Stratno | Stratigraphic Name | Category | Contents | Last update 
24150|Airport Creek Formation|Name source|Airport Creek; mouth of creek grid reference 121817, Derby 1:250 000 sheet.|16-MAY-23
24150|Airport Creek Formation|Type section locality|3 metres of partly indurated laminated sediment is exposed along banks and at the mouth of Airport Creek.  The top is in sharp contact with a grey soil unit called Double Nob Formation;  the base is not exposed.|16-MAY-23
24150|Airport Creek Formation|Extent|The unit is exposed along banks of Airport Creek, Doctors Creek and low tide zones near Derby.  Total outcrop and subsurface distribution is in excess of 200 km2. |16-MAY-23
24150|Airport Creek Formation|Thickness range|8 metres plus;  determined by coring under Derby Jetty;  base not reached.|16-MAY-23
24150|Airport Creek Formation|Lithology|Interlayered grey to buff calcareous and siliciclastic laminates, sandstone and sponge spicules in the sandstones.|16-MAY-23
24150|Airport Creek Formation|Relationships and boundaries|Basal relationships not accurately known; on shore the unit overlies Mowanjum Sands, as determined by augering at grid reference 123822, Derby Sheet area 1:250 000.  The unit is overlain by Double Nob Formation (soil) with gradational contact and locally by Doctors Creek Formation with sharp contact.|16-MAY-23
24150|Airport Creek Formation|Age reasons|Criteria of unconformity, weathering features and overlying soil unit place the unit in the Pleistocene (or ?Pliocene).|16-MAY-23
79060|Angas Hills Formation|Name source|Angas Hills (latitude 22° 52' S, longitude 128° 9' E).|16-MAY-23
79060|Angas Hills Formation|Unit history|Previously named Angas Hills beds (Blake and Towner, 1974; Blake, 1977).|16-MAY-23
79060|Angas Hills Formation|Geomorphic expression|Low hills, scarps, rises and plateaus.|16-MAY-23
79060|Angas Hills Formation|Type section locality|A cliff section 36 m high in the eastern Angas Hills, 12 km NE of Mt Webb (latitude 22° 51' 00"S, longitude 128° 12' 30"E), the reference section nominated by Blake and Towner (1974). Closest access is via a track from Kiwirrkurra to Lake Mackay.|16-MAY-23
79060|Angas Hills Formation|Extent|Known outcrops are restricted to the southern half of the Webb 1:250 000 scale map sheet in WA, most notably around the Angas Hills. The unit is restricted to outliers of the Amadeus Basin lying within basement of the Arunta region.|16-MAY-23
79060|Angas Hills Formation|General description|Regionally the unit consists of interbedded pebble and cobble conglomerate, sandstone, pebbly sandstone and siltstone. Pebble and cobble clasts are typically well rounded and are mainly of sedimentary or metasedimentary lithologies including quartzite, sandstone, metasandstone and chert, with minor vein quartz. Carbonate clasts were identified locally. The clayey sandstone matrix is friable and some exposures are limited to loose rounded pebbles and cobbles. Sandstone and siltstone are typically red-brown in colour due to iron oxides. Sandstones may be quartz-rich, but also contain a lithic content and clay matrix. Cross beds are common in sandstone facies while siltstones are finely laminated.|16-MAY-23
79060|Angas Hills Formation|Thickness range|About 300 m is exposed on the west side Angas Hills where the formations dips 15° to 20° southeast (Blake and Towner, 1974); this is a minimum thickness for the unit in this area as neither base nor top are exposed.|16-MAY-23
79060|Angas Hills Formation|Thickness range|About 36 m exposed at the type locality (Blake and Towner, 1974).|16-MAY-23
79060|Angas Hills Formation|Lithology|Based on Towner and Blake (1974) the basal 12 m at the type locality consists of coarse pebble conglomerate with some thin lenses and layers of clayey sandstone. The conglomerate is overlain by 24 m of partly pebbly cross-bedded sandstone, in the middle of which there are some interbeds of maroon mudstone about 10 cm thick. At this locality the strata dip 10° west.|16-MAY-23
79060|Angas Hills Formation|Depositional environment|Fluvial based on sedimentary facies. Paleocurrent data indicates derivation from the southwest. Detrital zircon data indicates derivation of the sandy component largely from the Musgrave region, consistent with deposition during the Petermann Orogeny. The laminated siltstones probably represent local lacustrine facies.|16-MAY-23
79060|Angas Hills Formation|Fossils|None observed.|16-MAY-23
79060|Angas Hills Formation|Diastems or hiatuses|None observed.|16-MAY-23
79060|Angas Hills Formation|Relationships and boundaries|Unconformably overlies Arunta region basement, Heavitree Quartzite and probably Bitter Springs Formation (Blake and Towner, 1974). Overlain by Cenozoic units.|16-MAY-23
79060|Angas Hills Formation|Identifying features|May be distinguished from pebbly sandstone, conglomerate and diamictite of the partly glacigene Permo-Carboniferous Paterson Formation by its deep red-brown colouration (freshly broken Paterson formation is typically white) and the lack of evidence for glacial influence.|16-MAY-23
79060|Angas Hills Formation|Structure and Metamorphism|Mostly flat lying or gently dipping (locally up to 20°), and unmetamorphosed.|16-MAY-23
79060|Angas Hills Formation|Age reasons|Upper Ediacaran to lower Cambrian based on detrital zircon provenance data (Wingate et al., 2013) which suggests deposition synchronously with the Petermann Orogeny (Haines et al., 2012). This is also supported by paleocurrent data (transport from the southwest) and lithological and clast similarities to Supersequence 4 units in the main part of the Amadeus Basin to the south.|16-MAY-23
79060|Angas Hills Formation|Correlations|Correlated with Supersequence 4 of the main Amadeus Basin, although correlation with any specific units has not been possible.|16-MAY-23
79060|Angas Hills Formation|Alteration and Mineralisation|None known.|16-MAY-23
79060|Angas Hills Formation|Geophysical Expression|Not distinguished on geophysical datasets.|16-MAY-23
79060|Angas Hills Formation|Geochemistry|No data.|16-MAY-23
79060|Angas Hills Formation|Defn author|Peter Haines and Heidi Allen (Geological Survey of Western Australia) 18-MAR-2015; original definition by Blake and Towner (1974).|16-MAY-23
79060|Angas Hills Formation|Comments|Previously inferred to be of late Paleozoic age (Blake and Towner, 1974).|16-MAY-23
79060|Angas Hills Formation|References|Blake, DH 1977, Webb, W.A.: Australia Bureau of Mineral Resources and Geological Survey of Western Australia, 1:250 000 Geological Series Explanatory Notes, 19p.  **Blake, DH and Towner, RR 1974, Geology of the Webb 1:250 000 sheet area, Western Australia: Australia Bureau of Mineral Resources Record 1974/53. **Haines, PW, Allen, HJ, Grey, K and Edgoose, C 2012, The western Amadeus Basin: revised stratigraphy and correlations, in Central Australian Basin Symposium III edited by GJ Ambrose and J Scott: Petroleum Exploration Society of Australia, Special Publication, CD-ROM, 6p. **Wingate, MTD, Kirkland, CL and Haines, PW 2013, 143741: sandstone, Angas Hills; Geochronology Record 1106: Geological Survey of Western Australia, 5p.|16-MAY-23
79992|Anthiby Formation|Name source|Named after Anthiby Well (Lat. -22.86056 Long. 116.73472), about 35 km west of the proposed type section, on the HARDEY 1:100 000 mapsheet|16-MAY-23
79992|Anthiby Formation|Unit history|The Anthiby Formation is equivalent to part of Trendall?s (1979) 'unnamed quartzite unit 3', all of 'quartzite 3' of Krapez et al. (2017), and the `upper Kazput Formation? of Martin et al. (2000) and Martin and Morris (2010). Goddard (1992) and Powell and Horwitz (1994) were the first to recognise a separate unconformity-bound unit below the Beasley River Quartzite in the core of the Hardey Syncline, distinct from 'unnamed quartzite unit 3'. This unit was later referred to as the 'upper Kazput Formation' by Martin et al. (2000) in order to distinguish it from the remainder of the Kazput Formation as originally defined by Thorne and Tyler (1996).|16-MAY-23
79992|Anthiby Formation|Constituents|N/A|16-MAY-23
79992|Anthiby Formation|Geomorphic expression|The Anthiby Formation forms a distinctive, slightly recessive-weathering unit below the Beasley River Quartzite wherever it is exposed.|16-MAY-23
79992|Anthiby Formation|Type section locality|2 km west of Cajuput Yard on Rocklea 1:100 000 sheet (Lat. -22.895 Long. 117.094). The proposed type section starts at Lat. -22.8848 Long. 117.0544, and follows a north-south trending creek on the northern limb of the Hardey Syncline.|16-MAY-23
79992|Anthiby Formation|Extent|Restricted to the Hardey Syncline.|16-MAY-23
79992|Anthiby Formation|Thickness range|71 m measured in the type section, but may be up to 100 m. The maximum measured thickness is about 90 m, but exposed sections west of the type area suggest that it may be locally thicker than this.|16-MAY-23
79992|Anthiby Formation|Lithology|[at type locality]. The Anthiby Formation consists mainly of planar-laminated siltstone and mudstone with minor intercalated fine-grained sandstone that is low-angle planar and trough cross-stratified, and also contains hummocky and swaley lamination.|16-MAY-23
79992|Anthiby Formation|Depositional environment|Interpreted to have been deposited in a shallow marine to deltaic environment (Powell and Horwitz, 1994; Martin et al., 2000)|16-MAY-23
79992|Anthiby Formation|Relationships and boundaries|The basal contact is an angular unconformity with the underlying Kungarra Formation. To the west of the type area, the basal unconformity also locally truncates the Munder, Kazput, and Koolbye Formations. The upper contact is a paraconformity to very low-angle unconformity with the Beasley River Quartzite at the base of the Shingle Creek Group.|16-MAY-23
79992|Anthiby Formation|Identifying features|All lithologies are locally manganiferous or ferruginous. Sandstones are locally hummocky and swaley cross-stratified|16-MAY-23
79992|Anthiby Formation|Structure and Metamorphism|The Anthiby Formation preserves a steep south-dipping Ophthalmian cleavage (Powell and Horwitz, 1994) and is metamorphosed to lower greenschist facies.|16-MAY-23
79992|Anthiby Formation|Age reasons|The Anthiby Formation is younger than the c. 2208 Ma Balgara Dolerite which it unconformably overlies in the type area, but 20 km to the west it is apparently cross-cut by discordant Balgara Dolerite sills, suggesting that deposition and sill intrusion took place at c. 2208 Ma|16-MAY-23
79992|Anthiby Formation|Defn author|D. McB. Martin, Geological Survey of Western Australia. 7-JUL-2020.|16-MAY-23
79992|Anthiby Formation|Comments|The Anthiby Formation has commonly been mapped as part of the Beasley River Quartzite. This new definition clearly establishes it as a separate unconformity-bound lithostratigraphic unit.|16-MAY-23
79992|Anthiby Formation|References|Goddard, AB 1992, The deposition style and tectonic setting of the Early Proterozoic Turee Creek Group in the Hardey Syncline, Hamersley Province, Western Australia: Unpublished BSc (Hons) Thesis, University of Western Australia, 94p.  **Krapez, B, Muller, SG, Fletcher, IR and Rasmussen, B 2017, A tale of two basins? Stratigraphy and detrital zircon provenance of the Paleoproterozoic Turee Creek and Horseshoe Basins of Western Australia: Precambrian Research, v. 294, p. 67-90.  **Martin, DMcB and Morris, PA 2010, Tectonic setting and regional implications of ca. 2.2 Ga mafic magmatism in the southern Hamersley Province, Western Australia: Australian Journal of Earth Sciences, v. 57, no. 7, p. 911-931.  **Martin, DMcB, Powell, CMcA and George, AD 2000, Stratigraphic architecture and evolution of the early Paleoproterozoic McGrath Trough, Western Australia: Precambrian Research, v. 99, p. 33-64.  **Powell, CMcA and Horwitz, RC 1994, Late Archaean and Early Proterozoic tectonics and basin formation of the Hamersley Ranges: Geological Society of Australia; 12th Australian Geological Convention, Excursion Guidebook 4, 53p.  **Thorne, AM and Tyler, IM 1996, Geology of the Rocklea 1:100 000 sheet: Geological Survey of Western Australia, 1:100 000 Geological Series Explanatory Notes, 15p.  **Trendall, AF 1979, A revision of the Mount Bruce Supergroup, in Annual Report for the year 1978: Geological Survey of Western Australia, Perth, Western Australia, p. 63-71.|16-MAY-23
24169|Baleine Formation|Name source|Baleine Bank; grid reference 515885, Pender 1:250 000 Sheet area.|16-MAY-23
24169|Baleine Formation|Type section locality|2966-4175 ft (904-1273 m) in Lacepede 1A (17o5'8"S, 121o26'41"E).|16-MAY-23
24169|Baleine Formation|Extent|The unit is present only in the subsurface of the offshore Canning Basin and southern Browse Basin.  Its limit to the east is uncertain, but its absence in either coastal wells or outcrop suggests it is west of the present shoreline.  No western limit is known due to lack of deep sea drilling.|16-MAY-23
24169|Baleine Formation|Thickness range|Drilled thickness ranges from 94 m to 504 m. Isopach contours suggest it thickens to approximately 1000 m in the Rowley Shoals area.|16-MAY-23
24169|Baleine Formation|Lithology|Chiefly claystone, grey, silty to arenaceous, common traces of glauconite as high as 10% and traces of mica and pyrite.  Towards the east the upper part is interbedded sandstone and siltstone.  The sandstone is grey; very fine to coarse grained, grain size decreases downhole to a very fine-grained argillaceous sandstone of siltstone; poor to well sorted with the degree of sorting increasing downhole; clay matrix; traces of glauconite carbonate cement up to 10% in the lower sandstone, and rock fragments.  Siltstone, grey, sandy and argillaceous.|16-MAY-23
24169|Baleine Formation|Relationships and boundaries|Overlies an unnamed Middle-Upper Jurassic sandstone.  Detailed palynological dating has established the disconformity at the base.  The base is easily picked on well logs by the change in lithology from the underlying sandstone to claystone.  The upper contact is less well defined.  Overlain by unnamed Neocomian sandstone or claystone.  Palynological dating indicates the upper contact is disconformable in the east and conformable in the west.|16-MAY-23
24169|Baleine Formation|Age reasons|Late Tithonian to early Neocomian.  The unit is diachronous from east to west.  Dating is based predominately on palynology from wells in the Canning Basin and fauna lists are contained in the offshore well completion reports for Keraudren 1, Bedout 1, Lacepede 1, Wamac 1, East Mermaid 1, Lynhner 1, and Leveque 1.|16-MAY-23
24169|Baleine Formation|Comments|The unit has no onshore correlatives. Previously it has been included in or correlated with the Jarlemai and Jowlaenga Formations. Although the unit has lithological similarities to both formations, it is younger than either formation.|16-MAY-23
24169|Baleine Formation|References|AMAX Petroleum (Australia) Inc, 1973 - Wamac 1, well completion report.  Bur. Miner. Resour. Aust. File 73/246. BOC of Australia, 1970 - Lacepede 1A, well completion report.  Bur. Miner. Resour. Aust. File 70/426 BOC of Australia, 1970 - Leveque 1, well completion report.  Bur. Miner. Resour. Aust. File 70/670. BOC of Australia, 1970 - Lyhner 1, well completion report. Bur. Miner. Resour. Aust. File 70/948 BOC of Australia, 1971 - Bedout 1, well completion report. Bur. Miner. Resour. Aust. File 71/435 Hematite Petroleum Pty Ltd, 1973 - Keraudren 1, well completion report. Bur. Miner. Resour. Aust. File 73/240 Lister T.R., 1972 - An applied scheme of palynomorph units for use in the stratigraphic rationalization of Jurassic-Cretaceous prospects located in the northwest shelf of Australia. Part 1 dinophyte cysts. BOC of Aust. Ltd. (Unpubl. Co. rep.) Powell D.E. 1976 - The geological evolution of the continental margin off northwest Australia. APEA J., 16(1), 13-23. Shell Development Pty Ltd, 1973 - East Mermaid 1, well completion report. Bur. Miner. Resour. Aust. File 73/1002.|16-MAY-23
79384|Balgara Dolerite|Name source|Named after Balgara Well (Lat. -23.18173 Long. 118.30858) in the Turee Creek Syncline on the SNOWY MOUNT 1:100 000 mapsheet.|16-MAY-23
79384|Balgara Dolerite|Unit history|The Balgara Dolerite is synonymous with dolerite sills that were dated at c. 2208 Ma by Muller et al. (2005).|16-MAY-23
79384|Balgara Dolerite|Geomorphic expression|Generally poorly exposed, forming isolated dolerite outcrops, except in the type area where exposure is more continuous. Forms one or more recessive units within the Beasley River Quartzite|16-MAY-23
79384|Balgara Dolerite|Type section locality|The type locality is in the vicinity of Lat. -22.8465 Long. 116.8474 in the Hardey Syncline where the intrusive relationships of the sills are well exposed along a strike length of about 6 km.|16-MAY-23
79384|Balgara Dolerite|Extent|Present throughout the southern and southwestern Hamersley province, on the WYLOO, MOUNT BRUCE and TUREE CREEK 1:250 000 map sheets.|16-MAY-23
79384|Balgara Dolerite|General description|The Balgara Dolerite is predominantly intruded as sills in the upper part of the Turee Creek Group, above the base of the Meteorite Bore Member of the Kungarra Formation, and in the basal Shingle Creek Group, below the top of the Nummana Member of the Cheela Springs Basalt.|16-MAY-23
79384|Balgara Dolerite|Thickness range|Individual sills are generally tens to hundreds of metres thick, with the thickest at least 500 m thick.|16-MAY-23
79384|Balgara Dolerite|Lithology|Medium-grained dolerite sills, with poorly exposed chilled margins consisting of fine-grained dolerite.|16-MAY-23
79384|Balgara Dolerite|Depositional environment|Interpreted as shallow-level intrusions coeval with the Cheela Springs Basalt (Martin and Morris, 2010).|16-MAY-23
79384|Balgara Dolerite|Relationships and boundaries|Sills intrude both the Turee Creek Group and the lower part of the Shingle Creek Group in the type area, and have been folded by the same folds that affect these units.|16-MAY-23
79384|Balgara Dolerite|Identifying features|Predominantly medium-grained dolerite, but margins of sills locally display characteristics of flows or shallow-level intrusion, such as vesicles/amygdales and hyaloclastite.|16-MAY-23
79384|Balgara Dolerite|Structure and Metamorphism|Sills have been folded by the Ophthalmia Orogeny but also appear to be truncated by the unconformity at the base of the Anthiby Formation within the Turee Creek Group, which formed during this orogeny (Martin and Morris, 2010).|16-MAY-23
79384|Balgara Dolerite|Age reasons|The Balgara Dolerite has been dated at 2208 +/- 10 Ma (Muller et al., 2005) in the Hardey Syncline where it intrudes the Turee Creek Group, and in the Turee Creek Syncline where it intrudes the Shingle Creek Group (Martin and Morris, 2010).|16-MAY-23
79384|Balgara Dolerite|Geophysical Expression|A very weak aeromagnetic signature allows lateral correlation of the sills under cover in the Hardey Syncline.|16-MAY-23
79384|Balgara Dolerite|Geochemistry|Geochemically indistinguishable from basalt flows in the lower Cheela Springs Basalt (Martin and Morris, 2010).|16-MAY-23
79384|Balgara Dolerite|Defn author|D. McB. Martin, Geological Survey of Western Australia 7-JUL-2020.|16-MAY-23
79384|Balgara Dolerite|Proposed publication|GSWA Report 203.|16-MAY-23
79384|Balgara Dolerite|References|Martin, DMcB and Morris, PA 2010, Tectonic setting and regional implications of ca. 2.2 Ga mafic magmatism in the southern Hamersley Province, Western Australia: Australian Journal of Earth Sciences, v. 57, no. 7, p. 911-931.  **Muller, SG, Krapez, B, Barley, ME and Fletcher, IR 2005, Giant iron-ore deposits of the Hamersley province related to the breakup of Paleoproterozoic Australia: New insights from in situ SHRIMP dating of baddeleyite from mafic intrusions: Geology, v. 33, no. 7, p. 577-580.|16-MAY-23
30078|Ballythanna Sandstone Member|Name source|Ballythanna Hill, 1 km west of well location.|16-MAY-23
30078|Ballythanna Sandstone Member|Type section locality|Ballythanna 1, 65-298 m.  26o03'42"S, 115o40'11"E.|16-MAY-23
30078|Ballythanna Sandstone Member|Lithology|Fine- to medium-grained sandstone, minor carbonaceous siltstone, locally bioturbated.|16-MAY-23
33645|Bardsley Formation|Name source|Bardsley Well, RHODES (MGA 310200E, 7182850N; Fig. 1).|16-MAY-23
33645|Bardsley Formation|Type section locality|The type area for the Bardsley Formation is the area north from the track that crosses Troy Creek (around MGA 319500E, 71893000N). No type section has been measured or is appropriate, due to the type of outcrop.|16-MAY-23
33645|Bardsley Formation|Extent|The Bardsley Formation has only been recognized in and adjacent to the headwaters of Troy Creek (Fig. 1), in the southern-central part of RHODES. Troy Creek cuts through a prominent range just south of the area of outcrop. This range may have served as a barrier that localized deposition.|16-MAY-23
33645|Bardsley Formation|Thickness range|The thickness of the Bardsley Formation is assumed to be only a few metres.|16-MAY-23
33645|Bardsley Formation|Lithology|The formation consists of poorly sorted, variably ferruginized lithic sandstone and granule conglomerate infilling an irregular topography on the underlying Earaheedy Group, and is massive to poorly bedded. Commonly, only 20 to 50 cm of section can be seen because the unit is exposed as rubbly flats adjacent to the creek. There are common solution pits infilled by pisolitic ferricrete and clay-cemented gravel reworked from the Earaheedy Group.|16-MAY-23
33645|Bardsley Formation|Relationships and boundaries|The Bardsley Formation clearly infills an irregular topography on the Earaheedy Group, and has not been folded or tilted like the Sydney Heads Pass Conglomerate, another unit of uncertain age on EARAHEEDY. The formation pre-dates the development of ferricrete, which probably occurred in the Oligocene or Eocene, but could have occurred in the Mesozoic (Hocking and Cockbain, 1990;  ockbain and Hocking, 1990). The lack of folding or tilting suggests that it post-dates the Collier  Group, which is moderately folded and faulted a few kilometres to the north and west. The distribution suggests southward-directed palaeocurrents, down Troy Creek.|16-MAY-23
33645|Bardsley Formation|Age reasons|The formation pre-dates the development of ferricrete, which probably occurred in the Oligocene or Eocene, but could have occurred in the Mesozoic (Hocking and Cockbain, 1990;  Cockbain and Hocking, 1990). The lack of folding or tilting suggests that it post-dates the Collier  Group, which is moderately folded and faulted a few kilometres to the north and west. The Bardsley Formation thus has a possible age range of early Cainozoic to late Mesoproterozoic;  however, its probable age is post-Proterozoic, as palaeocurrent measurements from the Collier Group indicate northward flow, and those from the lower Sunbeam Group are westward. Deposition over the West Australian Craton (used broadly) was most extensive during the Early Permian Gondwana glaciation, but there are no polymictic boulder lags nearby to support a Permian age.|16-MAY-23
33645|Bardsley Formation|Comments|During mapping on RHODES, an isolated area of consolidated grit was recognized at the headwaters of Troy Creek, infilling the creek depression and adjacent areas. Exposures are discontinuous because of topography developed on deformed rocks of the Earaheedy Group beneath. The unit resembles the Wiluna Hardpan of Bettenay and Churchward (1974), but is somewhat older as it is penetrated by solution pits infilled with pisolitic ferricrete and reworked Earaheedy Group rocks.  For this reason it is named the Bardsley Formation.|16-MAY-23
33645|Bardsley Formation|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
74625|Barn Hill Formation|Name source|Barn Hill, latitude/longitude coordinates 18º 21' 59" S, 122º 03' 01" E, Lagrange 1:250,000 Topographical Sheet.|16-MAY-23
74625|Barn Hill Formation|Geomorphic expression|As mixed red and white coastal dunes.|16-MAY-23
74625|Barn Hill Formation|Type section locality|Cliff exposure on coast near Barn Hill, latitude/longitude coordinates 18º 21' 53" S, 122º 02' 14" E, Lagrange 1:250,000 Topographical Sheet.|16-MAY-23
74625|Barn Hill Formation|Description at type locality|(top) 450 cm red quartz sand with interlayered thick beds of calcarenite, 50 cm thick, thin beds (1-5 cm thick) of calcarenite and red quartzose calcarenite, and red quartz sand with laminae of quartz and carbonate layers < 1 cm thick; 300 cm lens of limestone 3 m thick and circa 20 m long, with large-scale cross-laminated, cream calcarenite composed of quartz sand, bioclasts, and ooids; base with sharp contact with underlying mottled red sand of the Mowanjum Sand;|16-MAY-23
74625|Barn Hill Formation|Extent|The unit is widespread along the Canning Coast as a semi-continuous to scattered shoe-string to lensoid deposit.|16-MAY-23
74625|Barn Hill Formation|Thickness range|At type locality 7.5 m thick.  However, elsewhere, where exposed, the Formation has been recorded as up to 7 m thick. Regionally, the unit will appear as discontinuous shoe-string and lensoid deposits, individually, some tens of metres to several hundred of metres long, but only up to 100 m wide and 7 m thick.|16-MAY-23
74625|Barn Hill Formation|Lithology|In general, a red sand varying to orange quartz and light coloured to orange quartz-and-carbonate sand (depending on carbonate sand content), with millimetre to centimetre thick laminae and beds of carbonate-rich sand, and large to small limestone lenses, 2-4 m thick and 1-50 m long, composed of calcarenite; sand grains of the carbonate laminae and layers are bioclastic, carbonate-intraclast, carbonate-lithoclast, and oolitic; the cementing agent in the calcarenite layers is sparry calcite; sedimentary structures include lamination, cross-lamination, root-structured to structureless.|16-MAY-23
74625|Barn Hill Formation|Depositional environment|Supratidal coastal dunes.|16-MAY-23
74625|Barn Hill Formation|Fossils|Molluscan shells occur in some horizons within the Formation.  These are several metres above HAT, and appear to be middens.  The shells in the Formation include: Anadara granosa, Modiolus auriculatus, Modiolus micropterus, Modiolus cf. trailii, and Saccostrea cucullata.|16-MAY-23
74625|Barn Hill Formation|Diastems or hiatuses|Hiatuses exist throughout the Formation separating various episodes of red dune accretion and encroachment of white dunes onto older red dune surfaces.|16-MAY-23
74625|Barn Hill Formation|Relationships and boundaries|The unit rests, with sharp contact, directly on Mowanjum Sand (Semeniuk 1980), or on a gravel bed of ironstone pebbles that rests on the Mowanjum Sand.  The Formation is overlain with sharp contact, or gradational contact, by Church Hill Sand.  The Formation also locally is overlain with sharp contact, or gradational contact, by Shoonta Hill Sand; if gradational, the transitional zone, some 1 m thick, is orange sand with a mixture of quartz sand and carbonate sand.|16-MAY-23
