generally as in the type section.|16-MAY-23
24510|Sulieman Gneiss|Relationships and boundaries|The unit appears to have a concordant, possibly gradational, contact with metaediments assigned to the Jayah Creek Metabasalt (which is interpreted to overlie the gneiss), and a gradational contact with the Kallala Quartzite - thin lenses of glassy recrystallised quartzite and muscovite quartzite occur in the Sulieman Gneiss adjacent to the contact. The Kallala Quartzite may overlie the Sulieman Gneiss. However, no facing evidence has been found in either the Sulieman Gneiss or Kallala Quartzite. The gneiss is extensively intruded by granite regarded as forming part of the Sybella Granite batholith. It is also cut by pegmatite veins of at least two different ages and by granite veins that may be of several different ages.|16-MAY-23
24510|Sulieman Gneiss|Age reasons|Precambrian, probably Proterozoic.|16-MAY-23
24510|Sulieman Gneiss|Proposed publication|Blake & others, in preparation|16-MAY-23
24510|Sulieman Gneiss|Comments|Remarks: The Sulieman Gneiss has been regionally metamorphosed to amphibolite grade - the rocks are medium-grained, extensively recrystallised, and hornblende and clinopyroxene are common in the amphibolites and calc-silicates respectively. The common occurrence of minor chlorite, mainly replacing biotite, rarely amphibole, and sericite (replacing plagioclase) indicate that the formation has undergone a later low (greenschist) grade retrogressive regional metamorphism. The Sulieman Gneiss may be equivalent, at least partly, to the May Downs Gneiss mapped in the Mount Isa 1:100 000 Sheet area to the north (Derrick & others, 1976). However, hornblende schist, garnet-bearing gneiss and schist, para-amphibolite and calc-silicates have not been reported in the May Downs Gneiss by Derrick & others (1976).|16-MAY-23
24510|Sulieman Gneiss|References|R233; 79/01220; ? 98/29250|16-MAY-23
24510|Sulieman Gneiss|Defn Reference|R233    ?[82/22920[|16-MAY-23
24510|Sulieman Gneiss|Proposer|Bultitude R.J.|16-MAY-23
24510|Sulieman Gneiss|Reserved? Yes/No|Y|16-MAY-23
17534|Sunny Park Granodiorite|Name source|Sunny Park homestead at 8352-469566.   The grid reference is based on the AGD66 datum.|16-MAY-23
17534|Sunny Park Granodiorite|Geomorphic expression|The unit is characterised by gentle to moderately undulating terrain with rare tors and isolated boulder-sized outcrop.  On the Landsat 5 TM 1-4-7 (BGR) image, the Sunny Park Granodiorite is characterised by cleared areas with a yellow-orange hue. It has a strong, uniform magnetic response. The K response is high throughout the pluton, but the Th response is moderate in the south and high in the north. U response is patchy, but generally weak in the south and moderate in the north.|16-MAY-23
17534|Sunny Park Granodiorite|Type section locality|Along the Clermont-Peak Vale road from a prominent tor at 8352-486578 to the Sunny Park homestead turnoff at 8351-476563. Typical pink to grey, medium-grained, equigranular hornblende-biotite granodiorite to granite is exposed in this area.  The grid reference is based on the AGD66 datum.|16-MAY-23
17534|Sunny Park Granodiorite|Description at type locality|Typical pink to grey, medium-grained, equigranular hornblende-biotite granodiorite to granite is exposed in this area.|16-MAY-23
17534|Sunny Park Granodiorite|Extent|A north-trending rectangular body, 50 km2 in area, on the north-northwest margin of the Retreat Batholith. The pluton straddles the Clermont-Peak Vale road.|16-MAY-23
17534|Sunny Park Granodiorite|Lithology|Grey, fine to medium-grained, equigranular hornblende-biotite granodiorite to granite with subordinate pink, porphyritic microgranite.|16-MAY-23
17534|Sunny Park Granodiorite|Relationships and boundaries|Intrudes the Anakie Metamorphic Group and is faulted against and probably also intrudes the Early or Middle Devonian Theresa Creek Volcanics. It may intrude the adjacent Carney Creek Quartz Diorite. It is unconformably overlain by the Late Devonian to Early Carboniferous Silver Hills Volcanics west and north of Sunny Park homestead.|16-MAY-23
17534|Sunny Park Granodiorite|Age reasons|The precise age is unknown, but because of its relationships to the Silver Hills Volcanics and similarity to the Kilmarnock Granodiorite, a Devonian age is assigned.|16-MAY-23
17551|Surprise Creek Formation|Name source|Surprise Creek, a tributary of the Leichhardt River, which it joins 20 km west of Kajabbi, at latitude 20o01'35"S, longitude 139o50'40"E (6857-793852). The name "Surprise Creek Beds" was used by Carter & others (1961); it included rocks which are now mapped as Mount Isa Group, Myally Subgroup, and Surprise Creek and Quilalar Formations. However, a significant portion of the Surprise Creek Beds coincides with our proposed Surprise Creek Formation, hence we have retained the long-standing name "Surprise Creek" in this validation.|16-MAY-23
17551|Surprise Creek Formation|Geomorphic expression|Basal sandstone and quartzite (Pra) forms rugged, upstanding ridges and plateaux; sandstones of Prc commonly form harrow ridges which contrast with the generally low hills and valleys developed over the siltstone-fine sandstone facies (Prb, Prb).|16-MAY-23
17551|Surprise Creek Formation|Type section locality|The type section (holostratotype) of the Surprise Creek Beds proposed by Carter & others (1961) is in PROSPECTOR, 42 km southwest of Kajabbi; it extenads along Doughboy Creek westwards for 3 km to Glenroy homestead (6857-687533), then 2 km to the southwest. It was described by Carter & others as "faulted and incomplete". Nearly all of this type section is now mapped by us as Quilalar Formation and sediments of the Fiery Creek Volcanics; the remainder of Carter & others' type section includes rocks now mapped as Surprise Creek Formation, but extensive faulting renders this remaining section quite unsuitable for use as a type section for the proposed new unit, the Surprise Creek Formation. We therefore propose that the type section for the Surprise Creek Formation be as follows:- in ALSACE, just south of the Kajabbi-Gunpowder road, 25 km west-northwest of Kajabbi and 6 km northwest of the junction of Surprise Creek with the Leichhardt River. The base of the section is at latitude 19o59'20"S, longitude 139o48'20"E (6858-758883); the top of the section is 1.6 km west, at latitude 19o59'20"S, longitude 139o47'40"E (6858-743886). The type section exposes, from top to base, 300 m of cream, red-brown to buff-grey laminated siltstone, fine-grained sandstone and minor dolomitic sandstone (Prd). 170 m of buff to white medium-grained feldspathic sandstone and intercalated grey, green and buff siltstone and fine sandstone (Prc). 270 m of buff fine-grained feldspathic sandstone and siltstone, minor carbonaceous siltstone (Prd). 230 m of massive white, medium to coarse-grained feldspathic sandstone and pebbly sandstone (Pra). This section is overlain conformably by basal quartzite of the Mount Isa Group, and is underlain disconformably by dolomitic sediments within the Fiery Creek Volcanics. Reference sections (hypostratotypes) of the Surprise Creek Formation are located in ALSACE near 6858-800120, 16.5 km west of Dobbyn, where basal sandstone and conglomerate are exceptionally well developed; and in MYALLY along the old Dobbyn-Mount Oxide track near 6859-540635, 19 km northeast of Gunpowder, where the upper siltstone facies of the Formation is well developed. The latter section coincides largely with the reference section of Surprise Creek Beds nominated by Carter & others (1961), but includes a basal sandstone facies mapped by them as Myally Beds.|16-MAY-23
17551|Surprise Creek Formation|Extent|In north-trending, complexly folded and faulted synclinal belts 2 to 20 km wide immediately east, west and south of the Ewen Block and north-northwest of Mount Isa; in tightly-folded basin-and-dome structures extending northwards from Gunpowder; in a narrow belt extending from north of Alhambra westwards and southwards around a broad dome of Weberra Granite, Myally Subgroup and Quilalar Formation; and as prominent quartzite inliers surrounded by McNamara Group rocks southwest of Gunpowder.|16-MAY-23
17551|Surprise Creek Formation|Thickness range|The type section is 970 m thick; the reference sections are 1600 m and over 2000 m respectively. Thickness ranges from 200 m to over 2000 m; most thickness variation occurs in the basal conglomerate and pebbly sandstones.|16-MAY-23
17551|Surprise Creek Formation|Lithology|White, pale pink and buff medium to coarse-grained feldspathic sandstone (quartzite) and white clayey feldspathic sandstone; pebbly feldspathic sandstone and conglomerate; brown and gareen-grey micaceous sandstone and siltstone, minor shale, carbonaceous siltstone and ferruginous and dolomitic sandstone and siltstone. In most areas four informal subdivisions have been mapped; unit A (map symbol Pra) is the basal sandstone/conglomerate. Units B and D (Prb, Prd) are mainly siltstone and fine sandstone units separated by unit C (Prc), which in addition to siltstone contains a lower white sandstone marker and an upper brown sandstone marker traceable over large areas. Copper staining is present in units B, C, and D, especially the latter.|16-MAY-23
17551|Surprise Creek Formation|Relationships and boundaries|The Surprise Creek Formation overlies the Fiery Creek Volcanics and in some areas the Quilalar Formation disconformably, or with slight angular unconformity. It is overlain disconformably by basal orthoquartzite (Warrina Park Quartzite) of the Mount Isa Group east of Gunpowder and by the Torpedo Creek Quartzite of the McNamara Group west of Gunpowder. Southwest and northwest of Gunpowder the basal McNamara Group quartzite rests disconformably on massive basal sandstone of the Surprise Creek Formation, which indicates erosion or non-deposition (probably the former) of the upper siltstone facies.|16-MAY-23
17551|Surprise Creek Formation|Age reasons|Betaween 1680 m.y. (Carters Bore Rhyolite:- Fiery Creek Volcanics equivalent; Page, 1978) and about 1670 m.y., the age of tuff beds in the Mount Isa Group (Page, in prep.).|16-MAY-23
17551|Surprise Creek Formation|Correlations|The Surprise Creek Formation sandstone facies and siltstone facies are correlated with the Deighton Quartzite and White Blow Formation of the Mount Albert Group, respectively, in the Eastern Succession across the Kalkadoon-Leichhardt Block to the east and southeast. To the west the Surprise Creek Formation is a correlative of, and replaces, all except the upper part of Mammoth formation (i.e. excluding the Torpedo Creek quartzite member) proposed by Cavaney (1975).|16-MAY-23
17551|Surprise Creek Formation|Proposed publication|BMR Journal, 5(3) 1980|16-MAY-23
17551|Surprise Creek Formation|Comments|Remarks: The Surprise Creek Formation is of economic interest because of widespread traces of copper mineralisation (mainly as stratiform or stratabound chalcocite and malchite) in units Pr, Prc and Prd; the nature of the mineralisation resembles Zambian copper-belt occurrences.|16-MAY-23
17551|Surprise Creek Formation|Defn Reference|80/21252|16-MAY-23
17551|Surprise Creek Formation|Status|1|16-MAY-23
17666|Talbot Creek Granodiorite|Name source|Talbot Creek which joins the Delaney River at GR 682 613 (Georgetown 1:100 000 Sheet area).|16-MAY-23
17666|Talbot Creek Granodiorite|Unit history|Previously mapped as Forsayth Granite by White (1962g).|16-MAY-23
17666|Talbot Creek Granodiorite|Type section locality|On the north side of Talbot Creek at GR 755 566, 3.0 km northwest of Mt Talbot. Cream and grey muscovite-biotite leucogranodiorite crops out.|16-MAY-23
17666|Talbot Creek Granodiorite|Extent|Two known areas of outcrop in the Georgetown 1:100 000 Sheet area: (a) An east-west belt 9 km long between Talbot Creek and the western edge of the Newcastle Range in the south of the Sheet area about 19 km south-southeast of Georgetown. (b) In a small range of hills in a north-south belt between Quartz Blow Creek and Pack Saddle Creek (local name) about 5 km northeast of Mistletoe Homestead and 12 to 17 km north-northeast of Georgetown. In the Forsayth 1:100 000 Sheet area cream, white and pink muscovite-biotite leucogranite or granodiorite cropping out north of Spring Creek midway between "Tenavute" and "Jenkins Creek" Homesteads may be Talbot Creek Granodiorite.|16-MAY-23
17666|Talbot Creek Granodiorite|Lithology|Grey, pink or cream, medium even grained leucogranodiorite with biotite and minor muscovite; muscovite locally more abundant than biotite.|16-MAY-23
17666|Talbot Creek Granodiorite|Relationships and boundaries|Intrudes the Proterozoic Robertson River Metamorphics, Mistletoe Granite (new name). The rocks cropping out in the Forsayth 1:100 000 Sheet area are in contact with the Forsayth Granite and probably intrude it. One of the northern bodies is intruded by the Proterozoic White Springs Granodiorite (new name).|16-MAY-23
17666|Talbot Creek Granodiorite|Age reasons|Proterozoic; intruded by the White Springs Granodiorite.|16-MAY-23
17666|Talbot Creek Granodiorite|References|01/31334|16-MAY-23
26160|Tamaree Formation|Name source|From Tamaree Railway Station, north of Gympie.|16-MAY-23
26160|Tamaree Formation|Unit history|Part of the Upper Gympie Formation, L.S and S.S., of Dunstan (1911).|16-MAY-23
26160|Tamaree Formation|Type section locality|In a cutting on the North Coast railway south of Tamaree Station (Runnegar & Ferguson, 1969). A revisit in 2015 showed it to be overgrown due to realignment of the rail line. An alternate site is the cliff-like excavation just south of Langton Road, Monkland at the rear of Sunshine Mitre 10 complex QFG6803: (MGA 468905mE; 7100125mN). Archived drill core at Zillmere core library, Brisbane:GEGM drill hole G227: 12-23 m at South Inglewood (MGA 469895mN; 7098795mN)|16-MAY-23
26160|Tamaree Formation|Extent|Widespread along the eastern, western and southern margins of the main fault blocks.|16-MAY-23
26160|Tamaree Formation|Thickness range|Estimated by Runnegar & Ferguson (1969) to be about 670 m in the type section and 600m west of Mount Corella.|16-MAY-23
26160|Tamaree Formation|Lithology|Consists of repetitive, rhythmically graded interbeds of arenite, siltstone and mudstone, fining upwards to bioturbated siltstone, shale and mudstone. The arenite tends to be medium-grained and feldspathic, containing lithic grains of volcanic provenance. Roach (1990) observed an increase in the presence of quartz grains towards the top of the unit. Cross-bedding, load casts and flame structures have been recorded. Drill holes through the unit show that the siltstone and shale are carbonaceous and pyritic and the arenite can be calcareous (petrographic slide GG121). Arnold (1996) identified a cherty transitional unit at the base of the formation consisting of arenite and carbonaceous shale/siltstone interbedded with pale greenish cherty mudstone.|16-MAY-23
26160|Tamaree Formation|Relationships and boundaries|Regarded as conformably overlying the South Curra Limestone. Limited examination of outcrop of Tamaree Formation adjacent to Keefton Formation in Noosa Road near the Lewis Decline indicates this relationship is also conformable.|16-MAY-23
26160|Tamaree Formation|Age reasons|Runnegar & Ferguson (1969) describe known fauna, including corals, giving this unit a Late Permian age. Waterhouse & Balfe (1987) reviewed the few fossils found in this formation and assigned them a late Middle Permian or early Late Permian age. Li et al. (2015) collected detrital zircons from three sites for U¿Pb dating from which they determined a constraint on the age of deposition. For two samples, GY1307 and GY1311, they obtained a youngest peak age of ~255 Ma. For the third site, GY1317, which they ascribed to the Rammutt Formation but which remapping has indicated is Tamaree Formation, they obtained a youngest peak of ~265 Ma. They concluded that the deposition of the Tamaree Formation is limited to the Late Permian.|16-MAY-23
26160|Tamaree Formation|Defn author|Details taken from Stidolph at  al. (2016) GSQ Record 2016/05, p14-16.|16-MAY-23
26160|Tamaree Formation|Comments|The Tamaree Formation was defined and initially described by Runnegar & Ferguson (1969). Roach (1990) provided further description in considerable detail from his work on the south side of Gympie. Cranfield (1999) then summarised the geology based on the GSQ mapping program in the 1990s. The summary below is compiled from these three references and from Arnold (1996). The two main shafts at Monkland Mine and the Lewis Decline were all collared in the Tamaree Formation as were a considerable number of surface drill holes.|16-MAY-23
26160|Tamaree Formation|References|ARNOLD, G.O., 1996: Geology of the Southern Gympie Goldfield from core logging, and implications for mineralisation. Unpublished report to Gympie Eldorado Gold Mines Pty Ltd.  **DUNSTAN, B., 1911: Geology map of Gympie and environs. Geological Survey of Queensland Publication 221b.  **LI, P., ROSENBAUM, G., YANG, J-H. & HOY, D., 2015: Australian-derived detrital zircons in the Permian-Triassic Gympie terrane (eastern Australia): Evidence for an autochthonous origin. Tectonics, 34, 858-874.  **Roach (1990) - details not provided.  **RUNNEGAR, B. & FERGUSON, J.A., 1969: Stratigraphy of the Permian and Lower Triassic marine sediments of the Gympie District, Queensland. Paper of the Department of Geology, University of Queensland.  **WATERHOUSE, J.B. & BALFE, P., 1987: Stratigraphic and faunal subdivisions of the Permian rocks at Gympie. In: Murray, C.G. & Waterhouse, J.B. (Editors): 1987 Field Conference, Gympie District. Geological Society of Australia, Queensland Division, Brisbane, 20-29.|16-MAY-23
24512|Tangalooma Sandstone|Name source|"Tangalooma" homestead (GR 744070E, 7117810N Muggleton sheet 8745). Equivalent to interval 6 of the Injune Creek Group (Swarbrick, 1973). Informally termed Sandstone Unit (Zillman, 1979).|16-MAY-23
24512|Tangalooma Sandstone|Unit history|New name. Previously interval 6 of the Injune Creek Group (Swarbrick, 1973).|16-MAY-23
24512|Tangalooma Sandstone|Type section locality|GSQ Roma 5 (GR 740070E, 7117800N Muggleton sheet 8745). Occurs between the depths of 97.2 m and 180.4 m.|16-MAY-23
24512|Tangalooma Sandstone|Extent|Can be traced along strike from south-east of Wandoan to Injune. Intersected in the subsurface in numerous coal exploration holes and deep petroleum wells.|16-MAY-23
24512|Tangalooma Sandstone|Thickness range|Range: 50-200 m. Average: 150 m. Type Section: 83.2 m|16-MAY-23
24512|Tangalooma Sandstone|Lithology|Predominantly medium-grained lithic or feldspathic labile sandstone commonly with carbonate cement. Upward fining sequences are commonly developed, beginning with lag conglomeratic bands of fossil wood debris, ironstone and mudstone clasts and culminating in siltstone and mudstone. Thin coal members may also be present but do not persist laterally for any great distance. Carbonate-rich siltstones are also common and can be traced along the surface strike for several kilometres.|16-MAY-23
24512|Tangalooma Sandstone|Relationships and boundaries|The Tangalooma Sandstone conformably overlies the Taroom Coal Measures. In outcrop, the base of the unit is marked by the lowest resistant sandstone unit, whilst in subsurface it corresponds to the top of the last major coal member in the Taroom Coal Measures. The top of the Tangalooma Sandstone is gradational but is marked by a general increase in finer sediments especially mudstone.|16-MAY-23
24512|Tangalooma Sandstone|Age reasons|Middle Jurassic (Gould, 1968).|16-MAY-23
24512|Tangalooma Sandstone|Proposed publication|Coal Geology|16-MAY-23
24512|Tangalooma Sandstone|References|98/28995; 79/04193|16-MAY-23
24512|Tangalooma Sandstone|Defn Reference|82/22851|16-MAY-23
24512|Tangalooma Sandstone|Proposer|Jones G.D., Patrick R.B.|16-MAY-23
26282|Tank Creek Sandstone|Name source|Tank Creek which joins Gray Creek at 7859-658658.  The grid reference is based on the AGD66 datum.|16-MAY-23
26282|Tank Creek Sandstone|Unit history|The unit was previously mapped as part of the Broken River Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and described by Withnall & others (1988), but was not formally defined|16-MAY-23
26282|Tank Creek Sandstone|Geomorphic expression|Forms a prominent ridge with a maximum relief of about 100 m.|16-MAY-23
26282|Tank Creek Sandstone|Type section locality|South Chinaman Creek between 7859-605689 (base) and 604689 (top).  The grid reference is based on the AGD66 datum.|16-MAY-23
26282|Tank Creek Sandstone|Description at type locality|The section is about 80 m thick and consists of well-sorted coarse-grained quartzose sandstone near the base passing into fine and medium-grained sublabile lithic sandstone towards the top.|16-MAY-23
26282|Tank Creek Sandstone|Extent|A 7 km-long linear belt trending north from 'Pandanus Creek'.  A thin unit underlying the Dip Creek Limestone is also equated with the Tank Creek Sandstone.|16-MAY-23
26282|Tank Creek Sandstone|Thickness range|Up to 80 m.|16-MAY-23
26282|Tank Creek Sandstone|Lithology|Fine to coarse-grained quartzose to sublabile lithic sandstone as in the type section.  The sandstone is thin to medium bedded, with flat lamination and small to medium-scale trough and low-angle cross bedding.|16-MAY-23
26282|Tank Creek Sandstone|Fossils|The sandstone contains poorly preserved brachiopods.|16-MAY-23
26282|Tank Creek Sandstone|Relationships and boundaries|The unit is part of the Wando Vale Subgroup of the Broken River Group.  It overlies the Shield Creek Formation with apparent conformity, although the relationship could be disconformable.  It is overlain conformably by the Chinaman Creek Limestone near 'Pandanus Creek', and Dip Creek Limestone in the Dip Creek area.|16-MAY-23
26282|Tank Creek Sandstone|Age reasons|The age is probably Emsian, because of the unit's stratigraphic relationships.|16-MAY-23
26282|Tank Creek Sandstone|References|WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of 	Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes. **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River 	area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., 1989:  Revision of the stratigraphy of the Broken 	River area, north Queensland - Ordovician and Silurian units.  Queensland Government Mining Journal, 90, 213-218. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
17850|Tareela Volcanics|Name source|The Tareela Volcanics was first named by Wyatt & others (1970) who gave the name to a sequence of andesitic and rhyolitic lavas and pyroclastics that crop out over much of the Parish of Tareela.|16-MAY-23
17850|Tareela Volcanics|Unit history|The Tareela Volcanics were included in the Glenrock Group by Hutton & others (1994).|16-MAY-23
17850|Tareela Volcanics|Constituents|Two named units, the Ponto Basalt Member and the Eridge Volcanic Member (see separate definitions under respective names).|16-MAY-23
17850|Tareela Volcanics|Constituents|Our mapping has subdivided the formation into two members and several unnamed units. Basaltic to andesite volcanics have been divided into the Ponto Basalt Member and the unnamed unit Ctb, whereas the rhyolitic volcanics have been assigned to the Eridge Volcanic Member and the unnamed units Ct1 and Cta.|16-MAY-23
17850|Tareela Volcanics|Type section locality|Wyatt & others (1970) did not give a type section for the Tareela Volcanics. Type sections mapped through the two named units, the Ponto Basalt Member and the Eridge Volcanic Member (see separate definitions), are designated here as a composite type section for the Tareela Volcanics|16-MAY-23
17850|Tareela Volcanics|Extent|The Tareela Volcanics lie within a northwest-trending fault-bounded block, herein named the Tareela Graben which is some 11km wide and 25km long.|16-MAY-23
17850|Tareela Volcanics|Thickness range|The overall thickness of the Tareela Volcanics is difficult to determine. However, on the western limb of the syncline between Little Star River and Star River, the Ponto Basalt Member is 1000m thick and the Eridge Member is 1500m thick.|16-MAY-23
17850|Tareela Volcanics|Lithology|Unit Ct1:  Ct1 is the lowest unit of the Tareela Volcanics. It crops out on the western limb of a syncline and east of Little Star River in the core of the adjacent open anticline. The unit is predominantly light green, poorly sorted rhyolitic breccia, crystal-poor, moderately lithic-poor to lithic-rich rhyolitic lapilli breccia and minor spherulitic, flow-banded rhyolite.    Ponto Basalt Member:  The Ponto Basalt Member crops out between the Little Star River and Star River on the limbs of the syncline, and south of Little Star River in the anticline. It comprises dark grey, slightly to moderately porphyritic basalt to andesite, andesitic breccia, amygdaloidal basalt and basaltic andesite, andesitic lapilli breccia and aphyric basalt to andesite.   Eridge Member: The Eridge Member lies in the centre of a broad syncline between Little Star River and Star River. It consists predominantly of lithic-rich dacitic to rhyolitic volcaniclastics as described separately below.    Unit Cta:  Unit Cta  crops out north of Ben Lomond East, around the junction of the main two branches of Keelbottom Creek. The outcrop area is approximately 15km2. This unit is predominantly mottled green and maroon, crystal-poor to moderately crystal-rich, lithic-rich rhyodacite to rhyolite tuff and ignimbrite and felsic volcanic breccia. It is most likely equivalent to the Eridge Member because it also overlies the Ponto Member and is lithologically similar to unit Cte4 in the Eridge Member.    Unit Ctb: Unit Ctb overlies Cta. It consists of dark grey, aphyric to moderately porphyritic basalt and andesite, moderately crystal-rich, lithic-rich dacitic/andesitic lapilli breccia, and andesitic breccia. Like the Ponto Basalt Member, the unit forms generally recessive topography and is vegetated by good grass cover and scattered narrow-leaf ironbarks.|16-MAY-23
17850|Tareela Volcanics|Fossils|Lepidodendron veltheimianum was found in the Eridge Member (unit Cte1) at 8159-157687 in a volcaniclastic siltstone and suggests an Early Carboniferous age.  The grid reference is based on the AGD66 datum.|16-MAY-23
17850|Tareela Volcanics|Relationships and boundaries|At the north western end and various other locations near the margin of the Tareela Graben, the Tareela Volcanics disconformably overlie Devonian to Early Carboniferous Keelbottom Group (DCk). On the margins of the graben, the Tareela Volcanics are faulted against the Keelbottom Group and early Palaeozoic Argentine Metamorphics and Melon Creek Tonalite. No units overlie the Tareela Volcanics but they have been extensively intruded by Carboniferous to Permian granite and rhyolite.  Similarities between rocks in the upper part of the Tareela Volcanics and rocks of the Saint Giles Volcanics suggest that these units are equivalent in part. Other possible equivalent formations in the Townsville 1:250 000 Sheet area of similar age and rock types are the Percy Creek Volcanics, Saint James Volcanics and Ewan Formation, all of which are part of the Glenrock Group.|16-MAY-23
17850|Tareela Volcanics|References|*HUTTON, L.J., DRAPER, J.J., GUNTHER, M.C., WITHNALL, I.W. & LOCKHART, D.A., 1994: Glenrock Group; in DRAPER, J.J. & LANG, S.C. (Editors), Geology of the Devonian to Carboniferous Burdekin Basin. Queensland Geological Record 1994/9.    *WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127|16-MAY-23
24011|Taroborah Granodiorite|Name source|Taroborah siding on the main railway line west of Emerald at 8450-965960.  The grid reference is based on the AGD66 datum.|16-MAY-23
24011|Taroborah Granodiorite|Geomorphic expression|The Taroborah Granodiorite is mostly overlain by Quaternary, Tertiary and Permian cover and therefore could not be identified on the Landsat 5 TM 1-4-7 (BGR) image. It does however, show a high magnetic response over a large area on the detailed airborne geophysical data, as well as the older, regional Bureau of Mineral Resources data. This indicates that the isolated outcrops are part of a largely concealed batholith, that has an area of at least 600 km2, extending east from near Sapphire for about 30 km. It is separated from the Retreat Batholith by a belt of relatively non-magnetic Anakie Metamorphic Group and Fork Lagoons beds. Mapped outcrop areas generally have low responses in K, U and Th.|16-MAY-23
24011|Taroborah Granodiorite|Type section locality|At 8450-702982 along a fenceline, 3.7 km northeast of Gem Park homestead. The grid reference is based on the AGD66 datum.|16-MAY-23
24011|Taroborah Granodiorite|Description at type locality|Fresh outcrops of medium-grained biotite-hornblende granodiorite.|16-MAY-23
24011|Taroborah Granodiorite|Extent|Known from several isolated outcrop areas between Gem Park homestead and Fork Lagoons in the northern part of the Anakie and southern Rubyvale 1:100 000 Sheet areas.|16-MAY-23
24011|Taroborah Granodiorite|Lithology|Where unweathered, the unit consists mostly of granodiorite as at the type locality. Other rocks observed include augite-hornblende-biotite quartz diorite, dark grey gabbro and pink monzodiorite containing aplite and pegmatite veins. However, generally the unit is very weathered and lateritised and represented by sandy soil and grus.|16-MAY-23
