Stratno | Stratigraphic Name | Category | Contents | Last update 
2003|Blue Rock Creek Beds|Name source|Blue Rock Creek, a tributary of Anthill Creek; south of Walter's Plains Lake, Einasleigh 1:250 000 sheet area.|16-MAY-23
2003|Blue Rock Creek Beds|Type section locality|In a segment of an unnamed tributary running south-southeast into Blue Rock Creek, the segment being from 1.5 to 1.0 km upstream from this junction; latitude 18o25.4', longitude 145o12'.|16-MAY-23
2003|Blue Rock Creek Beds|Extent|The unit is exposed as a strip, 3 km long and 0.5 km wide, 13 km west of Wairuna Homestead.|16-MAY-23
2003|Blue Rock Creek Beds|Thickness range|Structural complexity has precluded an estimate of thickness.|16-MAY-23
2003|Blue Rock Creek Beds|Lithology|Micaceous and arkosic sandstone, grey and red shale and siltstones, minor conglomerate and some calcareous interbeds; massive, strongly jointed, coarsely recrystallised, somewhat silty limestone in which some interbeds of calcirudite and calcareous shale have been recognised.|16-MAY-23
2003|Blue Rock Creek Beds|Relationships and boundaries|In broad aspect, the unit comprises a long discontinuous ridge of limestone surrounded by poorly outcropping sandstone, siltstone and shale; these sediments are preserved as a folded strip, faulted to the east and surrounded by amphibolite and schist. A nonconformity at which a thin basal conglomerate overlies metamorphics is exposed at the western margin of the unit in the unnamed tributary of Blue Rock Creek.|16-MAY-23
2003|Blue Rock Creek Beds|Age reasons|Poorly preserved tabulate and rugose corals, brachiopod shells and crinoidal debris occur in restricted localities. The corals are dominantly compound, massive types and are evidently the remnants of a richer assemblage, much of which did not survive recrystallisation. Collections were made from two separate localities; their faunas are very similar and are here listed together as: Pseudoplasmopora, Favosites, Hattonia?, Dictyofavosites?, an indeterminate ptenophyllid comparable with Acanthophyllum, and an indeterminate crystiphyllid. Drs Hill and Jell (pers. comm.) regard the likely age of the assemblage to be early Devonian or possibly late Silurian.|16-MAY-23
25800|Booloumba Beds|Name source|Booloumba Creek, which flows from GR 619 459 to GR 675 552, Nambour 1:100 000 sheet area (from 152o37.1'E, 26o42.5'S to 152o40.4'E, 26o37.4'S).|16-MAY-23
25800|Booloumba Beds|Type section locality|Along the full length of Booloumba Creek upstream from its junction with Lobster Creek (GR 650 527, Nambour 1:100 000 sheet area; 152o38.9'E, 26o38.8'S).|16-MAY-23
25800|Booloumba Beds|Extent|The unit covers an area of 200 km2 drained by Summer, Peter, Booloumba, Bunderoo and Lobster Creeks southwest of Kenilworth. Its north-eastern boundary is a line from the junction of Summer and Little Yabba Creeks southeast to the junction of Booloumba and Lobster Creeks, and the Booloumba Beds extend about 15 km to the southwest to the headwaters of Peters Creek. Similar rock types extend continuously further to the southwest as far as the Kilcoy-Goomeri road, and south to the Kilcoy area. It is probable that these rocks can be assigned to the Booloumba Beds. The unit also appears to continue along strike to the northwest.|16-MAY-23
25800|Booloumba Beds|Thickness range|Unknown|16-MAY-23
25800|Booloumba Beds|Lithology|Slate, phyllite, foliated to massive greenstone, small lenses of jasper and chert, and rare thin bands of fine-grained arenite or siltstone. Manganese mineralisation is associated with some jasper and chert lenses. Greenstone forms lenses and bands up to 1 km thick throughout the sequence. All rocks have been metamorphosed to the greenschist facies.|16-MAY-23
25800|Booloumba Beds|Relationships and boundaries|The  Booloumba Beds appear to be conformable with the Amamoor Beds to the northeast, and are assumed to underlie the latter unit, although there is no direct evidence of facing in either unit. The northeastern boundary of the Booloumba Beds is placed along the southwest margin of a thick belt of massive basic volcanics within the Amamoor Beds.|16-MAY-23
25800|Booloumba Beds|Structure and Metamorphism|Dominant structure is a strong northwest trending foliation or slaty cleavage which locally has transposed bedding.|16-MAY-23
25800|Booloumba Beds|Age reasons|Since the Amamoor Beds contain Early Permian fossils, the depositional age of the Booloumba Beds is considered to be Carboniferous to Early Permian. Isotopic age determinations from the Kilkivan area suggest that the unit was metamorphosed in earliest Permian time.|16-MAY-23
25800|Booloumba Beds|Correlations|Before intrusion of the Triassic Neurum Tonalite, the Booloumba Beds appear to have been continuous along strike with the Rocksberg Greenstone and Kurwongbah Beds. The Booloumba Beds are lithological correlatives of the Kurwongbah Beds, which are similar in lithology, structure and metamorphic grade. Since the Kurwongbah Beds interfinger with the Rocksberg Greenstone, the Booloumba Beds may be time equivalents of at least part of both the Kurwongbah Beds and Rocksberg Greenstone. The Durundur Shales of Mathews (1955) are roof pendants in the Neurum Tonalite equivalent to the metamorphosed pelitic sediments of the Booloumba Beds and Kurwongbah Beds. Murphy et al. (1976) divided the Booloumba Beds into the Bunya Phyllite (in the sense of the Kurwongbah Beds) and undifferentiated Palaeozoic rocks. However, no significant lithological or structural differences can be discerned between these units, and the distinction is considered to be invalid. Burns (1961) and Hill and Tweedale (1955) regarded the Booloumba Beds as equivalents of the Neranleigh-Fernvale Beds. However, the two units are lithologically different, and the Booloumba Beds are probably younger than the Neranleigh-Fernvale Beds.|16-MAY-23
25800|Booloumba Beds|Defn approved by|Queensland Sub-Committee, Ward, W.T.|16-MAY-23
25800|Booloumba Beds|Reserved? Yes/No|Yes|16-MAY-23
2444|Bowthorn Siltstone Member|Name source|From Bowthorn homestead, at grid reference 143 966, in the Bowthorn 1:100 000 sheet area, Queensland (sheet 6561).|16-MAY-23
2444|Bowthorn Siltstone Member|Type section locality|Along a low ridge 1.5 km south of the access road to Bowthorn homestead, in the Bowthorn sheet area. The base is at grid reference 208 945, and the section runs west-southwest for 350 m, to the top of a low ridge, at grid reference 205 943.|16-MAY-23
2444|Bowthorn Siltstone Member|Extent|The unit forms an arcuate band up to 1 km wide, and crops out over about 50 km2 in the northwestern quarter of the Bowthorn 1:100 000 sheet area; minor outcrops occur to the north in the southwestern corner of the Hedleys Creek 1:100 000 sheet area (sheet 6562), and to the west, in the northeastern corner of the Cleanskin 1:100 000 sheet area (sheet 6461, Northern Territory).|16-MAY-23
2444|Bowthorn Siltstone Member|Thickness range|50 m at the type section; about 100 m in the Cleanskin and Hedleys Creek sheet areas.|16-MAY-23
2444|Bowthorn Siltstone Member|Lithology|Laminated purple and brown micaceous siltstone; a few thin interbeds of quartz sandstone. The type section is all siltstone; the sandstone interbeds occur farther north and west.|16-MAY-23
2444|Bowthorn Siltstone Member|Relationships and boundaries|A conformable member within the Constance Sandstone. The member conformably overlies cross-bedded medium-grained quartz sandstone, and is in turn overlain by similar sandstone. It is probably a lenticular siltstone body extending for no more than 50 km across the Bowthorn and adjacent 1:100 000 sheet areas. Although its contacts with the enclosing sandstone are sharp, there is no evidence of unconformity. The member, along with two previously-named members, forms prominent markers in an otherwise uniform sandstone sequence.|16-MAY-23
2444|Bowthorn Siltstone Member|Age reasons|The Bowthorn Siltstone Member and the remainder of the South Nicholson Group are designated "Carpentarian or Adelaidean". They unconformably overlie rocks which in turn overlie the Cliffdale Volcanics which have been dated at 1770+/-20 m.y. (A.W. Webb, AMDEL Rep., AN1814/73, unpubl.). The South Nicholson Group is correlated with the Roper Group in the McArthur Basin, from which glauconites have yielded ages from 1270-1390 m.y. (Plumb & Derrick, 1975). 1390 m.y. is regarded as a minimum age of deposition of the group. Because Dunn, Plumb & Roberts (1966) placed the Carpentarian/Adelaidean boundary at about 1400 m.y., the Roper Group and its correlatives are regarded as "Carpentarian or Adelaidean" in age.|16-MAY-23
2444|Bowthorn Siltstone Member|Defn author|Ian Sweet, May 1977?|16-MAY-23
2444|Bowthorn Siltstone Member|Proposed publication|BMR Report on geology of Hedleys Creek 1:100 000 sheet, Queensland.|16-MAY-23
2444|Bowthorn Siltstone Member|References|99/30042; 79/03449|16-MAY-23
37736|Burangoo Sandstone Member|Name source|From Burangoo, or Connolly, Waterhole, in the Nicholson River, centred on latitude 17deg53'S, longitude 138deg15'E, in WESTMORELAND.|16-MAY-23
37736|Burangoo 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 sc2 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.|16-MAY-23
37736|Burangoo Sandstone Member|Geomorphic expression|In areas of low dip forms extensive rocky plateaux, commonly with pseudokarstic weathering surfaces; in rarer steeply dipping outcrops forms sharp rocky ridges.|16-MAY-23
37736|Burangoo Sandstone Member|Type section locality|Along the northern side of the Nicholson River, from 209700E 8021700N (base), in a west to west-southwest direction to 207300E 8019000N (top), in WESTMORELAND. The type section is accessible from a Bowthorn Station and tourist track to Burangoo Waterhole.|16-MAY-23
37736|Burangoo Sandstone Member|Extent|Crops out north of Elizabeth Creek in northern Lawn Hill, and south of Hedleys Creek, in the southwestern Westmoreland 1:250 000 sheet area, and in adjacent parts of southeastern Calvert Hills and northeast and central Mount Drummond 1:250 000 sheet areas.|16-MAY-23
37736|Burangoo Sandstone Member|Thickness range|Estimated at 320 m in the type section, based on a dip of 5deg. Ranges from 130 m to 300 m thick in MOUNT DRUMMOND.|16-MAY-23
37736|Burangoo Sandstone Member|Lithology|Fine- to coarse-grained, lithic, sublithic and quartzose sandstone, with scattered grains and layers of quartz granules and pebbles up to 1 cm diameter; strongly trough cross-bedded in many outcrops; also planar cross-beds, planar bedding and hummocky cross-stratification.|16-MAY-23
37736|Burangoo Sandstone Member|Depositional environment|Mainly shallow marine, intertidal to upper shoreface; possibly minor braided fluvial.|16-MAY-23
37736|Burangoo Sandstone Member|Relationships and boundaries|The lower boundary, with the Pandanus Siltstone Member, is sharp but apparently conformable, and the upper contact, with the Wallis Siltstone Member, is similarly conformable. In northern MOUNT DRUMMOND the Schultz Sandstone Member truncates the Wallis Siltstone Member to lie disconformably on the Burangoo Sandstone Member.|16-MAY-23
37736|Burangoo 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 Burangoo Sandstone Member is judged to lie near the middle of this age range.|16-MAY-23
37736|Burangoo 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
37736|Burangoo Sandstone Member|Defn author|Ian Sweet, May 2006.|16-MAY-23
37736|Burangoo 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
37736|Burangoo Sandstone Member|Parent|A member of the Constance Sandstone, Accident Subgroup, South Nicholson Group.|16-MAY-23
4089|Claraville Beds|Name source|Claraville homestead, grid reference 553978 m (482658Y), Croydon 1:250 000 Sheet area, SE54-11.|16-MAY-23
4089|Claraville Beds|Unit history|The authors and others had originally included the sediments of the unit in the Wyaaba Beds.|16-MAY-23
4089|Claraville Beds|Type section locality|Reference Section: The top 39 m of BMR Croydon No. 1 shallow stratigraphic hole; position approximately latitude 18o18'S, longitude 141o30'E (Fig.   ).  (cf Needham et al., 1971).|16-MAY-23
4089|Claraville Beds|Extent|The unit underlies the Claraville Plain, which is generally southwest of Croydon, and between the Caron and Norman Rivers, Cooradine Creek and the Gregory Range. The unit may extend as far south as the Flinders River (Fig.  ).|16-MAY-23
4089|Claraville Beds|Thickness range|Maximum known thickness is 50 m in BMR Normanton 2. The unit could thicken westwards, and thins to nothing eastwards and southwards (Fig.   ).|16-MAY-23
4089|Claraville Beds|Lithology|In BMR Croydon No. 1, the unit consists of soft clayey sandstone and soft sandy mudstone, grey to white, poorly sorted and poorly consolidated. The sand is quartzose. The unit is sandier in BMR Normanton Nos 1 & 2*. It contains fragments of lateritic material.   *cf Needham et al., op.cit.|16-MAY-23
