Stratno | Stratigraphic Name | Category | Contents | Last update 
25755|Abydos Adamellite|Name source|Abydos Pastoral Research Station, Marble Bar 1:250 000 Sheet area (M.G.R. 165 324)|16-MAY-23
25755|Abydos Adamellite|Unit history|Noldart and Wyatt (1958, p.39) used the term 'Woodstock-Abydos (Western) Granite' without definition to refer to the entire Yule Batholith.  Similarly, the term 'Abydos - Woodstock Granite' was published without definition by Noldart and Wyatt (1962), applying to the whole Yule Batholith.|16-MAY-23
25755|Abydos Adamellite|Type section locality|The unit is well exposed along the Mount Newman Railway from the radio Transmitter (M.G.R. 165 314) southwestwards for about 10 km, and particularly west of the Abydos Aerodrome (Abn( (M.G.R. 165 307).  Access is by the Port Hedland Wittenoom Road.|16-MAY-23
25755|Abydos Adamellite|Extent|The Abydos Adamellite is an irregular elongate mass on the Yule River Batholith and extends from a position 13 km west from Abydos Station, 35 km southeastwards to about 8 km southeast of Woodstock.  The pluton is moderately well exposed over an area of 160 km2.  It occurs between latitudes 21o22'S and 21o40'S, and longitudes 118o46'E and 119o02'E.  See Fig. 1.|16-MAY-23
25755|Abydos Adamellite|Lithology|The Abydos Adamellite is a medium to coarse-grained porphyritic biotite adamellite and locally a porphyritic biotite hornblende adamellite.  The mass is well foliated by biotite schlieren and elongate xenoliths, and alignment of phenocrysts and groundmass grains of feldspar, biotite and locally of quartz.  Adjacent to dolerite dykes a foliation parallel to the dyke direction is exhibited by phenocrysts, feldspar, biotite and particularly quartz.  There are numerous medium even-grained biotite granodiorite xenoliths.  Some of these are porphyritized.  Locally, coarse magnetite grains are present.  The pluton contains coarse pegmatite veins.  Phenocrysts range in size from 1 x 1 cm to 1 x 3 cm.  In thin section well twinned microcline phenocrysts with biotite, quartz and albite-rimmed plagioclase inclusions, are seen to be set in an allotriomorphic granular, directionless to foliated groundmass of oligoclase with patches of coarse myrmekite, microcline and quartz with minor biotite and hornblende.  Oligoclase and microcline occur in sub-equal proportions.  There is accessory sphene, magnetite, apatite and zircon.  Secondary minerals are chlorite, muscovite, epidote and rare calcite.  Biotite is partly or wholly replaced by chlorite.  Plagioclase is slightly to thoroughly sericitized.|16-MAY-23
25755|Abydos Adamellite|Relationships and boundaries|The Abydos Adamellite intrudes the oldest nebulitic or migmatitic biotite granodiorite country rock with broad transitional boundaries, over which poorly porphyritic, medium to coarse-grained adamellite increases in outcrop proportion and becoming more porphyritic, progressing through disrupted country rock and xenolith rich margins into the marin mass of the pluton.  This may indicate an intermediate structural level for the Adamellite which has been derived originally by remobilization of the country rock.  The Abydos Adamellite is intruded by medium to coarse even-grained foliated adamellite (see Coorong Creek Adamellite and Woodstock Adamellite) with narrower transitional zones (1-2 km) than those described above.  The Abydos Adamellite has a sharp contact with the medium to coarse, even-grained Numbana Granite thought to be younger than the Adamellite.  The pluton is faulted, and well jointed and is intruded by north-trending and west-northwest-trending Lower Proterozoic dolerite dykes.|16-MAY-23
25755|Abydos Adamellite|Proposed publication|West. Australia Geol. Survey Ann. Rept. 1974|16-MAY-23
25755|Abydos Adamellite|References|*NOLDART A.J., and Wyatt J.D., (1958), Summary progress report on reconnaissance survey of portion of the Pilbara Goldfield:  West. Australia Geol. Survey Bull. 113, p. 35-44. ;    *GOLD 0825, p 199.|16-MAY-23
887|Baines Beds|Name source|Baines Hills Range, Billiluna 1:250 000 Sheet area, WA|16-MAY-23
887|Baines Beds|Unit history|Previously mapped as Kearney Beds (Wells 1962, Casey & Wells, 1964).|16-MAY-23
887|Baines Beds|Type section locality|Reference area:  Southern end of the Peterson Range between 19o22'12"S, 128o08'12"E and 19o22'40"S, 128o07'30"E.  Here 1000 m approx. is exposed consisting of medium to fine-grained mostly silicified quartz arenite and sublithic arenite.|16-MAY-23
887|Baines Beds|Extent|Petersons Range, Billiluna 1:250 000 Sheet area, WA|16-MAY-23
887|Baines Beds|Thickness range|About 1000 m.|16-MAY-23
887|Baines Beds|Lithology|Medium to fine grained, maroon, grey and pink quartz arenite and sublithic arenite, some of which contains shale pellets; greywacke, lithic arenite and conglomeratic sublithic arenite.|16-MAY-23
887|Baines Beds|Relationships and boundaries|Unconformably overlain by Palaeozoic rocks of the Canning Basin.  Separated by inferred faults from  Proterozoic rocks to the east.|16-MAY-23
887|Baines Beds|Age reasons|Carpentarian or Adelaidean.|16-MAY-23
1018|Bamboo Springs Adamellite|Name source|Bamboo Springs homestead, Roy Hill 1:250 000 Sheet area (M.G.R. 246 247).|16-MAY-23
1018|Bamboo Springs Adamellite|Type section locality|The Adamellite is well exposed along the Hillside-Bamboo Springs road.|16-MAY-23
1018|Bamboo Springs Adamellite|Extent|The Bamboo Springs Adamellite forms an irregular scalene triangle on the southern margin of the Marble Bar Sheet area, about 8 km southeast of Coondina mining centre.  The limits of the pluton on the adjacent Roy Hill Sheet have not been determined.  The mass crops out over an area of 160 km2 between latitudes 21o56'S and 22o00'S, and longitudes 119o18'E and 119o43'E. (See Fig. 1).|16-MAY-23
1018|Bamboo Springs Adamellite|Lithology|The Bamboo Springs Adamellite is a medium to coarse-grained porphyritic biotite adamellite.  A prominent steeply dipping foliation, generally parallel to the margin, is exhibited by biotite schlieren and alignment of phenocrysts and feldspar, biotite and locally quartz grains.  There are abundant xenoliths of fine to medium, even-grained biotite granodiorite or adamellite and rare amphibolite xenoliths.  These are commonly elongate and generally foliated parallel to the host rock foliation.  The microcline phenocrysts (up to 1 x 1 cm in size) are well twinned with quartz, plagioclase and chloritized biotite inclusions, and are set in a foliated allotriomorphic granular groundmass of oligoclase, microcline, quartz and biotite, with minor sphene and allanite.  Accessory minerals are magnetite, apatite and rare zircon.  Secondary minerals are epidote, chlorite and local calcite.  Plagioclase is moderately sericitized.|16-MAY-23
1018|Bamboo Springs Adamellite|Relationships and boundaries|The Bamboo Springs Adamellite has fairly sharp intrusive contacts with the surrounding medium even-grained migmatitic biotite granodiorite with abundant xenoliths of the country rock particularly near the margin.  At the eastern margin, the pluton intrudes Archaean greenstones.  Remobilized migmatitic medium to coarse-grained biotite adamellite occurring to the northeast of the Adamellite contains medium to coarse-grained porphyritic biotite adamellite xenoliths which may have been derived from the Bamboo Springs.  The younger jCoondina Adamellite has a sharp intrusive contact with the Bamboo Springs Adamellite.  These are also partly faulted into contact with each other.  North-northeast-trending Lower Proterozoic dolerite dykes intrude the pluton.|16-MAY-23
1018|Bamboo Springs Adamellite|Structure and Metamorphism|The pluton may be connected at depth with similar porphyritic biotite adamellite intruded as a small mass within the greenstones to the east of the main mass.|16-MAY-23
1018|Bamboo Springs Adamellite|Age reasons|Archaean|16-MAY-23
1597|Big Spring Member|Name source|Big Spring Bore, east Oscar Plateau.|16-MAY-23
1597|Big Spring Member|Unit history|Informally named Big Spring Member by Read (1973b).|16-MAY-23
1597|Big Spring Member|Type section locality|Representative Section: In bed of north-east flowing creek adjacent to Big Spring Bore, east Oscar Plateau (N 2769600 yds; E 328800 yds to N 2767800 yds; E 328200 yds); for detailed stratigraphic section see Read (1973b, Fig. 4).|16-MAY-23
1597|Big Spring Member|Thickness range|Probably thickest in Napier Range area but thickness difficult to measure due to poor exposure.  Over 200 m thick in east Oscar Plateau area.  Thins south and west to less than 15 m in the Oscar, Pillara and Emanuel Ranges.|16-MAY-23
1597|Big Spring Member|Lithology|Consists of interbedded sandstone, red and green siltstone and shale and very minor carbonate horizons.|16-MAY-23
1597|Big Spring Member|Relationships and boundaries|Basal unit of the Pillara Formation; unconformably overlies Precambrian rocks throughout most of the area; locally it unconformably overlies Ordovician rocks in the Emanuel Range.  Top placed at first occurrence of stromatoporoid-bearing limestones and interbedded terrigenous sediments of the Red Bull Member.|16-MAY-23
1597|Big Spring Member|Age reasons|Givetian to lowermost Frasnian|16-MAY-23
1597|Big Spring Member|Proposed publication|Bull. Can. Petrol. Geol., v.21, p.344-394.|16-MAY-23
1781|Black Flag Beds|Name source|Black Flag townsite|16-MAY-23
1781|Black Flag Beds|Unit history|Talbot (1934, p2) first proposed the name "Balck Flag Series" for the apparently conformable succession of sandstone, shale, tuff ,agglomerate and acidic lava which crop out in the vicinity of Kalgoorlie, Kurrawang Lakes and Black Flag. Gustafson and Miller (1937) used the same name for the slates, tuffs and grits which overlie the Golden Mile Dolerite at Kalgoorlie. Forman (1937, p17) used the term "Black Flag - Tuffaceous Series" for the same group of rocks described by Talbot.|16-MAY-23
1781|Black Flag Beds|Type section locality|1.5 miles south of Black Flag townsite (30deg33'30" S, 121deg14'45" E)|16-MAY-23
1781|Black Flag Beds|Extent|A broad belt approximately four miles east of the Kalgoorlie-Boulder line of greenstones and extending south at least as far as Feysville (16 miles SSE of Kalgoorlie). Also occurs 1.5 miles west of Kalgoorlie in a belt which extends south, at least as far as Mt Hunt (6 miles S of Kalgoorlie). This western belt is probably continuous with rocks of similar lithology exposed near the Black Flag townsite, 18 miles northwest of Kalgoorlie.|16-MAY-23
1781|Black Flag Beds|General description|Outcrop pattern: Broad, flat exposures in low-lying areas, especially adjacent to salt lakes.|16-MAY-23
1781|Black Flag Beds|Thickness range|Approx 10, 000 feet thick [~3050 m]|16-MAY-23
1781|Black Flag Beds|Lithology|Tuffs, agglomerates, slates, shales, sandstones, and acidic lavas. Drilling south of the Golden Mile indicates that the base of the unit at this locality is marked by slate which is overlain by dominantly tuffaceous and agglomeratic rocks.|16-MAY-23
1781|Black Flag Beds|Relationships and boundaries|Conformably overlies Golden Mile Dolerite. This rock unit will probably be raised to the status of Group when more detailed mapping is carried out and the constituent formations are defined.|16-MAY-23
1781|Black Flag Beds|Age reasons|Archaean|16-MAY-23
1781|Black Flag Beds|Defn author|Unknown, but likely to have been either GSWA geologists, around 1971, or R.W. Woodall, who first published a description of the unit in 1965.|16-MAY-23
1781|Black Flag Beds|Comments|This definition was noted in the Stratigraphic Lexicon card files (pre-ASUD data) and found in the BMR Technical file for the Kalgoorlie 1:250 000 sheet area,  with 6 others. They were found between two documents from mid-1971. This definition was added to the digital database in October 2012|16-MAY-23
1781|Black Flag Beds|References| **WOODALL, R.W. 1965 Structure of the Kalgoorlie goldfield. IN Geology of Australian Ore Deposits. Eighth Commonwealth Mining and Metallurgical Congress, Australia & New Zealand, 1965. Publications Vol 1, 71-79.   **TALBOT, H.W.B. 1934 The country north and west from Kalgoorlie, Western Mining Corporation Technical Report No. 72T/1 (unpublished).   **GUSTAFSON, J.K. , Miller, F.S. 1937 Kalgoorlie geology reinterpreted, Proc. Aust.Inst. Min. Met., No. 106, 93-125.   **FORMAN, F.G. 1937 A contribution to our knowledge of the Precambrian successions in some parts of Western Australia, J. Royal Soc. W.A. 17-27.|16-MAY-23
2068|Boee Beds|Name source|Boee Pool 19o10'45"E, 128o07'E, Billiluna 1:250 000 Sheet area, WA|16-MAY-23
2068|Boee Beds|Unit history|Previously mapped as Kearney Beds (Wells 1962, Casey and Wells 1964).|16-MAY-23
2068|Boee Beds|Type section locality|Reference Area: The maximum thickness of 350 m measured north-northwest from 19o24'40"S, 128o2'25"E.  Here 120 m of even-grained sublithic arenite is separated by sand plain, a few hundred metres wide, from overlying conglomeratic arenite that passes up into coarse, very poorly sorted conglomerate containing boulders of quartzite up to 30 cm across.|16-MAY-23
2068|Boee Beds|Extent|0.5-5 km East of the Peterson Range, between latitudes 19o23' and 19o30'S, Billiluna 1:250 000 Sheet area, WA|16-MAY-23
2068|Boee Beds|Thickness range|About 350 m|16-MAY-23
2068|Boee Beds|Lithology|Medium to fine-grained brown or cream sublithic arenite.  Medium bedded showing some cross-bedding and some layers with shale or clay pellets.  Conglomerate locally.|16-MAY-23
2068|Boee Beds|Relationships and boundaries|Contacts with other units not exposed. In the north the beds appear to overlie the Jawilga Beds.|16-MAY-23
2068|Boee Beds|Age reasons|Carpentarian or Adelaidean|16-MAY-23
24197|Bridget Adamellite|Name source|Bridget Creek'; grid referenace 328283 to 329293, Nullagine 1:250 000 Sheet area.|16-MAY-23
24197|Bridget Adamellite|Type section locality|2 km North East of Bridget Creek - Nullagine River confluence.|16-MAY-23
24197|Bridget Adamellite|Extent|15 km2 between Bridget Creek and the Cooke Creek Mining Centre (338298)|16-MAY-23
24197|Bridget Adamellite|Lithology|Hornblende adamellite to hornblende-quartz monzonite. Large amphibole laths up to 1 cm long give the rock a distianctive speckled appearance.|16-MAY-23
24197|Bridget Adamellite|Relationships and boundaries|Intrudes Archaean metasedimentary rocks of the Mosquito Creek Formation (Hickman, in prep.).|16-MAY-23
24197|Bridget Adamellite|Age reasons|Similar hornblende adamellite plugs intrude the Fortescue Group further north showing the rock to be Proterozoic or even younger in age (Hickman, in prep.).   (Comment:  Rather a sweeping generalisation which may be true but is unproven for this exposure.  MM Johnstone)|16-MAY-23
3559|Capricorn Member|Name source|The Capricorn Formation is a name used by Daniels (1968) for units then considered to be younger than the Ashburton Formation.  The name is here used as Capricorn Member and included in the Ashburton Formation (de la Hunty, 1965) of the redefined Wyloo Group (of Trendall, 1979).  It includes the units previously mapped as Capricorn Formation. The Capricorn Member occurs on the Turee Creek Sheet area and extends westwards on the Edmond Sheet area.  On the former it follows about the Ashburton River outcropping on both sides, and includes the Capricorn Ranges. It occurs essentially below but interfingers extensively to the north with the Mininer Turbidite Member (new name) and overlies, to the south, Wandarry Shale Member (new name). The Capricorn Member is estimated to be at least 6000 m of essentially silty shales but contains sandstones, conglomerates and separate turbidite cycles as well as sandstone, BIF, and volcanic rafts and slumped masses.  It is distinguished from the underlying Wandarry Shale Member by the first appearance of sandstones and allochthonous or parautochthonous units, and from the Mininer Turbidite Member by the first appearance of continuous turbidite cycles.  No type section was established.|16-MAY-23
3559|Capricorn Member|Proposed publication|Aust. CSIRO Inst. Earth Res. Rept No. FP 22.|16-MAY-23
24211|Carbana Pool Adamellite|Name source|Carbana Pool, Marble Bar 1:250 000 Sheet area (M.G.R. 277 308).|16-MAY-23
24211|Carbana Pool Adamellite|Type section locality|The pluton is well exposed around Carbana Pool.  Access is by fair quality station and mining tracks.|16-MAY-23
24211|Carbana Pool Adamellite|Extent|The Carbana Pool Adamellite forms a crescent-shaped mass in the Corunna Downs Batholith.  It is concave towards the northwest, and crops out over an area of 195 km2 between latitude 21o23'S and 21o42'S, and longitudes 119o45'E and 120o00'E (see Fig. 1).  A small portion along the northeast margin occurs on the adjacent Nullagine 1:250 000 Sheet.|16-MAY-23
24211|Carbana Pool Adamellite|Lithology|Carbana Pool Adamellite is a foliated medium to coarse-grained porphyritic biotite adamellite and hornblende biotite adamellite.  Microcline phenocrysts with simple or polysynthetic twinning contain inclusions of quartz, biotite and albite-rimmed plagioclase.  Subordinate generally poorly twinned plagioclase phenocrysts are also present.  In the northeastern portion of the pluton these are albite and appear to have replaced microcline, possibly due to soda-metasomatism.  The groundmass is allotriomorphic granular textured with microcline, oligoclase, quartz and minor biotite and horneblende.  Oligoclase is fresh to extensively sericitized.  Accessory minerals are sphene, magnetite, apatite, allanite and zircon.  Zircon locally forms crystals up to 1 mm long.  Secondary minerals are chlorite, epidote, muscovite, and calcite.  Prehnite and clinozoizite are locally present in the southern portion of the pluton.  Biotite is partly chloritized and some hornblende is pseudomorphed by epidote.  In the southern portion, local metamorphism of the pluton is indicated by a granofels texture with relic microcline and albite rimmed plagioclase phenocrysts, and porphyroblastic hornblende.  The metamorphism may be due to nearby dolerite dykes.|16-MAY-23