74625|Barn Hill Formation|Age reasons|Radiocarbon dating of shells and calcarenite within the Formation places it in the Holocene.  A whole-of-calcarenite sample for radiocarbon analysis returned an age of 2740 ± 120 yrs BP. Shells of Saccostrea cucullata from under a limestone lens returned an age of 900 ± 100 yrs BP.|16-MAY-23
74625|Barn Hill Formation|Correlations|The unit is laterally equivalent to Shoonta Hill Sand.|16-MAY-23
74625|Barn Hill Formation|Comments|A dune unit of red dune sand, white dune sand , and limestone lenses.|16-MAY-23
74625|Barn Hill Formation|References|For Canning Coast units: Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.   For Mowanjum Sand: Semeniuk V 1980 Quaternary stratigraphy of the tidal flats King Sound, WA. Journal of the Royal Society of Western Australia 63: 65-78.|16-MAY-23
82171|Barnicarndy Formation|Name source|Barnicarndy Hills ~ 27.6 km north-northwest of the Barnicarndy 1 stratigraphic drillhole (formerly Waukarlycarly 1). Approximate coordinates: Lat: 21degrees 14' 33.88" S Lon: 121deg 41' 30.95" E|16-MAY-23
82171|Barnicarndy Formation|Unit history|This subsurface unit has not been previously recognised due to the lack of deep drilling in the area prior to Barnicarndy 1, but may be a proximal, lateral equivalent to the Willara through to Nita formations and possibly parts of the Carribuddy Group.|16-MAY-23
82171|Barnicarndy Formation|Constituents|Informal upper and lower sandstone intervals|16-MAY-23
82171|Barnicarndy Formation|Geomorphic expression|The Barnicarndy Formation has been recorded only in the subsurface.|16-MAY-23
82171|Barnicarndy Formation|Type section locality|Barnicarndy 1 stratigraphic drillhole (-21.4785degS, 121.7823E) between 855 - 1345 m depth (490 m thick).|16-MAY-23
82171|Barnicarndy Formation|Confidential_type_locality|No|16-MAY-23
82171|Barnicarndy Formation|Description at type locality|The Barnicarndy Formation is composed of fine- to medium-grained, oxidized quartz sandstones and minor siltstone. It displays intervals of bioturbation, and evidence of tidal deposition, including local tidal mud drapes, and rare shelly horizons. These observations indicate a marine influence for at least part of the formation. Acoustic televiewer (ATV) logs have been used to interpret continuous deposition from the age-constrained underlying Nambeet Formation to the top of the section, and enable evaluation of paleocurrent patterns through the unit (Wilson and Thrane, 2020). The average paleo-flow direction was towards the northeast in the lower sandstone interval, but undergoes a sharp 90 degree change towards the northwest around 1070 m, approximately coincident with a subtle boundary seen in wireline logs (Walker, 2020). The change in paleo-flow direction may indicate a localized change in tectonic tilt, a disconformity or a subtle change in depositional setting between the upper and lower sandstone intervals.|16-MAY-23
82171|Barnicarndy Formation|Extent|The Barnicarndy Formation is recorded within a single stratigraphic drillhole, Barnicarndy 1 in the Barnicarndy Graben, southwestern Canning Basin. A seismic line through this well location (18GA-KB1) indicates that the Barnicarndy Formation extends across the graben in this area, and the unit can be tentatively identified on separate seismic lies in the northern part of the graben.|16-MAY-23
82171|Barnicarndy Formation|General description|The Barnicarndy Formation is dominated by sandstone and has only been identified in the Barnicarndy Graben in the southwest Canning Basin.|16-MAY-23
82171|Barnicarndy Formation|Thickness range|490 m thick at the type locality. The thickness variation is unconstrained as there is currently only one well intersection of the Barnicarndy Formation identified in Barnicarndy 1, and the associated seismic line does not show significant lateral variation in thickness across the graben.|16-MAY-23
82171|Barnicarndy Formation|Depositional environment|At the type section, the Barnicarndy Formation was deposited in fluvial to shallow marine, tidal and lower shoreface settings.|16-MAY-23
82171|Barnicarndy Formation|Fossils|Rare brachiopods and bivalves. Intervals of bioturbation.|16-MAY-23
82171|Barnicarndy Formation|Diastems or hiatuses|Preliminary detrital zircon geochronology and acoustic televiewer log analysis suggest continuous deposition from the underlying Nambeet Formation into the Barnicarndy Formation. A possible disconformity cannot be discounted between the lower and upper sandstone intervals of the Barnicarndy Formation.|16-MAY-23
82171|Barnicarndy Formation|Relationships and boundaries|At the type section the Barnicarndy Formation lies stratigraphically between the Grant Group (above) and Samphire Marsh Member of the Nambeet Formation (below). The depositional sequence from Samphire Marsh Member to the Barnicarndy Formation is gradational. The contact with the overlying Grant Group is a well-defined angular disconformity.|16-MAY-23
82171|Barnicarndy Formation|Identifying features|Distinguished from the underlying mudstone-dominated Samphire Marsh Member by the gradational change to sandstone dominated lithologies.|16-MAY-23
82171|Barnicarndy Formation|Structure and Metamorphism|Flat-lying to slightly dipping to the north at the well location. No metamorphism.|16-MAY-23
82171|Barnicarndy Formation|Age reasons|At the type section, the lower Barnicarndy Formation conformably overlies biostratigraphically dated late Floian to early Dapingian strata, while the upper Barnicarndy Formation is assigned a tentative maximum depositional age of 456 +/- 8 Ma (Darriwilian to Katian) based on the youngest zircon from GSWA sample 246757 at 902.01 - 902.44 m depth in Waukarlycarly 1 (Wingate et al., 2021).|16-MAY-23
82171|Barnicarndy Formation|Correlations|The Barnicarndy Formation is possibly laterally equivalent to units between the Willara Formation and Carribuddy Group within the main part of the southern Canning Basin.|16-MAY-23
82171|Barnicarndy Formation|Alteration and Mineralisation|None observed.|16-MAY-23
82171|Barnicarndy Formation|Geophysical Expression|The Barnicarndy Formation is differentiated from the overlying Grant Group and underlying Samphire Marsh Member on the Kidson Sub-basin seismic line (18GA-KB1).|16-MAY-23
82171|Barnicarndy Formation|Geochemistry|X-ray diffraction analyses of samples from the Barnicarndy Formation type section indicates a composition dominated by quartz (95.7 - 97.9%), k-feldspar (0- 2.0 %) and clay (1.6 - 3.3%), with no detected carbonate minerals.|16-MAY-23
82171|Barnicarndy Formation|Defn author|L Normore and P Haines, 2-FEB-2022.|16-MAY-23
82171|Barnicarndy Formation|Comments|Ongoing biostratigraphic analysis may help better define the age of both the upper and lower Barnicarndy Formation and thereby refine correlation to laterally equivalent formations.|16-MAY-23
82171|Barnicarndy Formation|References|Normore, LS, Haines, PW, Carr, LK, Henson, P, Zhan, Y, Wingate, M, Zhen, YY, Lu, Y, Martin, S, Kelsey, D, Allen, H, and Fielding, I 2021, Barnicarndy Graben, southern Canning Basin: stratigraphy defined by the Barnicarndy 1 stratigraphic well: The APPEA Journal, 61, 224-235, APPEA Conference June 2021 https://doi.org/10.1071/AJ20160  **Walker, M, 2020, Petrophysical Evaluation, Waukarlycarly-1 Stratigraphic Well, Canning Basin Western Australia, 39p, unpublished report available on WAPIMS, (https://wapims.dmp.wa.gov.au/wapims).  **Wilson, A and Thrane, L, 2020, Report DM-20-1, Waukarlycarly-1, Structural and sedimentological analysis of an Acoustic Televiewer borehole image log, Onshore Canning Basin, Western Australia, 117p, unpublished report available on WAPIMS, (https://wapims.dmp.wa.gov.au/wapims).  **Wingate, MTD, Lu, Y, Fielding, IOH, Normore, LS and Haines, PW 2021, 246757: quartz sandstone, Barnicarndy 1; Geochronology Record 1737: Geological Survey of Western Australia, 8p.|16-MAY-23
29218|Betty Formation|Name source|Lake Betty (19o32'S, 126o20'E)|16-MAY-23
29218|Betty Formation|Unit history|Consists of basal part of Grant Formation (Guppy et al, 1952) now termed the Grant Group.  The Betty Formation was previously referred to as Cuncudgerie Sandstone by Koop (1966) and as the "lower sandstone unit" by Crowe and Towner (1976).|16-MAY-23
29218|Betty Formation|Type section locality|Between 1057 and 1657 m in L. Betty No. 1 well (19o34'10"S, 126o19'52"E)|16-MAY-23
29218|Betty Formation|Extent|Through Canning Basin except possibly along northern margin and southern Anketell Shelf.|16-MAY-23
29218|Betty Formation|Thickness range|602 m thick at the type section but thickest in the Fitzroy Trough (1713 m thick in Grant Range No. 1).|16-MAY-23
29218|Betty Formation|Lithology|Consists mainly of moderately sorted, medium to coarse-grained sandstone with minor mudstone and conglomerate, rare glauconite and a high proportion of lithic fragments.|16-MAY-23
29218|Betty Formation|Relationships and boundaries|Conformably overlain by Winifred Formation except where overlapped.  Unconformably overlies rocks of Carboniferous to Precambrian age.  Believed to conformably overlie basal part of Paterson Formation and to interfinger with younger parts of it.|16-MAY-23
29218|Betty Formation|Age reasons|Late Carboniferous to Early Permian (Sakmarian sensu lato) based on palynomorphs (e.g. Crank, 1972).|16-MAY-23
29218|Betty Formation|Proposed publication|Annual Report Geological Survey of Western Australia for 1976|16-MAY-23
2189|Boobina Porphyry|Name source|Boobina Creek, Lat. 21o41'35"S, Long. 119o56'55"E, Marble Bar 1:250 000 Sheet area.|16-MAY-23
2189|Boobina Porphyry|Unit history|The "coarse-grained feldspar porphyry -- to fine-grained black feldspar porphyry" of Noldart and Wyatt (1962).|16-MAY-23
2189|Boobina Porphyry|Type section locality|2-3 km northwest from Copper Hills|16-MAY-23
2189|Boobina Porphyry|Extent|Approx. 50 km2, in two ovoid masses north and south of Copper Hills, Lat. 21o39'S, Long. 119o58'E.|16-MAY-23
2189|Boobina Porphyry|Lithology|Dacite porphyry.  Euhedral to subhedral plagioclase and quartz phenocrysts up to 5 mm long set in a dark aphanitic groundmass.  Plagioclase (An30) laths commonly form glomeroporphyritic groups.|16-MAY-23
2189|Boobina Porphyry|Relationships and boundaries|Intrudes Warrawoona Group (Lipple, 1975) and intruded by the Mondana Adamellite (Hickman and Lipple 1974).|16-MAY-23
2189|Boobina Porphyry|Age reasons|Archaean|16-MAY-23
29942|Bookingarra Group|Name source|Bookingarra Creek (Lat. 20° 55' 47" S., Long. 117° 45' 20" E.), 12 km southwest of Whim Creek mine (Lat. 20° 50' 48" S., Long. 117° 49' 53" E.).|16-MAY-23
29942|Bookingarra Group|Unit history|The name Bookingarra Group was first used between 2002 and 2006 to group five formations that unconformably overlie the Whim Creek Group (Pike and Cas, 2002; Pike et al., 2002). Van Kranendonk et al. (2006) subsequently revised this stratigraphy to rename the Bookingarra Group as a formation of the Croydon Group. The Bookingarra Formation was then defined as being composed of only two previously defined basaltic formations revised to member status (Louden Volcanic Member and Mount Negri Volcanic Member). The four resulting formations (Cistern Formation, Rushall Slate, Bookingarra Formation, Kialrah Rhyolite) were then combined with formations of the newly defined Croydon Group (Van Kranendonk et al., 2006). This stratigraphic change was based on an interpretation of stratigraphic continuity between the successions of the Whim Creek greenstone belt and the Mallina Basin.  Reinterpreted structural, stratigraphic, and geochronological data indicate that the succession of the Whim Creek greenstone belt was not deposited immediately adjacent to the succession of the Mallina Basin and that several of the correlations made by Van Kranendonk et al. (2006) are incorrect (Hickman, 2016). The two successions are separated by a major strike-slip fault (Loudens Fault) that tectonically juxtaposed the Whim Creek greenstone belt and Mallina Basin at c. 2940 Ma (after deposition of most of the Bookingarra Group). Prior to c. 2940 Ma the Whim Creek greenstone belt and Mallina Basin had different depositional and structural histories (Hickman, 2016). Additionally, the succession of the Bookingarra Group overlies a c. 2955 Ma regional unconformity and many previously correlated units of the Mallina Basin underlie this unconformity (Hickman, 2016).|16-MAY-23
29942|Bookingarra Group|Constituents|Kialrah Rhyolite, Mount Negri Volcanics, Louden Volcanics, Rushall Slate, Cistern Formation (oldest)|16-MAY-23
29942|Bookingarra Group|Geomorphic expression|The Bookingarra Group outcrops in low hills and strike-controlled ridges.|16-MAY-23
29942|Bookingarra Group|Type section locality|The type area is in the Whim Creek greenstone belt between Bookingarra Creek (Lat. 20° 55' 47" S., Long. 117° 45' 20" E), and Mount Negri (Lat. 20° 47' 09" S., Long. 117° 50' 46" E). No single type section can be nominated because the entire succession is not represented at any single locality. Type areas or sections are nominated for the component formations.|16-MAY-23
29942|Bookingarra Group|Extent|The Bookingarra Group occupies most of the Whim Creek and Peawah Hill greenstone belts (Hickman, 2016) which, prior to erosion, collectively extended across an area of at least 4000 km2.|16-MAY-23
29942|Bookingarra Group|General description|Several lines of evidence indicate that the Cistern Formation and Rushall Slate are restricted to small sections of the Whim Creek greenstone belt and were deposited adjacent to minor felsic intrusions of the c. 2950 Ma Sisters Supersuite (Hickman, 2016). The Louden Volcanics are regionally extensive within the Whim Creek greenstone belt, and have been interpreted to be the product of a mantle plume (Arndt et al., 2001). In this scenario, the Louden Volcanics are likely to have been erupted over a very large area of the northwest Pilbara, and related subvolcanic ultramafic-mafic intrusions should also have been emplaced over a large area. However, alternative origins for the Louden Volcanics were suggested by Smithies et al. (2007).|16-MAY-23
29942|Bookingarra Group|Thickness range|The maximum thickness of the Bookingarra Group reaches 3000 m in the Whim Creek greenstone belt (Hickman, 2016), but the average thickness is 1000-1500 m.|16-MAY-23
29942|Bookingarra Group|Lithology|Felsic volcaniclastic rocks and sedimentary rocks (Cistern Formation and Rushall Slate) are overlain by volcanic and sub-volcanic intrusive rocks (Louden Volcanics, Mount Negri Volcanics, and Kialrah Rhyolite). The lower sedimentary formations of the group comprise volcaniclastic conglomerate and sandstone, siltstone, shale, and minor chert. Overlying volcanic rocks include komatiite, komatiitic basalt, tholeiitic basalt, andesite, dacite, and rhyolite. Sub-volcanic sills of peridotite, pyroxenite, gabbro and dolerite are included in the group. Lenses of conglomerate, sandstone, and shale are present within the basaltic formations adjacent to growth faults.|16-MAY-23
29942|Bookingarra Group|Depositional environment|Most workers have interpreted that the Bookingarra Group was deposited and erupted in a zone of continental rifting and strike-slip faulting near the northwest margin of the Pilbara Craton. Nd model ages from the Louden Volcanics and Mount Negri Volcanics (Arndt et al., 2001; Smithies et al., 2004) average c. 3400 Ma indicating involvement of underlying Paleoarchean crust, or sedimentary material derived from Paleoarchean crust, in magma genesis. Trace element data (normalized to primitive mantle) support this conclusion, with significant enrichments in Th, Zr, and LREE (Smithies et al., 2007).|16-MAY-23
29942|Bookingarra Group|Fossils|None.|16-MAY-23
29942|Bookingarra Group|Diastems or hiatuses|Disconformities and unconformities are locally present within the group. Syn-depositional rifting and uplift resulted in abrupt lateral facies changes, lateral thickness variations, and local erosional surfaces within formations. The basal unconformity with the underlying Whim Creek Group is overlain by different formations of the Bookingarra Group in different areas of the Whim Creek greenstone belt. Internal unconformities are locally present between Mount Negri Volcanics and all underlying formations of the group (Hickman, 2016).|16-MAY-23
29942|Bookingarra Group|Relationships and boundaries|The Bookingarra Group unconformably overlies the Whim Creek Group, is unconformably overlain by the Fortescue Group, and is partly fault-bounded between the Sholl Shear Zone and the Loudens Fault. However, the Bookingarra Group extends to the northern side of the Sholl Shear Zone where it is poorly exposed between Balla Balla (Lat. 20° 41' 40" S., Long. 117° 47' 19" E.) and Cape Thouin (Lat. 20° 20' 10" S., Long. 118° 10' 55" E.) (Hickman et al., 2006).|16-MAY-23
29942|Bookingarra Group|Identifying features|Olivine- and pyroxene-spinifex textures are distinguishing features of the Louden Volcanics. Porphyritic and flow-banded rhyolite is confined to the Kialrah Rhyolite.|16-MAY-23
29942|Bookingarra Group|Structure and Metamorphism|The Bookingarra Group was folded by the c. 2940 Ma Whim Creek Anticline and faulted by the Sholl Shear Zone, Loudens Fault, and minor normal and strike-slip faults within the Central Pilbara Tectonic Zone (Hickman, 2016). The metamorphic grade of the Bookingarra Group varies from prehnite-pumpellyite to greenschist facies.|16-MAY-23
29942|Bookingarra Group|Age reasons|The maximum depositional age of c. 2955 Ma is defined by the regional unconformity that separates the Bookingarra Group from the underlying Whim Creek Group (Pike and Cas, 2002; Pike et al., 2002; Hickman, 2016). Isotopic evidence (detrital zircon U-Pb dating) establishes that the Cistern Formation is younger than 2964 +/- 6 Ma (Huston et al., 2002) and stratiform Pb-Zn mineralization within the Cistern Formation, interpreted to be syndepositional, has been dated at 2950 Ma (Richards and Blockley, 1984; Richards, 1986). Pb isotope data from syn-depositional mineralization in the Rushall Slate were interpreted by Huston et al. (2002) to indicate an age of c. 2948 Ma.  The minimum age of the Kialrah Rhyolite within the Whim Creek greenstone belt is 2943 +/- 7 Ma (Nelson, 1998), and rhyolite in the Mallina Basin that is correlated with the Kialrah Rhyolite is the same age within isotopic error. The minimum age of the Mount Negri Volcanics is poorly constrained by a c. 2922 Ma Pb-Pb date for galena in quartz veins (Thorpe et al., 1992).|16-MAY-23
29942|Bookingarra Group|Correlations|Upper basaltic formations of the Bookingarra Group are approximately the same age as relatively thin basaltic units in the upper part of the Mallina Basin succession. These units are the South Mallina Basalt Member of the Mallina Formation (Croydon Group) and the Salt Well Member of the Lalla Rookh Sandstone (Croydon Group). However, during deposition these successions were not closely adjacent.  The Louden Volcanics and Mount Negri Volcanics are also interpreted to be co-magmatic with certain ultramafic-mafic layered intrusions of the northwest Pilbara Craton, including the Sherlock and Opaline Well Intrusions, both of which underlie the Louden Volcanics and are likely to be subvolcanic (Hickman, 2016).|16-MAY-23
29942|Bookingarra Group|Alteration and Mineralisation|Varying degrees of silicification, epidote-chlorite alteration, and carbonate alteration affect all formations of the group. Economic deposits of VMS and epigenetic base metal mineralization (Cu-Pb-Zn) have been mined in the Cistern Formation and Rushall Slate (reviewed by Hickman, 2016). V-Ti-Fe deposits are present in the Sherlock Intrusion, interpreted to be subvolcanic to the Louden Volcanics.|16-MAY-23
29942|Bookingarra Group|Geophysical Expression|Linear zones of high and low TMI anomalies corresponding to outcrops of ultramafic, mafic, and sedimentary units.|16-MAY-23
29942|Bookingarra Group|Geochemistry|The geochemistry of most formations within the group has been documented by Glikson et al. (1986a, b), Arndt (2001), and Smithies et al. (2007).|16-MAY-23
29942|Bookingarra Group|Defn author|Hickman, A.H., GSWA 25-OCT-2017|16-MAY-23
29942|Bookingarra Group|References|Arndt, N, Bruzak, G and Reischmann, T 2001, The oldest continental and oceanic plateaus: geochemistry of basalts and komatiites of the Pilbara Craton Australia, in Mantle Plumes: Their Identification Through Time edited by RE Ernst and KL Buchan: Geological Society of America Special Publication 352, Boulder, Colorado, USA, p.359-387.  **Glikson, AY, Davy, R, Hickman, AH 1986a, Geochemical data files of Archaean volcanic rocks, Pilbara Craton, Western Australia: Australia BMR, Record 1986/14, 12p. **Glikson, AY, Pride, C, Jahn, B-M, Davy, R and Hickman AH 1986b, RE and HFS (Ti, Zr, Nb, P, Y) element evolution of Archaean mafic-ultramafic volcanic suites, Pilbara Block, Western Australia: Australia BMR, Record 1986/6, 85p. **Hickman, AH 2016, Northwest Pilbara Craton: a record of 450 million years in the growth of Archean continental crust: Geological Survey of Western Australia, Report 160, 104p. ** Hickman, AH, Smithies, RH and Strong, CA 2006, Interpreted bedrock geology of the northwestern Pilbara Craton (1: 250 000 scale): Geological Survey of Western Australia, Report 92, Plate 1. **Huston, DL, Sun, S -S, Blewett, R, Hickman, A, Van Kranendonk, M, Phillips, D, Baker, D, and Brauhart, C 2002, The timing of mineralisation in the Archaean Pilbara Craton, Western Australia: Economic Geology, v. 97, p. 733-755. **Nelson, DR 1998, 144261: rhyolite, Bradley Well, Geochronology Record 272: Geological Survey of Western Australia, 4p. **Pike, G and Cas, RAF 2002, Stratigraphic evolution of Archaean volcanic rock-dominated rift basins from the Whim Creek Belt, west Pilbara Craton, Western Australia, in Precambrian Sedimentary Environments: A Modern Approach to Depositional Systems edited by W Altermann and P Corcoran: International Association of Sedimentologists, Special Publication 33, Blackwell Science, Oxford, UK, p. 213-234. **Pike, G, Cas, RAF and Smithies, RH 2002, Geological constraints on base metal mineralization of the Whim Creek greenstone belt, Pilbara Craton, Western Australia: Economic Geology, v. 97, p. 827-845. **Richards, JR and Blockley, JG 1984, The base of the Fortescue Group, Western Australia: Further galena lead isotopic evidence of its age: Australian Journal of Earth Sciences, v. 31, p. 257-268. **Richards, JR, 1986, Lead isotope signatures: Further examination of comparisons between South Africa and Western Australia: Geological Society of South Africa Transactions, v. 89, p. 285-304. **Smithies, RH, Champion, DC and Sun, S-S 2004, Evidence for Early LREE-enriched Mantle Source Regions: Diverse Magmas from the ca. 3.0 Ga Mallina Basin, Pilbara Craton, NW Australia: Journal of Petrology, v. 45, p. 1515-1537. **Smithies, RH, Champion, DC, Van Kranendonk, MJ and Hickman, AH 2007, Geochemistry of volcanic units of the northern Pilbara Craton: Geological Survey of Western Australia, Report 104, 47p. **Thorpe, RI, Hickman, AH, Davis, DW, Mortensen, JK and Trendall, AF 1992, Constraints to models for Archaean lead evolution from precise U-Pb geochronology from the Marble Bar region, Pilbara Craton, Western Australia, in The Archaean: Terrains, processes and metallogeny, edited by JE Glover and SE Ho: University of Western Australia, Geology Department and University Extension, Publication no. 22, p. 395-408. **Van Kranendonk, MJ, Hickman, AH, Smithies, RH, Williams, IR, Bagas, L and Farrell, TR 2006, Revised lithostratigraphy of Archean supracrustal and intrusive rocks in the northern Pilbara Craton, Western Australia: Geological Survey of Western Australia, Record 2006/15, 57p.|16-MAY-23
30280|Browns Range Metamorphics|Name source|Browns Range, in Gordon Downs, Billiluna, Tanami, and Birrindudu 1:250 000 Sheet areas, WA and NT.|16-MAY-23
30280|Browns Range Metamorphics|Unit history|Unit previously mapped as undivided Halls Creek Group (e.g., Gemuts & Smith 1968) and undivided Tanami Complex (e.g., Blake et al 1979).|16-MAY-23
30280|Browns Range Metamorphics|Geomorphic expression|low hills and ridges.|16-MAY-23
30280|Browns Range Metamorphics|Type section locality|Low hills within 1 km of GR DE900040, Gordon Downs 1:100 000 Sheet area, in southeast Gordon Downs 1:250 000 Sheet area. Here the formation is represented by meta-arkose containing sparse to abundant pebbles and cobbles of vein quartz and quartzite. No clear bedding planes evident in field, but tight folding apparent on air photographs. Unconformity with scarp-forming Gardiner Sandstone of the Mesoproterozoic Birrindudu Group is exposed on SW side of type locality.|16-MAY-23
30280|Browns Range Metamorphics|Extent|Browns Range Dome, in SE Gordon Downs and adjoining parts of Billiluna (WA) and Tanami (NT) 1:250 000 Sheet areas|16-MAY-23
30280|Browns Range Metamorphics|Thickness range|>1000 m.|16-MAY-23
30280|Browns Range Metamorphics|Lithology|Pebbly arkose metamorphosed (upper amphibolite/granulite facies) to quartzofeldspathic granofels (granulitic texture) - primary feldspar altered to white mica and clay minerals; minor banded ironstone and metaconglomerate (at GR DE966125).|16-MAY-23
30280|Browns Range Metamorphics|Relationships and boundaries|base not exposed. Overlain unconformably by gently dipping Gardiner Sandstone, which is not metamorphosed. Intruded in the Tanami Sheet area by unnamed granite, dated at 1882 Ma, which postdates main metamorphism|16-MAY-23
30280|Browns Range Metamorphics|Age reasons|possibly late Archaean (Page et al. 1995b). Metasediments contain several age-groupings of detrital zircon, the youngest of which, dated at 2507 +/- 5 Ma, gives a maximum age for sedimentation. High-grade metamorphism predates 1880 Ma granite.|16-MAY-23
30280|Browns Range Metamorphics|Correlations|Late Archaean Rum Jungle and Waterhouse Complexes of Pine Creek province.|16-MAY-23
30280|Browns Range Metamorphics|Proposed publication|Gordon Downs , WA, 2nd edition Explanatory Notes.|16-MAY-23
30280|Browns Range Metamorphics|References|*BLAKE, D.H., Hodgson, I.M. & Muhling, P.C., 1979. Geology of The Granites-Tanami region, Northern Territory and Western Australia. Bureau of Mineral Resources, Australia, Bulletin 197    *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.    *PAGE, R.W., Sun, S-S., Blake, D.H., Edgecombe, D. & Pearcey, D., 1995. Geochronology of an exposed late Archaean basement terrane in The Granites-Tanami region. AGSO Research Newsletter, 22, 19-20.|16-MAY-23
25816|Budjan Creek Formation|Name source|Budjan Creek (Military Grid 272 273), Marble Bar 1:250 000 Sheet area.|16-MAY-23