4089|Claraville Beds|Relationships and boundaries|The unit overlies unconformably early Cretaceous units of the Carpentaria Basin (Allaru Mudstone, Toolebuc, Wallumbilla and Gilbert River Formations - Smart et al., 1971). It interfingers to the north with the deposits of the Gilbert Fan; these are not included in the Claraville Beds because the Fan members and their lithologies are not well enough known yet in vertical section. The unit interfingers to the west with the more clayey Wondoola Beds. To the east it abuts residual sand on Precambrian granite and Early Cretaceous sandstone - the Croydon and Strathpark Plains respectively, remnants of the Pliocene Strathgordon Surface (Doutch et al., op. cit.; Grimes & Doutch, op. cit.). The unit possibly overlies the Strathgordon Surface. The boundary in the south between the unit and residual sand needs further investigation. The unit is overlain by flood plains, floodout and overflow deposits of present-day rivers.|16-MAY-23
4089|Claraville Beds|Age reasons|Plio-Pleistocene. The unit contains no fossils or other material which can be dated at the moment. It interfingers with the adjacent Wondoola Beds, which are probably older than beach ridges dated as 5630 yrs old (Smart, in prep.). The Wondoola Beds are apparently equivalent to the Armraynald Beds in the Leichhardt River area to the west (Doutch et al., 1970); in the base of the Armraynald Beds is a fauna consisting of Pleistocene crocodilians and Nototherium ep., (Bartholomai, pers. comm.). However, the Claraville Beds may contain equivalents of Pliocene Wyaaba Beds (Grimes & Doutch, in prep.), which in the Gilbert-Mitchell Trough are separated from the fan deposits above them by the Strathgordon Surface or its remnants.|16-MAY-23
27286|Dead Horse Metabasalt Member|Name source|Dead Horse Creek which flows into the Gilbert River at GR 588 834 (Bellfield 1:100 000 Sheet area).|16-MAY-23
27286|Dead Horse Metabasalt Member|Unit history|The rocks were previously considered to be intrusive dolerite and gabbro and were assigned to the Cobbold Dolerite (White, 1959; 1962a,b).|16-MAY-23
27286|Dead Horse Metabasalt Member|Type section locality|About 750m exposed along an unnamed tributary of the Percy River between GR 632 823 (bottom) and 633 813 (top). The track between Iona homestead and Agate Creek is parallel to the section and a few hundred metres west of it. Most of the section consist of fine-grained, green, massive metabasalt, but the upper 200m (approx.) contain well-preserved pillows, hyalocrastic breccias and amygdales. Beds of grey/green phyllitic shale and siltstone up to 10m thick occur in several parts of the section. Some coarser-grained basic rocks may be metadolerite sills or dykes.|16-MAY-23
27286|Dead Horse Metabasalt Member|Extent|The unit is exposed in the northwestern quarter of the Gilberton 1:100 000 Sheet area where it has a total area of approximately 80km ^2. Similar rocks crop out over about 150km^2 in the North head 1:100 000 Sheet area in a belt extending east from near South Head homestead to the Roberston River; these rocks occupy a similar stratigraphic position in the Robertson River Formation to those in the Gilberton Sheet area, and are equated with them.|16-MAY-23
27286|Dead Horse Metabasalt Member|Thickness range|300 to 1000m thick.|16-MAY-23
27286|Dead Horse Metabasalt Member|Lithology|Metabasalt with minor interbedded siltstone and shale. Mostly metamorphosed in the greenschist facies and locally has developed a weak schistosity. Some higher-grade (amphibolite facies (metabasites in the Robertson River Formation may be equivalents of the Dead Horse Metabasalt Member, but at present they are all mapped as unassigned amphibolite. The metabasalt is mostly massive but pillow, amygdales and hyaloclastic breccias are relatively common.|16-MAY-23
27286|Dead Horse Metabasalt Member|Relationships and boundaries|A member within the lower part of the Robertson River Formation.|16-MAY-23
27286|Dead Horse Metabasalt Member|Age reasons|Proterozoic; older than 1570 Ma which is the age of the first deformation and metamorphic event to affect the Etheridge Group (Black & others, 1978).|16-MAY-23
27286|Dead Horse Metabasalt Member|Defn author|Withnall, I.W. ?1979.|16-MAY-23
27286|Dead Horse Metabasalt Member|References|Black, L.P., Bell, T.H., Rubenach, M.J., and Withnall, I.W., 1978: Geochronology of discrete structural-metamorphic events in a multiply-deformed Precambrian terrain. Tectonophysics.  **White, D.A., 1959: New stratigraphic units in north Queensland geology. Qld Govt Min J., 60, 442-447.  **White, D.A., 1962a: Gilberton - 1:250 000 Geological Series, Austr. Bur. Miner. Resour. Explan. Notes, E54-16.  **White, D.A., 1962b: Georgetown-1:250 000 Geological Series, Aust. Bur. Miner. Resour. Explan. Notes, E54-12.|16-MAY-23
27675|Dip Creek Limestone|Name source|Dip Creek which joins Gray (or Shield) Creek at 7859-658650.  The grid reference is based on the AGD66 datum.|16-MAY-23
27675|Dip Creek Limestone|Unit history|The limestone was referred to as 'C' lens by White (1965), and was defined as a member of the Broken River Formation (now Group) by Jell (1968).  It was raised to formation status by Withnall & others (1988), but was not redefined.|16-MAY-23
27675|Dip Creek Limestone|Geomorphic expression|Slightly elevated topography with low scattered limestone bluffs and ridges with well-developed karst features including caves (Withnall & others, 1988).|16-MAY-23
27675|Dip Creek Limestone|Type section locality|In Dip Creek between 7859-676648 (base) and 674653 (top) as designated by Jell (1968).  About 245 m of mainly bioclastic limestone crops out.  The grid references are based on the AGD66 datum.|16-MAY-23
27675|Dip Creek Limestone|Description at type locality|About 245 m of mainly bioclastic limestone crops out.REFERENCE SECTION::  Law (1985) studied a composite section to the southwest of the type section, and it is here designated as a reference section.  The section is from the base of the unit at 7859-680638 to 678627 (300 m), then 646606 in Atherton Creek to 648604 (350 m), and then 663613 to the top of the unit at 661614 (110 m).  The total thickness of the section is 760 m.  The unit consists mainly of bioclastic calcarenite, calcirudite, and lesser calcilutite (grainstone, packstone, and wackestone, with lesser mudstone).  Sandy and silty siliciclastic rocks are common in several intervals through the section.  See Withnall & others (1988, particularly figure 28) for more details.|16-MAY-23
27675|Dip Creek Limestone|Extent|A folded belt of rocks extending 20 km from the headwaters of Shield Creek to Turtle Creek in the east.|16-MAY-23
27675|Dip Creek Limestone|Thickness range|The total thickness of the reference section is 760 m.|16-MAY-23
27675|Dip Creek Limestone|Lithology|Bioclastic limestone as in the reference section; sandy and silty siliciclastic rocks usually less well developed elsewhere.|16-MAY-23
27675|Dip Creek Limestone|Fossils|The limestone contains a rich fauna of corals, and stromatoporoids, and less common brachiopods, bryozoans, gastropods, bivalves, ostracods, and conodonts.  It contains the lower two rugose coral faunas (Phillipsastrea and Sanidophyllum) recognised in the Chinaman Creek Limestone by Jell (in Wyatt & Jell, 1967).|16-MAY-23
27675|Dip Creek Limestone|Relationships and boundaries|The unit is part of the Wando Vale Subgroup of the Broken River Group.  It conformably overlies a thin quartzose sandstone unit equated with the Tank Creek Sandstone.  The sandstone is probably absent in places and the Dip Creek Limestone lies disconformably on the Shield Creek Formation.  On the southern limb of the Atherton Anticlinorium  the Dip Creek Limestone is conformably overlain by a thin mudstone interval equated with the Papilio Mudstone.  Neither the Tank Creek Sandstone nor Papilio Mudstone is thick enough to map out at 1:100 000 scale in this area.  On the northern limb of the anticlinorium and in the Dip Creek Syncline, the Dip Creek Limestone is unconformably overlain by the Bulgeri Formation and in places by the Turrets Formation.  Its southern and northern limits are faults.  It is faulted against the Mytton Formation along the Lockup Well Fault, and against the Bulgeri Formation along the Shield Creek Fault.  Originally it may have been continuous with both the Chinaman Creek and Lockup Well Limestones.|16-MAY-23
27675|Dip Creek Limestone|Age reasons|The age is middle Emsian to early Givetian.|16-MAY-23
27675|Dip 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.LAW, S.R., 1985:  Sedimentology of the Dip Creek Limestone 	Member, Broken River Formation, north Queensland.  B. Sc. (Hons) Thesis, University of Queensland (unpublished);  also issued as Geological Survey of Queensland Record 1986/18 (unpublished).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
25880|Dismal Creek Volcanics|Name source|Dismal Creek, on Forest Home 1:100 000 Sheet area, GR 7561-360910; the volcanics crop out in the headwaters of this creek.|16-MAY-23
25880|Dismal Creek Volcanics|Unit history|Mapped as part of the Galloway Volcanics by Branch (1966). The Dismal Creek Volcanics sequence is different in many respects to that of the Maureen Volcanics (and the Galloway Volcanics), in that sediments are much more abundant, and the predominant volcanic rocks are rhyodacitic or dacitic rather than rhyolitic. In addition, the Dismal Creek Volcanics appear to occupy a separate basinal structure.|16-MAY-23
25880|Dismal Creek Volcanics|Geomorphic expression|Forms low rounded hills which are generally rocky and have a very sparse vegetation cover dominated by "quinine bush"; has a very pale tone on airphotographs. Basal sediments produce very subdued topography with better vegetation cover; upper main body of sediments forms steep-sided, moderatley dissected strike ridges.|16-MAY-23
25880|Dismal Creek Volcanics|Type section locality|Along a bulldozed track, beside which several costeans have been dug, between GR 7561-422855 and -4008475, and thence west to -3978475.      The base of the type section is marked by fine to coarse sublithic and micaceous sublithic sandstones, with siltstone and minor rhyolite. These rocks elsewhere overlie poorly exposed quartzose sandstone and arkose which probably extend into the type section. The section then passes upwards into polymict dacitic agglomerate, a thick, folded sequence of sublithic sandstones and siltstones, and finally a thick, massive dacitic ignimbrite unit. A few hundred metres south of the track, fine-grained andesite partly underlies and partly interfingers with the thick sedimentary sequence. Possibly up to 1500 m exposed in this section.|16-MAY-23
25880|Dismal Creek Volcanics|Extent|Exposed over a "kidney-shaped" area with ends of logn axis at GR 7561-368895 and -415833, and ends of short axis at GR 7561-367843 and -400877; also exposed in a 500 m-wide area between GR 7561-421902 and -427885.|16-MAY-23
25880|Dismal Creek Volcanics|Thickness range|Highly variable: generally about 400 to 800 m thick; possibly up to 1500 m in the type section where repetition by folding and faulting makes estimation difficult.|16-MAY-23
25880|Dismal Creek Volcanics|Lithology|Dacitic (or rhyodacitic) ignimbrite, a wide variety of lithic-quartz sandstones and siltstones with or without feldspar and/or mica, quartzose sandstones and cobble, boulder, and pebble conglomerates; pebbly sandstone, arkose, tuffaceous sandstone, tuff, lithic siltstone, shale/mudstone; basic andesite; rhyolite; polymict dactic(?) agglomerate or breccia; rhyolite autobreccia, commonly altered; variety of polymict breccias, generally intensely sericitised.|16-MAY-23
25880|Dismal Creek Volcanics|Relationships and boundaries|Rests with marked angular unconformity on schist, quartzite, and metadolerite of the mid-Proterozoic Robertson River Formation and associated granitic rocks. Unconformably overlain by outliers of Yappar Member (of the Gilbert River Formation) and Bulimba Formation, both dominantly flat-lying quartzose sandstone. Intruded by Mount Darcy Microgranodiorite.|16-MAY-23
25880|Dismal Creek Volcanics|Age reasons|Mid-Carboniferous. Like the Maureen Volcanics,  the Dismal Creek Volcanics are similar in most respects to the 318+/- m.y. old (Black, 1973) Newcastle Range Volcanics in the northern Newcastle Range.|16-MAY-23
25880|Dismal Creek Volcanics|Proposed publication|Queensland Government Mining Journal|16-MAY-23
25880|Dismal Creek Volcanics|Defn Reference|79/20194|16-MAY-23