24211|Carbana Pool Adamellite|Relationships and boundaries|The Carbana Pool Adamellite intrudes the older foliated and migmatitic granodiorite and tonalite of the Corunna Downs Batholith, and the Archaean greenstones to the eastern margin of the Batholith.  The Adamellite has sharp intrusive contacts against the younger Mondana Adamellite.|16-MAY-23
24211|Carbana Pool Adamellite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, WA: West. Australia Geol. Survey Rec 1974/20 West. Australia Geol. Survey Ann. Rept 1974|16-MAY-23
4051|Chuall Beds|Name source|Chaull Pool, 19o10'S, 128o09'30"E.  Billiluna 1:250 000 Sheet area, WA.|16-MAY-23
4051|Chuall Beds|Unit history|Previously mapped as Gardiner Beds (Wells 1962, Casey & Wells 1964).|16-MAY-23
4051|Chuall Beds|Type section locality|4 km southeast of Sturt Creek homestead, Billiluna 1:250 000 Sheet area, above lithologies occur here, dipping 0-10o.|16-MAY-23
4051|Chuall Beds|Extent|Immediately southeast of Sturt Creek homestead, north central part of Billiluna 1:250 000 Sheet area, WA.|16-MAY-23
4051|Chuall Beds|Thickness range|Maximum exposed about 140 m, in reference area.|16-MAY-23
4051|Chuall Beds|Lithology|Clayey and micaceous quartzose to lithic sandstone; fine to medium grained, thin-bedded, many pellaty bands, cross-bedded.|16-MAY-23
4051|Chuall Beds|Relationships and boundaries|Inferred to be unconformable on adjacent Proterozoic units though contacts not exposed.|16-MAY-23
4051|Chuall Beds|Age reasons|Probably Palaeozoic|16-MAY-23
4485|Cooglegong Adamellite|Name source|Cooglegong Creek (M.G.R. 224 304) Marble Bar 1:250 000 Sheet area.|16-MAY-23
4485|Cooglegong Adamellite|Type section locality|The pluton is well exposed along the Cooglegong Creek, about 10 km southeast from Spear Hill with access by track from the main Marble Bar - Wittenoom Road, opposite Spear Hill.|16-MAY-23
4485|Cooglegong Adamellite|Extent|The Cooglegong Adamellite occurs in the Shaw Batholith, between latitudes 21o34'S and 21o48'S and longitudes 119o18'E and 119o38'E, as a broad irregular band extending east-west with a prominent projection towards the southeast, and encloses two large masses of migmatite (see Fig. 1).  The unit crops out over an area of 360 km2.|16-MAY-23
4485|Cooglegong Adamellite|Lithology|The rock is a medium to coarse-grained, poorly foliated porphyritic biotite adamellite with microcline always close to twice the plagioclase content.  Microcline is usually micro-perthitic and in porphyritic specimens large microcline phenocrysts are commonly mantled by plagioclase.  Plagioclase has an average composition of calcic oligoclase (An26 for N=22) ranging from oligoclase (An20) to sodic andesine (An31). Myrmekite occurs in small amounts but locally forms a significant component of the rock.  The northern margin of the pluton is locally granophyric.  Biotite is extensively chloritized and forms only a small proportion of the rock.  Zircon, apatite and opaque iron oxide are constant accessory minerals.  Sphene and allanite and rare stipnomelane are locally present. Apart from chlorite, alteration has produced muscovite and epidote throughout the rock.  Fluorite is usually found as small blebs associated with chlorite. The Adamellite is well jointed, and is generally massive to poorly foliated, particularly away from the margins.  Near the Black Range dolerite, a strong foliation is exhibited by feldspar, micas and quartz due to shearing.  Xenoliths of the surrounding medium-grained foliated or migmatitic granodiorite are distributed throughout the pluton but are most notable near the northern margin and near Eleys mining centre.  The unit crops out in rocky ridges and tors over most of its area. The unit and associated cassiterite deposits are described in much greater detail, including chemical analyses by Blockley (1970, 1973 and in prep.)|16-MAY-23
4485|Cooglegong Adamellite|Relationships and boundaries|The boundary between the younger Cooglegong Adamellite intrusion and surrounding older migmatites and foliated granodiorite, and older porphyritic adamellite (Eley Adamellite) are generally sharp and distinctive. The Cooglegong Adamellite is intruded by Archaean dacite and rhyolite dykes and Late Proterozoic dolerite dykes.  There are numerous faults some of which are quartz-filled.|16-MAY-23
4485|Cooglegong Adamellite|Structure and Metamorphism|The pluton exhibits little or no metamorphism, and granophyric textures are present in parts of the rock.  It is considered to represent a post-tectonic intrusion derived by remobilization and differentiation of the migmatites and emplaced at a high structural level with sharp contacts and numerous associated pegmatites intruding the surrounding country rock.  A structural connection with the very similar Spear Hill Adamellite may exist in depth (see Blockley, in prep.).|16-MAY-23
4485|Cooglegong Adamellite|Age reasons|Archaean.  Samples collected from near the watergap in the Black Range cut by Cooglegong Creek (M.G.R. 226 303) yielded a preliminary age of 2602 + 132 m.y. (de Laeter, pers. Comm.) with an initial 87Sr/86Sr ratio of 0.7310 + 0.029.|16-MAY-23
4606|Coondina Adamellite|Name source|Coondina Pool, on the Western Shaw River, Marble Bar 1:250 000 Sheet area (M.G.R. 218 272)|16-MAY-23
4606|Coondina Adamellite|Type section locality|The pluton is well exposed along a track from Coondina mining centre proceeding south next to the Western Shaw, and is also well exposed south of Garden Creek.|16-MAY-23
4606|Coondina Adamellite|Extent|The Coondina Adamellite occurs in the Shaw Batholith, between latitudes 21o52'S and 21o59'S, and longitudes 119o16'E and 119o25'E, as an irregularly-shaped mass cropping out over an area of 50 km2 (See Fig. 1).|16-MAY-23
4606|Coondina Adamellite|Lithology|The unit is a medium to coarse, equigranular, massive biotite adamellite with subequal microcline and calcic oligoclase, and chloritized biotite.  There is accessory zircon and fluorite and rare sphene, opaque iron oxides and allanite.  Plagioclase is sericitized and some perthite is partially replaced by muscovite fans.  Some secondary epidote is present.  The eastern portion of the pluton crops out as well jointed, low, rocky ridges but the western portion is partly obscured by thin colluvial sand deposits.|16-MAY-23
4606|Coondina Adamellite|Relationships and boundaries|The boundaries between the older greenstones, foliated and migmatitic granodiorite and Bamboo Springs Adamellite, and the younger, intrusive Coondian Adamellite are generally sharp and distinctive.  The Coondina Adamellite is intruded by an Archaean granitic dyke and the Lower Proterozoic Black Range dolerite.|16-MAY-23
4606|Coondina Adamellite|Age reasons|Archaean|16-MAY-23
75887|Corner Well Gabbro|Name source|Corner Well, 28º 33' S 118º 26' E|16-MAY-23
75887|Corner Well Gabbro|Unit history|Corner Well intrusion (Ahmat, 1986)|16-MAY-23
75887|Corner Well Gabbro|Geomorphic expression|outcrop is good, forming a raised area and some curved ridges are present on a large scale.|16-MAY-23
75887|Corner Well Gabbro|Type section locality| -28.539250 S, 118.477390 E, 500m north of Corner Well. Easy access on farmers'  tracks, weather permitting.|16-MAY-23
75887|Corner Well Gabbro|Description at type locality|Modally layered olivine gabbro grading into olivine gabbronorite interlayered with lherzolite, dunite, pyroxenite, and minor anorthosite; metamorphosed|16-MAY-23
75887|Corner Well Gabbro|Extent|pipe-shaped intrusions occur within the central part of the Windimurra Igneous Complex and extend onto the Challa mapsheet ~ 10 km to the north of the type locality.|16-MAY-23
75887|Corner Well Gabbro|General description|Igneous layers dip inwards in a concentric fashion making a 0.2 - 2 km diameter circular map feature.|16-MAY-23
75887|Corner Well Gabbro|Thickness range|Total thickness unknown. >300m.|16-MAY-23
75887|Corner Well Gabbro|Lithology|olivine gabbro grading into olivine gabbronorite interlayered with lherzolite, dunite, pyroxenite, and minor anorthosite on a decametre scale. Predominantly gabbroic rocks.|16-MAY-23
75887|Corner Well Gabbro|Depositional environment|Genesis: The composition reveals similarity with Windimurra Igneous Complex. Grainsize indicates a slow cooling, possibly indicating that the Windimurra Igneous Complex had not cooled completely as the phase intruded. There is a geochemical affinity with the Windimurra Igneous Complex.|16-MAY-23
75887|Corner Well Gabbro|Relationships and boundaries|Intrusive contact where melanocratic Corner Well gabbros intrude into leucogabbros of the lower zone of the Windimurra Igneous Complex. Contact not exposed at surface.|16-MAY-23
75887|Corner Well Gabbro|Identifying features|To distinguish from the host rocks of the lower zone of the Windimurra Igneous Complex, the Corner Well Gabbro has Clinopyroxene and orthopyroxene cumulate layers, a more layered appearance on a 1-10m scale and more abundant melanocratic rocks.|16-MAY-23
75887|Corner Well Gabbro|Structure and Metamorphism|Igneous layers contain modal layering of pyroxene and plagioclase crystals showing laminar crystal orientation features, orthocumulate and mesocumulate textures. Igneous layers dip at approximately 30° in from the margins of the intrusions. Greenschist-lower amphibolites facies metamorphism is common and minor shear zones are present <1m wide.|16-MAY-23
75887|Corner Well Gabbro|Age reasons| 2813 +/- 3 Ma, U-Pb zircon age of Windimurra Igneous Complex (Wingate et al. in prep).|16-MAY-23
75887|Corner Well Gabbro|Correlations|correlated with Windimurra Igneous Complex due to similar lithology and geochemistry.|16-MAY-23
75887|Corner Well Gabbro|Geophysical Expression| A weak circular magnetic high is apparent.|16-MAY-23
75887|Corner Well Gabbro|Geochemistry|Bulk geochemistry reveals an anhydrous komatiitic- basalt composition with primitive mantle affinity. LREE enrichment occurs in the most fractionated anorthosites.|16-MAY-23
75887|Corner Well Gabbro|Defn author|Dr Tim Ivanic, GSWA    23-FEB-2011|16-MAY-23
75887|Corner Well Gabbro|References|**AHMAT, AL 1986, Petrology, structure, regional geology and age of the gabbroic Windimurra complex, Western Australia: University of Western Australia, Perth, Western Australia, PhD thesis (unpublished), 279p.    **IVANIC, TJ, in prep, Coolamaninu, WA Sheet 2540, Geological Survey of Western Australia, 1: 100 000 Geological Series.     **IVANIC, T. J. , Wingate, M. T. D. , Kirkland, C. L. , Van Kranendonk, M. J. and Wyche, S.(2010) 'Age and significance of voluminous mafic-ultramafic magmatic events in the Murchison Domain, Yilgarn Craton', Australian Journal of Earth Sciences, 57: 5, 597 - 614.|16-MAY-23
24232|Crispin Conglomerate|Name source|Saint Crispin Gold Mine (Abn) (25o42'S, 118o50'E), Peak Hill 1:250 000.|16-MAY-23
24232|Crispin Conglomerate|Type section locality|5 km south of Peak Hill Mine|16-MAY-23
24232|Crispin Conglomerate|Extent|From a point 5 km south of Peak Hill Mine, eastward to vicinity of Saint Crispin Mine.|16-MAY-23
24232|Crispin Conglomerate|Thickness range|200 metres|16-MAY-23
24232|Crispin Conglomerate|Lithology|Boulder conglomerate with matrix of schistose sericitic grit.|16-MAY-23
24232|Crispin Conglomerate|Relationships and boundaries|Unconformably overlie Peak Hill Metamorphic Suite; forms basal formation of Glengarry Group in Peak Hill area.  Lateral equivalent of Juderina Sandstone.|16-MAY-23
24232|Crispin Conglomerate|Age reasons|Proterozoic - probably 2.0-1.8 b.y.|16-MAY-23
5368|Denison Beds|Name source|Denison Range, Billiluna 1:250 000 Sheet area, WA|16-MAY-23
5368|Denison Beds|Unit history|Previously mapped as Gardiner Beds (Wells 1962, Casey & Wells 1964)|16-MAY-23
5368|Denison Beds|Type section locality|The Denison Range, south of Pyramid Hill.  Here a few metres of thin bedded, sublithic arenite with abundant shale pellets overlies about 15 m of medium grained quartz arenite, cross-bedded, ripple marked surfaces abundant, and beds 1 cm-1 m thick.  This overlies about 10 m of thick-bedded quartz arenite showing disturbed cross-bedding.|16-MAY-23
5368|Denison Beds|Extent|Denison Range, Billiluna 1:250 000 Sheet area, WA.|16-MAY-23
5368|Denison Beds|Thickness range|About 30 cm|16-MAY-23
5368|Denison Beds|Lithology|Quartz arenite, cross-bedded, ripple-marked.  Sublithic arenite with abundant shale pellets.|16-MAY-23
5368|Denison Beds|Relationships and boundaries|Overlie Pindar Beds, probably unconformably.  Faulted against Jawilga Beds.|16-MAY-23
5368|Denison Beds|Age reasons|Carpentarian or Adelaidean|16-MAY-23
5368|Denison Beds|Proposed publication|Royal Society of W.A. Journal|16-MAY-23
5368|Denison Beds|First Reference|79/00475|16-MAY-23
5368|Denison Beds|Name first published by|Blake D.H., Yeates A.N., Passmore V.L., Hodgson I.M., Walton D.G., Muhling P.G., Crowe R.W.A., 1977|16-MAY-23
74167|Dodonea Carbonate Member|Name source|Dodonea 1 petroleum exploration well (19° 23' 6.15"S 125° 9' 43.35"E, Crossland 1:250 000 map sheet), in which the member is intersected close to the type and reference sections|16-MAY-23
74167|Dodonea Carbonate Member|Unit history|Previously referred to as the "lower carbonate member" (Lehmann, 1984).|16-MAY-23
74167|Dodonea Carbonate Member|Constituents|None.|16-MAY-23
74167|Dodonea Carbonate Member|Geomorphic expression|Sub-surface only.|16-MAY-23
74167|Dodonea Carbonate Member|Type section locality|The interval 596-613 m in Barbwire 1 (19° 10' 33.32"S 125° 1' 4.01"E; Crossland 1:250 000 map sheet), as nominated by Lehmann (1984) for the "lower carbonate member". Reference localities: Because the type section is not cored, the fully cored intervals 503.95 - 524.23 m in Acacia 1 (19° 19' 44.95"S 124° 59' 43.66"E) and 1002-1015 m Boab 1 (19° 34' 36.95"S 125° 8' 49.66"E) are nominated as reference sections. Core is stored in Geological Survey of Western Australia Perth core library.|16-MAY-23
74167|Dodonea Carbonate Member|Description at type locality|Off-white to pale green-grey finely crystalline dolomite; hard, brittle, pyritic, non-porous, calcite veining.|16-MAY-23
74167|Dodonea Carbonate Member|Extent|Best developed on the Barbwire Terrace, eastern Broome Platform and Crossland Platform of the Canning Basin, Western Australia. Absent in western and southern parts of the basin. Only known from the sub-surface.|16-MAY-23
74167|Dodonea Carbonate Member|Thickness range|17 m at type section, 20.28 m and 13 m at the Acacia 1 and Boab 1 reference sections, respectively. These thicknesses are typical for the unit throughout its distribution|16-MAY-23
74167|Dodonea Carbonate Member|Lithology|Dominated by massive carbonate, most commonly pale grey to beige dolomite, but including limestone in some wells. Grades to dolomitic or calcareous mudstone at the top. Minor sandy component in some wells.|16-MAY-23
74167|Dodonea Carbonate Member|Depositional environment|Shallow marginal marine, probably lagoonal.|16-MAY-23
74167|Dodonea Carbonate Member|Fossils|Conodonts and scelecodonts recovered from drill core from Boab 1 and Acacia 1 (Nicoll et al., 1994).|16-MAY-23
74167|Dodonea Carbonate Member|Diastems or hiatuses|None known.|16-MAY-23
74167|Dodonea Carbonate Member|Relationships and boundaries|Parent unit is Worral Formation. Overlies the Sahara Formation (Carribuddy Group) with apparent conformity. Sharply, but probably conformably overlain by the Elsa Sandstone Member at the type section and in nearby wells. Appears to interfinger with the Elsa Sandstone Member to the west|16-MAY-23
74167|Dodonea Carbonate Member|Age reasons|The conodont Ozarkodina hassi provides a Llandovery (Early Silurian) age (Nicoll et al., 1994). The earlier report of a Devonian ostracod and foraminifera fauna in this unit in Boab 1 (Jones and Nicoll, 1982; Nicoll et al., 1994) is no longer valid as the sample depth has been shown to be in error|16-MAY-23
74167|Dodonea Carbonate Member|Correlations|Appears to interfinger with the Elsa Sandstone Member to the west.|16-MAY-23
74167|Dodonea Carbonate Member|References|Lehmann, PR, 1984, The stratigraphy, palaeogeography and petroleum potential of the Lower to lower Upper Devonian sequence in the Canning Basin, in The Canning Basin, WA, edited by PG Purcell: Geological Society of Australia and Petroleum Exploration Society of Australia; Canning Basin Symposium, Perth, WA, 1984, Proceedings, p. 253-275.  **Nicoll, RS, Romine, KK, and Watson, ST, 1994, Early Silurian (Llandovery) Conodonts from the Barbwire Terrace, Canning Basin, Western Australia: AGSO Journal of Australian Geology and Geophysics, v. 15, p. 247-255.  **Jones, PJ, and Nicoll, RS, 1982, Conodont and ostracod faunas from WMC Boab No. 1, Canning Basin, WA, in BMR, Australia, Professional Opinion, Cont. Geol 82.002, in S Watson, Boab No. 1 well completion report, Canning Basin, appendix II: Geological Survey of Western Australia, Statutory petroleum exploration report, S1848 V1 A1 (unpublished).|16-MAY-23
74167|Dodonea Carbonate Member|Parent|Worral Formation|16-MAY-23
24251|Doolgunna Arkose|Name source|Doolgunna Homestead, Peak Hill 1:250 000|16-MAY-23
24251|Doolgunna Arkose|Type section locality|14 km SE of Ruby Well Find (25o59'S, 118o54'E)|16-MAY-23
24251|Doolgunna Arkose|Extent|Throughout western part of Nabberu Basin|16-MAY-23
24251|Doolgunna Arkose|Thickness range|5000 m, thinning to 200 m|16-MAY-23
24251|Doolgunna Arkose|Lithology|Quartz-plagioclase-microcline arenite with some mudstone|16-MAY-23