25816|Budjan Creek Formation|Type section locality|The unit is well exposed in gorges cut by the upper reaches of Budjan Creek (272 273).|16-MAY-23
25816|Budjan Creek Formation|Extent|The Budjan Creek Formation occurs in the Kelly Belt, from north of Coolbanacoula Pool (264 274) northeastwards to south of Copper Hills (283 283) as a strip 35 km long and up to 2.5 km wide.  The fault-displaced extension also crops out on the Nullagine 1:250 000 Sheet area.|16-MAY-23
25816|Budjan Creek Formation|Thickness range|Exposed thickness is between 1-1.5 km|16-MAY-23
25816|Budjan Creek Formation|Lithology|Basal conglomerate containing chert, vein quartz and dacite clasts overlain by shale, siltstone and sandstone units and capped by a thick conglomerate containing angular chert clasts.|16-MAY-23
25816|Budjan Creek Formation|Relationships and boundaries|Unconformably overlies Wyman Formation and Salgash Subgroup.  Upper margin partly concealed by unconformable cover of Proterozoic Fortescue Group, and partly faulted against divisions of Warrawoona Group.  Equivalent to Lalla Rookh Sandstone.|16-MAY-23
25816|Budjan Creek Formation|Age reasons|Archaean because overlain unconformably by Lower Proterozoic Fortescue Group.|16-MAY-23
23447|Butchers Gully Member|Name source|Butchers Gully, a tributary of Black Elvire River, confluence at GR CE793678, Halls Creek 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area, WA.|16-MAY-23
23447|Butchers Gully Member|Unit history|Brockman Volcanics (e.g., Ramsden et al. 1993, Taylor et al. 1995); Butchers Gully Volcanic Member (Warren 1997).|16-MAY-23
23447|Butchers Gully Member|Geomorphic expression|Strike ridges and valleys; local relief less than 100m|16-MAY-23
23447|Butchers Gully Member|Type section locality|Alkaline lavas, pyroclastics and volcaniclastic rocks intruded by subvolcanic sheets and interlayered with greywacke, siltstone and mudstone in low ridges, hills and creek beds around the Brockman REE prospect (at GR CE717740),    Halls Creek 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area.|16-MAY-23
23447|Butchers Gully Member|Extent|Halls Creek and Ruby Plains 1:100 000 Sheet areas in Gordon Downs 1:250 000 Sheet area and Dockrell 1:100 000 Sheet area in Mount Ramsay 1:250 000 Sheet area, WA.|16-MAY-23
23447|Butchers Gully Member|Thickness range|>1000 m.|16-MAY-23
23447|Butchers Gully Member|Lithology|Trachyandesite, trachyte, quartz trachyte and rhyolite lavas, including pillow lavas; subvolcanic syenite sheets; volcanic breccia; pyroclastic and volcaniclastic rocks (including niobium tuff of Chalmers, 1990); some interlayered turbiditic greywacke, siltstone and mudstone. Metamorphosed to mainly greenschist facies; commonly cleaved.|16-MAY-23
23447|Butchers Gully Member|Depositional environment|Submarine.|16-MAY-23
23447|Butchers Gully Member|Relationships and boundaries|Of the Olympio Formation of Halls Creek Group. Overlain and underlain conformably by turbidites of the Olympio Formation. Overlain unconformably by Moola Bulla Formation (Palaeoproterozoic).|16-MAY-23
23447|Butchers Gully Member|Age reasons|Palaeoproterozoic (Orosirian). Zircon from pillow lava in member is dated at 1848 +/- 3 Ma (AGSO's OZCHRON database). Zircon dated at 1870 +/- 4 Ma from niobium tuff (Taylor et al. 1995) at base of member is now thought to be detrital.|16-MAY-23
23447|Butchers Gully Member|Correlations|None, appears to be measurably younger (about 10 million years) than the Maude Headley Member of the Olympio Formation.|16-MAY-23
23447|Butchers Gully Member|References|*BLAKE, D.H., Tyler, I.M. & Sheppard, S., 1997. Geology of the Ruby Plains 1:100 000 Sheet area (4460), Western Australia,. Australian Geological Survey 	Organisation, Canberra.    *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.     *TAYLOR, W.R., Page, R.W., Esslemont, G., Rock, N.H.S. & Chalmers, D.I., 1995. 	Geology of the volcanic-hosted Brockman rare-metals deposit, Halls Creek Mobile Zone, northwest Australia, Part I - Volcanic environment, geochronology and petrography of the Brockman volcanics. Mineralogy and Petrology, 52, 209-230.    *TYLER, I.M. & Griffin, T.J., 1994. Dockrell, Western Australia, 1:100 000 geological map sheet (4360). Geological Survey of Western Australia, Perth.    *RAMSDEN, A.R., French, D.H. & Chalmers, D.I., 1993. The volcanic-hosted rare-metals deposit at Brockman, Western Australia: mineralogy and geochemistry of the Niobium Tuff. Mineralium Deposita, 28, 1-12.    *PAGE, R.W., Blake, D.H., Sun, S-S., Tyler, I.M., Griffin, T.J. & Thorne, A.M., 1994. New geological and geochronological constraints on volcanogenic massive sulphide prospectivity near Halls Creek (WA).  AGSO Research Newsletter, 20, 5-7.    *CHALMERS, D.I., 1990. Brockman multi-metal and rare earth deposit. In: Hughes, F.E. (editor), Geology of the Mineral Deposits of Australia and Papua New Guinea. The Australasian Institute of Mining and Metallurgy, Monograph, 14, 707-709.    *WARREN, R.G., 1997. Reconnaissance geological mapping in Dixon, SE McIntosh and northernmost Halls Creek 1:100 000 Sheet areas, East Kimberley, W.A. 1992-3. Australian Geological Survey Organisation, Record 1997/26.|16-MAY-23
21408|Cable Beach Sand|Name source|Cable Beach, north of Broome, latitude/longitude coordinates 17º 54' 54" S, 122º 12' 41" E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
21408|Cable Beach Sand|Constituents|Cable Beach Sand is mainly comprised of sand and shelly sand, but the formation contains two members, variably developed: Lombadina Conglomerate Member and the Cape Boileau Calcarenite Member.|16-MAY-23
21408|Cable Beach Sand|Geomorphic expression|In its contemporary setting, its geomorphic expression is an inclined shoreline sand deposit, with locally developed pavements and ribbons of beach rock, and a bouldery shoreline deposit.|16-MAY-23
21408|Cable Beach Sand|Type section locality|Cable Beach, latitude/longitude coordinates 17º 54' 29" S, 122º 12' 50" E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
21408|Cable Beach Sand|Description at type locality|FROM TOP :  10 cm shelly sand with Sepia and crab burrows;  90 cm layered/laminated medium sand; 100 cm laminated sand and shell gravel;  60 cm laminated coarse sand; and 60 cm laminated medium sand;  BASE|16-MAY-23
21408|Cable Beach Sand|Extent|The unit is widespread along the Canning Coast.|16-MAY-23
21408|Cable Beach Sand|Thickness range|At type locality 3.2 m thick.  Additionally, where coasts are retreating, the Cable Beach Sand tends to be a veneer 0.1-1 m thick underthe beach face.  Where intersected in cores and trenches, the Formation has been recorded as 3 m thick. Regionally, the unit appears as a sheet to discontinuous ribbon, some tens of kilometres long, but only up to 100-200 m wide and up to 3 m thick.|16-MAY-23
21408|Cable Beach Sand|Lithology|Light-coloured, laminated, bedded, to low-angle cross-bedded, medium to fine to coarse sand and shelly sand and some shell gravel. Locally, the Formation is cemented to form beachrock which occurs as a sloping rock pavement.  Sand grains may be dominantly quartz, or mixed quartz, bioclasts and limestone intraclasts and lithoclasts, and locally ooids. Shell content in the unit varies laterally, depending on the composition of the fauna that inhabited the contiguous low tidal flats. Locally, there are patches of mid- to high tidal cemented in situ beach rock forming shore-parallel ribbons, and indurated enough in some areas to form rock pavements. Where dominant, such cemented zones are referred to the Cape Boileau Calcarenite Member. Beachrock can be broken into slabs and reworked during storms, thus forming conglomerate and breccia beds in the upper-tidal zone; the slabs and breccia are embedded in laminated sand, bubble sand, and cross-laminated shelly sand and sand.  Thus, ribbons of limestone-intraclast conglomerate and breccia are present locally in the Formation.  Where dominant, such accumulations are referred to the Lombadina Conglomerate Member.|16-MAY-23
21408|Cable Beach Sand|Depositional environment|Beach|16-MAY-23
21408|Cable Beach Sand|Fossils|Autochthonous molluscan shells in middle to upper parts of the Formation include: Donax faba, Paphies sp., Nassarius dorsatus and Oliva lignaria. These are autochthonous biocoenoses. Transported molluscs shells include Acrosterigma reeveanum, Anadara crebricostata, Anadara granosa, Cardita incrassata, Melo amphora, Mimachlamys scabricostata, Oliva lignaria, Pinna bicolor, Septifer bilocularis, Solen kajiyamai, Spondylus wrightianus and Trisidos tortuosa.  It should be noted that much of the shell has been transported into the depositional lithotope from low tidal areas.  Shells in the upper part of the Formation include Donax faba, Sepia spp and Spirula spirula.|16-MAY-23
21408|Cable Beach Sand|Diastems or hiatuses|Hiatuses are developed locally within and on top of beachrock.|16-MAY-23
21408|Cable Beach Sand|Relationships and boundaries|The unit passes downwards, with gradational contact, into the underlying Port Smith Sand, and passes vertically upwards, with gradational contact, into the overlying Shoonta Hill Sand. The Formation is laterally equivalent to the Eighty Mile Beach Coquina which is adjoins with sharp contact, and to the Sandfire Calcilutite which it is cut into with sharp contact.  Locally, it interfingers with, and is overlain by the Cape Gourdon Formation.|16-MAY-23
21408|Cable Beach Sand|Age reasons|Radiocarbon dating of shells within the Formation places it in the Holocene, viz., 1090 +/- 160 yrs BP and 2100 +/- 180 yrs BP.|16-MAY-23
21408|Cable Beach Sand|Correlations|The formation is laterally equivalent to the Port Smith Sand, the Eighty Mile Beach Coquina, and the Sandfire Calcilutite|16-MAY-23
21408|Cable Beach Sand|Comments|Laminated sand and shelly sand , with in situ and reworked beachrock, and boulder conglomerate|16-MAY-23
21408|Cable Beach Sand|References|Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.|16-MAY-23
79373|Calgra Member|Name source|Calgra Bore (Lat. -22.97417 Long. 116.93583) on the Hardey 1:100 000 map sheet|16-MAY-23
79373|Calgra Member|Unit history|Previously included with the newly defined Cave Hill Member in the Meteorite Bore Member (e.g. Martin, 1999; Van Kranendonk et.al., 2015; Van Kranendonk and Mazumder, 2015), but now recognised as a separate unit above the Meteorite Bore Member.|16-MAY-23
79373|Calgra Member|Geomorphic expression|The Calgra Member is not extensively exposed, forming low hills in the type area in the Hardey Syncline that have a very distinctive chaotic, non-bedded, airphoto pattern and slightly darker weathering colour than the enclosing Kungarra Formation. It is also exposed in the nose of the Hardey Syncline, 2 km west-southwest of Cazput Yard, where it is truncated by the unconformity at the base of the Anthiby Formation.|16-MAY-23
79373|Calgra Member|Type section locality|About 15 km northwest of Calgra Bore on the Hardey 1:100 000 map sheet at Long. 116.873 Lat. -22.853. The type section starts at Long. 116.8726 Lat. -22.8526 and follows a south-southwest trending creek.|16-MAY-23
79373|Calgra Member|Extent|Exposure of the Calgra Member is limited, and is restricted to the northern limb of the Hardey Syncline along 2.5 km of strike in the vicinity of the type area, and in rare exposures in the core of the syncline.|16-MAY-23
79373|Calgra Member|Thickness range|Measured thickness of 59.7m in the type section along a north-northeast - south-southwest trending creek, at Long. 116.8726 Lat. -22.8526. Van Kranendonk et al. (2015) report a thickness of approximately 43 m in the type area, in contrast to the measured thickness of 59.7 m. Interpretation of aerial photographs suggests that thickness is indeed variable.|16-MAY-23
79373|Calgra Member|Lithology|The Calgra Member consists exclusively of glacigenic diamictite with striated and faceted dropstones consisting of carbonate, calc-silicate rock, sandstone, chert, and feldspar and/or quartz-phyric rhyolite (Martin, 1999; Van Kranendonk et al., 2015; Van Kranendonk and Mazumder, 2015).|16-MAY-23
79373|Calgra Member|Depositional environment|Deep-marine glacigenic diamictite deposited below storm wave-base and most likely reworked by mass flow.|16-MAY-23
79373|Calgra Member|Relationships and boundaries|The Calgra Member is conformably underlain and overlain by shales and fine-grained sandstones of the enclosing Kungarra Formation, but is truncated by the unconformity at the base of the Beasley River Quartzite, 1.5 km west of the type locality, and by the unconformity at the base of the Anthiby Formation in the core of the Hardey Syncline.|16-MAY-23
79373|Calgra Member|Identifying features|Contains distinctive striated dropstones of Woongarra Rhyolite and other lithologies derived from the underlying Fortescue and Hamersley Groups. Clast size appears to be significantly smaller on average than the Meteorite Bore Member.|16-MAY-23
79373|Calgra Member|Structure and Metamorphism|The Calgra Member has been strongly affected by the Ophthalmian cleavage in outcrop. Glacial dropstones are commonly preserved in strain shadows where this cleavage wraps around competent clasts. The metamorphic grade is no higher than lower greenschist facies.|16-MAY-23
79373|Calgra Member|Age reasons|Younger than the 2340 +/- 22 Ma maximum depositional age of the underlying Meteorite Bore Member (Caquineau et al., 2016; 2018), which has a Re-Os diagenetic age of 2312.7 +/- 5.6 Ma (Philippot et al. 2018), and older than the c. 2208 Ma Balgara Dolerite (Muller et al., 2005) that locally intrudes it.|16-MAY-23
79373|Calgra Member|Correlations|Prior to formal naming it was considered to be part of the Meteorite Bore Member, and correlated with the newly named Cave Hill Member (e.g. Martin, 1999), although it is now recognised as a stratigraphically distinct unit (e.g. Martin and Morris, 2010; Van Kranendonk et al., 2015; Van Kranendonk and Mazumder, 2015).|16-MAY-23
79373|Calgra Member|Defn author|D. McB. Martin, Geological Survey of Western Australia 7-JUL-2020.|16-MAY-23
79373|Calgra Member|Proposed publication|GSWA Report 203.|16-MAY-23
79373|Calgra Member|References|Caquineau, T, Paquette, J-L and Philippot, P 2016, In situ U?Pb zircon dating of the Meteorite Bore Member diamictites: constraints on the Paleoproterozoic glaciations and the Great Oxidation Event, in Goldschmidt Conference Abstracts: Goldschmidt Conference, Yokohama, Japan, 26 June 2016-1 July 2016, p. 364.   **Caquineau, T, Paquette, J-L and Philippot, P 2018, U-Pb detrital zircon geochronology of the Turee Creek Group, Hamersley Basin, Western Australia: Timing and correlation of the Paleoproterozoic glaciations: Precambrian Research, v. 307, p. 34-50.   **Martin, DMcB 1999, Depositional setting and implications of Paleoproterozoic glaciomarine sedimentation in the Hamersley Province, Western Australia: Geological Society of America Bulletin, v. 111, p. 189-203.  **Muller, SG, Krapez, B, Barley, ME and Fletcher, IR 2005, Giant iron-ore deposits of the Hamersley province related to the breakup of Paleoproterozoic Australia: New insights from in situ SHRIMP dating of baddeleyite from mafic intrusions: Geology, v. 33, no. 7, p. 577-580.   **Philippot, P 2016, Avila, JN, Killingsworth, BA, Tessalina, S, Baton, F, Caquineau, T, Muller, E, Pecoits, E, Cartigny, P, Lalonde, SV, Ireland, TR, Thomazo, C, Van Kranendonk, MJ and Busigny, V, 2018, Globally asynchronous sulphur isotope signals require re-definition of the Great Oxidation Event: Nature Communications, v.9, Article number 2245, 10 p.  **Van Kranendonk, MJ and Mazumder, R 2015, Two Paleoproterozoic glacio-eustatic cycles in the Turee Creek Group, Western Australia: Geological Society of America Bulletin, v. 127, no. 3-4, p. 596-607.  **Van Kranendonk, MJ, Mazumder, R, Yamaguchi, KE, Yamada, K and Ikehara, M 2015, Sedimentology of the Paleoproterozoic Kungarra Formation, Turee Creek Group, Western Australia: a conformable record of the transition from early to modern Earth: Precambrian Research, v. 256, p. 314-343.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Name source|Cape Boileau, latitude/longitude coordinates 17º 30' 58" S, 122º 11' 08" E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Geomorphic expression|As a shoreline pavement and locally as a cliffed calcarenite.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Type section locality|Cape Boileau, latitude/longitude coordinates 17º 30' 58" S, 122º 11' 08" E, Broome 1:250,000 Topographical Sheet|16-MAY-23
74631|Cape Boileau Calcarenite Member|Description at type locality|2 m of laminated to cross laminated calcarenite with layers of shells and pebbles.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Extent|Developed as a ribbon to lensoid body discontinuously along the coast from Pardoo Creek to Cape Leveque, though it tends to be better developed near headlands and rocky shores.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Thickness range|Thickness at type locality is 2 m.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Lithology|Cemented beachrock composed of laminated, bedded, to low-angle cross-bedded, medium to fine to coarse calcarenite and shelly calcarenite, with local layers of bubble sand, and locally incorporated slabs and breccia of (earlier cemented beachrock) intraclasts; ribbon deposit formed on and buried under the tidal beach face.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Depositional environment|Beach environment.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Fossils|Shells of the beach zone.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Diastems or hiatuses|Hiatuses are developed locally within and on top of beachrock ribbons and pavements.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Relationships and boundaries|Grades vertically and laterally into uncemented Cable Beach Sand; also the main sand lithology of the Cable Beach Sand may rest with sharp contact on this cemented calcarenitic Member; the Lombadina Conglomerate Member also often rests with sharp contact on this Member; at its type locality, the Cape Boileau Calcarenite Member abuts to landward a cemented orange Pleistocene palaeosol and Pleistocene aeolian calcarenite, and is onlapped to seaward by unconsolidated sand of the main Cable Beach Sand Formation.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Age reasons|Radiocarbon dating of shells within the Cable Beach Sand places this Member within the Holocene.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Correlations|As a Member with the formation of Cable Beach Sand, it shares the same stratigraphic boundary relationships and correlations as the cable Beach Sand, i.e., it is laterally equivalent to the Port Smith Sand, the Eighty Mile Beach Coquina, and the Sandfire Calcilutite.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Comments|Cemented beach sand, shelly sand, and pebbly sand.|16-MAY-23
74631|Cape Boileau Calcarenite Member|References|Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.|16-MAY-23
74631|Cape Boileau Calcarenite Member|Parent|Member of the Cable Beach Sand.|16-MAY-23
74624|Cape Gourdon Formation|Name source|After Cape Gourdon, latitude/longitude coordinates 18º 24' 22" S, 122º 01' 39" E, Lagrange 1:250,000 Topographical Sheet.|16-MAY-23
74624|Cape Gourdon Formation|Geomorphic expression|As alluvial fans emanating from the cliff cuts into Mowanjum Sand.|16-MAY-23
74624|Cape Gourdon Formation|Type section locality|Cliff exposure on coast near Cape Gourdon, latitude/longitude coordinates 18º 21' 52" S, 122º 02' 13" E, Lagrange 1:250,000 Topographical Sheet.|16-MAY-23
74624|Cape Gourdon Formation|Description at type locality|(top) 5 cm structureless orange sand; 80 cm interbedded laminated red sand, laminated orange sand, and laminated white sand, with local cobble-sized intraclast of calcarenite; 50 cm white structureless sand; and 10 cm structureless red muddy sand.|16-MAY-23
74624|Cape Gourdon Formation|Extent|The unit is widespread in the region as a semi-continuous to scattered lensoid deposit where Mowanjum Sand (Semeniuk 1980) crops out at the coast.|16-MAY-23
74624|Cape Gourdon Formation|Thickness range|Thickness at type locality 1.45 m.  Additionally, where exposed along the coast, the Formation has been recorded as up to 1.5 m thick. Regionally, the unit will appear as discontinuous lensoid deposits, individually, some tens of metres to several hundred of metres long, but only up to 100 m wide and 1.5 m thick.|16-MAY-23
74624|Cape Gourdon Formation|Lithology|In general, a bedded and laminated to cross-laminated interlayered red sand varying to orange quartz and quartz-and-carbonate sand (depending on carbonate sand content), and locally gravelly sand, and small limestone lenses composed of calcarenite; sand grains of carbonate laminae and layers are bioclastic, carbonate-intraclast, carbonate-lithoclast, and oolitic.|16-MAY-23
74624|Cape Gourdon Formation|Depositional environment|Alluvial fans debouching onto upper beach and supratidal beach environments.|16-MAY-23
74624|Cape Gourdon Formation|Fossils|Donax faba locally occurs in the lower parts of the Formation.  Anadara granosa shells underlying limestone lenses appear to be middens.|16-MAY-23
74624|Cape Gourdon Formation|Relationships and boundaries|The unit rests, with sharp contact, on layered sand of the Cable Beach Sand, or interfingers with the Cable Beach Sand.  It erosionally overlies and is cut into the Barn Hill Formation and the Shoonta Hill Sand.  It overlies the Mowanjum Sand and Barn Hill Formation with sharp inclined to gullied contact. The Formation also is overlain by Shoonta Hill Sand with sharp contact.|16-MAY-23
74624|Cape Gourdon Formation|Age reasons|No radiocarbon ages have been obtained from the Formation, but contemporary sedimentation and stratigraphic relationships with the Shoonta Hill Sand, Cable Beach Sand, and Barn Hill Formation (all dated as Holocene) places the Formation within the Holocene.|16-MAY-23
74624|Cape Gourdon Formation|Correlations|The formation is laterally equivalent to the Barn Hill Formation, the Shoonta Hill Sand and the Cable Beach Sand.|16-MAY-23
74624|Cape Gourdon Formation|Comments|Layered/laminated red and white sand and some shelly sand.|16-MAY-23
74624|Cape Gourdon Formation|References|For Canning Coast units: Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.For Mowanjum Sand: Semeniuk V 1980 Quaternary stratigraphy of the tidal flats King Sound, WA. Journal of the Royal Society of Western Australia 63: 65-78.|16-MAY-23
24214|Carolyn Formation|Name source|Carolyn Valley in the western St George Range (18o41'S, 124o55'E).|16-MAY-23
24214|Carolyn Formation|Unit history|Forms the upper part of the Grant Formation (Guppy et al, 1952) now termed Grant Group.  Referred to as the Binda Member in unpublished company reports and as "The upper sandstone unit" by Crowe & Turner (1976b).|16-MAY-23
24214|Carolyn Formation|Type section locality|Composite section of sequences at 18o44'20"S, 124o55'52"E and 18o41'53"S, 124o54'30"E.|16-MAY-23
24214|Carolyn Formation|Extent|Exposed in northern, eastern and southern parts of Canning Basin.  Distributed throughout the basin in the subsurface except where removed by erosion after deposition of the Grant Group.  Includes Wye Worry and Millajiddee Members defined in the Fitzroy Trough (Crowe & Towner, 1976a).|16-MAY-23
24214|Carolyn Formation|Thickness range|Thickest in the northwestern part of the Fitzroy Trough (364 m in Sisters No. 1).|16-MAY-23
24214|Carolyn Formation|Lithology|Mainly consists of massive or poorly bedded, moderate to poorly sorted, medium grained quartz arenite with some lithic and feldspathic wacke.  Details are given by Crowe & Towner (1976b).|16-MAY-23
24214|Carolyn Formation|Relationships and boundaries|Conformably overlies Winifred Formation and is overlain unconformably (in Fitzroy Trough) and conformably (elsewhere) by the Poole Sandstone.  In the southern Canning Basin the unit probably interfingers laterally with the Paterson Formation.|16-MAY-23
24214|Carolyn Formation|Age reasons|Contains pelecypods Eurydesma? Sp. Ind., Deltopecten lyonensis, Etheripecten cf. Tenuicollis, Streblopteria sp. In Wye Worry Member which Dickins et al (in press) believe indicate a late Sakmarian sensu lato age.|16-MAY-23
24214|Carolyn Formation|Proposed publication|Annual Report Geological Survey of Western Australia for 1976|16-MAY-23
79372|Cave Hill Member|Name source|Cave Hill (Lat. 116.5401 Long. -22.4978), west of Duck Creek Homestead on the Farquhar 1:100 000 mapsheet|16-MAY-23
79372|Cave Hill Member|Unit history|Prior to this definition, the unit was correlated with the Meteorite Bore Member of the Kungarra Formation, despite being at the top of the Boolgeeda Iron Formation (e.g. Martin, 1999; Van Kranendonk et.al., 2015; Van Kranendonk and Mazumder, 2015)|16-MAY-23
79372|Cave Hill Member|Geomorphic expression|A recessive weathering unit within the upper BIF of the Boolgeeda Iron Formation that includes the uppermost 10 m of BIF in this formation. Topographic expression is highly dependent on dip, and may be masked by regolith. The presence of the Cave Hill Member can be inferred by aerial photographic interpretation wherever the Boolgeeda Iron Formation appears to comprise a third narrow resistant BIF ridge, above the second ridge.|16-MAY-23
79372|Cave Hill Member|Type section locality|At the upper contact of the Boolgeeda Iron Formation 2.5 km southwest of Cave Hill on the Hardey 1:100 000 map sheet (Lat. 116.5221 Long. -22.5148)|16-MAY-23
79372|Cave Hill Member|Extent|The Cave Hill Member was initially thought to be restricted to the northwest Hamersley Province, north of a line between the Wyloo and Rocklea Anticlines. It is now considered likely to be present throughout the region, but local preservation is strongly affected by a paraconformity at the base of the Turee Creek Group and by regolith cover. Consequently, no outcrops of the Cave Hill Member have yet been found in the Turner or Turee Creek Synclines, or in the far eastern Hamersley Province. Good exposures of the member are rare, but have been confirmed from Yeera Bluff, and the Duck Creek, Hardey, and Brockman Synclines where they are relatively common.|16-MAY-23
79372|Cave Hill Member|Thickness range|The measured thickness of the glacigenic facies in the type area southwest of Cave Hill varies between 1.9 m (Martin, 1999) and 3.3 m (Van Kranendonk and Mazumder, 2015), but the full thickness of the member including the non-glacigenic lithologies has not been measured. In the Hardey Syncline, the total measured thickness is about 25 m. The glacigenic component of the Cave Hill Member thins from north to south. It is 4 m thick at Yeera Bluff (2.9 m according to Van Kranendonk and Mazumder, 2015), 1.9 m in the type section in the Duck Creek Syncline (3.35 m according to Van Kranendonk and Mazumder, 2015), and 0.55 m at Woongarra Pool. The total thickness of the Cave Hill member is varialble, due to the paraconformity at the base of the Turee Creek Group, but it is about 25 m thick at Woongarra Pool.|16-MAY-23