24246|Doherty Formation|Name source|Doherty Waterhole, situated on the Florence River at GR 603531, Mount Angelay 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24246|Doherty Formation|Unit history|The Doherty Formation was previously mapped as part of the Corella Formation (Carter & others, 1961; Carter & Opik, 1963). However, it is geographically separated from the belt of Corella Formation containing the type section (in the Marraba 1;100 000 Sheet area), it is in contact with units which cannot be correlated with any confidence with those adjacent to the type section Corella Formation, and it is probably at least 40 m.y. younger than the type section Corella Format+B22ion (which is intruded by 1740 m.y. old granite).|16-MAY-23
24246|Doherty Formation|Type section locality|Along the gorge of the Maramungee River from GR 874 186, 19 km NW of Answer Downs homestead, where calc-silicate breccia of the Doherty Formation is in contact with schist of the Soldiers Cap Group, west for 2.7 km to an outcrop of unnamed granite, which intrudes the formation, at GR 851181. There are continuous exposures of the predominant rock types of the formation - banded calc-silicate granofels and calc-silicate breccia, in about equal proportions - together with some intrusive metadolerite, along this gorge section.|16-MAY-23
24246|Doherty Formation|Extent|The formation crops out in a N to NNW-trending belt up to 21 km wide extending from the eastern central part of the Selwyn 1:100 000 Sheet area (about 21o49'S, 140o56'E) northwards for over 100 km through the Mount Angelay 1:100 000 Sheet area and into the southern part of the Cloncurry 1:100 000 Sheet area, Duchess and Cloncurry 1:250 000 Sheet areas.|16-MAY-23
24246|Doherty Formation|Thickness range|Probably several thousand metres, but uncertain because of tight folding and lack of facing evidence.|16-MAY-23
24246|Doherty Formation|Lithology|The formation consists predominantly of thinly banded calc-silicate granofels and massive calc-silicate breccia which are variably calcareous, feldspathic, amphibolitic, scapolitic, and diopsidic. Minor rock types locally present include massive calc-silicate granofels, metarhyolite, metabasalt, banded quartz-tourmaline rock, mica schist, black slate, and variably calcareous feldspathic quartzite.|16-MAY-23
24246|Doherty Formation|Relationships and boundaries|Contacts between the Foherty Formation and adjacent non-intrusive Precambrian units (Soldiers Cap Group, Kuridala Formation, Staveley Formation) are generally marked by faults and breccia zones, hence the stratigraphic relationships of the formation are uncertain. The formation may overlie the Soldiers Cap Group, either conformably or disconformably, may be similar in age to the Kuridala Formation, and may be older than the Staveley Formation (e.g. Blake & others, in prep. b). It is intruded by amphibolite, metadolerite, dolerite, and by granites of the Williams Batholith (Saxby, Mount Angelay, Squirrel Hills, Cowie, and Blackeye Granites, all new names, and unnamed granite), and is overlain unconformably by flat-lying Mesozoic sediments.|16-MAY-23
24246|Doherty Formation|Age reasons|Proterozoic; in the Selwyn 1:100 000 Sheet area the formation includes metarhyolite, thought to be extrusive, which has been dated at about 1700 m.y. by the U-Pb method (R.W. Page, personal communication, 1980).|16-MAY-23
24246|Doherty Formation|Proposed publication|Blake & others, in prep. A - see References|16-MAY-23
24246|Doherty Formation|Comments|Remarks: The Doherty Formation has been regionally metamorphosed mainly to amphibolite grade, and is relatively resistant to erosion, forming hilly terrain throughout its outcrop area. It forms a mostly well-defined and mappable unit easily distinguished from adjacent stratigraphic units (though not always from irregular granitic intrusions).|16-MAY-23
24246|Doherty Formation|Defn Reference|82/22710|16-MAY-23
24246|Doherty Formation|First Reference|82/22920|16-MAY-23
24246|Doherty Formation|Proposer|Blake D.H., Donchak P.J.T.|16-MAY-23
30138|Eridge Member|Name source|The unit is named from the Parish of Eridge, County of Wilkie Gray.|16-MAY-23
30138|Eridge Member|Type section locality|The type section is from the base in unit Cte1 at 8159-162705 on the limb of the syncline to the top of unit Cte4 at 8159-187681 in the hinge.  The grid reference is based on the AGD66 datum.|16-MAY-23
30138|Eridge Member|Description at type locality|Consists, from bottom to top, of the following informal units: - about 250m of light green, crystal-poor, lithic-poor to moderately lithic-rich rhyolitic ignimbrite (Cte1);  - about 200m of dark pink to dark purple, crystal-poor, moderately lithic-rich rhyodacitic tuff and ignimbrite (Cte2); - about 100m of light green, crystal-poor, lithic-rich rhyolitic ignimbrite and minor spherulitic rhyolite (Cte3); - about 100m of mottled green and maroon, dacitic lapilli breccia (Cte4).|16-MAY-23
30138|Eridge Member|Extent|The Eridge Member lies in the centre of a broad syncline between Little Star River and Star River. The outcrop area is approximately 50km2 and roughly triangular in shape. Parts of the member have been intruded by Carboniferous to Permian granite or rhyolite.|16-MAY-23
30138|Eridge Member|Thickness range|On the western limb of the syncline between Little Star River and Star River, the Eridge Member is 1500m thick.|16-MAY-23
30138|Eridge Member|Lithology|The Eridge Member consists predominantly of lithic-rich dacitic to rhyolitic volcaniclastics. The member has been divided into four informal units (Cte1, Cte2, Cte3, Cte4) as in the type section These units have been separated largely on colour and spatial distribution:- Cte1-  is the lowest unit of the Eridge Member and consists mainly of light green to green, crystal-poor to moderately crystal-rich, moderately lithic-rich rhyolitic ignimbrite. Grey, moderately crystal-rich to crystal-rich rhyolitic ignimbrite, moderately lithic and moderately crystal-rich rhyolitic and dacitic tuff, rhyolitic lapilli breccia, spherulitic rhyolite, flow-banded rhyolite and minor fossiliferous volcaniclastic siltstone are also present.  Cte2 - consists of dark purple to purple, crystal-poor to moderately crystal-rich, moderately lithic-poor to moderately lithic-rich dacitic lapilli breccia and ignimbrite. The ignimbrites range from moderately fiamme-poor to fiamme-rich.  Unit Cte3 - is mainly light green to light grey, crystal-poor to moderately crystal-poor, moderately lithic-rich to lithic-rich rhyolitic ignimbrite and minor spherulitic rhyolite.  The uppermost unit (Cte4) - consists of dark purple, dacitic breccia, crystal-poor, lithic-rich dacitic ignimbrite and mottled green and maroon, dacitic lapilli breccia.|16-MAY-23
30138|Eridge Member|Relationships and boundaries|The Eridge Member is part of the Tareela Volcanics. Lepidodendron veltheimianum was found in the 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
6814|Forest Home Granodiorite|Name source|Forest Home Station and homestead (GR 7561-146 815), near the Gilbert River, on the western side of Forest Home 1:100 000 Sheet area.|16-MAY-23
6814|Forest Home Granodiorite|Unit history|Intruded by White (1962, 1965) as part of the Esmeralda Granite, and related to the Forsayth Granite by Sheraton and Labonne (1978); the Forest Home Granodiorite differs markedly in most respects from both. Rossiter (1978) referred to a pluton in the Black Gin Creek-Knights of Malta area as "a pluton of the Forest Home Granodiorite", based on early results of our work. Subsequent work has shown that this pluton differs in some respects from plutons of the Forest Home Granodiorite clustered together farther to the north, and it has been named separately (Carnes Granodiorite).|16-MAY-23
6814|Forest Home Granodiorite|Geomorphic expression|Relatively subdued topography, especially compared to the Langdon River Formation generally broken by very prominent bouldery outcrops and large tors. Characteristic vegetation cover of very open low forest with short "kerosene" grass, producing a very pale airphotograph tone, with boulders/tors commonly visible.|16-MAY-23
6814|Forest Home Granodiorite|Type section locality|A pluton about 6 km east-southeast of Forest Home homestead near the Gilbert River at GR 7561-200790 (approximately); abundant fresh exposure is readily accessible by track in the Stake Lagoon area (GR 7561-173662, and this is designated a representative area.|16-MAY-23
6814|Forest Home Granodiorite|Extent|Forms 15 discrete plutons (thus far recognised) and a number of smaller intrusive bodies, in the southwestern corner of Forest Home Sheet area, south of the Gilbert River (one is north) and west of 143o10'E. Centres of plutons are at GR 7561-163824, -200790, -207735, -220780, -224732, -210685, -173657, -190648, -193655, -229651, -146637, 145608, 164620 and 167620 (two very small bodies), -166580, and -149551. A dyke-like body is exposed at -204629, and a few boulders are exposed at -153839 next to the Gulf Developmental Highway.|16-MAY-23
6814|Forest Home Granodiorite|Lithology|Fine to medium-grained, less commonly coarse-grained biotite granodiorite. Weakly to moderately porphyritic in places near contacts. Some smaller bodies contain disseminated pyrite.|16-MAY-23
6814|Forest Home Granodiorite|Relationships and boundaries|Intrudes Candlow and Langdon River Formations; by far the greater exposed area of Forest Home Granodiorite occurs within the Langdon River Formation. The plutons all have contact metamorphic aureoles.|16-MAY-23
6814|Forest Home Granodiorite|Age reasons|Probably mid-Proterozoic (minimum) age; does not intrude Malacura Formation, which is overlain unconformably by rocks dated at 1429 +/-75 m.y. (Oversby et al., 1976). An age of 1265 m.y. has been obtained by Black (1973) from biotite in rock from "near Forest Home Station".|16-MAY-23
6814|Forest Home Granodiorite|Proposed publication|Queensland Government Mining Journal|16-MAY-23
6814|Forest Home Granodiorite|First Reference|80/20966|16-MAY-23
25913|Fork Lagoons Beds|Name source|Fork Lagoons' homestead, located 23o25'S, 148o56'E; GR 61630820 Emerald 1:250 000 Sheet area.|16-MAY-23
25913|Fork Lagoons Beds|Type section locality|Reference section: Along a northeast trending fence line starting from grid reference 61300840, about 4 km northwest of 'Fork Lagoons' homestead, and 0.5 to 1.5 km west of a prominent basalt ridge.|16-MAY-23
25913|Fork Lagoons Beds|Extent|The unit has been recognised over an area of 15 km2, located some 30 km west northwest of the town of Emerald.|16-MAY-23
25913|Fork Lagoons Beds|Thickness range|Undeterminable, probably no more than 500 m.|16-MAY-23
25913|Fork Lagoons Beds|Lithology|Siltstone, grey where fresh, quartz rich, indurated with milky quartz veins; limestone lenses, dark grey-fawn, fossiliferous, partly recrystallised; minor calcarenite.|16-MAY-23
25913|Fork Lagoons Beds|Relationships and boundaries|Base not exposed, top overlain unconformably by Permian Reids Dome Beds and Aldebaran Sandstone.|16-MAY-23
25913|Fork Lagoons Beds|Age reasons|Determintions on the conodont fauna (Palmieri, in prep.), and the coral and stromatoporoid fauna (Fleming pers. Comm.) indicate a Late Ordovician age. Diagnostic conodonts include: Acodus similaris Rhodes, Acodus trigonius (Schopf), Amorphognathus ordovicica Branson and Mehl, Panderodus staufferi Branson, Mehl, and Branson, Phragmodus undatus Branson and Mehl, Prioniodina furcata (Hinde), Protopanderodus insculptus (Branson and Mehl), Tetraprioniodus delicatus (Branson and Mehl), and macrofauna include: Tabulate Corals - halysitid indet (Quepora or Catenipora), Plasmopora sp, Pseudoplasmopora sp, Plasmoporella sp, Palaeofavosites sp; Rugose Corals - Palaeophyllum sp, Favistella sp; Stromatoporoids - cf Stratodictyon sp, Clathriodictyon ? sp.|16-MAY-23
25913|Fork Lagoons Beds|Defn author|Anderson J.C.,. Palmieri V., 1977|16-MAY-23
25913|Fork Lagoons Beds|Proposed publication|Queensland Government Mining Journal|16-MAY-23
25913|Fork Lagoons Beds|Comments|Notes: The unit crops out as a basement high in the crest of an anticline in Permian rocks. It is considered part of the Anakie Inlier. A small serpentinite body intrudes the Fork Lagoons Beds.|16-MAY-23
23603|Fullarton River Group|Name source|Fullarton River; Kuridala 1:100 000 geological special sheet, northeast corner.|16-MAY-23
23603|Fullarton River Group|Unit history|The Fullarton RIver Group is [was] part of previously undifferentiated Soldiers Cap Group, but is now recognised as the lowermost stratigraphic unit of the Fullarton River Group.|16-MAY-23
23603|Fullarton River Group|Constituents|The Fullarton River Group consists of  the Gandry Dam Gneiss, Glen Idol Schist and New Hope Arkose. The latter two formations are thougt ot be lateranl equivalents, and younger than the Gandry Dam Gneiss.|16-MAY-23
23603|Fullarton River Group|Type section locality| This section is composite, consisting of type sections outlined for its constituent formations.|16-MAY-23