24011|Taroborah Granodiorite|Relationships and boundaries|Intrudes the Fork Lagoons beds, although the actual contacts are obscured by Permian to Cainozoic cover. Hornfelsing of the Fork Lagoons beds in the Sapphire area indicates the near proximity of the concealed batholith.   The Taroborah Granodiorite is overlain by outliers of the Late Devonian to Early Carboniferous Silver Hills Volcanics near Gem Park homestead, and elsewhere by Permian Reids Dome beds and Aldebaran Sandstone, Tertiary Red Mountain Formation, duricrust, basalt, and extensive soil and colluvium.|16-MAY-23
24011|Taroborah Granodiorite|Age reasons|Webb & others (1963) obtained K-Ar biotite and hornblende ages corrected to 372 Ma and 374 Ma respectively from a single sample from west of Anakie. The age is therefore probably Middle Devonian.|16-MAY-23
24011|Taroborah Granodiorite|References|WEBB, A.W., COOPER, J.A. & RICHARDS, J.R., 1963: K-Ar ages on some Central Queensland granites. Journal of the Geological Society of Australia, 10, 317-324.|16-MAY-23
36987|Taromeo Igneous Complex|Unit history|The Taromeo Igneous Complex is a new name for the Taromeo Tonalite as defined by Murphy & others (1976).  Gradwell (1949) informally named the complex as the 'Yarraman Granodiorite' and 'Taromeo Tonalite' and more recently Willey (1999) informally named the southern-most portion the 'Googa Googa Granodiorite' and 'Googa Googa Tonalite' respectively.|16-MAY-23
36987|Taromeo Igneous Complex|Geomorphic expression|Outcrop within the Taromeo Igneous Complex is generally poor with most of the units forming gently rolling soil covered hills and valleys.  Good exposures of rock can be found along the old coach road linking Blackbutt and Nanango (PRgmt) and beside Seven Mile Diggings Road south of Nanango (PRgmgd2).  Large tors of PRgmgd2 are present beside the D'Aguilar Highway north-west of Nanango. Tors of Rgmgd2 crop out on hillsides east of the D'Aguilar Highway in the Cooyar Creek valley and scattered outcrop can be found on the hills north of Blackbutt near the abandoned Taromeo and Ashington mines.  Exposure of PRgmgd1 is poor although minor weathered outcrop is present in some gullies.  Duricrust and weathered Tertiary sediments and volcanics obscure the majority of the unit. Further north, exposure of Rgmd in the headwaters of Taromeo Creek is impressive where it forms prominent steep creek banks.  Sub-unit Rgmgd1 forms the topographically low area of the Googa Googa Creek valley and adjoining Emu Creek.  Here, scattered outcrop is present on the valley floor north of Emu Creek.  Subunit Rgmg is exposed as roadside boulders on the access road to Blackbutt Heights Estate.|16-MAY-23
36987|Taromeo Igneous Complex|Extent|The spatially and genetically related intrusions (Wherle, 1995) making up the complex, form a roughly north-north-west trending mass extending from Emu Creek, south of Blackbutt, to Barkers Creek north-west of Nanango and cover an overall area of approximately 300km2 (See Table 7).|16-MAY-23
36987|Taromeo Igneous Complex|Lithology|Gradwell (1949) described rocks of the area as being tonalite and granodiorite in composition.  Murphy and others (1976) acknowledged the variability of the Taromeo Igneous Complex and described rock types ranging from granite to gabbro.  Tonalite was found to be the dominant rock type.  Wherle (1995) also recognised two rock types within the complex, tonalite and granodiorite, but identified three granitoid groups using normalised REE patterns.  He considered that variations in rock geochemistry could most easily be explained through crystal fractionation (removal and accumulation) of mineral phases.  Current mapping has identified a wide range of rock types including tonalite, granodiorite, granite, quartz diorite, diorite, quartz gabbro and quartz monzodiorite. Costituents comprise:: PRgmt - major rock type appears to be tonalite although significant granodiorite is present , with minor granite and rare quartz gabbro.  Rgmg - Grey-pink medium to coarse-grained granite and granodiorite are main rock types.Rgmd - Primarily of quartz diorite and quartz monzodiorite, and minor diorite to granodiorite. Rgmgd2 - Light and dark grey granodiorites are main rock types but smaller proportions of granite, tonalite and quartz diorite are also present.  A smaller central portion is predominantly medium to coarse-grained grey-pink granite, and has been described as a separate unit (Rgmg).Rgmgd1 - Willey (1999) divided Rgmgd1 area into the `Googa Googa Tonalite¿ and `Googa Googa Granodiorite¿.  Unit Rgmgd1 is composed primarily of granodiorite (16km2) with tonalite (0.8km2) restricted to the easternmost portion of the unit.  Radiometric dating by Willey (1998) indicated the tonalite phase (240 Ma) is older than the granodiorite (233 Ma).  The eastern extremity of the unit abuts a leuco diorite (`Black Boy Hill Diorite¿) reported by Willey (1998) as Permian (270Ma) in age. Petrographic analysis of the granodiorite has revealed a composition of oligoclase-andesine plagioclase (30-50%), quartz (15-40%), orthoclase (5-10%), hornblende (5-10%), biotite (10-15%) and accessory sphene, zircon and opaques.  The tonalite phase was described by Willey (1999), as `hornblende (12-22%), biotite (3-8%), oligoclase (55-62%) and quartz (18-22%)¿.PRgmgd2 - Murphy and others (1976) nominated this unit as the type area for Taromeo Tonalite - composed primarily of grey medium grained granodiorite but also contains quartz monzonite, quartz monzodiorite, tonalite and granite.|16-MAY-23
36987|Taromeo Igneous Complex|Relationships and boundaries|The Taromeo Igneous Complex intrudes the Devonian to Carboniferous Maronghi Creek beds and Sugarloaf Metamorphics, and the Permian to Triassic Gilla Volcanics.  At least part of the complex intrudes the Early to Middle Triassic Esk Formation near the Red Queen Mine.  Murphy and others (1976) reported a faulted contact with the Esk Formation east of Benarkin.  Tertiary sediments and Tertiary Main Range Volcanics overlie part the complex.Within the complex, PRgmt, PRgmgd2 and PRgmgd1 appear to be oldest and are crosscut or intruded by the younger phases Rgmgd2, Rgmgd1 and Rgmd.  At least part of the complex intrudes the Early to Middle Triassic Esk Formation near the Red Queen Mine.  Murphy and others (1976) reported a faulted contact with the Esk Formation east of Benarkin.  Tertiary sediments and Tertiary Main Range Volcanics overlie part the complex.Within the complex, PRgmt, PRgmgd2 and PRgmgd1 appear to be oldest and are crosscut or intruded by the younger phases Rgmgd2, Rgmgd1 and Rgmd.|16-MAY-23
36987|Taromeo Igneous Complex|Age reasons|Staff of the University of Queensland recalculated six radiometric age dates for different areas of the Taromeo Igneous Complex using 1980 constants (Holcombe and others, 1998).  Recalculation of the original GSQ, Webb and McDougall (1968) and Harding (1969) dates gives an age range of hornblende Ar/Ar 263.3 Ma to biotite K/Ar 225.7 Ma.  Significantly, the oldest and youngest ages were calculated from the same quartz monzonite sample located within PRgmgd2.  Together with other ages recorded from PRgmt [242.9 Ma Webb and McDougall (1968)] and Rgmgd1 [233, 240 Ma (Willey, 1998)] an age of Latest Permian to Late Triassic can be assigned to this complex.  The crosscutting relationship displayed by Rgmgd2 on the RTP magnetic image shows it to be younger than PRgmt (242.9 Ma).  This is confirmed by an Ar/Ar date of 229¿11 Ma (Green, UQ unpublished laboratory notes).  No radiometric dates have been undertaken on unit Rgmd although its intrusive relationship shown by hornfelsing of Early to Middle Triassic Esk Formation (AMG 416700 7035400) indicates a probable Middle-Late Triassic age.  A relational age for unit PRgmgd1 is difficult to establish.  A paucity of outcrop, deep weathering and Tertiary cover makes sampling for radiometric dating difficult.  The grid references are based on the AGD66 datum.|16-MAY-23
36987|Taromeo Igneous Complex|Geochemistry|Geochemical samples were collected for all subunits, except PRgmgd1, and analysed at the Government Chemical Laboratories.  All samples were obtained using a sledgehammer.  Analyses have been plotted onto standard geochemical diagrams and are presented in the geochemistry chapter of this report.|16-MAY-23
36987|Taromeo Igneous Complex|Comments|MINERALISATION - Several abandoned mines and mineral occurrences are present in PRgmt and were worked for gold and copper in the early part of this century, although returns were low (Randall and others, 1996).  Seven-Mile Diggings, Yarraman Creek diggings and Resurrection Mine, all exploited low-grade alluvial gold.  Sawers (1967) reported the presence of minor bismuthinite at the Bismuth Prospect, close to the Seven-Mile Diggings.  Ashington Mine, Taromeo Copper Mine and Golden Bird Mine produced copper, gold and silver from chloritic and silicic altered shear zones within PRgmt.  Small amounts of cobaltite were noted at Golden Bird (Denmead, 1934).|16-MAY-23
36987|Taromeo Igneous Complex|Comments|Other studies undertaken over various parts of the complex include QUT student theses by Barrie (1982), Bowden (1985), Robertson (1987) and Wherle (1995).|16-MAY-23
36987|Taromeo Igneous Complex|References|BARRIE, B.,1982,Geology of the central Cooyar Creek district, Blackbutt, Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology",Regional Geology,Nanango.BOWDEN, M.A.,1985,Geology of the Yarraman Creek area, SE Qld.,Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology",Regional Geology,Nanango.DENMEAD, A.K.,1934, Golden Bird Proprietry Limited, Blackbutt","Queensland Government Mining Journal, 35, 76-77.GRADWELL, R.,1949,The petrology of the eruptive rocks of the Yarraman district. Papers, Department of Geology, University of Queensland. 3(8).HARDING, 1969, Catalogue of age determinations on Australian rocks, 1962-1965. Report of Bureau of Mineral Resources. Geology and Geophysics., Australia., 117.,Age Dating.HOLCOMBE, R.J.,  & others,1998,New England Fold belt age database. University of Queensland, Department of Earth Science (unpublished). MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.RANDALL, R.E., OSBORNE, J.H., DONCHAK, P.J.T., CROSBY, G.C., & SCOTT, M.,1996, A review of mineral exploration and known mineral occurrences within the Goomeri (9345) Nambour (9444) and Nanango (9344) 1:100 000 Sheet Areas, South-east Queensland, Geological Survey of Queensland, Record 1996/4. ROBERTSON, S.D.,1987,The geology of Yarraman, Undergraduate Thesis, School of Natural Resource Sciences, Queensland University of Technology.SAWERS, J.D.,1967, Bismuth prospect, M.L.  Application 131, Nanango","Queensland Government Mining Journal, 68, 71-73.WEBB, A.W. & MCDOUGALL, I.1968, The geochronology of the igneous rocks of eastern Queensland. ,"Journal of the Geological Society of Australia., 15, 313-346WEHRLE, A.C.1995,The Complexity of Granitoid Pulses that Comprise the Taromeo Tonalite.,"Honours Thesis, School of Natural Resource Sciences, Queensland University of Technology.WILLEY, E.C., 1998, The Maronghi Creek beds: A preliminary appraisal. Queensland Government Mining Journal. 99 (No. 1161), 49-56.WILLEY, E.C., 1999, Intrusives in the southern outcrop of the Maronghi Creek beds (SE Qld). Regional Geology. Tectonics and Metallogenesis. New England Orogen.  Papers presented at a conference held at The University of New England, Armidale. 1-3 February 1999.|16-MAY-23
17861|Tarong beds|Name source|Hill and Tweedale (1955) first used the name Tarong beds for the Triassic sediments identified west of Yarraman and Nanango.  Day & others (1974) discussed the regional geology of the Tarong Basin and it was summarised by Murphy &others (1976).  Flood (1983), Garces & Flood (1984), and Garces (1985) used standard basin analysis techniques, as described by Miall (1983,1984), to undertake detailed sedimentological studies of the basin.  Flood & Garces (1986) and Pegram (1986) summarised the geology and structure of the Tarong Basin.|16-MAY-23
17861|Tarong beds|Geomorphic expression|The Tarong Basin sediments form gently rolling to moderately steep country.  Aerial photographs show a characteristic steep sided drainage pattern for the unit especially in the Cooyar Creek area.|16-MAY-23
17861|Tarong beds|Extent|The Tarong basin is a NNW-SSE trending basin of approximately 75km in length and about 10km in width, located approximately 10km west of Nanango and a few kilometres west of Yarraman on KINGAROY.  Smaller areas of probable Tarong Basin sediments, forming a roughly linear belt, have been identified approximately 15km north of Nanango on NANANGO, further north on GOOMERI and extending north to approximately 3km west of Lake Barambah on MURGON.  Some of these sediments were considered to be Tertiary in age by Murphy & others (1976).|16-MAY-23
17861|Tarong beds|General description|PROVENANCE:: The unit was derived from erosion of granite from the Boondooma Igneous Complex and metasediments of the Maronghi Creek Beds.|16-MAY-23
17861|Tarong beds|Thickness range|Hempton & Dunne (1983) used comparitive sedimentological studies of modern and ancient basins to suggest that pull-apart basins exhibit the relationship y = .08x + .26, where y is the thickness and x is the "overlap".  Using this relationship, Flood & Garces, (1986) calculated a total thickness of 1.86km for the Tarong basin.  This estimate of sediment cover was considered reasonable as vitrinite reflectance values of the coal at the surface averaged 0.64%.  A similar vitrinite reflectance value can be obtained under about 1km of cover and a normal geothermal gradient.|16-MAY-23
17861|Tarong beds|Lithology|The Tarong Basin is made up of clastic sedimentary rocks ranging in grainsize and bedding characteristics from laminated mudstone to massive cobble-boulder polymictic conglomerate.  The basin contains significant economically important coal reserves that are currently being exploited at Meandu Mine for power generation.  Other coal resources are known from the Kunioon area south of Kingaroy.  Flood & Garces (1986), summarised the sediments of the basin as being composed of massive, matrix supported, debris-flow breccias, massive to thinly bedded clast supported, sheet-flow gravel fan conglomerates, sandy matrix-supported distal-flow conglomerates and horizontally stratified, cross-bedded, trough cross-bedded, planar cross-bedded and massive, distal fan or sandy braid-plain sandstones.  Thick deposits of laminated mudstone are also present within the basin, most notably close to the coal deposits, and are interpreted as representing waning flood sedimentation in a lacustrine environment.  They most likely correspond to the stone bands present in the coal.   Flood (1983), Garces & Flood (1984), and Garces (1985) using standard basin analysis techniques, as described by Miall (1983,1984), identified three east-flowing transverse alluvial deposits on the western margin of the basin.  These were referred to as the Stuart, Tanduringie, and Cooyar 'fans' because of their spatial relationship to the palaeodrainage of the Stuart River, Tanduringie Creek and Cooyar Creek.  Sediments of the central Tanduringie 'fan' interdigitate with the Kunioon and Meandu coal deposits that occur on either side of this 'fan'.  Flood & Garces (1986) reported that vertical profile analyses of surface expressions and subsurface bore cores suggested the gravelly deposits are of the Scott-type while the sandy deposits are more closely related to the Donjek-type (sensu Miall, 1978). The Scott-type model for braided river deposits consists of roughly horizontally bedded gravels with minor sand wedges whereas the Donjek-type model consists of fining upward cycles of mixed bedload of sand and gravel.  COARSE-GRAINED FACIES: Conglomerates within the Tarong Basin represent high-energy fan and braided stream deposits.  They increase and dominate near the basin margins and with depth, and appear to increase towards the south (Pegram, 1986).  On the western margin of the basin the conglomerates contain significant granitic material sourced from the Permo-Triassic Boondooma Igneous Complex.FINE-GRAINED FACIES: Sandstones and finer-grained facies are common in the Tarong Basin and were deposited as distal fans or as sandy braid-plains.  They also predominate in the main coal bearing areas of the basin and consist of labile poorly sorted sandstones associated with polymictic conglomerates, minor siltstones, mudstones and claystones (Pegram, 1986).|16-MAY-23
17861|Tarong beds|Depositional environment|Sediments of the Tarong Basin were deposited in a fresh water fluviatile environment with a significant paludal component (Murphy & others, 1976).  Coarse-grained facies were deposited in high-energy alluvial fans and talus-slope debris-flows.  Finer-grained sandstones and pebbly conglomerates were deposited in distal fans and braided stream environments. In the Meandu Mine area finer-grained facies, represented by laminated mudstones, siltstones and very fine-medium sandstones that often exhibit ripple markings (Pegram, 1986), were deposited as interfingering beds within the coal deposits in low energy marshy areas.|16-MAY-23
17861|Tarong beds|Relationships and boundaries|The Tarong beds unconformably overlie the Maronghi Creek beds and Sugarloaf Metamorphics and part of the Permo-Triassic Boondooma Igneous Complex.  The Tarong beds have been intruded by younger phases of this unit south of the Nyora Clay pit at about AMG 38290 704440.  The Triassic to Jurassic Bundamba Group and the Tertiary Main Range Volcanics unconformably overlie the unit.|16-MAY-23
17861|Tarong beds|Age reasons|Murphy & others (1976) summarised the palynological studies undertaken on samples from the Tarong basin and these are presented below.  Jones (1947) described flora collected from the Tarong Basin, approximately 6km south-west of Yarraman as Phlebopteris sp., Dicroidium odontopteroides (Morris) Gothan, and Czekanowskia tenuifolia (Johnston) Jones and de Jersey, and assigned a Late Triassic age to the unit.  Later Woods & Dear (1962) described a macroflora including Equisetites sp., Cladophlebis australis (Morris) Seward, Dicroidium odontopteroides (Morris) Gothan, Taeniopteris spatulata McClelland, and Sagenopteris sp., from approximately 11km west of Nanango and suggested a Late Triassic to Early Jurassic age.  De Jersey & Hamilton (1965) described what they considered as Late Triassic microflora from sediments beneath Tertiary Main Range Volcanics near Taabinga, approximately 4km south of Kingaroy.  These sediments are considered part of the Tarong Basin and were mapped as such by Murphy & others (1976).  De Jersey (1970), following further microflora studies, assigned the Tarong Basin sediments to a Late Triassic (Carnian) age essentially equivalent to the age of sediments of the Ipswich Basin to the east.|16-MAY-23
17861|Tarong beds|Correlations|The Tarong Basin is an age correlative of the Ipswich Basin to the south-east of the mapped area around Ipswich.|16-MAY-23
17861|Tarong beds|References|DAY, R.W., CRANFIELD, L.C. & SCHWARZBOCK, H.,1974,Stratigraphy and structural setting of Mesozoic basins in southeast Queensland and northeastern New South Wales;  In: Denmead, A.K., Tweedale, G.W. & Wilson, A.F., (editors), The Tasman Geosyncline - A Symposium.  Geological Society of Australia, Queensland Division, 319-364. Regional Geology.  **DE JERSEY, N.J. & HAMILTON, M.,1965,Palynology of samples from the Kingaroy area, Queensland Government Mining Journal 66, 74-76.  **DE JERSEY, N.J., 1970, Palynology from samples of Tarong Beds, Queensland Government Mining Journal, 71, 308-310.  **FLOOD, P.G. & GARCES, B. Jun.,1986,A late Triassic strike-slip (pull-apart) basin containing alluvial fan and coal-rich fluviatile sediments In: Willmott (editor), Geological Society of Australia, Queensland Division., 1986 Field Conference, South Burnett District p 77-81.   **GARCES, B., Jr,1985, The sedimentology, depositional environments and development of the Late Triassic Tarong Basin.  Unpublished M.Sc. Thesis, Department of Geology, University of New England. Basin Analysis. **GARCES, B., Jr, & FLOOD, P.G.,1984,Alluvial fan and braided stream sedimentation within the Late Triassic Tarong Basin, SE Queensland. Proceedings of the Eighteenth Symposium, Advances in the study of the Sydney Basin.  Department of Geology, University of Newcastle, 81-84. Basin Analysis.  **HEMPTON, M.R. & DUNNE, L.A.,1983, Sedimentation in pull-apart basins:  active examples in eastern Turkey., Journal of Geology, 92, 513-530.   **HILL, D. & TWEEDALE , G.W.,1955, Geological Map of the Moreton District with parts of the Darling Downs, Burnett and Wide Bay Districts, Queensland, at a scale of 6 miles to an inch. Government Printing Office, Brisbane.Regional Geology.  **JONES, O.A., 1947,Report on collection of plants from Tarong Beds by C.C. Morton, Geological Survey of Queensland, Unpublished Report 22/1/47.MIALL, A.D.,1978, Lithofacies types and vertical profile models in braided river deposits - a summary. In: Miall, A.D., (editor) Fluvial Sedimentology.  Canadian Society of Petroleum Geologists Memoir 5, 597-604. Sedimentology.  **MIALL, A.D.,1983, Basin analysis of fluvial sediments, In: Collison, J.D. & Lewin, J., (editors), Modern and Ancient Fluvial Systems. International Association of Sedimentologists Special Publication 6, 279-286.,Basin Analysis.  **MIALL, A.D.,1984, Principles of Sedimentary Basin Analysis. Springer-Verlag, New York, 490p.Basin Analysis.  **MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.  **PEGREM, B.J.,1986,Geology of the Tarong Area and Meandu Coal Mine.,In: Willmott (editor), Geological Society of Australia, Queensland Division., 1986 Field Conference, South Burnett District p 82-90.  **WOODS, J.T. & DEAR, J.F.,1962, Report on fossil plants from the Tarong Beds, west of Nanango, Geological Survey of Queensland Unpublished Report|16-MAY-23
24514|Taroom Coal Measures|Name source|Taroom township (GR 7810003 7161000N, Taroom Sheet 8846).|16-MAY-23
24514|Taroom Coal Measures|Unit history|New name. Previously intervals 3, 4 and 5 of the Injune Creek Group (Swarbrick, 1973). Equivalent to intervals 3, 4 and 5 of the Injune Creek Group (Swarbrick, 1973). Informally termed the Lower Coal Measures. (Zillman, 1979).|16-MAY-23
24514|Taroom Coal Measures|Type section locality|GSQ Roma 1 (GR 798700 7121000N Taroom Sheet 8846). Occurs between the depths of 100.9 m and 252.1 m.|16-MAY-23
24514|Taroom Coal Measures|Extent|Crops out along strike from south-east of Wandoan to Injune. Intersected in subsurface in numerous coal exploration holes and deep petroleum wells.|16-MAY-23
24514|Taroom Coal Measures|Thickness range|Range: 50 to 200 m. Average: 180 m. The formation thins towards Injune. Type Section: 151.2 m.|16-MAY-23
24514|Taroom Coal Measures|Lithology|Fine to medium grained lithic and feldspathic sandstone predominates, especially taowards the base of the formation. Interbedded siltstone, mudstone, carbonaceous shale and coal. The siltstone is grey and hard and generally contains interbeds of mudstone and ironstone. Impure limestone occasionally occur interbedded with siltstone and ironstone. There is an increase in the thickness of coal members towards the top of the unit. Three coal members can be correlated within the formation but at present are not defined. The top most coal member (as found in the Taroom coal deposit) marks the top of the unit.|16-MAY-23
24514|Taroom Coal Measures|Relationships and boundaries|Within the northeastern Surat Basin the Taroom Coal Measures conformably overly the Eurombah Formation although the boundary is gradational. The top of the uppermost major coal member marks the top of the formation.|16-MAY-23
24514|Taroom Coal Measures|Age reasons|Middle Jurassic (Gould, 1968).|16-MAY-23
24514|Taroom Coal Measures|Proposed publication|Coal Geology|16-MAY-23
24514|Taroom Coal Measures|References|98/28995; 79/04193; |16-MAY-23
24514|Taroom Coal Measures|Defn Reference|82/22851|16-MAY-23
24514|Taroom Coal Measures|Proposer|Jones G.D., Patrick R.B.|16-MAY-23
17919|Teddy Mount Formation|Name source|Teddy Mount, a prominent hill at 7859 451629 northwest of the Montgomery Range.|16-MAY-23
17919|Teddy Mount Formation|Unit history|Previously mapped as part of the Bundock Creek Formation (now Group) by White (1959, 1962, 1965), and 'upper' Bundock Creek Formation by Wyatt & Jell (1980).  The name was first published and described by Withnall & others (1988), but was not formally defined.|16-MAY-23
17919|Teddy Mount Formation|Geomorphic expression|The Teddy Mount Formation has a subdued outcrop pattern because of the dominance of siltstone and mudstone.  Sporadic widely spaced ridges are formed by sandstone and limestone.  It has a smooth-textured aerial photo-pattern reflecting the usually well-grassed cover, with an open canopy of tall ironbarks and other eucalypts.|16-MAY-23
17919|Teddy Mount Formation|Type section locality|A composite section is designated.  The lower part is along Montgomery Creek from 7859 518463 (base) to 521481 and then along an unnamed tributary normal to strike to 518488 (base of Dyraaba Member).  The grid reference is based on the AGD66 datum.|16-MAY-23
17919|Teddy Mount Formation|Description at type locality|The base of the Teddy Mount Formation is placed at the bottom of a sequence of very thick-bedded, greenish grey, calcareous mudstone and siltstone about 230 m thick).  This is overlain by 780 m of a generally coarser sequence of very thick-bedded brown mudstone with interbeds of thin to very thick-bedded, fine to medium-grained grey, lithofeldspathic to feldspathic, micaceous, calcareous sandstone.  Above this, 25 m of pale, brown-grey mudstone underlies the Dyraaba Member.  The upper part of the composite section is the type section of the Dyraaba Member in a tributary of Mount Brown Creek, about 3 km to the southwest of the lower section, between 499462 and 497466.  It is 385 m thick and consists of sandstone (similar to that in the lower part of the unit), siltstone, and mudstone.  Plant remains are abundant.See Withnall & others (1988, pages 90-92) for more details.|16-MAY-23
17919|Teddy Mount Formation|Extent|Widely distributed from near 'Gregory Springs' in the southwest to Teddy Mount in the northeast, and 'Oak Valley' in the northwest.|16-MAY-23
17919|Teddy Mount Formation|Thickness range|1420 m in the type section.  Elsewhere the overall thickness is difficult to determine because of the folding.|16-MAY-23
17919|Teddy Mount Formation|Lithology|Fine to medium-grained, micaceous, feldspathic to lithofeldspathic, calcareous sandstone, siltstone, mudstone, and minor dirty limestone.  The sandstones contain small to medium-scale trough and low-angle planar and tabular cross-beds, ripple cross-laminae, horizontal planar laminae, parting lineation, and  soft-sediment deformation.  Ripple cross-laminae, planar laminae, and burrows are common in the finer lithologies.|16-MAY-23
17919|Teddy Mount Formation|Fossils|The Teddy Mount Formation contains an abundant shallow marine fauna dominated by gastropods; brachiopods, bivalves, nautiloids, crinoids, bryozoans, and fish scales also occur. Microfossils include ostracodes, phyllocarids, fish teeth and other microremains, together with rare conodonts.  The fauna is described in more detail by Lang (1985, 1986a), and is summarised by Withnall & others (1988).|16-MAY-23
17919|Teddy Mount Formation|Relationships and boundaries|Conformably overlies the Turrets Formation and distinguished by being more calcareous and containing more sparsely distributed sandstone beds.  It contains the Dyraaba Member which is distinguished by the presence of abundant plant remains, and by being more sandy.  The Teddy Mount Formation is conformably overlain by the Boroston Formation, and is distinguished from it by the lack of quartz-rich sandstones.  It is intruded by the Carboniferous or ?Permian Montgomery Range Igneous Complex.|16-MAY-23
17919|Teddy Mount Formation|Age reasons|The rare conodonts indicate a latest Famennian age. The unit may range into the Tournaisian.|16-MAY-23
17919|Teddy Mount Formation|References|LANG, S.C., 1985:  Devonian-Carboniferous stratigraphy of the southeastern Bundock Basin, Broken River area, north Queensland. B.Sc. (Hons) Thesis, University of Queensland (unpublished).LANG, S.C., 1986a:  Devonian-Carboniferous stratigraphy of the southeastern Bundock Basin, Broken River area, north Queensland. Geological Survey of Queensland, Record 1986/5 (unpublished).WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28.WHITE, D.A., 1962:  Clarke River - Qld E/55-13.  Bureau of Mineral 	Resources, Australia 1:250 000 Geological Series Explanatory Notes.WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.D., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5.|16-MAY-23
26167|Telegraph Creek Member|Name source|Telegraph Creek; GR 299,000E, 7,384,000N Gladstone 1:100 000 topographic sheet.|16-MAY-23
26167|Telegraph Creek Member|Unit history|Part of The Narrows Beds (Kirkegaard et al, 1970) and part of the Rundle Formation (Henstridge and Missen, 1982).|16-MAY-23
26167|Telegraph Creek Member|Type section locality|91 m of claystone with minor interbeds of oil shale, calcareous claystone and impure dolomite; from 163.3 to 254.1 m in drill hole RDD66 (GR 299,441E 7,382,121N, Gladstone 1:100 000 topographic sheet), which is part of the type section of the Rundle Formation. The greenish-grey to dark greenish-grey claystone contains three major oil shale beds, the uppermost being a very distinctive marker throughout The Narrows Graben. In the type section the oil shale beds are from 180.0 to 185.2 m, 208.9 to 211.0 m and 215.6 to 217.8 m. There are numerous thin impure dolomite lenses (up to 1.35 m thick); a 14 cm thick dolomite bed marks the base of the member. In part, the claystone is strongly calcareous. Minor oil shale beds occur in the basal part of the type section, from 241.0 to 241.6 m and from 247.7 to 250.5 m.|16-MAY-23