79372|Cave Hill Member|Lithology|In the type locality, the Cave Hill Member consists of diamictite, sandstone, conglomerate, shale, and banded iron-formation (BIF).|16-MAY-23
79372|Cave Hill Member|Depositional environment|The association with underlying and overlying banded iron formation suggests deposition of deep marine glacigenic sandstone, diamictite, mudstone, and local conglomerate, below storm wave-base, most likely in a pelagic to hemipelagic setting (Martin, 1999).|16-MAY-23
79372|Cave Hill Member|Relationships and boundaries|Conformably underlain by BIF of the Boolgeeda Iron Formation, and disconformably overlain by shales of the Kungarra Formation of the Turee Creek Group. The base of the Cave Hill Member is defined by the first appearance glacigenic diamictite in the Boolgeeda Iron Formation, and includes all overlying units below the contact with the Turee Creek Group.|16-MAY-23
79372|Cave Hill Member|Identifying features|Contains distinctive striated glacial dropstones of Woongarra Rhyolite derived from the underlying Hamersley Group. Glacigenic features are well-preserved in the type section, and in a reference section at Yeera Bluff on the Pannawonnica 100 000 map sheet (Lat. 116.1408 Long. -21.7066).|16-MAY-23
79372|Cave Hill Member|Structure and Metamorphism|The Cave Hill Member is preserved exclusively in synclines cored by the Turee Creek Group, and has not been as strongly overprinted by the Ophthalmian cleavage as the Meteorite Bore Member in the Hardey Syncline, consequently primary depositional features are well-preserved. The metamorphic grade is lower greenschist facies.|16-MAY-23
79372|Cave Hill Member|Age reasons|The Cave Hill Member is younger than the c. 2446 Ma maximum depositional age of the Boolgeeda Iron Formation (Simonson et al., 2014), and older than the 2340 +/- 22 Ma maximum depositional age of the Meteorite Bore Member (Caquineau et al., 2016; 2018). The maximum depositional age of the Cave Hill Member, as determined on a sample of the underlying Woongarra Rhyolite from Woongarra Pool is 2444 +/-3 Ma (GSWA 195892, Wingate et al. 2018).|16-MAY-23
79372|Cave Hill Member|Correlations|Prior to formal naming, the Cave Hill Member was considered a correlative of the Meteorite Bore Member, which also included the newly defined Calgra Member (e.g. Martin, 1999)|16-MAY-23
79372|Cave Hill Member|Defn author|D. McB. Martin, Geological Survey of Western Australia, 7-JUL-2020.|16-MAY-23
79372|Cave Hill Member|Proposed publication|GSWA report 203|16-MAY-23
79372|Cave Hill Member|References|Caquineau, T, Paquette, J-L and Philippot, P 2016, In situ U-Pb zircon dating of the Meteorite Bore Member diamictites: constraints on the Paleoproterozoic glaciations and the Great Oxidation Event, in Goldschmidt Conference Abstracts: Goldschmidt Conference, Yokohama, Japan, 26 June 2016-1 July 2016, p. 364.   **Caquineau, T, Paquette, J-L and Philippot, P 2018, U-Pb detrital zircon geochronology of the Turee Creek Group, Hamersley Basin, Western Australia: Timing and correlation of the Paleoproterozoic glaciations: Precambrian Research, v. 307, p. 34-50.   **Martin, DMcB 1999, Depositional setting and implications of Paleoproterozoic glaciomarine sedimentation in the Hamersley Province, Western Australia: Geological Society of America Bulletin, v. 111, p. 189-203.  **Simonson, BM, O'Brien, M, Buchwaldt, R, Bowring, SA, Hassler, SW and Beukes, NJ 2014, New geochronological data from the Boolgeeda BIF and Woongarra Rhyolite, Hamersley Group (Western Australia), in Abstracts: Geological Society of America; 2014 GSA Annual Meeting, Vancouver, British Columbia, 19 October 2014.  **Van Kranendonk, MJ and Mazumder, R 2015, Two Paleoproterozoic glacio-eustatic cycles in the Turee Creek Group, Western Australia: Geological Society of America Bulletin, v. 127, no. 3?4, p. 596-607.  **Van Kranendonk, MJ, Mazumder, R, Yamaguchi, KE, Yamada, K and Ikehara, M 2015, Sedimentology of the Paleoproterozoic Kungarra Formation, Turee Creek Group, Western Australia: a conformable record of the transition from early to modern Earth: Precambrian Research, v. 256, p. 314-343.  **Wingate, MTD, Lu, Y, Kirkland, CL and Johnson, SP 2018, 195892: rhyodacite, Woongarra Pool: Geochronology Record 1453, Geological Survey of Western Australia, 4 p.|16-MAY-23
80796|Charlotte Supersequence|Name source|The Charlotte Supersequence was defined using a sequence stratigraphic framework (integrating 2D seismic interpretations, new biostratigraphy & well log analysis).  It mostly coincides with Charlotte Sandstone hence has been assigned a similar name.|16-MAY-23
80796|Charlotte Supersequence|Unit history|The Charlotte Sandstone was briefly described by Backhouse (1984) and subsequently Crostella & Backhouse (2000) formalised the unit.|16-MAY-23
80796|Charlotte Supersequence|Type section locality|Charlotte 1 (-31.80879499, 115.45037501). The type section is the interval between 1574.4 and 2163.4 m (total thickness of 589 m). [GDA 94 assumed]|16-MAY-23
80796|Charlotte Supersequence|Extent|The Charlotte Supersequence is the youngest syn-rift sequence deposited prior to the breakup in the Valanginian (Seggie, 1990; Nicholson et al., 2008). Due to limited well penetration it is poorly defined. Palynological reports in Charlotte 1 (West Australian Petroleum Pty Ltd, 1971) and Peel 1 (Phillips Australian Oil Company, 1978) indicate a non-marine setting. Seggie (1990) interpreted the depositional environments to be lacustrine to fluvio lacustrine. From an increase in spore pollen counts from the underlying Carnac Formation, Ingram (1991) inferred that the sequence was deposited in a lower coastal - deltaic environment, however Marshall et al., (1993) interpreted it as fluvio-deltaic. Nicholson et al (2008) interpreted the Charlotte Supersequence to be deposited during a discrete extensional episode, possibly with slightly different direction of extension in comparison to the previous extensional phase which precedes the Valanginian breakup. See also distribution diagram in MS Word version of definition.|16-MAY-23
80796|Charlotte Supersequence|Thickness range|0 to 3625 m.  Thickness estimate is based on isochore thickness measurements derived from surfaces generated in 3D geological model (Borissova et al., 2014). The Supersequence exhibits a westward thickening growth wedge geometry within the Bathurst Syncline. Based on isochore thickness measurements (derived from surfaces generated in 3D model as described Borissova et al., 2014), its maximum thickness is 3625 m north of Parmelia 1.|16-MAY-23
80796|Charlotte Supersequence|Lithology|The Charlotte Supersequence consists predominantly of a very fine to very coarse quartzose sandstone with minor interbedded mudstone and coal. The effective porosity ranges from 0.05 to 0.25, and the permeability is from 0.119 to 441.82 mD.|16-MAY-23
80796|Charlotte Supersequence|Depositional environment|The Charlotte Supersequence is the youngest syn-rift sequence deposited prior to the breakup in the Valanginian (Seggie, 1990; Nicholson et al., 2008). Due to limited well penetration it is poorly defined. Palynological reports in Charlotte 1 (West Australian Petroleum Pty Ltd, 1971) and Peel 1 (Phillips Australian Oil Company, 1978) indicate a non-marine setting. Seggie (1990) interpreted the depositional environments to be lacustrine to fluvio lacustrine. From an increase in spore pollen counts from the underlying Carnac Formation, Ingram (1991) inferred that the sequence was deposited in a lower coastal - deltaic environment, however Marshall et al., (1993) interpreted it as fluvio-deltaic. Nicholson et al (2008) interpreted the Charlotte Supersequence to be deposited during a discrete extensional episode, possibly with slightly different direction of extension in comparison to the previous extensional phase which precedes the Valanginian breakup.|16-MAY-23
80796|Charlotte Supersequence|Fossils|Fusiformacysta tumida, Biretisporites eneabbaensis, Pentafidia charlottensis, P. punctate, Tetrachacysta baculata, ?Moorodinium sp.|16-MAY-23
80796|Charlotte Supersequence|Relationships and boundaries|It is unconformably overlain by the Valanginian to Aptian Warnbro Megasequence and is unconformably underlain by the Berriasian Hawley Member of the Carnac Formation. There is a major unconformity at the base onto which the Charlotte Supersequence onlaps in an easterly direction. The unconformity corresponds on seismic to a very high amplitude reflector.|16-MAY-23
80796|Charlotte Supersequence|Age reasons|Berriasian to Valanginian as determined by the presence of diagnostic microfossils as described above.  Helby et al (1987) and Partridge (2006) define the unconformity at the top of Dissimulidinium lobispinosum.|16-MAY-23
80796|Charlotte Supersequence|Defn author|Lech, M., 27-NOV-2013.|16-MAY-23
80796|Charlotte Supersequence|Comments|The base of the Charlotte Supersequence is equivalent to major sequence boundary "126" (Haq et al., 1987), the top of E. torynum of Helby et al., (1987) and near top "TS K1" sequence (Seggie, 1990).|16-MAY-23
80796|Charlotte Supersequence|References|Backhouse, J. (1984) Revised Late Jurassic and Early Cretaceous stratigraphy in the Perth Basin: Western Australia Geological Survey, Report 12, Professional papers, p1-6.  **Crostella, A. & Backhouse, J., 2000. Geology and petroleum exploration of the central and southern Perth Basin, Western Australia. Western Australia Geological Survey, Report 57, 85p (unpublished).  **Helby, R., Morgan, R. and Partridge, A.D., 1987: A palynological zonation of the Australian Mesozoic. In: Jell, P.A. (editor), Studies in Australian Mesozoic palynology; Memoir of the Association of Australasian Palaeontologists, no.4, p.1-94. **Ingram, B.S., 1991. Palynological review of wells in the Northern Vlaming Sub-basin, Perth Basin. Ampol Exploration Report 12694, DAR1164 (unpublished).  **Marshall, J.F., Ramsay, D.C., Moore, A.M.G., Shafik, S., Graham, T.G. & Needham, J. 1993. The Vlaming Sub-basin, offshore South Perth Basin. AGSO, Continental Margins Folio 7.  **Nicholson, C.J., Borissova, I., Krassay, A.A., Boreham, C.J., Monteil, E., Neumann, V., di Primio, R. & Bradshaw B.E., 2008. New exploration opportunities in the southern Vlaming Sub-basin, APPEA Journal, 371-379. **Seggie, R., 1990. Geological cross-sections of the Vlaming Sub-basin, South Perth Basin. Bureau of Mineral Resources, Geology and Geophysics, Record 1990/64.  **Phillips Australian Oil Company, 1978. Well completion report Peel No. 1 (unpublished). **West Australian Petroleum Pty Ltd, 1971 Well completion report Charlotte No. 1 (unpublished).|16-MAY-23
3926|Charteris Basalt|Name source|Charteris Creek'; grid reference 301312 to 305321 Nullagine 1:250 000 Sheet area.|16-MAY-23
3926|Charteris Basalt|Type section locality|6 km northeast of Spinaway Well (29353015) in the headwaters of Sandy Creek.|16-MAY-23
3926|Charteris Basalt|Extent|The formation is exposed over 50 km2 in the headwaters of Yandicoogina Creek.|16-MAY-23
3926|Charteris Basalt|Thickness range|Primary thickness 1 000 m.  Range after deformation 500-2 000 m.|16-MAY-23
3926|Charteris Basalt|Lithology|Pillow basalt with very subordinate chert and felsic lava.|16-MAY-23
3926|Charteris Basalt|Relationships and boundaries|Conformably overlies Corboy Formation (References a and b).  Conformably underlies Paddy Market Formation (References a and b).  Forms part of the Gorge Creek Group (References a and b).  Locally underlies Lalla Rookh Sandstone (References a and b) as a result of structural modification 10 km South of Yandicoogina Mining Centre (3070 3250).|16-MAY-23
3926|Charteris Basalt|Age reasons|Archaean, since forms part of Gorge Creek Group.|16-MAY-23
3926|Charteris Basalt|Comments|The formation is a local wedge-shaped volcanic unit within the Gorge Creek Group.  In this sense it is similar to the Honeyeater Basalt (References a and b) but the latter overlies the Paddy Market Formation.|16-MAY-23
3941|Cheela Springs Basalt|Unit history|The Cheela Springs Basalt is part of the Precambrian Wyloo Group (redefined, Trendall, 1979), south of the Hamersley Ranges.  The Cheela Springs Basalt (de la Hunty, 1965) is here raised from a member to a formation and excluded from the Mount McGrath Formation because it is overlain disconformably by clastics which are retained in the latter. (Map ref. Geological 1:250 000 Sheets Wyloo, Mount Bruce and Turee Creek). |16-MAY-23
3941|Cheela Springs Basalt|Extent| [?] Map ref. Geological 1:250 000 Sheets Wyloo, Mount Bruce and Turee Creek.|16-MAY-23
3941|Cheela Springs Basalt|Lithology|In the Cheela Springs area it is composed, at long. About 117degrees 58', of 900m of dominantly vesicular basalt with basal tuffaceous-looking shales which rest conformably on clastic rocks of the Beasley River Quartzite.|16-MAY-23
3941|Cheela Springs Basalt|Correlations|The correlation by Daniels (1968) of the Cheela Springs Basalt with formations composed largely of basic lavas in the Turee Creek Syncline and the Mount McGuire district are accepted. In the Mount McGuire area however, the Formation is thicker and contains shale bands with red chert nodules at other levels than the base. These units might well have been eroded prior to deposition of the overlying clastics in the Cheela Springs district.|16-MAY-23
3941|Cheela Springs Basalt|Proposed publication|Aust. CSIRO Inst. Earth Res. Rept No. FP. 22|16-MAY-23
3941|Cheela Springs Basalt|Comments|It was not re-examined in the Turee Creek Syncline area.|16-MAY-23
3941|Cheela Springs Basalt|References|02/32050, 79/04924, 99/29801, 81/21674, 80/20705|16-MAY-23
33196|Chiall Formation|Name source|Chiall Spring, Princess Ranges, WONGAWOL.|16-MAY-23
33196|Chiall Formation|Type section locality|The type area is along the Wongawol-Wiluna road, north from the foot of the range north of Kepaltin Pool (Fig. 1, WONGAWOL, MGA 393700E, 7099000N to 393500E, 7109200N).|16-MAY-23
33196|Chiall Formation|Extent|The Chiall Formation occupies the central part of the Earaheedy Basin, and comprises the rocks previously mapped as 'Wandiwarra Formation' and 'Princess Ranges Quartzite'. Three members are recognized within the Chiall Formation: the Karri Karri, Wandiwarra, and Princess Ranges Members.|16-MAY-23
33196|Chiall Formation|Thickness range|The Chiall Formation is about 1000 m thick, and perhaps about 1500 m in the central part of the NABBERU 1:250 000 sheet (Bunting, 1986).|16-MAY-23
33196|Chiall Formation|Lithology|The base of the type section is a ferruginized and glauconitic intraclast breccia dominated by clasts derived from stromatolitic carbonate of the Windidda Formation immediately below. In deeper parts of the basin, to the north and west, the hardground and overlying conglomerate and sandstone interval is now thought to be represented by the Karri Karri Member, the base of which is the top of the last granular iron-formation or chert interval. The formation is a coarsening- and shallowing-upward succession, dominated by siltstone and shale, but punctuated by sandstone intervals that become increasingly thick and common upward and eastward. Essentially, the Wandiwarra Member contains texturally and compositionally less mature sandstone intervals than the Princess Ranges Member ¿ much of the Wandiwarra Member is lithic wacke and quartz wacke, whereas the Princess Ranges Member is characterized by the presence of quartz arenite. The Karri Karri Member is defined separately.|16-MAY-23
33196|Chiall Formation|Relationships and boundaries|The Chiall Formation is conformable between the Frere or Windidda and Wongawol Formations. A conglomerate at the lower contact was interpreted by Bunting (1986) as indicating a probable disconformity, but it is now interpreted as a submarine hardground marking a rapid transgression rather than emergence. In more distal areas, the Karri Karri Member largely correlates with the hardground and conglomerate.|16-MAY-23
33196|Chiall Formation|Age reasons|Palaeoproterozoic (see Sweetwaters Well Member).|16-MAY-23
33196|Chiall Formation|Comments|The 'Wandiwarra Formation' and 'Princess Ranges Quartzite' were amalgamated into the Chiall Formation after the recognition that the two units form a single depositional package that can be consistently mapped as one unit. Fine-grained portions of the formation are commonly little different to the Wongawol Formation above. The Karri Karri Member is a distal equivalent of the Wandiwarra Member.|16-MAY-23
33196|Chiall Formation|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
24220|Christine Point Clay|Name source|Christine Point grid reference 123834 Derby 1:250 000 Sheet area.|16-MAY-23
24220|Christine Point Clay|Type section locality|6 metres are exposed in cliff 1.5 km south of Derby Jetty.|16-MAY-23
24220|Christine Point Clay|Extent|Exposed along banks of tidal creeks and foreshores between high and low tides between Christine Point and Airport Creek (grid references 123834 and 121817, Derby 1:250 000 Sheet).  Occurs in subsurface between Airport Creek and Point Torment (grid reference 119854, Derby 1:250 000 Sheet).  Over 100 km2 distributed in outcrop and subsurface.|16-MAY-23
24220|Christine Point Clay|Thickness range|Maximum recorded thickness 7.5 m, general thickness is 4-6 m.|16-MAY-23
24220|Christine Point Clay|Lithology|Homogenous to mottled slate grey clay; abundant mangrove stumps (up to 1.2 m diameter) and root fibers; scattered carbonate nodules; fauna includes Uca spp, Scylla serrata and Teredo spp and Thalassina anomala.  Fossil flora include Avicennia sp and Ceriops sp as in situ tree stumps.|16-MAY-23
24220|Christine Point Clay|Relationships and boundaries|Overlies Double Nob Formation (soil) with gradational contact or locally sharp contact.  Overlies Mowanjum Sands with gradational contact; transitional zone is mottled, mud, muddy sand, and sand, varigated colouration ranging from grey to orange to red.  Top is sharply overlain by Doctors Creek Formation contact is steeply inclined to irregular and may be marked by mud block breccia, mud ball conglomerate or fossil wool debris.|16-MAY-23
24220|Christine Point Clay|Age reasons|The unconformity, regional stratigraphic relationships and the fossil flora suggest a late Pleistocene age for the unit.|16-MAY-23
4046|Christmas Creek Member|Name source|Christmas Creek, tributary of the Fitzroy River which flows across the eastern part of the Noonkanbah Sheet area.|16-MAY-23
4046|Christmas Creek Member|Type section locality|Mt Piper in the Poole Range, Lat 18o54'00"S, Long 125o47'30"E.|16-MAY-23
4046|Christmas Creek Member|Extent|Crops out in the highest part of the Poole Range and at Mt Thorlan.  Discontinuously exposed on the plains between the Poole Range and the St George Range and along the northern flank of the St George Range.|16-MAY-23
4046|Christmas Creek Member|Thickness range|15 m at type section.  Maximum thickness is probably less than 25 m.|16-MAY-23
4046|Christmas Creek Member|Lithology|Consists of large-scale, cross-bedded, poorly sorted granule conglomerate and fine to coarse-grained sandstone.  Thin to medium-bedded, and in places some graded bedding.  Asymmetrical ripple-marks occur on bedding planes.|16-MAY-23
4046|Christmas Creek Member|Age reasons|No fossils found in the member which is dated as Artiniskian based on the ages of the overlying and underlying units.|16-MAY-23
74626|Church Hill Sand|Name source|After Church Hill, latitude/longitude coordinates 18º 21' 51" S, 122º 03' 52" E, Lagrange 1:250,000 Topographical Sheet.|16-MAY-23
74626|Church Hill Sand|Geomorphic expression|As red quartz sand dominated coastal dunes.|16-MAY-23
74626|Church Hill Sand|Type section locality|Sand dunes near coast adjoining Church Hill, latitude/longitude coordinates 18º 21' 51" S, 122º 02' 30" E, Lagrange 1:250,000 Topographical Sheet.|16-MAY-23
74626|Church Hill Sand|Description at type locality|400 cm structureless red quartz sand; sharp contact with mottled red sand of the Mowanjum Sand.|16-MAY-23
74626|Church Hill Sand|Extent|The unit is widespread along the Canning Coast as a semi-continuous to scattered shoe-string to lensoid deposit.|16-MAY-23
74626|Church Hill Sand|Thickness range|Thickness at type locality is 4 m.  However, where exposed along the coast, the Formation is usually 2-3 m thick, but has been recorded as up to 4 m thick. Regionally, the unit will appear as discontinuous shoe-string and lensoid deposits, individually, some tens of metres to several hundred of metres long, but only up to 100 m wide and 2-4 m thick.|16-MAY-23
74626|Church Hill Sand|Lithology|In general, a red quartz sand, mainly structureless, but locally with lamination and cross-lamination.|16-MAY-23
74626|Church Hill Sand|Depositional environment|Coastal environment.|16-MAY-23
74626|Church Hill Sand|Fossils|None.|16-MAY-23
74626|Church Hill Sand|Relationships and boundaries|The unit rests, with sharp to gradational contact, on Barn Hill Formation.  Locally it rests with sharp contact directly on Mowanjum Sand (Semeniuk 1980).  The Formation is overlain with sharp contact, or gradational contact, by Shoonta Hill Sand; if gradational, the transitional zone, some 1 m thick, is orange sand with a mixture of quartz sand and carbonate sand.|16-MAY-23
74626|Church Hill Sand|Age reasons|The Formation overlies the Barn Hill Formation which has been dated as Holocene, and hence the age of the Church Hill Sand also is Holocene.|16-MAY-23
74626|Church Hill Sand|Correlations|The Formation is laterally equivalent to the Shoonta Hill Sand, and the Barn Hill Formation.|16-MAY-23
74626|Church Hill Sand|Comments|Red coastal dune quartz sand where coastal processes have reworked the Mowanjum Sand.|16-MAY-23
74626|Church Hill Sand|References|For Canning Coast units: Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.For Mowanjum Sand: Semeniuk V 1980 Quaternary stratigraphy of the tidal flats King Sound, WA. Journal of the Royal Society of Western Australia 63: 65-78.|16-MAY-23
4067|Cistern Formation|Name source|Place name not recorded when stratigraphic name first used (Miller and Gair, 1975). Cistern is not recorded as a place name in the Gazetteer of Australian Place Names database.|16-MAY-23
4067|Cistern Formation|Unit history|Informally referred to as `Cistern formation? and 'Cistern rhyolite' when first used (Miller and Gair, 1975). Considered to be part of the Mons Cupri Volcanics (now Red Hill Volcanics) by Fitton et al. (1975). Formally defined as a formation of the Whim Creek Group by Smithies (1998). Assigned to the Bookingarra Group by Pike and Cas (2002) and Pike et al. (2002). Assigned to the Croydon Group by Van Kranendonk et al. (2006). Re-assigned to the Bookingarra Group by Hickman (2016) based on geochronological data and on sedimentological and structural evidence against correlation with units of the Mallina Basin succession (Croydon Group).|16-MAY-23
4067|Cistern Formation|Geomorphic expression|Different parts of the Cistern Formation outcrop on hills, ridges, or low-lying ground according to lithology.|16-MAY-23
4067|Cistern Formation|Type section locality|Mons Cupri (Lat. 20deg 53' S., Long. 117deg 48' E.) Roebourne 1:250 000 Sheet area.|16-MAY-23
4067|Cistern Formation|Description at type locality|At Mons Cupri the Cistern Formation comprises a lower felsic agglomerate facies and an upper volcaniclastic sedimentary facies including rhyolitic tuff, conglomerate, sandstone, and chert. The conglomerate is polymictic and poorly sorted with sub-angular to locally rounded clasts and blocks up to 10 m across. The clasts are mainly composed of porphyritic rhyolite, granite, and lesser basalt. The matrix of the conglomerate contains rhyolite shards, and has been intruded by felsic sills and dykes (Huston et al., 2000), providing evidence of volcanism coeval with sedimentary deposition.|16-MAY-23
4067|Cistern Formation|Extent|The Cistern Formation is confined to the Whim Creek greenstone belt, within which it is restricted to relatively small outcrops between Whim Creek and Red Hill (Lat. 20deg 58' S., Long. 117deg 32' E.), and in the Salt Well area (Lat. 20deg 45' S., Long. 117deg 42' E ).|16-MAY-23
4067|Cistern Formation|General description|Several lines of evidence indicate that deposition of the Cistern Formation and Rushall Slate was restricted to relatively small sections of the Whim Creek greenstone belt (Hickman, 2016). The proximal sedimentary facies of the Cistern Formation indicates that it was deposited adjacent to small felsic volcanic centres (Barley, 1987), related to local felsic intrusions of the c. 2950 Ma Sisters Supersuite (Hickman, 2016). Thin units of felsic tuff within the Rushall Slate are consistent with deposition during felsic volcanism of the Cistern Formation; however, the Rushall Slate was deposited farther away from the felsic volcanic centres.|16-MAY-23
4067|Cistern Formation|Thickness range|Up to 300 m thick (Smithies, 1998).|16-MAY-23
4067|Cistern Formation|Lithology|Outside the Mons Cupri area, the Cistern Formation is entirely represented by the upper volcaniclastic and sedimentary facies, which includes basal conglomerate unconformably overlying the Red Hill Volcanics of the Whim Creek Group. The Cistern Formation becomes finer grained and more siliciclastic upwards. In the respective type areas of the Cistern Formation and the Rushall Slate these formations are easily distinguished and constitute well defined separate mappable units; however, in other areas where transitional facies are dominant the distinction is less clear.|16-MAY-23
4067|Cistern Formation|Depositional environment|The regional setting was a zone of continental rifting and strike-slip faulting near the northwest margin of the Pilbara Craton. The Cistern Formation was deposited in high-energy depositional environments close to c. 2950 Ma volcanic centres (Barley, 1987). These centres were located above intrusions of the Sisters Supersuite. The Cistern Formation comprises proximal facies including volcaniclastic breccia and conglomerate. Detrital zircon ages in metasandstone of the Cistern Formation (Nelson, 2000) indicate derivation from 3006 - 2982 Ma felsic igneous rocks such as the Red Hill Volcanics (Whim Creek Group) or Maitland River Supersuite. Less common younger detrital zircons (2980?2960 Ma) in the Cistern Formation suggest an additional source not yet identified in the northwest Pilbara Craton.|16-MAY-23
4067|Cistern Formation|Relationships and boundaries|Parent is the Bookingarra Group.