23603|Fullarton River Group|Extent|Crops out over a total area of 1300 km2. The most extensive development occurs within the eastern Fairmile belt, with the Gandry Dam Gneiss and the Glen Idol Schist. Outcrop in the western Selwyn belt consists of  New Hope Arkose only. Gravity and image-processed aeromagnetic data also indicate these metasediments extend east and south, at depth, beneath the Eromanga Basin.|16-MAY-23
23603|Fullarton River Group|Thickness range|At least 3800m.|16-MAY-23
23603|Fullarton River Group|Lithology|Quartzofeldspathic migmatite-composite gneiss-schist, feldspathic psammite, calc-silicate schist and gneiss, garnet pelite, blue quatzite, BIF, gahnite quartzite, para- and ortho-amphibolite and pegmatite swarms.|16-MAY-23
23603|Fullarton River Group|Relationships and boundaries|The base of the Fullarton River Group is not evident from current mapping. Tectonic disruption has resulted in multiple repetition of the stratigraphic sequence. The group is overlain conformably by the Soldiers Cap Group. There is evidence for major thrusting of portions of the Soldiers Cap Group over the Fullarton River Group, and for emplacement of a tectonic sheet of Doherty Formation over the Fullarton RIver Group sediments.|16-MAY-23
23603|Fullarton River Group|Age reasons|Younger than 1865 Ma; older than 1720 Ma. Evidence cited in Beardsmore et al. (1988).|16-MAY-23
23603|Fullarton River Group|Defn author|Newbery S.P., Beardsmore, T.J.,  Laing, W.P., (1988)|16-MAY-23
23603|Fullarton River Group|Proposed publication|Newbery S.P., Beardsmore, T.J.,  Laing, W.P., in prep. The new Maronan Supergroup - some definitions, and implications for stratigraphic revision in the Cloncurry Fold Belt, northwestern Queensland. Submitted to Queensland Government mining Journal|16-MAY-23
23603|Fullarton River Group|References|Beardsmore, T.J., Newbery, S.P., 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 40/41, p487-507.|16-MAY-23
37735|Hedleys Sandstone Member|Name source|From Hedleys Creek, an east-southeast-flowing tributary of the Nicholson River, whose confluence with that river is at latitude 18deg52'30"S, longitude 137deg24'30"E, in WESTMORELAND.|16-MAY-23
37735|Hedleys Sandstone Member|Unit history|Not differentiated 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 sc1 on the second editions of LAWN HILL  - Hutton & Grimes (1983); WESTMORELAND, Grimes & Sweet (1979); 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.|16-MAY-23
37735|Hedleys Sandstone Member|Geomorphic expression|Ranges from a low narrow ridge where member is thin or steeply dipping, to broad rocky ridges and plateaux where it is thicker or gently dipping.|16-MAY-23
37735|Hedleys Sandstone Member|Type section locality|South of Wire Creek, in WESTMORELAND. The base is at 197822E 8025670N, and the top lies 1.2 km to the southeast, at 198922E 8024970N.|16-MAY-23
37735|Hedleys 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 central MOUNT DRUMMOND.|16-MAY-23
37735|Hedleys Sandstone Member|Thickness range|Around 90 m in the type section, thinning westwards. As thin as 1 m in western Seigal 1:100 000 sheet area, and 10-50 m to the south in MOUNT DRUMMOND.|16-MAY-23
37735|Hedleys Sandstone Member|Lithology|In the type section, cross-bedded, friable, medium- and coarse-grained quartz-rich sandstone with scattered granule and pebble bands. Conglomeratic lenses at the base, consisting of well-rounded pebbles and cobbles of white quartz and quartzite, and subangular to subrounded clasts of stromatolitic and oolitic chert, all set in a matrix of coarse-grained quartz sandstone (Sweet et al 1981, p 19). In MOUNT DRUMMOND it is subtly finer-grained, and lacks conglomerate interbeds.|16-MAY-23
37735|Hedleys Sandstone Member|Depositional environment|Shallow marine, mostly intertidal, and possibly minor fluvial component.|16-MAY-23
37735|Hedleys Sandstone Member|Relationships and boundaries|Unconformable on the Fickling Group in the type area - it lies disconformably on the Doomadgee Formation throughout the Hedleys Creek 1:100 000 sheet area, but to the west, in the Seigal 1:100 000 sheet area, it progressively truncates older formations in the Fickling Group westwards (Sweet et al 1981). In MOUNT DRUMMOND, it disconformably overlies the Caulfield beds in the north and Doomadgee Formation in the northeast. The upper boundary, with the Pandanus Siltstone Member, is sharp but apparently conformable. It is placed at the abrupt change from fine- or medium-grained quartz sandstone to laminated or thinly interbedded shale, siltstone and fine-grained lithic sandstone.|16-MAY-23
37735|Hedleys 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) provide the most reliable estimate for the age of the lower part of that Group, and hence for the South Nicholson Group. The age of the Hedleys Sandstone Member is judged to lie near the middle of this age range.|16-MAY-23
37735|Hedleys 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
37735|Hedleys Sandstone Member|Defn author|Ian Sweet, May 2006|16-MAY-23
37735|Hedleys Sandstone Member|Comments|The Hedleys Sandstone Member is that part of the Constance Sandstone lying beneath the Pandanus Siltstone Member, ie the basal sandstone unit within the formation. It can only be recognised where the Pandanus Siltstone Member is also present, and thus is mapped only north of the Elizabeth Creek Fault Zone.|16-MAY-23
37735|Hedleys 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
37735|Hedleys Sandstone Member|Parent|Constance Sandstone, Accident Subgroup, South Nicholson Group.|16-MAY-23
23667|Jessey Springs Limestone|Name source|The abandoned Jessie Springs yards and hut at 7859-689535.  Some confusion exists as to the correct spelling, because the name does not appear on the published topographic maps.  White (1965, page 53) gave the spelling as 'Jessie', and a Jessie Creek is shown on the Burges 1:100 000 Topographic Sheet further east.  However, Mawson & others (1985) published the name of the unit as Jessey Springs Limestone Member, so that spelling must be retained.  The grid reference is based on the AGD66 datum.|16-MAY-23
23667|Jessey Springs Limestone|Unit history|The limestone was shown as 'E' lens of the Broken River Formation by White (1965).  The name was first published as the Jessey Springs Limestone Member by Mawson & others (1985) who gave a partial measured section .  It was raised to formation status and briefly described by Withnall & others (1988), but was not formally defined.|16-MAY-23
23667|Jessey Springs Limestone|Geomorphic expression|Low relief with some low limestone bluffs with well-developed karst features, and commonly covered in vine scrub.|16-MAY-23
23667|Jessey Springs Limestone|Type section locality|In the hinge of the Wade Anticline, 2 km southeast of Jessey Springs from 7859-701529 (base) to 698526 (top).  The grid reference is based on the AGD66 datum.|16-MAY-23
23667|Jessey Springs Limestone|Description at type locality|The section is 280 m thick and consists of well-bedded bioclastic calcarenite (commonly crinoidal), and locally calcirudite.  The section was sampled by Mawson & others (1985, figure 3).|16-MAY-23
23667|Jessey Springs Limestone|Thickness range|Up to 300m.|16-MAY-23
23667|Jessey Springs Limestone|Lithology|Bioclastic calcarenite and calcirudite, and probably some mudstone.|16-MAY-23
23667|Jessey Springs Limestone|Fossils|The limestone contains corals, stromatoporoids, and conodonts.  The latter have been studied in detail (Telford, 1975; Mawson & others, 1985; Mawson, 1987; Mawson & Talent, in press)|16-MAY-23
23667|Jessey Springs Limestone|Relationships and boundaries|The unit is part of the Wando Vale Subgroup of the Broken River Group.  It interfingers with the Burges Formation which is mapped as both underlying and overlying the limestone.  Under the laterite cover to the northeast, the Jessey Springs Limestone may be continuous with the Lockup Well Limestone.|16-MAY-23
23667|Jessey Springs Limestone|Age reasons|Conodonts indicate a late Emsian to probably early Givetian age.|16-MAY-23
23667|Jessey Springs Limestone|References|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.   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
27169|Judea Beds|Name source|Judea Block of the Wando Vale Holding; Map 4M.89 of the Department of Lands, Survey Office, Brisbane.|16-MAY-23
27169|Judea Beds|Unit history|Previously the Judea Beds were mapped as part of the Wairuna Formation by White (1962). White (1959), in establishing the Wairuna Formation, specifically referred to reference sections in Gray Creek and the Broken River. It is now apparent that the Wairuna Formation of White and his co-workers comprises a heterogeneous assortment of rocks:  1. A zone of multiply deformed spilite, clastics and limestone on the western margin of the Camel Creek sub-province of late Ordovician or early Silurian age. Included in the northern part of this zone is the type area of the Wairuna Formation near Wairuna Homestead. These rocks are considered as distinct from the Judea Beds;  2. The Judea Beds area described here;  3. Zones of fossiliferous strata, which, as outlined above, overlie the unconformity in the Graveyard Creek Sub-province and are best referred to the Graveyard Creek Formation.  White et al. (1962) mapped spilite of the Judea Beds exposed adjacent to the Broken River as intrusive Devonian dolerite.|16-MAY-23
27169|Judea Beds|Type section locality|Quartz rich greywacke, slate and spilite exposed in a segment of The Broken River from 5.5 km to 8.5 km upstream from the junction of Diggers Creek. The area is 60 km south-southwest of Greenvale townsite, North Queensland. Granitic rocks are excluded. Other reference sections are nominated in Horse Creek from 0 to 1 km upstream from its junction with Gray Creek, and in Diggers Creek 6 km upstream from its junction with the Broken River.|16-MAY-23
27169|Judea Beds|Extent|The unit is exposed over some 200 km2 as a discontinuous folded strip running south-southwest of the Greenvale townsite, North Queensland.|16-MAY-23
27169|Judea Beds|Thickness range|Structural complexity has precluded an assessment of thickness for the Judea Beds.|16-MAY-23
27169|Judea Beds|Lithology|Alternating beds of greywacke and slate 2-25 cm in width dominate the sedimentary assemblage but thicker beds of fine grained greywacke, laminatead siltstone and shale also occur. Pebbly greywacke is subordinate with pebbles of quartz and chert generally less than 1 cm in diameter. Deformation has disrupted many of the primary structures of these rocks but they are flysch-like in aspect. Thicker greywacke beds are commonly graded and complete and partial Bouma sequences are not uncommon. Sole markings are abundant. Spilite associated with minor manganiferous and haematitic chert typically occurs as substantial, discrete intervals and is rarely interbedded with other sediments.|16-MAY-23
27169|Judea Beds|Relationships and boundaries|Thought to nonconformably overlie rocks of the Gray Creek Complex. Unconformably succeeded by the Graveyard Creek Formation, typically with a angular discordance.|16-MAY-23
27169|Judea Beds|Age reasons|No fossils have been found in the Judea Beds. They unconformably underlie the Graveyard Creek Formation for which fossils indicate a maximum age of late Llandoverian or Wenlockian. Their likely age is thought to be Cambrian or Ordovician.|16-MAY-23
27169|Judea Beds|Defn author|Arnold G.O., Henderson R.A., 1976|16-MAY-23
27169|Judea Beds|Proposed publication|Journal of the Geological Society of Australia|16-MAY-23
23691|Kelly St George Granite|Defn author|Halfpenny & Hegarty|16-MAY-23
23691|Kelly St George Granite|Proposed publication|Queensland Resource Industries Record 1991/6 p.19|16-MAY-23
23691|Kelly St George Granite|Name first published by|Halfpenny & Hegarty|16-MAY-23
23691|Kelly St George Granite|Reserved? Yes/No|Yes|16-MAY-23
24346|Kurbayia Migmatite|Name source|Kurbayia siding, on the Duchess-Mount Isa railway at GR 580703, Duchess 1:100 000 Sheet area, NW Queensland.|16-MAY-23
24346|Kurbayia Migmatite|Unit history|Included as part of the undivided Tewinga Group on the Duchess Region 1:100 000 map and as part of the Leichhardt Metamorphics on the Mary Kathleen 1:100 000 map.|16-MAY-23
24346|Kurbayia Migmatite|Type section locality|In Duchess 1:100 000 Sheet area: from east side of rocky ridge 2 km southeast of O'Briens Tank, at latitude 21o14'08"S, longitude 139o37'54"E, GR 586510, west-northwest for 7.5 km, to east side of ridge at GR 518540, where the unit is seen to be overlain unconformably by metasediments and metavolcanics of the Bottletree Formation. Along this line, and within 1 km to either side, the main rock types of the Kurbayia Migmatite - tightly folded, thinly banded migmatic gneiss (metasediments) and massive migmatitic gneiss (metavolcanics) - are well exposed on low ridges, undulating terrain, and rock pavements in creek beds. They are seen to be intruded by pale grey medium-grained granite, various phases of Kalkadoon Granite (dark grey tonalite, porphyritic granodiorite, even-grained granite, and leucogranite), and numerous dykes of metadolerite, and felsic porphyry of Bottletree type.|16-MAY-23