24251|Doolgunna Arkose|Relationships and boundaries|Conformable between Juderina Sandstone and Karolundi Formation|16-MAY-23
24251|Doolgunna Arkose|Age reasons|Proterozoic - probably 2.0 - 1.8 b.y.|16-MAY-23
24251|Doolgunna Arkose|Proposed publication|Western Australia Geological Survey Annual Report for 1978 (Pub 1979)|16-MAY-23
24251|Doolgunna Arkose|Defn approved by|Western Australia Sub-Committee|16-MAY-23
28162|Dudawa Beds|Name source|Dudawa Estate on the Morawa-Arrino road about 16 km southwest of the Billeranga Hills.  The type area lies just east of this estate (19o23'S, 115o46'E). Perenjori 1:250 000 Sheet area.|16-MAY-23
28162|Dudawa Beds|Type section locality|No type section has been designated because of the poorness of exposure.|16-MAY-23
28162|Dudawa Beds|Extent|From just west of the Billeranga Hills to near the Darling Fault, and as far south as the Coodawa talc deposit, 9 km east-northeast of Three Springs.|16-MAY-23
28162|Dudawa Beds|Thickness range|The exposed thickness of the Dudawa Beds is unknown because outcrops are poor and discontinuous and no accurate sections have been measured.  Arriens and Lalor (1959) conservatively estimated that the beds are at least 150 m thick.|16-MAY-23
28162|Dudawa Beds|Lithology|Predominantly chert and orthoquartzite, with minor dolomite and a thin basal unit of sandstone.|16-MAY-23
28162|Dudawa Beds|Relationships and boundaries|A disconformable relationship with the underlying Billaranga Group is inferred from the presence in the basal sandstone of pebbles of black flint thought to have been derived from the underlying Campbell Sandstone (the highest unit of the group).  The top of the Dudawa Beds is not exposed.|16-MAY-23
28162|Dudawa Beds|Age reasons|The only fossils known are algal stromatolites of Collenia type.  A Middle or Late Proterozoic age for the unit seems probable.|16-MAY-23
28162|Dudawa Beds|Proposed publication|Geology of Western Australia; West. Aust. Geol Survey, Memoir 2, in press|16-MAY-23
28162|Dudawa Beds|Comments|High quality talc is being mined from the Dudawa Beds at Coodawa, 9 km east-northeast of Three Springs.|16-MAY-23
28162|Dudawa Beds|Defn approved by|Western Australia Sub-Committee|16-MAY-23
28162|Dudawa Beds|Proposer|Low G.H.|16-MAY-23
28162|Dudawa Beds|Resdate|15-JAN-1975|16-MAY-23
24264|Eley Adamellite|Name source|Eley mining centre, Marble Bar 1:250 000 Sheet area (M.G.R. 226 292).|16-MAY-23
24264|Eley Adamellite|Type section locality|The Eley Adamellite is well exposed west and southwest of Eley mining centre. Access is by fair quality mining tracks from Hillside homestead.|16-MAY-23
24264|Eley Adamellite|Extent|The Eley Adamellite has an irregular crescent shape extending from north of Hillside homestead eastwards to Eley mining centre and southwards to east of Hillside homestead (see Fig. 1).  The pluton crops out as rugged hills and ridges, with only minor obscuring Quaternary sand, over an area of 120 km2, between latitudes 21o37'S and 21o50'S, and longitudes 119o24'E and 119o33'E.|16-MAY-23
24264|Eley Adamellite|Lithology|Eley Adamellite is a medium to coarse-grained porphyritic biotite adamellite.  A moderate to prominent foliation is formed by mafic schlieren and alignment of phenocrysts and feldspar, biotite and locally quartz grains in the groundmass.  There are abundant xenoliths of medium even-grained migmatitic biotite granodiorite and rare amphbibolite.   Microcline phenocrysts range in size up to 1.5 x 3 cm.  These are well-twinned with inclusions of quartz, plagioclase and biotite and are set in an allotriomorphic granular textured groundmass of fresh sodic oligoclase with myrmekite, microcline, quartz, biotite and minor sphene.  Oligoclase exceeds microcline.  Accessory minerals are magnetite, apatite and rare zircon.  There is secondary chlorite and epidote.  In the western portion, near the margin, the phenocrysts are of oligoclase set in a microcline-oligoclase groundmass.|16-MAY-23
24264|Eley Adamellite|Relationships and boundaries|The Eley Adamellite intrudes and contains abundant xenoliths of the surrounding migmatitic biotite granodiorite.  The boundary between them is a broad transitional zone, particularly in the area adjacent to the concave side of the pluton where migmatite is intruded by veins of porphyritic adamellite which progress in width towards the pluton, grading through a zone in which the country rock is disrupted and progressively disoriented passing into the main mass of the Adamellite.  Hence the boundaries shown in Fig. 1 are only approximate. Boundaries of the southern portion of the mass are sharper.  The pluton is intruded by the Cooglegong Adamellite and the margins are generally sharp.  The Lower Proterozoic Black Range Dolerite intrudes the pluton, trending in a north-northwest direction.  The pluton is strongly jointed and has quartz veins along fault zones.|16-MAY-23
24264|Eley Adamellite|Structure and Metamorphism|Smaller porphyritic medium to coarse-grained biotite adamellite plutons southwest and west of Eley Adamellite are probably cogenetic and some of those closest to it may be connected in depth since the broad mixed zone of migmatite and porphyritic adamellite on the southwest side of the pluton suggests that it plunges in that direction.|16-MAY-23
24264|Eley Adamellite|Age reasons|Archaean|16-MAY-23
24264|Eley Adamellite|Defn approved by|Western Australia Sub-Committee|16-MAY-23
24264|Eley Adamellite|First Reference|82/22443 - First indexed but publ. 1980.|16-MAY-23
24264|Eley Adamellite|Resdate|15-JAN-1975|16-MAY-23
24264|Eley Adamellite|Reserved? Yes/No|Y|16-MAY-23
25916|Friendly Creek Formation|Name source|Friendly Creek, tributary of Yule River.  Approximate coordinates 21o15'S, 118o22'E, Pyramid 1:250 000 Sheet area.|16-MAY-23
25916|Friendly Creek Formation|Unit history|Mafic part of formation equated with Talga-Talga Subgroup of Marble Bar and Nullagine 1:250 000 Sheets, felsic portion equated with Duffer Formation of same sheets (Hickman & Lipple, in press).|16-MAY-23
25916|Friendly Creek Formation|Description at type locality|1020 metres of mafic and felsic volcanics and banded chert.  Lower 600 m sheared chloritic meta-basalts and gabbro, then 20 m banded chert followed by 600 m of felsic tuffs.  Metamorphosed to greenschist and locally amphibolite facies.|16-MAY-23
25916|Friendly Creek Formation|Extent|The formation is exposed over a strike length of 40-50 km in the NE of the Pyramid 1:250 000 Sheet area in the vicinity of the Yule River.|16-MAY-23
25916|Friendly Creek Formation|Thickness range|Range 300-1020 metres|16-MAY-23
25916|Friendly Creek Formation|Relationships and boundaries|Lowest formation of Teichmans Group. Base of formation intruded by granite.  Overlain by Hong Kong Chert.|16-MAY-23
25916|Friendly Creek Formation|Age reasons|Lower Archaean >3000 m.y.|16-MAY-23
25916|Friendly Creek Formation|Comments|Equivalent rocks in East Pilbara (Marble Bar-Nullagine area) attain much greater thicknesses than in type area in West Pilbara.|16-MAY-23
25916|Friendly Creek Formation|Reserved? Yes/No|Y|16-MAY-23
24288|Glengarry Group|Name source|Glengarry 1:250 000 Sheet WA|16-MAY-23
24288|Glengarry Group|Unit history|"Glengarry axial sequence" Bunting and others (1977) "pre-Padbury group" Elias and Williams (1977).|16-MAY-23
24288|Glengarry Group|Constituents|Juderina Sandstone, Crispin Conglomerate Doolgunna Arkose, Karalundi Formation, Narracoota Volcanics, Thaduna Greywacke, Horseshoe Formation, Labouchere Formation.|16-MAY-23
24288|Glengarry Group|Extent|Western part of Nabberu Basin in Peak Hill and Glengarry 1:250 000 Sheets|16-MAY-23
24288|Glengarry Group|Relationships and boundaries|Unconformably overlies Archaean basement, unconformably overlain by Padbury Group.|16-MAY-23
24288|Glengarry Group|Age reasons|Proterozoic, maximum age limit of 2.4 b.y. on Archaean basement and minimum age limit of 1.7 b.y. on contained metamorphic muscovite.|16-MAY-23
24288|Glengarry Group|Proposed publication|Western Australia Geological Survey Annual Report for 1978 (Pub 1979)|16-MAY-23
24288|Glengarry Group|References|70/00670|16-MAY-23
24288|Glengarry Group|Defn approved by|Western Australia Sub-Committee|16-MAY-23
24288|Glengarry Group|Defn Reference|80/20704|16-MAY-23
8047|Hannans Lake Serpentinite|Name source|From Hannans Lake, a salt lake six miles south-south-east of Kalgoorlie.|16-MAY-23
8047|Hannans Lake Serpentinite|Type section locality|The hills due east of Mt Hunt which form the western shores of Hannans Lake (30deg 50'00" S, 121deg31"00" E).|16-MAY-23
8047|Hannans Lake Serpentinite|Extent|A south-south-east trending belt extends from 2 miles south of the Golden Mile for at least a further 10 miles. A smaller area of similar trend extends north-wards from the Transcontinental Railway Cutting, 1/2 mile north-north-east of Mt Charlotte Reservoir, for at least two miles.|16-MAY-23
8047|Hannans Lake Serpentinite|General description|Outcrop pattern: Prominent hills with poorly defined strike ridges. Specimen No. 3218, collected and analysed by the Geological Survey of Western Australia, is typical of the outcrops at the type section (Bulletin 6, p75)|16-MAY-23
8047|Hannans Lake Serpentinite|Thickness range|3,000 - 5,000 feet [915 - 1525 m]|16-MAY-23
8047|Hannans Lake Serpentinite|Lithology|Massive, fine-grained greenish-black rock composed of serpentine minerals.|16-MAY-23
8047|Hannans Lake Serpentinite|Relationships and boundaries|These are the oldest exposed rocks in the Kalgoorlie district. They are conformably overlain by the Devon Consols Basalt.|16-MAY-23
8047|Hannans Lake Serpentinite|Age reasons|Archaean|16-MAY-23
8047|Hannans Lake Serpentinite|Defn author|Unknown, but likely to have been either GSWA geologists, around 1971, or R.W. Woodall, who first published a description of the unit in 1965.|16-MAY-23
8047|Hannans Lake Serpentinite|Comments|This definition was noted in the Stratigraphic Lexicon card files (pre-ASUD data) and found in the BMR Technical file for the Kalgoorlie 1:250 000 sheet area,  with 6 others. They were found between two documents from mid-1971. This definition was added to the digital database in October 2012.|16-MAY-23
8047|Hannans Lake Serpentinite|References|GSWA Bulletin No. 6.  **WOODALL, R.W. 1965 Structure of the Kalgoorlie goldfield. IN Geology of Australian Ore Deposits. Eighth Commonwealth Mining and Metallurgical Congress, Australia & New Zealand, 1965. Publications Vol 1, 71-79.   **TALBOT, H.W.B. 1934 The country north and west from Kalgoorlie, Western Mining Corporation Technical Report No. 72T/1 (unpublished).   **GUSTAFSON, J.K. , Miller, F.S. 1937 Kalgoorlie geology reinterpreted, Proc. Aust.Inst. Min. Met., No. 106, 93-125.   **FORMAN, F.G. 1937 A contribution to our knowledge of the Precambrian successions in some parts of Western Australia, J. Royal Soc. W.A. 17-27.|16-MAY-23
8326|Hidden Basin Beds|Name source|Hidden Basin, a broad depression containing Lake Wills & Lake Hazlett, Stansmore 1:250 000 Sheet area.|16-MAY-23
8326|Hidden Basin Beds|Unit history|Previously mapped as part of the Gardiner Beds (Casey & Wells, 1964)|16-MAY-23
8326|Hidden Basin Beds|Type section locality|25 km southwest of Lake Hazlett, at 21o40'S, 128o25'E.  Here 1800 m of quartz arenite and sublithic arenite is overlain by 280 m of interbedded shale, siltstone and fine sublithic arenite and 150 m of glassy quartz arenite.  The sequence dips steeply west.|16-MAY-23
8326|Hidden Basin Beds|Extent|Central part of the Stansmore 1:250 000 Sheet area, Western Australia.|16-MAY-23
8326|Hidden Basin Beds|Thickness range|Maximum thickness exposed is about 3000 m.|16-MAY-23
8326|Hidden Basin Beds|Relationships and boundaries|Overlies, possibly conformable, Erica Sandstone, but contacts with Proterozoic rock units are concealed under superficial deposits.  The unit is termed beds rather than formation because of uncertain relationships.|16-MAY-23
8326|Hidden Basin Beds|Age reasons|Probably Adelaidean.|16-MAY-23
8326|Hidden Basin Beds|First Reference| 79/00474, 79/00462|16-MAY-23
8326|Hidden Basin Beds|Name first published by|Blake D.H., Yeates A.N., Walton D.C., 1976.    Blake D.H., 1976.  |16-MAY-23
8326|Hidden Basin Beds|State(s)|WA|16-MAY-23
8455|Honeyeater Formation|Name source|Honeyeater Creek (which crosses the unit at Military Grid reference 203 346), Marble Bar 1:250 000 Sheet area.|16-MAY-23
8455|Honeyeater Formation|Type section locality|Adjacent to the Honeyeater Creek|16-MAY-23
8455|Honeyeater Formation|Extent|The Honeyeater Formation occurs in the centre of the Soanesville Syncline and the southern portion of the Lalla Rookh Syncline.|16-MAY-23
8455|Honeyeater Formation|Thickness range|0.5 km|16-MAY-23
8455|Honeyeater Formation|Lithology|The Honeyeater Formation consists of a monotonous sequence of variolitic, vesicular, pillowed basalt lavas.|16-MAY-23
8455|Honeyeater Formation|Relationships and boundaries|Conformably overlies the sedimentary rocks of the Soanesville Subgroup in the Soanvesville Syncline, and the Paddy Market Formation in the Lalla Rookh Syncline.  It is conformably overlain by the Lalla Rookh Sandstone.|16-MAY-23
8455|Honeyeater Formation|Age reasons|Archaean|16-MAY-23
8455|Honeyeater Formation|Defn author|Lipple S.L., 1975 - as Honeyeater Basalt|16-MAY-23
8455|Honeyeater Formation|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
8455|Honeyeater Formation|Defn Reference|79/02598|16-MAY-23
8455|Honeyeater Formation|Name first published by|Geological Survey of Western Australia, 1973|16-MAY-23
8671|Ima Ima Beds|Name source|Ima Ima Pool on Sturt Creek at 19o18'S, 127o53'E, Billiluna 1:250 000 Sheet area, WA|16-MAY-23
8671|Ima Ima Beds|Unit history|Mapped as Kearney Beds by Casey & Wells (1964) and as Gardiner Beds by Gemuts & Smith (1968) where they extend into the Gordon Downs 1:250 000 Sheet area.|16-MAY-23
8671|Ima Ima Beds|Type section locality|Reference area:  10 km north-northeast of Wolf Creek Meteorite Crater, where a sequence about 450 m thick dips southeast.  It consists mainly of sublithic arenite but includes thin interbeds and lenses of pebble conglomerate.|16-MAY-23
8671|Ima Ima Beds|Extent|Northwest part of Billiluna 1:250 000 Sheet area|16-MAY-23
8671|Ima Ima Beds|Thickness range|Maximum exposed is about 1000 m|16-MAY-23
8671|Ima Ima Beds|Lithology|Predominantly sandstone-medium to thin bedded, medium to coarse-grained sublithic arenite and quartz arenite, cross bedding and scattered pebbles common. Minor lenses and bands of conglomerate.  Local shearing and quartz veining.|16-MAY-23
8671|Ima Ima Beds|Relationships and boundaries|Not known, as outcrops are separated by sand plains from outcrops of other Precambrian rock units.  May be correlated with either the Carpentarian Birrindudu Group or the probably Adelaidean Redcliff Pound Group.|16-MAY-23
8671|Ima Ima Beds|Age reasons|Carpentarian or Adelaidean|16-MAY-23
8671|Ima Ima Beds|Defn approved by|Taken from xerox copy of approved def. Sent by Western Australian Sub-Committee|16-MAY-23
8671|Ima Ima Beds|Defn Reference|Described in 79/00470|16-MAY-23
8671|Ima Ima Beds|First Reference|79/00475|16-MAY-23
8671|Ima Ima Beds|Name first published by|Blake D.H., Yeates A.N., Passmore V.L., Hodgson I.M., Walter D.G., Muhling P.G., Crowe R.W.A., 1977|16-MAY-23
8890|Jawilga Beds|Name source|Jawilga Pool, 19o05'S, 128o16'40"E.  Billiluna 1:250 000 Sheet area, WA|16-MAY-23
8890|Jawilga Beds|Type section locality|Reference area: West side of the Denison Range about 2.5 km west of the northern Palm Springs, where the beds are about 130 m thick, in a narrow fault bounded slice.  Sublithic arenite and chert granule conglomerate are exposed here.|16-MAY-23
8890|Jawilga Beds|Extent|South of Sturt Creek homestead between Denison and Peterson Ranges, Billiluna 1:250 000 Sheet area, WA.|16-MAY-23
8890|Jawilga Beds|Thickness range|Maximum exposed about 130 m|16-MAY-23
8890|Jawilga Beds|Lithology|Medium to fine grained sublithic arenite; medium to thin-bedded, showing cross-bedding and ripple marks.  Chert granule pebble conglomerate.|16-MAY-23
8890|Jawilga Beds|Relationships and boundaries|Only contacts exposed are faulted.  Possibly unconformable on Denison Beds.  Possibly unconformably overlain by Boee Beds.|16-MAY-23
8890|Jawilga Beds|Age reasons|Carpentarian or Adelaidean|16-MAY-23
8890|Jawilga Beds|Defn approved by|Taken from xerox copy of approved def. Sent by Western Australian Sub-Committee|16-MAY-23
8890|Jawilga Beds|First Reference|79/00475|16-MAY-23
8890|Jawilga Beds|Name first published by|Blake D.H., Yeates A.N., Passmore V.L., Hodgson I.M., Walton D.G., Muhling P.G., Crowe R.W.A., 1977|16-MAY-23
8890|Jawilga Beds|State(s)|WA|16-MAY-23
24323|Juderina Sandstone|Name source|Juderina Bore (119o12'E, 25o53'S) Peak Hill 1:250 000 Sheet|16-MAY-23
24323|Juderina Sandstone|Type section locality|3 km north of Juderina Bore|16-MAY-23
24323|Juderina Sandstone|Extent|Around margin of Goodin Dome|16-MAY-23
24323|Juderina Sandstone|Thickness range|30 M|16-MAY-23
24323|Juderina Sandstone|Lithology|Orthoquartzitic sandstone|16-MAY-23
24323|Juderina Sandstone|Age reasons|Proterozoic - probably 2.0 - 1.8 b.y.|16-MAY-23
28205|Kangan Granite|Name source|Kangan homestead, Marble Bar 1:250 000 Sheet area (M.G.R. 1175 3615)|16-MAY-23
28205|Kangan Granite|Type section locality|The Granite is well exposed along the banks of a large creek, draining northwestwards from Numbana mine, from about 8 km and further northwest from Round Hummock. It is also well exposed from 1 km east of Round Hummock and in the area northwest of Mount Francisco. Access is by poor to fair quality mining and station tracks.|16-MAY-23