26167|Telegraph Creek Member|Extent|Subcrops in an area of about 28 km2 in The Narrows Graben, NW of Gladstone, Queensland. Sparse, weathered outcrops are recorded. There is one outcrop of fresh oil shale at the confluence of Kerosene and Munduran Creeks, GR 300,850E, 7,382,220N. The member has been identified from drill hole core.|16-MAY-23
26167|Telegraph Creek Member|Thickness range|90.8 m (estimated true thickness 90.5 m corrected for an apparent dip of 4o in RDD66) in type section. Range of true thickness of the member as intersected in drill holes is 51.3 m to 109.2 m.|16-MAY-23
26167|Telegraph Creek Member|Lithology|Claystone, greenish-grey to dark greenish-grey, soft to moderately hard, generally calcareous, mostly thickly bedded but in places thinly laminaated or brecciated. There are tough impure dolomite beds (up to 1.4 m thick) at various stratigraphic levels within the member but these are generally not correlatable between drill holes. Two persistent impure dolomite beds (0.1 to 0.5 m apart) commonly form the base of the member. Two oill shale beds (0.5 to 2 m thick) and 4 to 6 m apart are persistent in the central part of the member. A very persistent oil shale marker bed up to 10 m thick occurs from 10 to 15 m below the top of the member. There are two persistent oil shale beds within the basal 20 m of the member which attenuate along the eastern margin of the graben. To the northwest and east within the graben, there are sandy claystone and sandstone interbeds and a decrease in the thickness of oil shale beds. Current bedding is recorded in the upper sandy claystones in the northwestern part of the graben. Cyclicity of rock types within the member is common and there are desiccation features throughout the sequence. Ther are sporadic gastropod and ostracode fossils and rare vertebrate remains. Bioturbation occurs within the claystone, particularly where sandy.|16-MAY-23
26167|Telegraph Creek Member|Relationships and boundaries|The member is conformable with the underlying Munduran Creek kMember and is the contact between oil shale and claystone or, in places, the sharp contact between oil shale and dolomite. The upper boundary is conformable with the Kerosene Creek Member and is the contact between oil shale and claystone. The member is faulted against Devonian to Carboniferous rocks of the Curtis Island Group along the western edge of The Narrows Graben.|16-MAY-23
26167|Telegraph Creek Member|Age reasons|Mid to late Eocene - as for the Rundle Formation.|16-MAY-23
26167|Telegraph Creek Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
26167|Telegraph Creek Member|Comments|Note: Drill-core from RDD66 is stored at Southern Pacific Petroleum's Research and Core Storage Facility located in Gladstone, Queensland.|16-MAY-23
26167|Telegraph Creek Member|References|79/02402|16-MAY-23
26168|Teningie Creek Member|Name source|Teningie Creek; GR 306,000E, 7,375,200N, Gladstone 1:100 000 topographic sheet.|16-MAY-23
26168|Teningie Creek Member|Unit history|Part of The Narrows Beds (Kirkegaard et al, 1970) and part of the Rundle Formation (Henstridge and Missen, 1982).|16-MAY-23
26168|Teningie Creek Member|Type section locality|68 m of oil shale with lesser interbeds of claystone and rare impersistent dolomite; from 335.1 to 403.2 m in drill hole ERD 169 (GR 300,999E, 7,380,998N, Gladstone 1:100 000 topographic sheet). The olive brown to olive grey oil shale contains four major greyish-green claystone beds in the upper part of the unit (from 335.1 to 338.8 m, 341.0 to 344.7 m, 350.6 to 353.9 m and 356.7 to 358.2 m in type section) and a lower interbedded greyish-green claystone zone from 393.7 to 400.0 m in type section. Minor interbeds of claystone also occur in the oil shale. Yellowish-grey impure dolomite is recorded from 340.3 to 340.4 m, 348.6 to 348.9 m and 357.0 to 357.5 m in type section. Cyclicity of lithologies is a feature.|16-MAY-23
26168|Teningie Creek Member|Extent|Subcrops in an area of about 88 km2 in The Narrows Graben, NW of Gladstone, Queensland. The member has been identified from drill hole core.|16-MAY-23
26168|Teningie Creek Member|Thickness range|68.1 m (estimated true thickness 67.1 m corrected for an apaprent dip of 9o in ERD 169) in type section. Range of true thickness of the member as intersected in drill holes is 36.7 m to 67.1 m.|16-MAY-23
26168|Teningie Creek Member|Lithology|Oil shale, olive brown to olive grey; calcareous, carbonaceous and clayey cyclicity; very thinly to very thickly bedded (up to 2m); brecciated and peloidal, laminated in part. Lesser interbeds of greyish-green claystone; rare discontinuous yellowish-grey impure dolomite and very rare dark grey carbonaceous shale. Particularly in the upper part of the unit, oil shale beds attenuate towards the east, southeast and northwest in The Narrows Graben with a corresponding increase in the commonly silty to sandy claystone. Claystone and brecciated clayey oil shale beds generally show bioturbation features, often displaying well-preserved burrows. Ostracode tests can be extremely abundant, sometimes forming thin to moderately thick beds of soft coquina. Also recorded from the Teningie Creek Member are gastropods, vertebrate remains (crocodile, turtle), fish elements and coprolites.|16-MAY-23
26168|Teningie Creek Member|Relationships and boundaries|The member is conformable with the underlying Monte Christo Member and is the conformable contact between claystone and oil shale. The upper boundary is the conformable contact between claystone and oil shale of the Ramsay Crossing Member. The member is faulted against Devonian to Carboniferous rocks of the Curtis Island Group along the western edge of The Narrows Graben.|16-MAY-23
26168|Teningie Creek Member|Age reasons|Mid to late Eocene - as for the Rundle Formation.|16-MAY-23
26168|Teningie Creek Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
26168|Teningie Creek Member|Comments|Note: Drill-core from ERD 169 is stored at Southern Pacific Petroleum's Research and Core Storage Facility located in Gladstone, Queensland.|16-MAY-23
26168|Teningie Creek Member|References|79/02402|16-MAY-23
17975|Termite Range Formation|Name source|Termite Range, a prominent topographic feature which extends from Little Creek in the south to Mitton Creek in the north in the Lawn Hill Sheet area.|16-MAY-23
17975|Termite Range Formation|Unit history|The rocks now mapped as the Termite Range Formation were previously included in the Ploughed Mountain Beds by Carter & others (1961). Cavaney (1975) originally named this unit the "Gregory Quartzite" but this name is invalid due to previous usage.|16-MAY-23
17975|Termite Range Formation|Type section locality|Holostratotype: Across the southern part of the Termite Range between 576070 (base) and 560064 (top) in the Lawn Hill 1:100 000 Sheet area. This section lies about 14 km northeast of Riversleigh homestead. It comprises three subunits, the lower (240 m) and upper (300 m) ofa which consist of massive, structureless quartzwacke, greywacke and sandstone rhythmically interbedded with siltstone. The upper subunit contains a higher percentage of massive arenite beds than the lower. The middle subunit comprises 540 m of interbedded light coloured clayey siltstone and ferruginous, coarse quartz siltstone.|16-MAY-23
17975|Termite Range Formation|Extent|The unit is best exposed in the Termite Range and in a series of domes and anticlines (such as the Ploughed Mountain anticline in the Lawn Hill Sheet area) which extend from the Gregory River near Riversleigh in the south to Elizabeth Creek in the northern part of the Bowthorn Sheet area in the north, and from Archie Creek in the east to the Constance Range escarpment in the west.|16-MAY-23
17975|Termite Range Formation|Thickness range|The unit is 1080 m thick in the type section, and has a minimum thickness of 200 m on the western flank of the Kamarga Dome.|16-MAY-23
17975|Termite Range Formation|Lithology|Outside the Termite Range area, the three-fold subdivision of the unit is not recognised. The basal subunit lenses out and the central subunit becomes indistinguishable from the underlying Riversleigh Siltstone. In the Ploughed Mountain and Caroline Range areas, approximately 550 m of greywacke, quartzwacke and sandstone with interbedded siltstone crop out. Similar lithologies crop out in a series of anticlinal structures in the eastern part of the Bowthorn Sheet area.|16-MAY-23
17975|Termite Range Formation|Relationships and boundaries|The Termite Range Formation conformably overlies the Riversleigh Siltstone and is conformably overlain by the Lawn Hill Formation. Both upper and lower boundaries are marked by a strong change in relief from low rolling hills of the Riversleigh Siltstone and Lawn Hill Formation to the high relief furrowed appearance of the Termite Range Formation. Where the basal subunit lenses out, the middle subunit is indistinguishable from the underlying Riversleigh Siltstone and is mapped as part of it on the Lawn Hill 1:100 000 Geological Map.|16-MAY-23
17975|Termite Range Formation|Age reasons|Mid Proterozoic (Carpentarian).|16-MAY-23
17975|Termite Range Formation|Proposed publication|Queensland Government Mining Journal.|16-MAY-23
17975|Termite Range Formation|References|B051|16-MAY-23
17975|Termite Range Formation|Proposer|Hutton L.J., Cavaney R.J., Sweet I.P.|16-MAY-23
25525|Tewinga Group|Name source|Tewinga County, which covers the northeastern quarter of the Prospector 1:100 000 Sheet area (6857) and extends on to the adjoining sheets to the north, northeast and east. The County surrounds the township of Kajabbi, which is located at latitude 20o02'S, longitude 140o02'E.|16-MAY-23
25525|Tewinga Group|Constituents|The Tewinga Group consists of the Leichhardt Metamorphics, the Magna Lynn Metabasalt and the Argylla Formation.|16-MAY-23
25525|Tewinga Group|Extent|The group has been mapped in the Dobbyn, Cloncurry and Duchess 4-mile Geological Sheet areas (Carter et al., 1961), but mapping of the Marraba, Mary Kathleen and Prospector 1:100 000 Sheet areas has shown the Group to be less extensive than previously mapped (Derrick et al., 1971; Derrick et al., 1974; Wilson et al., in prep.). The main exposure occurs in a north-trending belt about 30 km wide and 280 km long which extends from 70 km south of Duchess to 50 km horth of Kajabbi. West of this belt one large outcrop is present about 50 km northwest of Kajabbi and to the east several separate blocks of Tewinga Group rocks crop out as a result of faulting and/or folding. Large fold and fault blocks are also located in the Duck Creek and Bulonga Anticlines (15 to 50 km southeast of Mary Kathleen), near the Blockade copper mine (5 to 25 km northwest of Mary Kathleen), and in the contact zone of the Wonga Granite (north and south of Mary Kathleen). A smaller outcrop of Argylla Formation occurs 10 km west-northwest of Cloncurry.|16-MAY-23
25525|Tewinga Group|Thickness range|The minimum thickness of the Group is in excess of 200 m, and some sequences are at least 5000 m thick. The base of the Group is not exposed.|16-MAY-23
25525|Tewinga Group|Lithology|Metamorphosed acid and basic volcanic rocks, minor arenaceous metasediments, muscovite schists and acid to intermediate gneisses.|16-MAY-23
25525|Tewinga Group|Relationships and boundaries|No older units are known in the region. The Group is overlain unconformably or disconformably by the Mount Guide Quartzite, Eastern Creek Volcanics and Surprise Creek Beds in the west and the Ballara Quartzite and the Deighton Quartzite in the east. The Marraba Volcanics appear to overlie the Group conformably. The Group is intruded by the Kalkadoon Granite, Wonga Granite, Wimberu Granite, several swarms of dolerite dykes, and some acid porphyry bodies.|16-MAY-23
25525|Tewinga Group|Age reasons|The base of the Group is considered to be the base of the Carpentarian succession (Middle Proterozoic) in the Mount Isa/Cloncurry region. Rubidium-strontium dating of the Leichhardt Metamorphics and Argylla Formation has produced a range of dates, some of which are dubious, but a minimum age of about 1710 m.y. is probable for the Leichhardt Metamorphics (R.W. Page, BMR, pers. comm.). Published dates on the Ewen and Kalkadoon Granites which intrude the Group ranges from 1660 m.y. (Page & Derrick, 1973) to 1930 m.y. (Farquharson & Wilson, 1971). The tewinga Group has been tentatively correlated with the Cliffdale and Edith River Volcanics in Queensland and the Northern Territory, which are dated at about 1770 to 1750 m.y. old respectively (Plumb & Derrick, 1975).|16-MAY-23
25525|Tewinga Group|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
25525|Tewinga Group|Proposed publication|Queensland Government Mining Journal|16-MAY-23
25525|Tewinga Group|References|B051; 71/056; B193; 79/01431; 77/004.|16-MAY-23
27302|The Fisheries Basalt|Name source|The Fisheries crossing of the Mulgrave River (GR 641002, Bartle Frere 1:100 000 Sheet area), 11 km southwest of Gordonvale.|16-MAY-23
27302|The Fisheries Basalt|Unit history|Previously included in the Atherton Basalt by Best (1960) and de Keyser (1964).|16-MAY-23
27302|The Fisheries Basalt|Type section locality|Several basalt flows in an unnamed tributary of the Mulgrave River at GR 636997 (Bartle Frere 1:100 000 Sheet area), 800 m southwest of The Fisheries. Outcrops consist of fine-grained basalt with rare phenocrysts and vesicules. Moderately weathered basalt of a flow on the ridge crest caps completely weathered or decomposed basalt in a lower flow or flows nearer to Goldsborough Road.|16-MAY-23
27302|The Fisheries Basalt|Extent|Numerous scattered outliers restricted to the valleys of the Mulgrave River and Little Mulgrave River. Total area of exposure of about 42 km2.|16-MAY-23
27302|The Fisheries Basalt|Lithology|Dark grey, fine-grained basalt; porphyritic texture with phenocrysts of olivine and minor augite. Vesicular variants are subordinate. Some chilled olivine basalt has a glassy groundmass. Cinder or klinker material is associated with a scoria cone at an eruption centre (GR 665014) east of The Fisheries. Light to dark grey, porous travertine limestone exposed in the Little Mulgrave River valley appears to have formed on the basalt in freshwater bogs between volcanic eruptions.|16-MAY-23
27302|The Fisheries Basalt|Relationships and boundaries|The Fisheries Basalt represents part of the Atherton Volcanic Province. Lavas erupted from an assymetrical scoria cone east of The Fisheries flowed into the Mulgrave River valley, and backed up into the West Mulgrave River and Little Mulgrave River. Lavas erupted from volcanoes on the Atherton Tableland may have contributed minor amounts to the sequence by descending the escarpment via Toohey Creek and possibly Christmas Creek. The basalt flows unconformably overlie the Hodgkinson Formation and the Bellenden Ker Granite.|16-MAY-23
27302|The Fisheries Basalt|Age reasons|Uncertain, but probably Pliocene to Pleistocene (de Keyser, 1964; Stephenson & others, 1980). Considerable dissection of the lavas by the Mulgrave River suggests at least an early Pleistocene age.|16-MAY-23
27302|The Fisheries Basalt|Proposed publication|1:100 000 Geological Map Commentary, Cairns Region, Queensland. Geological Survey of Queensland.|16-MAY-23
27302|The Fisheries Basalt|References|? 60/078; R200; B084; 82/22416.|16-MAY-23
27302|The Fisheries Basalt|Category|2|16-MAY-23
18166|Timberoo Member|Name source|Timberoo mine, 8 km north of Mitakoodi siding, latitude 20o52'30"S, longitude 140o18'20"E.|16-MAY-23
18166|Timberoo Member|Geomorphic expression|Quartzite beds form low, rounded, bouldery ridges and hills, but the other rock types form pediments with abundant scree and soil cover.|16-MAY-23
18166|Timberoo Member|Type section locality|A northwest-trending section from 3 km east of the Banjo mine; i.e., latitude 20o53'S, longitude 140o13'40"E to latitude 20o52'10"S, longitude 140o13'E, 38 km west-southwest of Cloncurry, GR 6956-190905 to 6956-176907. The type section contains a steeply dipping, tightly folded sequence, about 700 m thick, of grey siltstone, calcareous sandstone, shale, phyllite, micaceous siltstone, and 1 or 2 flows of basic lava. A good reference section is present for 1 km east of Mount Sheaffe.|16-MAY-23
18166|Timberoo Member|Extent|This member has been mapped in detail in only the Marraba 1:100 000 Sheet area. The member is exposed in a folded M-shaped belt in the Duck Creek And Bulonga anticlines.|16-MAY-23
18166|Timberoo Member|Thickness range|Maximum thickness is about 750 m in the east; the unit thins markedly towards the west in the Bulonga anticline.|16-MAY-23
18166|Timberoo Member|Lithology|Grey laminated, fine-grained sandstone and siltstone predominate. Calcareous sandstone and siltstone, slate, and mica schist are common. Some of the sandstone contains abundant magnetite and hematite. Minor constituents are laminated cherty quartzite, limestone, basic lava flows, and tuffaceous sediments. Some fine-grained and ripple-marked labile quartzite displays prominent bouldery outcrop.|16-MAY-23
18166|Timberoo Member|Relationships and boundaries|The Timberoo Member is the top member of the Marraba Volcanics. It is overlain conformably by the Mitakoodi Quartzite.|16-MAY-23
18166|Timberoo Member|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
18166|Timberoo Member|Proposed publication|Queensland Government Mining Journal, 1976|16-MAY-23
18166|Timberoo Member|Name first published by|Derrick G.M., Millist G., Little M., 1976|16-MAY-23
18185|Timothy Creek Sandstone Member|Name source|Named after Timothy Creek which drains part of the outcrop area west of Dajarra, Ardmore 1:100 000 Sheet area (Urandangi 1:250 000 Sheet area).|16-MAY-23
18185|Timothy Creek Sandstone Member|Unit history|Mapped as Eastern Creek Volcanics by Noakes & others (1959).|16-MAY-23
18185|Timothy Creek Sandstone Member|Type section locality|About 17 km NW of Dajarra, from GR 314089 to GR 332104. The lower part of the member consists of mainly sericitic meta-arenite which grades up into quartzose, feldspathic, and sericitic meta-arenite and minor quartzite and rare quartz-muscovite schist in the upper part. Scattered rounded pebbles and thin pebbly beds occur in the sequence. Cross-beds and ripple marks are common in the meta-arenites and quartzites, many of which (especially the sericitic meta-arenites) are friable.|16-MAY-23
18185|Timothy Creek Sandstone Member|Extent|The member forms a NNE-trending belt of prominent ridges and hills in the E of the Ardmore 1:100 000 Sheet area, and extends N into the Oban 1:100 000 Sheet area.|16-MAY-23
18185|Timothy Creek Sandstone Member|Thickness range|The member is about 2000 m thick in the type section. It appears to be significantly thicker in the far N of the Ardmore 1:100 000 Sheet area, but the sequence has been extensively deformed there and may be folded or partly repeated by faulting, or both.|16-MAY-23
18185|Timothy Creek Sandstone Member|Lithology|The predominent lithologies in the member are similar to those described above. Minor rock types present include micaceous metasiltstone, dark grey fine-grained quartzite, fine-grained quartz-sericite schist, labile meta-arenite, and fine to medium-grained quartz-biotite-muscovite schist.|16-MAY-23
18185|Timothy Creek Sandstone Member|Relationships and boundaries|The member is overlain and underlain, apparently conformably, by mafic metavolcanics and interlayered metasediments mapped as part of the Jayah Creek Metabasalt. It is cut by numerous, mainly northerly-trending dykes and pods of metadolerite.|16-MAY-23
18185|Timothy Creek Sandstone Member|Age reasons|Precambrian, probably Proterozoic.|16-MAY-23
18185|Timothy Creek Sandstone Member|Proposed publication|Blake & others, in preparation|16-MAY-23
18185|Timothy Creek Sandstone Member|Comments|Remarks: The member forms a continuous, relatiavely thick, in most places relatively little-deformed unit. It may be equivalent to the Lena Quartzite Member of the Eastern Creek Volcanics (Derrick & others, 1976), or possibly to the Mount Guide Quartzite - the predominant rock types in the two units are very similar.|16-MAY-23
18185|Timothy Creek Sandstone Member|References|79/01220|16-MAY-23
18185|Timothy Creek Sandstone Member|Defn Reference|82/22920|16-MAY-23
18185|Timothy Creek Sandstone Member|Resdate|05-NOV-1980|16-MAY-23
24524|Tin Hill Quartzite Member|Name source|Tin Hill, a prominent hill in a range of quartzite ridges, at GR 730 163 (Forsayth 1:100 000 Sheet area), about 12.5 km west-northwest of Robin Hood homestead.|16-MAY-23
24524|Tin Hill Quartzite Member|Unit history|Previously ;mapped as an unnamed member of the Robertson River Metamorphics of White (1962) and Bain & others (1976).|16-MAY-23
24524|Tin Hill Quartzite Member|Type section locality|The southern side of Tin Hill at 730 163, about 30 m of white quartzite are exposed in the cliff face.|16-MAY-23
24524|Tin Hill Quartzite Member|Extent|Forms a series of large ridges near the Robertson River between the Forsayth-Agate Creek and Forsayth-Robin Hood roads. The unit is traceable farther east towards the Newcastle Range, but does not form any prominent topographic feature.|16-MAY-23
24524|Tin Hill Quartzite Member|Thickness range|5 to 40 m.|16-MAY-23
24524|Tin Hill Quartzite Member|Lithology|Mainly white quartzite consisting almost wholly of quartz. Some finer-grained grey quartzite is also present and minor schist is interlayered.|16-MAY-23
24524|Tin Hill Quartzite Member|Relationships and boundaries|The unit is a member of the Robertson River Formation (mainly within the "schist phase"). Although there appear to be three distinct quartzite layers, detailed mapping and structural analysis by T.H. Bell and M.J. Rubenach of James Cook University (pers. comm., 1978) have shown these to be one layer folded by isoclinal folds with roughly horizontal axes. The Tin Hill Quartzite member is within the lower part of the Robertson River Formation, but its position with respect to the Dead Horse Metabasalt Member is not yet known.|16-MAY-23
24524|Tin Hill Quartzite Member|Age reasons|Proterozoic; older than 1570 m.y. which is the age of the first deformation and metamorphic event in the Etheridge Group (Black & Others, 1978).|16-MAY-23
24524|Tin Hill Quartzite Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24524|Tin Hill Quartzite Member|References|80/20677; ? 98/29014|16-MAY-23
24524|Tin Hill Quartzite Member|Unit name|Tin Hill Quartzite Member (of Robertson River Formation)|16-MAY-23
18192|Tinaroo Granite|Name source|Tanaroo Falls Dam (GR 453015, Bartle Frere 1:100 000 Sheet area, 8063) which is adjacent to the southern edge of the unit.|16-MAY-23
18192|Tinaroo Granite|Unit history|Formerly included within the Mareeba Granite (de Keyser, 1964) but this term is now restricted to granites near Mareeba town, following Richards (1980). The term Tinaroo Batholith has been used previously by Richarads (1980) and Mancktelow (1982).|16-MAY-23
18192|Tinaroo Granite|Type section locality|Exposures in Davies Creek, for 2 km from the contact with the Hodgkinson Formation along the Davies Creek National Park road (GR 474197, Bartle Frere 1:100 000 Sheet area, 8063).|16-MAY-23
18192|Tinaroo Granite|Extent|In a north-trending batholith forming the Lamb Range and part of the catchment for Tinaroo Falls Dam. The total area of outcrop is about 300 km2.|16-MAY-23
18192|Tinaroo Granite|Lithology|Relatively uniform, white, medium to coarse-grained biotite granite which is commonly porphyritic. In places towards the margin, such as northwest of Tinaroo Falls Dam, it becomes less porphyritic, and close to the margin it is fine grained, with some small feldspar phenocrysts. Aplite veins, pegmatite veins, biotite layering and xenoliths of country rock are common near the contact, such as in Davies Creek.|16-MAY-23
18192|Tinaroo Granite|Relationships and boundaries|Intrudes the ?Mareeba Granite on the west along a sharp line, which is visible on the aerial photographs. The contact is presumed to be steeply dipping outwaards. It also intrudes metasediments of the Hodgkinson Formation and has apparently produced a metamorphic aureole up to 6 km wide within these.|16-MAY-23
18192|Tinaroo Granite|Age reasons|Mid-Permian, based on dates of 262 to 269 million years on samples from north of Tinaroo Falls Dam, and from a quarry south of the dam (Richards & others, 1966). A slightly older age is suggested by Rb-Sr dates of 284-288 million years (Black 1978).|16-MAY-23
18192|Tinaroo Granite|Proposed publication|1:100 000 Geological Map Commentary, Cairns Region, Queensland. Geological Survey of Queensland.|16-MAY-23
18192|Tinaroo Granite|References|82/22558; 82/22424; 98/29234; R200|16-MAY-23
18254|Toby Barty Sandstone Member|Name source|Toby Barty copper mine, 11 km east of Mitakoodi railway siding, and 30 km south-southwest of Cloncurry, latitude 20o57'40"S, longitude 140o24'30"E (6956 385820).|16-MAY-23
18254|Toby Barty Sandstone Member|Geomorphic expression|The member forms dissected plateaux and low hills.|16-MAY-23
18254|Toby Barty Sandstone Member|Type section locality|A section extending 0.85 km northeastwards from a point latitude 20o58'7"S, longitude 140o24'12"E (6956 380810) 1 km south-southwest of Toby Barty mine. The base is defined by the sharp change from the underlying siltstone and phyllite of the lower Marimo Slate to the fine to medium sandstone of the Member; the top of the Member is defined by the change from sandstone to grey slate and black carbonaceous slate.|16-MAY-23
18254|Toby Barty Sandstone Member|Extent|This member forms a narrow belt 1 to 2 km wide extending south-southeast from Toby Barty for at least 6 km. It occurs on the Marraba and Malbon 1:100 000 Sheet areas, which arae within the Cloncurry and Duchess 1:250 000 Sheet areas respectively.|16-MAY-23
18254|Toby Barty Sandstone Member|Thickness range|The member is about 800 m thick.|16-MAY-23
18254|Toby Barty Sandstone Member|Lithology|Fine to medium feldspathic sandstone and minor pebble conglomerate; cross-beds and ripple marks are abundant.|16-MAY-23
18254|Toby Barty Sandstone Member|Relationships and boundaries|This member is a conformable lens within the lower part of the Marimo Slate.|16-MAY-23
18254|Toby Barty Sandstone Member|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1977.|16-MAY-23
18254|Toby Barty Sandstone Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
18263|Toko Group|Name source|From Toko Range in TOBERMORY-GLENORMISTON-MOUNT WHELAN.|16-MAY-23
18263|Toko Group|Name source|(Orig. Defn) Toko Range, straddling the Queensland-Northern Territory border west of Boulia.|16-MAY-23
18263|Toko Group|Unit history|(Orig. Defn) The term Toko was first used by Whitehouse (1936) as the Toko Series which referred to a sequence of Middle Ordovician age. The sequence comprising a cephalopod-rich limestone overlain by flat lying sandstones containing asaphid trilobites occupies the Toko Ranges, westward to the Tarlton Range and beyond. There is no doubt that the sequence described as the Toko Series by Whitehouse is the upper part of the Nora Formation and the Carlo Sandstone. The Toko Series were the only Ordovician rocks known in the area at that time. In 1953, the Geological Map of Queensland used the name Toko Group for marine Ordovician rocks southwest of a line joining old Linda Downs homestead and Mount Idamea. That is, it was used for all Ordovician rocks above the Ninmaroo Formation as now defined. Casey (1959) preferred the name Toko Beds for the Early-Middle Ordovician rocks overlying the Ninmaroo Formation, but excluded an undifferentiated sandstone of either Ordovician or Devonian age. Beds were used because the formations had not yet been named. Pritchard (1960) followed Casey's usage although his informal unit Om-11, which is partly equivalent to the undifferentiated sandstone of Casey, is included within the Toko Beds. Following the naming of the constituent units, Casey (in Smith, 1963) proposed the term Toko Group to include the Kelly Creek Formation, Coolibah Formation, Nora Formation, Carlo Sandstone and Mithaka Formation, but subsequently (Casey in Smith, 1965), the Kelly Creek Formation was deleted from the Group. Smith (1972) in the major publication on the stratigraphy of the Georgina Basin accepted the latter. Recently, the recognition of the Ethabuka Sandstone (Draper, in preparation) has resulted in a need to redefine the Toko Group. The inclusion of the Ethabuka Sandstone in the Group is based on lithological similarities with the underlying units. Unit Om-11 of Pritchard is equivalent to the Ethabuka Sandstone (Draper, in preparation) and was placed in the Toko Beds by him. Therefore, on both lithological and on historical grounds the Ethabuka Sandstone is placed in the Toko Group. The depletion of the Coolibah Formation from the Toko Group is based on purely lithologic grounds. The Coolibah Formation (Casey, in Smith, 1965) is dominantly a carbonate unit with the carbonates generally being fine grained and of algal origin (Shergold & others, 1976). On the other hand, the Nora Formation and the overlying units are siliciclastic except for some skeletal limestones in the Nora Formation, which is transgressive on the Coolibah Formation. It is therefore considered that the Coolibah Formation does not have sufficient lithological features in common with the Nora Formation and the overlying units to warrant its inclusion in the Toko Group. The Toko Group is hereby redefined to exclude the Coolibah Formation.|16-MAY-23