24346|Kurbayia Migmatite|Extent|Crops out in belt 80 km long and up to 10 km wide on west side of the Kalkadoon-Leichhardt Belt, Mount Isa Inlier, extending north from McPhee Creek in the Duchess 1:100 000 Sheet area to 6 km north of the Barkly Highway in the Mary Kathleen 1:100 000 Sheet area (Duchess and Cloncurry 1:250 000 Sheets), northwest Queensland.|16-MAY-23
24346|Kurbayia Migmatite|Thickness range|Not known because of structural complexities and concealed base.|16-MAY-23
24346|Kurbayia Migmatite|Lithology|Thinly banded, pale to dark grey, medium-grained, micaceous quartzofeldspathic gneiss with fine to coarse leucosomes, representing probably tuffaceous metasediments and commonly showing complex tight folding; subordinate grey, massive, fine-grained, crenulated gneiss with wispy leucosomes, representing dacitic metavolcanics; minor gneissic amphibolite veined by leucogranite.|16-MAY-23
24346|Kurbayia Migmatite|Relationships and boundaries|The Kurbayia Migmatite is overlain unconformably by the Bottletree Formation (age 1790 Ma) to the west and is faulted against felsic metavolcanics of the Leichhardt Volcanics (age 1860-1875 Ma) to the east; it is intruded by Kalkadoon Granite (age ~1860 Ma), metadolerite, and felsic dykes of Bottletree type.|16-MAY-23
24346|Kurbayia Migmatite|Age reasons|Probably early Proterozoic (pre-1900 Ma): zircon from migmatitic metadacite in the type section (at GR 585510) has been dated at 1866+/-5 Ma (Page, 1983, Precambrian Research, 21, 223-245), but this zircon may be metamorphic or related to Kalkadoon Granite, rather than being volcanic.|16-MAY-23
24346|Kurbayia Migmatite|Proposed publication|BMR Bulletin 226 'Geology of the Proterozoic Mount Isa Inlier and environs' and accompanying 1:500 000 scale geological map (Blake, in press).|16-MAY-23
24346|Kurbayia Migmatite|Comments|Remarks: Before being intruded by Kalkadoon Granite at about 1860 Ma, the protoliths of the Kurbayia Migmatite were buried, regionally metamorphosed to amphibolite facies, and partially melted to form migmatite. Hence they are significantly older than the Kalkadoon Granite and may be correlated with the Yaringa Metamorphics to the west, which are older than 1900 Ma. The Kurbayia Migmatite was regionally metamorphosed again, to upper greenschist and amphibolite facies, when the Leichhardt Volcanics, Kalkadoon Granite, and Bottletree Formation were first metamorphosed and deformed on a regional scale, 1620-1550 Ma ago.|16-MAY-23
24346|Kurbayia Migmatite|Resdate|01-MAY-1985|16-MAY-23
9941|Kurwongbah Beds|Name source|Lake Jurwongbah: GR 955855, Caboolture 1:100 000 Sheet area (9443).|16-MAY-23
9941|Kurwongbah Beds|Unit history|Denmead (1928) described these rocks as the basal part of his Bunya "Series". Bryan and Jones (1950) included them in the basal part of their Bunya "Phyllites". Mathews (1954) described these rocks as a "Transition zone" between Bunya "Phyllites" and Rocksberg "Greenstones" and Hill and Tweedale (1955) adopted this usage. Wilson and Wilson (1971), Wilson (1973), and Cranfield et al. (1976) included this unit in the Bunya Phyllite.|16-MAY-23
9941|Kurwongbah Beds|Type section locality|The type locality is defined as the channel bed from the foot of the spillway of the Sideling Creek Dam, to 200 m below the spillway, GR 953848.|16-MAY-23
9941|Kurwongbah Beds|Extent|The unit crops out over 130 km2 from Petrie 975835 in the south to the Wamuran district 864090 in the north, Caboolture 1:100 000 Sheet area. Small outcrops of rock types probably from this unit also occur at Russell Island and Arawoolum.|16-MAY-23
9941|Kurwongbah Beds|Thickness range|Unknown. The structure of the unit is complex and outcrop is poor.|16-MAY-23
9941|Kurwongbah Beds|Lithology|This unit comprises mostly grey, well-cleaved phyllite and slate; green, massive to schistose metavolcanics, minor cream coloured chert, muscovite schist and siltstone.|16-MAY-23
9941|Kurwongbah Beds|Relationships and boundaries|The western boundary of this unit is conformable and transitional with the Rocksberg Greenstone which is structurally and probably stratigraphically beneath the Kurwongbah Beds. The Kurwongbah Beds comprise mainly phyllitic metasediments, and their boundary with the Rocksberg Greenstone is placed where these rock types become dominant over the basic metavolcanics. The relationships near the transition are best seen in cuttings on the Petrie-Dayboro road 9 km and 11 km west-northwest of Petrie. The Triassic Brisbane Tuff unconformably overlies this unit as does the Triassic to Jurassic Landsborough Sandstone which is also faulted against it by the Bracalba Fault. The Kurwongbah Beds are intruded by the Triassic Neurum Tonalite. Tertiary volcanics unconformably overlie the unit near Mount Mee.|16-MAY-23
9941|Kurwongbah Beds|Age reasons|Unknown. A Palaeozoic age is assigned to the unit on stratigraphic grounds.|16-MAY-23
9941|Kurwongbah Beds|Proposed publication|Queensland Government Mining Journal|16-MAY-23
9941|Kurwongbah Beds|Defn approved by|Definition approved after amendment, by Sub-Committee for Stratigraphic Nomenclature, Queensland Division|16-MAY-23
9941|Kurwongbah Beds|Defn Reference|79/20127|16-MAY-23
9941|Kurwongbah Beds|First Reference|79/20128|16-MAY-23
26310|Lady Clayre Dolomite|Name source|The Lady Clayre Dolomite is named after Lady Clayre Creek which flows across the formation in a northeasterly direction to the south of the Knapdale Range and joins the Dugald River 1 km southwest of Mount Roseby homestead in the Quamby 1:100 000 Sheet area.|16-MAY-23
26310|Lady Clayre Dolomite|Unit history|The Lady Clayre Dolomite was included in the Corella Formation by Carter & others (1961). The name was introduced informally by Wilson & others (1979b).|16-MAY-23
26310|Lady Clayre Dolomite|Geomorphic expression|The unit is characterised by low elevation and very little relief. It forms a broad plain with minor strike ridges reaching heights of several metres.|16-MAY-23
26310|Lady Clayre Dolomite|Type section locality|The east-west type section is defined between 3 and 6 km west (and slightly south) of the Dugald River lead-zinc prospect from a point at ltitude 20o15'36"S, longitude 140o7'26"E (GR 086594) to a point about 100 m east of Cabbage Tree Creek at latitude 20o15'36"S, longitude 140o5"50"E (GR 057 594). The type section contains a sequence which is tightly folded, especially in the basal eastern part. The rock types (and estimated stratigraphic thicknesses) from east to west are: very dark grey to black fine-grained dolomite and dolomitic siltstone (300 m), dark grey pyrrhotitic and scapolitic dolomitic siltstone (350 m), dark brown to dark grey pyrrhotitic dolomitic siltstone interbedded with thin quartzose siltstone, pyrrhotitic fine-grained sandstone, and micaceous sandstone (350 m), and dark grey fine-grained pyrrhotitic dolomitic siltstone and minor interbeds of quartzose siltstone (600 m).|16-MAY-23
26310|Lady Clayre Dolomite|Extent|The unit is exposed in a north-trending belt approximately 20 km long and 4 km wide extending north from Gulliver Creek and lying between the Knapdale Range and Cabbage Tree Creek in the north. The total area of outcrop is about 60 km2.|16-MAY-23
26310|Lady Clayre Dolomite|Thickness range|Folding and relatively uniform lithology hinder determination of the thickness of the Lady Clayre Dolomite. The type section is about 1600 m thick and the maximum thickness probably does not exceed 3000 m.|16-MAY-23
26310|Lady Clayre Dolomite|Lithology|The main rock type is dark brown to black, thin-bedded to laminated dolomite and pyrrhotitic dolomitic siltstone, which typically contains ovoid porphyroblasts of chiastolite, scapolite, or actinolite. The dolomite contains a mosaic of small (0.05 mm) interlocking carbonate grains, anhedral quaratz grains, some euhedral muscovite flakes, a fine dusting of  (graphitic?) opaques, elongate patches of pyrrhotite, and rare spots of pyrite. Garnet, chlorite, and tourmaline are minor constituents of some specimens. Some 100 to 200 mm thick interbeds of grey laminated fine-grained siliceous sandstone and siltstone occur in the unit. Weathering of the sulphides to limonite has produced the brown colouration.|16-MAY-23
26310|Lady Clayre Dolomite|Relationships and boundaries|The Lady Clayre Dolomite appears to overlie the Coocerina Formation conformably, but the contact is in a fault zone which contains sheared rocks and quartz veins. This boundary coincides with the change from grey siltstone and granofels of the Coocerina Formation to black to dark brown laminated dolomite. The only Proterozoic unit which may be younger than the Lady Clayre Dolomite in the Quamby Sheet area is the Quamby Conglomerate but it is not in contact with the dolomite. The dolomite is overlain unconformably by Mesozoic sandstone, and by Cambrian quartzite at the base of the Kajabbi Formation (Wilson & others, 1979a). Most contacts with the Kajabbi Formation and all contaacts with the Corella Formation are faulted.|16-MAY-23
26310|Lady Clayre Dolomite|Structure and Metamorphism|The Lady Clayre Dolomite generally youngs and dips west at 60o to 80o in the north but refolded isoclinal folds are evident in the southern exposures. Metamorphic grade probably reached the lower greenschist facies, however, the dolomite is surprisingly fine-grained and porphyroblasts are rare.|16-MAY-23
26310|Lady Clayre Dolomite|Age reasons|The Lady Clayre Dolomite is younger than the Corella Formation which was deposited between 1760 and 1740 Ma ago, and older than the regional metamorphism and major deformation which occurred between 1450 and 1670 Ma (Page 1978, 1981).|16-MAY-23
26310|Lady Clayre Dolomite|Comments|Discussion: The sedimentation evidently occurred in a low-energy environment resulting in a few ripple marks or cross beds in the fine-grained clastic sediments. The abundant sulphides also supports a quiet, possibly euxinic depositional environment. Similarities of this unit with the Dugald River Shale Member of the Corella Formation and the underlying dolomitic footwall limestone have been used by some exploration company geologists to correlate the two sequences, but this correlation is not supported by the structural and younging information. The Lady Clayre Dolomite may correlate with the White Blow Formation. Similar dolomite is not known in the White Blow Formation (Derrick & others, 1977a), but is moderately common in the lower formations of the Mount Isa and McNamara Groups such as the Native Bee Siltstone and Paradise Creek Formation, which are considerably younger (1670 Ma; Page 1981).|16-MAY-23
10153|Langdon River Siltstone|Geomorphic expression|Produces a characteristic topography with a dense dendritic drainage pattern, in places partly rectilinear due to strike-ridge control, and rounded but steep-sided hills of uniform size and height. Vegetation cover ranges from dense Acacia forest to open mixed forest.|16-MAY-23
10153|Langdon River Siltstone|Type section locality|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
10153|Langdon River Siltstone|Extent|Crops out in the western portions of Forest Home and North Head 1:100 000 Sheet areas, and along the eastern edges of Esmeralda and Gilbert River 1:100 000 Sheet areas, in the watershed between the Langdon River system and the Black Gin Creek system, and along the valley of the Langdon River between the Gilbert River (about 18o15'S), and 18o53'S.|16-MAY-23
10153|Langdon River Siltstone|Thickness range|Variable: about 800 m in the type section; 1400 m or more in the north, where there is some repetition by complex folding within the unit.|16-MAY-23
10153|Langdon River Siltstone|Lithology|Variably carbonaceous and ferruginous (fine-grained pyrite?) phyllitic siltstone, siltstone, phyllite, rare micaceous fine sandstone and sandy siltstone. Generally very thin-bedded or laminated. Weathered rocks display characteristic alternating bands of grey and red-brown or maroon (more pyritic(?) layers) about 1 to 5 cm thick. Has a discontinuous highly carbonaceous bed at its base.|16-MAY-23
10153|Langdon River Siltstone|Relationships and boundaries|Conformably overlies Candlow Formation (top of White's (1959) "Etheridge Formation") and unconformably overlain by Malacura Sandstone. In one place (approximately GR 7460-080240), the Malacura Sandstone rest directly on Candlow Formation. The Langdon River Formation has been intruded by Esmeralda Granite and Forest Home Granodiorite. In the south, it is in part unconformably overlain by a succession of Mesozoic sandstone units, outliers of which rest on the unit farther to the north.|16-MAY-23