28205|Kangan Granite|Extent|The Kangan Granite forms an irregular ellipse, elongated towards the northeast and is bisected by the western margin of the Sheet area. A separate elongate mass occurs east of the Wodgina greenstones and is included in the unit. The main mass crops out over an area of 180 km2 (in the Marble Bar Sheet area) and is located south of Kangan homestead and west of Wodgina mining centre between latitudes 21o10'S and 21o23'S, and longitudes 118o30'E and 118o38'E. The eastern mass crops out over an area of about 60 km2.  See Fig. 1.|16-MAY-23
28205|Kangan Granite|Lithology|The Kangan Granite is a porphyritic, medium to coarse-grained, poorly foliated to moderately foliated, biotite granite. The texture is allotriomorphic granular and directionless. There is some myrmekite, and quartz locally appears to corrode plagioclase. Well-twinned microcline phenocrysts contain numerous inclusions of plagioclase, some of which are albite rimmed. Plagioclase is poorly to well-twinned and is variably sericitized.  It is oligoclase to sodic andesine (An26 for N=4) in composition. Biotite is generally chloritized. Some muscovite is present. There is accessory hornblende, sphene, large anhedral magnetite grains, and rare allanite. In addition to chlorite, there is secondary epidote. The unit is generally strongly outcropping and well jointed, particularly in the southern area. In the northern portion, it is locally obscured by superficial Quaternary sand.|16-MAY-23
28205|Kangan Granite|Relationships and boundaries|The Kangan Granite intrudes and contains minor xenoliths of the surrounding Archaean medium even-grained gneissic and migmatitic biotite granodiorite. The boundaries are fairly sharp. The contact between the Kangan Granite and the (?younger) Numbana Granite is generally sharp. The eastern porphyritic mass assigned to the Kangan Granite intrudes the Wodgina Archaean greenstones and is also faulted against them by a major northeast-trending fault.  The granite has sharp intrusive contacts with the (?younger) fine to medium, even-grained Nardoopiquithanna Adamellite. The Granite is intruded by west-northwest-trending dolerite dykes of Lower Proterozoic age. The pluton occurs in an area further described by Blockley (1971).|16-MAY-23
28205|Kangan Granite|Structure and Metamorphism|It seems probable that before faulting, the two masses of the Kangan Granite were connected at depth. The granite forms an irregular mass with steeply dipping margins in enclosing migmatite. A supimposed tectonic foliation parallel to the major fault direction is locally exhibited in the eastern mass by alignment of quartz and feldspar grains.|16-MAY-23
28205|Kangan Granite|Age reasons|Archaean|16-MAY-23
28205|Kangan Granite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, WA: West. Australia Geol. jSurvey Rec. 1974/20. West. Australia Geol. Survey Ann. Rept 1974|16-MAY-23
28205|Kangan Granite|Comments|84/24329 - Hickman & Lipple 1975|16-MAY-23
28205|Kangan Granite|First Reference|82/22443|16-MAY-23
28205|Kangan Granite|Name first published by|Blockley J.G., 1980 as Kangan Adamellite|16-MAY-23
9792|Koongaling Volcanics|Name source|Koongaling Hill'; grid reference 413367, Nullagine 1:250 000 Sheet area.|16-MAY-23
9792|Koongaling Volcanics|Unit history|Forms part of 'Gregory Range Granite'. (Noldart and Wyatt, 1962).|16-MAY-23
9792|Koongaling Volcanics|Type section locality|East of Ragged Hills. Easy access along road to Telfer, Paterson Range Sheet area|16-MAY-23
9792|Koongaling Volcanics|Extent|Generally 5 km wide outcrop belt on the eastern side of the Gregory Range from 20 km north of Koongaling Hill south southeast to 5 km north of Binbianna R.H. (443261) a distance of 120 km.|16-MAY-23
9792|Koongaling Volcanics|Thickness range|At least 1000 m, base not exposed.|16-MAY-23
9792|Koongaling Volcanics|Lithology|Dacite lava, tuff and agglomerate. Lava is typically porphyritic.|16-MAY-23
9792|Koongaling Volcanics|Relationships and boundaries|Conformably underlies Kylena Basalt (MacLeod and de la Hunty, 1966). Base not exposed but probably unconformably overlies Archaean granitic rocks outcropping in the desert area to the east. Forms lower part of Fortescue Group (MacLeod and others, 1963).|16-MAY-23
9792|Koongaling Volcanics|Age reasons|Lower Proterozoic, since forms part of the Fortescue Group.B9|16-MAY-23
9792|Koongaling Volcanics|Defn author|Hickman A.H., 1978|16-MAY-23
9792|Koongaling Volcanics|Proposed publication|West Australia Geological Survey 1:250 000 Geological Series Explanatory Notes (Nullagine)|16-MAY-23
9792|Koongaling Volcanics|Comments|The formation is correlated with the "Mount Roe Basalt" (Kriewaldt, 1964) but differs in being of felsic composition. Both formations contain much pyroclastic material.|16-MAY-23
9792|Koongaling Volcanics|Name first published by|DeLaeter J.R., Hickman A.H., Trendall A.F., Lewis J.D., 1977|16-MAY-23
10049|Lake George Beds|Name source|Lake George (22o37'S, 123o40'E)|16-MAY-23
10049|Lake George Beds|Unit history|Correlated with the Lampe Beds (Lowry et al, 1972) which occur farther south.|16-MAY-23
10049|Lake George Beds|Type section locality|At 22o50'00"S, 123o42'55"E, 8 km southeast of Helen Hill|16-MAY-23
10049|Lake George Beds|Extent|In the Sahara, Percival, Tabletop, Runton and Ural Sheet areas in the southern Canning Basin.|16-MAY-23
10049|Lake George Beds|Thickness range|5 m at type section but it may be thicker elsewhere.|16-MAY-23
10049|Lake George Beds|Lithology|Mainly massive poorly sorted, fine to very coarse-grained quartz wacke and granule conglomerate.|16-MAY-23
10049|Lake George Beds|Relationships and boundaries|Unconformably overlies Early Cretaceous Anketell Sandstone and is overlain by laterite which is probably mainly Tertiary in age.|16-MAY-23
10049|Lake George Beds|Age reasons|A Cretaceous to Tertiary age is assigned to the unit.|16-MAY-23
10049|Lake George Beds|Proposed publication|Annual Report Geological Survey of Western Australia for 1976|16-MAY-23
10049|Lake George Beds|Defn Reference|83/23481|16-MAY-23
10049|Lake George Beds|First Reference|79/19603|16-MAY-23
10049|Lake George Beds|Name first published by|Yeates A.N., Towner R.R., Young G.A., Walton, D.G., 1978|16-MAY-23
27458|Lake Willson Beds|Name source|Lake Willson, 19o23'S, 128o16'E, Billiluna 1:250 000 sheet area, WA|16-MAY-23
27458|Lake Willson Beds|Unit history|Previously mapped as Gardiner Beds (Wells 1962, Casey & Wells 1964).|16-MAY-23
27458|Lake Willson Beds|Type section locality|Reference area: 20 km south of Sturt Creek homestead, on track to Balgo; here about 150 m of interbedded chert and sublithic arenite dips 70o northwest.|16-MAY-23
27458|Lake Willson Beds|Extent|South of Sturt Creek homestead, between the Denison and Peterson Ranges, Billiluna 1:250 000 sheet area, WA|16-MAY-23
27458|Lake Willson Beds|Thickness range|Maximum exposed about 150 m, at reference  area.|16-MAY-23
27458|Lake Willson Beds|Lithology|Stromatolitic chert and medium to coarse grained cross-bedded sublithic arenite. Laterite capping in north.|16-MAY-23
27458|Lake Willson Beds|Relationships and boundaries|Overlain by Pindar Beds. The Lake Willson Beds is the oldest unit in the Denison Range area, being exposed in the core of a major anticline.|16-MAY-23
27458|Lake Willson Beds|Age reasons|Carpentarian or Adelaidean|16-MAY-23
27458|Lake Willson Beds|Defn approved by|Taken from xerox copy of approved def. Sent by Western Australian Sub-Committee.|16-MAY-23
27458|Lake Willson Beds|Name first published by|Blake D.H., Passmore V.L., Muhling 1977|16-MAY-23
24368|Madang Tuff Member|Name source|Madang Well.  Mt Bruce 1:250 000 Geological Sheet 1964 Edition.  Lat 22o49'S, long. 117o28'E.|16-MAY-23
24368|Madang Tuff Member|Type section locality|1 km east of Madang Well|16-MAY-23
24368|Madang Tuff Member|Extent|The unit is exposed over about 15 square kilometres in the Rocklea, Milli-Milli and Bellary domes of the Mt Bruce (SF 50, 11) and the Turee Creek (SF 50, 15) 1:250 000 sheets. It is lensoid in distribution.|16-MAY-23
24368|Madang Tuff Member|Lithology|Thickness ranges from 0 to about 130 m. The rock type is chiefly an intermediate tuff. It has vitric and lithic fragments in an andesitic to basaltic matrix, now typically composed of fine grained actinolite and chlorite with plagioclase, minor quartz, rare stilpnomelane and secondary carbonate. In rare localities, such as at the type section, the base of the tuff member is marked by a thin (2-5 m) acid accretionary lapilli tuff. On the northeastern side of the Bellary dome the tuff member contains an amygdular basaltic flow of limited extent. A characteristic feature of the tuff is the presence of rounded quartz and some microcline grains which are regarded as xenocrystic.  14 km north of Mt Bennett in the Milli-Milli dome the tuff contains large (up to 15 cm) fragments of Hardey Sandstone.  Rarely coarse layering is observed within the tuff.|16-MAY-23
24368|Madang Tuff Member|Relationships and boundaries|The tuff is a lensoid member within the Hardey Sandstone. It is conformably bounded above and below by coarse arkose.|16-MAY-23
24368|Madang Tuff Member|Age reasons|A shale within the Hardey Sandstone has been dated at 1650 m.y. by Hickman and de Laeter (1977).|16-MAY-23
24368|Madang Tuff Member|Proposed publication|Geological Survey of Western Australia, Report Series|16-MAY-23
24368|Madang Tuff Member|First Reference|86/25278 |16-MAY-23
24368|Madang Tuff Member|Name first published by|Blight D.F., 1985. Mention P13, Plate 2A-2C, Fig. 24 as Madang Tuff.  |16-MAY-23
24368|Madang Tuff Member|Proposer|Blight D.F.|16-MAY-23
11244|Marble Bar Chert|Name source|The Marble Bar (Military Grid Reference 2535 3520), Marble Bar 1:250 000 Sheet area. This is the popular name given to the chert where it crops out in the Coongan River, and from which the adjacent pool and nearby township derive their names|16-MAY-23
11244|Marble Bar Chert|Unit history|The same unit was referred to by Noldart and Whatt (1962 p. 114-116) as the Marble Bar Jaspilite. It was also described by Maitland (1908, p.19, 204).|16-MAY-23
11244|Marble Bar Chert|Type section locality|The Marble Bar, in the Coongan River, 5 km southwest of Marble Bar township.|16-MAY-23
11244|Marble Bar Chert|Extent|In the Marble Bar Belt and the Warrawoona Syncline.  Although it may occur elsewhere in the Marble Bar Sheet area, it has not been recognised.|16-MAY-23
11244|Marble Bar Chert|Thickness range|100 m|16-MAY-23
11244|Marble Bar Chert|Lithology|The Marble Bar Chert is a colourful red and white banded chert exhibiting local hydroplastic brecciation with injection veins of massive dark grey chart. The chert is illustrated by Maitland (1908, Fig. 45-48) and Noldart and Wyatt (1962, p. 108-109).|16-MAY-23
11244|Marble Bar Chert|Relationships and boundaries|The Marble Bar Chert occurs conformably within the Salgash Subgroup near the contact with the underlying Duffer Formation.|16-MAY-23
11244|Marble Bar Chert|Age reasons|Archaean|16-MAY-23
11244|Marble Bar Chert|Defn author|Lipple S.L., 1975|16-MAY-23
11244|Marble Bar Chert|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
11611|Meentheena Carbonate Member|Name source|Meentheena Homestead (Military Grid Reference 339 340)|16-MAY-23
11611|Meentheena Carbonate Member|Type section locality|Meentheena Basin, south of Tumbiana Pool on Nullagine River (no type section measured)|16-MAY-23
11611|Meentheena Carbonate Member|Extent|See Tumbiana Formation.  Sheet-like member extends from the Gregory Range into the Pyramid Sheet area.|16-MAY-23
11611|Meentheena Carbonate Member|Thickness range|20-50 m|16-MAY-23
11611|Meentheena Carbonate Member|Lithology|Ripple-bedded dark grey siliceous carbonate rocks|16-MAY-23
11611|Meentheena Carbonate Member|Relationships and boundaries|Underlies Nymerina Basalt, overlies Mingah Tuff Member. Comprises upper part of Tumbiana Formation.|16-MAY-23
11611|Meentheena Carbonate Member|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
11611|Meentheena Carbonate Member|Comments|Contains algal stromatolites and syn-depositional slump structures. Also contains ripple marks.|16-MAY-23
11611|Meentheena Carbonate Member|Name first published by|Lipple S.L., 1975|16-MAY-23
37210|Menyous Limestone Member|Name source|Named after Menyous Gap, Pillara Range, the type section of the Pillara Formation (Guppy et al. 1958).|16-MAY-23
37210|Menyous Limestone Member|Unit history|Informally named Menyous Member by Read (1973b).|16-MAY-23
37210|Menyous Limestone Member|Type section locality|Representative section: Menyous Gap (N 268900 yds; E 380200 yds to N 2691500 yds; E 380700 yds); detailed stratigraphic section shown in Read (1973b; Fig. 6).|16-MAY-23
37210|Menyous Limestone Member|Lithology|Thickest in southern part of Lennard Shelf; maximum measured thickness 420 m at Menyous Gap, Pillara Range. Unit thins locally to 80 m in the northern Emanuel Range, but probably thickens into the southern Emanuel Range. The Menyous Limestone Member thins markedly to the north and east into the Geikie Range-Oscar Plateau area and is not present in the Napier Range area.|16-MAY-23
37210|Menyous Limestone Member|Relationships and boundaries|Uppermost unit of Pillara Formation; conformably overlies Red Bull Member and is overlain by the Sadler Limestone, Virgin Hills or Napier formations. Most contacts between the Menyous Limestone Member and overlying Sadler/Virgin Hills/Napier formations are faulted (Semeniuk and Logan, in prep.). The Menyous Limestone Member is conformable or mildly disconformable with the overlying Sadler Limestone in the northern Emanuel Range; the contact is difficult to define and is placed at the change from brachiopod limestone up into crinoidal limestone (Guppy et al. 1958)|16-MAY-23
37210|Menyous Limestone Member|Age reasons|Givetian to lowermost Frasnian|16-MAY-23
37210|Menyous Limestone Member|Proposed publication|Bull. Can. Petrol. Geol., v.21, p.344-394|16-MAY-23
11904|Mingah Tuff Member|Name source|Mingah Well, Meentheena Station (Military GR 334 338).|16-MAY-23
11904|Mingah Tuff Member|Type section locality|Meentheena Basin, south of Tumbiana Pool on the Nullagine River.|16-MAY-23
11904|Mingah Tuff Member|Extent|See Tumbiana Formation. Range as for Meentheena Carbonatae Member.|16-MAY-23
11904|Mingah Tuff Member|Thickness range|100-150 m.|16-MAY-23
11904|Mingah Tuff Member|Lithology|Basaltic to intermediate tuff. Minor siltstone, mudstone and basalt.|16-MAY-23
11904|Mingah Tuff Member|Relationships and boundaries|Underlies Meentheena Carbonate Member, overlies Kylena Basalt. Comprises lower part of Tumbiana Formation.|16-MAY-23
11904|Mingah Tuff Member|Proposed publication|West Australia Geological Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
11904|Mingah Tuff Member|Comments|Remarks: Ripple marks locally.|16-MAY-23
28208|Mondana Adamellite|Name source|Mondana Pool (MGR 266 282) on Budjan Creek, which passes through the centre of the mass, Marble Bar 1:250 000 Sheet area.|16-MAY-23
28208|Mondana Adamellite|Type section locality|The rock is well exposed at Mondana Pool and access to the area is by poor quality station tracks.|16-MAY-23
28208|Mondana Adamellite|Extent|The pluton occurs in the Corunna Downs Batholith (See Fig. 1) between latitudes 21o35'S and 21o50'S, and longitudes 119o43'E and 120o00'E, as a crescent-shaped mass cropping out over an area of 280 km2. The extent of the pluton on the adjacent Nullagine 1:250 000 Sheet is shown by Hickman (in prep).|16-MAY-23
28208|Mondana Adamellite|Lithology|The Mondana Adamellite is a medium to coarse, even-grained, massive to poorly foliated biotite adamellite and biotite hornblende adamellite with rare feldspar phenocrysts and with a texture varying from allotriomorphic granular to hypidiomorphic granular. Locally, it has a granofels texture. In the northeastern portion, the rock is fine to medium-grained with a moderately developed foliation. In the northwestern area, the rock is also well foliated. Near the margins, the rock contains fine to medium-grained aplite veins which are locally pyritic. Microcline, usually perthitic, is in excess of oligoclase. Oligoclase exhibits well developed albite twinning, and some subhedral to euhedral grains exhibit compositional zoning and have a more seriticised core. This zoning is particularly well developed near the margins of the pluton. Biotite is partially chloritized and occurs throughout the pluton, but in variable proportions. Hornblende, often euhedral and twinned and partially chloritized, is concentrated near the margins adjacent to the greenstone country rock. Accessory minerals include opaque iron oxides, zircon, apatite and rare sphene. Secondary minerals are chlorite, sericite, epidote and rare prehnite. One chemical analysis of this rock is presented in Table 12 of Hickman and Lipple (1974).|16-MAY-23
28208|Mondana Adamellite|Relationships and boundaries|The Mondana Adamellite has sharp intrusive contacts against Archaean greenstones along its southern margin and against the older Carbana Pool Adamellite along the northern margin. At its eastern boundary, the Mondana Adamellite intrudes the older Copper Hills Dacite Porphyry. The Adamellite is intruded by Archaean quartz feldspar porphyry dykes, quartz veins along faults and by Lower Proterozoic dolerite dykes.|16-MAY-23
28208|Mondana Adamellite|Age reasons|Archaean. The unit is correlatead with other post-tectonic adamellites of the East Pilbara with approximate age of 2600 m.y.|16-MAY-23
28208|Mondana Adamellite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, W.A.: West. Australia Geol. Survey Rec. 1974/20. West. Australia Geol. Survey Ann. Reprt 1974.|16-MAY-23
28208|Mondana Adamellite|Name first published by|Hickman A.H., 1975|16-MAY-23
26038|Mons Cupri Volcanics|Name source|Mons Cupri Copper Mine; GR 20o52'S 117o50'E, Roebourne 1:250 000.|16-MAY-23