18263|Toko Group|Unit history|(2003 Defn) This new definition of the Toko Group is basically a return to the concept of the Toko Series of Whitehouse (1936) who applied the name to dominantly clastic rocks overlying dominantly carbonate rocks.  Toko Series (Whitehouse 1936); lower-medial portion of Dulcie Sandstone of Joklik (1955) in part; units Ol-6 to Ol-8 and Om-9 to Om-11 of Pritchard (1960) in part; Ethabuka beds (Mulready 1975) in part; Withillindarmna Dolostone Member (Radke and Duff 1980) in part.|16-MAY-23
18263|Toko Group|Constituents|Kelly Creek Formation, Coolibah Formation, Nora Formation, Carlo Sandstone, Mithaka Formation, Ethabuka Sandstone.|16-MAY-23
18263|Toko Group|Constituents|(Orig. Defn) The Toko Group comprises, from top to bottom: Ethabuka Sandstone (Draper, in preparation); Mithaka Formation, Carlo Sandstone, Nora Formation (Casey, in Smith, 1963).|16-MAY-23
18263|Toko Group|Extent|(Orig. Defn) The Toko Group rocks constitute the scarp, plateau and internal hills of the Toko Range. It is also present in the associated Toomba Range and in the Tarlton Range in the Northern Territory where the upper part of the Group is eroded. The Nora Formation is also present in the Dulcie Range further west. In the subsurface, it is known from the Toko Syncline.|16-MAY-23
18263|Toko Group|Extent|BARROW CREEK, ALCOOTA, ELKEDRA, HUCKITTA, TOBERMORY, HAY RIVER, MOUNT WHELAN, GLENORMISTON.|16-MAY-23
18263|Toko Group|Thickness range|(Orig. Defn) The maximum known thickness is 1678 m in AOD Ethabuka No. 1, although the upper part may have been eroded.|16-MAY-23
18263|Toko Group|Lithology|(Orig. Defn) Quartzose sandstone, commonly containing clay pellets, siltstone and mudstone. Skeletal limestones are present in the Nora Formation; these brachiopod-rich limestones contain numerous cephalopod fossils.|16-MAY-23
18263|Toko Group|Fossils|(Orig. Defn) A prolific and varied fauna is found throughout the group particularly within the Nora and Mithaka Formations. The fauna includes trilobites, nautiloids, brachiopods, pelecypods, rostroconchs, conodonts, gastropods, Receptaculites, sponge spicules, bryozoa, fish, chitinozoans, and ostracods. Abundant ichnofossils are present.|16-MAY-23
18263|Toko Group|Relationships and boundaries|(Orig. Defn) The group conformably overlies the Coolibah Formation and is conformably overlain by either the Devonian Cravens Peak Beds or Mesozoic rocks. The Ordovician sequence in the Toko Range area is, from top to bottom: Ethabuka Sandstone; Mithaka Formation; Carlo Sandstone; and Nora Formation (Toko Group). Coolibah Formation; Kelly Creek Formation; Ninmaroo Formation.|16-MAY-23
18263|Toko Group|Relationships and boundaries|Conformably overlies Tomahawk Formation, conformably to locally disconformably (Reynolds 1968, Jones et al 1971) overlies Ninmaroo Formation (both of Cockroach Group) or where these are absent, unconformably overlies Georgina Limestone of Narpa Group. Unconformably overlain by Cravens Peak beds (Devonian) or where these are absent, Mesozoic sedimentary rocks.|16-MAY-23
18263|Toko Group|Age reasons|(Orig. Defn) Based on various faunal studies, the age ranges from Lower Ordovician (Arenik) for the Nora Formation (Shergold & othes, 1976) to Middle Ordovician for the Ethabuka Sandstone (Draper, in preparation).|16-MAY-23
18263|Toko Group|Age reasons|Conodonts suggest late Late Cambrian (late Datsonian; Jones et al 1971) or early Early Ordovician (early Warendian; Druce in Shergold 1978, revised according to Shergold and Nicoll 1992) age for basal Kelly Creek Formation. Diverse but largely undescribed fauna of Ethabuka Sandstone suggests a Middle Ordovician (late Llanvirnian) age (Shergold 1985).|16-MAY-23
18263|Toko Group|Correlations|Pacoota Sandstone, Horn Valley Siltstone, Stairway Sandstone, Stokes Siltstone, Carmichael Sandstone of Amadeus Basin, Djagamara Formation and Kerridy Sandstone of Ngalia Basin, Hanson River beds of Wiso Basin (Webby et al 1981, Shergold et al 1985).|16-MAY-23
18263|Toko Group|Proposed publication|Queensland Government Mining Journal|16-MAY-23
18263|Toko Group|Comments|Casey (in Smith 1963a), Smith (1972) and Draper (1980b) have outlined the nomenclatural history of the Toko Group. The original Toko Series of Whitehouse (1936) was intended to encompass all Ordovician rocks (at that time unnamed) west of Boulia, Queensland. Following subdivision and naming of the succession, Casey (in Smith 1963a) assigned the Kelly Creek Formation to Mithaka Formation inclusive to the Toko Group. Subsequently, Casey (in Smith 1965) excluded the Kelly Creek Formation. Draper (1980b) additionally excluded the Coolibah Formation and included the Ethabuka Sandstone. Webby et al (1981) rejected Draper's (1980b) proposals and retained the conception of Casey (in Smith 1965), and this was followed by Kruse et al (2002a). The present conception of the group is thus the most inclusive yet advanced, but accords with the intentions of Whitehouse (1936). The Kelly Creek Formation is included in the Toko Group rather than the Cockroach Group because of its Ordovician age, and because of its reported local basal disconformity (Reynolds 1968, Jones et al 1971).|16-MAY-23
18263|Toko Group|References|81/21354; 98/29187; 79/03925; 98/29337; 98/29478; B111.|16-MAY-23
18263|Toko Group|State(s)|QLD & NT|16-MAY-23
26176|Tommy Creek Microgranite|Name source|Tommy Creek, 25 km west of Cloncurry latitude 20o42'S, longitude 140o15'45"E (6956 233107), flows northeast through the main areas of the Microgranite.|16-MAY-23
26176|Tommy Creek Microgranite|Geomorphic expression|Moderately rugged hills, ridges and dissected plateaux, separated by valleys containing metaedments of the Corella Formation.|16-MAY-23
26176|Tommy Creek Microgranite|Type section locality|In the vicinity of the Pinnacles, 25 km west of Cloncurry, latitude 20o40'S, longitude 140o15'E (6956 221147), where white to pink sheared biotite-flecked fine-grained acid porphyries are exposed.|16-MAY-23
26176|Tommy Creek Microgranite|Extent|The Tommy Creek Microgranite covers approximately 100 km2 in the Marraba 1:100 000 Sheet area. It occurs mostly to the north of the Barkly Highway from 20 to 40 km west of Cloncurry.|16-MAY-23
26176|Tommy Creek Microgranite|Thickness range|The unit forms sills which range from 400 m to 1 km in thickness.|16-MAY-23
26176|Tommy Creek Microgranite|Lithology|Fine-grained to aphanitic microgranite containing phenocrysts up to 3 mm long of quartz, plagioclase and potash feldspar. The groundmass is composed almost entirely of quartz and potash feldspar. The unit is described by Derrick et al. (1971).|16-MAY-23
26176|Tommy Creek Microgranite|Relationships and boundaries|The Tommy Creek Microgranite is intrusive into the middle unit of the Corella Formation (Derrick et al., 1971); most contacts are grossly concordant but locally discordant.|16-MAY-23
26176|Tommy Creek Microgranite|Age reasons|Proterozoic. The sills are younger than the Corella Formation which overlies the Tewinga Group for which there is a minimum age of 1770 m.y. (Pagae, 1976a).|16-MAY-23
26176|Tommy Creek Microgranite|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1978|16-MAY-23
26176|Tommy Creek Microgranite|Proposed publication|Queensland Government Mining Journal, 79 (1978)|16-MAY-23
26176|Tommy Creek Microgranite|Comments|Discussion: The microgranite is easily misidentified as a sheared feldspathic quartzite but it lacks any sedimentary structures and commonly has phenocrysts set in a very fine-grained quartzo-feldspathic mosaic. This texture is more typical of a volcanic rather than an intrusive rock and it is probable that the Tommy Creek Microgranite is a sub-volcanic equivalent of a deeper-seated acid intrusion such as the Naraku Granite, which crops out about 10 km to the northeast. Some of the ;Microgranite may represent acid lavas or tuffs that were cogmagmatic with the intrusion. The Tommy Creek Microgranite was previously mapped as Naraku Granite in the Pinnacles area, Chumvale Breccia in an area 3 to 6 km northwest of Butcher Bore, and in other areas it was not differentiated from the Corella Formation.|16-MAY-23
26176|Tommy Creek Microgranite|Defn approved by|Queensland Sub-Committee|16-MAY-23
26176|Tommy Creek Microgranite|Name first published by|Glikson A.Y., Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
18370|Toole Creek Volcanics|Name source|Toole Creek, 20 km southeast of Cloncurry, latitude 20o50'S, longitude 140o40'E, i.e. (7056 665965).|16-MAY-23
18370|Toole Creek Volcanics|Geomorphic expression|This formation forms low rounded bouldery ridges and hills.|16-MAY-23
18370|Toole Creek Volcanics|Type section locality|The proposed type section is the eastern end of the section which was used by Carter et al. (1961) in defining the Soldiers Cap Formation. It is about 32 km southeast of Cloncurry and extends for 4.5 km from a point at latitude 20o54'40"S, longitude 140o43'30"E (7056 713875) to a point on Weatherly Creek at latitude 20o53'40"S, longitude 140o45'30"E (7056 750895). The base (western end) of this type section is marked by a thin belt of amphibolite that is probably; metabasalt. It is overlain by 750 m of alternating metabasalt and metasediment, mainly metasiltstone, slate and some chert. This sequence is overlain by 1000 m of metasiltstone, slate, chert, and quartzite, then 300 m of metabasalt, 300 m of metasiltstone, slate, chert and quartzite, and at the eastern end of the section, about 500 m of chert and pelitic metasediments containing several bands of amphibolite. The top of the formation is not exposed in the type section.|16-MAY-23
18370|Toole Creek Volcanics|Extent|The Toole Creek Volcanics are exposed in a complex, tighly folded, wedge-shaped zone that extends 25 km east and 50 km southeast from Cloncurry. Most of this formation is in the Cloncurry 1:100 000 Sheet area and has been delineated by Glikson & Derrick (1970). The southern extension into the Mount Angelay 1:100 000 Sheet area has been interpreted mainly from air-photographs (Glikson, 1972), and occurs in a belt flanking the Fullarton River.|16-MAY-23
18370|Toole Creek Volcanics|Thickness range|The formation is at least 2800 m thick.|16-MAY-23
18370|Toole Creek Volcanics|Lithology|Metabasalt, metadolerite, ortho-amphibolite, metasiltstone, phyllite, slate, feldspathic sandstone, chert, jaspilite, and calc-silicate rocks.|16-MAY-23
18370|Toole Creek Volcanics|Relationships and boundaries|The Toole Creek Volcanics are underlain conformably by the Mount Norna Quaratzite and overlain unconformably by the Corella Formation, the Roxmere Quartzite, and Mesozoic strata. The formation is intruded by dolerite, the Naraku Granite and the Williams Granite.|16-MAY-23
18370|Toole Creek Volcanics|Age reasons|Precambrian, probably Carpentarian (Middle Proterozoic).|16-MAY-23
18370|Toole Creek Volcanics|Proposed publication|Queensland Government Mining Journal|16-MAY-23
18370|Toole Creek Volcanics|Comments|Remarks: Honman (1939) included this unit in his Upper or Volcanic stage of the Soldiers Cap series. Carter et al. (1961) recognised this sequence of "interbedded metabasalt, cherty quartzite, chert and slate" but did not formally define it as a subdivision of the Soldiers Cap Formation. The name Toole Creek metavolcanics was used as an informal stratigraphic term by Glikson (1972). The formal name proposed here is Toole Creek Volcanics, which is consistent with the usage of Volcanics in naming other basic metavolcanic units in the region e.g. Eastern Creek Volcanics and Marraba Volcanics (Carter et al., 1961). These three stratigraphic units are considered to be broadly correlative. The topmost 800 m of mainly metasedimentary rocks in the upper part of this formation were previously mapped as the Mount Norna Quartzite in an area 15 to 20 km east-northeast of Cloncurry township (Glikson & Derrick, 1970; Glikson, 1972). In this area the upper Toole Creek Formation sequence of iron formation and siltstone; greywacke, feldspathic quartzite and minor basalt; and topmost stromatolitic chert, jaspilite and calcareous shale are now thought to be lateral equivalents of the upper Marraba Volcanics, Mitakoodi Quartzite and Overhang Jaspilite, respectively.|16-MAY-23
18370|Toole Creek Volcanics|References|B051; 79/01757; 70/024.|16-MAY-23
18375|Toolebuc Formation|Type section locality|Casey (1959) nominated a type area "on the Boulia-Winton main road 7 miles east of Hamilton" in the Boulia 1:250 000 Sheet area, and a reference section "6 miles east of Spring Creek artesian bore". Unfortunately due to an error in the geographic location of this reference section it cannot be relocated. Casey (pers. comm.) agrees an alternate section be defined as the type section of this unit. Because of poor exposure of this unit a drill hole section near Casey's (1959) type area is proposed as the type section.|16-MAY-23
18375|Toolebuc Formation|Identifying features|Introduction: The late Albian Toolebuc Member of the Wilgunya Formation was defined by Casey (1959) from the Boulia area of the northwest Eromanga Basin. Vine et al. (1967) upgraded the member to Toolebuc Limestone. Smart (1972) discussed the Toolebuc Limestone in some detail and showed that it is a heterogenous unit and that "Toolebuc Formation" would be a more appropriate name, although he did not rename it. The present authors agree with Smart (1972) that the formation is heterogeneous, and recent drilling by the BMR (Senior & Smart, 1973; Burger 1974) has confirmed that limestone is subordinate to calcareous and bituminous siltstone, black labile sandstone, and shale. Limestone is in fact absent in some areas (Williamson, 1967; D. Senior, 1971). Accordingly we propose the name TOOLEBUC FORMATION for the calcareous heterogeneous sequence which overlies the Wallumbilla Formation and underlies the Allara Mudstone. Definition: The type section of the Toolebuc Formation is designated as the sequence between 25.3 and 35.8 m in stratigraphic drill hole BMR Boulia 3A. The hole was drilled 13.7 km east of Hamilton, about 100 m north of the Boulia-Winton Highway. (Type section/hole location 22o47'00"S, 140o43'30"E). The sequence consists of black mudstone with a few thin limestone beds and shell fragments down to 30.5 m, and hard concretionary limestone and thin crystalline limestone beds interbedded with soft black mudstone down to 35.8 m. The core is available for inspection at the Bureau of Mineral Resources Core and Cuttings Laboratory, Fyshwick, ACT.|16-MAY-23
18375|Toolebuc Formation|Proposed publication|The Toolebuc and Cadna-owle Formations in the Eromanga Basin Queensland. Queensland Government Mining Journal.|16-MAY-23
18375|Toolebuc Formation|References|74/039; 79/03899; 79/03993; 79/04481.|16-MAY-23
18375|Toolebuc Formation|Status|1|16-MAY-23
18404|Toondahra Granite|Unit history|The unit was mapped initially by Withnall (1971) as part of a honours thesis in the southern part of the Munduberra 1: 250 000 Sheet area.  The unit was included on the Munduberra 1:250 000 map Sheet (Whitaker & others, 1974).|16-MAY-23
18404|Toondahra Granite|Geomorphic expression|The unit is characterised by a very strongly developed pattern of north-east and north-west joints.  The northern part of the unit (north-west of Manar homestead) forms high resistant hills.  This photopattern is typical of tin granites in Queensland (similar to the Elizabeth Creek Granite in North Queensland, and the Crows Nest Granite to the south).  The unit contains topographically flat areas (due to weathering) at the top of the range about 5 km north-west of Manar.  In this area the vegetation is dominated by grass trees (Xanthorrea sp. And paperbarks (Melaleuca sp.).  Callitrus sp with local ironbark dominates vegetation adjacent to the Boyne River in this unit north of Boondooma Dam.  This vegetation is associated with either rhyolite or microgranite exposures.|16-MAY-23
18404|Toondahra Granite|Extent|The unit occurs adjacent to outcrop of Aranbanga Volcanic Group rocks on the Munduberra sheet and extends south into the northeastern part of the Bondooma 1:100 000 Sheet area.  Outcrop of the unit extends west into the Allies Creek area.|16-MAY-23
18404|Toondahra Granite|Lithology|The main part of the unit granite (Rgto) is most commonly fine or fine to medium grained, pink in colour (varying locally to grey or cream), equigranular and leucocratic, containing small amounts (~ 3% or less) of very fine biotite and rarely blue-green hornblende. Chlorite -epidote alteration is common in places. Textures show local variation, ranging from medium to coarse-grained equigranular varieties, to inequigranular varieties with either coarse quartz aggregates or phenocrysts in a finer grained matrix, or feldspar phenocrysts in a microgranitic matrix. In thin section, the granites commonly display well-developed graphic intergrowth textures between quartz and alkali feldspar.  A very fine-grained, locally flow banded porphyritic microgranite phase has been mapped east of Allies Creek (subunit Rgtof). Some of the microgranites east of Allies Creek village display columnar jointing.The granite body east of Allies Creek displays prominent north-south jointing and shearing in places, and is intruded by sporadic massive to flow banded porphyritic rhyolite dykes near its margin. The dykes are also common in the adjacent country rock. In the northeastern part of the BOONDOOMA the unit comprises tor exposure of altered pink granite.  Considerable areas of altered microgranite and rhyolite are present immediately north of Boondooma Dam where they are associated with rhyolitic ignimbrite and dyke swarms of mainly rhyolitic in composition.  These units are probably part of the outlier of the Aranbanga Volcanic Group.  The area east of Manar homestead is composed mainly of intercalated microgranite cut by rhyolite dykes that are locally sparsely porhyritic and strongly flow-banded........... The dykes also locally show a vegetation anomaly; for example at AMG 346839 7112002 a change from mainly Eucalyptus crebra to Callitris is coincident with rubbly outcrop of mariolitic cavities in sparsely k-feldspar-phyric microgranite. Rhyolite dykes intrude brecciated granite containing granite clasts in darker green groundmass are associated with higher magnetic response at AMG 336366, 7119250.Coarse-grained biotite granodiorite forms pavements associated with flow-banded rhyolite at AMG 337927 7116808.  Very fine to medium to coarse granite and biotite microgranite with minor xenoliths occurs at AMG 348431, 7116964...........................Outcrop of a discrete body of relatively fresh tonalite at AMG 338083, 7120980 near Manar homestead comprises mainly quartz and plagioclase (30 and 40 % respectively) with minor K-feldspar (5% untwinned), biotite and hornblende (trace).  The biotite and hornblende are altered to chlorite.  Apatite is a minor accessory.Kaolinised and decomposed granite are present at AMG 327509, 7110838 and 329703, 7114892.  Exposures of light grey to white even grained biotite with minor rhyolite were noted at 329852, 7113906 and 338118 7119923.|16-MAY-23
18404|Toondahra Granite|Relationships and boundaries|The unit is intruded by unit Rid, and is probably comagmatic with rhyolite ignimbrite of the Aranbanga Volcanic Group.|16-MAY-23
18404|Toondahra Granite|Comments|GEOPHYSICAL EXPRESSION:: The unit has a strong radiometric signature in the ternary K-Th-U image (close to white being high in all channels).  It has a generally low magnetic response in the aeromagnetic data and a generally low magnetic susceptibility.  High magnetic susceptibility associated with the unit is caused by later intrusions of dacite (see unit Rid).MINERLISATION:: Crossing Rocky Creek adjacent to tin workings described by Ball (1903) is on strongly jointed rhyolite at AMG 322523, 7118930.  Along Rocky Creek is a large hill from operations conveyor belts, tyre dump (trucks) mound to 6m; large pits at AMG 165 7119005, mullock heaps along creek westwards for about 200m.  Outcrop of granite, pegmatite and microgranite at AMG 325393.|16-MAY-23
18438|Torpedo Creek Quartzite|Name source|Torpedo Creek which joins Gunpowder Creek at 6758-300293.|16-MAY-23
18438|Torpedo Creek Quartzite|Unit history|Rocks now mapped as Torpedo Creek Quartzite have previously been assigned to the Gunpowder Creek Formation, Mingera Beds, Judenan Beds, Ploughed Mountain Beds and Myally Beds by Carter & others (1961).|16-MAY-23
18438|Torpedo Creek Quartzite|Type section locality|Holostratotype: On Torpedo Creek, approximately 750 m west of the Mammoth Mine to Mount Oxide road at 6758-273321. The section consists of about 120 m of massive, medium-grained white orthoquartzite.|16-MAY-23
18438|Torpedo Creek Quartzite|Extent|It crops out extensively in the Mammoth Mines, Kennedy Gap and Mount Oxide 1:100 000 Sheet areas and around the Kamarga dome in the Lawn Hill 1:100 000 Sheet area.|16-MAY-23
18438|Torpedo Creek Quartzite|Thickness range|The unit is approximately 120 m thick in the type section. Its thickness varies markedly along strike ranging from 0 to 150 m.|16-MAY-23
18438|Torpedo Creek Quartzite|Lithology|The unit is generally medium-grained white orthoquartzite, but locally it contains basal conglomerate. Pseudomorphs after gypsum occur locally in the orrthoquartzite.|16-MAY-23
18438|Torpedo Creek Quartzite|Relationships and boundaries|The Torpedo Creek Quartzite is conformably overlain by siltstone of the Gunpowder Creek Formation. The unit unconformably overlies several units, mainly the Surprise Creek Formation, Myally Subgroup, Fiery Creek Volcanics, Carters Bore Rhyolite, Eastern Creek Volcanics and Leander Quartzite. The Torpedo Creek Quartzite is difficult to identify when it concordantly overlies quartzites of the Surprise Creek Formation and Myally Subgroup.|16-MAY-23
18438|Torpedo Creek Quartzite|Age reasons|Mid Proterozoic (Carpentarian)|16-MAY-23
18438|Torpedo Creek Quartzite|Defn author|Hutton L.J., Cavaney R.J., Sweet I.P. 1981.|16-MAY-23
18438|Torpedo Creek Quartzite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
18438|Torpedo Creek Quartzite|References|Carter, E.K., Brooks, J.H., Walker, K.R. 1961. The Precambrian mineral belt of North-western Queensland. BMR Bulletin 51. Name first published in: Derrick G.M., Wilson I.H., Hill R.M., 1976.|16-MAY-23
24534|Townley Formation|Name source|Parish of Townley, County of Gilbert; also Townley Creek, which joins the Gilbert River at GR 7560-462316 and crosses much of the unit.|16-MAY-23
24534|Townley Formation|Unit history|White (1965) included the rocks now defined as Townley Formation in his "Etheridge Formation".|16-MAY-23
24534|Townley Formation|Geomorphic expression|Variable; ranges from subdued to gently or moderately hilly, generally with differential weathering and erosion picking out fairly well defined lithological layering in many areas, but not as marked as in the Heliman Formation.|16-MAY-23
24534|Townley Formation|Type section locality|Along a tributary of Black Gin Creek from its head at GR 7560-290446 downstream to -275448. The section consists of white to grey sericitic or lithic-quartz siltstone and fine sandstone with minor (a few percent) quartzose siltstone and sandstone (cf. Heliman Formation). Blocky-jointed carbonaceous siltstone is common in the middle of the unit. Thickness in the type section is about 1400 m, but is difficult to determine more precisely because of the variable dips.|16-MAY-23
24534|Townley Formation|Extent|The formation crops out in a generally northerly trending, strongly folded belt that extends from the Reedy Creek area (GR 7560-300150 approx.) and "North Head" homestead to "Riverview" homestead (GR 7561-310770 approx).|16-MAY-23
24534|Townley Formation|Thickness range|The unit ranges from 400 m to about 1500 m thick, but complex folding prevents determination of thickness in many areas, especially in the Mosquito Creek-Mount Clark area.|16-MAY-23
24534|Townley Formation|Lithology|Generally as in the type section; the dominant siltstone and fine sandstone are locally carbonaceous, and there is a basal sequence of white laminated sericitic siltstone and sandstone which is locally gossanous in weathered outcrops.|16-MAY-23
24534|Townley Formation|Relationships and boundaries|Conformably overlies Robertson River Formation. The base is defined by the change from dominantly carbonaceous siltstone and shale to white to light grey fine sericitic quartz sandstone and siltstone. Conformably overlain by the Heliman Formation which contains a much higher proportion of resistant siliceous beds and is topographically more prominent. Intruded by Forsayth Granite, Gongora and Carnes Granodiorites, Prestwood Microgranite, and several small stocks of Carboniferous microgranodiorite porphyry.|16-MAY-23
24534|Townley Formation|Age reasons|Probably mid-Proterozoic; a minimum age of 1570+/-30 m.y. can be inferred from dating in underlying rocks (Robertson River Formation) of a deformation-metamorphism event (Black et al., in press) which has affected the Townley Formation. The unit is intruded by granitic rocks closely similar to the type Forsayth Granite, for which a preliminary isotopic age of 1600 m.y. has been obtained (L P Black, pers. comm., 1978).|16-MAY-23
24534|Townley Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24534|Townley Formation|References|80/20677; B071|16-MAY-23
24534|Townley Formation|Proposer|Withnall I.W.|16-MAY-23
79125|Tozer Basalt Member|Name source|After Tozer Street near the Gympie Railway Station.|16-MAY-23
79125|Tozer Basalt Member|Unit history|First used informally as Tozer volcanics by Gympie Eldorado Gold Mines at Monkland Mine and subsequently referred to by Cranfield (1999), Sivell & Arnold (1999), Sivell & McCulloch (2001), Li & others (2015).|16-MAY-23
79125|Tozer Basalt Member|Type section locality|Exposed on the lowest level of the Municipal quarry west of Laurenceson Road at MGA 469005mE; 7098990mN. Lat: -26°13'42" Long: 152°41'23" Permission is required on site to enter the quarry.  Reference drill hole at the Zillmere core library in Brisbane is GEGM drill hole G215, 126.9-178 m (MGA 467424mE; 7101493mN, Lat: -26°12'21"  Long: 152°40'26").|16-MAY-23
79125|Tozer Basalt Member|Extent|Apart from the quarry in Six Mile Block flows, sills and dykes are well developed in the deeper levels of Monkland Mine and are recorded through the Dawn Block though not shown on the map.|16-MAY-23
79125|Tozer Basalt Member|Thickness range|The lavas occur intermittently over a vertical interval of about 100 m. The intrusive Tozer basalts occur as dykes, sills and plugs, ranging from 1 cm to 100 m wide.|16-MAY-23
79125|Tozer Basalt Member|Lithology|Both the flows and dykes are massive green basalts commonly containing coarse clinopyroxene phenocrysts up to 8 mm in diameter (Photograph 22). These basalts appear to equate to the ankaramite described as 'Highbury ankaramite' by Sivell & Arnold (1999) in which they identify the pyroxene as chrome diopside. They are similar in composition to the Mary Basalt but are probably extruded in a deeper marine environment as they lack both flow tops and hematite, and some are flanked by proximal hyaloclastites. The lavas can be amygdaloidal. Internal jigsaw breccias are recorded inside flow margins with alteration of finer shards to pale green chert. Pillows are not common but fragmented quenched rims are found. Lavas and dykes can be very similar and are only readily recognised in cross sections. Dykes and sills are partly amygdaloidal and contain about 10% 1-6 mm pyroxene phenocrysts. Dark chlorite occurs on fractures and in amygdales. Chilled margins are often quenched and occasionally peperitic.|16-MAY-23
79125|Tozer Basalt Member|Relationships and boundaries|The lavas occur at the base of the Mary Basalt and as flows near the top of the Hall Clastics where they are flanked by hyaloclastite.  On the north side of the lowest bench in the municipal quarry the relatively massive basalt dips at about 30-40° beneath disrupted Mary Basalt, suggesting it may be a sill.  The Tozer intrusions have probably fed both the Tozer and Mary lavas and they occur throughout the stratigraphic package below the Mary basalts but never above it. Feeder dykes and sills to these lavas occur throughout the underlying Dawn Formation.|16-MAY-23
79125|Tozer Basalt Member|Geochemistry|Sivell and McCulloch (2001) interpret the basalt dykes through Dawn Formation, the Tozer basalt in Hall Clastics, and the Mary Basalt as island-arc tholeiites with distinctive island-arc signatures.|16-MAY-23
79125|Tozer Basalt Member|Defn author|Pat Stidolph, retired, ex- Gympie Eldorado Gold Mines (GEGM), Monkland Mine, Gympie, 12-JAN-2017.|16-MAY-23
79125|Tozer Basalt Member|References|Cranfield, L.C., 1999: Gympie Special Sheet 9445, Part 9545, Queensland 1:100,000 Geological Map Commentary. Queensland Department of Mines and Energy, Brisbane.  **Sivell, W.J. and Arnold, G.O. 1999: Geochemical and volcanic stratigraphy of a segment of an island arc - Gondwana rim accretion zone, Gympie Province, southeast Queensland.  In Flood, P.G. (Editor): Regional Geology, Tectonics and Metallogenesis, New England Orogen, NEO '99 Conference, 255-266.  **Sivell, W.J. and McCulloch, M.T. 2001: Geochemical and Nd-isotopic systematics of the Permo-Triassic Gympie Group, southeast Queensland.  Australian Journal of Earth Sciences 48, 377-394.  **Li, P., Rosenbaum, G., Yang, J-H. and Hoy, D. 2015. Australian-derived detrital zircons in the Permian-Triassic Gympie terrane (eastern Australia): Evidence for an autochthonous origin. Tectonics, 34, 858-874.|16-MAY-23