10153|Langdon River Siltstone|Identifying features|Revised Definition: The Langdon River Formation was originally defined by White (1959), a definition which included rocks that, as a result of recent field work, have been shown to unconformably overlie the upper part of White's "Etheridge Formation" as well as the lower part of his "Langdon River Formation". The unit is now redefined to include rocks conformably overlying the upper part of White's "Etheridge Formation" (now Candlow Formation) and below the unconformity at the base of the Malacura Formation (new name). The name is changed to Langdon River Siltstone because the unit is predominantly siltstone.|16-MAY-23
10153|Langdon River Siltstone|Age reasons|Mid-Proterozoic. Has been affected by metamorphism dated in underlying rocks at 1570+/-30 m.y. (Black et al., in press), so 1570 m.y. is a minimum age.|16-MAY-23
10153|Langdon River Siltstone|Status|1|16-MAY-23
10313|Leichhardt Metamorphics|Name source|Leichhardt River (see Carter et al., 1961).|16-MAY-23
10313|Leichhardt Metamorphics|Type section locality|As nominated by Carter et al., 1961; the type area is in the Prospector 1:100 000 Sheet area, and extends west for about 8 km from the Referee copper mine (6857718524)*. In this type area the Metamorphics are intruded by Kalkadoon Granite and dolerite dykes.   *Australian Map Grid reference, zone 54 (metric)|16-MAY-23
10313|Leichhardt Metamorphics|Extent|See Carter et al., 1961.|16-MAY-23
10313|Leichhardt Metamorphics|Thickness range|The maximum thickness of the Leichhardt Metamorphics is unknown because the base is not exposed, but a minimum thickness of nearly 4000 m is recorded from near Blockade mine (Derrick et al., 1974).|16-MAY-23
10313|Leichhardt Metamorphics|Lithology|Grey, porphyritic acid volcanics, mainly dacite, rhyodacite and fluidal rhyolite, rhyolite breccia and acid tuffaceous rocks.|16-MAY-23
10313|Leichhardt Metamorphics|Relationships and boundaries|Redefinition of the Leichhardt Metamorphics is necessary because of new boundary criteria. Carter et al (1961, p.61) considered that the Leichhardt Metamorphics were conformably overlain by the Argylla Formation. It is now clear that a sequence of basic volcanics overlies the Leichhardt Metamorphics with apparent conformity (Derrick et al., 1974, Wilson et al., in prep.). This basic volcanic sequence is known as the Magna Lynn Metabasalt, and the contact between the Metamorphics and Magna Lynn Metabasalt is exposed about 6 km northeast of the Referee mine, near the old type section. The Argylla Formation overlies the Magna Lynn Metabasalt conformably.|16-MAY-23
10313|Leichhardt Metamorphics|Identifying features|For original definition, see Carter et al., 1961).|16-MAY-23
10313|Leichhardt Metamorphics|Proposed publication|Queensland Government Mining Journal|16-MAY-23
10313|Leichhardt Metamorphics|Status|1|16-MAY-23
10574|Lockup Well Limestone|Name source|Lockup Well, at 7859-758664.  The grid reference is based on the AGD66 datum.|16-MAY-23
10574|Lockup Well Limestone|Unit history|The limestone was shown as 'D' lens of the Broken River Formation by White (1965), and was defined as a member of the Broken River Formation (now Group) by Jell (1968).  It was raised to formation status by Withnall & others (1988), but was not redefined.|16-MAY-23
10574|Lockup Well Limestone|Geomorphic expression|Generally low relief with low limestone outcrops.|16-MAY-23
10574|Lockup Well Limestone|Type section locality|Jell (1968) defined a type section in Magpie Creek between 7859-753650 and 744662 (top).  The base of the unit is nowhere exposed, being covered by Tertiary ferricrete and basalt.  About 400 m of bioclastic calcarenite and calcirudite are exposed in this section.   The grid references are based on the AGD 66 datum.|16-MAY-23
10574|Lockup Well Limestone|Extent|A narrow belt up to 600 m wide on the northern edge of the large laterite plateau in central BURGES, and extending for 8 km southwest from Lockup Well.|16-MAY-23
10574|Lockup Well Limestone|Thickness range|190 to 690 m.|16-MAY-23
10574|Lockup Well Limestone|Lithology|Mainly bioclastic calcirudite and calcarenite with only sporadic thin siliciclastic interbeds.|16-MAY-23
10574|Lockup Well Limestone|Fossils|The limestone contains a fauna dominated by corals, and stromatoporoids, but has not been studied in detail.  Conodonts have been studied by Telford (1975) and Mawson & Talent (in press).|16-MAY-23
10574|Lockup Well Limestone|Relationships and boundaries|The unit is part of the Wando Vale Subgroup of the Broken River Group.  The base is obscured by Tertiary ferricrete and basalt.  It is overlain by a thin mudstone interval equated with the Papilio Mudstone, although this is generally too thin to map out at 1.100 000 scale and the Mytton Formation is usually shown directly overlying the limestone.  The limestone is faulted against the Shield Creek Formation for much of its length.  Under the basalt and ferricrete cover it may be continuous with the Jessey Springs Limestone, and prior to faulting may have been continuous with the Dip Creek Limestone.|16-MAY-23
10574|Lockup Well Limestone|Age reasons|The age is Emsian to early Givetian.|16-MAY-23
10574|Lockup Well Limestone|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. ***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.WHITE, D.A., 1965:  The geology of the Georgetown/Clarke River area, Queensland.  Bureau of Mineral Resources, Australia, Bulletin 71.|16-MAY-23
24373|Maramungee Granite|Name source|Named after E-flowing Maramungee Creek, branches of which drain NE part of outcrop area of unit, Selwyn 1:100 000 Sheet area, Duchess 1:250 000 Sheet area.|16-MAY-23
24373|Maramungee Granite|Unit history|Like all 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
24373|Maramungee Granite|Type section locality|In the vicinity of GR 905130, 13 km NW of Answer Downs homestead, on either side of a north-draining tributary of Maramungee Creek, Selwyn 1:100 000 Sheet area. Here there are extensive, mainly bouldery exposures of heterogeneous leucocratic granitic rocks in low hilly terrain. Intrusive contacts with metamorphic rocks of the Soldiers Cap Group are exposed 400 m to the east and west.|16-MAY-23
24373|Maramungee Granite|Extent|Forms NNE-trending outcrop 5 km long and up to 1 km wide in NE of Selwyn 1:100 000 Sheet area, centred at GR 905130, Duchess 1:250 000 Sheet area.|16-MAY-23
24373|Maramungee Granite|Lithology|Heterogeneous, mainly medium to fine-grained leucocratic granitic rocks - granite, granodiorite and tonalite - but also includes some pegmatite. The granitic rocks range from massive to strongly foliated, and generally contain less than 5 percent dark minerals - mostly partly altered biotite.|16-MAY-23
24373|Maramungee Granite|Relationships and boundaries|Intrudes Soldiers Cap Group. Cut by east-trending dolerite dyke.|16-MAY-23
24373|Maramungee Granite|Age reasons|Proterozoic|16-MAY-23
24373|Maramungee Granite|Proposed publication|Blake & others, in prep. - see References|16-MAY-23
24373|Maramungee Granite|Comments|Remarks: The Maramungee Granite forms a well-defined, readily mappable, intrusive body geographically separated from other granitic intrusions. It is probably related to the petrographically similara Blackeye and Cowie Granites (new names) to the south. It forms part of the Williams Batholith (new structural term), which includes all granites previously mapped as Williams Granite, together with the Wimberu Granite.|16-MAY-23
24373|Maramungee Granite|Defn Reference|82/22920|16-MAY-23
24373|Maramungee Granite|Proposer|Blake D.H.|16-MAY-23
24373|Maramungee Granite|Resdate|08-JUN-1979, 17-OCT-1980|16-MAY-23
27088|Marimo Slate|General description|Revision: The Marimo Slate was formally defined by Carter et al (1961) with reference to a type section extending about 7.3 km westwards and 9.8 km eastwards from Mount McNamara. The detailed mapping has confirmed the presence of extensive faulting and  repetition by folding in the section as reported by Carter et al. (1961). Also, the internal stratigraphy of the formation has been clarified and this is displayed in a reference section in two parts; the lower part runs for 1.5 km east of a small rock hole 3 km north of the Eight-Mile Rock Hole (from 6956 400839 to 6956 416893): the upper part runs in a northeasterly direction from the Mount McNamara copper mine for 1.5 km (from 6956 396863 to 6956 403877). The internal stratigraphy of the formation from the top to the base is as follows: Up to 380 m of ferruginous siltstone, fine-grained sandstone, rare marl and calcareous sandstone; in places a fine to medium-grained sandstone unit is present and has been mapped separately as the Mick Creek Sandstone Member; it has a minimum thickness of 500 m; these rocks overlie in order - 400 m of grey slate and black carbonaceous slate; 280 m of marly siltstone, limestone and attenuated siltstone;380 m of phyllite, mica schist, and siltstone, and at the base 820 m of clean fine to medium-grained feldspathic sandstone, which has been formally named the Toby Barty Sandstone Member. The total thickness of the Slate is about 2000 m.  The Marimo Slate appears to conformably overlie a thin sequence of carbonate sediments believed to belong to the lower unit of the Corella Formation; a limestone unit occupying synclinal keels in the Marimo Slate has been mapped as the upper unit of the Corella Formation; this means that the Marimo Slate is broadly equivalent to the middle unit of the Corella Formation. As detailed mapping of the Marimo Slate has been confined to the Marraba 1:100 000 Sheet area, its relationship to the Answer Slate, Kuridala Formation and Staveley Formation to the south has not been clarified.|16-MAY-23
27088|Marimo Slate|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1977|16-MAY-23
27088|Marimo Slate|Proposed publication|Queensland Government Mining Journal|16-MAY-23
25693|Maureen Volcanics|Name source|"Maureen" uranium-molybdenum-fluorite prospect, 35 km NNW from Georgetown, GR 7561-571078 (camp) 7562-570085 (main lode).|16-MAY-23
25693|Maureen Volcanics|Unit history|The Maureen Volcanics have previously been included in the Galloway Volcanics (Branch, 1966 (defined); White, 1962, 1965). However, the Maureen Volcanics appear to be a separate geological entity in that they form a basin-like structure that has no physical connection with the main body of Galloway Volcanics to the northeast.|16-MAY-23
25693|Maureen Volcanics|Geomorphic expression|Very low, rounded hills, moderately to extremely rocky, moderate to very sparse stunted vegetation; pale tone on airphotographs.|16-MAY-23
25693|Maureen Volcanics|Type section locality|Along Fiery Creek, between GR 7561-571080 and 7562-532129.  From the base upwards consists of: 1. Micaceous and/or (lithic-) quartz sandstone, siltstone, conglomerate, arkose, shale - about 200 m.  2. Flow-banded, massive, and brecciated glassy rhyolites; minor tuff - about 100 m.  3. Micaceous and/or (lithic-) quartz sandstone, siltstone, tuff, rhyolite, rhyolite breccia  intruded by plugs of coarse polymict rhyolitic agglomerate and flow-banded rhyolite - about 200.  4. Rhyolitic tuff, ash, agglomerate, minor ignimbrite; minor tuffaceous sandstone - about 200 m.  5. Strongly flow-banded/laminated rhyolite - about 80 m.  6. Fine-grained asphanitic basalt or basaltic andesite - about 60 m.  7. Massive polymict coarse rhyolitic agglomerate, intrusive in part - uncertain.  8. Fine-grained aphanitic basalt or basaltic andesite - 100 m.  9. Rhyolitic ignimbrite and agglomerate; some rhyolite, rhyolitic breccia and tuff - about 150-170 m.  10. Dacitic ignimbrite; some agglomerate (overlies 9) - uncertain.  11. Reappearance of unit 3.  12. Stream crosses again into unit 9.  13. Faulted boundary against Robertson River Formation.|16-MAY-23
25693|Maureen Volcanics|Extent|Exposed over a roughly triangular area in the northeastern corner of Forest Home and the southeastern corner of Abingdon Downs 1:100 000 Sheet; corners at GR 7562-560110, 7561-410980, 7561-370060 (approx.). Small inliers exposed (from beneath Mesozoic-Tertiary cover) at GR 7562-360160 and -390145 (approx.).|16-MAY-23
25693|Maureen Volcanics|Thickness range|Highly variable, probably averaging about 1000 m, and up to 1500 m or more in the northeast.|16-MAY-23
25693|Maureen Volcanics|Lithology|Rhyolitic ignimbrite, dacitic ignimbrite, rhyolite, rhyolitic agglomerate, ash, and tuff, basalt, andesite, micaceous and/or lithic-quartz sandstones; siltstone, conglomerate, arkose, shale (in approximate order of abundance).|16-MAY-23
25693|Maureen Volcanics|Relationships and boundaries|Unconformably overlies Robertson River Formation and enclosed granitic rocks in a strongly angular relationship. Base of volcanic sequence commonly marked by sandstone, conglomerate, or arkose. Overlain unconformably by late Jurassic-early Cretaceous Yappar Member of the Gilbert River Formation and late Cretaceous-early Tertiary Bulimba Formation.|16-MAY-23