26038|Mons Cupri Volcanics|Type section locality|A sequence of felsic tuffs, agglomerates and flows 2.5 km east of Mons Cupri. The base of the unit is generally a tuffaceous unit, while the top is always a reworked quartz, feldspar rich tuff.|16-MAY-23
26038|Mons Cupri Volcanics|Extent|A 5 km wide arcuate belt flanking the southern and eastern margins of the Caines Well Granite on the Roebourne 1:250 000 sheet.|16-MAY-23
26038|Mons Cupri Volcanics|Thickness range|Up to 700 m.|16-MAY-23
26038|Mons Cupri Volcanics|Lithology|The Mons Cupri Volcanics contain local units of felsic tuff, agglomerate, flows, plagioclase porphyry and spherulitic rhyolitic intrusions with intercalated cherts and fine sediments.|16-MAY-23
26038|Mons Cupri Volcanics|Relationships and boundaries|Overlies the Warambie Basalt and is overlain by Mallina Formation.|16-MAY-23
26038|Mons Cupri Volcanics|Age reasons|Compston and Airiens (1967) have dated felsic volcanic rock from this unit at 3050 m.y. but later recalculations by Ariens puts the age at approx. between 2500 and 2300 m.y.|16-MAY-23
26038|Mons Cupri Volcanics|Defn author|Fitton M.J., Horwitz R.C., Sylvester G., 1975.|16-MAY-23
26038|Mons Cupri Volcanics|Proposed publication|CSIRO, Minerals Research Laboratories, Report No. FP. 11|16-MAY-23
26038|Mons Cupri Volcanics|Comments|Notes: Several units within the Mons Cupri Volcanics have been named by Miller and Gair (in press). These units are the Mount Brown Rhyolite, the Domal Porphyry and the Cistern Rhyolite. The name Mount Brown Rhyolite is retained and given Member Status. The other names are discarded.|16-MAY-23
26038|Mons Cupri Volcanics|Defn approved by|Western Australia Sub-Committee|16-MAY-23
27200|Moolyella Adamellite|Name source|The Moolyella Adamellite takes it sname from Moolyella mining centre (MGR 276 358) on Moolyella Creek which drains the western side of the mass, Mable Bar 1:250 000 Sheet area.|16-MAY-23
27200|Moolyella Adamellite|Type section locality|The rock is well exposed east of the Moolyella mining centre and access is readily made by the Marble Bar-Bamboo Creek Road from which numerous mining tracks lead to the edges of the unit.|16-MAY-23
27200|Moolyella Adamellite|Extent|The unit occurs in the Mount Edgar Batholith (see Fig. 1), between latitudes 21o05'S and 21o11'S, and longitudes 119o54'E and 120o0'E as a elephantine-shaped mass cropping out over an area of about 55 km2.|16-MAY-23
27200|Moolyella Adamellite|Lithology|The Moolyella Adamellite is a medium even-grained, poorly foliated, allotriomorphic granular textured albite adamellite. Near the margins, it is fine-grained, and elsewhere it is locally coarse-grained. Microcline and albite (average An8 for N=23) are in equal to subequal proportions. Albite is variably altered to sericite, epidote and some carbonate. Microcline is fresh, polysynthetically twinned and invariably microperthitic including very fine spindles of plagioclase which are crystallographically oriented. Biotite is partially or totally replaced by chlorite. The rock contains some muscovite and pumpellyite, ?ferrohastingsite, colourless garnet and colourless to intensely purple fluorite. Accessory minerals include epidote, euhedral zircon, apatite, sphene; tourmaline, a black opaque mineral and possible metamict allanite. The unit crops out strongly as rocky ridges and tor fields. On aerial and satellite photographs, it exhibits a dark photo-pattern. A detailed study of the Moolyella Adamellite, particularly of its geochemistry and associated cassiterite deposits is given by Blockley (in prep.). Its average chemical composition is presented in Table 12 of Hickman and Lipple (1974).|16-MAY-23
27200|Moolyella Adamellite|Relationships and boundaries|The Adamellite has sharp intrusive contacts with the surrounding older migmatitic biotite adamellite and biotite granodiorite, and contains rare xenoliths of the host rocks. It is well jointed and has quartz veins along shear zones and faults. The unit is intruded by a quartz feldspar porphyry and by Lower Proterozoic dolerite dykes. Coarse pegmatites associated with the mass occur both internally and in the surrounding migmatites and contain cassiterite mineralisation (see Blockley, 1970, 1973).|16-MAY-23
27200|Moolyella Adamellite|Structure and Metamorphism|From the distribution of pegmatites, outcrop shape of the mass, and increasing grain size towards the northeastern margin, the Adamellite appears to be a small southwest-plunging stock.|16-MAY-23
27200|Moolyella Adamellite|Age reasons|de Laeter and Blockley (1972) discuss the Moolyella Adamellite and give an age of 2670 +/- 95 m.y. with an initial 87Sr/86Sr ratio of 0.7397 +/- 0.0419, and suggest that the Adamellite possibly originated by remobilization of the surrounding migmatitic biotite granodiorites and biotite adamellites.|16-MAY-23
27200|Moolyella Adamellite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, WA: West. Australia Geol. Survey Rec. 1974/20. West Australia Geol. Survey Ann. Rept 1974.|16-MAY-23
27200|Moolyella Adamellite|Defn approved by|Western Australia Sub-Committee|16-MAY-23
27200|Moolyella Adamellite|Name first published by|de Laeter J.R., Blockley J.G., 1972|16-MAY-23
24402|Mount Leake Sandstone|Name source|Mt Leake, Peak Hill 1:250 000 Sheet.|16-MAY-23
24402|Mount Leake Sandstone|Type section locality|Southern slope of Mt Leake 25o47'S, 119o09'E).|16-MAY-23
24402|Mount Leake Sandstone|Extent|Bilyuin to Mt Leake, Peak Hill Sheet.|16-MAY-23
24402|Mount Leake Sandstone|Thickness range|about 15 metres|16-MAY-23
24402|Mount Leake Sandstone|Lithology|Well sorted, cross bedded orthoquartzite sandstone, partly silicified and chalcedonic.|16-MAY-23
24402|Mount Leake Sandstone|Relationships and boundaries|Unconformably overlies Glengarry Group. Probably younger than Padbury Group.|16-MAY-23
24402|Mount Leake Sandstone|Age reasons|Proterozoic - probably between 1.7-1.0 b.y.|16-MAY-23
24402|Mount Leake Sandstone|Proposed publication|Western Australia Geological Survey Annual Report for 1978 (Pub. 1979).|16-MAY-23
24402|Mount Leake Sandstone|Defn Reference|80/20704|16-MAY-23
24402|Mount Leake Sandstone|Proposer|Gee R.D.|16-MAY-23
13279|Mowanjum Sands|Name source|Mowanjum Mission; grid reference130813 Derby 1:250 000 Sheet area.|16-MAY-23
13279|Mowanjum Sands|Type section locality|Sand Quarry on northern margin of Derby townsite (grid ref. 128820; Derby 1:25 000 Sheet).|16-MAY-23
13279|Mowanjum Sands|Extent|The unit is exposed as surface dunes over 4000 km2 in the Derby region.  Additionally the unit is cliffed and exposed in low tide zones at Black Rocks (grid reference 119847, Derby 1:250 000 Sheet) and is penetrated in water wells tens of metres deep.|16-MAY-23
13279|Mowanjum Sands|Thickness range|Total thickness unknown. Bore hole data show thickness in excess of 15 m. Tongues of this unit (thinning down to 5 cm) interdigitate with Airport Creek and Christine Point Formations.|16-MAY-23
13279|Mowanjum Sands|Lithology|Red-orange quartzose sand, locally white; homogenous to mottled; locally lateritic; Fe-oxide and/or clay mottles locally present.|16-MAY-23
13279|Mowanjum Sands|Relationships and boundaries|Base locally exposed and rests on basement Tertiary laterite highs (see Casey 1958); contact with underlying laterite is sharp. Top of unit is the contemporary surface. The unit intertongues with Airport Creek, Christine Point and Doctors Creek Formations; the tongues located at unconformities.|16-MAY-23
13279|Mowanjum Sands|Age reasons|The bulk of the unit underlies all Quaternary units in this area, thus its age is Pleistocene (or ? Pliocene).|16-MAY-23
13279|Mowanjum Sands|Proposed publication|Journal of the Royal Society of WA|16-MAY-23
13359|Mulgandinnah Adamellite|Name source|Mulgandinnah Hill, Marble Bar 1:250 000 Sheet area (MGR 2153 3167).|16-MAY-23
13359|Mulgandinnah Adamellite|Type section locality|The Mulgandinnah Adamellite is well exposed at Mulgandinnah Hill (MGR 2153 3167) and easy access is via station and mining tracks leading west and northwestwards from Spear Hill. The rock is also well exposed 0.5 km west of Pilga homestead (abandoned).|16-MAY-23
13359|Mulgandinnah Adamellite|Extent|The Mulgandinnah Adamellite occurs in the Shaw Batholith and forms several small ovoid masses, the largest of which is about 2 km in diameter extending in a zone from several kilometres northwest to east from Spear Hill (see Fig. 1).|16-MAY-23
13359|Mulgandinnah Adamellite|Lithology|The Mulgandinnah Adamellite is a fine to medium equigranular, well foliated biotite adamellite. The foliation is constituted by a alignment of feldspar and ;mica grains, biotite schlieren and wisps and elongate migmatite xenoliths.  Magnetite octahedra are common. The adamellite contains microcline and saussuritized plagioclase in sub-equal amounts, and minor biotite. The plagioclase is a calcic oligoclase with average composition (for N=7) of An23, ranging between An20+ and An29.  Allanite is a common accessory mineral. Secondary muscovite and epidote are present. Biotite is generally altered to chlorite. The usual texture is allotriomorphic granular but a foliation may be outlined by elongate quartz blebs and the rock locally exhibits a texture indicating protoclastic shearing. Further details of the Mulgandinnah Adamellite, including chemical composition, are presented by Blockley (in prep.).|16-MAY-23
13359|Mulgandinnah Adamellite|Relationships and boundaries|The Mulgandinnah Adamellite is a typical example of remobilised Archaean migmatitic granitic rocks. The remobilised material occurs as small stocks (Mulgandinnah Adamellite) having diffuse contacts with the enclosing migmatite. Some apophyses extend into the country rock along the foliation direction and generally the regional foliation persists within the stock as alignment of feldspars and micas. A "ghost stratigraphy" of biotite schlieren and wisps, and xenoliths of the migmatite also persists within the Adamellite. The Adamellite is intruded by Archaean dacite and rhyolite dykes and Lower Proterozoic dolerite dykes.|16-MAY-23
13359|Mulgandinnah Adamellite|Age reasons|Archaean|16-MAY-23
13359|Mulgandinnah Adamellite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, WA: West. Australia Geol. Survey Rec. 1974/20 West. Australia Geol. Survey Ann. Rept 1974.|16-MAY-23
13359|Mulgandinnah Adamellite|Name first published by|Lewis J.D., Rosman K.J.R., DeLaeter J.R., 1975|16-MAY-23
13845|Naracoota Volcanics|Name source|Narracoota Homestead, Peak Hill 1:250 000 Sheet.|16-MAY-23
13845|Naracoota Volcanics|Type section locality|Mikhaburra-Bashman area, 10-15 km south of Narracoota.|16-MAY-23
13845|Naracoota Volcanics|Extent|South, northeast and northwest of Narracoota.|16-MAY-23
13845|Naracoota Volcanics|Thickness range|Possibly 6 km.|16-MAY-23
13845|Naracoota Volcanics|Lithology|Massive basalt in lower part, ultramafic phyllite in upper part. Includes picritic lavas and pyroclastics.|16-MAY-23
13845|Naracoota Volcanics|Relationships and boundaries|Conformable above Karalundi Formation, laterally equivalent to, and also conformably below Thaduna Greywacke.|16-MAY-23
13845|Naracoota Volcanics|Age reasons|Proterozoic - probably 2.0-1.8 b.y.|16-MAY-23
13845|Naracoota Volcanics|Proposed publication|Western Australia Geological Survey Annual Report for 1978 (Pub. 1979)|16-MAY-23
13845|Naracoota Volcanics|First Reference|80/20704|16-MAY-23
13845|Naracoota Volcanics|Unit name|Narracoota Volcanics|16-MAY-23
13970|Negri Volcanics|Name source|'Mount Negri' (20o48'S, 117o51'E) Roebourne 1:250 000 Sheet area.|16-MAY-23
13970|Negri Volcanics|Unit history|Mt Negri Volcanics (5); Negri Volcanics (1). Distribution and relations incompletely defined by (5). (1) include rocks now referred to as the Louden Volcanics within the unit but as noted above, and by (2) the two units are lithologically different and now regarded as unconformable.|16-MAY-23
13970|Negri Volcanics|Type section locality|Mount Negri.|16-MAY-23
13970|Negri Volcanics|Extent|6 km2 at Mount Negri and approximately 30 km2 6 km southwest of Mons Cupri (20o53'S, 117o48'E). (See Fig. 28 of Hickman 1977).|16-MAY-23
13970|Negri Volcanics|Thickness range|Range up to approx. 500 m.|16-MAY-23
13970|Negri Volcanics|Lithology|Variolitic mafic to intermediate lava flows. Minor conglomerate 3 km southwest of Mons Cupri.|16-MAY-23
13970|Negri Volcanics|Relationships and boundaries|Unconformably overlies the Mons Cupri Volcanics (1) at Mount Negri and Mons Cupri. In faulted contact with the Louden Volcanics (3) at Mons Cupri and considered to unconformably overlie the Louden Volcanics at Mount Negri (contact obscured but the Negri Volcanics are almost flat lying whereas the Louden Volcanics are inclined at 40-60o). No contact exists with the Mount Roe Basalt (4) but the latter is regarded as unconformably overlying the Negri Volcanics because the latter are cleaved and the former not.|16-MAY-23
13970|Negri Volcanics|Age reasons|Late Archaean because of probable relationship to the Mount Roe Basalt (basal formation of the Lower Proterozoic Fortescue Group in the Pilbara) noted above.|16-MAY-23
13970|Negri Volcanics|Proposed publication|Geology of the Pilbara Block and its environs, GSWA Bull.|16-MAY-23
13970|Negri Volcanics|Status|1|16-MAY-23
14274|North Pole Adamellite|Name source|North Pole mining centre (MGR 213 363), Marble Bar 1:250 000 Sheet area.|16-MAY-23
14274|North Pole Adamellite|Unit history|The name, North Pole Granite, was used without definition for the same mass by Noldart and Wyatt, 1958, p.40 and 42; ibid, 1962, p.98 and 176.|16-MAY-23
14274|North Pole Adamellite|Type section locality|The pluton is well exposed over most of its extent.  Access is by the Marble Bar-Normay road thence cross country south of the Normay mine or by mining tracks leading from Breens copper mine.|16-MAY-23
14274|North Pole Adamellite|Extent|The North Pole Adamellite is a small oval shaped pluton in the centre of the North Pole Dome (see Fig. 1), centred 6 km southeast of the North Pole mining centre. It crops out over an area of 25 km2 between latitudes 21o06'S and 21o08'S and longitudes 119o22'E and 119o25'E.|16-MAY-23
14274|North Pole Adamellite|Lithology|The North Pole Adamellite is a medium even-grained poorly to well foliated biotite adamellite (N5). There is some grain size variation and the rock is weakly porphyritic in some areas. Zoned oligoclase is in excess of microcline. There is moderate biotite and accessory sphene, opaques, apatite and zircon. Secondary minerals are chlorite (after biotite), muscovite and epidote. Oligoclase crystals up to 6 mm across are zoned, subhedral and strongly saussuritized. Near the margins, the pluton is a silicified granophyric granite with quartz forming a patchy replacement of microcline. The unit is locally a biotite granodiorite near the southeastern margin (GSWA specimen 7361 reported on by Noldart and Wyatt, 1962, p.173-185).|16-MAY-23
14274|North Pole Adamellite|Relationships and boundaries|The North Pole Adamellite is a small pluton intruded by ultramafic dykes.|16-MAY-23
14274|North Pole Adamellite|Age reasons|Archaean|16-MAY-23
14274|North Pole Adamellite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, WA: West. Australia Geol. Survey Rec. 1974/20. West. Australia Geol. Survey Ann. Rept 1974|16-MAY-23
26084|Numbana Granite|Name source|The Numbana Granite takes its name from Numbana mine, Marble Bar 1:250 000 Sheet area (MGR 133 332).|16-MAY-23
26084|Numbana Granite|Type section locality|The rock is well exposed along the upper reaches of the West Turner River and access is attained by poor quality exploration tracks.|16-MAY-23
26084|Numbana Granite|Extent|The pluton occurs in the Yule River Batholith (see Fig. 1) between latitudes 21o15'S and 21o28'S, and longitudes 118o30'E and 118o51'E having an irregular shape elongate in an east-west direction, and cropping out over an area of 440 km2.|16-MAY-23
26084|Numbana Granite|Lithology|The Numbana Granite is a medium to coarse, even-grained poorly to moderately foliated granitic rock with abundant finer-grained granitic xenoliths distributed throughout the mass, and rare mafic schlieren. There are some coarse pegmatite veins. The pluton crops out strongly as low rocky ridges and tor fields. It has pronounced jointing and quartz veining along shear zones and faults. The composition of the pluton is uncertain since no thin sections are available but it is probably between biotite adamellite and granite. Part of the Numbana Granite is within an area discussed by Blockley (1971).|16-MAY-23
26084|Numbana Granite|Relationships and boundaries|The Numbana Granite has a transitional contact zone against the older Nardoopiquithanna Adamellite to the north with abundant xenoliths of the latter decreasing towards the south. The contact against the older Abydos Adamellite to the southeast is sharp, as is the contact against older migmatitic biotite granodiorite along the southern margin. The contact of the Numbana Granite with the Kangan Granite to the northwest is generally sharp but the relationship of the two masses is uncertain, possibly the latter is oldest. The Numbana Granite is intruded by Lower Proterozoic dolerite dykes of the Round Hummock and Mundine Well suites. There are also quartz veins along faults in the Granite.|16-MAY-23
26084|Numbana Granite|Age reasons|Archaean|16-MAY-23
26084|Numbana Granite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, WA: West. Australia Geol. Survey Rec. 1974/20. West. Australia Geol. Survey Ann. Rept 1974.|16-MAY-23
26084|Numbana Granite|Name first published by|Hickman A.H., 1975|16-MAY-23
24452|Pearana Basalt|Name source|Pearana Creek'; grid reference 439267 to 419261, Nullagine 1:250 000 Sheet area.|16-MAY-23
24452|Pearana Basalt|Type section locality|3 km east Woodie Woodie mining centre (427298).|16-MAY-23