26962|Tungi Creek Granodiorite|Name source|From Tungi Creek at GR 5638 6900 in the Gympie 1:250 000 Sheet area SG 56-10.|16-MAY-23
26962|Tungi Creek Granodiorite|Type section locality|The type area is along the headwaters of Yabba Creek east of Jimna, grid reference 56206872 to grid reference 56786874.|16-MAY-23
26962|Tungi Creek Granodiorite|Extent|The unit crops out over approximately 110 km2 in an oval shaped area. The western edge is 2 km east of Jimna grid reference.|16-MAY-23
26962|Tungi Creek Granodiorite|Lithology|The rock is a medium to coarse-grained, light grey, hornblende-biotite granodiorite.|16-MAY-23
26962|Tungi Creek Granodiorite|Relationships and boundaries|The unit intrudes undifferentiated Palaeozoic rocks, undifferentiated Palaeozoic Bunya Phyllite, and Carboniferous to Permian Amamoor Beds.|16-MAY-23
26962|Tungi Creek Granodiorite|Age reasons|The unit was dated radiometrically (K/Ar) at 221 m.y. or Early to Middle Triassic. However, because of the proximity to granitic bodies which are in part as old as Late Permian, the age of the Tungi Creek Granodiorite is considered to be Permo-Triassic.|16-MAY-23
26962|Tungi Creek Granodiorite|Proposed publication|Report of the Geological Survey of Queensland|16-MAY-23
26962|Tungi Creek Granodiorite|Name first published by|Geological Survey of Queensland 1975.|16-MAY-23
24052|Turrets Formation|Name source|Parish of Turrets, County of Philp (Clarke River 1:250 000 Cadastral map).|16-MAY-23
24052|Turrets Formation|Unit history|Previously mapped as part of the Bundock Creek Formation (now Group) by White (1959, 1962, 1965), and the lowermost part of the 'upper' Bundock Creek Formation by Wyatt & Jell (1980).  The name was first published and described by Withnall & others (1988), but not formally defined.|16-MAY-23
24052|Turrets Formation|Geomorphic expression|The thick sandstone units form a series of distinct ridges, separated by more recessive, gullied areas corresponding to the finer grained interbeds.  It is covered by a variety of generally stunted eucalypts.  It contrasts strongly with the subdued topography of the shale-dominated Teddy Mount formation and their mutual boundary is easily photo-interpreted.|16-MAY-23
24052|Turrets Formation|Type section locality|From 7859 530460 (base) in the Broken River to 518463 (top) in Montgomery Creek, where the unit is 770 m thick.  The grid reference is based on the AGD66 datum.|16-MAY-23
24052|Turrets Formation|Description at type locality|A sinuous folded belt from near 'Gregory Springs' in the southwest to near 'Pandanus Creek' in the northeast. Also in the northwest near 'Oak Valley'.|16-MAY-23
24052|Turrets Formation|Thickness range|Up to 840 m on the northern limb of the Boroston Syncline, 560 m on the northern limb of the Montgomery Creek Anticline, and 430 m in the Six Mile Syncline.  It ranges from 100 to 480 m in the Dip Creek Syncline where it onlaps over the Bulgeri Formation onto the Dip Creek Limestone.|16-MAY-23
24052|Turrets Formation|Lithology|Feldspathic to lithofeldspathic (locally volcaniclastic) sandstone, mudstone, lesser conglomerate, and reworked tuff, as described in the type section.  The sandstone and conglomerate contain cross-bedding, horizontal planar laminae, parting lineation, bioturbation, rootlets.|16-MAY-23
24052|Turrets Formation|Fossils|The unit contains abundant plant remains, mostly of calamitean affinities.|16-MAY-23
24052|Turrets Formation|Relationships and boundaries|Conformably overlies the Bulgeri Formation, and is distinguished from the latter by the lack of redbeds.  In the Dip Creek Syncline, the Turrets Formation onlaps the Bulgeri Formation, and unconformably overlies the Dip Creek Limestone of the Broken River Group.  The base is under a unit of white, thick-bedded, pebbly, quartzose sandstone and conglomerate.  The Turrets Formation is conformably overlain by the Teddy Mount Formation, which is distinguished by being more shaley and containing thinner bedded, more widely spaced sandstone beds.  It is intruded by the Carboniferous or ?Permian Montgomery Range Igneous Complex.|16-MAY-23
24052|Turrets Formation|Age reasons|It is probably Famennian in age, because of its stratigraphic position.|16-MAY-23
24052|Turrets Formation|References|WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36; 5(11), 26-28. **WHITE, D.A., 1962:  Clarke River - Qld E/55-13.  Bureau of Mineral 	Resources, Australia 1:250 000 Geological Series Explanatory Notes.  **WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. **WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R. & DRAPER, J.D., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5. **WYATT, D.H. & JELL, J.S., 1980:  Devonian and Carboniferous stratigraphy of the northern Tasman Orogenic Zone in the Townsville hinterland.  In. Henderson, R.A. & Stephenson, P.J. (editors), The Geology and Geophysics of Northeastern Australia.  Geological Society of Australia, Queensland Division, Brisbane, 201-228.|16-MAY-23
26329|Twiddler Hill Basalt|Name source|The symmetrical double cone forming Twiddler Hill (GR 443 179, Bartle Frere 1:100 000 Sheet area, 8063), 12 km ESE of Mareeba, Queensland.|16-MAY-23
26329|Twiddler Hill Basalt|Unit history|Previously included in the Atherton Basalt by Best (1960) and de Keyser (1964).|16-MAY-23
26329|Twiddler Hill Basalt|Type section locality|Tichum Creek Quarry ;(GR 441 233, Cairns 1:100 000 Sheet area) where two lava flows of dark grey, fine-grained olivine basalt are exposed. The upper flow is 3 to 4 m thick and the lower flow is at least 15 m thick and has columnar joints.|16-MAY-23
26329|Twiddler Hill Basalt|Extent|Twiddler Hill double volcanic cone, its flanks, and a few basaltic lava flows which infilled the Pliocene Emerald Creek valley. The total area of exposure is about 10 km2.|16-MAY-23
26329|Twiddler Hill Basalt|Lithology|The basalt is dark grey, fine grained, and slightly porphyritic with phenocrysts of olivine and subordinate augite. Coarse bouldery scoria forms the double cone at Twiddler Hill.|16-MAY-23
26329|Twiddler Hill Basalt|Relationships and boundaries|The Twiddler Hill Basalt is considered to represent volcanic activity in the Atherton Volcanic Province. It overlies and possibly interfingers with poorly consolidated sediments of presumed Pliocene-Pleistocene age in the valley of the Clohesy River, as well as overlying the Hodgkinson Formation.|16-MAY-23
26329|Twiddler Hill Basalt|Age reasons|Believed to be Pliocene-Pleistocene, based on ages obtained from other volcanoes in the Atherton area.|16-MAY-23
26329|Twiddler Hill Basalt|Proposed publication|1:100 000 Geological Map Commentary, Cairns Region, Queensland. Geological Survey of Queensland.|16-MAY-23
26329|Twiddler Hill Basalt|References|60/078; ?63/079; B084; 82/22416|16-MAY-23
26329|Twiddler Hill Basalt|Category|2|16-MAY-23
18819|Unbunmaroo Member|Name source|From Mount Unbunmaroo (Black Mountain) (140o17'E, 22o32'S), Boulia 1:250 000 Sheet area.|16-MAY-23
18819|Unbunmaroo Member|Unit history|Generally comprises Unit 1 and Unit 2 of Casey :(1968), Member(I) of Druce (1976) and part of the Variegated Limestone/Dolomite Member of Jones et al. (1971). |16-MAY-23
18819|Unbunmaroo Member|Type section locality|Black Mountain the lower 165 m of the Ninmaroo Formation between 0m and 165 m on the section from 261083 (140o17'00"E, 22o31'55"S) to 2597087 (140o16"45"E, 22o31'40"S).|16-MAY-23
18819|Unbunmaroo Member|Extent|The unit is exposed in a 90 km belt from Dribbling Bore in the south to Swift Hills in the north on the Boulia 1:250 000 Sheet area.|16-MAY-23
18819|Unbunmaroo Member|Thickness range|165 m at Black Mountain, 250 m at Mt Ninmaroo, 120 m at Mt Datson, 69+ m of probable dolomitised Unbunmaroo Member at Dribbling Bore and 40 m+ at Lily Creek.|16-MAY-23
18819|Unbunmaroo Member|Lithology|Medium to thick bedded limestones (peloidal (pellet-like) clast and peloidal grainstone (Dunham, 1962), micrite (probably stromatolitic), sandy peloidal grainstone) Pseudomorphs of gypsum and anhydrite.|16-MAY-23
18819|Unbunmaroo Member|Relationships and boundaries|Overlies the Lily Creek Sandstone Member of the Chatsworth Limestone conformably at Black Mountain, Mount Ninmaroo, Mount Datson and probably at Dribbling Bore. In the Lily Creek area the relationship between Lilly Creek Member and Unbunmroo Member is probably unconformable. At Black Mountain the base is recognised by the presence of a thick cross-stratified peloid and ooid grainstone which locally encloses or surrounds biohermal mounds of stromatolitic boundstone (Dunham, 1962). This basal unit is commonly dolomitised and is sandy in places. The upper boundary is marked by the increased occurrence of colour mottled (two-tone) limestones.|16-MAY-23
18819|Unbunmaroo Member|Age reasons|The Member is latest Late Cambarian (late Payntonian) to Early Ordovician (early Datsonian). The fauna includes trilobites (Shergold, 1975), conodonts (Druce & Jones, 1971) and rostroconch molluscs (Pojeta et al., 1977), as well as nautiloids.|16-MAY-23
18819|Unbunmaroo Member|Proposed publication|BMR publication, BMR 1:100 000 Special - The Southern Burke River Structural Belt.|16-MAY-23
18819|Unbunmaroo Member|References|B110; 79/02306/ B171; B153|16-MAY-23
24550|Venetia Formation|Name source|Parish of Venetia, County of Clarke.|16-MAY-23
24550|Venetia Formation|Unit history|Previously part of the Clarke River Formation (now Group) (White, 1959).|16-MAY-23
24550|Venetia Formation|Type section locality|The holostratotype is located in the ridges north of the Clarke River between GR 997528 (base) and GR 972534 (top). The base is the unconformity with underlying deformed flyschoid sedimentary rocks. The top is identified by the change from predominantly epiclastic to volcaniclastic detritus. In this sequence, which is about 500 m thick, the unit consists mainly of lithofeldspathic gritty sandstones (locally pebbly) which fine up through the sequence into medium to fine-grained micaceous, feldspathic sandstones with minor tuff and siltstone. The sandstones are locally cross-stratified. None of the marine sedimentary rocks has been recognised in th type section. Reference section: The section about 237 m thick exposed along the Clarke River from GR 981477 (base) to GR 969477 (top) is designated as a reference section (parastratotype) for the Venetia Formation. The top is faulted against the Lyall Formation and the base unconformably overlies deformed sedimentary rocks of the Broken River Embayment. Gritty, pebbly sandstone is well exposed in the section. The Marine sedimentary rocks appear to be better developed in the Blue Range area (Wyatt & Jell, 1980), and a reference section eventually could be designated there.|16-MAY-23
24550|Venetia Formation|Extent|The Venetia Formation crops out along the northern side of the Clarke River about 40 km southeast of Greenvale. Further north outcrop is restricted to windows within a Tertiary laterite cover. Small outliers also occur to the southeast on Niall Station, to the north in the Gill Creek area, east of Gray Creek near Lucky Springs homestead, and near the junction of Horse and Gray Creeks. The basal part of the sequence in the Blue Range area probably can be assigned to the Venetia Formation although it has not yet been studied in this survey.|16-MAY-23
24550|Venetia Formation|Thickness range|The thickness ios difficult to determine because of the irregular open folding. In the type section the formation is about 500 m thick, although some minor repetition by folding is likely.|16-MAY-23
24550|Venetia Formation|Lithology|Basal conglomerate; coarse-grined to gritty, poorly sorted lithofeldspathic and quartzose sandstone (locally pebbly); micaceous siltstone; medium to fine-grained, micaceous, feldspathic sandstone; minor tuff. Local marine rocks towards the base of the unit consist of fine-grained sandstone, siltstone and rare limestone.|16-MAY-23
24550|Venetia Formation|Relationships and boundaries|The formation is the lower most unit of the Clarke River Group. It unconformably overlies, or is faulted against, deformed flyschoid sedimentary rocks (mainly of Ordovician to Silurian age) of the Broken River Embayment. The basement is distinguished from Clarke River Group by the steep to overturned dips and numerous zones of broken formation. In contrast the Clarke River Group is only weakly deformed; dips are mostly less than 20o. The Venetia Formation is overlain by Lyall Formation (with possible disconformity ; and local angular unconformity). The top of the Venetia Formation is defined by the change from micaceous, lithofeldspathic sandstone/siltstone (containing mainly sedimentary lithic clasts) to pebbly sandstones, conglomerates and micaceous, red-green siltstones characterised by the presence of acid volcanic clasts. The Venetia Formation forms the more rugged topography of the Clarke River Basin. Outcrop is plentiful, particularly near the Clarke River. However, it is mainly the coarser, thick-bedded, massive sandstones which crop out. The ridges of the Venetia Formation are generally thickly wooded and have a dark tone on aerial photographs. They can be distinguished from the older Palaeozoic basement rocks which are not as thickly vegetated and are less rugged. Bedding trends and shallow dip slopes of the Venetia Formation are also readily discernable on airphotos.|16-MAY-23
24550|Venetia Formation|Age reasons|The Venetia Formation is probably mainly Tournaisian in age, but may range from latest Devonian to late Visean (Jell & Playford, in press). A possible hiatus has been suggested near the top of the Venetia Formation, on the basis of microfossil evidence.|16-MAY-23
24550|Venetia Formation|Defn author|Coote S.M., 1986|16-MAY-23
24550|Venetia Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24550|Venetia Formation|Defn Reference|86/25587|16-MAY-23
24550|Venetia Formation|Proposer|Scott M.|16-MAY-23
24551|Waddy Point Volcanics|Name source|Waddy Point, on the east coast of Fraser Island, 355390 m, Waddy Point 1:100 000 Sheet area.|16-MAY-23
24551|Waddy Point Volcanics|Type section locality|At Waddy Point, the coastal cliffs expose a sequence of 20 m of trachytic lavas overlain by up to 10 m of volcanic agglomerate which is in turn overlain by a further 20 m of lavas. A map and description of the area is presented in Grimes (1977). The volcanics continue below sea level and their base has not been seen. They are overlain by Pleistocene dune sands.|16-MAY-23
24551|Waddy Point Volcanics|Extent|Rocky headlands, and a few inland outcrops along a 5 km stretch of coast from Waddy Point south to Indian Head.|16-MAY-23
24551|Waddy Point Volcanics|Thickness range|The total thickness is not known as the beds extend below sea level. The volcanics rise to 80 m above sea level and this is taken as the minimum thickness.|16-MAY-23
24551|Waddy Point Volcanics|Lithology|The rocks are described in Grimes (1977). Briefly they comprise dark grey and green trachytic lavas with anorthoclase phenocrysts. They are massive or flow banded and often closely jointed parallel to the flow banding. Irregular lenses of agglomerate occur in several places and a bed of agglomerate up to 10 m thick occurs at Waddy Point. This agglomerate is green to red in colour and generally weathered. It contains fragments of the trachytes up to several metres across in a tuffaceous matrix.|16-MAY-23
24551|Waddy Point Volcanics|Relationships and boundaries|The base of the un;it has not been seen but is assumed to overlie either Tertiary sediments or the Mesozoic rocks of the Maryborough Basin. The upper boundary is a weathered erosional surface, buried beneath the Pleistocene dunes. They have been intruded by basaltic dykes which have chilled margins.|16-MAY-23
24551|Waddy Point Volcanics|Age reasons|The volcanics contain no fossils. Carlson & Wilson (1968) refer to a "basalt" (sic) sample from Middle Rocks which was dated at 32.3 million years (K/Ar method) and three other basalt (sic) samples from the same area ranged from 29.7 to 37.4 m.y. No further details are given but it seems unlikely that sampling would have been restricted to the basalt dykes, and it may well be that 'basalt' is a field name for the dark trachytes. If so the age of the volcanics is Oligocene. This age is in agareement with the age : latitude relationship noted by Wellman and McDougall (1974) for central volcanoes in eastern Australia - the Waddy Point |16-MAY-23
24551|Waddy Point Volcanics|Proposer|Grimes K.G.|16-MAY-23
27922|Wakeful Metabasalt Member|Name source|Wakeful mine, 30 km west-southwest of Cloncurry, latitude 20o47'20"S, longitude 140o13'20"E.|16-MAY-23
27922|Wakeful Metabasalt Member|Geomorphic expression|The unit forms valleys in the Mitakoodi Quartzite.|16-MAY-23
27922|Wakeful Metabasalt Member|Type section locality|A section about 300 m thick trending northeast towards an old track 18 km west-southwest of Cloncurry, i.e., near latitude 20o45'S, longitude 140o20'E, GR 6956-309042 to 6956-313046. In the type section there are several flows of massive and amygdaloidal metabasalt, as well as aglomerate with interbeds of fine-grained sandstone.|16-MAY-23
27922|Wakeful Metabasalt Member|Extent|The member has been mapped in detail in the Marraba Sheet area, and is continuous across the Bulonga and Duck Creek anticlines; it is known to extend south into the Malbon Sheet area. From the type section south, along the eastern limb of the Duck Creek anticline, a second thin basalt unit is present in the Mitakoodi Quartzite, about 750 m below the Wakeful Metabasalt Member.|16-MAY-23
27922|Wakeful Metabasalt Member|Thickness range|Maximum thickness is 340 m in any one sequence of flows.|16-MAY-23
27922|Wakeful Metabasalt Member|Lithology|Amygdaloidal and massive metabasalt with sandstone, siltstone, and shale interbeds, and minor agglomerate, silicified sandstone, cherty limestone, and chlorite and magnetic schists. The rocks have been metamorphosed in the greenschist facies.|16-MAY-23
27922|Wakeful Metabasalt Member|Relationships and boundaries|The Wakeful Metabasalt Member occurs as an apparently conformable layer within the Mitakoodi Quartzite.|16-MAY-23
27922|Wakeful Metabasalt Member|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
27922|Wakeful Metabasalt Member|Proposed publication|Queensland Government Mining Journal, 1976|16-MAY-23
27922|Wakeful Metabasalt Member|Comments|Remarks: Copper mineralisation is common where dolerite dykes cut metabasalt.|16-MAY-23
27922|Wakeful Metabasalt Member|Name first published by|Derrick G.M., Millist G., Little M., 1976|16-MAY-23
19228|Walford Dolomite|Name source|Walford Creek, which drains the eastern portion of the Hedleys Creek 1:100 000 Sheet area, Queensland (Sheet 6562).|16-MAY-23
19228|Walford Dolomite|Unit history|Included by Carter (1959) in the 'Wollogorang Formation'; that name is now restricted to a older formation in the Tawallah Group in the McArthur Basin (Roberts et al., 1963). The Walford Dolomite was included in the Fickling Beds of Roberts et al. (1963). These now become the Fickling Group, of which the Walford Dolomite forms the basal unit.|16-MAY-23
19228|Walford Dolomite|Type section locality|Over 400 m of dolomite, shale and minor sandstone. The base at GR 860249, 2 km north-northwest of Galena Pits prospect, in the southwestern Hedleys Creek Sheet area; the section runs 2.3 km on a bearing of 170o, and the top is about 200 m south-west of Galena Pits prospect at GR 864228.|16-MAY-23
19228|Walford Dolomite|Extent|About 100 km2 in the southwestern Hedleys Creek Sheet area (Qld. - and the adjacent eastern Seigal Sheet area (Northern Territory).|16-MAY-23
19228|Walford Dolomite|Thickness range|From 250 m to over 400 m.|16-MAY-23
19228|Walford Dolomite|Lithology|In Hedleys Creek a basal member, of limonite concretions and leached shale (originally pyritic?) is overlain by stromatolitic, intraclastic and oolitic dolomite with minor black shale, and glauconitic and dolomitic sandstone. Many of the dolomite exposures are silicified, and a variety of cherts, in which the original textures are preserved, are present.|16-MAY-23
19228|Walford Dolomite|Relationships and boundaries|Although sharp, the basal contact with the Fish River Formation appears to be conformable. The upper contact with the Mount Les Siltstone is conformable, and the two units probably intertongue.|16-MAY-23
19228|Walford Dolomite|Age reasons|Proterozoic-Carpentarian. Correlation of part of the underlying Peters Creek Volcanics with the Hobblechain Rhyolite Member of the Masterton Formation in the McArthur Basin suggests an age of less than 1575 m.y. (age of the Hobblechain Rhyolite Mbr). Younger age limit provided by 1280 m.y. old dolerites which intrude equivalents of the South Nicholson Group which unconformably overlies the Walford Dolomite.|16-MAY-23
19228|Walford Dolomite|Proposed publication|BMR Bulletin: Precambarian geology of the Westmoreland region, Northern Australia.|16-MAY-23
19228|Walford Dolomite|Defn Reference|82/22568|16-MAY-23
26330|Wallabadah Siltstone|Name source|Wallabadah' outstation; GR 7362-410130 (Wallabadah 1:100 0000 Sheet).|16-MAY-23
26330|Wallabadah Siltstone|Unit history|Branch (1966) noted the siltstone on his map of the Croydon area as 'white siltstone conformably under rhyodacite' and indicated a thickness for it of 15 m+ at the base of a section of the "Croydon Volcanics".|16-MAY-23
26330|Wallabadah Siltstone|Geomorphic expression|The unit occurs in flat or gently undulating terrain mostly covered by alluvium; outcrops are generally creek-bed exposures.|16-MAY-23
26330|Wallabadah Siltstone|Type section locality|Because exposures are limited and none represents a complete section, a composite type section is nominated. The uppermost part of the unit is exposed in the bed of Scrubby Creek, beside the Croydon-"Wallabadah" outstation road, at GR 7362-397112, where about 15 m of weathered, well-bedded, quartzose siltstone is conformably overlain by Goat Creek Andesite. A 50 m-long, east-west creek section at GR 7361-488088 exposes about 10-15 m of the middle and lowermost exposed parts of the unit, and is made up of weathered, white to red-brown or purple, thin-bedded to laminated quartzose siltstone and fine sandstone. No base to the unit can be defined because of concealment beneath Tertiary to Quaternary fluviatile sediments.|16-MAY-23
26330|Wallabadah Siltstone|Extent|The unit crops out in several places on the southern edge of the Wallabadah 1:100 000 sheet and the northern edge of the adjacent Croydon 1:100 000 Sheet, extending from 3 km southwest to 15 km southeast of 'Wallabadah' outstation.|16-MAY-23
26330|Wallabadah Siltstone|Thickness range|The total thickness of the formation is unknown, because the base of the formation is not exposed. Maximum thickness exposed in any one outcrop is not more than 15 m, but maximum total thickness may be 30 m or more.|16-MAY-23
26330|Wallabadah Siltstone|Lithology|The siltstone ranges from white to red-brown and purple, and is commonly laminated; in some places it contains interbeds up to 0.3 m thick of massive siltstone which contain sparse, cobble-sized clasts of fine, purple sandstone similar to that in the Langlovale Group. Outcrop of silicified quartzose sandstone and abundant siltstone float were noted at GR 7362-490106.|16-MAY-23
26330|Wallabadah Siltstone|Relationships and boundaries|The siltstone is overlain, apparently conformably, by Goat Creek Andesite, and/or by B Creek Rhyolite. Its base is concealed by Tertiary and Quaternary continental sediments.|16-MAY-23
26330|Wallabadah Siltstone|Age reasons|The age is Middle Proterozoic (or possibly older), based on the age of the Croydon Volcanic Group.|16-MAY-23
26330|Wallabadah Siltstone|Defn author|Mackenzie D.E., Henderson G.A.M., Warnick J.V., Bain J.H.C., 1985|16-MAY-23
26330|Wallabadah Siltstone|Proposed publication|Queensland Government Mining Journal|16-MAY-23
26330|Wallabadah Siltstone|References|B076; 83/23589|16-MAY-23
26330|Wallabadah Siltstone|Defn Reference|86/25125|16-MAY-23
26330|Wallabadah Siltstone|Proposer|Mackenzie D.E., Warnick J.V., Henderson G.A.M.|16-MAY-23
19303|Walloon Coal Measures|Type section locality|Type section was designated as the interval 7-235m in drillhole N.S.84 by Cameron (1970). - from p87 in: Green et al., 1997. Lithostratigraphic units in the Bowen and Surat Basins, Queensland. Queensland Minerals and Energy Review Series. p41-108.|16-MAY-23
24074|Wando Vale Subgroup|Name source|Wando Vale Holding (Clarke River 1.250 000 Cadastral map).|16-MAY-23
24074|Wando Vale Subgroup|Unit history|The Subgroup was previously mapped as part of the Broken River Formation (now Group) (White, 1959, 1962, 1965).  The name was first published and described by Withnall & others (1988), but was not formally defined.  It was introduced as an overall name for the interval between the Shield Creek Formation and the Mytton Formation, both of which can be recognised over most of the Graveyard Creek Subprovince, and are relatively uniform lithologically.  However the interval between them, by contrast, is a transgressive sequence with a complexly interfingering range of facies, predominantly limestone, mudstone, and lesser sandstone.  The individual formations which correspond to these facies are generally restricted spatially.  An overall unit to include these formations, and other areas which are as yet unassigned, is both convenient and informative in descriptions of the Broken River Group.|16-MAY-23
24074|Wando Vale Subgroup|Constituents|Dosey-Broken River area: Papilio Mudstone (including Spanner Limestone Member), Dosey Limestone, Storm Hill Sandstone, Lomandra Limestone, Bracteata Mudstone. Gorge Creek-Diggers Creek area: Papilio Mudstone,  Burges Formation. Jessey Springs area: Burges Formation,  Jessey Springs Limestone. Dip Creek area: Papilio Mudstone, Dip Creek Limestone, Tank Creek Sandstone. Lockup Well area: Lockup Well Limestone. Pandanus Creek area: Chinaman Creek Limestone, Tank Creek Sandstone.|16-MAY-23
24074|Wando Vale Subgroup|Extent|A sinuous folded belt up to 3 km wide from near 'Pandanus Creek' in the north, extending about 50 km to 'Dosey' and the Clarke River in the south.  A small, partly fault-bounded area occurs along Catfish Creek northeast of 'Gregory Springs' in the southwest.|16-MAY-23
24074|Wando Vale Subgroup|Thickness range|Up to 1200 m.|16-MAY-23
24074|Wando Vale Subgroup|Lithology|Limestone, mudstone, labile to quartzose sandstone, and polymictic conglomerate.|16-MAY-23
24074|Wando Vale Subgroup|Fossils|The limestone and mudstone units contain rich shallow marine faunas including corals and stromatoporoids, as well as brachiopods, bivalves, gastropods, nautiloids, crinoids, trilobites, bryozoa, ostracods, fish, and conodonts, and algal and vascular plants.|16-MAY-23
24074|Wando Vale Subgroup|Relationships and boundaries|Generally overlies the Shield Creek Formation, which consists of feldspathic arenite, with possible disconformity.  West of the Six Mile Syncline, the Shield Creek Formation is difficult to recognise, and the Wando Vale Subgroup may lie directly on the Graveyard Creek Group. Further west it is faulted against the Silurian Dido Tonalite of the Georgetown Province.  In the Dosey area, northwest of Storm Hill, the Wando Vale Subgroup (Storm Hill Sandstone) unconformably overlies the Judea Formation.  In the southwest, near 'Gregory Springs', it unconformably overlies granitoids and metamorphic rocks of the Georgetown Province.  The Wando Vale Subgroup is overlain, apparently conformably, by the Mytton Formation.|16-MAY-23
24074|Wando Vale Subgroup|Age reasons|Studies of the corals (Hill in White, 1965; Jell, 1967; Jell in Wyatt & Jell, 1967) and conodonts (Telford, 1975; Mawson, 1987; Mawson & others, 1985; Mawson & Talent, in press and unpublished data) indicate that the Subgroup ranges from Emsian to Givetian in age.  See also the summary in Withnall & others (1988).|16-MAY-23
24074|Wando Vale Subgroup|References|JELL, J.S., 1967:  Geology and Devonian rugose corals of Pandanus Creek, north Queensland.  Ph.D. Thesis, University of Queensland (unpublished). ***MAWSON, R., 1987:  Documentation of conodont assemblages across the Early Devonian-Middle Devonian boundary, Broken River, north Queensland, Australia.  Courier Forschungs-Institut Senckenburg, 92, 251-273. ***MAWSON R., JELL, J.S., & TALENT, J.A., 1985:  Stage boundaries within the Devonian:  implications for application to Australian sequences.  Courier Forschungs-Institut Senckenburg, 75, 1-16.   ***MAWSON, R., & TALENT, J.A., in press:  Late Emsian-Givetian stratigraphy and conodont biofacies - carbonate slope and offshore shoal to sheltered lagoon and nearshore carbonate ramp - Broken River, north Queensland.  Courier Forschungs-Institute Senckenburg.***TELFORD, P.G., 1975:  Lower and Middle Devonian conodonts from the Broken River Embayment, north Queensland, Australia.  Special Papers in Palaeontology, 15. ***WHITE, D.A., 1959:  New names in Queensland stratigraphy, Parts 2, 3, and 4.  Australian Oil and Gas Journal, 5(9), 31-36; 5(10), 31-36;  5(11), 26-28. ***WHITE, D.A., 1962:  Clarke River, Qld, Sheet E/55-13.  Bureau of Mineral Resources, Australia, 1:250 000 Geological Series Explanatory Notes. ***WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River 	area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71. ***WITHNALL, I.W., LANG, S.C., JELL, J.S., McLENNAN, T.P.T., TALENT, 	J.A., MAWSON, R., FLEMING, P.J.G., LAW, S.R., MACANSH, J.D., SAVORY, P., KAY, J.R., DRAPER, J.J., 1988:  Stratigraphy, sedimentology, biostratigraphy and tectonics of the Ordovician to Carboniferous Broken River Province, north Queensland.  Australasian Sedimentologists Group Field Guide Series No 5. ***WYATT, D.H. & JELL, J.S., 1967:  Devonian of the Townsville 	hinterland, Queensland, Australia; in Oswald, D.H. (editor), International Symposium on the Devonian System, Volume 2.  Alberta Society of Petroleum Geologists, Calgary, 99-105.|16-MAY-23