25693|Maureen Volcanics|Age reasons|Mid-Carboniferous, by correlation and/or analogy with the Newcastle Range Volcanics, dated at 318+/-5 m.y. (Black, 1973). Many similarities exist between the sequence in the northern Newcastle Range and the Maureen Volcanics in the type area.|16-MAY-23
25693|Maureen Volcanics|Proposed publication|Queensland Government Mining Journal|16-MAY-23
25693|Maureen Volcanics|Proposer|Mackenzie D.E.|16-MAY-23
27191|May Downs Gneiss Member|Name source|May Downs homestead, 22 km northwest of Mount Isa, latitude 20o35'20"S, longitude 139o20'30"E (6756 272124)*, lies 10 km north-northwest of the northern limit of the Gneiss.  *Australian Map Grid Reference, zone 54 (metric).|16-MAY-23
27191|May Downs Gneiss Member|Geomorphic expression|Flat to gently undulating sand-covered pediments and some rounded residual hills.|16-MAY-23
27191|May Downs Gneiss Member|Type section locality|The type area is between 10 km west-northwest and 9 km northwest of Mount Isa, from latitude 20o42'S, longitude 139o23'50"E (6756 331102)* to latitude 20o41'20"S, longitude 139o24'30"E (6756 345115) along Big Sandy Creek, where the May Downs Gneiss Member is exposed in a complexly folded anticline. The main rock types here are grey microcline-quartz gneiss, biotite-quartz gneiss, sillimanite-muscovite-quartz gneiss and minor schist.|16-MAY-23
27191|May Downs Gneiss Member|Extent|Mount Isa 1:100 000 Sheet area: the main outcrop occurs in a 22 km long north-trending belt 7 to 10 km west of Mount Isa. Other areas of poorly exposed gneissic rock occur 10 km west of the May Downs homestead.|16-MAY-23
27191|May Downs Gneiss Member|Thickness range|Because of limited exposure, poorly defined bedding and complex structure, the thickness cannot be measured. A minimum thickness of 500 m is probable.|16-MAY-23
27191|May Downs Gneiss Member|Lithology|Foliated grey biotite-muscovite-microcline-quartz gneiss, biotite-quartz gneiss, pink, grey and white microcline-quartz gneiss, quartz-muscovite-biotite schist, quartzite, sillimanite-muscovite quartz gneiss and schist, and opaque-banded quartzite. |16-MAY-23
27191|May Downs Gneiss Member|Relationships and boundaries|The base of the May Downs Gneiss Member is not exposed. The Gneiss is overlain conformably by the upper unit of the Mount Guide Quartzite. Both the Sybella Granite and veins of quartz, dolerite, and muscovite-feldspar-quartz pegmatite intrude the Gneiss.|16-MAY-23
27191|May Downs Gneiss Member|Age reasons|Precambrian, probably Carpentarian (Middle Proterozoic). The Sybella Granite, dated in parat (by Rb/Sr methods) as 1656 m.y. (Plumb & Derrick, 1975), provides a minimum age for the May Downs Gneiss Member.|16-MAY-23
27191|May Downs Gneiss Member|Comments|Remarks: Gneiss was recognised west of Mount Isa by Joplin (1955) and by Brooks and Shipway (1960). Carter et al. (1961, p.66) considered that it might be referred to the Mount Guide Quartzite. Wilson (1972) divided the quartzofeldspathic rocks into an upper quartzite, which he termed Mount Guide Quartzite, and a lower gneiss unit, which he informally called May Downs gneiss. The May Downs Gneiss Member of the Mount Guide Quartzite is probably equivalent to the arkosic and micaceous lower unit of the Mount Guide Quartzite. The schistose and gneissic textures have developed in the May Downs Gneiss Member because of higher metamorphic grade, probably related to the intrusion of the Sybella Granite.|16-MAY-23
27191|May Downs Gneiss Member|Status|1|16-MAY-23
13028|Mount Philp Agglomerate|Identifying features|Revision: The Mount Philp Agglomerate was formally defined by Carter et al. (1961) with reference to a type section extending 2.5 km southeast from the edge of outcrop of the formation about 0.5 km southeast of the abandoned township of Ballara to a large waterhole on Read Creek. In the detailed mapping the unit is restricted to a north-northeast trending belt covering about 15 km2 in the southeast corner of the Mary Kathleen 1:100 000 Sheet area and extending south into the Duchess 1:100 000 Sheet area. Some metasediments and metavolcanics previously mapped as part of the formation are now included in the middle unit of the Corella Formation. The most common rock type in the Mount Philp Agglomerate is a crystal tuff, which grades into the next most common rock type - a lithic tuff or agglomerate; another common type is fine-grained basic rock which occurs as bombs or xenoliths. Minor blocks of contorted laminated calc-silicate rocks also occur. The rocks have all been metamorphosed in the high greenschist or low amphibolite facies. The Mount Philp Agglomerate overlies metasediments and metavolcanics of the middle unit of the Corella Formation, and is probably overlain by a small block of laminated calc-silicate rock which may be part of the upper unit of the Corella Formation. The Mount Philp Agglomerate is either synchronous with, or postdates the middle member of the Corella Formation. It is intruded by dolerite, gabbro and numerous acid veins and garnetiferous pegmatites related to the Burstall Granite. No internal stratigraphy has been defined but the unit is less than one kilometre thick. The origin of the Mount Philp Agglomerate is still not resolved. The evidence for a volcanic origin for this formation includes the agglomeratic texture, basic igneous clasts, and a close association with amygdaloidal basalt and andesitic tuff in the underlying sequence of the middle member of the Corella Formation. However the petrographic studies of the Mount Philp Agglomerate have not excluded the possibility  that the 'agglomerate' is a brecciated, metamorphosed, metasomatized sequence of  calcareous sediments extensively intruded by dolerite.|16-MAY-23
13028|Mount Philp Agglomerate|Defn author|Derrick G.M., Wilson I.H., Hill R.M., 1977|16-MAY-23
13028|Mount Philp Agglomerate|Proposed publication|Queensland Government Mining Journal|16-MAY-23
13028|Mount Philp Agglomerate|Status|1|16-MAY-23
16178|Robertson River Formation|Name source|Robertson River, a major tributary of the Gilbert River.|16-MAY-23
16178|Robertson River Formation|Geomorphic expression|Robertson River Metamorphics (White 1959, 1962, 1965; Bain & others 1976, Oversby and others 1978). White gave the name to an area of metamorphic rocks in the Robertson River area; the relationship between these rocks and the lower-grade Etheridge Formation to the west was not known. Work by the joint BMR-GSQ party and James Cook University staff and students has recognised that the Robertson River Metamorphics grades into the lower part of the former Etheridge Formation. We therefore extend the unit to include these low-grade equivalents to conform with Section 20 of the Australian Code of Stratigraphic Nomenclature. The name is here changed from Robertson River Metamorphics to Robertson River Formation because ordinary stratigraphic principles can be applied to a large part of the unit, and to be consistent with the nomenclature of the units above and below in the sequence. The high-grade parts of the unit (lower to upper amphibolite facies) are referred to as 'Robertson River Formation (schist phase)'.|16-MAY-23
16178|Robertson River Formation|Type section locality|White (1959) designated the section exposed in the Robertson River between the Forsayth-Agate Creek road (GR 653 113) and Tin Hill (GR 718 110 approx.) as the type area of the unit. We consider this to be an adequate type section for the intensely deformed amphibolite facies "schist phase" of the unit. The rocks exposed in the type section include quartz-mica schist, micaceous quartzite and garnet-staurolite-quartz-mica schist. Unassigned amphibolite (which could, in part, be an equivalent of the Dead Horse Metabasalt Member) and the Tin Hill Quartzite Member also occur in the section. Because the Robertson River Formation as now defined has been extended to include rocks in which a stratigraphy is recognised, and as the type section probably represents a relatively small interval in this sequence, it is considered desirable to nominate several reference sections to more adequately define the unit. 1. Percy River between 633 788 (Gilberton 1:100 000 Sheet area-base of the Robertson River Formation) and 622 796 (Bellfield 1:100 000 Sheet area - base of the Dead Horse Metabasalt Member). Between 500 and 600 m of grey to green, commonly laminated cleaved siltstone, shale, and minor fine sandstone are exposed. Some of the rocks are slightly carbonaceous and locally weakly calcareous, particularly towards the base.  2. Slatey Creek in the North Head 1:100 000 Sheet area between 479 125 (top of Dead Horse Metabasalt Member) and 477150 (base of upper part) of the Robertson River Formation). The rocks consist of grey to green generally non-laminated slate and phyllite, commonly containing chloritoid. The thickness of the section is unknown because of the lack of preserved bedding and the complex multiple folding. A maximum of 1500 m is present but the true thickness is probably less than 1000 m. Similar rocks in the same stratigraphic position are also well exposed in the gorge of Stake Yard Creek upstream from the Forsayth-North Head road at 400 192 to 413 159.  3. Eastern bank of the Robertson River between the Irrigation and Water Supply Commission gauging stations at 484 223 (North Head 1:100 000 Sheet area - base of upper part ) and 471 251 (base of the Townley Formation). The rocks consist predominantly of grey to dark grey phyllitic siltstone, which is locally strongly carbonaceous, and minor fine-grained sandstone; minor calcareous rocks are present. The thickness of this section is not known because of the probable repetition of the sequence by minor folds. It is unlikely to represent more than 1000 m.|16-MAY-23
16178|Robertson River Formation|Extent|Crops out in a belt approximately 50 km wide by 150 km long extending north from around Gilberton homestead to the Ironhurst area, and mostly between the Gilbert River and the Newcastle Range. Total area approximately 5000 km2.|16-MAY-23
16178|Robertson River Formation|Thickness range|The thickness of the Robertson River Formation is difficult to determine because of the intense multiple deformation which has affected it over much of its outcrop area. A composite section made up of the reference sections given above plus the Dead Horse Metabasalt Member is about 3000 m thick. This is only a rough order of magnitude, because the constituent subunits undoubtedly vary considerably in thickness.|16-MAY-23
16178|Robertson River Formation|Lithology|The low grade (greenschist to lower amphibolite facies) and less intensely deformed parts of the Robertson River Formation can be divided into two parts. The lower part which includes the Dead Horse Metabasalt Member consists mainly of grey (slightly carbonaceous) to green siltstone and shale, generally cleaved and commonly well laminated, particularly below the metabasalt member, where fine-grained locally calcareous sandstone is also present. Above the metabasalt, the lower part appears to be predominantly siltstone and shale; chloritoid is a common metamorphic mineral in this part of the sequence. The upper part consists of grey, commonly strongly carbonaceous cleaved siltstone and fine sandstone. Calcareous siltstone and impure limestone are also constituents and grade into calc-silicate rocks and impure marble where the metamorphic grade approaches amphibolite facies. The Robertson River Formation (schist phase), which accounts for more than half of the outcrop area, consists mainly of quartz-mica schist and micaceous quartzite; depending on the original composition and metamorphic grade, minerals such as andalusite, staurolite, garnet and sillimanite are also present in the schists. Northeast of Ironhurst the rocks grade into migmatite. With more detailed mapping than so far attempted, the two subunits described above could probably be traced into the more intensely deformed and more highly metamorphosed "schist phase".|16-MAY-23
16178|Robertson River Formation|Relationships and boundaries|The Robertson River Formation conformably overlies Bernecker Creek Formation and is conformably overlain by Townley Formation. The base is defined as the change from predominantly calcareous to non-calcaraeous siltstone and sandstone (or their metamorphic equivalents). The top is defined by the change from predominantly carbonaceous siltstone and shale to white to light grey fine-grained sericitic quartz sandstone and siltstone. The unit grades into Einasleigh Metamorphics which is recognised as consisting predominantly of quartzofeldspathic biotite gneiss rather than quartz-mica schist. Because of the intense multiple deformation it is not yet known whether this is a lateral or vertical gradation. The unit contains two named members, the Dead Horse Metabasalt Member and Tin Hill Quartzite Member. Metadolerite and metagabbro sills intrude the Robertson River Formation and are folded and metamorphosed with it. In the "schist phase" these grade into amphibolite. Numerous mid-Proterozoic, late Proterozoic or Devonian, and late Palaeozoic granitoids intrude the unit.|16-MAY-23