The Cistern Formation unconformably overlies the Whim Creek Group and pebbles of rhyolite, dacite and basalt eroded from that unit are important constituents of its conglomerates. Granitic pebbles in these conglomerates were derived from pre-2955 Ma granitic intrusions, especially intrusions of the Maitland River Supersuite. The Cistern Formation is conformably overlain by the Rushall Slate, in some areas via a transitional sequence of fine-grained volcaniclastic and siliciclastic rocks. Where the Rushall Slate is absent the Cistern Formation is disconformably or unconformably overlain by either the Louden Volcanics or the Mount Negri Volcanics.|16-MAY-23
4067|Cistern Formation|Identifying features|Coarse felsic volcaniclastic rocks and thick units of felsic tuff are not present in other formations of the Bookingarra Group.|16-MAY-23
4067|Cistern Formation|Structure and Metamorphism|Local thrusting and folding of the Rushall Slate and Cistern Formation were reported by Krapez and Eisenlohr (1998). These structures might be related to folding of the c. 2940 Ma Whim Creek Anticline rather than belonging to a separate phase of deformation.|16-MAY-23
4067|Cistern Formation|Age reasons|Detrital zircon U-Pb dating establishes that the Cistern Formation is younger than 2964 +/- 6 Ma (Huston et al., 2002) and stratiform Pb-Zn mineralization within the Cistern Formation, interpreted to be syndepositional, has been dated at 2950 Ma (Richards and Blockley, 1984; Richards, 1986). The age of the unconformity that separates the Bookingarra Group from the underlying Whim Creek Group (Pike and Cas, 2002) is c. 2955 Ma (Hickman, 2016).|16-MAY-23
4067|Cistern Formation|Correlations|The Cistern Formation is partly laterally equivalent to the Rushall Slate, the units being linked by transitional facies. Stratigraphic correlations with formations outside the Whim Creek greenstone belt are impeded by major strike-slip movement on the Loudens Fault at c. 2940 Ma (Hickman, 2016). Additionally, the volcanic and sedimentary facies of the Cistern Formation indicate very localized deposition.	|16-MAY-23
4067|Cistern Formation|Alteration and Mineralisation|Varying degrees of silicification, epidote?chlorite alteration, and carbonate alteration affect the formation. A copper-rich stockwork at Mons Cupri is associated with intense chloritic alteration. This disseminated stockwork mineralization is overlain by a stratiform, 5 -10 m-thick Pb-Zn-Ag zone (Huston, 2006). The copper-rich stockwork contains chalcopyrite with minor sphalerite and galena, whereas the stratiform Pb-Zn zone contains pyrite, sphalerite, and galena with minor chalcopyrite and tetrahedrite and has carbonate alteration. Venturex Resources Limited (2015) estimated total resources at Mons Cupri to be 4.607 Mt at 0.9% Cu, 1.3% Zn, 0.5% Pb, and 24.1 g/t Ag.|16-MAY-23
4067|Cistern Formation|Geophysical Expression|Low TMI anomalies corresponding to the felsic composition of most of the formation.|16-MAY-23
4067|Cistern Formation|Geochemistry|Huston (2006) reported geochemical analyses of sandstone from the Cistern Formation to investigate alteration assemblages.|16-MAY-23
4067|Cistern Formation|Defn author|A.H. Hickman, Geological Survey of Western Australia, 2017.|16-MAY-23
4067|Cistern Formation|Proposed publication|Redefined as a formation of the Bookingarra Group (Hickman, AH, 2016, Northwest Pilbara Craton: a record of 450 million years in the growth of Archean continental crust: Geological Survey of Western Australia, Report 160, 104p).|16-MAY-23
4067|Cistern Formation|References|Barley, ME 1987, The Archaean Whim Creek Belt, an ensialic fault-bounded basin in the Pilbara Block, Australia: Precambrian Research, v. 37, p. 199-215.  **Fitton, MJ, Horwitz, RC and Sylvester, G 1975, Stratigraphy of the Early Precambrian in the West Pilbara: CSIRO Minerals Research Laboratories, Division of Mineralogy, Report FP 11, 41p.  **Hickman, AH 2016, Northwest Pilbara Craton: a record of 450 million years in the growth of Archean continental crust: Geological Survey of Western Australia, Report 160, 104p.  ** Huston, DL 2006, Mineralization and regional alteration at the Mons Cupri stratiform Cu-Zn-Pb deposit, Pilbara Craton, Western Australia: Mineralium Deposita, v. 41, p. 17-32.  **Huston, DL, Smithies, RH and Sun, S-S 2000, Correlation of the Archaean Mallina-Whim Creek basin: Implications for base-metal potential of the central part of the Pilbara granite-greenstone terrane: Australian Journal of Earth Sciences, v. 47, p. 217-230.  **Huston, DL, Sun, S -S, Blewett, R, Hickman, A, Van Kranendonk, M, Phillips, D, Baker, D, and Brauhart, C 2002, The timing of mineralisation in the Archaean Pilbara Craton, Western Australia: Economic Geology, v. 97, p. 733-755.  **Krapez, B and Eisenlohr, B 1998, Tectonic settings of Archaean (3325-2775 Ma) crustal-supracrustal belts in the West Pilbara Block: Precambrian Research, v. 88, p. 173-205.  **Miller, LJ and Gair, HS 1975, Mons Cupri copper-lead-zinc deposit, in Economic Geology of Australia and Papua New Guinea - Metals, edited by CL Knight: Australasian Institute of Mining and Metallurgy, Monograph 5, p. 195-202. **Nelson, DR 2000, 142949: metasandstone, Whim Creek, Geochronology Record 299: Geological Survey of Western Australia, 4p.  **Pike, G and Cas, RAF 2002, Stratigraphic evolution of Archaean volcanic rock-dominated rift basins from the Whim Creek Belt, west Pilbara Craton, Western Australia, in Precambrian Sedimentary Environments: A Modern Approach to Depositional Systems edited by W Altermann and P Corcoran: International Association of Sedimentologists, Special Publication 33, Blackwell Science, Oxford, UK, p. 213-234.  **Richards, JR and Blockley, JG 1984, The base of the Fortescue Group, Western Australia: Further galena lead isotopic evidence of its age: Australian Journal of Earth Sciences, v. 31, p. 257-268.  **Richards, JR, 1986, Lead isotope signatures: Further examination of comparisons between South Africa and Western Australia: Geological Society of South Africa Transactions, v. 89, p. 285-304.   **Smithies, RH 1998, Geology of the Sherlock 1:100 000 sheet: Geological Survey of Western Australia, 1:100 000 Geological Series Explanatory Notes, 29p.  **Van Kranendonk, MJ, Hickman, AH, Smithies, RH, Williams, IR, Bagas, L and Farrell, TR 2006, Revised lithostratigraphy of Archean supracrustal and intrusive rocks in the northern Pilbara Craton, Western Australia: Geological Survey of Western Australia, Record 2006/15, 57p.  **Venturex Resources Limited 2015, 2015 Annual Report: Report to Australian Stock Exchange, 30 September, 2015, 49p|16-MAY-23
79343|Cobb Formation|Name source|Lake Cobb (centred around 24deg 12'S, 126deg 16'E), and the eponymous Cobb Embayment of the Canning Basin, within which the unit is situated.|16-MAY-23
79343|Cobb Formation|Unit history|The sedimentary succession now recognised as Cobb Formation was first reported during water drilling by Farbridge (1967, 1968). These rocks were later found to sparsely outcrop and were mapped as an unnamed unit of presumed Permian age on the Scott 1:250 000 geological map (Daniels, 1972). During definition of the Cobb Embayment, these rocks were referred to as Paterson Formation (lateral equivalent to Grant Group) by Hocking (1994).|16-MAY-23
79343|Cobb Formation|Geomorphic expression|Isolated low scarps, hills and rises surrounded by extensive Cenozoic cover.|16-MAY-23
79343|Cobb Formation|Type section locality|Due to the scattered nature of outcrop, no single type section can be assigned to the Cobb Formation. The type locality encompasses a sparse cluster of small hills in the centre of the DICKENSON 1:100 000 map sheet area, 22-30 km east to east-northeast of Wanarn Community; centred around 25deg 15'S 127deg 48'E. The outcrops trend in a north-northwest direction from 1.5 -10 km north of the Great Central Road. Within this area three short gently dipping reference sections are nominated that represent the best exposures and include sites sampled for biostratigraphy and detrital zircon geochronology. Reference section 1: Base 25deg 13.227'S; 127deg 45.874'E; top 25deg 13.251'S 127deg 45.558'E. Reference section 2: Base 25deg 14.949'S 127deg 48.365'E; top 25deg 15.019'S 127deg 48.376'E. Reference section 3: Base 25deg 16.520'S 127deg 49.791'E; top 25deg 16.533'S, 127deg 49.356'E.|16-MAY-23
79343|Cobb Formation|Extent|Outcrops of the formation are restricted to the Cobb Embayment of the southeast Canning Basin, Western Australia. It is possible that the Cobb Formation extends west into the contiguous parts of Ryan Shelf under cover, but it has not been intersected in drillholes farther afield.|16-MAY-23
79343|Cobb Formation|General description|Beyond the type locality the Cobb Formation is dominated by sandstone, pebbly sandstone and conglomerate, with minor siltstone. Halite pseudomorphs have been noted in interbedded siltstone and fine grained sandstone at two localities. Regional paleocurrent data suggests predominant transport to northwest along the axis of the embayment. Trace fossils are rare outside the type locality and fish fossils have not been observed elsewhere.|16-MAY-23
79343|Cobb Formation|Thickness range|The thickness at the type locality is poorly constrained from surface data as individual outcrops in this area do not expose more than 20-30 m of section, at most. Regional thickness variations are poorly constrained due to sparse outcrop and limited subsurface data. Interpretation from the seismic line along the Great Central Road just east of the type locality suggest that the formation may reach up to 800 m in thickness near the Woodroffe Thrust, thinning north, but potentially this thickness could include unknown older stratigraphic units beneath the Cobb Formation. The formation thins to a featheredge along the northern and eastern extremities of the Cobb Embayment.|16-MAY-23
79343|Cobb Formation|Lithology|Predominantly fine- to coarse-grained red-brown sandstone, with recessive intervals of siltstone. Minor local conglomerate. A thin grey silty dolostone bed at the base of reference section 1.|16-MAY-23
79343|Cobb Formation|Depositional environment|Fluvial to restricted shallow marginal marine at the type locality. Poorly exposed conglomerate along the Woodroffe Thrust may be the remnants of alluvial fan deposits.|16-MAY-23
79343|Cobb Formation|Fossils|Fragmentary arandaspid fish fossils. Trace fossils include vertical and horizontal burrows and the arthropod traces Cruziana and Diplichnites.|16-MAY-23
79343|Cobb Formation|Diastems or hiatuses|None observed.|16-MAY-23
79343|Cobb Formation|Relationships and boundaries|Relationships at the type locality are not exposed, but the unit unconformably overlies Mesoproterozoic igneous and metasedimentary rocks of the Musgrave region to the east of the type area along the northern margin of the Cobb Embayment and locally overlies lower Neoproterozoic rocks of the Amadeus Basin to the northwest. It is possibly that the Cobb Formation could overlie older Canning Basin units in the depocentre of the Cobb Embayment beneath the type locality. The formation is inferred to abut rocks of the Musgrave region along the Woodroffe Thrust to the south, a structure that was active during sedimentation. The contact with the upper Carboniferous to lower Permian Grant Group outcropping west of the type locality is not exposed; it is assumed that the Grant Group overlies the Cobb Formation with a direct unconformable contact, but an intervening younger unit under cover is possible.|16-MAY-23
79343|Cobb Formation|Identifying features|Distinguished from the overlying Grant Group by its dominant red-brown colouration (Grant Group is typically grey to white), absence of glacial facies, and the local presence of distinctive fish and trace fossils. Quartz clasts dominate Cobb Formation conglomerates in contrast to the polymict composition of clasts in Grant Group conglomerate and diamictite.|16-MAY-23
79343|Cobb Formation|Structure and Metamorphism|Flat-lying to gently dipping and affected by minor faulting; dips may locally reach up to 30deg near faults. The southern margin of the Cobb Embayment was controlled by activity on the Woodroffe Thrust during deposition. No metamorphism.|16-MAY-23
79343|Cobb Formation|Age reasons|Ordovician, most likely mid-Ordovician, based on the arandaspid fish fossils and trace fossil assemblage. Early Ordovician maximum deposition age based on detrital zircon dating.|16-MAY-23
79343|Cobb Formation|Correlations|Because of the imprecise age, correlation of the Cobb Formation with other Ordovician units of the Canning Basin is uncertain. However it may correlate with fully marine units including the Willara, Goldwyer and Nita formations, or the paralic Carribuddy Group. None of these units, which mostly lack sandstones (except the Acacia Sandstone Member of the Willara Formation), are lithologically similar to the Cobb Formation.|16-MAY-23
79343|Cobb Formation|Alteration and Mineralisation|None observed.|16-MAY-23
79343|Cobb Formation|Geophysical Expression|Poorly imaged on seismic data along the Great Central Road, showing a southward thickening wedge terminating along the Woodroffe Thrust.|16-MAY-23
79343|Cobb Formation|Geochemistry|No data.|16-MAY-23
79343|Cobb Formation|Defn author|P.W. Haines and H-J. Allen  18 -DEC-2020.|16-MAY-23
79343|Cobb Formation|References|Daniels, JL (compiler) 1972, Scott, Western Australia: Geological Survey of Western Australia, 1:250 000 Geological Series Explanatory Notes, 19p.  **Farbridge, RA 1967, Drilling for water in Cobb depression, north of Wingellina: Geological Survey of Western Australia, Record 1967/17, 5p.  **Farbridge, RA 1968, Drilling for water in Cobb Depression, north of Wingellina, in Annual report for the year 1967: Geological Survey of Western Australia, Perth, Western Australia, p. 21-22.  **Hocking, RM 1994, Subdivisions of Western Australian Neoproterozoic and Phanerozoic sedimentary basins: Geological Survey of Western Australia, Record 1994/4, 85p.|16-MAY-23
4460|Constantine Sandstone|Name source|Mount Constantine; grid reference Long. 117o50', Lat. 21o03' on the Pyramid 1:250 000 Sheet.|16-MAY-23
4460|Constantine Sandstone|Type section locality|A sequence of arkosic grits, conglomerates and dominantly sandstone exposed in the Croydon Anticline between Croydon Station and Toweranna.|16-MAY-23
4460|Constantine Sandstone|Extent|The unit is well exposed in an area some 12 km west of Croydon Station and extends east through Croydon and some 30 km east of it.|16-MAY-23
4460|Constantine Sandstone|Thickness range|Up to 5 km in the type area.|16-MAY-23
4460|Constantine Sandstone|Lithology|Mainly quartz sandstone with basal arkosic grits and conglomerates.  There are minor intercalated greywackes.|16-MAY-23
4460|Constantine Sandstone|Relationships and boundaries|The unit is underlain by rocks of the Teichmans Group and overlain by the Mallina Formation.|16-MAY-23
4460|Constantine Sandstone|Age reasons|The unit is thought to be the equivalent of the Mons Cupri Volcanics and therefore to have an age approximately in the range between 2,500 and 2,300 m.y. (P.A. Arriens, pers. Com. 1975).|16-MAY-23
26299|Coorong Creek Adamellite|Name source|Coorong Creek, Marble Bar 1:250 000 Sheet area (M.G.R. 165 299).|16-MAY-23
26299|Coorong Creek Adamellite|Type section locality|The Coorong Creek Adamellite is well exposed near the lower reaches of Coorong Creek and along the Yule River above its junction with the creek.|16-MAY-23
26299|Coorong Creek Adamellite|Extent|The Coorong Creek Adamellite occurs in the Yule Batholith (see Fig. 1) as an irregular elongate mass (which resembles the outline of Italy), extending northwest and southwest across the lower reaches of Coorong Creek, west of Woodstock homestead, between latitudes 21o32'S and 21o45'S and longitudes 118o48'E and 119o00'E.  The pluton has an area of about 110 km2.|16-MAY-23
26299|Coorong Creek Adamellite|Lithology|The rock is a medium to coarse, even-grained biotite adamellite.  There are rare phenocrysts.  It is poorly to moderately foliated by alignment of feldspar, biotite, quartz and some biotite wisps and schlieren.  Medium, even-grained biotite granodiorite xenoliths and rare amphibolite xenoliths occur scattered throughout the pluton.  Pegmatites occur in most outcrops but are generally a minor feature.  The northwestern portion of the pluton has a more prominent foliation and contains more abundant xenoliths.  The adamellite contains microcline, oligoclase with myrmekite; biotite; accessory opaques, apatite, sphene, zircon and secondary chlorite, epidote, sericite and minor carbonate.|16-MAY-23
26299|Coorong Creek Adamellite|Relationships and boundaries|Contacts with the adjacent migmatite complex are diffuse but clearly intrusive.  The abundance of migmatite remnants within the pluton suggests remobilization of the complex and emplacement at higher structural levels.  Its relationship with the Abydos Adamellite is uncertain.  Possibly the Coorong Creek Adamellite intrudes the Abydos Adamellite.  The Coorong Creek Adamellite is intruded by quartz veins occurring along faults and by Lower Proterozoic dolerite dykes including the Round Hammock suite and contaminated, xenolith-bearing Mundine Well suite.  Much of the pluton is obscured by thin Quaternary sand and gravel deposits.|16-MAY-23
26299|Coorong Creek Adamellite|Age reasons|Archaean|16-MAY-23
28476|Corboy Formation|Name source|Corboy mining centre (military grid 248 285), Marble Bar 1:250 000 Sheet area.|16-MAY-23
28476|Corboy Formation|Type section locality|The type area for the Corboy Formation is around the Corboy mining centre in the Coongan Syncline.|16-MAY-23
28476|Corboy Formation|Extent|The Corboy Formation occurs in the centre of the Coongan Syncline.|16-MAY-23
28476|Corboy Formation|Thickness range|1-2 km|16-MAY-23
28476|Corboy Formation|Lithology|The unit consists mostly of quartzite, sandstone and psammopelitic sedimentary rocks.  There are minor felsic volcanics and ultramafic rocks in the southern portion of the formation and basalt, usually pillowed lavas, in the northern portion.|16-MAY-23
28476|Corboy Formation|Relationships and boundaries|The relationships of the Corboy Formation to the surrounding units is obscured by regional slides.  However, it probably overlies conformably the Wyman Formation and conformably underlies the Paddy Market Formation.  It is stratigraphically equivalent to rocks of the Soanesville Subgroup in the Soanesville Belt.|16-MAY-23
28476|Corboy Formation|Age reasons|Archaean|16-MAY-23
74633|Crab Creek Calcilutite Member|Name source|Crab Creek, latitude/longitude coordinates 17º 59' 46" S, 122º 22' 43" E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
74633|Crab Creek Calcilutite Member|Geomorphic expression|Mid to low tidal mud flats.|16-MAY-23
74633|Crab Creek Calcilutite Member|Type section locality|The type location is on the tidal flat seaward of Crab Creek, latitude/longitude coordinates 17º 59' 41''S, 122º 22 '13'' E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
74633|Crab Creek Calcilutite Member|Description at type locality|450 cm of interlayered cream laminated to burrow structured to bioturbated carbonate mud and shelly mud, with tellinid mollusc fragments dominating the shell content.|16-MAY-23
74633|Crab Creek Calcilutite Member|Extent|Developed in local areas such as as broad bays and embayments and lagoons where there are low energy conditions on the low tidal flats (e.g., Roebuck Bay).|16-MAY-23
74633|Crab Creek Calcilutite Member|Thickness range|The member generally is up to 5 m thick, but locally in the seaward parts of mud-filled tidal channels and ebb-tidal fans at the mouths of tidal creeks, it can be up to 8 m thick.|16-MAY-23
74633|Crab Creek Calcilutite Member|Lithology|White/cream shelly, laminated to burrow-structured calcilutite.|16-MAY-23
74633|Crab Creek Calcilutite Member|Depositional environment|Middle to low tidal flats.|16-MAY-23
74633|Crab Creek Calcilutite Member|Fossils|Molluscan shell remains in this Member include the bivalves Anadara granosa, Anomalocardium squamosa, Paphies striata, Tellina capsoides, Tellina piratica, Tellina spp, and the gastropod Nassarius dorsatus.|16-MAY-23
74633|Crab Creek Calcilutite Member|Relationships and boundaries|Gradationally overlain by Lagrange Calcilutite Member and gradationally locally underlain by Port Smith Sand; grades laterally into Port Smith Sand.|16-MAY-23
74633|Crab Creek Calcilutite Member|Age reasons|Location within Sandfire Calcilutite, its contemporary depositional setting, and some radiocarbon dates (Semeniuk 2008) indicate a Holocene age.|16-MAY-23
74633|Crab Creek Calcilutite Member|Correlations|Laterally equivalent to the Cable Beach sand and Port Smith Sand.|16-MAY-23
74633|Crab Creek Calcilutite Member|Comments|Laminated to burrow structured weakly shelly cream calcilutite.|16-MAY-23
74633|Crab Creek Calcilutite Member|References|Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.|16-MAY-23
74633|Crab Creek Calcilutite Member|Parent|Member of the Sandfire Calcilutite.|16-MAY-23
39658|Cudalgarra Member|Name source|Cudalgarra Claypans, 19deg 17' S, 122deg 03' E.|16-MAY-23
39658|Cudalgarra Member|Type section locality|Fully cored CRA Exploration P/L mineral exploration hole DD87SS7, 19deg12' 56.03" S 122deg19' 25.70"  E, from 1463.3 m to 1482.9m. Reference section with limited core, cuttings, and wireline logs in petroleum exploration hole Great Sandy 1, 19deg 12' 42.73" S, 122deg 21' 22.02" E,  from 1447 to 1469 m.|16-MAY-23
39658|Cudalgarra Member|Defn author|McCracken, S. (1994).|16-MAY-23
5437|Devon Consols Basalt|Name source|From the Devon Consols Gold Mining Lease 5913E.|16-MAY-23
5437|Devon Consols Basalt|Type section locality|Underground workings on the Devon Consols Gold Mining Lease (30deg44'00"S, 121deg28'40"E), 1/2 mile north-north-east of Mt Charlotte Reservoir.|16-MAY-23
5437|Devon Consols Basalt|Extent|In several belts resulting from repetition by folding. One belt trends noth-north-west from Williamstown for at least two miles; another of the same strike lies between the Golden Mile and Boulder townsite, and this same belt is traceable south for at least four miles.|16-MAY-23
5437|Devon Consols Basalt|General description|Outcrop pattern: Rare low rises.  See Specimen No. 12731, collected and analysed by the Geological Survey of Western Australia, Bulletin 69, p55.|16-MAY-23
5437|Devon Consols Basalt|Thickness range|Varies from 200 - 600 feet [61 - 183 m]|16-MAY-23
5437|Devon Consols Basalt|Lithology|Meta-basaltic lavas, in part pillow lavas, typically amphibolitic and zoisitic.|16-MAY-23
5437|Devon Consols Basalt|Relationships and boundaries|Conformably overlies the Hannan's Lake Serpentinite and is conformably overlain by the Kapai Slate.|16-MAY-23
5437|Devon Consols Basalt|Age reasons|Archaean.|16-MAY-23
5437|Devon Consols Basalt|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
5437|Devon Consols Basalt|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
5437|Devon Consols Basalt|References|GSWA Bulletin No. 69.   **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
24244|Diemals Formation|Name source|"Diemals" homestead, lat 37o39'S, long 119o18'E, BARLEE 1:250 000 Sheet area.|16-MAY-23
24244|Diemals Formation|Type section locality|17 km south-southwest of "Diemals" homestead.|16-MAY-23
24244|Diemals Formation|Extent|Poorly exposed in a roughly longitudinally trending belt 35 km long and up to 14 km wide, from 5 km west of Pigeon Rocks to 20 km west-northwest of "Diemals" homestead.|16-MAY-23
24244|Diemals Formation|Thickness range|Maximum thickness of 5 km (measured from airphotos)|16-MAY-23
24244|Diemals Formation|Lithology|The lowermost unit of the formation is a silty argillite with interbedded, lensoid oligomictic conglomerate containing rounded clasts up to15 cm long of quartz-albite porphyry and jaspilite.  Overlying this argillite is a metamorphosed coarse-grained argillaceous quartz arenite with narrow intraformational pebble conglomerate layers.  Interbedded with the meta-arenite are lenticular beds of quartzite.  The formation has been metamorphosed to low amphibolite facies.|16-MAY-23
24244|Diemals Formation|Relationships and boundaries|Unconformably overlies metavolcanics and graphitic phyllite of a greenstone belt and is intruded by biotite adamellite.  The base of the formation is poorly exposed while the top is unconformably overlain by Tertiary sediments.|16-MAY-23
24244|Diemals Formation|Age reasons|The intruding biotite adamellite is about 2.6-2.7 b.y. (H Chapman pers. comm. 1979) and the underlying greenstones are considered to have developed about 2.7 b.y. (Gee 1979).  The age is therefore about 2.6-2.7 b.y.|16-MAY-23
24244|Diemals Formation|Proposed publication|Western Australia Geological Survey Record|16-MAY-23
24244|Diemals Formation|Proposer|Walker I.W., Blight D.F.|16-MAY-23
24244|Diemals Formation|Resdate|22-MAR-1980|16-MAY-23
24244|Diemals Formation|Reserved? Yes/No|Y|16-MAY-23
36000|Dingo Creek Granite|Name source|Dingo Creek (409500E 7363500N MGA 94) on the Edmund 100K sheet area|16-MAY-23
36000|Dingo Creek Granite|Unit history|Named as the Dingo Granite by Pearson (1996) and Pearson et al (1996). The unit was renamed as the Dingo Creek Granite by Martin et al. (2002).|16-MAY-23
36000|Dingo Creek Granite|Geomorphic expression|Typically, low rounded hills covered in tors and boulders. Whalebacks present locally.|16-MAY-23
36000|Dingo Creek Granite|Type section locality|About 5.5 km WSW of Red Hill Bore on the Edmund 100k map sheet centred at 714300E 7367500N (MGA94, Zone 50). The type locality can be accessed via a station track from Red Hill Bore and then by travelling off road. The main rock type here, as elsewhere in the unit, is a medium-grained biotite-muscovite syenogranite with a trachytic texture defined by thin tabular phenocrysts of K-feldspar.|16-MAY-23
36000|Dingo Creek Granite|Extent|The unit comprises several elongate plutons aligned in an eastsoutheasterly direction, along with some small plugs and numerous dykes and veins. The unit outcrops in two belts less than 10 km wide and up to 30-40 km long within the Mangaroon Terrane in the northern Gascoyne Complex.|16-MAY-23
36000|Dingo Creek Granite|Lithology|Mainly consists of medium- to fine-grained porphyritic biotite-muscovite syenogranite or syenogranite. K-feldspar phenocrysts comprise 40% or more of the rocks, and define a trachytic texture. Contacts between syenogranite and monzogranite phases with slightly different composition, grainsizes or phenocryst abundances are common within the plutons.|16-MAY-23
36000|Dingo Creek Granite|Relationships and boundaries|The Dingo Creek Granite intruded rocks of the <c. 1680 +/- 13 Ma Pooranoo Metamorphics, as well as the c. 1675 Ma Pimbyana Granite. The Dingo Creek Granite is extensively intruded by veins and dykes of muscovite-biotite-tourmaline granite and pegmatite also belonging to the Durlacher Supersuite. The Dingo Creek Granite is unconformably overlain by sedimentary rocks of the Edmund Group (Bangemall Supergroup) on the Mangaroon and Edmund 100K sheets.|16-MAY-23
36000|Dingo Creek Granite|Age reasons|The Dingo Creek Granite has been dated by Pearson (1996) on the Mount Phillips 250k sheet at 1674 +/- 6 Ma, and by Nelson (GSWA 169062; Nelson, 2002) [, 2002 #870/ GSWA 169062] on Edmund at 1674 +/- 8 Ma. In addition, a sample from nearly 50km to the west-northwest on Mangaroon (GSWA 178028; Nelson, in prep.) gave an identical age of 1674 +/- 8 Ma.|16-MAY-23
36000|Dingo Creek Granite|References|Nelson D. R. 2002. Compilation of geochronology data 2001. Western Australia Geological Survey, Record 2002/2. ***Nelson D. R. in prep. Compilation of geochronology data, 2003. Western Australia Geological Survey, Record 2004/2 ***Pearson J. M. 1996. Alkaline rocks of the Gifford Creek Complex, Gascoyne Province, Western Australia - their petrogenetic and tectonic significance. PhD thesis (unpublished), University of Western Australia. ***Pearson J. M. Taylor W. R. & Barley M. E. 1996. Geology of the alkaline Gifford Creek Complex, Gascoyne Complex, Western Australia. Australian Journal of Earth Sciences 43, 299-309. ***Martin D. M. Thorne A. M. & Occhipinti S. A. 2002. Edmund, W.A. Sheet 2150. Western Australia Geological Survey,1:100 000 Geological Series.|16-MAY-23
74634|Djugun Member|Name source|Djugun Well north of Broome, latitude/longitude coordinates 17º 55' 44" S, 122º 14' 21'' E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
74634|Djugun Member|Geomorphic expression|High tidal to supratidal low gradient flat fringing the red sand dunes of the hinterland in the Canning region.|16-MAY-23