24452|Pearana Basalt|Extent|2-5 km wide outcrop belt along the Western margin of the Gregory Range from 443256 to 400386 a distance of 140 km (strike is North North West).|16-MAY-23
24452|Pearana Basalt|Thickness range|Approximately 500 metres.|16-MAY-23
24452|Pearana Basalt|Lithology|Vesicular and porphyritic basalt. Upper part of the formation includes felsic lava.|16-MAY-23
24452|Pearana Basalt|Relationships and boundaries|Conformably overlies Tumbiana Formation (References a and b). Conformably underlies Lewin Shale (Reference c). Forms part of Fortescue Group (Reference d).|16-MAY-23
24452|Pearana Basalt|Age reasons|Lower Proterozoic, since forms part of the Fortescue Group.|16-MAY-23
24452|Pearana Basalt|Proposed publication|West Australia Geological Survey 1:250 000 Geological Series Explanatory Notes (Nullagine)|16-MAY-23
24452|Pearana Basalt|Comments|The formation is correlated with the succession Nymerina Basalt/Kuruna Siltstone/Maddina Basalt (Reference e).|16-MAY-23
24452|Pearana Basalt|First Reference|81/21317|16-MAY-23
24452|Pearana Basalt|Proposer|Hickman A.H.|16-MAY-23
28207|Pincunah Adamellite|Name source|Pincunah Waterhole, Marble Bar 1:250 000 Sheet area (MGR 153 349).|16-MAY-23
28207|Pincunah Adamellite|Type section locality|The Adamellite is well exposed along the Mount Newman Railway and along the Turner River. Access is by the Wittenoom-Port Hedland Road.|16-MAY-23
28207|Pincunah Adamellite|Extent|The Pincunah Adamellite forms an irregular mass elongate longitudinally, occurring west of Pilgangoora Syncline between latitudes 21o09'S and 21o22'S, and longitudes 118o50'E and 118o56'E. The rock crops out ovr an area of 165 km2. See Fig. 1.|16-MAY-23
28207|Pincunah Adamellite|Lithology|Pincunah Adamellite is a medium to coarse-grained, coarsely porphyritic biotite adamellite. Phenocrysts are generally 1.5 x 1.5 cm in size, ranging up to 1.5 x 2 cm. A strong foliation is exhibited by alignment of phenocrysts and feldspar in the groundmass, biotite and mafic schlieren, but the direction is variable even over a single outcrop. There are abundant xenoliths of amphibolite ultramafic schist and medium, even-grained biotite granodiorite. Minor aplite and later coarse pegmatite veins discordant to the foliation are present. Mafic schlieren and xenoliths locally form a stromatic fabric. Along the northern margin adjacent to the Archaean greenstones, prominent tectonic foliation parallel to the margin is exhibited by the alignment of phenocrysts, and feldspar, biotite and particularly quartz grains. The phenocrysts are well twinned microcline containing albite-rimmed plagioclase inclusions and are set in an allotriomorphic granular groundmass of oligoclase, microcline, quartz and biotite. There is accessory magnetite, apatite, allanite and zircon and secondary muscovite, chlorite, epidote and rare calcite. Partly recrystallized, much of the plagioclase occurs as small myrmekitic grains between larger grains. Plagioclase is in excess of microcline. Locally, the pluton exhibits compositional variation, probably due to contamination by xenoliths, and includes portions of biotite granodiorite and biotite tonalite composition. Both varieties contain sphene as an additional accessory mineral.|16-MAY-23
28207|Pincunah Adamellite|Relationships and boundaries|The Pincunah Adamellite intrudes the Archaean greenstones along the eastern margin and migmatitic biotite granodiorite to the north, east and south. It has sharp intrusive contact with the (?younger) Nardoopiquithanna Adamellite and Numbana Granite. The pluton is intruded by north-trending Archaean dolerite dykes. The unit is well exposed and only locally obscured by thin Quaternary sand. The northern margin is obscured by Quaternary gravel deposits.|16-MAY-23
28207|Pincunah Adamellite|Age reasons|Archaean.|16-MAY-23
28207|Pincunah Adamellite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, WA: West. Australia Geol. Survey Rec 1974/20 West. Australia Geol. Survey Ann. Rept 1974.|16-MAY-23
25398|Pindar Beds|Name source|Pindar Yard, 19o05'S, 128o16'15"E, Billiluna 1:250 000 Sheet area, WA.|16-MAY-23
25398|Pindar Beds|Unit history|Previously mapped as Gardiner and Kearney Beds (Wells 1962, Casey and Wells 1964).|16-MAY-23
25398|Pindar Beds|Type section locality|Reference area:  2 km southwest of the northern Palm Springs in the Denison Range; above lithologies present steeply dipping and locally overturned.|16-MAY-23
25398|Pindar Beds|Extent|South of Sturt Creek homestead, between the Denison & Peterson Ranges; Billiluna 1:250 000 Sheet area, WA.|16-MAY-23
25398|Pindar Beds|Thickness range|About 300 m in the reference area.|16-MAY-23
25398|Pindar Beds|Lithology|Medium to coarse grained quartz arenite and sublithic arenite, cross-bedded and locally pellety. Quartz veins and slickensided surfaces common.|16-MAY-23
25398|Pindar Beds|Relationships and boundaries|Overlie the Lake Willson Beds, possibly conformably. Overlain probably unconformably by Denison Beds.|16-MAY-23
25398|Pindar Beds|Age reasons|Carpentarian or Adelaidean.|16-MAY-23
25398|Pindar Beds|Defn approved by|Taken from xerox copy of approved def. Sent by WA Sub-Committee|16-MAY-23
25398|Pindar Beds|Name first published by|Blake D.H., Yeates A.N., Passmore V.L., Hodgson I.M., Walton D.G., Muhling P.G., Crowe R.W.A., 1977|16-MAY-23
32640|Pinjian Breccia|Name source|Pinjian Pool, 20o59'S, 120o39'E, Yarrie1:250 000 Sheet area.|16-MAY-23
32640|Pinjian Breccia|Unit history|Named 'Pinjian Chert Breccia' by Noldart and Wyatt (1962). Renaming is necessary because only binomial names are acceptable under the Code.|16-MAY-23
32640|Pinjian Breccia|Type section locality|Pinjian Pool (Noldart and Wyatt, 1962, p.77).|16-MAY-23
32640|Pinjian Breccia|Extent|Crops out between Pinjian Pool and Carrowina Pool (22o35'S, 121o02'E, Balfour Downs 1:250 000 Sheet area), and over an area of approximately 3 000 km2.|16-MAY-23
32640|Pinjian Breccia|Thickness range|Up to 100 m.|16-MAY-23
32640|Pinjian Breccia|Lithology|A residual and replacement deposit consisting of angular chert fragments cemented by a chert matrix. Local concentrations of manganese and iron oxides.|16-MAY-23
32640|Pinjian Breccia|Relationships and boundaries|Unconformably overlain by the Waltha Woora Formation (Noldart and Wyatt, 1962) and unconformably overlies the Carawina Dolomite (Maitland, 1919 - 'Carawina Dolomite Series'; Talbot, 1920).|16-MAY-23
32640|Pinjian Breccia|Age reasons|Lower or Middle Proterozoic formation, but see comments.|16-MAY-23
32640|Pinjian Breccia|Proposed publication|Yarrie, WA: West Australia Geol. Survey 1:250 000 Series Explan. Notes|16-MAY-23
32640|Pinjian Breccia|Comments|Where unconformities with overlying Middle Proterozoic and Permian formations are not preserved it is difficult to distinguish the Pinjian Breccia from Tertiary cap rock (both contain the same components and formed by the same mechanism).|16-MAY-23
32640|Pinjian Breccia|Status|1|16-MAY-23
24468|Ragged Hills Granophyre|Name source|Ragged Hills mine (21o18'S, 121o09'E). Nullagine 1:250 000 Sheet area.|16-MAY-23
24468|Ragged Hills Granophyre|Unit history|Included in the Gregory Range Granite of (2).|16-MAY-23
24468|Ragged Hills Granophyre|Type section locality|8 km east of Ragged Hills mine, and to the south of the Telfer-Braeside road.|16-MAY-23
24468|Ragged Hills Granophyre|Extent|Crops out intermittently over an area of approximately 500 km2.|16-MAY-23
24468|Ragged Hills Granophyre|Thickness range|Vertical thickness unknown, a high-level hypabyssal intrusion.|16-MAY-23
24468|Ragged Hills Granophyre|Lithology|Pink, medium grained granophyre containing scattered rounded phenocrysts of perthite in a granophyric matrix. Mafic minerals are biotite, hornblende and aegirine augite. The rock is generally massive but locally cleaved. To the north and south of the type area the rock becomes finer grained and more closely resembles lava of the adjacent Koongaling Volcanics (1) to which it is thought to be genetically related.|16-MAY-23
24468|Ragged Hills Granophyre|Relationships and boundaries|Of similar chemistry to the Koongaling Volcanics. Small peripheral dykes of granophyre intrude the basal section of the Koongaling Volcanics. Other relations obscured by sand cover.|16-MAY-23
24468|Ragged Hills Granophyre|Age reasons|Thought to be Early Proterozoic. Geochronology in progress, preliminary results of which indicate an age of 2 600-2 400 my.|16-MAY-23
24468|Ragged Hills Granophyre|Proposed publication|Geology of the Pilbara Block and its environs, GSWA Bull.|16-MAY-23
24468|Ragged Hills Granophyre|Proposer|Hickman A.H.|16-MAY-23
30591|Shepherds Bore Plutonic Complex|Name source|Shepherds Bore, at GR CE559903, Halls Creek 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area.|16-MAY-23
30591|Shepherds Bore Plutonic Complex|Unit history|Equivalent to Shepherds Bore Granite and some undivided gabbro in adjoining McIntosh 1:100 000 Sheet area (Tyler et al. 1997a) to north, in Dixon Range 1:250 000 Sheet area.|16-MAY-23
30591|Shepherds Bore Plutonic Complex|Geomorphic expression|Low hills and depressions.|16-MAY-23
30591|Shepherds Bore Plutonic Complex|Type section locality|Vicinity of Shepherds Bore, HALLS CREEK, GR CE555905, where typical rocks of the complex are well exposed.|16-MAY-23
30591|Shepherds Bore Plutonic Complex|Extent|Northwestern Halls Creek 1:100 000, Gordon Downs 1:250 000 Sheet area, extending north into McIntosh 1:100 000 Sheet area, Dixon Range 1:250 000 Sheet area.|16-MAY-23
30591|Shepherds Bore Plutonic Complex|Lithology|Porphyritic and even-grained granitic rocks (ranging in composition from tonalite to leucogranite); gabbro and dolerite; intermediate hybrid rocks; inclusions of hornfels; many net-veined complexes (intimate mixtures of granite, gabbro and hybrid rocks).|16-MAY-23
30591|Shepherds Bore Plutonic Complex|Relationships and boundaries|Intrudes Koongie Park Formation; overlain unconformably by King Leopold Sandstone of Kimberley Group; intruded by rhyolite and dolerite dykes.|16-MAY-23
30591|Shepherds Bore Plutonic Complex|Age reasons|Palaeoproterozoic: Orosirian. Older than c. 1790 Ma (age of Hart Dolerite, which intrudes the Kimberley Group, and younger than 1843 Ma (age of Koongie Park Formation).|16-MAY-23
30591|Shepherds Bore Plutonic Complex|Correlations|Some plutons of the Sally Downs supersuite of Bow River batholith:.|16-MAY-23
30591|Shepherds Bore Plutonic Complex|Comments|Complex postdates main folding and regional metamorphism of the Koongie Park Formation.|16-MAY-23
30591|Shepherds Bore Plutonic Complex|References|Blake, D.H., Tyler, I.M., Griffin, T.J., Sheppard, S., Thorne, A.M. & Warren, R.G., 1998. Geology of the Halls Creek 1:100 000 Sheet area (4461), Western Australia. Australian Geological Survey Organisation, Canberra.  **Sheppard, S., Tyler, I.M. & Hoatson, D.M., 1997. Geology of the Mount Remarkable 1:100 000 sheet. Geological Survey of Western Australia, 1:100 000 Geological Series Explanatory Notes.  **Tyler, I.M., Sheppard, S., Hoatson, D.M. & Blake, D.H., 1997a.  McIntosh, Western Australia, 1:100 000 geological map (sheet 4462). Geological Survey of Western Australia.|16-MAY-23
17068|Soanesville Subgroup|Name source|Soanesville mining centre (Military Grid Reference 1945 3105), Marble Bar 1:250 000 Sheet area.|16-MAY-23
17068|Soanesville Subgroup|Type section locality|The Soanesville Subgroup consists of the Paddy Market Formation (youngest) and the Corboy Formation, and unassigned sedimentary and volcanic rocks in the Soanesville Belt.|16-MAY-23
17068|Soanesville Subgroup|Extent|The Soanesville Subgroup occurs in the Soanesville Belt, Western Shaw Belt, Coongan Syncline, Pilgangoora Syncline and Lalla Rookh Syncline.|16-MAY-23
17068|Soanesville Subgroup|Thickness range|Maximum, 5-8 km.|16-MAY-23
17068|Soanesville Subgroup|Lithology|The Subgroup includes sandstone, siltstone, ferruginous shales, banded iron formations and pillowed basalt. Some ultramafic and gabbroic sills are also included.  (?Can intrusives be included in the unit they intrude?).|16-MAY-23
17068|Soanesville Subgroup|Relationships and boundaries|Conformably overlain by Honeyeater Formation and overlies with local unconformity the Wyman Formation, Salgash Sub-group and Talga Talga Subgroup. In the Soanesville Belt, unassigned rocks of the Subgroup are unconformably overlain by a thin, flat lying sequence of felsic lavas, centres on Military Grid Reference 187328, which have not been assigned to any younger division. The connection of the unassigned Soanesville Sub-Group sedimentary rocks with the Corboy Formation further north is obscured by structural complexity and further study is required to elucidate the nature of this connection.|16-MAY-23
17068|Soanesville Subgroup|Age reasons|Archaean because of tectonic style and unconformably overlain by Lower Proterozoic Mount Roe Basalt.|16-MAY-23
17068|Soanesville Subgroup|Defn author|Lipple S.L., 1975|16-MAY-23
17068|Soanesville Subgroup|Proposed publication|West Australia Geol. Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
32523|Sophie Downs Granophyre Member|Name source|Sophie Downs homestead, at GR, Halls Creek 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area.|16-MAY-23
32523|Sophie Downs Granophyre Member|Unit history|Sophie Downs Granite of Gemuts & Smith 1968, Dow & Gemuts 1969, Gemuts 1971.|16-MAY-23
32523|Sophie Downs Granophyre Member|Geomorphic expression|Undulating and low hilly terrane|16-MAY-23
32523|Sophie Downs Granophyre Member|Type section locality|Northern side of Sophie Downs Dome, near GR CF830005, Halls Creek 1:100 000 Sheet area, where porphyritic granophyre, the characteristic rock type of the member, is overlain unconformably by Saunders Creek Formation, Halls Creek Group.|16-MAY-23
32523|Sophie Downs Granophyre Member|Extent|NE Halls Creek 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area, W.A..|16-MAY-23
32523|Sophie Downs Granophyre Member|Thickness range|>1000 m.|16-MAY-23
32523|Sophie Downs Granophyre Member|Lithology|Granophyre, generally porphyritic, recrystallised in places to granofels;  some igneous flow-banding; breccia of flow-margin type present locally at contact with overlying Saunders Creek Formation.|16-MAY-23
32523|Sophie Downs Granophyre Member|Relationships and boundaries|Base not seen; overlain unconformably by sandstone and conglomerate of Saunders Creek Formation, Halls Creek Group; intruded by mafic bodies. Relationships with adjacent metamorphic rocks of Ding Dong Downs Volcanics not clear.|16-MAY-23
32523|Sophie Downs Granophyre Member|Age reasons|Palaeoproterozoic, Orosirian; isotopically dated (U-Pb zircon) at 1912+/-2 Ma.|16-MAY-23
32523|Sophie Downs Granophyre Member|Correlations|Junda Microgranite|16-MAY-23
32523|Sophie Downs Granophyre Member|Comments|Confined to core of Sophie Downs Dome. Same age as, and similar in chemistry to, felsic volcanics of Ding Dong Downs Volcanics. Presence of igneous flow-banding and breccia of flow-margin type show that the member forms an extrusive or subvolcanic dome rather than a plutonic intrusion.|16-MAY-23
32523|Sophie Downs Granophyre Member|References|Blake, D.H., Tyler, I.M., Griffin, T.J., Sheppard, S., Thorne, A.M. & Warren, R.G., 1998. Geology of the Halls Creek 1:100 000 Sheet area (4461), Western Australia. Australian Geological Survey Organisation, Canberra.  **Dow, D.B. & Gemuts, I., 1969. Geology of the Kimberley region, Western Australia: the East Kimberley. Bureau of Mineral Resources, Australia, Bulletin 106, & Geological Survey of Western Australia, Bulletin 120.  **Gemuts, I., 1971. Metamorphic and igneous rocks of the Lamboo Complex, East Kimberley Region, Western Australia. Bureau of Mineral Resources, Australia, Bulletin 107.  **Gemuts, I. & Smith, J.W., 1968. Gordon Downs, Western Australia -- 1:250 000 Geological Series. Bureau of Mineral Resources, Australia, Explanatory Notes SE/52-10.|16-MAY-23
25488|Spear Hill Adamellite|Name source|The Spear Hill Adamellite is named after Spear Hill, Marble Bar 1:250 000 Sheet area (MGR 2205 3125).|16-MAY-23
25488|Spear Hill Adamellite|Type section locality|The Spear Hill Adamellite is well exposed at Spear Hill and access is readily made from the Marble Bar-Wittenoom Road.|16-MAY-23
25488|Spear Hill Adamellite|Extent|The pluton occurs in the Shaw Batholith, between latitudes 21o30'S and 21o31'S and longitudes 119o23'E and 119o25'E, as a small tear-shaped mass cropping out over an area of 8 km2 (see Fig. 1).|16-MAY-23
25488|Spear Hill Adamellite|Lithology|The Spear Hill Adamellite is a massive, coarse, even-grained biotite adamellite with local porphyritic, or coarse granophyric textures. Microcline is in excess of oligoclase, and is characterised by coarse, twinned exsolution blebs of oligoclase. The large perthitic microcline also encloses early formed crystals of oligoclase. Plagioclase has an average composition of calcic oligoclase (An28 for N=7) ranging from oligoclase (An24) to sodic andesine (An33). Biotite is generally chloritised and there is widespread secondary muscovite. Fluorite and allanite are rare accessory minerals and there is rare to minor epidote. The unit generally crops out prominently in contrast to the typical quartz and pegmatite scree associated with the surrounding migmatite. Detailed description of the Adamellite, particularly of the chemical composition and associated cassiterite deposits is made by Blockley (1970, 1973 and in prep.).|16-MAY-23
25488|Spear Hill Adamellite|Relationships and boundaries|The boundaries between the intrusive Spear Hill Adamellite and the surrounding older migmatite and foliated granodiorite are sharp and distinctive. Along the northwestern margin, the Adamellite intrudes a large Archaean amphibolite-quartzite xenolith in the migmatites. The Adamellite is intruded by Archaean rhyolite dykes and Lower Proterozoic dolerite dykes. Some of the Adamellite is obscured by a thin cover of Quaternary sand.|16-MAY-23