24557|Wangetti Granite|Name source|Township of Wangetti at the mouth of Hartleys Creek on the coast north of Cairns (GR 470578, Cairns 1:100 000 Sheet).|16-MAY-23
24557|Wangetti Granite|Unit history|Previously included within Mareeba Granite (Fardon & de Keyser, 1964) but this term is now restricted to one batholith near Mareeba (see Richards, 1980).|16-MAY-23
24557|Wangetti Granite|Type section locality|Road cuttings along the Captain Cook Highway from Wangetti (GR 468582) north to the northern boundary of the pluton (GR 460599).|16-MAY-23
24557|Wangetti Granite|Extent|A small zoned pluton straddling Hartleys Creek, extending from Wangetti to north of Slip Cliff Point. Area of exposure is about 3.5 km2.|16-MAY-23
24557|Wangetti Granite|Lithology|Outer zone of medium to coarse-grained, even grained, white, leucocratic tourmaline-muscovite granite, with patches of pegmatite and greisen. Inner core of porphyritic grey, coarse-grained, muscovite-biotite granite, with abundant phenocrysts of potash feldspar to 7 cm in length. Well exposed in bed of Hartleys Creek, along highway road cuts, and in sea cliffs.|16-MAY-23
24557|Wangetti Granite|Relationships and boundaries|Intrudes greywacke of Hodgkinson Formation.|16-MAY-23
24557|Wangetti Granite|Age reasons|Late Permian, based on K-Ar age of 255 million years (recalculated) from Richards & others (1966).|16-MAY-23
24557|Wangetti Granite|Proposed publication|1:100 000 Geological Map Commentary, Cairns Region, Queensland, Geological Survey of Queensland.|16-MAY-23
24557|Wangetti Granite|References|B088; 98/29307; 82/22424|16-MAY-23
24557|Wangetti Granite|Category|2|16-MAY-23
40141|Warminster Formation|Name source|The name Warminster comes from Mount Warminster, situated 1 km NW of Mount Chalmers.|16-MAY-23
40141|Warminster Formation|Geomorphic expression|Because the unit is so restricted, its topographic expression cannot be determined.|16-MAY-23
40141|Warminster Formation|Type section locality|The type area constitutes the 300 m2 area mapped.|16-MAY-23
40141|Warminster Formation|Extent|The Warminster Formation is located 1 km NW of Mount Chalmers and covers an area of 300 m2. Outcrop is scarce due to clearing and establishment of pineapple plantations in the area.|16-MAY-23
40141|Warminster Formation|General description|The Warminster Formation is a unit covering only 300 m2. It constitutes fine to coarse sandstone, and granule to pebble polymictic breccia (Figure 15).|16-MAY-23
40141|Warminster Formation|Thickness range|The Warminster Formation is estimated to be less than 100 m thick|16-MAY-23
40141|Warminster Formation|Lithology|The sandstone of the Mount Warminster Formation is dark green-grey, fine to coarse, and well sorted. The other rock type is dark green-grey, massive, poorly sorted, matrix supported, granule to pebble polymictic breccia. The breccia has a siliceous, fine to coarse sandstone matrix with volcanic clasts, siltstone clasts and cherty-looking clasts. The clasts are up to 30 mm in diameter and are angular in shape, suggesting little reworking.The rock is strongly silicified and chloritised.|16-MAY-23
40141|Warminster Formation|Depositional environment|The molluscs and gastropods found in the Warminster Formation are marine and indicate a shallow water environment. The presence of breccia tends to suggest minimal reworking.|16-MAY-23
40141|Warminster Formation|Fossils|The unit contains the bivalve Glyptoleda and an indeterminate gastropod. The macrofossils found in the Warminster Formation are the same age as those of the upper Barfield Formation, lower Flat Top Formation, Ingelara Formation and lower Peawaddy Formation in the Bowen Basin. The age of the unit is Late Permian.|16-MAY-23
40141|Warminster Formation|Relationships and boundaries|A contact cannot be seen between Warminster Formation and underlying Berserker Group. Fossil evidence suggests that an unconformable relationship exists between the Upper Permian Warminster Formation and the Lower Permian Berserker Group. The relationship between the Warminster Formation and the intrusive units of the region is unknown.|16-MAY-23
40141|Warminster Formation|Age reasons|The age of the unit is Late Permian.|16-MAY-23
40141|Warminster Formation|Defn Reference|SOURCE OF INFORMATION --Crouch. S, Parfrey. S, and Taube. A  [DATE ?]. 'Geology, tectonic setting and metallogenesis of the Berserker Subprovince, northern New England Orogen'. Supplied by Ian Withnall (GSQ), September 2008.(Incomplete reference)|16-MAY-23
19533|Warrina Park Quartzite|Name source|Warrina Park recreation reserve, below the spillway of Lake Moondarra, 20 km northeast of Mount Isa, latitude 20o35'S, longitude 139o34'20"E, 6856-514234.|16-MAY-23
19533|Warrina Park Quartzite|Geomorphic expression|Characteristically forms a prominent ridge and dip slope.|16-MAY-23
19533|Warrina Park Quartzite|Type section locality|Near Lake Moondarra, 1 km south of Warrina Park reserve, and 18 km northeast of Mount Isa; near latitude 20o35'30"S, longitude 139o34'20"E, 6856-513224 to 6856-514225. At this locality the Mount Isa-Lake Moondarra road cuts across about 60 metres of orthoquartzite and minor conglomerate.|16-MAY-23
19533|Warrina Park Quartzite|Extent|Mary Kathleen, Prospector, Alsace, Mammoth Mines, Kennedy Gap, and Mount Isa 1:100 000 Sheet areas: the main outcrops are from immediately east of Mount Isa 20 km northeastwards to Warrina Park, and in fault blocks in the Paroo Range, Paroo Creek, and Crystal Creek areas, 40, 48, and 80 km north of Mount Isa, respectively.|16-MAY-23
19533|Warrina Park Quartzite|Thickness range|35-150 m.|16-MAY-23
19533|Warrina Park Quartzite|Lithology|Orthoquartzite, feldspathic quartzite, and conglomerate; the latter contains mainly quartzite clasts.|16-MAY-23
19533|Warrina Park Quartzite|Relationships and boundaries|Both conformable and unconformable on 'Mammoth Formation' correlatives; unconformable on Myally Subgroup and the three Members of the Eastern Creek Volcanics; overlain conformably by Moondarra Siltstone.|16-MAY-23
19533|Warrina Park Quartzite|Age reasons|The maximum age of the Warrina Park Quartzite is inferred to be about 1570 m.y.; the partly equivalent Gunpowder Creek Formation unconformably overlies Sybella Granite dated at 1577+/-12 m.y. (Plumb & Derrick, 1975).|16-MAY-23
19533|Warrina Park Quartzite|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
19533|Warrina Park Quartzite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
19533|Warrina Park Quartzite|Comments|Remarks: The Warrina Park Quartzite is the basal formation of the Mount Isa Group, and corresponds to the Quartzite Marker or Member of previous workers.|16-MAY-23
19533|Warrina Park Quartzite|Name first published by|Glikson A.Y., Derrick G.M., Wilson I.H., Hill R.M., 1976.|16-MAY-23
24083|Watershed North Rhyolite|Name source|The name is derived from the Watershed North Block which lies in the north-west corner of the Parish of Saint James, County of Wilkie Gray.|16-MAY-23
24083|Watershed North Rhyolite|Unit history|The Watershed North Rhyolite was previously mapped as quartz and quartz-feldspar porphyries (C-Pg)and Unnamed Acid Volcanics (Cuv) by Wyatt & others (1970).|16-MAY-23
24083|Watershed North Rhyolite|Geomorphic expression|The Watershed North Rhyolite forms steep resistant, rubbly ridges and scarps.|16-MAY-23
24083|Watershed North Rhyolite|Type section locality|The type area for the lower unit, Ca1, is on the southeast side of Ben Lomond East (8159 313543).  The grid reference is based on the AGD66 datum.|16-MAY-23
24083|Watershed North Rhyolite|Description at type locality|Dark grey, crystal-rich rhyolitic ignimbrite containing quartz, feldspar, minor biotite and rare angular to subrounded, dark grey, aphyric, felsic clasts and dark grey fiamme up to 1.5cm. The type area for the upper unit, Ca2 is at 8159-311548 about 500m north of the type area for unit Ca1. At this locality, cream, moderately crystal and lithic-rich rhyolitic ignimbrite is well exposed in a road cutting, and contains quartz and feldspar crystals, grey felsic volcanic clasts and grey fiamme up to 6cm long.  The grid reference is based on the AGD66 datum.|16-MAY-23
24083|Watershed North Rhyolite|Extent|The Watershed North Rhyolite consists of upper (Ca2) and lower (Ca1) units, which crop out over areas of 5-8km² in the Ben Lomond East area. The lower unit also crops out over about 2.5km²  south of the Hervey Range Road between the headwaters of Gin and Three Mile Creeks.|16-MAY-23
24083|Watershed North Rhyolite|Thickness range|A thickness of 145m was calculated for unit Ca1 using an average dip of 15degrees to the northwest. Approximately 270m of unit Ca2 is exposed at Ben Lomond East.|16-MAY-23
24083|Watershed North Rhyolite|Lithology|The lower unit, Ca1, consists predominately of grey to dark grey, crystal-rich to very crystal-rich rhyolitic ignimbrite. The upper unit, Ca2, mainly comprises cream, moderately crystal and lithic-rich rhyolitic ignimbrite.|16-MAY-23
24083|Watershed North Rhyolite|Relationships and boundaries|The Watershed North Rhyolite unconformably overlies folded Early Carboniferous Saint James Volcanics and hornfelsed Devonian to Early Carboniferous sedimentary rocks of the Burdekin Basin. It is unconformably overlain by the Late Carboniferous Insolvency Gully Formation, and intruded and hornfelsed by the Late Carboniferous to Permian Speed Creek Granite.|16-MAY-23
24083|Watershed North Rhyolite|Age reasons|The unit is probably of Early Carboniferous age.|16-MAY-23
24083|Watershed North Rhyolite|References|WYATT, D.H., PAINE, A.G.L., CLARKE, D.E., GREGORY, C.M. & HARDING, R.R., 1970: Geology of the Townsville 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 127.|16-MAY-23
23161|Weaner Vale Granite|Name source|Weaner Vale homestead at GR 3293 77779 on the Lolworth 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
23161|Weaner Vale Granite|Unit history|The Weaner Vale Granite was previously mapped as the Lolworth Igneous Complex by Wyatt & others (1971), Clarke & Paine (1970).|16-MAY-23
23161|Weaner Vale Granite|Type section locality|The type locality of the Weaner Vale Granite lies at the crossing of Lolworth Creek at the Lolworth Diggings at GR 3242 77740 in the Lolworth 1:100 000 Sheet area.  The grid reference is based on the AGD66 datum.|16-MAY-23
23161|Weaner Vale Granite|Description at type locality|Here a grey to pink, medium grained, rarely porphyritic biotite granite is intruded by numerous pegmatite dykes and cut by abundant fractures filled by a dark alteration product (chloritic alteration?). It comprises quartz, large poikilitic K-feldspar, subhedral albite, lath-shaped plagioclase and biotite, with minor muscovite, zircon and opaques.|16-MAY-23
23161|Weaner Vale Granite|Lithology|Granite like that exposed at the type at the type locality occurs throughout the outcrop area. The Weaner Vale Granite is similar to the adjacent Amarra Granite, but it has a distinctive signature on the TM image distinguishing it from the Amarra Granite. Samples from Niggers Bounce, a hill within the Weaner Vale Granite, show extensive subgrain development in feldspar grain boundaries, probably due to post crystallisation fluid interaction. It may be that this fluid interaction is responsible for the distinctive TM signature. However several samples from the Weaner Vale Granite contain rare euhedral epidote grains, a feature not found in the Amarra Granite.|16-MAY-23
23161|Weaner Vale Granite|Relationships and boundaries|The relationship of the Weaner Vale Granite to the adjacent Amarra Granite is unclear. The distribution of the two units suggests that the Weaner Vale Granite intrudes the Amarra Granite.|16-MAY-23
23161|Weaner Vale Granite|Age reasons|The age of the Weaner Vale Granite is uncertain. An age of Late Silurian to Early Devonian is assigned on the basis of lithologic similarity to other members of the Amarra Suite in the Lolworth Batholith.|16-MAY-23
23161|Weaner Vale Granite|Comments|Magnetic susceptibilities from the type locality are 91-570 x 10[superscript]-5 SI units. Throughout the unit, susceptibilities are 2-756 10[superscript]-5 SI units, probably reflecting alteration. However the high values in most samples may indicate that the alteration is localised along fractures and is not pervasive.|16-MAY-23
23161|Weaner Vale Granite|References|Hutton, L.J., Garrad, P.D., & Withnall, I.W., (in prep): Subdivision of the Lolworth Batholith -  new intrusive units in the batholith and its surrounds. Queensland Geological Record.|16-MAY-23
24567|Welfern Granite|Name source|Welfern Pastoral holding on which most of the unit crops out; Welfern homestead is at GR 096 946 (Gilberton 1:100 000 Sheet area).|16-MAY-23
24567|Welfern Granite|Unit history|Previously mapped as Dumbano Granite by White (1962).|16-MAY-23
24567|Welfern Granite|Type section locality|Along the Kidston/Gilberton road between GR 102 935 and 094 907 (Gilberton 1:100 000 Sheet area); the metamorphic roof pendant is exposed along the part of this section between GR 097 927 and 092 915. The granite exposed in the type area is a pink equigranular to slightly porphyritic medium grained foliated biotite granite.|16-MAY-23
24567|Welfern Granite|Extent|An elongate intrusion about 10 km2 in the northeast corner of the Gilberton 1:100 000 Sheet area; a large roof pendant of Einasleigh Metamorphics gives the intrusion an annular shape.|16-MAY-23
24567|Welfern Granite|Lithology|As in the type area. The unit is characterised by a relatively high radiometric background (about twice as high as that of the metamorphics).|16-MAY-23
24567|Welfern Granite|Relationships and boundaries|Intrudes the Proterozoic Einasleigh Metamorphics.|16-MAY-23
24567|Welfern Granite|Age reasons|Probably mid-Proterozoic; the presence and the orientation of the strong foliation suggests the unit was intruded syn-tectonically with either the first or second major deformation in the area which have been dated at about 1570 m.y. and 1470 m.y. respectively (Black & others, 1979).|16-MAY-23
24567|Welfern Granite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24567|Welfern Granite|First Reference|80/20677|16-MAY-23
24567|Welfern Granite|Proposer|Withnall I.W., Bain J.H.C.|16-MAY-23
24569|Wheatley Oil Shale Member|Name source|Wheatley homestead, GR 70700E 92100N Miriam Vale 1:100 000 Sheet area.|16-MAY-23
24569|Wheatley Oil Shale Member|Unit history|Part of the Lowmead Beds for Cribb, 1960; Mack, 1972; and Ellis and Whitaker, 1976.|16-MAY-23
24569|Wheatley Oil Shale Member|Type section locality|32.9 m (estimated true thickness 32.4 m) from 213.6 m to 246.5 m in LDD 14 (GR 64906E 95222N Miriam Vale 1:100 000 Sheet area).|16-MAY-23
24569|Wheatley Oil Shale Member|Description at type locality|This interval is within the type section of the Lowmead Formation. Carbonaceous oil shale is the dominant rock type. The upper boundary of the member is identified by the contact of carbonaceous oil shale with brown oil shale of the Korenan Oil Shale Member. The lower boundary is the contact with claystone of the underlying Harpur Creek Member. Rock Types: The carbonaceous oil shale is brownish-black and hard. It is composed of alternating kerogenous, carbonaceous to coaly and clay laminae in beds up to 3.3 m thick. There are claystone beds up to 4.25 m thick. They are olive grey, hard and massive and increase in thickness and frequency from the top of the base of the member.|16-MAY-23
24569|Wheatley Oil Shale Member|Extent|Subcrops in an area of about 4 km2 northwest of Wheatley homestead. There is sparse, highly weathered outcrop. The member has been identified from drill core.|16-MAY-23
24569|Wheatley Oil Shale Member|Thickness range|32.9 m in type section; true thickness is 32.4 metres, corrected for a 10o dip of a strata in LDD 14. The member ranges from 14.3 m to 41.7 m in thickness.|16-MAY-23
24569|Wheatley Oil Shale Member|Relationships and boundaries|The Wheatley Oil Shale Member is conformably overlain by the Korenan Oil Shale Member and overlies the Harpur Creek Member of the Lowmead Formation. It is faulted against igneous rocks of the Miriam Vale Granodiorite and the Agnes Waters Volcanics (Ellis and Whitaker, 1976) along the boundaries of the Lowmead Graben.|16-MAY-23
24569|Wheatley Oil Shale Member|Age reasons|Early Tertiary - as for the Lowmead Formation.|16-MAY-23
24569|Wheatley Oil Shale Member|Defn author|McConochie M.J., Henstridge D.A., 1985.|16-MAY-23
24569|Wheatley Oil Shale Member|Comments|Note: Drill core of LDD 14 is stored at Southern Pacific Petroleum's Research and Core Storage fcility in Gladstone, Queensland.|16-MAY-23
24569|Wheatley Oil Shale Member|References|79/01354|16-MAY-23
24569|Wheatley Oil Shale Member|Defn Reference|80/25154|16-MAY-23
19883|Whitdale Granodiorite|Name source|Whitdale homestead at 8451-545082.  The grid reference is based on the AGD66 datum.|16-MAY-23
19883|Whitdale Granodiorite|Geomorphic expression|This pluton forms moderately undulating terrain with abundant boulder-sized outcrop in the north of the pluton around Silver Hills homestead.   On Landsat 5 TM images the Whitdale Granodiorite cannot be distinguished from the adjacent Mount Newsome Granodiorite. Magnetic anomalies do not correlate well with the mapped extent of the unit, but the data suggest that the unit is magnetic. Weak to moderate K, and low Th and U responses are associated with the unit.|16-MAY-23
19883|Whitdale Granodiorite|Type section locality|At 8451-555016, about 1 km west-southwest of Silver Hills Homestead. The grid reference is based on the AGD66 datum.|16-MAY-23
19883|Whitdale Granodiorite|Description at type locality|Foliated, porphyritic biotite granodiorite.|16-MAY-23
19883|Whitdale Granodiorite|Extent|A north-trending elongate body, 20 km2 in area, centred 2 km south-southwest of Silver Hills homestead.|16-MAY-23
19883|Whitdale Granodiorite|Lithology|Grey, foliated and lineated medium to coarse-grained, porphyritic biotite granodiorite, characterised by large, pink alkali feldspar phenocrysts. The tectonic lineation is characterised by the alignment of the alkali feldspar phenocrysts and quartz and biotite.|16-MAY-23
19883|Whitdale Granodiorite|Relationships and boundaries|Intrudes the Anakie Metamorphic Group and Gem Park Granite, and appears to be intruded by the Mount Newsome Granodiorite near Silver Hills homestead.  It is unconformably overlain by Late Devonian to Early Carboniferous Silver Hills Volcanics and sedimentary rocks of the Drummond Basin.|16-MAY-23
19883|Whitdale Granodiorite|Age reasons|A corrected K-Ar biotite age of 370 Ma was obtained by Webb & McDougall (1968). This age is younger than those of some other units, whereas the strong foliation or lineation in the granite suggests it may be an older part of the batholith. The young age could be the result of resetting by the emplacement of the Mount Newsome Granodiorite.|16-MAY-23
19883|Whitdale Granodiorite|References|WEBB, A.W. & MCDOUGALL, I., 1968: The geochronology of the igneous rocks of Eastern Queensland. Journal of the Geological Society of Australia, 15, 313-346.|16-MAY-23
27254|White Blow Formation|Name source|White Blow Hill, 15 km northwest of Mary Kathleen town, latitude 20o42'20"S, longitude 139o51'25"E (6856 809100).|16-MAY-23
27254|White Blow Formation|Geomorphic expression|Low hills and rises with abundant soil cover.|16-MAY-23
27254|White Blow Formation|Type section locality|The proposed type section extends for 1 km in a northwesterly direction from a point 1.5 km southwest of Deighton Pass to the axis of an east-trending syncline, I.e. latitude 20o42'5"S, longitude 139o53'20"E (6856 842107) to latitude 20o41'40"S, longitude 139o53'E (6856 836114). At the base of this section, red-brown medium-grained feldspathic and sericitic sandstone of the Deighton Quartzite is gradationally and conformably overlain by laminated siltstone of the White Blow Formation. The top ;of the formation is defined as the uppermost bed at the synclinal axis. No younger strata are known in the formation. The type section exposes 915 m of sediments which are described by Derrick et al. (1974) as follows (from oldest to youngest):  95 m of grey laminated calcareous and micaceous siltstone and interbedded fine-grained labile sandstone;  240 m of blocky grey laminated limestone, calcareous quartzite and minor black slate;  80 m of grey to black slate with abundant holes resulting from the weathering out of sulphides or porphyroblasts;  120 m of calcareous siltstone, grey slate, and buff fine to medium-grained sandstone;  40 m of blocky medium-grained sandstone; and  350 m of red-brown garnetiferous phyllite and micaceous siltstone.|16-MAY-23
27254|White Blow Formation|Extent|The White Blow Formation is exposed over 6 km2 east of White Blow Hill to as far as Deighton Pass, and over a similar area near Cattle Creek, 12 to 18 km south-southwest of Mary Kathleen.|16-MAY-23
27254|White Blow Formation|Thickness range|The formation is about 1000 m thick in the Cattle Creek area and 915 m thick in the type section.|16-MAY-23
27254|White Blow Formation|Lithology|Micaceous siltstone, phyllite and schist that are locally garnetiferous, and in the Cattle Creek area staurolite-bearing; laminated limestone and scapolitic calcareous biotitic granofels; grey to black slate with rare porphyroblasts of andalusite; and blocky fine to medium-grained quartzite and feldspathic sandstone. The different rock types typically are highly lenticular.|16-MAY-23
27254|White Blow Formation|Relationships and boundaries|The White Blow Formation conformably or possibly disconformably overlies the Deighton Quartzite. Local discordant contacts are possibly due to the highly lenticular nature of the underlying Deighton Quartzite, and do not necessarily represent a major tectonic and erosional event. The White Blow Formation may be lithological equivalents of Units B, C, and D in the Surprise Creek Beds (Wilson et al., in prep.). No igneous rocks are known to intrude the Formation.|16-MAY-23
27254|White Blow Formation|Age reasons|Precambrian, probably Carpentarian (Middle Proterozoic).|16-MAY-23
27254|White Blow Formation|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1977.|16-MAY-23
27254|White Blow Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
27254|White Blow Formation|Comments|Remarks: Carter et al. (1961) included these rocks in the Corella Formation but as these rocks overlie the Deighton Quartzite which in turn unconformably or disconformably overlies the Corella Formation their correlation has been revised.B4+B161|16-MAY-23
27254|White Blow Formation|References|77/004; B051.|16-MAY-23
27254|White Blow Formation|Name first published by|Glikson A.Y., Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
24571|White Bull Member|Name source|White Bull Bore, on Candlow pastoral holding, GR7560-189355, 26 km due west of the Gilbert River-Robertson River junction.|16-MAY-23
24571|White Bull Member|Unit history|Included in the upper part of the "Etheridge Formation" by White (1962, 1965).|16-MAY-23
24571|White Bull Member|Geomorphic expression|Commonly forms low, rounded ridges that rise above the generally flat terrain on the Candlow Formation. Beds of siliceous siltstone crop out prominently on such ridges, which generally are light in tone on airphotographs. The ridges are commonly grassed with spinifex rather than the more usual long grasses of the area.|16-MAY-23
24571|White Bull Member|Type section locality|Within the type section of the Candlow Formation, between GR 7560-234386 (base) and -232384 (top).|16-MAY-23
24571|White Bull Member|Extent|From the Gilbert River (about 18o15'S) southward along the valley of Pinnacle Creek, then westward into the valley of the upper Black Gin Creek, then generally southward to the Candlow area and to about 18o50'S in the headwaters of the Langdon River (where it disappears beneath a cover of Mesozoic sandstones) and in the Reedy Creek area (GR 7560-250160).|16-MAY-23
24571|White Bull Member|Thickness range|About 200 m in type area; ranges from 100 to 300 m.|16-MAY-23
24571|White Bull Member|Lithology|Sericitic siltstone, sublithic fine sandstone, dark grey siliceous siltstone, carbonaceous siltstone, minor quartzose sandstone, and shale. Predominantly sericitic siltstone and dark grey siliceous siltstone in type area.|16-MAY-23
24571|White Bull Member|Relationships and boundaries|A mappable sub-unit in the lower part of the Candlow Formation. Distinguished by the relative abundance of hard, prominently outcropping dark grey siliceous siltstone and consequent relative topographic prominence. Intruded by Forest Home Granodiorite.|16-MAY-23
24571|White Bull Member|Age reasons|Probably mid-Proterozoic, as is the enclosing Candlow Formation.|16-MAY-23
24571|White Bull Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24571|White Bull Member|References|B071|16-MAY-23
24571|White Bull Member|Proposer|Mackenzie D.E., Withnall I.W.|16-MAY-23
29274|White Springs Granodiorite|Name source|White Springs Creek which joins the Einasleigh River at GR 056 036 (Georgetown 1:100 000 Sheet area).|16-MAY-23
29274|White Springs Granodiorite|Unit history|Mapped as Forsayth Granite by White (1959, 1962c, 1965).|16-MAY-23
29274|White Springs Granodiorite|Type section locality|Along the Georgetown-Mt Surprise road northeast from the eastern scarp of the Newcastle Range between 943 733 and 046 806. In this area the unit consists mainly of medium even grained to slightly porphyritic biotite granodiorite. Muscovite-biotite granodiorite grading into muscovite leucogranite crops out east of Nigger Creek.|16-MAY-23
29274|White Springs Granodiorite|Extent|Two separate areas east and west of the Newcastle Rnage in the central part of the Georgetown 1:100 000 Sheet area. The western area extends from O'Brien Creek to the Newcastle Range escarpment and the eastern area from the western side of the range along White Springs Creek to within one kilometre of McMillan Creek.|16-MAY-23
29274|White Springs Granodiorite|Lithology|Mainly medium, even grained to slightly porphyritic biotite granodiorite with some more leucocratic medium grained porphyritic muscovite-biotite granite and granodiorite. The leucocratic, porphyritic varieties are mostly restricted to the southeast between White Springs and McMillan Creeks.|16-MAY-23
29274|White Springs Granodiorite|Relationships and boundaries|Intrusive into Proterozoic Einasleigh Metamorphics and Talbot Creek Granodiorite (new name). Muscovite leucogranites intrude the biotite granodiorite locally ;but elsewhere grade into muscovite-biotite granodiorite and granite. Some of these muscovite leucogranites may be related to the Digger Creek Granite but are probably more likely to be a late stage marginal phase of the White Springs Granodiorite. Unconformably overlain by the Carboniferous Newcastle Range Volcanics and intruded by rhyolite and andesite dykes realted to the volcanics.|16-MAY-23
29274|White Springs Granodiorite|Age reasons|Proterozoic; Rb/Sr dating of muscovite from a sample collected 16 km west of "Eveleigh" Homestead gave a minimum age of 1085 million years; biotite from the same sample gave 414 million years indicating resetting (Black, 1973).|16-MAY-23
29274|White Springs Granodiorite|References|73/050; 98/29026; B071;+|16-MAY-23
19936|Whitula Formation|Name source|Whitula Creek, Canterbury 1:250 000 Sheet area, Qld.|16-MAY-23
19936|Whitula Formation|Type section locality|The type section lies between 1.5 m and 55 m in BMR Canterbury 4, Latitude 25o21'00", Longitude 142o29'30" Canterbury 1:250000 Sheet.|16-MAY-23
19936|Whitula Formation|Extent|Wilson Depression, Cooper Syncline, Yamma Yamma Depression and Thomson Syncline; Durham Downs, Barrolka, Canterbury, Windorah and Jundah 1:250 000 Sheet areas.|16-MAY-23
19936|Whitula Formation|Thickness range|Range 0-204 metres (BMR Canterbury 5 204 m). It is inferred to be at least 150 m thick along the axis of major downwarps and in BMR Barrolka 1 located on the west margin of the Yamma Yamma Depression 104 m (base not reached) was penetrated.|16-MAY-23
19936|Whitula Formation|Lithology|Interbedded friable quartzose sandstone, laminer siltstone, mudstone and claystone, minor conglomerate; lignitic and gypsiferous in part. The sandstones vary from white to red-brown in colour and the argillaceous beds are grey, black, sometimes yellow or pink. Indurated layers due to slight silicification or ferruginisation are present throughout. Thin gypsum beds are numerous, and on resistivity logs of drill holes, are correlatable over large distances (Senior, 1971).|16-MAY-23
19936|Whitula Formation|Fossils|Core samples examined for spores and pollens were devoid of organic material probably due to contemporaneous oxidation.|16-MAY-23
19936|Whitula Formation|Relationships and boundaries|Conformable below Quaternary alluvium of the Cooper and Whitula Creek drainage systems and rests unconformably on the Early Tertiary Glendower Formation.|16-MAY-23
19936|Whitula Formation|Age reasons|The Whitula Formation is younger than the Early Tertiary Glendower Formation and underlies alluvium of Quaternary age.|16-MAY-23