74634|Djugun Member|Type section locality|near Djugun Well, latitude/longitude coordinates 17º 55' 44" S, 122º 14' 21" E, Broome 1:250,000 Topographical Sheet|16-MAY-23
74634|Djugun Member|Description at type locality|175 cm of grey muddy sand and mottled orange/grey muddy sand; mud is calcilutaceous and kaolinitic.|16-MAY-23
74634|Djugun Member|Extent|Extensively developed along the Canning Coast as ribbon unit along the interface of Sandfire calcilutite and Mowanjum Sand (Semeniuk 1980).|16-MAY-23
74634|Djugun Member|Thickness range|0.3-2.0 m thick.|16-MAY-23
74634|Djugun Member|Lithology|Within the Sandfire Calcilutite, the deposits which are muddy red quartz sand, muddy brown quartz sand (mud in the muddy sand is kaolinitic and/or calcilutaceous); sheet-like deposit occurring between red sand and calcilutite.|16-MAY-23
74634|Djugun Member|Depositional environment|High tidal to mid-tidal zone where red sand dunes are onlapped by and mixed with carbonate mud accumulating from marine sedimentation, and kaolinitic clay is washed from the hinterland.|16-MAY-23
74634|Djugun Member|Fossils|Generally fossils are absent, but locally, there is mangrove wood and mangrove-habitat shells.|16-MAY-23
74634|Djugun Member|Relationships and boundaries|Interfingers with the Mowanjum Sand and the Lagrange Calcilutite Member of the Sandfire Calcilutite; along its base it rests on the Mowanjum Sand.|16-MAY-23
74634|Djugun Member|Age reasons|Stratigraphic considerations and one radiocarbon date (Semeniuk 2008) indicate a Holocene age.|16-MAY-23
74634|Djugun Member|Correlations|Laterally equivalent to the Lagrange Calcilutite Member.|16-MAY-23
74634|Djugun Member|Comments|Calcilutaceous muddy sand fringing the red sand dune hinterland.|16-MAY-23
74634|Djugun Member|References|For Canning Coast units: Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.For Mowanjum Sand: Semeniuk V 1980 Quaternary stratigraphy of the tidal flats King Sound, WA. Journal of the Royal Society of Western Australia 63: 65-78.|16-MAY-23
74634|Djugun Member|Parent|Member of the Sandfire Calcilutite.|16-MAY-23
24245|Doctors Creek Formation|Name source|Doctors Creek 2-10 km immediately north of Derby 1:250 000 Sheet area.|16-MAY-23
24245|Doctors Creek Formation|Type section locality|Banks of Doctors Creek|16-MAY-23
24245|Doctors Creek Formation|Extent|Well exposed along banks of Doctors Creek, Airport Creek and Alligator Creek; also along cliff foreshores of Mary Islands and south of Airport Creek.|16-MAY-23
24245|Doctors Creek Formation|Thickness range|Average thickness 9-12 m.|16-MAY-23
24245|Doctors Creek Formation|Lithology|4 main lithologies present typically in a fining-upward sequence.  Base composed of quartzose skeletal sand, laminated and cross-laminated up to 3 m(+) thick; upper part contains clay seams and flaser units; overlain by interlayered sand silt and clay laminates (2-3 m thick); sand and silt layers are quartzose and skeletal flaser bedding locally present; overlain by homogeneous-burrowed clay and silty clay 3-4 m thick with abundant roots and stumps of mangroves; locally shelly; overlain by laminated silt and clay alternating with vesicular clay (totalling c/m thick); abundant desiccation cracks and locally occurrence of mud chip conglomerates.  Limestone pebble mud-pebble and wood-debris conglomerates locally are developed at the unconformity and at erosional hiatuses within the formation.|16-MAY-23
24245|Doctors Creek Formation|Relationships and boundaries|Overlies Christine Point Clay with sharp erosional contact that is steeply inclined to irregular; contact may be marked by breccia, mud ball conglomerates and fossil wood debris.  Top of unit either is a contemporary depositional surface of the tidal flats neary Derby or is an eroded surface cut by contemporary erosional tidal processes.|16-MAY-23
24245|Doctors Creek Formation|Age reasons|The relationship of the unit and its facies to the contemporary tidal flat surface, the freshness of the fauna (shells), the composition of the floral community and stratigraphic relationships suggest this unit is Holocene-Recent in age.|16-MAY-23
24245|Doctors Creek Formation|Defn approved by|Western Australia Sub-Committee|16-MAY-23
24245|Doctors Creek Formation|Reserved? Yes/No|Yes|16-MAY-23
24254|Double Nob Formation|Name source|Double Nob Hillock; grid reference 821121, Derby 1:250 000 Sheet area.|16-MAY-23
24254|Double Nob Formation|Type section locality|0.3 m-1.0 m of grey, gravelly, muddy sand exposed at low tide along small cliff line between |16-MAY-23
24254|Double Nob Formation|Extent|The unit is exposed best at mouth of Airport Creek and in low tide zones between Airport Creek and Derby.  Elsewhere (e.g. Doctors Creek banks) the unit is patchily distributed.|16-MAY-23
24254|Double Nob Formation|Thickness range|0.3 m - 1.0 m.|16-MAY-23
24254|Double Nob Formation|Lithology|Grey muddy sand (quartzose) with scattered granules of pedogenic carbonate|16-MAY-23
24254|Double Nob Formation|Relationships and boundaries|Overlies the Airport Creek Formation with gradational contact.  Underlies Christine Point Clay; contact is sharp or locally gradational with transition zone (few decimeters thick) of burrow mottles, biogenic mixing and root casts.|16-MAY-23
24254|Double Nob Formation|Age reasons|Criteria of unconformity, soil features, and regional stratigraphic relationships place this unit in the Pleistocene.|16-MAY-23
24254|Double Nob Formation|Defn approved by|Western Australia Sub-Committee|16-MAY-23
24254|Double Nob Formation|Reserved? Yes/No|Yes|16-MAY-23
31270|Douri Sandstone|Name source|Douri dam, at GR CE832509, Ruby Plains 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area, WA.|16-MAY-23
31270|Douri Sandstone|Unit history|previously mapped mainly as Mount Forster Sandstone (Gemuts & Smith 1968)|16-MAY-23
31270|Douri Sandstone|Geomorphic expression| low hills and ridges.|16-MAY-23
31270|Douri Sandstone|Type section locality|6 km north of Beaudesert Bore, Ruby Plains 1:100 000 Sheet area, across northern limb of east-west trending syncline. Here the Douri Sandstone, dipping about 50? south, lies conformably on Boonall Dolomite (at GR CE657145) and is inferred to be overlain conformably by concealed Timperley Shale (at GR CE657142).|16-MAY-23
31270|Douri Sandstone|Extent|Southern and central Ruby Plains 1:100 000 Sheet area, Gordon Downs 1:250 000m Sheet area, WA; extends south into, but not mapped in, Billiluna 1:250 000 Sheet area..|16-MAY-23
31270|Douri Sandstone|Thickness range|maximum about 150 m, in type section.|16-MAY-23
31270|Douri Sandstone|Lithology|feldspathic/lithic to quartz-rich sandstone, minor micaceous siltstone, shale, and calcareous beds. Many beds contain pellet casts and quartz pebbles and granules. Ripple marks are common, and cross-bedding and desiccation cracks occur in places|16-MAY-23
31270|Douri Sandstone|Depositional environment|supratidal flats?|16-MAY-23
31270|Douri Sandstone|Relationships and boundaries|Of  Albert Edward Group. Appears to be conformable between Boonall Dolomite (below) and Timperley Shale (above).|16-MAY-23
31270|Douri Sandstone|Age reasons|Neoproterozoic. Part of the Albert Edward Group, which correlates with Supersequence 3 of the Centralian basin of Walter et al. (1995).|16-MAY-23
31270|Douri Sandstone|Correlations|sandstone band at base of Timperley Shale to north|16-MAY-23
31270|Douri Sandstone|References|*BLAKE, D.H., Tyler, I.M. & Sheppard, S., 1997. Geology of the Ruby Plains 1:100 000 Sheet area (4460), Western Australia,. Australian Geological Survey 	Organisation, Canberra.    *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.    *WALTER, M.J., Veevers, J.J., Calver, C.R. & Grey, K., 1995. Late Proterozoic stratigraphy of the Centralian Superbasin, Australia. Precambrian Research, 73, 173-195.|16-MAY-23
37648|Durlacher Supersuite|Name source|Durlacher Creek (407500E 7347400N MGA 94) on the Edmund 100K sheet area|16-MAY-23
37648|Durlacher Supersuite|Constituents|Pimbyana Granite, Dingo Creek Granite, Yangibana Granite and several other un-named units|16-MAY-23
37648|Durlacher Supersuite|Geomorphic expression|Typically, low rounded hills covered in tors and boulders. Whalebacks are common in some units.|16-MAY-23
37648|Durlacher Supersuite|Extent|Forms plutons, plugs and dykes mainly in a southeasterly trending terrane about 50 km wide in the northern Gascoyne Complex. However, large plutons belonging to the supersuite are also present on the central part of the Maroonah 100K sheet farther north (Martin et al., 2004), and on the Mount Phillips and Daurie Creek 100K sheets farther to the south (Culver, 2001; Nelson, 2001, GSWA 169848). On the Marquis 100K sheet, large plutons of the c. 1620 Ma Discretion Granite intrude reworked granitic gneisses in the Yarlarweelor Gneiss Complex to the southeast of the Gascoyne Complex (Sheppard and Swager, 1999).|16-MAY-23
37648|Durlacher Supersuite|Lithology|Mainly consists of monzogranite and granodiorite, with lesser syenogranite, and minor amounts of tonalite and rare gabbro. The granodiorite, monzogranite and syenogranite are medium to coarse grained and porphyritic (mainly tabular phenocrysts - megacrysts of K-feldspar). They contain biotite only, biotite and muscovite, or muscovite, biotite and tourmaline. Mesocratic granodiorite and tonalite phases are mostly equigranular. Gabbro intrusions contain xenocrysts of K-feldspar and quartz and contain mingling textures with the granites.|16-MAY-23
37648|Durlacher Supersuite|Relationships and boundaries|Granites (and gabbro) of the supersuite extensively intruded rocks of the <c. 1680 +/- 13 Ma Pooranoo Metamorphics, in contrast to older granites of the Moorarie Supersuite. However, where granites of the two supersuites intrude older rocks, they cannot reliably be distinguished unless dated. Granites of the Durlacher Supersuite are unconformably overlain by sedimentary rocks of the Edmund Group (Bangemall Supergroup) on the Maroonah and Mangaroon 100K sheets.|16-MAY-23
37648|Durlacher Supersuite|Age reasons|Several phases of the supersuite have been dated, including the Pimbyana, Yangibana and Dingo Creek Granites. Most granites that intruded the Pooranoo Metamorphics have igneous crystallization ages between 1685 and 1660 Ma (Sheppard and Occhipinti, in prep.). However, granites with crystallization ages between c. 1650 and c. 1620 Ma are known from elsewhere in the Gascoyne Complex (Sheppard and Swager, 1999; Culver, 2001; Nelson, 2001, GSWA 169848).|16-MAY-23
37648|Durlacher Supersuite|References|*NELSON D. R. 1998. Compilation of SHRIMP U-Pb zircon geochronology data, 1997. Western Australia Geological Survey, Record 1998/2.    *NELSON D. R. 2001. Compilation of geochronology data, 2000. Western Australia Geological Survey, Record 2001/2.    *CULVER K. E. 2001. Structure, metamorphism and geochronology of the northern margin of the Gurun Gutta granite, Central Gascoyne Complex, Western Australia. B.Sc (Hons) thesis, Curtin University of Technology    *SHEPPARD S. & Swager C. P. 1999. Geology of the Marquis 1:100 000 sheet. Western Australia Geological Survey, 1:100 000 Geological Series Explanatory Notes, 21p.    *MARTIN D. M. Sheppard S. Thorne A. M. & Copp I. A. 2004. Maroonah, W.A. Sheet 2051. Western Australia Geological Survey, 1:100 000 Geological Series.|16-MAY-23
21735|Eighty Mile Beach Coquina|Name source|Eighty Mile Beach, latitude/longitude coordinates 19º 40' 53" S, 120º 49' 44" E, Mandora 1:250,000 Topographical Sheet.|16-MAY-23
21735|Eighty Mile Beach Coquina|Geomorphic expression|Where contemporary, the geomorphic expression is as a plane, inclined, shoreline surface.|16-MAY-23
21735|Eighty Mile Beach Coquina|Type section locality|Coastal zone north east of Mandora homestead, latitude/longitude coordinates 19º 40' 31" S, 120º 51' 26" E, Mandora 1:250,000 Topographical Sheet.|16-MAY-23
21735|Eighty Mile Beach Coquina|Description at type locality|Top50 cm shelly sand with cuttlefish Sepia and crab burrows; 20 cm layered/laminated shell hash and sand; 10 cm sandy shell hash; 15 cm shelly sand; 10 cm sand with bubble structures; 40 cm shelly gravel; 20 cm shell gravel with sandy matrix; and 10 cm shell gravel with shell grit matrix(base).|16-MAY-23
21735|Eighty Mile Beach Coquina|Extent|The unit is widespread, though discontinuous, along the Canning Coast, particularly along the central parts of thr Canning Coast.|16-MAY-23
21735|Eighty Mile Beach Coquina|Thickness range|At type locality 1.75 m thick.  Additionally, in sections where coasts are retreating, the Eighty Mile Beach Coquina tends to be a 30-50 cm thick veneer on the beach face. In sections that are progradational, the Formation is developed as a ribbon 1-2 m thick.  Where intersected in cores and trenches, the Formation has been recorded as 3 m thick. Regionally, the unit will appear as a discontinuous ribbon, some tens of kilometres long, but only up to 100-200 m wide and up to 3 m thick.|16-MAY-23
21735|Eighty Mile Beach Coquina|Lithology|Light-coloured, laminated, bedded to cross-laminated, polymictic shell gravel, shell grit, shelly sand, and some coarse and medium sand layers. Sand grains are quartz, bioclasts and limestone intraclasts and lithoclasts. Lower parts of the Formation, where sandy, have scattered vertical burrows of the sand bubbler crab Scopimera, and middle to upper parts have scattered vertical burrows of the ghost crab Ocypode.|16-MAY-23
21735|Eighty Mile Beach Coquina|Depositional environment|High energy mid-high tidal beaches.|16-MAY-23
21735|Eighty Mile Beach Coquina|Fossils|Mixed allochthonous assemblages of molluscs, including the bivalves Acrosterigma reeveanum, Acrosterigma vlamingi, Anadara crebricostata, Anadara granosa, Antigona chemnitzii, Cardita incrassata, Chama reflexa, Chama sp. 1, Donax faba, Dosinia incisa, Eucrassatella pulchra, Hyotissa hyotis, Macoma praetexta, Mimachlamys scabricostata, Paphia semirugata, Paphies heterodon, Paphies striata, Pinna bicolor, Placamen gravescens, Placuna placenta, Saccostrea cucullata, Solen kajiyamai, Spondylus wrightianus, Tapes literatus, Tellina piratica, Trisidos semitorta, Trisidos tortuosa, Venus lamellaris, and unidentified Pectinid, and an unidentified Venerid, and the gastropods Bulla ampulla, Bulla guoyii, Chicoreus rubiginosus, Chicoreus ryosukei, Chicoreus sp., Cominella cf. lineolata, Conus textile, Conus trigonus, Cypraea pyriformis, Duplicaria duplicata, Ficus eospila, Fusinus colus, Herpetopoma atrata, Melo amphora, Murex macgillivrayi, Murex cf. acanthostephes, Nassarius dorsatus, Naticarius alapapiliones, Oliva lignaria, Planaxis sulcatus, Polinices conicus, Strombus campbelli, Terebralia palustris, and an unidentified Trochid.|16-MAY-23
21735|Eighty Mile Beach Coquina|Relationships and boundaries|The unit passes downwards, with sharp erosional contact, into the underlying Port Smith Sand, and passes vertically upwards, with sharp contact, into the overlying Shoonta Hill Sand. Locally, the Formation has a sharp erosional contact with the laterally equivalent Sandfire Calcilutite.  The Eighty Mile Beach Coquina is also laterally equivalent to the Cable Beach Sand, and its lateral contacts here are sharp (erosional), or interfingering.|16-MAY-23
21735|Eighty Mile Beach Coquina|Age reasons|Radiocarbon dating of shells within the Formation places it in the Holocene, viz., 3680 +/- 210 yrs BP.|16-MAY-23
21735|Eighty Mile Beach Coquina|Correlations|At the level of its depositional lithosome, the formation is laterally equivalent to the Port Smith Sand, the Cable Beach Sand, and the Sandfire Calcilutite|16-MAY-23
21735|Eighty Mile Beach Coquina|Comments|A coquina of shell gravel.|16-MAY-23
21735|Eighty Mile Beach Coquina|References|Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.|16-MAY-23
30279|Eliot Range Dolomite|Name source|Eliot Range, western central Antrim 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area, WA.|16-MAY-23
30279|Eliot Range Dolomite|Unit history|Previously mapped as part of the Bungle Bungle Dolomite (e.g., Gemuts & Smith, 1968), but now known, on stromatolite evidence, to be Neoproterozoic rather than Mesoproterozoic (Grey & Blake, in prep.)|16-MAY-23
30279|Eliot Range Dolomite|Geomorphic expression|hills, ridges and cuestas.|16-MAY-23
30279|Eliot Range Dolomite|Type section locality|Albert Edward Range, Halls Creek 1:100 000 Sheet area, from concordant contact with underlying Mount Kinahan Sandstone at GR CE730616 to concordant contact with overlying Illjarra Sandstone, at GR CE732614. Here the Eliot Range Dolomite is about 150 m thick and dips about 40? to the southeast.|16-MAY-23
30279|Eliot Range Dolomite|Extent|Ruby Plains, Halls Creek and Antrim 1:100 000 Sheet area in Gordon Downs 1:250 000 Sheet area, and Dixon 1:100 000 Sheet area in Dixon Range 1:250 000 Sheet area, WA.|16-MAY-23
30279|Eliot Range Dolomite|Thickness range|maximum probably less than 500 m; about 150 m in type section.|16-MAY-23
30279|Eliot Range Dolomite|Lithology|thickly to thinly bedded dolomitic mudstone, siltstone, and sandstone; dolomitic breccia; minor thin bands and lenses of chert; commonly stromatolitic - Linella avis identified by K. Grey (Grey & Blake, in prep.); ripple marks and cross-bedding evident in places.|16-MAY-23
30279|Eliot Range Dolomite|Depositional environment|shallow marine (Grey & Blake, in prep.).|16-MAY-23
30279|Eliot Range Dolomite|Relationships and boundaries|Of Ruby Plains Group. Overlies Mount Kinahan Sandstone conformably or disconformably; overlain conformably or disconformably by Illjarra Sandstone and unconformably by Moonlight Valley Tillite of Duerdin Group.|16-MAY-23
30279|Eliot Range Dolomite|Age reasons|Neoproterozoic - Tonian or Cryogenian. The Ruby Plains Group correlates with Supersequence 1 of the Centralian basin of Walter et al. (1995)|16-MAY-23
30279|Eliot Range Dolomite|Correlations|Bitter Springs Formation of Amadeus Basin, etc|16-MAY-23
30279|Eliot Range Dolomite|References|Blake, D.H., Tyler, I.M. & Sheppard, S., 1997. Geology of the Ruby Plains 1:100 000 Sheet area (4460), Western Australia,. Australian Geological Survey 	Organisation, Canberra. **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. **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. **Grey, K. & Blake, D.H., in press. **Walter, M.J., Veevers, J.J., Calver, C.R. & Grey, K., 1995. Late Proterozoic stratigraphy of the Centralian Superbasin, Australia. Precambrian Research, 73, 173-195.|16-MAY-23
6150|Empress Formation|Name source|Empress Gold Mine (abandoned); grid reference 21o9'S, 118o19'E, Pyramid 1:250 000 Sheet area.|16-MAY-23
6150|Empress Formation|Unit history|Correlated with Salgash Subgroup of Marble Bar and Nullagine 1:250 000 Sheets (Hickman & Lipple, in press).|16-MAY-23
6150|Empress Formation|Type section locality|2 km of mafic and ultramafic lavas, intercalated banded cherts, minor acid volcanics and thin sediments.|16-MAY-23
6150|Empress Formation|Extent|The formation strikes northeasterly from Teichmans Gold Mine and is best exposed in the region between that mine and the Yule River.  Rocks of this formation also occur between Kangan and Wodgina.|16-MAY-23
6150|Empress Formation|Thickness range|Range 1-2.5 km|16-MAY-23
6150|Empress Formation|Relationships and boundaries|Overlies Hong Kong Chert and conformably overlain by Wyman Formation.  Third formation of Teichmans Group.|16-MAY-23
6150|Empress Formation|Comments|Ultramafic lavas (peridotitic Komatiites) and high magnesian basalts (basaltic Komatiites) are characteristic of this formation.  A thin but persistent chert unit within this formation has a known strike length of at least 60 km and divides a lower from a lower mafic/ultramafic assemblage.|16-MAY-23
6150|Empress Formation|Reserved? Yes/No|Y|16-MAY-23
6229|Erica Sandstone|Name source|Erica Range, Stansmore 1:250 000 Sheet area 21o05S, 129o30'E.|16-MAY-23
6229|Erica Sandstone|Unit history|Mapped as partly Gardiner Beds and partly Phillipson Beds by Casey and Wells (1964; Wells, 1962).  Is youngest unit of the Redcliff Pound Group, which unconformably overlies Gardiner Sandstone north of the Lucas 1:250 000 Sheet.|16-MAY-23
6229|Erica Sandstone|Type section locality|North-facing scarp slope in the Erica Range, from 21o05'50"S 128o30'00"E to 21o07'00"S 128o29'00"E, where a sequence about 400 m thick of sublithic arenite is exposed.|16-MAY-23
6229|Erica Sandstone|Extent|Eastern part of Stansmore and southeast part of Lucas 1:250 000 Sheet areas, WA.|16-MAY-23
6229|Erica Sandstone|Thickness range|Maximum thickness exposed is about 700 m, in the southeast part of Stansmore 1:250 000 Sheet area.|16-MAY-23
6229|Erica Sandstone|Lithology|Sandstone.  Mainly medium-bedded, current bedded, well-sorted medium to fine grained, sublithic arenite with a clay matrix; minor quartz arenite.  Also flaggy micaceous sandstone and siltstone and rare conglomeratic sandstone.|16-MAY-23
6229|Erica Sandstone|Relationships and boundaries|Conformable on Murraba Formation.  Overlain, possibly unconformably, by Hidden Basin Beds, but contact concealed.|16-MAY-23
6229|Erica Sandstone|Age reasons|Probably Adelaidean|16-MAY-23
6229|Erica Sandstone|Defn author|Blake D.H., Hodgson I.M., 1975|16-MAY-23
6229|Erica Sandstone|Defn approved by|Western Australia. Taken from xerox copy of approved def. sent by Sub-Committee|16-MAY-23
6229|Erica Sandstone|Defn Reference|79/00465|16-MAY-23
6229|Erica Sandstone|First Reference|79/00474 Stansmore|16-MAY-23
6229|Erica Sandstone|Name first published by|Blake D.H., Yeates A.N., Walton D.C., 1976|16-MAY-23
6229|Erica Sandstone|Reserved? Yes/No|Y|16-MAY-23
6483|Fairfield Group|Name source|Fairfield' property, 125o04'E, 17o33'30"S, Lennard River 1:250 000 Sheet area.|16-MAY-23
6483|Fairfield Group|Constituents|Comprises the Gumhole Formation, Yellow Drum Sandstone, and Laurel Formation (Druce & Radke, in prep).|16-MAY-23
6483|Fairfield Group|Extent|Along the northerly margin of the Canning Basin for about 300 km.|16-MAY-23
6483|Fairfield Group|Thickness range|Range 370 m - 900+ m|16-MAY-23
6483|Fairfield Group|Lithology|Comprises limestone, sandstone, shale, siltstone and dolomite.|16-MAY-23
6483|Fairfield Group|Relationships and boundaries|The group conformably overlies sediments of the Upper Devonian Reef Complex (unnamed Famennian Birdseye limestone) and the Luluigui Formation.  It is overlain conformably by the Anderson Formation and unconformably by the Grant Formation.|16-MAY-23
6483|Fairfield Group|Age reasons|The Group straddles the Devonian-Carboniferous boundary.  It has yielded abundant brachiopods, conodonts, corals, nautiloids ostracods and microflora which indicate an age range from latest Late Devonian (?do V-do V) to Early Carboniferous (Tournaisian). |16-MAY-23
6483|Fairfield Group|Defn Reference|B200   ?[79/20374] |16-MAY-23
6483|Fairfield Group|Reserved? Yes/No|N|16-MAY-23
6483|Fairfield Group|Status|1|16-MAY-23
21803|Fly Flat Member|Name source|Fly Flat Bore ~ 21.3 Km north, north-west of the Olympic 1 well. Approximate coordinates: Lat: 18.12768deg S Lon: 122.55072deg E|16-MAY-23
21803|Fly Flat Member|Unit history|This unit has previously been informally referred to as the 'lower sandstone unit' of the Nambeet Formation including 'basal transgressive deposits' referred to by Kennard et al. (1994).|16-MAY-23
21803|Fly Flat Member|Geomorphic expression|The Fly Flat Member has been recorded only in the subsurface.|16-MAY-23
21803|Fly Flat Member|Type section locality|Olympic 1 well (-18deg17'57.60"S, 122deg38'23.40"E) between 1383.57 - 1447.53 m depth (63.53 m continuous drill core). Drill core archived in Geological Survey of Western Australia Perth Core Library.|16-MAY-23
21803|Fly Flat Member|Extent|The Fly Flat Member is recorded across the central-western parts of the Canning Basin, although confident identification is restricted to locations where the Nambeet Formation has been intersected by drilling. It has been drilled on the following tectonic sub-divisions: Broome Platform, Willara Sub-basin, Barbwire Terrace, Munro Arch, and Kidson Sub-basin and recently identified in the Waukarlycarly Embayment. It is probable that the member is present in the Samphire Graben, and extends further south into the Kidson Sub-basin than indicated by current records. The Nambeet Formation, and thus the Fly Flat Member, is interpreted to be absent on the southwestern edge of the Broome Platform based on seismic (Zhan 2019).|16-MAY-23
21803|Fly Flat Member|General description|The Fly Flat Member is identified as a sandstone package below a thick carbonate-mudstone sequence, most commonly overlying basement. A basal conglomerate or medium- to coarse-grained poorly consolidated sandstone and granitic 'basement wash' is present in some parts of the basin, particularly the north-west (e.g. wells Hedonia 1, Goldwyer 1 and Leo 1).|16-MAY-23
21803|Fly Flat Member|Thickness range|63.53 m was cored at the type locality, however, this is a minimum thickness as the base of the section was not recovered. Thickness of the Fly Flat Member varies from as thin as ~42 m to just over ~200 m, interpreted at Hilltop 1.|16-MAY-23
21803|Fly Flat Member|Lithology|The Fly Flat Member is composed of well-sorted, very fine-grained subarkose sandstone and minor siltstone. Sandstone composition is dominated by quartz and feldspar, with calcareous allochems comprising between 5-50% of grains. Calcareous allochems are predominantly fossil fragments and the incertae sedis cyanobacteria, Nuia. Minor to common detrital clay matrix is observed and may be locally enriched in organic material. Glauconite is present in trace amounts. Bioturbation is common ranging from minor to locally extensive, and bored hardgrounds with glauconite veneers are observed in the lower parts of the member. In other parts of the basin the Fly Flat Member contains a basal conglomerate or medium- to coarse-grained poorly consolidated sandstone and granitic 'basement wash'. This conglomeratic unit is not always present. X-ray diffraction indicates a quartz content of 50.9 - 79.9%, a K-feldspar content between 6.4-23.8 % and a carbonate content of between 10.2 - 31.4 % for the Fly Flat Member at the type section.|16-MAY-23
21803|Fly Flat Member|Depositional environment|At the type section the Fly Flat Member was deposited in shallow marine, shoreface settings (ranging upper to lower). Deposition occurred as part of early marine transgression into the Canning Basin.|16-MAY-23
21803|Fly Flat Member|Fossils|Conodonts, echinoderms, possible brachiopods, possible bivalves and the incertae sedis cyanobacteria, Nuia.|16-MAY-23
21803|Fly Flat Member|Diastems or hiatuses|Sharp planar or bored hardground surfaces are found between 1417.0 - 1447.8 m at the type locality. The upper contact of the member with the overlying Samphire Marsh Member is represented by an abrupt sequence boundary|16-MAY-23
21803|Fly Flat Member|Relationships and boundaries|At the type section the Fly Flat Member lies stratigraphically between the Samphire Marsh Member (above) and basement (below). Although the depositional sequence from Fly Flat to Samphire Marsh Member is regionally continuous, the contact at the type section is likely a disconformity. The lower basement contact is interpreted from seismic data at the type locality and  correlations to wells Hedonia 1, Hilltop 1, Goldwyer 1, Leo 1, Calamia 1, Samphire Marsh 1, Thangoo 1A, Thangoo 2 and Pictor 1 where drilling has shown it to overlie basement.|16-MAY-23
21803|Fly Flat Member|Relationships and boundaries|At the type section the Fly Flat Member lies stratigraphically between the Samphire Marsh Member (above) and basement (below). Although the depositional sequence from Fly Flat to Samphire Marsh Member is regionally continuous, the contact at the type section is likely a disconformity. The lower basement contact is interpreted from seismic data at the type locality and  correlations to wells Hedonia 1, Hilltop 1, Goldwyer 1, Leo 1, Calamia 1, Samphire Marsh 1, Thangoo 1A, Thangoo 2 and Pictor 1 where drilling has shown it to overlie basement.|16-MAY-23
21803|Fly Flat Member|Identifying features|Distinguished from the overlying Samphire Marsh Member by the abrupt change from dominantly sandy siliciclastic to carbonate-mudstone lithologies.|16-MAY-23
21803|Fly Flat Member|Structure and Metamorphism|Flat-lying to gently dipping depending on structural position. Locally affected by faulting (Zhan 2019). No metamorphism.|16-MAY-23
21803|Fly Flat Member|Age reasons|At the type section, the Fly Flat Member is assigned a Lower Ordovician, Tremadocian age based on the presence of the Paroistodus proteus conodont Biozone recorded in the top ~60 m of the member and into the overlying Samphire Marsh Member (Zhen et al., 2017). A U-Pb radiometric date of 479.37 +/- 0.16 Ma is recorded from a bentonite bed at 1383.27 m, 30 cm above the top of the member in the Samphire Marsh Member (Normore et al., 2017).|16-MAY-23