25488|Spear Hill Adamellite|Structure and Metamorphism|The Spear Hill Adamelite is very similar in appearance and composition to the Cooglegong Adamellite and is certainly genetically related to it, and may be physically connected in depth.  The Adamellite represents a post-tectonic, high level intrusion, probably derived by remobilization and differentiation of the migmatites.|16-MAY-23
25488|Spear Hill Adamellite|Age reasons|Archaean|16-MAY-23
25488|Spear Hill Adamellite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, WA: West. Australia Geol. Survey Rec. 1974/20 West. Australia Geol. Survey Ann. Rept 1974.|16-MAY-23
25488|Spear Hill Adamellite|Name first published by|DeLaeter J.R., Lewis J.D., Blockley J.G., 1975|16-MAY-23
17165|Spinaway Porphyry|Name source|Spinaway Well, Nullagine 1:250 000 Sheet area. (MGR 2935 3035).|16-MAY-23
17165|Spinaway Porphyry|Unit history|Correlated with the Bamboo Creek Porphyry by Noldart and Wyatt (1962 p.89).|16-MAY-23
17165|Spinaway Porphyry|Type section locality|The Spinaway Porphyry is well exposed 18 km south of Spinaway Well near the Great Northern Highway.|16-MAY-23
17165|Spinaway Porphyry|Extent|The unit occurs along the eastern margin of the Marble Bar Sheet area, in the Kelly Belt, 10 km and 25 km south of Copper Hills and is continuous onto the Nullagine 1:250 000 Sheet area (Hickman and Thom, in prep) adjacent to the great Northern Highway between 10 km north of Nullagine township and 10 km south of Spinway Well.|16-MAY-23
17165|Spinaway Porphyry|Thickness range|Maximum, 100 metres.|16-MAY-23
17165|Spinaway Porphyry|Lithology|Coarse-grained plagioclase-quartz dacite porphyry with abundant euhedral calcic oligoclase phenocrysts and quartz phenocrysts set in a dark blue black siliceous groundmass.|16-MAY-23
17165|Spinaway Porphyry|Relationships and boundaries|Intrusive sill into the Hardey Sandstone of the Fortescue Group and partly an extrusive lava (Hickman and Thom, in prep., and Noldart and Wyatt, 1962, p.91). It is conformably overlain by the Kylena Basalt.|16-MAY-23
17165|Spinaway Porphyry|Age reasons|Lower Proterozoic since overlain by part of the Fortescue Group sequence. Preliminary geochronological studies indicate an age of 2124 +/- 195 m.y. (Trendall, pers. comm).|16-MAY-23
17165|Spinaway Porphyry|Defn author|Lipple S.L., 1975|16-MAY-23
17165|Spinaway Porphyry|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
17165|Spinaway Porphyry|Name first published by|Trendal A.F., 1975|16-MAY-23
17420|Strelley Granite|Name source|Strelley Pool, Marble Bar 1:250 000 Sheet area (MGR 1884 3610) on a creek (Six Mile) which drains the northern position of the mass.|16-MAY-23
17420|Strelley Granite|Unit history|Noldart and Wyatt (1958, p.40) apparently refer to the whole mass as the Shaw River Granite.|16-MAY-23
17420|Strelley Granite|Extent|The Strelley Granite is bounded by the Soanesville Belt, the Lalla Rookh and Pilgangoora Synclines (see Fig. 1). The unit is egg-shaped and crops out over an area of 180 km2 between latitudes 21o09'S and 21o21'S, and longitudes 119o06'E and 119o13'E.|16-MAY-23
17420|Strelley Granite|Lithology|The Strelley Granite consists of two units, a younger porphyritic biotite hornblende granite in the central and western portion (95 km2) intruding an outer margin of granophyre and alkali-feldspar granite (85 km2). i) Porphyritic biotite hornblende Granite: the central unit is a medium to coarse-grained porphyritic biotite hornblende granite. A moderate foliation is exhibited by biotite schlieren and alignment of phenocrysts and feldspar, biotite, and quartz grains in the groundmass. There are numerous medium even-grained and locally porphyritised granitic xenoliths which are often elongate parallel to the host rock foliation. Phenocrysts of Carlsbad-twinned perthite are set in an hypidiomorphic granular textured groundmass of perthite, oligoclase, quartz, hornblende, and biotite. Oligoclase is fresh to moderately sericitized, and partly albite-rimmed. There are accessory magnetite, apatite and zircon. Secondary minerals are epidote, chlorite and sericite.  ii) Medium to coarse, even-grained granophyre and alkali-feldspar Granite: The outer zone of the Strelley Granite consists of grey, medium to coarse, even-grained granophyre in the eastern portion grading northwards into a medium to coarse-grained, locally sheared alkali-feldspar granite, and grading westwards into medium, even-grained massive granite spotted with biotite and containing minor feldspar phenocrysts. The unit is cut by fine to medium even-grained granitic dykes with a lower biotite content than the host. The granophyre is massive to poorly foliated with no pegmatite veins. Radial jointing is prominent and there are some quartz veins along shears. The granophyre consists of a granophyric intergrowth between calcic oligoclase and quartz with some euhedral quartz and microcline crystals and minor anhedral calcic oligoclase, perthite and chlorite grains. Accessory minerals are pyrite, magnetite, zircon, rutile and rare ragged grains of colourless clinopyroxene. Sericitization is pervasive. Secondary calcite is common and there is minor epidote. The medium to coarse-grained, massive alkali feldspar granite in the northwestern portion of the unit contains microcline, perthite, minor biotite and zircon with accessory opaques and sphene, and secondary chlorite, epidote and rutile.|16-MAY-23
17420|Strelley Granite|Relationships and boundaries|Within the Strelley Granite, the outer alkali-feldspar granite-granophyre unit is intruded by the porphyritic hornblende-biotite granite. A distinctive white columnar-jointed, amygdaloidal rhyolite is conformable around the eastern margin of the granophyre, suggesting a genetic relationship. In detail however, the granophyre is locally intrusive into the rhyolite. The structure resembles the cauldron subsidence complex of the younger Nigerian granites (MacLeod et al., 1971). Both granite units are well jointed, and faulted and intruded by dolerite and coarse gabbro dykes. Both units intrude the surrounding Archaean greenstones. Several large masses of Archaean basalt enclosed by the pluton may have been roof pendants. Both units are well exposed as rocky ridges and only locally obscured by thin Quaternary sand.|16-MAY-23
17420|Strelley Granite|Age reasons|Archaean.|16-MAY-23
17420|Strelley Granite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, WA: West. Australian Geol. Survey Rec. 1974/20 West. Australia Geol. Survey Ann. Rept 1974|16-MAY-23
17420|Strelley Granite|Name first published by|Hickman A.H., 1975|16-MAY-23
32536|Sweetwaters Well Member|Name source|Sweetwaters Well, MERRIE (Fig. 1). `Sweetwaters Well'  is used rather than the shorter 'Sweetwaters'  because the name Sweetwater Formation is reserved for use in the Northern Territory.|16-MAY-23
32536|Sweetwaters Well Member|Type section locality|Around the southern margin of an island in Lake Nabberu (NABBERU, MGA 272000E, 7144800N* to 272500E, 7145300N; Fig. 1). The exposures near Sweetwaters Well (MGA 238800E, 7164800N) are a reference locality, and between 314.5 and 373.8 m drilled depth in drillhole DDH 28 (NABBERU, MGA 264200E, 7161250N; core held by Geological Survey of Western Australia (GSWA) is a reference section.|16-MAY-23
32536|Sweetwaters Well Member|Extent|The Sweetwaters Well Member is recognized along the southwestern and western margins of the Earaheedy Basin. Scattered carbonate rocks along the deformed northern margin on METHWIN (Hocking and Jones, 1999) and FAIRBAIRN (Adamides et al., 1999) may be part of the member, but are not formally assigned to it because their stratigraphic position is uncertain. They may be at the same level or facies equivalents lower in the Yelma Formation.|16-MAY-23
32536|Sweetwaters Well Member|Thickness range|The Sweetwaters Well Member is commonly about 100 m thick in complete sections, with a maximum thickness of 151 m in drillhole TDH 1 on NABBERU.|16-MAY-23
32536|Sweetwaters Well Member|Lithology|The characteristic lithology is stromatolitic and laminated dolomite, locally brecciated and commonly chertified. Minor siltstone and sandstone interbeds are present within the member, and metre-scale shallowing-upward cyclicity can be seen in most exposures. Stromatolites include Asperia digitata Grey 1984 (Grey, 1994; restricted, quiet-water environment, possibly supratidal pond), Pilbaria deverella Grey 1984 (moderately high energy, lagoonal environment), Ephyaltes edingunnensis Grey 1984 (deeper quiet-water environment), and Murgurra nabberuensis Grey 1984 (patch reef, moderate energy environment). The stromatolite types and the shallowingupward cyclicity are similar to those in the Duck Creek Dolomite (upper Wyloo Group; Grey, (1994), 500 km to the northwest. Tepee structures, crystal-mush horizons, and flat-pebble carbonate conglomerate can be recognized in drillcore from the unit. The remainder of the Yelma Formation is a siliciclastic succession of mixed sandstone and siltstone, with minor amounts of conglomerate in the north and west.|16-MAY-23
32536|Sweetwaters Well Member|Relationships and boundaries|The Sweetwaters Well Member is at or near the top of the Yelma Formation. Sandstone and siltstone locally overlie it, below the lowest iron formation of the Frere Formation.|16-MAY-23
32536|Sweetwaters Well Member|Age reasons|Palaeoproterozoic. The age of the Earaheedy Group is poorly constrained. The group was unaffected by the c. 1800 Ma Capricorn Orogeny (Tyler et al., 1998), which suggests, but does not prove, that it postdates the orogeny. The Earaheedy Group was deformed in the Stanley Fold Belt prior to the deposition of the Bangemall Supergroup, possibly during the c. 1760 Ma second phase of the Yapungku Orogeny (Bagas and Smithies, 1998).  Glauconite from the Yelma Formation (at the base of the Earaheedy Group) on the DUKETON 1:250 000 sheet gave minimum K/Ar ages of about 1700 Ma and minimum Rb/Sr ages of between 1590 and 1710 Ma (Preiss et al., 1975). Horwitz (1975) reported a K/Ar age of 1688 +/- 72 Ma from glauconite in sandstone of the Wandiwarra Member (near the middle of the group). However, K/Ar isotopic dating is subject to resetting and this may have happened to glauconite from rocks of the Earaheedy Group. A major dynamic and thermal event in the region was the meteorite impact that formed the Shoemaker impact structure, for which a whole-rock Rb/Sr date of 1630 Ma was determined (Pirajno and Glikson, 1998). Richards and Gee (1985) reported a lead isotope age of 1700 Ma from galena within stromatolitic dolomite of the upper Yelma Formation. Nelson (1997) obtained a U/Pb sensitive high-resolution ion microprobe (SHRIMP) age of 1785 ± 11 Ma on detrital zircons from the Mount Leake Formation (on the PEAK HILL 1:250 000 sheet), which may correlate with the basal Yelma Formation, but is geographically isolated from the remainder of the group.|16-MAY-23
32536|Sweetwaters Well Member|Comments|The Sweetwaters Well Member is a distinctive stromatolitic dolomite facies at the top of the Yelma Formation. Jones et al. (in prep.) interpreted the member as a coastal saline lagoon deposit.|16-MAY-23
32536|Sweetwaters Well Member|Defn Reference|SOURCE DOCUMENT::   HOCKING, R. M., JONES, J. A., PIRAJNO, F., and GREY, K., 2000, Revised lithostratigraphy for Proterozoic rocks in the Earheedy Basin and nearby areas: Western Australia Geological Survey, Record 2000/16, 22p.|16-MAY-23
17748|Tambourah Granodiorite|Name source|Tambourah homestead (ruins) (MGR 194 283), Marble Bar 1:250 000 Sheet area.|16-MAY-23
17748|Tambourah Granodiorite|Unit history|The name, Tambourah Granite, was used without definition for the same mass by Noldart and Wyatt (1962).|16-MAY-23
17748|Tambourah Granodiorite|Type section locality|The pluton is well exposed along the Mount Newman Railway. Access is also possible by poor quality station tracks leading southwards from the main road southeast of Woodstock. Elsewhere access by vehicle is extremely difficult.|16-MAY-23
17748|Tambourah Granodiorite|Extent|The Tambourah Granodiorite is a large oval-shaped pluton, elongate towards the north-northeast, located in the central southern  portion of the Marble Bar 1:250 000 Sheet area. The pluton crops out over an area of 665 km2 between latitudes 21o41'S and 22o03'S and longitudes 118o57'E and 119o12'E.|16-MAY-23
17748|Tambourah Granodiorite|Lithology|The Tambourah Granodiorite is a well foliated, nebulitic to stromatically banded, locally gneissose or schistose, medium to coarse-grained biotite granodiorite. Thin leucosome bands have formed parallel to the foliation. Coarse discordant pegmatites occur within the mass and are common in its northern portion. North of Tambourah these contain lepidolite. Alignment of biotite, feldspar and quartz grains and leucosome veins and mafic schlieren and bands form a moderate to prominent foliation. The pluton margins are strongly schistose and contain abundant xenoliths of Archaean basalt. Schistosity is most pronounced along the western margin. The pluton is dominantly a biotite granodiorite in composition but grades into biotite adamellite in its northern portion. In the southwestern part, the mass contains calcic oligoclase (An27), quartz, microcline, biotite and locally minor hornblende. There are accessory  opaques, apatite, zircon and ?allanite. Secondary minerals are chlorite (after biotite), calcite, epidote, sericite and locally prehnite. The texture varies from poorly foliated metamorphic granofels to banded and gneissose. The rock contains coarse-grained, massive, igneous-textured veins of leuco-granite containing well twinned perthitic microcline poikilitically enclosing albite-rimmed plagioclase and with oligoclase, accessory biotite and rare opaques, sphene and zircon. The central portion of the mass was unvisited. The composition of the pluton in the northern portion is generally biotite adamellite to granodiorite with oligoclase, quartz, microcline, moderate to minor biotite and accessory ilmenite, sphene, zircon, apatite, ?allanite and locally fluorite. Secondary minerals are chlorite, muscovite and epidote. Small veins of pumpellyite and ankerite were noted. Microcline is well twinned. Oligoclase is sericitized and biotite is chloritized. The texture varies from allotriomorphic granular to foliated and gneissose. Specimens 1 km and 4 km northwest from Tambourah (GSWA 7342 and 7339 respectively) are described by Wyatt (1962 p.173-185), including analyses indicating 71.1 and 71.7 percent silica content. Further north-west from Tambourah, the pluton is a gneissic biotite hornblende tonalite with a moderate proportion of hornblende and only accessory microcline.|16-MAY-23
17748|Tambourah Granodiorite|Relationships and boundaries|The Tambourah Granodiorite intrudes the surrounding Archaean greenstones on the eastern, northern and northwestern margins. It is sheared against the migmatitic root zone of the greenstone belt along its western margin. The pluton is intruded by a small medium to coarse, even-grained biotite adamellite mass in the northern end of the pluton which is probably remobilized material from, and containing abundant xenoliths of Tambourah Granodiorite. The Granodiorite is intruded by north-northeast trending Archaean dolerite and felsic dykes and by west-northeast trending Archaean dolerite and felsic dykes and by west-northwest-trending Proterozoic dolerite dykes. Along the southern margin, the pluton is unconformably overlain by the Mingah Tuff Member of the Tumbiana Formation (and by theKylena Basalt on the Roy Hill 1:250 000 Sheet area). The pluton is well jointed. Faults are generally denoted by quartz-veining. The rock is only locally obscured by thin Quaternary colluvium. The centre of the mass, which was not visited, crops out as rugged hills and ridges. A dark satellite (ERTS) photo-pattern similar to that of the Moolyella and Cooglegong Adamellite and other cassiterite-bearing Upper Archaean Adamellites, may indicate the presence of a younger granitic unit included with the Tambourah Granodiorite.|16-MAY-23
17748|Tambourah Granodiorite|Age reasons|Archaean|16-MAY-23
17748|Tambourah Granodiorite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, WA: West. Australia Geol. Survey Rec. 1974/20 West. Australia Geol. Survey Ann. Rept 1974.|16-MAY-23
27580|Tandalgoo Sandstone|Name source|The Tandalgoo Red Beds was formally defined by Koop (1966). The type section for this unit occurs in WAPET Sahara 1 well between 1128 m and 1727 m. Under the Stratigraphic Code (1973), the Tandalgoo Red Beds fulfilled the requirements for the definition of a formation. However, under the revised version of the Australian Stratigraphic Code, all units with the name "Beds" were given a lower case "b" for beds.  Since the Tandalgoo Red Beds definition is a formation definition, and so that this formational status can be preserved, the name has been changed to Tandalgoo Sandstone.|16-MAY-23
27580|Tandalgoo Sandstone|Type section locality|The type section for this unit occurs in WAPET Sahara 1 well between 1128 m and 1727 m [as per the type section for the Tandalgoo Red Beds of Koop (1966).].|16-MAY-23
27580|Tandalgoo Sandstone|Proposed publication|Summary Geology of onshore Canning Basin, BMR Bulletin 215|16-MAY-23
27580|Tandalgoo Sandstone|Defn Reference|83/23481|16-MAY-23
17925|Teichmans Group|Name source|Teichmans Gold Mine (abandoned); grid reference 21o16'N, 118o12'E, Pyramid 1:250 000 Sheet area.|16-MAY-23