19936|Whitula Formation|Proposed publication|The Geology of the Central Eromanga Basin, Bur. Miner. Resour. Aust. Rept|16-MAY-23
19936|Whitula Formation|First Reference|? 79/03877 NO.  79/03888 RefID 33078|16-MAY-23
19936|Whitula Formation|Name first published by|Senior B.R., Johnston I.D., 1974. Central Eromanga Basin, Queensland, 1:1 000 000 geological map.|16-MAY-23
19939|Whitworth Quartzite|Name source|Whitworth' holding , near the Paroo Range, 40 km north of Mount Isa, latitude 20o25'S, 139o35'E, Cloncurry 1:250 000 Sheet area.|16-MAY-23
19939|Whitworth Quartzite|Type section locality|Between Paroo and Conglomerate Creek, 16 km southwest of Julius dam, in the Prospector 1:100 000 Sheet area. About 1850 m of feldspathic sandstone form an upstanding plateau or series of planated ridges, from 562598 (base) to 573628 (top), I.e. from latitude 20o15'10"S, longitude 139o37'25"E, to latitude 20o13'35"S, longitude 139o38'E.|16-MAY-23
19939|Whitworth Quartzite|Extent|The formation is exposed in a north-trending belt 200 km long and 50 km wide. Mount Isa is near the southern limits of the formation.|16-MAY-23
19939|Whitworth Quartzite|Thickness range|650 to 2000 m.|16-MAY-23
19939|Whitworth Quartzite|Lithology|Highly feldspathic quartzite and sandstone, grey, buff and pale pink, fine to medium-grained, massive to blocky, thin-bedded; extensively cross-bedded and ripple-marked; minor pebbly beds, micaceous sandstone and siltstone.|16-MAY-23
19939|Whitworth Quartzite|Relationships and boundaries|Conformable between the Bortala Formation and Lochness Formation. Both upper and lower contacts are sharp lithological and topographic breaks. The much younger Mount Isa Group rests unconformably on the Whitworth Quartzite in the Paroo and Leander Ranges, 30 km and 50 km north of Mount Isa respectively.|16-MAY-23
19939|Whitworth Quartzite|Age reasons|Carpentarian; minimum age about 1650 m.y. set by intrusion of the Sybella Granite into time equivalent rocks west of Mount Isa.|16-MAY-23
19939|Whitworth Quartzite|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
19939|Whitworth Quartzite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
19939|Whitworth Quartzite|Comments|Remarks: This formation is the dominant unit in the redefined Myally Subgaroup (formerly the Myally Beds, Carter et al., 1961).|16-MAY-23
19939|Whitworth Quartzite|References|B051.|16-MAY-23
19939|Whitworth Quartzite|Name first published by|Glikson A.Y., Derrick G.M., Wilson I.H., Hill R.M., 1976|16-MAY-23
27305|Widdallion Sandstone Member|Name source|Widdallion Creek, a distributary of the Lawn Hill Creek.|16-MAY-23
27305|Widdallion Sandstone Member|Unit history|The rocks of the Widdallion Sandstone Member were included in the Lawn Hill Formation by Carter & others (1961). In the Carrara Range area of the Northern Territory they were mapped as part of the Bluff Range Beds by Smith & Roberts (1963).|16-MAY-23
27305|Widdallion Sandstone Member|Type section locality|Holostratotype: The holostratotype of the Widdallion Sandstone Member forms part of the hypostratotype of the Lawn Hill Formation. It lies between 528057 (base) and 523057 (top) in the Lawn Hill 1:100 000 Sheet area. It comprises approximately 550 m of friable, massive and blocky, thick bedded, reddish-brown to cream, lithic feldspathic fine grained arenite and feldspathic greywacke.|16-MAY-23
27305|Widdallion Sandstone Member|Extent|The unit crops out in a long narrow belt from the Gregory River in the south to Edith Range, 15 km northwest of Lawn Hill homestead in the north. It is also mapped in an inlier of Lawn Hill Formation in the headwaters of Stockyard Creek, 75 km northwest of Lawn Hill homestead, and in the Carrara Range area of the Northern Territory.|16-MAY-23
27305|Widdallion Sandstone Member|Thickness range|The holostatotype is approximately 550 m thick. This is one of the few sections where the thickness can be measured because of the presence of younger units. In other areas the Widdallion Sandstone Member is unconformably overlain by younger sediments of the South Nicholson Group or the Georgina Basin, and the top of the unit cannot be seen.|16-MAY-23
27305|Widdallion Sandstone Member|Lithology|The lithologies of the type section are consistent throughout the unit.|16-MAY-23
27305|Widdallion Sandstone Member|Relationships and boundaries|The unit is conformably overlain and underlain by siltstones and tuffs of the Lawn Hill Formation. Throughout most of the outcrop area, it is unconformably overlain by the Carpentarian South Nicholson Group and Cambrian limestones of the Georgina Basin.|16-MAY-23
27305|Widdallion Sandstone Member|Age reasons|Mid Proterozoic (Carpentarian).|16-MAY-23
27305|Widdallion Sandstone Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
27305|Widdallion Sandstone Member|References|B051; ?98/29491.|16-MAY-23
27305|Widdallion Sandstone Member|Proposer|Hutton L.J., Cavaney R.J., Sweet I.P.|16-MAY-23
33426|Wilfred Creek Igneous Complex|Name source|The unit is named after Wilfred Creek that drains the southern apex of the outcrop area.|16-MAY-23
33426|Wilfred Creek Igneous Complex|Unit history|Reiser (1971) previously included rocks of this unit in a large area of unnamed granite of probable Permian age in the CHINCHILLA 1:250 000 sheet.|16-MAY-23
33426|Wilfred Creek Igneous Complex|Geomorphic expression|The complex forms low wooded hills that range in elevation from about 360 to 420m and are locally capped by dissected surfaces of duricrust.|16-MAY-23
33426|Wilfred Creek Igneous Complex|Type section locality|The type area stretches for around 2km west-southwest of Di Di homestead.|16-MAY-23
33426|Wilfred Creek Igneous Complex|Extent|The Wilfred Creek Igneous Complex forms a lozenge-shaped body outcropping over an area of around 20km2 about 8km north-west of Boondooma Homestead and 30km west of Proston.|16-MAY-23
33426|Wilfred Creek Igneous Complex|Lithology|The unit dominantly consists of mafic igneous rock types, including diorite, quartz diorite, tonalite and more rarely gabbro. The unit also contains zones of monzogranite which commonly contains numerous large (up to 50cm across) xenoliths of the more mafic varieties which comprise up to 50% of the total rock. All the rock types are mid to dark grey, equigranular, and generally fine to medium grained, although coarser grained gabbros and megacrystic monzogranites occur locally. Poikiolitic hornblende dominates over biotite in the mafic rocks and both crystals show some evidence of alteration to chlorite.|16-MAY-23
33426|Wilfred Creek Igneous Complex|Relationships and boundaries|The northern culmination of the body is in contact with the Toondahra Granite, with which its relationship is uncertain.  To the south unit Rgbo (Boondooma Igneous Complex) surrounds the rest of the body.  Rgbo is interpreted as a younger intrusive unit than the Wilfred Creek Igneous Complex due to the presence of numerous gently-dipping pegmatite and aplite dykes and veins of Rgbo that cut the marginal phases of the Wilfred Creek Igneous Complex.|16-MAY-23
33426|Wilfred Creek Igneous Complex|Age reasons|No age dating of the unit has been undertaken, but a Middle to Late Triassic age is considered most likely.|16-MAY-23
33426|Wilfred Creek Igneous Complex|Comments|GEOPHYSICAL EXPRESSION::  The rocks of the complex exhibit moderately high magnetic susceptibilities, contrasting well on aerial magnetic surveys to the surrounding poorly magnetised granite units.  The unit also has a distinctive dark response on airborne radiometric images of the area.|16-MAY-23
20124|Wills Creek Granite|Name source|Named after Wills Creek, the main watercourse in the western part of Duchess 1:250 000 Sheet area.|16-MAY-23
20124|Wills Creek Granite|Unit history|None; included within outcrops mapped as Argylla Formation and Kalkadoon Granite by Carter & Opik (1963).|16-MAY-23
20124|Wills Creek Granite|Type section locality|N of the Dajarra/The Monument road, in the vicinity of GR 682892, Dajarra 1:100 000 Sheet area. Here the unit crops out as low rocky ridges of pink medium to coarse leucocratic granite, cut by some quartz veins and mafic dykes, and it can be seen to intrude and thermally metamorphose quartz-feldspar porphyry of the Leichhardt Volcanics.|16-MAY-23
20124|Wills Creek Granite|Extent|The unit crops out at several localities in the central part of Dajarra 1:100 000 Sheet area, Duchess 1:250 000 Sheet area, covering about 50 km2 mainly E of Wills Creek.|16-MAY-23
20124|Wills Creek Granite|Lithology|The unit consists of pale pink, leucocratic, biotite granite, which is mainly medium to coarse-grained and even-grained, and minor aplite.|16-MAY-23
20124|Wills Creek Granite|Relationships and boundaries|The granite intrudes undivided Tewinga Group and Leichhardt Volcanics and is cut by mafic dykes.|16-MAY-23
20124|Wills Creek Granite|Age reasons|Proterozoic|16-MAY-23
20124|Wills Creek Granite|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
20124|Wills Creek Granite|Comments|Remarks: Wills Creek Granite differs petrographically from other granitic units in the area by being made up predominantly of leucocratic, non-foliated, and non-porphyritic granite.|16-MAY-23
20124|Wills Creek Granite|References|R233; 98/29253.|16-MAY-23
20124|Wills Creek Granite|Defn Reference|82/22920|16-MAY-23
20124|Wills Creek Granite|Proposer|Blake D.H.|16-MAY-23
20288|Wire Creek Sandstone|Name source|Wire Creek, a tributary of the Nicholson River, into which it flows at GR 025193, Hedleys Creek 1:100 000 Sheet area (Sheet 6562, Qld).|16-MAY-23
20288|Wire Creek Sandstone|Unit history|Previously mapped as Westmoreland Conglomerate by Carter (1959), in the Westmoreland 1:250 000 Sheet area, Qld, and by Roberts et al. (1963), in the Calvert Hills 1:250 000 Sheet area, NT. The Westmoreland Conglomerate is the basal sedimentary unit in the McArthur Basin, and is separated from the Wire Creek Sandstone, the basal unit of the 'Lawn Hill Platform', by a belt of basement rocks. This belt probably formed a topographic high during deposition in both basins, and it is likely that units in the two basins were never connected.|16-MAY-23
20288|Wire Creek Sandstone|Type section locality|A small gorge where Wire Creek intersects the unit. The base is at GR 907367, Hedleys Creek 1:100 000 Sheet area, and the section extends east-southeastwards along Wire Creek for a distance of 1 km.|16-MAY-23
20288|Wire Creek Sandstone|Extent|Exposed as a strike ridge over a distance of 70 km from the headwaters of Peters Creek in the central part of the Hedleys Creek 1:100 000 Sheet area, Queensland, to the Fish River, in the southern central part of the adjacent Seigal 1:100 000 Sheet area in the Northern Territory.|16-MAY-23
20288|Wire Creek Sandstone|Thickness range|1-70 m.|16-MAY-23
20288|Wire Creek Sandstone|Lithology|Conglomeratic quartz sandstone, white to purple, medium to coarse grained, clayey; scattered pebbles of quartz and quartzite; conglomerate lenses, clasts up to 30 cm of quartz, quartzite and acid volcanics.|16-MAY-23
20288|Wire Creek Sandstone|Relationships and boundaries|Nonconformably overlies Cliffdale Volcanics and Nicholson Granite Complex - uneven erosion surface, and cobbles and boulders of underlying acid volcanics are present in basal conglomerate. Upper boundary sharp, but apparently conformable with overlying amygdaloidal basalts of the Peters Creek Volcanics.|16-MAY-23
20288|Wire Creek Sandstone|Age reasons|Proterozoic-Carpentarian. 1770 m.y., the age of the nonconformably underlying younger than Cliffdale Volcanics.|16-MAY-23
20288|Wire Creek Sandstone|Defn author|?Ian Sweet, 1976.|16-MAY-23
20288|Wire Creek Sandstone|Proposed publication|BMR Bulletin Precambarian geology of the Westmoreland Region, Northern Australia|16-MAY-23
20288|Wire Creek Sandstone|References|? 98/29257;|16-MAY-23
20288|Wire Creek Sandstone|Defn Reference|82/22568|16-MAY-23
20316|Withersfield Quartz Syenite|Name source|Parish of Withersfield.|16-MAY-23
20316|Withersfield Quartz Syenite|Geomorphic expression|The Withersfield Quartz Syenite forms highly dissected terrain with steep-sided ridges, a relief of over 100 m, and abundant outcrop.   On the Landsat 5 TM (1-4-7 BGR) image, the Withersfield Quartz Syenite is a well-defined oval body, red-brown in colour with high relief. It is strongly magnetic. U is uniformly high, but K and Th have variable response; they are high over most of the pluton, but are low along the southern margin.|16-MAY-23
20316|Withersfield Quartz Syenite|Type section locality|At 8351-538015 on the southeastern margin of the pluton. The grid reference is based on the AGD66 datum.|16-MAY-23
20316|Withersfield Quartz Syenite|Description at type locality|Pink, fine to medium-grained, equigranular hornblende-biotite quartz syenite.|16-MAY-23
20316|Withersfield Quartz Syenite|Extent|A northwest-trending oval pluton, 6 km long by 4 km wide, centred 5 km west of Silver Hills homestead, and intruding sedimentary units of the Drummond Basin.|16-MAY-23
20316|Withersfield Quartz Syenite|Lithology|Pink, fine to medium-grained, equigranular hornblende-biotite quartz syenite and quartz monzonite. The geophysical data suggest that the pluton is composite. Because the pluton largely lies outside the Anakie Inlier in the Drummond Basin sedimentary rocks, it was only briefly examined. Subsequent work by geologists from Billiton (Australia) Pty Ltd indicate that the pluton includes quartz monzonite as well as quartz syenite.|16-MAY-23
20316|Withersfield Quartz Syenite|Relationships and boundaries|The Withersfield Quartz Syenite intrudes the Late Devonian to Early Carboniferous Telemon Formation, Raymond Sandstone and Mount Hall Formation. Two small outcrop areas of olivine gabbro and dolerite within the pluton are possibly related to Tertiary basalt flows that overlie the pluton.|16-MAY-23
20316|Withersfield Quartz Syenite|Age reasons|Webb & McDougall (1968) obtained corrected ages of 287 to 306 Ma, by K-Ar dating of biotite and hornblende. The unit is therefore probably Late Carboniferous.|16-MAY-23
20316|Withersfield Quartz Syenite|References|WEBB, A.W. & MCDOUGALL, I., 1968: The geochronology of the igneous rocks of Eastern Queensland. Journal of the Geological Society of Australia, 15, 313-346.|16-MAY-23
24583|Wonnemarra Rhyolite|Name source|The name Wonnemarra is derived from the Parish of Wonnemarra, County of Esmeralda; Georgetown, Queensland 1:250 000 series cadastral sheet.|16-MAY-23
24583|Wonnemarra Rhyolite|Unit history|Branch (1966), included the Wonnemarra Rhyolite in the "Croydon Volcanics" (undivided), although he did note the presence of a basal "sheet" in the east, made up of grey, rhyolitic to rhydacitic rocks probably equivalent to the Wonnemarra, B Creek, and Carron Rhyolites. The unit was informally named and described as 'Wonnemarra rhyolite' by Mackenzie (1983).|16-MAY-23
24583|Wonnemarra Rhyolite|Geomorphic expression|Like the Idalia Rhyolite, The Wonnemarra Rhyolite is characterised by moderate, commonly rocky relief, subdued to steep slopes and sparse vegetation cover. Its soil cover is a little darker than that of the Carron Rhyolite.|16-MAY-23
24583|Wonnemarra Rhyolite|Type section locality|The type section of the unit extends from GR 7460-055280, near Snake Creek mine, where the lower contact is faulted, but is very close to the base, southwestward to -045276 (top). The section consists of massive, blue-grey to green-grey, medium-grained, moderately crystal-rich rhyolitic ignimbrite containing sparsely scattered, rounded pellets of graphite up to 5 mm long; its thickness is about 500 m. The base of the unit is faulted here, but elsewhere it unconformably overlies low-grade metasediments of the Middle Proterozoic Etheridge and Langlovale Groups. Its top is marked by an abrupt transition into dark grey, fine-grained, crystal-poor rhyolitic ignimbrite and sparsely porphyritic, flow-banded rhyolite of the Carron Rhyolite.|16-MAY-23
24583|Wonnemarra Rhyolite|Extent|The Wonnemarra Rhyolite crops out as a curved, discontinuous lens, extending from GR 7460-074393 14 km southward to -057250, in the Dingo Creek-Snake Creek area.|16-MAY-23
24583|Wonnemarra Rhyolite|Thickness range|The unit varies considerably in thickness, which is difficult to estimate because of the lack of dip indicators, but probably ranges between 450 m and 800 m over most of its strike length.|16-MAY-23
24583|Wonnemarra Rhyolite|Lithology|Like the Idalia Rhyolite, the Wonnemarra Rhyolite consists of medium greenish to bluish-grey, medium-grained, moderately crystal-rich rhyolitic ignimbrite, containing 10 to 20 percent by volume crystals (or crystal fragments) of quartz, K-feldspar, and sericitised plagioclase, and up to 5 percent variably chloritised biotite. Fayalite, variably altered to chlorite or bowlingite, or replaced by green biotite and magnetite, is commonly present (up to 1%), and graphite, generally as rounded pellets, up to 5 mm across is present in trace amounts. The rock is extensively recrystallised near the Dregger Granite.|16-MAY-23
24583|Wonnemarra Rhyolite|Relationships and boundaries|The Wonnemarra Rhyolite appears to unconformably overlie rocks of the Proterozoic Etheridge and Langlovale Groups in places (north of Snake Creek), and is faulted against them in others. It is conformably overlain by the Carron Rhyolite, another formation of the Croydon Volcanic Group, from which it is distinguished primarily by its more abundant, larger crystals. It is intruded and, in part, recrystallised and hornfelsed by the Dregger Granite, and is unconformably overlain in places by Jurassic Hampstead Sandstone and Tertiary to Quaternary continental sediments.|16-MAY-23
24583|Wonnemarra Rhyolite|Age reasons|The Wonnemarra Rhyolite is considered to be of Middle Proterozoic age (about 1400 +/- 75 Ma; Black, 1973), the same as the Idalia Rhyolite.|16-MAY-23
24583|Wonnemarra Rhyolite|Defn author|Mackenzie D.E., Henderson G.A.M., Warnick J.V., Bain J.H.C., 1985|16-MAY-23
24583|Wonnemarra Rhyolite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
24583|Wonnemarra Rhyolite|References|73/050; B076.|16-MAY-23
24583|Wonnemarra Rhyolite|Defn Reference|86/25125|16-MAY-23
24583|Wonnemarra Rhyolite|Proposer|Mackenzie D.E., Warnick J.V., Henderson G.A.M.|16-MAY-23
26233|Woolshed Mountain Granodiorite|Unit history|This name was proposed by Cranfield and Schwarzbock (1974b) for the granodiorite that occurs at the boundary of the ESK and NANANGO sheets, south southwest of Blackbutt.  Murphy & others (1976) extended the unit by mapping in the Gympie 1: 250 000 Sheet area.  The extent of the unit  approximates the original defined extents shown by previous regional mapping.|16-MAY-23
26233|Woolshed Mountain Granodiorite|Geomorphic expression|The granodiorite forms undulating lightly timbered country ranging in elevation from about 340 to 500m above sea level, and forms, with a typical dendritic drainage pattern.|16-MAY-23
26233|Woolshed Mountain Granodiorite|Lithology|Cranfield & others (1976) described the granodiorite as a pale pinkish-grey, mottled by dark biotite flakes, medium to coarse-grained, holocrystalline, and hypidiomorphic granular.  Petrography:: Thin section constituents are zoned plagioclase (andesine), with sericite alteration, quartz, orthoclase, and biotite, together with minor hornblende, magnetite, epidote, clinozoisite, and chlorite.  Accessories include zircon, apatite, and allanite.  The plagioclase is of two generations: the earlier generation is coarser-grained, minutely oscillatory zoned, and saussuritised (oligoclase to andesine in composition); the later generation is fresh unzoned andesine.  Orthoclase is perthitic, and has reacted with biotite to form iron oxides, and myrmekitic and wormlike intergrowths. Quartz forms anhedral grains. Biotite is pleochroic brown to green, is altered to epidote and chlorite, and has inclusions of wedge- shaped crystals of allanite and euhedral zircon. Hornblende is blue- green, sub- hedral, and constitutes approximately 1 per cent of the rock. Apatite typically occurs as inclusions in plagioclase.  In the current mapping thin section from AMG 404469 7011358, contained biotite and hornblende (locally twinned) that have minor metamict textures and minor alteration to chlorite.  There was no apparent difference in rock type from the magnetic and non-magnetic pats of the unit.|16-MAY-23
26233|Woolshed Mountain Granodiorite|Relationships and boundaries|The unit intrudes the Sugarloaf Metamorphics and is intruded by the Djuan Tonalite.  Cranfield & others (1976) reported intrusions of spherulitic rhyolite dykes and a basic dyke within this unit.  East west trending rhyolite dykes up to 5m wide appear to be offset by minor faulting at AMG 405980 7012470.  Scott (1963) reported the contact between the Djuan Tonalite and Woolshed Mountain Granodiorite is gradational, and can be distinguished as a mixed phase over less than 15m. Contact metamorphism of the country rock by the granodiorite is not pronounced.  The unit is unconformably overlain by Main Range Volcanics and Tertiary sediments in the north on NANANGO and by a small area of Main Range Volcanics at Woolshed Mountain on ESK.  A small area of Woolshed Mountain Granodiorite was recorded within the Djuan Tonalite at AMG 402000 7007300.|16-MAY-23
26233|Woolshed Mountain Granodiorite|Age reasons|The Woolshed Mountain Granodiorite was initially assigned a radiometric (K/Ar) age of 253 +/- 8 Ma.  This was recalculated to 258.2 +/- 8 Ma (Late Permian) by Day & others (1983).|16-MAY-23
26233|Woolshed Mountain Granodiorite|Geophysical Expression|The RTP magnetic image shows a general low response over the Woolshed Mountain Granodiorite.  However the south and southeast part of the body has a higher response, possibly indicating that the Djuan Tonalite occurs beneath the granodiorite in this area. At AMG 404867 7013056, in the area of low magnetic response on the image, magnetic susceptibility readings average 31 x 10-5SI units. At AMG 404469 7011358, in the area of higher magnetic response on the image, magnetic susceptibility readings average 436 x 10-5SI units.  The radiometric image shows distinct pink tones for the area of outcrop of the Woolshed Mountain Granodiorite which contrast well with the darker response of the Djuan Tonalite and the lighter response of the Sugarloaf Metamorphics.|16-MAY-23
26233|Woolshed Mountain Granodiorite|References|CRANFIELD, L.C. & SCHWARZBOCK, H., 1974, New and revised stratigraphic names for the Ipswich 1:250 000 Sheet area.,Queensland Government Mining Journal, 75, 322-323.CRANFIELD, L.C., SCHWARZBOCH, H. and DAY, R.W.,1976, Geology of the Ipswich and Brisbane 1:250 000 Sheet areas. Geological Survey of Queensland Report, 95. Regional Geology.DAY, R.W.,1983, Geology of Queensland,Department of Mines.MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.SCOTT, I.F.,1963, The geology of the Emu Creek area southeast Queensland.,University of Queensland BSc honours thesis (unpublished).|16-MAY-23
27306|Woonigan Granite|Name source|Named after Woonigan railway siding on the main Mount Isa to Townsville railway line, about 25 km NW of Duchess, Duchess 1:100 000 Sheet area (Duchess 1:250 000 Sheet area).|16-MAY-23
27306|Woonigan Granite|Unit history|Previously mapped as Kalkadoon Granite and Leichhardt Metamorphics (Carter & Opik, 1963).|16-MAY-23
27306|Woonigan Granite|Type section locality|About 5.5 to 6 km NE of Woonigan railway siding, from about GR 687599 to GR 704591, in area drained by unnamed tributaries of Alligator Creek. In this area the unit consists of mainly medium to coarse-grained, even-grained to sparsely porphyritic, leucocratic biotite granite, together with minor finer grained leucocratic, porphyritic biotite granite adjacent to some contacts with country rocks.|16-MAY-23
27306|Woonigan Granite|Extent|The granite crops out as small discrete plutons and pods on the margins of the Kalkadoon Granite belt on the Duchess 1:100 000 Sheetarea. It is most extensively exposed NE of Woonigan railway siding.|16-MAY-23
27306|Woonigan Granite|Lithology|The main rock types present in the larger bodies are non-foliated, coarse to fine, even-grained to slightly porphyritic biotite leucogranite and leucocratic porphyritic biotite microgranite. Many small lpods and marginal zones of the larger plutons comprise mainly non-foliated leucocratic porphyritic microgranite containing quartz and feldspar phenocrysts in a fine-grained groundmass containing small scattered aggregates of biotite grains. In a few places relatively thick (10-15 m) veins of leucogranite intrude Kalkadoon Granite and are characterised by fairly strongly foliated (foliation generally parallel to contacts) marginal zones containing small feldspar and quartz phenocrysts in a fine-grained groundmass, and coarser, more even-grained central parts. However, many leucogranite veins assumed to be related to the Woonigan Granite are non-foliated and even-grained.|16-MAY-23
27306|Woonigan Granite|Relationships and boundaries|The Woonigan Granite intrudes Kalkadoon Granite and Leichhardt Volcanics. It is cut by numerous non-foliated to foliated amphibolitic metadolerite dykes, many of which show relict igneous textures, and by scattered dykes of grey, porphyritic granophyre (which also cut Leichhardt Volcanics).|16-MAY-23
27306|Woonigan Granite|Age reasons|Proterozoic.|16-MAY-23
27306|Woonigan Granite|Proposed publication|Blake & others, in preparation.|16-MAY-23
27306|Woonigan Granite|Comments|Remarks: A possible equivalent of the Woonigan Granite is the Wills Creek Granite in the Dajarra 1:100 000 Sheet area so the south. The Woonigan Granite has not been isotopically dated and consequently its age is uncertain.|16-MAY-23
27306|Woonigan Granite|References|R233; 98/29253.|16-MAY-23
27306|Woonigan Granite|Defn Reference|82/22920|16-MAY-23
27306|Woonigan Granite|First Reference|82/22710  82/22663|16-MAY-23
27306|Woonigan Granite|Proposer|Bultitude R.J.|16-MAY-23
27306|Woonigan Granite|Resdate|18-FEB-1980|16-MAY-23
33431|Wooroolin Granite|Name source|The granite is named after the small township of Wooroolin, located 6km to the northeast of the unit.|16-MAY-23
33431|Wooroolin Granite|Unit history|Murphy & others (1976) previously mapped the unit as part of the Boondooma Igneous Complex.|16-MAY-23
33431|Wooroolin Granite|Geomorphic expression|The unit is moderately well exposed as recessive undulating country forming the valley of the Stuart River.  Elevations range from about 390 m to 438m.|16-MAY-23
33431|Wooroolin Granite|Type section locality|The type area is on the north shore of Gordonbrook Dam around AMG 375700 7074400.  The grid reference is based on the AGD66 datum.|16-MAY-23
33431|Wooroolin Granite|Extent|The unit forms an arcuate 1-2km wide belt, extending southeast for around 15km from West Wooroolin homestead, north of Kingaroy.|16-MAY-23
33431|Wooroolin Granite|Lithology|The unit is dominated by leucocratic, pink, medium to locally fine grained, equigranular biotite granite.  The biotite occurs as discrete plates scattered throughout the rock.  Blocky aplitic phases occur locally.  Potassic and limonitic alteration of the granite is widepread and fresh exposure is rare.  The granite is intruded by a network of shallow dipping aplite veins and occasional thick basalt dykes.|16-MAY-23
33431|Wooroolin Granite|Relationships and boundaries|The granite intrudes the Devonian to Carboniferous Maronghi Creek beds and their probable metamorphosed equivalents, the Fifer Creek Metamorphics.  The relationship between the lithologically different Stuart River and Hivesville Granites to the north is unknown, although the Wooroolin Granite may be co-genetic with the latter.  The Wooroolin Granite is locally overlain by silicified Tertiary sandstones and lateritised basalt flows of the Main Range Volcanics (and intruded by related basalt dykes).|16-MAY-23
33431|Wooroolin Granite|Age reasons|The unit has yielded a 274+/-28Ma Rb/Sr whole rock age and a 258.2 Ma K/Ar biotite age from a site 5km south-west of Memerambi (Webb & McDougall, 1968). These dates are nominally of Permian age, but the imprecision of the error bar on the Rb/Sr age makes it possible that the granite ranges up into the Late Triassic.|16-MAY-23
33431|Wooroolin Granite|Comments|GEOPHYSICAL EXPRESSION::  The unit has a low magnetic response on aeromagnetic images and displays pink tones on the radiometric images.|16-MAY-23
33431|Wooroolin Granite|References|MURPHY, P.R., SCHWARZBOCK, H., CRANFIELD, L.C., WITHNALL, I.W., &  MURRAY, C.G. ,1976,Geology of the Gympie 1:250 000 Sheet Area, Geological Survey of Queensland, Report 96",Regional Geology, Gympie 1:250 000 Sheet.WEBB, A.W. & MCDOUGALL, I.1968, The geochronology of the igneous rocks of eastern Queensland. ,"Journal of the Geological Society of Australia., 15, 313-346|16-MAY-23
24588|Wyandotte Formation|Name source|Wyandotte Creek/Wyandotte Station; GR 773198 Conjuboy 1:100 000 Sheet (7860).|16-MAY-23
24588|Wyandotte Formation|Type section locality|Exposed on the western bank of Wyandotte Creek at approx. 7860 773198 (18o40'45"S 144o50'20"E). 5 m of partially indurated blue-grey muds, gravels, sandy gravels and well sorted sands overlying orange-brown basement regolith. Modern soils (black and loamy) cap and obscure the nature of the upper boundary.|16-MAY-23
24588|Wyandotte Formation|Extent|The unit is exposed in ribbon-like aspect along the course of Wyandotte Creek for approx. 10 km upstream of the junction with Dry River on Wyandotte Station. Distribution beyond Wyandotte Creek is unknown at present.|16-MAY-23
24588|Wyandotte Formation|Thickness range|Never more than 15 metres.|16-MAY-23