21803|Fly Flat Member|Correlations|The Fly Flat Member is laterally equivalent to the lower Wilson Cliffs Sandstone, which is recorded in the south eastern sections of the Canning Basin (wells Contention Heights 1, Kidson 1, Patience 2 and Wilson Cliffs 1 [type section]). As deposition is continuous from the Fly Flat Member into the Samphire Marsh Member at most localities, it is likely that the very top of the Wilson Cliffs Sandstone is equivalent to the base of the Samphire Marsh Member. The lower portions of the Fly Flat Member are also considered equivalent to the Kunian Sandstone (Prices Creek Group) described by Nicoll et al. (1993) in far northern parts of the Canning Basin. It is also possibly equivalent to the overlying Kudata Dolomite of the same group also described by Nicoll et al. (1993).|16-MAY-23
21803|Fly Flat Member|Geophysical Expression|This member is not differentiated from the Samphire Marsh Member on seismic work completed to date.|16-MAY-23
21803|Fly Flat Member|Defn author|L Dent and L Normore (18-Jan-2021)|16-MAY-23
21803|Fly Flat Member|Proposed publication|Dent, LM, Normore, LS, and Martin, SK 2021, Reference section, revised stratigraphy and facies analysis of the Ordovician Nambeet Formation, Canning Basin, Western Australia, Geological Survey of Western Australia, Report in press.|16-MAY-23
21803|Fly Flat Member|References|Kennard, JM, Jackson, MJ, Romine, KK, Shaw, RD and Southgate, PN 1994, Depositional sequences and associated petroleum systems of the Canning Basin, WA, in The sedimentary basins of Western Australia edited by PG Purcell and RR Purcell: Petroleum Exploration Society of Australia, Western Australian Branch, Perth, Western Australia, p. 657-676.  **Nicoll, RS, Laurie, JR and Roche, MT 1993, Revised stratigraphy of the Ordovician (late Tremadoc-Arenig) Prices Creek Group and Devonian Poulton Formation, Lennard Shelf, Canning Basin, Western Australia: Journal of Australian Geology and Geophysics, v. 14, p. 65-76.  **Normore, LS, Zhen, YY, Dent, LM, Crowley, JL, Percival, IG and Wingate, MTD 2018, Early Ordovician CA-IDTIMS U-Pb zircon dating and conodont biostratigraphy, Canning Basin, Western Australia: Australian Journal of Earth Sciences, v. 65, p. 61-73.  **Zhan, Y 2019, A seismic interpretation of the Broome Platform, Willara Sub-basin and Munro Arch of the Canning Basin, Western Australia: Geological Survey of Western Australia, Report 193, 43p.  **Zhen, Y, Percival, IG, Normore, LS and Dent, LM 2017, Floian (Early Ordovician) Conodonts of the Canning Basin, Western Australia - Biostratigraphy and Palaeobiogeographic Affinities with Chinese Faunas, in Proceedings of the International Geoscience Programme (IGCP) Project 653 Annual Meeting, p. 235-241.|16-MAY-23
80793|Gage Lowstand Fan|Name source|It largely coincides with the Gage Sandstone [?so named after Gage Sandstone].|16-MAY-23
80793|Gage Lowstand Fan|Unit history|It largely coincides with the Gage Sandstone. The Gage Sandstone Member was initially introduced by West Australian Petroleum Pty Ltd, (1969) and was formally recognised by Playford el al., (1976) as a member of the South Perth Shale. Davidson (1995) elevated the unit to a Gage Formation, but this name has since been superseded. A summary of the unit is outlined in Crostella and Backhouse (2000). Its upper boundary is equivalent to the 121.5 sequence boundary of Haq et al., (1987) and the ¿G.mutabilis¿ sequence boundary (Seggie, 1990). It is similar to the Top Gage Sandstone mapped by Causebrook et al., (2006), and the ¿Val_ts¿ horizon of Nicholson et al., (2008).|16-MAY-23
80793|Gage Lowstand Fan|Type section locality|Warnbro 1, -32.23769, 115.347327.  The type section is the interval between 2117.8 and 1949.5 m (total thickness of 164.3 m). [Core availability?]|16-MAY-23
80793|Gage Lowstand Fan|Extent|The Gage Lowstand Fan is penetrated by 8 petroleum exploration wells: Charlotte 1, Mullaloo 1, Minder Reef 1, Gage Roads 1, Warnbro 1, Peel 1, Parmelia 1, and Challenger 1. The Gage Lowstand Fan is absent where it onlaps topographic highs including the Roe and Parmelia highs, Mandurah Terrace, Vasse Shelf and Sugarloaf Arch. See distribution in figure included in MS Word definition document.|16-MAY-23
80793|Gage Lowstand Fan|Thickness range|The Gage Lowstand Fan 164.3 m thick at Warnbro 1.  The maximum known thickness intersected at a well is 309.7 m in Mullaloo 1. Based on the isochore thickness map, it is thickest (up to 630 m) at the mouth of a large, broad canyon adjacent to the Mandurah Terrace/Badaminna Fault Zone, approximately 20 km northeast of Warnbro 1, and on the inclined, undulating basin plain west of Warnbro 1.|16-MAY-23
80793|Gage Lowstand Fan|Lithology|Consists of poorly sorted fine-grained to granular feldspathic sandstone interbedded with dark grey/black micaceous mudstone and siltstone. It is a good reservoir with core porosities of 9.5-23.9% and permeabilities from 52-1340 mD. Based on measurements obtained from the conventional core, Causebrook et al., (2006) classified the Gage Sandstone as grain-supported subarkose sandstone, with an average grain composition classified on a ternary diagram as Q89.3F9.2R1.7. They identified three minor mineral associations: 1) ferroan carbonate-rich subarkose sandstone, 2) calcite-cemented subarkose sandstone and 3) pyrite-cemented subarkose sandstone). From examination of core, a range of textures from "very poorly sorted massive sandstone to fine to medium-grained laminated sandstone interbedded with siltstone and mudstone" were also determined.|16-MAY-23
80793|Gage Lowstand Fan|Depositional environment|Deposited in palaeotopographic lows of the Valanginian breakup unconformity, it is a sand-rich submarine fan system, similar to the model proposed by Richards et al., (1998).  It consists of lowstand deposits including channelised turbidity current deposits,slumps, debrites, lateral accretionary packages and fine-grained suspension deposits.. G. mutabilis dinoflagellates were originally deposited in a lagoonal (or similar) environment and were subsequently redeposited in an enclosed embayment via mass transport flows (Macphail, 2012). The interpretation of the Gage as a lowstand deposit concurs with previous interpretations of the Gage Sandstone (Spring and Newell, 1993; Causebrook, 2006 and Nicholson et al., 2008). Mapping the position of the shelf break, slope and the basin plain on the 2D seismic indicates that the Gage Lowstand Fan was deposited in water depths of at least 300 m.|16-MAY-23
80793|Gage Lowstand Fan|Fossils|Gagiella mutabilis, Aprolobocysta galeata, Batiacasphaera sp, Pentafidia charlottensis, Antulsporites saevus, Laevigatosporites belfordii, Polypodiidites horridus, Aequitriradites dandangarensis, Ruffordiasp. australiensis.|16-MAY-23
80793|Gage Lowstand Fan|Relationships and boundaries|It is a constituent within the LST of South Perth Sequence 2 of the South Perth Supersequence.  The Gage Lowstand Fan downlaps and onlaps the Valanginian Unconformity. At Warnbro 1, it uncomfortably overlies the Jervoise Sandstone. The Valanginian Unconformity here was identified between G. mutabilis and F. tumida Dinocyst zones. The boundary between the Gage Lowstand Fan and the overlying South Perth Sequence 2 is a major flooding surface (characterised by a sharp shift downwards to a lower gamma ray signature). At Warnbro 1 this surface is located between the G. mutabilis and K. scrutillinum Dinocyst zones. The relationship between the Gage Lowstand Fan and the underlying strata ranges from angular to conformable in nature. The top of the Gage Lowstand Fan corresponds to a strong seismic reflection. The section above is characterised by evident downlaps and onlaps onto the Valanginian Unconformity and downlaps on the top of the Gage Lowstand Fan. This made extrapolation from the well ties relatively easy.|16-MAY-23
80793|Gage Lowstand Fan|Identifying features|The Gage Lowstand Fan contains poorly-sorted interbedded sandstone and siltstone which were identified by their topographic position and by the presence of the G. mutabilis Dinocyst Zone (Backhouse, 1988). Based on the microplankton range chart from Backhouse (1988) and Ingram (1991), the G. mutabilis Dinocyst Zone is subdivided into upper and lower subzones, of which the Gage Lowstand Fan is represented by the Lower G. mutabilis Dinocyst subzone. This was based on the observation that the upper subzone contains the marine dinoflagellates Senoniasphaera tabulata which marks a ¿gentle marine incursion¿ (Monteil, 2005) and the onset of deeper-water marine conditions, whereas the lower subzone does not contain these species. The flooding surface identifying the top of the lowstand fan is at 136.6 Ma and corresponds to the top of S. areolata Dinocyst Zone (Helby et al., 1987; Partridge, 2006).|16-MAY-23
80793|Gage Lowstand Fan|Age reasons|Valanginian as determined by the presence of diagnostic microfossils, particularly the presence of the Lower Gagiella mutabilis Dinocyst subzone. The Lower G. mutabilis Dinocyst subzone contains the following diagnostic microfossils: Aprolobocysta galeata, Batiacasphaera sp, Pentafidia charlottensis, Antulsporites saevus, Laevigatosporites belfordii, Polypodiidites horridus, Aequitriradites dandangarensis, Ruffordia sp. and Australiensis (Macphail, 2012).|16-MAY-23
80793|Gage Lowstand Fan|Defn author|Lech, M. 21-NOV-2013|16-MAY-23
80793|Gage Lowstand Fan|Comments|Where subdivision between the Upper and Lower G. mutabilis Dinocyst subzones was possible, the Gage Lowstand Systems Tract is confined to the Lower G. mutabilis Dinocyst subzone. Mullaloo 1 is the exception. The subdivision by Ingram (1991) assigns the top of the lowstand sand in the Upper G. mutabilis Dinocyst subzone. However, he admitted low confidence in this sub-division as i) no marine dinoflagellates were found in the upper subzone, and ii) there were downhole cavings. Subsequent studies either didn¿t differentiate the upper and lower subzones (Monteil, 2005) or have not sampled the zone previously identified as the Upper G. mutabilis Dinocyst subzone (Macphail, 2012), thus it is most likely that the flooding surface at the top of the Gage Lowstand Fan is indeed in the Lower G. mutabilis Dinocyst subzone. At Warnbro 1, Macphail (2012) provided an different K. scrutillinum- G. mutabilis Dinocyst Zone boundary by revising the G. mutabilis Dinocyst Zone boundary up from 1961.1 m (Monteil, 2005) to 2094.281 m, and lowering the K. scrutillinum Dinocyst Zone boundary from 1939.9 m (Monteil, 2005) to 2011.68 m. This was based on the assumption that ¿specimens of G. mutabilis at 1966.87 mRT are contaminants¿. Key sidewall cores at the K. scrutillinum - G. mutabilis Dinocyst zones boundary were affected by mud-contamination and as a consequence, the confidence ratings were very low or indeterminate. Therefore this interpretation has been disregarded. The original interpretation aligns better with the upper boundary of the Gage Lowstand Fan being within the G. mutabilis Dinocyst Zone. For all wells except Parmelia 1, all Dinocyst zones from the G. mutabilis to B. jaegeri are intersected in every well. At Parmelia 1, the K. scrutillinum Dinocyst Zone is not identified suggesting that this particular succession was subject to erosion after the deposition of G. mutabilis Dinocyst Zone. Possible explanations for this were explored by Causebrook et al., (2006).|16-MAY-23
80793|Gage Lowstand Fan|References|Backhouse, J., 1988. Late Jurassic and Early Cretaceous palynology of the Perth Basin, Western Australia: Western Australia Geological Survey, Bulletin 135, 233p.  **Causebrook, R., Dance, T., Bale, K., 2006. Southern Perth Basin site investigation and geological model for storage of Carbon dioxide. CO2CRC Report Number; RP06-0162 (unpublished).  **Crostella, A. & Backhouse, J., 2000. Geology and petroleum exploration of the central and southern Perth Basin, Western Australia. Western Australia Geological Survey, Report 57, 85p (unpublished).  **Davidson, W.A., 1995. Hydrogeology and groundwater resources of the Perth region, Western Australia: Western Australia Geological Survey, Bulletin 142, 257p. **Helby, R., Morgan, R. and Partridge, A.D., 1987. A palynological zonation of the Australian Mesozoic. In: Jell, P.A. (Ed.), Studies in Australian Mesozoic palynology; Memoir of the Association of Australasian Palaeontologists, 4, 1-94.  **Ingram, B.S., 1991. Palynological review of wells in the Northern Vlaming Sub-basin, Perth Basin. Ampol Exploration Report 12694, DAR1164 (unpublished).  **Macphail M., 2012. Palynostratigraphic analyses of samples encompassing the Valanginian unconformity in Challenger-1, Mullaloo-1, Parmelia-1, Peel-1, Quinns Rock-1 & Warnbro-1, Warnbro & Parmelia groups, Vlaming Sub-basin, Perth Basin (unpublished).  **Monteil, E., 2005. Biostratigraphic re-appraisal of nine wells from the northern Vlaming Sub-basin, Perth Basin, Australia. Geoscience Australia Professional Opinion 2005/05 (unpublished).
Nicholson, C.J., Borissova, I., Krassay, A.A., Boreham, C.J., Monteil, E., Neumann, V., di Primio, R. & Bradshaw B.E., 2008. New exploration opportunities in the southern Vlaming Sub-basin, APPEA Journal, 371-379.  **Partridge, A.D., 2006. Jurassic ¿ Early Cretaceous dinocyst zonation NWS Australia: 1st Update of HMP 2004. In: Monteil E. (Ed.): Australian Mesozoic and Cenozoic Palynology Zonations - updated to the 2004 Geologic Time Scale. Geoscience Australia Record 2006/23.  **Playford, P. E., Cockbain, A. E., & Low. G. H., 1976. The geology of the Pert Basin. Western Australia Geological Survey. Bulletin 124, 311p.  **Spring, D.E. & Newell, N.A., 1993. Depositional systems and sequence stratigraphy of the Cretaceous Warnbro Group, Vlaming Sub-basin, Western Australia. The APPEA Journal 33(2), 190-204.   **West Australian Petroleum Pty Ltd, 1969. Gage Roads 1 No 1 well completion report (unpublished).|16-MAY-23
26586|Golden Mile Dolerite|Name source|The Golden Mile is the well established name of the main gold producing area of the Kalgoorlie field. It is centered about the Fimiston Post Office  and embraces the present (1963) producing leases of Great Boulder Gold Mines Ltd  and Lake View and Star Ltd, the Fimiston leases of Gold Mines of Kalgoorlie (Aust.) Ltd, and the southern leases of North Kalgurli (1912) Ltd.|16-MAY-23
26586|Golden Mile Dolerite|Type section locality|Underground workings on the Golden Mile, centred about the Fimiston Post Office (30deg46'40''S, 121deg 27'50''E).|16-MAY-23
26586|Golden Mile Dolerite|Description at type locality|Workings on the Eastern Lode system mainly expose the chloritic variety, while those on the Western Lode System expose both altered chloritic and original amphibolitic varieties. The two lode systems are separated by a tight infold of the overlying Black Flag Beds.|16-MAY-23
26586|Golden Mile Dolerite|Extent|From the Golden Mile the sill trends north-north-west and south-south east in several belts, the result of repetition by folding.|16-MAY-23
26586|Golden Mile Dolerite|General description|Outcrops are poor and may be completely oxidised or quite fresh. In either case, outcrops form low rubbly rises. Well represented by speciments collected and analysed by the Geological Survey of Western Australia: (a) chlorite-carbonate variety - No's 1728, 1729, 1730, 1750, 1751, 1753, 1796, 1800, 2502, 11184, 13464, 13466, 13472, 13473. (b) quartz-dolerite and meta-quartz-gabbro - No's 2117, 10436, 11008. These numbers are the original numbers given in Geological Survey of Western Australia Bulletin Nos. 6, 42, 51, 67, 69 and 94.|16-MAY-23
26586|Golden Mile Dolerite|Thickness range|2000 - 4000 ft [610 - 1220 m]|16-MAY-23
26586|Golden Mile Dolerite|Lithology|A sill of meta-quartz-dolerite, with minor meta-quartz-gabbro; more basic towards the base. In the Golden Mile itself, is represented mainly by an altered form, essentially a quartz-chlorite-carbonate rock, locally termed "quartz dolerite greenstone".|16-MAY-23
26586|Golden Mile Dolerite|Relationships and boundaries|Conformably overlies the Paringa Basalt and is conformably overlain by the Black Flag Beds. The lower contact is usually marked by a thin slate band.|16-MAY-23
26586|Golden Mile Dolerite|Age reasons|Archaean.|16-MAY-23
26586|Golden Mile Dolerite|Geochemistry|See analyses in various GSWA Bulletins for specimens noted in General Description|16-MAY-23
26586|Golden Mile Dolerite|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
26586|Golden Mile Dolerite|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
26586|Golden Mile Dolerite|References|GSWA Bulletin Nos. 6, 42, 51, 67, 69 and 94.  **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
25928|Goldwyer Formation|Name source|Goldwyer No. 1 exploration well, 38 lm east of Cape Villaret, the well in which the formation was first described.|16-MAY-23
25928|Goldwyer Formation|Unit history|None.|16-MAY-23
25928|Goldwyer Formation|Constituents|Not formally subdivided, though an informal threefold subdivision is evident in several of the wells. Where the carbonate is abundant enough to be identified as a distinct zone it forms a middle member. - mainly limestone containing interbeds of shale - which separates and grades into the upper and lower membrs of shale. The relative thickness of each member varies.|16-MAY-23
25928|Goldwyer Formation|Type section locality|Two additional wells are here nominated as reference sections. These are Solanum 1, 19?21'53.95" S, 124?57'46.66" E (283-563 m; Plate 4; Appendix 5) on the Barbwire Terrace, and CRAE mineral exploration drillhole DD87SS7 19?12'56.03" S,  122?19'25.70" E (1546-1780 m; Appendix 5) in the Admiral Bay Fault Zone. Both are fully cored through the Goldwyer Formation, have complete wireline logs, and are archived in the Geological Survey of Western Australia core library in Perth. DD87SS7 is also the stratotype for two members of the Nita Formation (McCracken, 1994).|16-MAY-23
25928|Goldwyer Formation|Type section locality|2782 - 3477 feet (848 - 1060 m) in Thangoo No. 1A (18deg 21' 52" S, 122deg 53' 09" E|16-MAY-23
25928|Goldwyer Formation|Description at type locality|The type section in Thangoo No.1A is incomplete and not representative of the formation in most of the basin. A more typical section is that from Edgar Range No.1, which contains: 177 m Shale, grey to black, fissile, hard, fossiliferous, with thin limestone beds. The interbedded limestone is grey, hard, fine-grained, nodular, and lenticular. 100  m Limestone, grey, argillaceous, fine-grained, hard, with interbeds of black to grey shale that constitutes up to 50% of the lithology. 153 m Shale, grey to black, slightly silty, micaceous, pyritic in part, and calcareous. A few thin limestone stringers are present in the upper part, and the lower part becomes more silty.|16-MAY-23
25928|Goldwyer Formation|Extent|No outcrop. Blackstone No. 1, Matches Springs No.1, Edgar Range No.1, Thangoo Nos. 1, 1A, 2, Goldwyer No. 1, Parda No.1, Willara No.1, Munro No.1, Barbwire No.1, McLarty No.1, Contention Heights No.1, Wilson Cliffs No.1, Kidson No.1. It extends over mos tof the Cannning Basin south of the Fenton Fault aqnd more than half of the area norht of the fault. The known northern limit is the Lennard Shelf, Billiluna Shelf, and Pender Terrace. Its presence on the Margaret Terrace is confirmed by Blackstone No. 1. Although it has not been penetrated in the Fitzroy Graben its presence north and south of the graben strongly supports the assumption that it also occurs there. Its eastern limit is uncertain, but it probably covers most if not all of the Kidson Sub-basin. Its offshore limits are unknown.|16-MAY-23
25928|Goldwyer Formation|Thickness range|Willara No. 1 encountered the thickest section - 736 m. Most other wells in the basin have intersected much thinner sequences, ranging from 134 m in Kidson No.1, to 430 m in Edgar Range No.1.|16-MAY-23
25928|Goldwyer Formation|Lithology|Mainly shale, green to black, fossiliferous, calcareous, pyritic, with interbedded limestone and dolomite, minor lenses of siltstone. the shale is generally uniform across the basin. Slickensides and jointing were recorded in wells from the Kidson and Willara Sub-basins.Traces of anhydrite and phosphatic debris are presnt in Wilson Cliffs No.1, and gypsum in Kidson No. 1. Siltstone, usually a minor constituent, is most abundant near the base of the formation; in the Kidson Sub-basin, and in Thangoo No.2 on Broome Arch, the siltstone grades into sandstone at the base of the formation. The carbonate is usually limestone, grey to white, crystalline, argillaceous, dolomitic in places, commonly dense and tight, forming pods, lenses and beds. In Edgar Range No. 1 these beds are nodular and lenticular. Dolomite partly replaces the limestone in a few wells; it forms thin beds interbedded with limestone or shale as in Barbwire No.1 and Blackstone No.1, and more massive beds as in Thangoo Nos. 1 and 1A. Generally, the sandsotne and limestone beds in the Goldwyer Formation exhibit low porosity and little if any permeability. Porosities average 4%, and permeabilities from 11 to 23 md. A few very thin reservoirs are present in the sandstone beds in Wilson Cliffs No.1. Primary porosities are not evident in the limestone beds. Porosity is evident in vugs in dolomite veins at the base of the dolomite in Thangoo No 1A, where - however - permeability is poor. Several wells had hydrocarbon shows (stain and fluorescence).|16-MAY-23
25928|Goldwyer Formation|Relationships and boundaries|Conformably overlies Willara Formation and is conformably overlain by Nita Formation in most of basin. Basal contact (with Willara Formation) may be disconformable in Thangoo Nos. 1, 1A, 2.Overlain disconformably by Carribuddy Formation in Kidson Sub-basin. Erosian has stripped much of the Palaeozoic sediments from parts of the western end of the Broome Arch, where Goldwyer Formation is unconformably overlain by Permian Grant Formation. North of the Fitzroy Graben the Gap Creek Formation may conformably underlie the Goldwyer Formation but is unconfirmed in this area; no deep drilling there has reache dthe base of the Goldwyer Formation. The Goldwyer Formation is a diachronous unit; its lower part is a time correlative of the upper part of the Willara and Gap Creek Formations, and its upper part is a time correlative of the Nita Foramtion south of the Fenton Fault.|16-MAY-23
25928|Goldwyer Formation|Age reasons|Llanvirnian (middle Ordovician). The abundant fauna includes trilobites, graptolites, brachiopods, nautiloids, ostracods, bivalves, conodonts, chitinozoans and acritarchs. The formation is intensely diachronous across the basin.|16-MAY-23
25928|Goldwyer Formation|Defn author|Elliot, R.M.L. (1961). Appendix 7. New and amended formation names, IN: Thangoo No 1. and No 1A wells, Western Australia compiled by V. Pudovskis and S.P. Willmott, (?of West. Australian Petroleum Pty Ltd).. BMR Petroleum Search Subsidies Act  Publication, 14, 43p|16-MAY-23
25928|Goldwyer Formation|Defn author|Haines, P.W. (2004). GSWA Record 2004/7|16-MAY-23
27160|Gorge Creek Group|Name source|Gorge Creek (Military Grid Reference 2315 3925) which crosses the Great Northern Highway, about 1 km west of Farrell Well, Port Hedland 1:250 000 Sheet area.|16-MAY-23
27160|Gorge Creek Group|Unit history|The term Gorge Creek Group, supersedes "Gorge Creek Formation" of Low (1965, p.8), Kriewaldt and Ryan (1967, Table 2), Noldart and Wyatt (1962, p.105-106), and Ryan 1964 and 1965).|16-MAY-23
27160|Gorge Creek Group|Constituents|The Gorge Creek Group consists of the Lalla Rookh Sandstone (youngest) Budjan Creek Formation, Honeyeater Formation and the Soanesville Subgroup.|16-MAY-23
27160|Gorge Creek Group|Extent|Pilbara region generally|16-MAY-23
27160|Gorge Creek Group|Thickness range|Maximum 5-8 km|16-MAY-23
27160|Gorge Creek Group|Lithology|It consists mainly of sandstone, grit, conglomerate, argillaceous sedimentary rocks, banded iron formations and minor basalt|16-MAY-23
27160|Gorge Creek Group|Relationships and boundaries|Conformably (locally unconformable) overlies the Warrawoona Group.  Unconformably overlain by the Fortescue Group. Intruded by Archaean granitic rocks (Low, pers. comm.).|16-MAY-23
27160|Gorge Creek Group|Age reasons|Archaean because of tectonic style and intruded by Archaean granitic rocks.  Unconformably overlain by Lower Proterozoic Fortescue Group succession.|16-MAY-23
27160|Gorge Creek Group|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
25034|Gumhole Formation|Name source|Gumhole Bore; 125o28'E, 18o07'S, Noonkanbah 1:250 000 Sheet area.|16-MAY-23
25034|Gumhole Formation|Unit history|Equals the Fairfield Beds of Thomas (1957) and is included in Fairfield Formation of Playford & Lowry (1966).|16-MAY-23
25034|Gumhole Formation|Type section locality|(WCB 001 plus WCB 202) 70 metres of limestone, siltstone, and shale exposed along the Great Northern Highway 19 km west-northwest of Fitzroy Crossing.|16-MAY-23
25034|Gumhole Formation|Extent|The unit crops out in a linear pattern for a distance of 280 km on the northerly margin of the Canning Basin from Red Bluffs in the southeast to the Napier Range in the northwest.|16-MAY-23
25034|Gumhole Formation|Thickness range|About 70 metres.|16-MAY-23
25034|Gumhole Formation|Lithology|Limestone, siltstone and shale with minor dolomite and sandstone.  The limestone is commonly light brown, pink to red and light green grey bioclastic, intraclastic and oolitic sandy grainstones.|16-MAY-23
25034|Gumhole Formation|Relationships and boundaries|Overlies "birdseye" limestone of Famennian age, the Luluigui Formation and possible equivalents of the Napier Formation. Base of unit marked by first occurrence of bioclastic limestones.  Conformably overlain by and interfingers with Yellow Drum Sandstone.|16-MAY-23
25034|Gumhole Formation|Age reasons|Faunas are dominated by brachiopods together with pelecypods, corals, bryozoans, nautiloids, fish, conodonts, ostracods, algae and a microflora.  The flora and fauna indicates latest Late Devonian (do V. VI Zones of the German standard).|16-MAY-23
25034|Gumhole Formation|Proposed publication|Bureau of Mineral Resources|16-MAY-23
25034|Gumhole Formation|Defn Reference|B200 - 1979|16-MAY-23
25034|Gumhole Formation|Name first published by|Radke B.M., 1976|16-MAY-23
8463|Hong Kong Chert|Name source|Hong Kong Gold Mine (abandoned); grid reference 21o10'S, 118o20'E, Pyramid 1:250 000 Sheet area.|16-MAY-23
8463|Hong Kong Chert|Unit history|Equated with Marble Bar Chert on Marble Bar 1:250 000 sheet (Hickman & Lipple, in press).|16-MAY-23
8463|Hong Kong Chert|Type section locality|150 metres of bluish-black, brown and white banded chert.|16-MAY-23
8463|Hong Kong Chert|Extent|The unit outcrops as two parallel ridges in the region between Teichmans Gold Mine and Annie Gap and is repeated by folding to the north of Pilbara Mining Centre.|16-MAY-23
8463|Hong Kong Chert|Thickness range|Range 50-150 m|16-MAY-23
8463|Hong Kong Chert|Relationships and boundaries|Overlies Friendly Creek Formation and conformably overlain by Empress Formation.  Second oldest formation of Teichmans Group.|16-MAY-23
8463|Hong Kong Chert|Age reasons|Lower Archaean >3000 m.y.|16-MAY-23
8463|Hong Kong Chert|Defn author|Fitton M.J., Horwitz R.C., Sylvester G., 1975|16-MAY-23
8463|Hong Kong Chert|Proposed publication|CSIRO, Minerals Research Laboratories, Report No. FP 11.|16-MAY-23
8463|Hong Kong Chert|Category|2, 1|16-MAY-23
27801|Horseshoe Formation|Name source|Horseshoe Range, Peak Hill 1:250 000 Sheet.|16-MAY-23
27801|Horseshoe Formation|Unit history|Formerly Horseshoe Beds (MacLeod 1970)|16-MAY-23
27801|Horseshoe Formation|Type section locality|Three km section extending west from Horseshoe Gold Mine across the Horseshoe Range|16-MAY-23
27801|Horseshoe Formation|Extent|Horseshoe Range |16-MAY-23
27801|Horseshoe Formation|Thickness range|1000 m|16-MAY-23
27801|Horseshoe Formation|Lithology|Quartz-mica-feldspar, carbonate-cemented greywacke and shale, and iron formation|16-MAY-23
27801|Horseshoe Formation|Relationships and boundaries|Conformable above, and gradational with Thaduna Greywacke.|16-MAY-23
27801|Horseshoe Formation|Age reasons|Proterozoic, probably 2.0-1.8 b.y.|16-MAY-23
27801|Horseshoe Formation|Proposed publication|Western Australia Geological Survey Annual Report for 1978 (Pub. 1979)|16-MAY-23
27801|Horseshoe Formation|Defn approved by|Western Australia Stratigraphic Nomenclature Subcommission|16-MAY-23
27801|Horseshoe Formation|Name first published by|Gee R.D., 1979|16-MAY-23
74627|Horsewater Soak Calcarenite|Name source|Horsewater Soak, latitude/longitude coordinates 18deg 21' 51" S, 122deg 03' 52" E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