16178|Robertson River Formation|Identifying features|Original definition: White (1959)|16-MAY-23
16178|Robertson River 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
16178|Robertson River Formation|Proposed publication|Queensland Government Mining Journal|16-MAY-23
16178|Robertson River Formation|References|80/20677; 98/29026; ?98/29014|16-MAY-23
17301|Station Creek Adamellite|Name source|Derived from Station Creek, 20 km south-southeast of Kilkivan, GR 5433 7422.|16-MAY-23
17301|Station Creek Adamellite|Unit history|"Karandah adamellite" and "Station Creek adamellite" of Brooks et al. (1974).|16-MAY-23
17301|Station Creek Adamellite|Type section locality|Along headwaters of Station Creek, 5 km east-northeast of the Shamrock Mine (GR 542 743 to 544 743, Gympie 1:250 000 Sheet area.   (Amendment 23-OCT-1975).|16-MAY-23
17301|Station Creek Adamellite|Extent|The unit covers an irregularly shaped area of 380 km in the northern central part of the Gympie 1:250 000 Sheet area SG 56-10, between Kilkivan and Gympie.|16-MAY-23
17301|Station Creek Adamellite|Lithology|Leucocratic biotite adamellite is the dominant rock type but hornblende-biotite diorite, biotite granite and hornblende-biotite monzonite are also present.|16-MAY-23
17301|Station Creek Adamellite|Relationships and boundaries|The unit intrudes undifferentiated Palaeozoic sediments, volcanics and serpentinite, the Permo-Carboniferous Amamoor Beds and Biggenden Beds and the Permian Gympie Group. The unit is apparently overlain by the Lower to Middle Triassic Neara Volcanics.|16-MAY-23
17301|Station Creek Adamellite|Age reasons|K/Ar age determinations by Webb and McDougall (1967), 226 m.y. and Brooks et al. (1974), 231 m.y., indicate a Lower to Middle Triasic age.|16-MAY-23
17301|Station Creek Adamellite|Proposed publication|Report of the Geological Survey of Queensland|16-MAY-23
17301|Station Creek Adamellite|References|79/00626; 99/29927.|16-MAY-23
17301|Station Creek Adamellite|Name first published by|Brooks J.H., Syvret, J.N., Sawers J.D., 1974|16-MAY-23
17301|Station Creek Adamellite|Reserved? Yes/No|N|16-MAY-23
17301|Station Creek Adamellite|Status|2|16-MAY-23
17352|Stockyard Creek Siltstone Member|Name source| After White (1959), Stockyard Creek, which joins the Gilbert River at longitude 143deg16' and latitude 18 deg 34', in the central part of the Georgetown four mile sheet.|16-MAY-23
17352|Stockyard Creek Siltstone Member|Geomorphic expression|Crops out prominently as steep-sided but rounded, generally rocky ridges and loaf-shaped hills with a characteristic dense cover of Acacia shirleyi ("lancewood").|16-MAY-23
17352|Stockyard Creek Siltstone Member|Type section locality|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
17352|Stockyard Creek Siltstone Member|Extent|In a discontinuously exposed bed of variable thickness (may pinch out in places) from 7 km SE of Forest Home homestead (GR 7561-207780) generally southward along the valley of Pinnacle Creek, then along the upper valley of Black Gin Creek, to about 18o50'S, where it disappears beneath Mesozoic cover rocks in the headwaters of the Langdon River and in the Reedy Creek area (GR 7560-262180).|16-MAY-23
17352|Stockyard Creek Siltstone Member|Thickness range|Averages 100 to 150 m; range from less than 50 m to about 300 m; may pinch out entirely in places.|16-MAY-23
17352|Stockyard Creek Siltstone Member|Lithology|Black, generally pyritic (or originally pyritic) finely laminated to massive carbonaceous siltstone; minor white quartzose fine sandstone in places; thin interbeds of micaceous siltstone, phyllite, and fine dark grey sandstone in places in the north (Pinnacle Creek area).|16-MAY-23
17352|Stockyard Creek Siltstone Member|Relationships and boundaries|Intercalated in the upper part of the Candlow Formation, between the carbonaceous sandy uppermost division and the pyritic silty middle division. Has a characteristic outcrop form (see Topography), and is almost everywhere recognisable by its massive, pale grey to black, porous, and commonly slightly friable nature in outcrop. Appreciably more carbonaceous than stratigraphically adjacent rocks. Intruded in two places by Forest Home Granodiorite.|16-MAY-23
17352|Stockyard Creek Siltstone Member|Identifying features|Definition: More detailed work in the area has resulted in the following amendments to White's (1959) definition of the Stockyard Creek Siltstone Member.|16-MAY-23
17352|Stockyard Creek Siltstone Member|Age reasons|Probably mid-Proterozoic; a minimum age of 1570+/-30 m.y. may be inferred from dating in metamorphic rocks stratigraphically below the Candlow Formation of a metamorphic-structural event (Black et al., in press) which has affected the Candlow Formation.|16-MAY-23
17352|Stockyard Creek Siltstone Member|Proposed publication|Queensland Government Mining Journal|16-MAY-23
17352|Stockyard Creek Siltstone Member|References|80/20677; 98/29026, refID 44059:  **White, D.A. 1959. New stratigraphic units in north Queensland geology. Queensland Government Mining Journal 60 (692 ), p442-447|16-MAY-23
17352|Stockyard Creek Siltstone Member|Reserved? Yes/No|N|16-MAY-23
17352|Stockyard Creek Siltstone Member|Status|1|16-MAY-23
19312|Walloon Sub-Group|Name source|Previously termed the Walloon Coal Measures (Reid, 1921, Whitehouse, 1955, Swarbrick 1973) the unit has been upgraded to sub-group status in the northeastern Surat Basin to include three newly named formations, namely the Taroom Coal Measures, the Tangalooma Sandstone and the Juandah Coal Measures (in stratigraphic order).|16-MAY-23
19312|Walloon Sub-Group|Unit history|Walloon Coal Measures (Swarbrick, 1973). Equivalent to the Walloon Coal Measures of the Moreton Basin and the Birkhead Formation of the Eromanga Basin.|16-MAY-23
19312|Walloon Sub-Group|Type section locality|The type section for the Walloon Coal Measures (Whitehouse 1955) has been retained for the unit. In the northeastern Surat Basin, the unit essentially consists of a lower coal measure sequence (Taroom Coal Measures) followed by an essentially sandstone sequence (Tangalooma Sandstone) which is in turn overlain by the upper coal measure sequence (Juandah Coal Measures).|16-MAY-23
19312|Walloon Sub-Group|Thickness range|The unit develops its maximum thickness in the Mimosa Syncline where it exceeds 500 m. The unit thins appreciably towards the west down to 150 metres near Injune.|16-MAY-23
19312|Walloon Sub-Group|Relationships and boundaries|Conformably overlies the Eurombah Formation although the boundary is gradational. Conformably overlain by the Springbok Sandstone.|16-MAY-23
19312|Walloon Sub-Group|Age reasons|Middle Jurassic (Gould, 1968).|16-MAY-23
19312|Walloon Sub-Group|Defn author|G.D. Jones, R.B.Partick. Approved 30-JUL-1981.|16-MAY-23
19312|Walloon Sub-Group|Proposed publication|Coal Geology|16-MAY-23
19312|Walloon Sub-Group|Comments|Notes: The type section for the Walloon Coal Measures is stated by Whitehouse (1955) as the mining region about the township of Walloon (GR 467000E, 6946000N, Ipswich Sheet 9442).|16-MAY-23
19312|Walloon Sub-Group|References|Gould, R.E., 1968. The Walloon Coal Measures: A compilation. Qld Govt Min. J., 69, pp509-515.  ** Reid, J.H., 1921. Geology of the Walloon-Rosewood Coalfield. Qld Govt Min.J., 22, pp22-227.  **Swarbrick, C.F.J., 1973.Stratigraphic and economic potential of the Injune Creek Group in the Surat Basin. GSQ Report 79.  ** Whitehouse, F.W., 1955. The geology of the Queensland portion of the Great Australia Basin; Appendix G, IN Artesian Water Suplied in Queensland. Dep.Co-ord. Gen.Pub.Wks. Qld Parl Ppaer A56-1955.|16-MAY-23
19312|Walloon Sub-Group|Status|1|16-MAY-23
33430|Woroonden Granodiorite|Name source|The unit is named after the Parish of Woroonden within which most of the unit is exposed.|16-MAY-23
33430|Woroonden Granodiorite|Unit history|Murphy & others (1976) previously mapped the unit as part of the Wigton Adamellite. The northern part of the unit was mapped in some detail as part of Queensland University of Technology honours study (Lowien, 1997).|16-MAY-23
33430|Woroonden Granodiorite|Geomorphic expression|The unit is poorly exposed in the alluvial flats to the east of Barambah Creek. To the west of the creek, the unit is slightly better exposed and forms undulating low hills with elevations ranging from  to  m................|16-MAY-23
33430|Woroonden Granodiorite|Type section locality|The type area for the unit is centred on AMG 372200 7118200.  The grid reference is based on the AGD66 datum.|16-MAY-23
33430|Woroonden Granodiorite|Extent|The unit occurs as a north-north-west trending body exposed in the valley of Barambah Creek north of Hivesville, covering an area of around 16 km2.|16-MAY-23
33430|Woroonden Granodiorite|Lithology|The characteristic rock type is cream to pale or dark grey, fine or medium-grained, equigranular, biotite-hornblende granodiorite, containing sparse to locally abundant (up to 60%) mafic clots and xenoliths.  Compositional variations include quartz monzodiorite, monzodiorite, and tonalite. Dark grey, medium to coarse-grained gabbro to dolerite occurs in places north of Crystal Springs homestead, but has not been mapped as a separate entity.  The granodiorite has a hypidiomorphic granular texture in thin section and commonly contains abundant accessory magnetite accounting for its moderate to strong magnetic signature. The relative proportions of plagioclase and alkali feldspar vary, with either locally predominating over the other.  A similar relationship occurs between hornblende and biotite, which combined generally make up to 7% of the total rock.  Both the latter minerals commonly form coarse locally poikilitic grains.  Mafic clots and even grained to porphyritic mafic xenoliths are common throughout much of the pluton, locally making up to 60% of the rock.  Zones of chloritic alteration occur in areas of known mineralisation.  The granodiorite locally shows evidence of moderate tectonic recrystallisation. In the Golden Spur mine area, east-northeast trending shears along which aplite dykes have been intruded cut the granite.|16-MAY-23
33430|Woroonden Granodiorite|Relationships and boundaries|The unit probably intrudes the Late Triassic Aranbanga Group, and is intruded by or co-magmatic with granite bodies mapped as unit Rg4 or Rg6.  The pluton is locally intruded by aplite, diorite, andesite, rhyolite and dacite dykes, which are probably only slightly younger than the granodiorite. The Woroonden Granodiorite is unconformably overlain by Oakdale Sandstone, and is capped by Tertiary duricrust surfaces in places.  Alluvial deposits of Barambah Creek and Tertiary basalts and sediments of the Main Range Volcanics mantle geophysical (magnetic)-interpreted extensions of the unit to the south.|16-MAY-23
33430|Woroonden Granodiorite|Age reasons|No age dating of the unit has been undertaken, but the unit is probably slightly younger than the Late Triassic Aranbanga Volcanic Group which it is interpreted to intrude.|16-MAY-23
33430|Woroonden Granodiorite|Comments|GEOPHYSICAL EXPRESSION:: On the ternary radiometric images, the unit has a mottled dark brown/pink tone, partly reflecting colluvial, alluvial and weathered soil mantling as well as the primary lithological response. The main body of the unit has a characteristic medium to high magnetic response on the RTP magnetic images. However, some marginal areas have a relatively low magnetic response. GEOCHEMISTRY:: Whole rock analyses by Lowien (1997) suggested that the unit was part of a metaluminous, medium-K, calc-alkaline complex.  He proposed that the parent magma was derived from a high degree of melting of a slightly depleted mantle wedge source, modified by LIL-enriched fluids originating from subducting oceanic lithosphere. MINERALISATION:: Significant gold mineralisation occurs at a number of small, fracture-controlled deposits on the east bank of Barambah Creek, east of Crystal Springs.  These deposits include the Bar 23 (worked for a short period ....), and the Red Rock, Misst, and Golden Spur deposits worked by small single-miner operations since the 1930's. Mineralisation: Significant gold mineralisation occurs at a number of small, fracture-controlled deposits on the east bank of Barambah Creek, east of Crystal Springs.  These deposits include the Bar 23 (worked for a short period in when!!), and the Red Rock, Misst, and Golden Spur deposits worked by small single-miner operations since the 1930's.|16-MAY-23
33430|Woroonden Granodiorite|References|LOWIEN,1997 ??  **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