24588|Wyandotte Formation|Lithology|Two distinctive lithofacieas associations. The lower association (Unit A) is 2-3 m thick and sits unconformably on basement regolith. It consists of a basal granule gravel 10-5 cm thick and an overlying massive blue-grey clay containing flecks of carbonised plant material 1-10 mm in diameter. Lenticular granule gravel stringers 1-20 m in length occur within the massive blue-grey clay. In-situ occurrences of disarticulated bones and teeth are noted for the basal and lenticular granule gravels but not for the massive blue-grey clay. Unit B lithofacies association overlies Unit A but in some outcrops lies directly on basement. It fines upwards from a basal cobble to boulder gravel 15-75 cm thick into crossbedded fine-medium sands and  laminated to crosslaminated sands up to 2 m thick. Minor silt and mud drapes 1-10cm thick above the gravel bed also outcrop along section. The contact between Units A & B is erosional. It represents the erosion of typical vertical accretion facies of Unit A by stream channel action depositing the classic lateral accretion facies of Unit B. Units A & B represent different depositional regimes within the one depositional system. Unit B is capped by loamy to black soil containing basalt boulders. The upper boundary is obscure but in many places appears gradational. In-situ disarticulated bones and teeth are noted for the basal gravel and the gravelly sands directly above the basal gravel. Other lithofacies found elsewhere and not represented in the type section are a grey diatomaceous clay facies that occurs within both units and a chocolate brown flecked clay facies that occurs as a vertical accretion equivalent to Unit B.  Unit B also shows areas of patchy carbonate cement (mainly near the type section) and lenticular concentrations of gastropod and bivalve debris.|16-MAY-23
24588|Wyandotte Formation|Fossils|Vertebrate fossil fauna: Unit A: undet Teleost fish; undet Chelid turtles; Meiolania cf platyceps; Megalania prisca; undet Varanid lizard/s; undet Elapid snakes(2); undet Ziphodont crocodile/s; Pallimnarchus pollens/Crocodylus porosus; undet Anatid birds; Anas sp.; Anseranus semipalmata; undet Palorchestid diprotodontid/s; undet Zygomaturine diprotodontid; Macropus sp.; Rattus sp.; Isoodon macrorous; and Antechinus sp.. Unit B: undet Chelid turtle; Anhinga Mealanogaster; Protemnodon sp.; Rattus sp.; and ?Pseudomys sp..  Fauna not in-situ: Wonambi cf naracoortensis; Diprotodon optatum; ?Eowenia sp.; Phascolonus cf gigas; and Dasyurus sp..|16-MAY-23
24588|Wyandotte Formation|Relationships and boundaries|Overlies basement granitoids and metamorphics of Proterozoic and ?Palaeozoic age (Griffin, 1977), their lateritised equivalents, lateritised sediments and other indurated sediments of unassigned age and regolith. It occurs within a broad valley bounded to the south by a narrow basalt flow and to the north by basement outcrop. The palaeovalley that accreted the sediments is essentially coincident with the valley occupied by the modern-day creek. The modern creek is eroding and exposing the older fill within this valley.|16-MAY-23
24588|Wyandotte Formation|Age reasons|The basalt flow forming the southern margin of the Wyandotte valley is perched on the topographic high point between the Dry River to the south and Wyandotte Creek to the north. This flow is dated at 410,000 ybp (Griffin, 1977) and fills a narrow channel cut into unassigned age (post laterite) sediments and other basement rocks. The broad valley now containing the Wyandotte Formation could only have begun eroding after the basalt filled the earlier channel and reorganised the drainage. Carbon from the basal gravels of Unit A submitted for C-14 dating proved to be beyond range (>45,000 ybp). Given that the valley did not begin forming until after 410,000 ybp it seems likely that the base of Unit A is no older than 200,000 ybp. Bivalve shell from the base of Unit B returned a C-14 date of 30,400 ybp. The Wyandotte Formation is therefore a Late Pleistocene accumulation, a fact reflected by the typical Late Pleistocene nature of the vertebrate fossil fauna.|16-MAY-23
24588|Wyandotte Formation|Proposed publication|Australian Journal of Earth Sciences|16-MAY-23
24588|Wyandotte Formation|Comments|category 2|16-MAY-23
24588|Wyandotte Formation|First Reference|93/27510 McNamara, Qld Mus. Mem. 28(1) 1990.|16-MAY-23
24588|Wyandotte Formation|Proposer|McNamara G.C.|16-MAY-23
20695|Wyandra Sandstone Member|Name source|Wyandra' town; GR 36397618, Wyandra 1:250 000 Sheet Queensland.|16-MAY-23
20695|Wyandra Sandstone Member|Type section locality|The type section lies between 1170' (356 m) and 1225' (373 m) in water bore no. 2049 (QIWSC records) which is located 15 km northeast of Wyandra town (27o10'10"S, Long. 146o5'30"E).|16-MAY-23
20695|Wyandra Sandstone Member|Extent|Widespread in the cental part of the Eromanga Basin in Queensland, and extends into northeast South Australia and northwest New South Wales.|16-MAY-23
20695|Wyandra Sandstone Member|Thickness range|Range from 3 to 18 m, with variations occurring gradually over considerable distances.|16-MAY-23
20695|Wyandra Sandstone Member|Lithology|Medium to coarse grained quartzose to sublabile sandstone with scattered pebbles and carbonate cement. Driller's lithological logs of water bores regard it as 'sandrock' or 'sandstone'. The sandstone is porous and permeable and stratigraphically is the highest major aquifer in the Great Artesian Basin.|16-MAY-23
20695|Wyandra Sandstone Member|Depositional environment|This widespread sandstone overlies the paralic Cadna-owie Formation is very consistent in thickness and may well be a beach sand representing the widespread Lower Cretaceous marine transgression.|16-MAY-23
20695|Wyandra Sandstone Member|Relationships and boundaries|The member forms the upper part of the Cadna-owie Formation in much of the Eromanga Basin, and is conformably overlain by the Doncaster Mudstone.|16-MAY-23
20695|Wyandra Sandstone Member|Age reasons|Spores a microplankton of Evan's (1966) spore division Kla were recovered from BMR Eulo 1 (Core 3) in the Eulo Ridge area (Senior, 1971). These are Neocomian to Early Aptian in age. On stratigraphic grounds the age of the member is Late Neocomian or earliest Aptian.|16-MAY-23
20695|Wyandra Sandstone Member|Defn author|Senior B.R., Exon N.F., Burger D., 1975|16-MAY-23
20695|Wyandra Sandstone Member|Defn author|Senior B.R., Exon N.F., Burger D., 1975|16-MAY-23
20695|Wyandra Sandstone Member|Proposed publication|Journal of the Geological Society of Australia|16-MAY-23
20695|Wyandra Sandstone Member|Comments|Notes: This Member was formerly included and described as a sandstone bed within the informal division "Upper Hooray Sandstone". The "Upper Hooray Sandstone" is laterally continuous with the Cadna-owie Formation as defined by Freytak et al (1967). The name Cadna-owie Formation is adopted and the Wyandra Sandstone Member is a new name to define the prominent sandstone bed at the top of this Formation. The member is readily interpreted on gamma-ray logs at water bores and wireline logs of petroleum exploration wells and by this means can be correlated over large distances.|16-MAY-23
20695|Wyandra Sandstone Member|References|79/03882|16-MAY-23
20695|Wyandra Sandstone Member|Defn approved by|Playford G.E. (see Party file 73/574)|16-MAY-23
20722|Wynyard Metamorphics|Name source|Wynyard Holding (Zig Zag 1:100 000 Cadastral Series map).|16-MAY-23
20722|Wynyard Metamorphics|Unit history|Previously mapped as Anakie Metamorphics (Malone & others, 1964; Veevers & others, 1964a, b) and now part of the Anakie Metamorphic Group.|16-MAY-23
20722|Wynyard Metamorphics|Geomorphic expression|The Wynyard Metamorphics generally form a more recessive topography than the Monteagle Quartzite and strike ridges are less developed. The unit has reddish tones on aerial photographs and orange tones on the images from Landsat 5 TM bands 1-4-7 (BGR). This is in part due to a veneer of ferruginised gravels, a remnant of more extensive Tertiary cover that may have been thicker over the less resistant Wynyard Metamorphics. It may also be due in part to the greater abundance of more Fe-rich biotite schists compared with the Monteagle Quartzite, although the reddish tone is not apparent south of Peak Vale where the gravels are absent. Most of the unit is outside the area of the airborne geophysical survey. However, south of Peak Vale, the unit is recognisable on the radiometric images by its higher response in the K and Th channels.|16-MAY-23
20722|Wynyard Metamorphics|Type section locality|Along the Clermont-Barcaldine power line between 8351-296428 (the boundary with the Monteagle Quartzite) and 276420 (the faulted contact with the Late Devonian-Carboniferous Drummond Group).  The grid references are based on the AGD66 datum.|16-MAY-23
20722|Wynyard Metamorphics|Extent|A belt up to 5 km wide extending for about 45 km south from the Clermont-Alpha road near Red Mountain to the Zig Zag Range in the extreme west of the Anakie Inlier. A small area of phyllite and meta-arenite, about 5 km west of Moorlands homestead, has also been assigned to the Wynyard Metamorphics. It is separated from the main area of Wynyard Metamorphics by extensive Cainozoic deposits.|16-MAY-23
20722|Wynyard Metamorphics|Lithology|Predominantly grey to brown, micaceous, feldspathic to quartzose meta-arenite and muscovite-biotite schist. The metamorphic grade is mainly lower amphibolite facies, except in the Moorlands area where it is greenschist facies. Retrogressed porphyroblasts of staurolite and andalusite are present locally.|16-MAY-23
20722|Wynyard Metamorphics|Relationships and boundaries|The Wynyard Metamorphics structurally overlie the Monteagle Quartzite, and are distinguished from it by the lack of white quartzite and greater abundance of biotite-rich schist. The lower grade rocks west of Moorlands homestead resemble the Scurvy Creek Meta-arenite, and it is possible that the Wynyard Metamorphics are equivalent to this unit. The Monteagle Quartzite could thus be equivalent to the Hurleys Metamorphics.    The Wynyard Metamorphics are intruded by the various plutons that are part of or related to the Devonian Retreat Batholith, and also by a swarm of felsic dykes north of Eastern Creek. They are overlain unconformably by the Devonian-Carboniferous Silver Hills Volcanics and various Cainozoic deposits.|16-MAY-23
20722|Wynyard Metamorphics|Age reasons|The original age is still uncertain, but is probably Early Cambrian or Neoproterozoic.|16-MAY-23
20722|Wynyard Metamorphics|References|MALONE, E.J., CORBETT, D.P.W., & JENSEN, A.R., 1964: Geology of the Mount Coolon 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 64.VEEVERS, J.J., RANDAL, M.A., MOLLAN, R.G., & PATEN, R.J., 1964a: The geology of the Clermont 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report, 66.VEEVERS, J.J., MOLLAN, R.G., OLGERS, F., & KIRKEGAARD, A.G., 1964b: The geology of the Emerald 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 68.|16-MAY-23
24133|Yan Can Greenstone Member|Name source|Yan Can Block, Portion 13, Parish of Drummond (Queensland Department of Lands, Parish map).|16-MAY-23
24133|Yan Can Greenstone Member|Unit history|Previously mapped as Anakie Metamorphics (Malone & others, 1964; Veevers & others, 1964a, b) and now part of the Anakie Metamorphic Group.|16-MAY-23
24133|Yan Can Greenstone Member|Geomorphic expression|The unit can be identified on aerial photographs and Landsat 5 TM images (1-4-7 BGR) by red or orange colours. It is topographically more subdued than the surrounding metasedimentary rocks. On the radiometric geophysical images, it is recognised by its low response in all three (K, Th and U) channels. The greenstone has a low magnetic susceptibility and consequently there is very little difference it and the metasedimentary rocks on magnetic images.|16-MAY-23
24133|Yan Can Greenstone Member|Type section locality|Along the Clermont-Alpha road between 8352-424719 and 396699.  The grid references are based on the AGD66 datum.|16-MAY-23
24133|Yan Can Greenstone Member|Description at type locality|Fine-grained, green, foliated greenstone is exposed in road cuttings and adjacent creeks and gullies.|16-MAY-23
24133|Yan Can Greenstone Member|Extent|Centred about 25 km west-southwest of Clermont, straddling the Clermont-Alpha road. It is about 12 km2 in area, and consists of two lobes. The eastern lobe is the core of a northerly-trending, doubly plunging synform, and narrows westwards into a doubly plunging antiform. The western lobe forms the western limb of the antiform. A narrow 'tail' to the western lobe, about 0.3 km wide, can be traced for about 6 km south where it appears to lens out. The Yan Can Greenstone Member is formally named because of it size and relative homogeneity compared with the numerous smaller belts of greenstone in the Bathampton Metamorphics.|16-MAY-23
24133|Yan Can Greenstone Member|Lithology|Superficially similar to the other greenstones in the Bathampton Metamorphics, as described above. However, the rocks of the Yan Can Greenstone Member are mostly not as strongly laminated and are commonly non-laminated. Many outcrops are well foliated and consist of green chlorite schist with a platy, anastomosing foliation. In places, the foliation encloses massive to weakly foliated, ellipsoidal pods of fine-grained greenstone up to 1 m across and several metres long.|16-MAY-23
24133|Yan Can Greenstone Member|Relationships and boundaries|Part of the Bathampton Metamorphics, appearing to lie stratigraphically between the unnamed thin greenstone units (see above) and the Rolfe Creek Schist.|16-MAY-23
24133|Yan Can Greenstone Member|Age reasons|The original age is still uncertain, but is probably Early Cambrian or Neoproterozoic.|16-MAY-23
24133|Yan Can Greenstone Member|References|MALONE, E.J., CORBETT, D.P.W., & JENSEN, A.R., 1964: Geology of the Mount Coolon 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 64.VEEVERS, J.J., RANDAL, M.A., MOLLAN, R.G., & PATEN, R.J., 1964a: The geology of the Clermont 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report, 66.VEEVERS, J.J., MOLLAN, R.G., OLGERS, F., & KIRKEGAARD, A.G., 1964b: The geology of the Emerald 1:250 000 Sheet area, Queensland. Bureau of Mineral Resources, Australia, Report 68.|16-MAY-23
20835|Yappo Member|Name source|Named after Yappo Creek, the headwaters of which drain part of the outcrop area in the Duchess and Oban 1:100 000 Sheet areas (Duchess and Urandangi 1:250 000 Sheet areas).|16-MAY-23
20835|Yappo Member|Unit history|Mapped mainly as Mount Guide by Carter & Opik (1963), and included as part of the Rifle Creek beds (informal name) by Bultitude & others (1977).|16-MAY-23
20835|Yappo Member|Type section locality|From GR 449769 to GR 486754, about 3 km N of Mount Guide, in the NW corner of the Duchess 1:100 000 Sheet area. Here the member consists mainly of grey pebbly metagreywacke, and metagreywacke conglomerate and grit, together with minor meta-arkose, and labile, sericitic, feldspathic, and quartzose meta-arenite and quartzite containing heavy mineral-rich laminae.|16-MAY-23
20835|Yappo Member|Extent|The member is exposed in N-trending belts and forms undulating to hilly country in the W parts of the Duchess and Dajarra and the E parts of the adjoining Ardmore and Oban 1:100 000 Sheet areas.|16-MAY-23
20835|Yappo Member|Thickness range|The Yappo Member displays marked thickness variations. In the Duchess 1:100 000 Sheet area it is about 3750 m thick in the type section, locally less than 100 m thick in the central west, and about 700 m thick in the SW.|16-MAY-23
20835|Yappo Member|Lithology|The rocks are generally as in the type section. Locally, meta-arkose and conglomeratic meta-arkose are common to predominant rock types. Other, less abundant rock types present locally are sericite schist, muscovite-biotite schist, metasiltstone, epidotic quartzite, metabasalt and pink to grey? felsic tuff. The unit has undertone greenschist to amphibolite grade regional metamorphism, and a N-trending axial plane cleavage or schistosity is present in many areas.|16-MAY-23
20835|Yappo Member|Relationships and boundaries|The Yappo Member overlies the Bottletree Formation, apparently conformably. Both units contain similar sedimentary rock types, the arbitrary boundary ;between them being placed so as to exclude all but very thin possible felsic metavolcanic units from the Yappo Member. The Yappo Member has a gradational contact wioth the overlying upper member of the Mount Guide Quartzite, the boundary being placed at the marked topographic break between undulating and hilly terrain formed on the Yappo Member and upstanding ridges formed on the overlying meta-arenites and quartzites. The formation is cut by rare quartz-feldspar porphyry dykes, by a small quartz-feldspar body tentatively assigned to the Garden Creek Porphyry, and by numerous dykes and small pods of amphibolitic metadolerite.|16-MAY-23
20835|Yappo Member|Identifying features|Definition: In the Duchess and Urandangi 1:250 000 Sheet areas, two units have been delineated within the Mount Guide Quartzite as defined by Carter & others (1961). The basal unit is characterised by an abundance of regionally metamorphosed greywacke, greywacke conglomerate and grit, and arkose, and is defined as the Yappo Member. The overlying sequence of mainly meta-arenite and quartzite forming the upper part of the Mount Guide Quartzite has not been formally named.|16-MAY-23
20835|Yappo Member|Age reasons|Precambrian. The member overlies the Bottletree Formation provisionally dated at about 1800 m.y. (R W Page, BMR, personal communication, 1980).|16-MAY-23
20835|Yappo Member|Proposed publication|Blake & others, in preparation.|16-MAY-23
20835|Yappo Member|Comments|Remarks: The Yappo Member is equivalent to the lower part of the Mount Guide Quartzite as defined by Carter & others (1961) but, as the unit contains very little quartzite and is radily mappable, it has been referred to a separate member. The unit is equivalent to most of the lower Mount Guide Quartzite mapped in sheet areas to the N (Derrick & others, 1976).|16-MAY-23
20835|Yappo Member|References|J0204/06;B051; 98/29253; 79/01220.|16-MAY-23
20835|Yappo Member|Defn Reference|82/22920|16-MAY-23
20835|Yappo Member|First Reference|81/21343|16-MAY-23
26242|Yardida Tillite|Name source|Yardida Bore, Hay River 1:250 000 Sheet area.|16-MAY-23
26242|Yardida Tillite|Unit history|This is the glacial unit of the Field River Beds of Smith (1963).|16-MAY-23
26242|Yardida Tillite|Type section locality|A composite section comprised on section GEO709 (4 part sections between Middle Dam and BMR Hay River No. 5), the full length of BMR Hay River Nos. 5 & 6, the area 6 km SSE of Aroota Bore, and the section at depth at the end of seismic traverse 3 (grid reference 53KRQ047288) - all these are on the Field River Anticline, Adam Special 1:100 000 Geological Sheet. The cores are stored in the BMR Core & Cuttings Laboratory, Canberra|16-MAY-23
26242|Yardida Tillite|Extent|The formation is exposed on the Hay River, Tobermory and Mt Whelan 1:250 000 Sheet areas.|16-MAY-23
26242|Yardida Tillite|Thickness range|2900 m measured and estimated in the type section, apparently thinning to about 650 m in the Desert Syncline (where very poor outcrop and faulting preclude an accurate estimate).|16-MAY-23
26242|Yardida Tillite|Lithology|Light to dark green-grey diamictite and laminated siltstone with infrequent fine to very coarse grained brown to grey sandstone and arkose, rarely pebbly. Locally at the top there is at least 102 m of dark grey, laminated, dolomitic shale with, in its lower half, abundant lenses of dolomite (in BMR Hay River No. 10, Adam Special 1:100 000 Geological Sheet).|16-MAY-23
26242|Yardida Tillite|Relationships and boundaries|The unit overlies the Yackah Beds with inferred disconformity and is disconformably overlain by red arkose, siltstone and shale of the Black Stump Arkose (Walter, 1979). The top of the unit is taken at the base of the overlaying red-brown sequence; this can be difficult to locate precisely, as in BMR Hay River No. 7 (Adam Special 1:100 000 Geological Sheet). The lower boundary is not exposed; at the W end of seismic traverse 3 (Adam Special 1:100 000 Geological Sheet) it is placed at a prominent reflector at a depth of about 1400 m.|16-MAY-23
26242|Yardida Tillite|Age reasons|This is the lower of the two late Proterozoic tillites of central Australia (Preiss and others, 1978). It is Adelaidean.|16-MAY-23
26242|Yardida Tillite|State(s)|NT|16-MAY-23
24594|Yarman Formation|Name source|Parish of Yarman, County of Lang, Queensland.|16-MAY-23
24594|Yarman Formation|Unit history|Previously mapped as part of the "Etheridge Formation" or the Langdon River Formation of White (1959, 1962, 1965). The "Etheridge Formation", now redefined as a Group containing Robertson River, Townley, Heliman, Candlow (and other) formations and the Langdon River siltstone, unconformably underlies the Yarman Formation and Malacura Sandstone.|16-MAY-23
24594|Yarman Formation|Geomorphic expression|Surface expression: Steep but rounded hills, generally with scattered protruding sandstone beds; red-brown tone on airphotographs; sparse, stunted vegetation cover.|16-MAY-23
24594|Yarman Formation|Type section locality|Unnamed tributary of the upper Langdon River, southeast of Snake Creek, between GR 7460-06622345 and -05622198.|16-MAY-23
24594|Yarman Formation|Description at type locality|About 1800 m of shale, siltstone and minor sandstone as described below  (under Lithology) are exposed.|16-MAY-23
24594|Yarman Formation|Extent|Exposed along an unnamed taributary of the upper Langdon River from GR 7460-102168 to -068139, in a crudely triangular area in the upper Langdon River drainage with "corners" at GR 7460-056237, -077227, and -167189, and in a small area near the Langdon River centred on GR 7461-075542 (Esmeralda and Gilbert River 1:100 000 Sheet areas).|16-MAY-23
24594|Yarman Formation|Thickness range|At least 1800 m; top is not exposed.|16-MAY-23
24594|Yarman Formation|Lithology|Dark grey, weathering to marooon or red-brown, laminated, thin bedded, or massive shale with lesser amounts of finely interbedded fine to medium-grained siltstone; 1 cm to 1 m-thick beds of fine to medium-grained, commonly cross-bedded micaceous sublithic sandstone, making up about 5 to 10 percent of the total thickness, are distributed throughout the unit.|16-MAY-23
24594|Yarman Formation|Relationships and boundaries|Conformably overlies Malacura Sandstone, where predominant sandstones are succeeded by predominant maroon or red-brown-weathering shale and siltstone. Unconformably overlain by or faulted against Croydon Volcanics and unconformably overlain by Mesozoic sandstone; top is not exposed. Intruded by Esmeralda Granite.|16-MAY-23
24594|Yarman Formation|Age reasons|Early upper Proterozoic. Rocks underlying the Yarman Formation and Malacura Sandstone have been affected by deformation and metamorphism, dated at 1570 +/- 30 m.y. (Black et al., in press), which do not affect these Formations. The Yarman Formation is unconformably overlain by the Croydon Volcanics, dated at 1429 +/- 75 m.y. (Oversby et al., 1976).|16-MAY-23
24594|Yarman Formation|Proposed publication|Queensland Government Mining Journal.|16-MAY-23
24594|Yarman Formation|References|80/20677; 79/03304; 98/29026; B071.|16-MAY-23
26245|Yataga Granodiorite|Name source|Parish of Yataga, County of Einasleigh (Queensland Lands Dept. 4-Mile New Series, 4M.30).|16-MAY-23
26245|Yataga Granodiorite|Unit history|Bain, et al. (1975) referred to the intrusion as the "Dambo Complex". However, as Dambo is the name of a mineral lease within the outcrop area and not a proper geographical name, and as the relationships within the stock are not particularly complex, the name is dropped in preference to Yataga Granodiorite.|16-MAY-23
26245|Yataga Granodiorite|Type section locality|The Ironhurst-Dagworth track between GR 706071 (Georgetown 1:100 000 Sheet area) and GR 77470100 (Red River 1:250 000 Sheet area). Rocks exposed in this area are mainly grey, medium even-grained hornblende-biotite granodiorite with some pink hornblende-biotite granite, both intruded by minor fine even-grained biotite granite.|16-MAY-23
26245|Yataga Granodiorite|Extent|A circular stock, 9 km in diameter, about 30 km north-northeast of Georgetown.|16-MAY-23
26245|Yataga Granodiorite|Lithology|Mainly grey hornblende-biotite granodiorite and tonalite; subsidiary finer grained grey to pink biotite granite. The last probably intrudes the granodiorite in the central part of the stock. Veins and small dykes of pink aplite cut the granodiorite and granite locally.|16-MAY-23
26245|Yataga Granodiorite|Relationships and boundaries|Intrudes, and has strongly hornfelsed, the Proterozoic Robertson River Metamorphics and Mistletoe Granite.|16-MAY-23
26245|Yataga Granodiorite|Age reasons|Late Palaeozoic (Permian or Carboniferous) intrusive rocks of Permian and Carboniferous age with similar mineralogy are common in northeastern Queensland, e.g. Hammonds Creek Granodiorite, Bakerville Granodiorite, Kalunga Granodiorite, Almaden Granite, and various phases of the Herbert River Granite (Sheraton & Labonne, in press). A K/Ar date on a sample of biotite from the Yataga Granodiorite gave an age of 262 million years.|16-MAY-23
26245|Yataga Granodiorite|References|B169; +|16-MAY-23
20928|Yeldham Granite|Name source|Parish of Yeldham between latitudes 18o33'S and 18o48'S and longitudes 138o05'E and 139o05'E in the Lawn Hill and Gregory Downs 1:100 000 Sheet areas.|16-MAY-23
20928|Yeldham Granite|Unit history|The Yeldham Granite has been previously referred to as the Weberra Granite by Carter, Brooks & Walker (1961), and Cavaney (1975). The Weberra Granite is defined in the Alhambra area in the Mount Oxide 1:100 000 Sheet area, which is 60 km to the southeast of the Yeldham Granite. These granite masses are of different chemistry and petrology (Wyborn, pers. comm.) and have no common contact.|16-MAY-23
20928|Yeldham Granite|Geomorphic expression|The granite crops out as low relief platforms and broad hills with rarely more than 50 metres relief.|16-MAY-23
20928|Yeldham Granite|Type section locality|The type locality of the Yeldham Granite is nominated to lie approximately 100 metres to the southeast of the road connecting Rankins Yard to Gregory Downs approximately 18 km due south of the Lawn Hills to Gregory Downs road (GR LH 773230). It is situated 21 km southwest of Yeldham Station.|16-MAY-23
20928|Yeldham Granite|Extent|The Yeldham Granite crops out as several bodies in the faulted core of a large dome in the eastern part of the Lawn Hill 1:100 000 Sheet area. The largest of these bodies crops out over 8 km2 in the core of the Kamarga Dome. The dome is cut by a prominent faulting causing displacement of the granite.|16-MAY-23
20928|Yeldham Granite|Lithology|The rock is an equigranular, medium-grained, pink-grey, muscovite granite. Grain size varies between 1 mm and 6 mm but averages 1-2 mm. Adjacent to the margin of the pluton, some hornblende is present. Other lithologies within the pluton are coarse-grained pegmatite, greisen and large graphitic quartz-hematite xenoliths.|16-MAY-23
20928|Yeldham Granite|Relationships and boundaries|The pluton intrudes the Kamarga Volcanics and is nonconformably overlain by the McNamara Group.|16-MAY-23
20928|Yeldham Granite|Age reasons|The age of the Yeldham Granite is unknown. It is overlain nonconformably by equivalents of the Mount Isa Group which has been isotopically dated at between 1650 m.y. and 1670 m.y. (Page, 1979).|16-MAY-23
20928|Yeldham Granite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
20928|Yeldham Granite|References|B051|16-MAY-23
20928|Yeldham Granite|Proposer|Hutton L.J., Sweet I.P.|16-MAY-23
24599|Yellow Waterhole Granite|Name source|Named after Yellow Waterhole, GR 558865, 3 km to S of the granite outcrop area, Selwyn 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24599|Yellow Waterhole Granite|Unit history|Like all other granites in the eastern part of the Duchess 1:250 000 Sheet area, the Yellow Waterhole Granite was mapped as Williams Granite by Carter & Opik (1963).|16-MAY-23
24599|Yellow Waterhole Granite|Type section locality|Tors and spheroidal boulders of pink, non-foliated, weakly porphyritic, medium to coarse biotite granite at GR 533910, close to the Selwyn/Hamilton River road 29 km SSE of Selwyn.|16-MAY-23
24599|Yellow Waterhole Granite|Extent|The unit crops out as elongate body 19 km long and up to 2.5 km wide trending E in SW Selwyn and SE Mount Merlin 1:100 000 Sheet areas, Duchess 1:250 000 Sheet area.|16-MAY-23
24599|Yellow Waterhole Granite|Lithology|The unit consists of massive (non-foliated), even-grained to porphyritic, fine to coarse biotite granite and hornblende-biotite granite, and minor aplite.|16-MAY-23
24599|Yellow Waterhole Granite|Relationships and boundaries|The granite intrudes Kuridala Formation and is overlain by flat-lying Mesozoic sediments.|16-MAY-23
24599|Yellow Waterhole Granite|Age reasons|Proterozoic|16-MAY-23
24599|Yellow Waterhole Granite|Comments|Remarks: Yellow Waterhole Granite forms a well-defined intrusive body strongly oblique to northerly trends of adjacent country rocks. It is probably closely related to the petrographically similar Squirrel Hills Granite (new name) to the east, and belongs to the Williams Batholith (new structural term).|16-MAY-23
24599|Yellow Waterhole Granite|References|98/29253|16-MAY-23
24599|Yellow Waterhole Granite|Defn Reference|82/22920|16-MAY-23