17925|Teichmans Group|Unit history|Equated with Nickel River Formation on Yarraloola 1:250 000 Sheet and Talga Talga/Salgash Subgroups on Marble Bar and Nullagine 1:250 000 sheets (Hickman) & Lipple, in press).|16-MAY-23
17925|Teichmans Group|Type section locality|3.15 km of dominantly mafic and ultramafic volcanic rocks, intercalated banded cherts, minor acid volcancis and volcanoclastic sediments. Typical "greenstone" succession.|16-MAY-23
17925|Teichmans Group|Extent|The group occurs throughout the West Pilbara Goldfield but is best developed between Teichmans Gold Mine and the Yule River.|16-MAY-23
17925|Teichmans Group|Thickness range|Range 1-4 km|16-MAY-23
17925|Teichmans Group|Relationships and boundaries|Oldest known Archaean rocks in West Pilbara Goldfield. Basal unit intruded by diapiritic ganites. Overlain conformably by Gorge Creek Group.|16-MAY-23
17925|Teichmans Group|Age reasons|Lower Archaean > 3000 m.y.|16-MAY-23
17925|Teichmans Group|Defn author|Fitton M.J., Horwitz R.C., Sylvester G., 1975|16-MAY-23
17925|Teichmans Group|Proposed publication|CSIRO, Minerals Research Laboratories, Report No. FP 11.|16-MAY-23
17925|Teichmans Group|Comments|Notes on this Group were previously included as part of the Regal Formation of the Roebourne Group on both the Roebourne and Pyramid 1:250 000 Sheets.|16-MAY-23
27910|Thaduna Greywacke|Name source|Thaduna Mine, Peak Hill,1:250 000 Sheet.|16-MAY-23
27910|Thaduna Greywacke|Unit history|Thaduna Beds (MacLeod 1970).|16-MAY-23
27910|Thaduna Greywacke|Type section locality|Thaduna Mine area.|16-MAY-23
27910|Thaduna Greywacke|Extent|Throughout western part of Nabberu Basin.|16-MAY-23
27910|Thaduna Greywacke|Thickness range|Uncertain - about 4 km|16-MAY-23
27910|Thaduna Greywacke|Lithology|Feldspathic and lithic greywacke, displaying turbidity current features.|16-MAY-23
27910|Thaduna Greywacke|Relationships and boundaries|Lateral equivalent to Doolgunna-Karalundi-Narracoota stratigraphic interval.|16-MAY-23
27910|Thaduna Greywacke|Age reasons|Proterozoic - probably 2.0-1.8. b.y.|16-MAY-23
27910|Thaduna Greywacke|Proposed publication|Western Australia Geological Survey Annual Report for 1978 Pub. 1979)|16-MAY-23
27910|Thaduna Greywacke|Defn approved by|M.H. Johnstone, Western Australia Strat Names Committee.|16-MAY-23
24541|Turkey Hill Beds|Name source|Turkey Hill; Lat 28o07'S; Long. 124o16.5'E; Rason 1:250 000 Sheet area.|16-MAY-23
24541|Turkey Hill Beds|Unit history|Gower and Boegli (1973) describe this unit as an unnamed deposit in the section "Proterozoic geology".|16-MAY-23
24541|Turkey Hill Beds|Type section locality|The immeidate vicinity of Miller Soak, 6 km to the south of Turkey Hill.|16-MAY-23
24541|Turkey Hill Beds|Extent|The unit is exposed on the Rason 1:250 000 Sheet area around Turkey hill from Miller Soak to Stoney Point (south of Lake Yeo) and near Point Salvation.|16-MAY-23
24541|Turkey Hill Beds|Thickness range|Several hundred metres|16-MAY-23
24541|Turkey Hill Beds|Lithology|Sandstone: fine-grained sandstone, siltstone and claystone; may include diamictite (tillite) but structural and stratigraphic relations of the diamictite occurrence and sandstone are not clear.|16-MAY-23
24541|Turkey Hill Beds|Relationships and boundaries|Is believed to nonconformably overlie granite near Point Salvation. Base of unit not known in type area. Unconformably overlain by Permian Paterson Formation.|16-MAY-23
24541|Turkey Hill Beds|Age reasons|Proterozoic - because of its steep dips (up to 65o) in the little deformed Officer Basin sequence, and the fact that it is overlain by flat-lying Permian Paterson Formation the unit is considered to be Proterozoic in age. If the diamictite indeed forms part of the sandstone sequence the Miller Soak Beds will correlate with the Late Proterozoic glacials.|16-MAY-23
24541|Turkey Hill Beds|Proposed publication|The geology of the Western Australian part of the Officer Basin; GSWA and BMR bulletin|16-MAY-23
24541|Turkey Hill Beds|Proposer|van de Graaff W.J.E.|16-MAY-23
24541|Turkey Hill Beds|Resdate|15-JAN-1975|16-MAY-23
25697|Wandarry Shale Member|Name source|The Wandarry Shale Member is a new member of the Ashburton Formation (de la Hunty, 1965) of the redefined Wyloo Group (Trendall, 1979) south of the Ashburton River on the Turee Creek Geological Sheet area (Daniels, 1968). The name is derived from Wandarry Creek, south of Ashburton Downs.|16-MAY-23
25697|Wandarry Shale Member|Extent|The Wandarry Shale Member is the lowest exposed unit of the Ashburton Formation in the Ashburton Trough (Gee, 1979), first defined Wyloo Trough (Horwitz & Smith, 1978), on the Turee Creek Sheet area.  To the north, it is overlain by the Capricorn Member (redefined). The base is not exposed, to the south it is overlapped by the Bangemall Group (of Daniels & MacLeod, 1965).|16-MAY-23
25697|Wandarry Shale Member|Thickness range|It is estimated to be at least 3000 m thick and composed dominantly of silty shales with minor fine to medium grained greywackes. Some rare, thin, white flinty, tuffaceous bands occur which exist in all three members of the Ashburton Formation of the Turee Creek Sheet area.|16-MAY-23
25697|Wandarry Shale Member|Relationships and boundaries|The boundary with the overlying Capricorn Member was set at the first appearance of coarse sandy or gritty beds or at the first appearance of foreign slabs in silty shales. No type area was established.|16-MAY-23
25697|Wandarry Shale Member|Proposed publication|Aust. CSIRO Inst. Earth Res. Rept No. FP 22|16-MAY-23
25697|Wandarry Shale Member|Proposer|Horwitz R.C.|16-MAY-23
25697|Wandarry Shale Member|Resdate|21-JUN-1979 / 12-FEB-1980|16-MAY-23
24555|Wandy Wandy Shale|Name source|Wandy Wandy Creek' Lat. 21o29'S, Long. 121o15'E, gives its name to the region containing the type area. Nullagine 1:250 000 Sheet area.|16-MAY-23
24555|Wandy Wandy Shale|Type section locality|As above.|16-MAY-23
24555|Wandy Wandy Shale|Extent|Western margin of the Great Sandy Desert 25 km east of Mt Sydney, Lat. 21o24'S, Long. 121o11'E.|16-MAY-23
24555|Wandy Wandy Shale|Thickness range|At least 1000 m (poor exposure).|16-MAY-23
24555|Wandy Wandy Shale|Lithology|Reddish brown cleaved pelitic rocks.|16-MAY-23
24555|Wandy Wandy Shale|Relationships and boundaries|Overlies, apparently conformably, the Bocrabee Sandstone (de la Hunty, 1964).|16-MAY-23
24555|Wandy Wandy Shale|Age reasons|Proterozoic|16-MAY-23
24555|Wandy Wandy Shale|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan Notes, Nullagine|16-MAY-23
24555|Wandy Wandy Shale|First Reference|81/22261|16-MAY-23
24555|Wandy Wandy Shale|Proposer|Hickman A.H.|16-MAY-23
24555|Wandy Wandy Shale|State(s)|WA |16-MAY-23
24576|Wilthorpe Conglomerate|Name source|Wilthorpe Gold Mine (Abu) Robinson Range 1:250 000 Sheet.|16-MAY-23
24576|Wilthorpe Conglomerate|Type section locality|5 km ENE of Wilthorpe Mining Centre|16-MAY-23
24576|Wilthorpe Conglomerate|Extent|Mt Padbury-Mt Fraser-Wilthorpe area.|16-MAY-23
24576|Wilthorpe Conglomerate|Thickness range|1000 metres|16-MAY-23
24576|Wilthorpe Conglomerate|Lithology|Boulder and pebble conglomerate, granule sandstone|16-MAY-23
24576|Wilthorpe Conglomerate|Relationships and boundaries|Forms base of Padbury Group, unconformably overlies Labouchere Formation.|16-MAY-23
24576|Wilthorpe Conglomerate|Age reasons|Proterozoic - probably 1.8-1.7 b.y.|16-MAY-23
24576|Wilthorpe Conglomerate|Proposed publication|Western Australia Geological Survey Annual Report for 1978 (Pub. 1979)|16-MAY-23
24576|Wilthorpe Conglomerate|Proposer|Gee R.D.|16-MAY-23
20224|Windimurra Intrusion|Name source|Windimurra homestead, lat. 28o19'35"S, long. 118o32'50"E, in western part of Youanmi 1:250 000 Sheet area.|16-MAY-23
20224|Windimurra Intrusion|Unit history|Windimurra Complex of de la Hunty L.E., 1970, Rept Dept Mines WA for 1969, 53.  Windimurra Gabbro, de la Hunty, 1973, Cue 1:250 000 geological series. Geol. Surv. West. Aust. Explan. Notes SG/50-15  Windimurra Complex, Williams I.R., 1974, Rept Dept Mines WA for 1973, 53-59. Windimurra Intrusion, Gee R.D., 1975, in Knight C.L. (Ed.) Economic Geology of Australia and Papua New Guinea - I Metals.  Aust. Inst. Min. Metall. Monogr. Ser. 5, 43-55.|16-MAY-23
20224|Windimurra Intrusion|Type section locality|Series of north-south ridges extending E/W over 3 km between lat. 28o17'30"S, long. 118o32'30"E, and lat. 28o17'30"S, long. 118o34'00"E, 4 km north of Windimurra homestead.|16-MAY-23
20224|Windimurra Intrusion|Extent|Northwest part of Youanmi, and extends into Kirkalocka, Cue and Sandstone. Total area 2120 km2 (exclusive of overlying felsic volcanics).|16-MAY-23
20224|Windimurra Intrusion|Lithology|Comprises scores of layers about 1 to 50 m thick composed of gabbro, dolerite, norite, olivine norite, clinopyroxene norite, melagabbro, leucogabbro, leuconorite, hypersthene melagabbro, pyroxenite, anorthosite, and magnetite rock; layers and masses of gabbro pegmatite and veins of microdolerite and microdiorite are also regarded as part of the Intrusion. Cumulate textures well preserved. Original igneous assemblage preserved in many places, elsewhere partly or completely metamorphosed to greenschist facies.|16-MAY-23
20224|Windimurra Intrusion|Relationships and boundaries|Intrudes and hornfelses sedimentary country rock and felsic volcanic rocks of Kantie Murdanna Volcanics (Baxter, J.L., Lipple S.L., & Marston, R.J., 1980 - Explanatory notes on the Kirkalocka 1:250 000 geological sheet, Western Australia. Geol. Sur. WA Record 1980/3 (unpubl.). Intruded by plutonic and hypabyssal granitoids, and by E/W dolerite dykes.|16-MAY-23
20224|Windimurra Intrusion|Age reasons|The intrusive granitoid dykes give Rb-Sr whole-rock isotopic dates in excess of 2500 Ma; therefore, the Windimurra Intrusion is Archaean (A. Ahmat & J. de Laeter, pers. comm. 1980).|16-MAY-23
20224|Windimurra Intrusion|Correlations|Co-magmatic with Youanmi Intrusion, a similar layered mafic intrusion 15 km SE of the Windimurra Intrusion.|16-MAY-23
20224|Windimurra Intrusion|Proposed publication|Youanmi 1:250 000 Explan. Notes|16-MAY-23
25648|Woodstock Adamellite|Name source|Woodstock homestead, Marble Bar 1:250 000 Sheet area (MGR 1680 2985).|16-MAY-23
25648|Woodstock Adamellite|Unit history|Noldart and Wyatt (1958, p.39) used the term 'Woodstock-Abydos (Western) Granite' without definition to refer to the entire Yule Batholith.|16-MAY-23
25648|Woodstock Adamellite|Type section locality|The Woodstock Adamellite is well exposed northeast of Mundine Well, around Dead Bullock Well and in the upper reaches of Coorong Creek and the Turner River.|16-MAY-23
25648|Woodstock Adamellite|Extent|The Woodstock Adamellite occurs in the Yule Batholith (see Fig. 1) east and northeast of Woodstock homestead, between latitudes 21o23'S and 21o42'S, and longitudes 118o57'E and 119o07'E. The pluton has an irregular shape, elongate in a longitudinal direction and has an area of about 265 km2.|16-MAY-23
25648|Woodstock Adamellite|Lithology|The Woodstock Adamellite is a medium to coarse, even-grained, well foliated biotite adamellite which contains numerous biotite schlieren, amphibolite and ultramafic xenoliths and abundant medium-grained biotite granodiorite xenoliths. The latter are probably derived from the adjacent migmatite complex. The margins are transitional zones of mixed lithologies, particularly in the southern area. Pegmatites and aplites form a minor feature in most of the pluton. Some pegmatites are quite coarse. Minor microcline phenocrysts up to 1 x 2 cm occur erratically throughout the adamellite, but are more common in the northern portion. Plagioclase is very sericitized over much of the pluton. The primary foliation formed by feldspar, mica, quartz and biotite schlieren has been overprinted or even destroyed by a pronounced tectonic foliation exhibited by quartz, mica and feldspar alignment. In areas of strong deformation, such as along the greenstone margin, feldspar phenocrysts have been altered to augen. The rock is strongly jointed. In the southern portion, inselbergen are prominently developed. Near the road proceeding southeast from Woodstock, some of these inselbergen exhibit coarse magnetite octahedra.|16-MAY-23
25648|Woodstock Adamellite|Relationships and boundaries|The Woodstock Adamellite has transitional margins with the adjacent migmatite complex (Agm) and xenoliths are abundant throughout the pluton. This suggests that it has been remobilized from the migmatite and emplaced at a higher structural level. The pluton intrudes Archaean greenstones along the southeastern margin, but the contact along the north-eastern margin consists of a major fault. The Woodstock Adamellite has sharper intrusive contacts with the older Abydos Adamellite than those with the migmatite but the former contacts are still of a transitional nature, often extending over 1-2 km. The Adamellite has sharp intrusive contacts along the northern margin with older fine-grained biotite granodiorite (Agt). The latter exhibits pegmatites and porphyroblasts formed by the Woodstock Adamellite. The Woodstock Adamellite is extensively faulted and quartz veins occur along some faults. The rock is intruded by dolerite dykes including Lower Proterozoic dolerite of the Mundine Well suite. The unit is locally obscured by thin deposits of Quaternary sand and gravel. In the northern portion, small mesas of Tertiary pisolite unconformably overlie the Adamellite.|16-MAY-23
25648|Woodstock Adamellite|Age reasons|Archaean|16-MAY-23
25648|Woodstock Adamellite|Proposed publication|Explan. Notes on Marble Bar 1:250 000 Sheet area, WA: West. Australia Geol. Survey Rec. 1974/20 West. Australia Geol. Survey Ann. Rept 1974.|16-MAY-23
25648|Woodstock Adamellite|Status|1|16-MAY-23
20796|Yampi Member|Name source|From Yamp Sound; Yampi 1:250 000 Sheet area; Yampi Sound 1:100 000 (proposed)|16-MAY-23
20796|Yampi Member|Type section locality|(1962E, 29290N) on south side of Shoal Bay; Cockatoo Island (Reid 1958, Table 2).|16-MAY-23
20796|Yampi Member|Description at type locality|Rocky, steep-sided plateaux on islands to north of Yampi Sound; photo-pattern is striped due to rapid alternation of hard hematitic sandstone and soft siltstone. Rounded hills and cuestas in the east.|16-MAY-23
20796|Yampi Member|Extent|A semi-continuous belt from Bathurst Island eastwards to Eagle Point. Includes Cockatoo, Koolam and Wood Islands.|16-MAY-23
20796|Yampi Member|Thickness range|1600 feet on south side of Shoal Bay; 1400-1800 feet on Cockatoo Island (Reid 1958).|16-MAY-23
20796|Yampi Member|Lithology|Hematitic sandstone and minor hematite rock; pale brown feldspathic sandstone and arkose; siltstone; minor grey glauconitic sandstone.|16-MAY-23
20796|Yampi Member|Relationships and boundaries|Apparently conformable on lower beds (white quartz sandstone) of Pentecost Sandstone in east. Apparently conformable (or para-conformable?) on Elgee Siltstone on Yampi Sound islands.|16-MAY-23
20796|Yampi Member|Identifying features|The high contents of hematite (in the west) and feldspar and hematite in the east, distinguish rocks of this member from the underlying white quartz sandstone of the Pentecost Sandstone.|16-MAY-23
20796|Yampi Member|Age reasons|Lower Carpentarian|16-MAY-23
20796|Yampi Member|Comments|The proposed member formalises the previously undefined "Yampi Beds" of Harms (1959). Lateral equivalents of both the lower part of the Pentecost Sandstone and of the Yampi Member in the area between Talbot Bay and Strickland Bay comprise a uniform siltstone sequence that has not been subdivided.|16-MAY-23
26247|Yilgalong Granite|Name source|Yilgalong Creek', Nullagine, 1:250 000 Sheet area.|16-MAY-23
26247|Yilgalong Granite|Unit history|Informally referred to as Elsie Creek batholith by Noldart and Wyatt (1962), p.98.|16-MAY-23
26247|Yilgalong Granite|Type section locality|As above.|16-MAY-23
26247|Yilgalong Granite|Extent|500 km2 in the headwaters of Yilgalong Creek.|16-MAY-23
26247|Yilgalong Granite|Lithology|Biotite granite to biotite adamellite, locally ;migmatitic and commonly sheared.|16-MAY-23
26247|Yilgalong Granite|Relationships and boundaries|Unconformably overlain by Fortescue Group (MacLeod and others, 1963) in north and east. Locally intrusive into Warrawoona Group (Lipple, 1975) and sheared with Warrawoona Group by Archaean deformation in west and south.|16-MAY-23
26247|Yilgalong Granite|Age reasons|Archaean, for reasons given above.|16-MAY-23
24600|Youanmi Intrusion|Name source|Youanmi townsite, lat. 28o37'00"S, long. 118o50'00"E, in southwest of Youanmi 1:250 000 Sheet area.|16-MAY-23
24600|Youanmi Intrusion|Type section locality|Small well exposed prominent rocky hill about 800 m across and 10 m high situated at lat. 28o38'25"S, long. 118o43'00"E, 11 km west-southwest of Youanmi townsite.|16-MAY-23
24600|Youanmi Intrusion|Extent|Oval area about 20 km by 10 km extending southwest from Youanmi to Freddie Well.|16-MAY-23
24600|Youanmi Intrusion|Lithology|Numerous layers up to about 10 m thick composed of gabbro, leucogabbro, norite, melagabbro, pyroxenite, anorthosite, and magnetite. Original igneous assemblage preserved at type locality; commonly metamorphosed to greenschist facies elsewhere.|16-MAY-23
24600|Youanmi Intrusion|Relationships and boundaries|Intrudes metamorphosed felsic volcanics at Freddie Well zinc prospect, 3 km west of Freddie Well. Intruded by lepidolite-bearing granite pegmatite.|16-MAY-23
24600|Youanmi Intrusion|Age reasons|Presumbed to be co-eval with Windimurra Intrusion; Archaean.|16-MAY-23
24600|Youanmi Intrusion|Correlations|Co-magmatic with Windimurra Intrusion, 15 km to the northwest.|16-MAY-23
24600|Youanmi Intrusion|Proposed publication|Youanmi 1:250 000 Explan. Notes, BMR|16-MAY-23
24600|Youanmi Intrusion|Reserved? Yes/No|Yes|16-MAY-23
24600|Youanmi Intrusion|Unit name|Youanmi Intrusion (formal)|16-MAY-23