74627|Horsewater Soak Calcarenite|Geomorphic expression|As coastal limestone ridges.|16-MAY-23
74627|Horsewater Soak Calcarenite|Type section locality|Cliff exposure on shores of Willie Creek, near Horsewater Soak, latitude/longitude coordinates 17deg 46' 06" S, 122deg 12' 54" E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
74627|Horsewater Soak Calcarenite|Description at type locality|350 cm large-scale cross-bedded and cross-laminated cream fine-grained quartzose, bioclastic and sparsely oolitic calcarenite; sharp contact with underlying Kennedys Cottage Limestone.|16-MAY-23
74627|Horsewater Soak Calcarenite|Extent|The unit is widespread along the Canning Coast as a semi-continuous to scattered shoe-string to lensoid deposit.|16-MAY-23
74627|Horsewater Soak Calcarenite|Thickness range|Thickness at type locality is 3.5 m.  However, where exposed along the coast the Formation is generally 2 m to 3 m thick, but has been recorded as up to 5.5 m thick. Regionally, the unit will appear as discontinuous shoe-string and lensoid deposits, individually, some tens of metres to several hundred of metres long but only up to 100 m wide and generally 2-3 m thick.|16-MAY-23
74627|Horsewater Soak Calcarenite|Lithology|A fine to medium sand-sized bioclastic and quartzose and locally oolitic calcarenite.  The cementing agent is sparry calcite.  The limestone is laminated, cross-laminated, cross-bedded, to large-scale festoon-bedded.|16-MAY-23
74627|Horsewater Soak Calcarenite|Depositional environment|Mid-Holocene supratidal coastal dune environments.|16-MAY-23
74627|Horsewater Soak Calcarenite|Fossils|Donax faba.|16-MAY-23
74627|Horsewater Soak Calcarenite|Relationships and boundaries|Generally, the Formation rests with sharp contact on the Kennedys Cottage Limestone.  Locally, the Formation rests on Willie Creek Calcarenite.  The Formation is overlain by Shoonta Hill Sand.  Where it is being eroded by aeolian action, the Formation is yielding sand to the Shoonta Hill Sand.  The base of the Formation is located about 1.5 to 2 m above the base of its contemporary lithosome where the base of modern dune deposits are located today.|16-MAY-23
74627|Horsewater Soak Calcarenite|Age reasons|There are no radiocarbon ages derived from this Formation, but ages of 5500 +/- 160 yrs BP, 5590 +/- 240 yrs BP and 6910 +/- 180 yrs BP from underlying calcarenites demonstrate its Holocene age.|16-MAY-23
74627|Horsewater Soak Calcarenite|Correlations|The Formation is probably laterally equivalent to parts of the Barn Hill Formation.|16-MAY-23
74627|Horsewater Soak Calcarenite|Comments|Large scale cross bedded calcarenite.|16-MAY-23
74627|Horsewater Soak Calcarenite|References|Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.|16-MAY-23
30206|Illjarra Sandstone|Name source|Illjarra Bore, at GR CE512362, Ruby Plains 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area, WA.|16-MAY-23
30206|Illjarra Sandstone|Unit history|previously mapped as part of the Mount Parker Sandstone (e.g., Gemuts & Smith, 1968) and Wade Creek Sandstone (Blake et al. 1979), but now known to be Neoproterozoic rather than Mesoproterozoic.|16-MAY-23
30206|Illjarra Sandstone|Geomorphic expression|strike ridges, cuestas and intervening valleys and depressions.|16-MAY-23
30206|Illjarra Sandstone|Type section locality|Ruby Plains 1:100 000 Sheet area - from base at GR CE693456, where the Illjarra Sandstone concordantly overlies Eliot Range Dolomite, to top at GR CE677440, where the Illjarra Sandstone is overlain disconformably by Moonlight Valley Tillite. Lithic sandstone of the Illjarra Sandstone here, about 360 m thick, dips at around 10? southwest, forming a series of cuestas.|16-MAY-23
30206|Illjarra Sandstone|Extent|Ruby Plains and Halls Creek 1:100 000 Sheet areas, Gordon Downs 1:250 000 Sheet area, WA.|16-MAY-23
30206|Illjarra Sandstone|Thickness range|more than 1000 m in south; thinner to north.|16-MAY-23
30206|Illjarra Sandstone|Lithology|ridge-forming lithic (and feldspathic?) sandstone; minor quartz sandstone (locally at base), dolomitic beds (locally near base), and recessive bands of shale, mudstone, siltstone and sandstone in south. Lithic sandstone has abundant to sparse clayey matrix and is well bedded, but rarely cross-bedded.|16-MAY-23
30206|Illjarra Sandstone|Depositional environment|marine shelf?|16-MAY-23
30206|Illjarra Sandstone|Relationships and boundaries|Of Ruby Plains Group. Unconformable on Olympio Formation in south; concordant (conformable?) on Eliot Range Dolomite to north. Overlain disconformably by Duerdin Group (Redbank Yard Formation in south, Moonlight Valley Tillite to north).|16-MAY-23
30206|Illjarra Sandstone|Age reasons|Neoproterozoic - Tonian or Cryogenian. The Ruby Plains Group correlates with Supersequence 1 of the Centralian Superbasin of Walter et al. (1995).|16-MAY-23
30206|Illjarra Sandstone|Correlations|basal quartz sandstone and overlying dolomitic beds locally present in south may be correlatives of Mount Kinahan Sandstone and Eliot Range Dolomite, respectively, exposed to north.|16-MAY-23
30206|Illjarra Sandstone|References|Blake, D.H., Hodgson, I.M. & Muhling, P.C., 1979. Geology of The Granites - Tanami region, Northern Territory and Western Australia. Bureau of Mineral 	Resources, Australia, Bulletin 197.**Blake, D.H., Tyler, I.M. & Sheppard, S., 1997. Geology of the Ruby Plains 1:100 000 Sheet area (4460), Western Australia,. Australian Geological Survey 	Organisation, Canberra. **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. **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. **Walter, M.J., Veevers, J.J., Calver, C.R. & Grey, K., 1995. Late Proterozoic stratigraphy of the Centralian Superbasin, Australia. Precambrian Research, 73, 173-195.|16-MAY-23
9256|Kapai Slate|Name source|From the Kapai Gold Mining Lease 6044E.|16-MAY-23
9256|Kapai Slate|Type section locality|Surface and underground workings on the Kapai Gold Mining Lease (30deg43'40"S, 121deg28'30"E). The Kapai main shaft is 3/4 mile north of Mt Charlotte Reservoir.|16-MAY-23
9256|Kapai Slate|Extent|Marks the lower contact of the Williamstown Dolerite from Williamstown north-north-west for three miles, and also extends from the western limits of the Golden Mile for 5 miles south-south-east.|16-MAY-23
9256|Kapai Slate|General description|Outcrop pattern: a prominent marker bed which has a fine-grained siliceous and ferruginous outcrop. Forms low outcrops, and occasionally prominent low strike ridges. See Specimen No. 12947 of the Geological Survey of Western Australia, Bulletin 69, p44.|16-MAY-23
9256|Kapai Slate|Thickness range|varies from <1 - 50 feet [<0.3 - 15.25 m], averages 10 feet [3.05 m]|16-MAY-23
9256|Kapai Slate|Lithology|Graphitic slate|16-MAY-23
9256|Kapai Slate|Relationships and boundaries|Conformably overlies Devon Consols Basalt and is conformably overlain by the Williamstown Dolerite.|16-MAY-23
9256|Kapai Slate|Age reasons|Archaean.|16-MAY-23
9256|Kapai Slate|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
9256|Kapai Slate|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
9256|Kapai Slate|References|GSWA Bulletin No. 69.  **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
24332|Karalundi Formation|Name source|Karalundi Road House, Glengarry 1:250 000 Sheet.|16-MAY-23
24332|Karalundi Formation|Type section locality|Along E-W fence, 11 km NW of Karalundi.|16-MAY-23
24332|Karalundi Formation|Extent|Karalundi-Ruby Well-Doolgunna area.|16-MAY-23
24332|Karalundi Formation|Thickness range|About 1000 m|16-MAY-23
24332|Karalundi Formation|Lithology|Ferruginous cemented snadstone, shale, chert, basaltic tuff and dolomite.|16-MAY-23
24332|Karalundi Formation|Relationships and boundaries|Conformable between Doolgunna Arkose and Narracoota Volcanics|16-MAY-23
24332|Karalundi Formation|Age reasons|Proterozoic - probably 2.0 - 1.8. b.y.|16-MAY-23
24332|Karalundi Formation|Proposed publication|Western Australia Geological Survey Annual Report for 1978 (Pub. 1979)|16-MAY-23
24332|Karalundi Formation|Defn Reference|80/20704|16-MAY-23
22076|Kazput Formation|Name source|Named after Kazput Pool (Lat. -22.97507 Long. 117.19247) on the ROCKLEA 1:100 000 mapsheet (Thorne and Tyler, 1996).|16-MAY-23
22076|Kazput Formation|Unit history|The revised Kazput Formation, as defined here, is equivalent to the 'unnamed carbonate and shale unit' of Trendall (1979). However, the original definition of Thorne and Tyler (1996) included 'unnamed quartzite unit 2' and part of 'unnamed quartzite unit 3' of Trendall (1979). Following the original definition of Thorne and Tyler (1996), an informal subdivision of lower, middle and upper units has also been used, and the revised definition corresponds to the 'lower Kazput Formation' (Martin et al. 2000; Martin and Morris 2010).|16-MAY-23
22076|Kazput Formation|Constituents|Wonangara Member|16-MAY-23
22076|Kazput Formation|Geomorphic expression|Forms low hills and valleys above the Koolbye Formation and below the prominent hills and cliffs of the overlying Munder Formation.|16-MAY-23
22076|Kazput Formation|Type section locality|There is no complete type section of the Kazput Formation, owing to the presence of faults and unconformities in the type area, but the best exposures are centred around Lat. -22.890 Long. 116.977 in the Hardey Syncline.|16-MAY-23
22076|Kazput Formation|Extent|Currently only confirmed from the Hardey and Turee Creek Synclines.|16-MAY-23
22076|Kazput Formation|Thickness range|The true thickness of the Kazput Formation is difficult to determine, owing to the presence of faults and unconformities in the type area, but it is estimated to be at least 1000 m thick.  Thickness is highly variable, owing to the presence of faults and unconformities, including one internal unconformity. Poor exposure of the Kazput Formation in the Turee Creek Syncline precludes an accurate estimate of its thickness there.|16-MAY-23
22076|Kazput Formation|Lithology|The Kazput Formation consists of interbedded argillite, dolomite, limestone, fine-grained sandstone and minor iron-formation and diamictite. Thorne and Tyler (1996) also document minor basalt, but these outcrops have not been relocated.|16-MAY-23
22076|Kazput Formation|Depositional environment|The Kazput Formation is interpreted to have been deposited on a progradational mixed carbonate-siliciclastic platform, with much of the formation apparently deposited above storm wave-base.|16-MAY-23
22076|Kazput Formation|Fossils|The Kazput Formation is characterised by a number of distinctive stromatolites, including domal, columnar, conical, thrombolitic and Tungussiform forms, as well as large microbial bioherms.|16-MAY-23
22076|Kazput Formation|Diastems or hiatuses|A single very low-angle unconformity is present within the formation at the base of the uppermost informal siliciclastic-dominated interval.|16-MAY-23
22076|Kazput Formation|Relationships and boundaries|The Kazput Formation conformably overlies the Koolbye Formation, although some authors have described this contact as unconformable (e.g. Krapez 1996; Krapez et al. 2017), and is unconformably overlain by the newly defined Munder Formation.|16-MAY-23
22076|Kazput Formation|Identifying features|The dolomites are commonly stromatolitic, and the sandstones dolomitic with hummocky and swaley cross-stratification. Additionally, distinct member-level lithologic intervals can be identified that are dominated by either carbonate or siliciclastic rocks. The lower mixed siliciclastic-carbonate interval is named the Wonangara Member, and contains minor diamictite of possible glacial origin.|16-MAY-23
22076|Kazput Formation|Structure and Metamorphism|Preserved in the cores of two regional synclines formed during the Ophthalmia Orogeny, namely the Hardey and Turee Creek Synclines. The former is also cut by a series of younger faults. Metamorphic grade does not exceed lower greenschist facies.|16-MAY-23
22076|Kazput Formation|Age reasons|The Kazput Formation is older than the c. 2208 Ma Balgara Dolerite sills (Muller et al., 2005) which intrude both the Turee Creek and Shingle Creek Groups (Martin and Morris, 2010), and is younger than the 2312.7 +/- 5.6 Ma diagenetic age of the Meteorite Bore Member in the underlying Kungarra Formation (Philippot et al. 2018).|16-MAY-23
22076|Kazput Formation|Defn author|D. McB. Martin, Geological Survey of Western Australia 7-JUL-2020.|16-MAY-23
22076|Kazput Formation|Proposed publication|GSWA Report 203|16-MAY-23
22076|Kazput Formation|References|Krapez, B 1996, Sequence stratigraphic concepts applied to the identification of basin-filling rhythms in Precambrian successions: Australian Journal of Earth Sciences, v. 43, p. 355-380.  **Krapez, B, Muller, SG, Fletcher, IR and Rasmussen, B 2017, A tale of two basins? Stratigraphy and detrital zircon provenance of the Paleoproterozoic Turee Creek and Horseshoe basin of Western Australia: Precambrian Research, v. 294, p. 67-90.  **Martin, DMcB and Morris, PA 2010, Tectonic setting and regional implications of ca. 2.2 Ga mafic magmatism in the southern Hamersley Province, Western Australia: Australian Journal of Earth Sciences, v. 57, no. 7, p. 911-931.  **Martin, DMcB, Powell, CMcA and George, AD 2000, Stratigraphic architecture and evolution of the early Paleoproterozoic McGrath Trough, Western Australia: Precambrian Research, v. 99, p. 33-64.  **Muller, SG, Krapez, B, Barley, ME and Fletcher, IR 2005, Giant iron-ore deposits of the Hamersley province related to the breakup of Paleoproterozoic Australia: New insights from in situ SHRIMP dating of baddeleyite from mafic intrusions: Geology, v. 33, no. 7, p. 577-580.  **Philippot, P 2018, Avila, JN, Killingsworth, BA, Tessalina, S, Baton, F, Caquineau, T, Muller, E, Pecoits, E, Cartigny, P, Lalonde, SV, Ireland, TR, Thomazo, C, Van Kranendonk, MJ and Busigny, V, 2018, Globally asynchronous sulphur isotope signals require re-definition of the Great Oxidation Event: Nature Communications, v.9, Article number 2245, 10 p.  **Thorne AM and Tyler IM 1996, Geology of the Rocklea 1:100 000 sheet: Western Australia Geological Survey, 1:100 000 Geological Series Explanatory Notes, 15p.  **Trendall, AF 1979, A revision of the Mount Bruce Supergroup, in Annual Report for the year 1978: Geological Survey of Western Australia, Perth, Western Australia, p. 63-71.|16-MAY-23
74628|Kennedys Cottage Limestone|Name source|After Kennedys Cottage, latitude/longitude coordinates 17º 45' 18" S, 122º 12' 16" E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
74628|Kennedys Cottage Limestone|Geomorphic expression|The Formation is exposed along cliff cut by tidal creeks, or along limestone rocky shores.|16-MAY-23
74628|Kennedys Cottage Limestone|Type section locality|Cliff exposure on shores of Willie Creek, near Kennedys Cottage, latitude/longitude coordinates 17º 46' 06" S, 122º 12' 54" E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
74628|Kennedys Cottage Limestone|Description at type locality|75 cm laminated to low angle cross-laminated fine and medium calcarenite, with shell layers; 50 cm lens of conglomerate composed of cobble-sized laminated calcarenite intraclasts; 20 cm laminated to low angle cross-laminated fine and medium calcarenite, with scattered oriented shell and 5 cm thick layer of bubble sand structures; 50 cm laminated to low angle cross-laminated fine and medium calcarenite, with shell layers; sharp contact with the underlying Willie Creek Calcarenite.|16-MAY-23
74628|Kennedys Cottage Limestone|Extent|The unit is widespread along the Canning Coast as a semi-continuous to scattered ribbon deposit.|16-MAY-23
74628|Kennedys Cottage Limestone|Thickness range|Thickness at type locality is1.95 m,  However, where exposed along the coast, the Formation is 1.5-2.0 m thick, but has been recorded as up to 4 m thick. Regionally, the unit will appear as discontinuous ribbon deposit, individually, some tens of metres to several hundred of metres long, but only up to 100 m wide and generally up to 2 m thick.|16-MAY-23
74628|Kennedys Cottage Limestone|Lithology|A fine to medium to coarse sand-sized bioclastic, quartzose and sparsely oolitic calcarenite, with layers of shells, layers of bubble sand structures, and in its upper parts, lenses and wedges of limestone intraclast conglomerate and breccia, with clasts varying from cobble- and pebble-size to boulder-size.  Sand grains are oolitically coated molluscs, quartz, foraminifera, intraclasts, and lithoclasts, and echinoderm fragments. The cementing agent in the main body of the calcarenite is sparry calcite.  Locally, there is in situ beach rock.|16-MAY-23
74628|Kennedys Cottage Limestone|Depositional environment|Mid-Holocene beach environment.|16-MAY-23
74628|Kennedys Cottage Limestone|Fossils|Bivalves Acrosterigma cf. fultoni, Anadara crebricostata, Anadara granosa, Anadara sp., Arca avellana, Asaphis violascens, Barbatia foliata, Callista impar, Donax faba, Donax sp., Dosinia sp., Fragum hemicardium, Gafrarium tumidum, Modiolus micropterus, Saccostrea cucullata, and an unidentified Venerid, and the gastropod Melo amphora.|16-MAY-23
74628|Kennedys Cottage Limestone|Relationships and boundaries|The Formation rests with sharp contact on the laminated, cross-laminated and bioturbated shelly Willie Creek Calcarenite.  The Formation is overlain by aeolianite of the Horsewater Soak Calcarenite.|16-MAY-23
74628|Kennedys Cottage Limestone|Age reasons|Radiocarbon dating of shells within the Formation places it in the Holocene, viz., 5500 ± 160 yrs BP and 5590 +/- 240 yrs BP.|16-MAY-23
74628|Kennedys Cottage Limestone|Correlations|The Formation is laterally equivalent to older part of the Sandfire Calcilutite.|16-MAY-23
74628|Kennedys Cottage Limestone|Comments|Laminated calcarenite and shelly calcarenite with conglomerate beds and bubble sand structures.|16-MAY-23
74628|Kennedys Cottage Limestone|References|Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.|16-MAY-23
35001|Kialrah Rhyolite|Name source|Kialrah Pool on Jones River (Lat. 20deg 59' S., Long. 117deg 23' E). Roebourne 1:250 000 Sheet.|16-MAY-23
35001|Kialrah Rhyolite|Unit history|Name unchanged since first introduced and published (Hickman, 1997). However, the formation has been assigned to different groups: not assigned to a group (Hickman, 1997); assigned to the Bookingarra Group (Pike et al., 2002); assigned to the Croydon Group (Van Kranendonk et al., 2006); re-assigned to the Bookingarra Group (Hickman, 2016).|16-MAY-23
35001|Kialrah Rhyolite|Geomorphic expression|The Kialrah Rhyolite locally outcrops in isolated low hills but is mainly confined to poorly exposed rock pavements within areas of sand plain.|16-MAY-23
35001|Kialrah Rhyolite|Type section locality|The type area is 2 km southwest of Warambie Homestead (Lat. 20° 57¿ S., Long. 117° 22¿ E).|16-MAY-23
35001|Kialrah Rhyolite|Description at type locality|Feldspar-porphyritic flow banded rhyolite dipping steeply to the south and overlying the Louden Volcanics|16-MAY-23
35001|Kialrah Rhyolite|Extent|The Kialrah Rhyolite outcrops over a strike length of 12 km in the Whim Creek greenstone belt. Approximately 10 km northwest of Mount Goldsworthy large units of rhyolite within the Mallina Basin are correlated with the Kialrah Rhyolite. In this interpretation, the east¿west extent of the formation is at least 230 km.|16-MAY-23
35001|Kialrah Rhyolite|General description|The c. 2940 Ma age of the Kialrah Rhyolite coincides with the age of major strike-slip faulting in the Central Pilbara Tectonic Zone (D8, Hickman, 2016), and with the ages of several monzogranite intrusions of the Sisters Supersuite in the Pilbara Craton.|16-MAY-23
35001|Kialrah Rhyolite|Thickness range|1000 m in type area.|16-MAY-23
35001|Kialrah Rhyolite|Lithology|Feldspar-porphyritic flow banded rhyolite. Plagioclase phenocrysts are disseminated through a fine-grained felsic matrix of plagioclase, quartz, and K-feldspar.|16-MAY-23
35001|Kialrah Rhyolite|Depositional environment|Most workers have interpreted that the Bookingarra Group was deposited in a zone of continental rifting and strike-slip faulting near the northwest margin of the Pilbara Craton. The Kialrah Rhyolite was erupted and intruded during the final stages of the deposition of the Bookingarra Group.|16-MAY-23
35001|Kialrah Rhyolite|Relationships and boundaries|Parent is the Bookingarra Group. The Kialrah Rhyolite overlies and locally intrudes the Louden Volcanics. Lithologically identical rhyolite intrudes the Mallina Formation at several localities in the Mallina Basin, and has approximately the same crystallization age as the Kialrah Rhyolite at the type locality in the Whim Creek greenstone belt (see AGE & EVIDENCE). This suggests that the Kialrah Rhyolite includes volcanic and subvolcanic units related to c. 2940 Ma granitic intrusions of the Sisters Supersuite.|16-MAY-23
35001|Kialrah Rhyolite|Identifying features|Feldspar-porphyritic flow banded rhyolite.|16-MAY-23
35001|Kialrah Rhyolite|Structure and Metamorphism|The Kialrah Rhyolite was folded during the North Pilbara Orogeny. Metamorphic grade is extremely low in all areas studied.|16-MAY-23
35001|Kialrah Rhyolite|Age reasons|The Kialrah Rhyolite has been dated by the zircon U-Pb method at three localities: (1) type area, Whim Creek greenstone belt, 2 km southwest of Warambie Homestead, 2943 +/- 7 Ma (GSWA 144261, Nelson, 1998; Van Kranendonk et al., 2006); (2) in the Mallina Basin 10 km northwest of Mount Goldsworthy (Lat. 20deg 21' S., Long. 119deg 31' E ), 2948 +/- 3 Ma (GSWA 169025, Nelson, 2002) or c. 2940 Ma (Hickman, 2016); (3) in the Mallina Basin 3 km north of Mount Satirist (Lat. 21deg 05' S., Long. 118deg 08' E ), 2941 +/- 4 Ma (GSWA 142892, Nelson, 1999).|16-MAY-23
35001|Kialrah Rhyolite|Correlations|The Kialrah Rhyolite of the Whim Creek greenstone belt is correlated with units of flow-banded rhyolite in the Mallina Basin.|16-MAY-23
35001|Kialrah Rhyolite|Alteration and Mineralisation|Propylitic alteration assemblages in the type area. No known mineralization.|16-MAY-23
35001|Kialrah Rhyolite|Geophysical Expression|Moderately high magnetic anomalies.|16-MAY-23
35001|Kialrah Rhyolite|Defn author|A.H. Hickman, Geological Survey of Western Australia, 2016.|16-MAY-23
35001|Kialrah Rhyolite|Proposed publication|Redefined as a formation of the Bookingarra Group in Hickman (2016, Northwest Pilbara Craton: a record of 450 million years in the growth of Archean continental crust: Geological Survey of Western Australia, Report 160, 104p).|16-MAY-23
35001|Kialrah Rhyolite|References|Hickman, AH 1997, A revision of the stratigraphy of Archaean greenstone successions in the Roebourne-Whundo area, west Pilbara: Geological Survey of Western Australia Annual Review 1996-97, p. 76-82. **Hickman, AH 2016, Northwest Pilbara Craton: a record of 450 million years in the growth of Archean continental crust: Geological Survey of Western Australia, Report 160, 104p. ** Nelson, DR 1998, 144261: rhyolite, Bradley Well, Geochronology Record 272: Geological Survey of Western Australia, 4p. **Nelson, DR 1999, 142892: porphyritic rhyolite, Two Mile Well, Geochronology Record 356: Geological Survey of Western Australia, 4p. **Nelson, DR 2002, 169025: rhyolite, Knaptons Well, Geochronology Record 145: Geological Survey of Western Australia, 3p. **Pike, G, Cas, RAF and Smithies, RH 2002, Geological constraints on base metal mineralization of the Whim Creek greenstone belt, Pilbara Craton, Western Australia: Economic Geology, v. 97, p. 827-845. **Van Kranendonk, MJ, Hickman, AH, Smithies, RH, Williams, IR, Bagas, L and Farrell, TR 2006, Revised lithostratigraphy of Archean supracrustal and intrusive rocks in the northern Pilbara Craton, Western Australia: Geological Survey of Western Australia, Record 2006/15, 57p.|16-MAY-23
9793|Koongie Park Formation|Name source|Koongie Park Homestead, at GR CE451713, Halls Creek 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area, WA.|16-MAY-23
9793|Koongie Park Formation|Unit history|Previously mapped as part of the Biscay and Olympio Formations of the Halls Creek Group (e.g., Gemuts & Smith, 1968), but is younger than this group. Hosts several volcanogenic massive sulphide deposits which are currently subeconomic.|16-MAY-23
9793|Koongie Park Formation|Geomorphic expression|low hills and ridges.|16-MAY-23
9793|Koongie Park Formation|Type section locality|across southern limb of an anticline, from GR CE468749 to GR CE469746, Halls Creek 1:100 000 Sheet area. Aphyric rhyolite at base is overlain by about 200 m of mudstone with minor laminated chert, about 50 m of Onedin Member (ironstone, shale, chert), and, at top, sandstone, shale and aphyric rhyolite (Orth 1997).|16-MAY-23
9793|Koongie Park Formation|Extent|Angelo and Dockrell 1:100 000 Sheet areas of Mount Ramsay 1:250 000 Sheet area, Halls Creek 1:100 000 Sheet area of Gordon Downs 1:250 000 Sheet area, McIntosh 1:100 000 Sheet area of Dixon Range 1:250 000 Sheet area, WA.|16-MAY-23
9793|Koongie Park Formation|Thickness range|probably at least 1000 m.|16-MAY-23
9793|Koongie Park Formation|Lithology|rhyolitic and dacitic lavas, pyroclastics and subvolcanic intrusions; basaltic lavas and volcaniclastics; shale, mudstone, turbiditic quartz greywacke, pebbly sandstone, arkose, conglomerate, chert, ironstone and carbonate rocks. Regionally metamorphosed to mainly greenschist facies and contact metamorphosed to higher grades.|16-MAY-23
9793|Koongie Park Formation|Depositional environment|marine?|16-MAY-23
9793|Koongie Park Formation|Relationships and boundaries|base not exposed; overlain concordantly by Moola Bulla Formation in southwest; intruded and contact metamorphosed by plutons of Sally Downs Supersuite of Bow River Batholith (e.g., Loadstone Monzogranite, Shepherds Bore Plutonic Complex, unnamed granite and gabbro bodies) and by Armanda layered mafic intrusion; overlain unconformably by King Leopold Sandstone of Kimberley Group.|16-MAY-23
9793|Koongie Park Formation|Age reasons|Palaeoproterozoic - Orosirian. Isotopically dated (U-Pb zircon) at 1843 +/- Ma (Page et al. 1994).|16-MAY-23
9793|Koongie Park Formation|Correlations|probably part of Tickalara Metamorphics in central zone of Halls Creek Orogen to north.|16-MAY-23
9793|Koongie Park Formation|Comments|Synonomy: Koongie Park Member of Tickalara Metamorphics (Griffin & Tyler 1992).|16-MAY-23
9793|Koongie Park Formation|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. **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 **Griffin, T.J. & Tyler, I.M., 1992. Geology of the southern Halls Creek Orogen - a summary of field work in 1992. Geological Survey of Western Australia, Record 1992/17.  **Griffin, T.J. & Tyler, I.M., 1994. Angelo, Western Australia, 1:100 000 geological map (sheet 4361). Geological Survey of Western Australia, Perth. **Orth, K.,1997. Notes on the geology of the Koongie Park Formation southwest of Halls Creek, Western Australia. Australian Geological Survey Organisation, Record 1997/25. **Page, R.W., Blake, D.H., Sun, S-S., Tyler, I.M., Griffin, T.J. & Thorne, A.M., 1994. New geological and geochronological constraints on volcanogenic massive 	sulphide prospectivity near Halls Creek (WA).  AGSO Research Newsletter, 20, 5-7. **Tyler, I.M. & Griffin, T.J., 1994. Dockrell, Western Australia, 1:100 000 geological map sheet (4360). Geological Survey of Western Australia, Perth.|16-MAY-23
25983|Labouchere Formation|Name source|Mt Labouchere, Robinson Range 1:250 000 Sheet.|16-MAY-23
25983|Labouchere Formation|Unit history|Variation of definition of Barnett (1975) to remove Labouchere Formation from Padbury Group, and to remove coarse conglomerate (now Wilthorpe Conglomerate) from top of Labouchere Formation.|16-MAY-23
25983|Labouchere Formation|Type section locality|Mt Labouchere, Robinson Range 1:250 000 Sheet.|16-MAY-23
25983|Labouchere Formation|Extent|From Horseshoe Range (Peak Hill 1:250 000) to Mt Labouchere|16-MAY-23
25983|Labouchere Formation|Thickness range|Approx. 7 km|16-MAY-23
25983|Labouchere Formation|Lithology|Sandstone, shale|16-MAY-23
25983|Labouchere Formation|Relationships and boundaries|Conformable above Horseshoe Formation, base defined by prominent orthoquartzite bed about 100 metres thick.|16-MAY-23
25983|Labouchere Formation|Defn author|Denis Gee, 1979.|16-MAY-23
25983|Labouchere Formation|Proposed publication|Western Australia Geological Survey Annual Report for 1978 (Pub. 1979)|16-MAY-23
74632|Lagrange Calcilutite Member|Name source|Lagrange Bay, latitude/longitude coordinates 18º 35' 51"S, 121º 48' 16" E, Lagrange 1:250,000 Topographical Sheet.|16-MAY-23
74632|Lagrange Calcilutite Member|Geomorphic expression|(mangrove vegetated) mid-high tidal mud flats.|16-MAY-23
74632|Lagrange Calcilutite Member|Type section locality|Lagrange Bay, latitude/longitude coordinates 18º 35' 51"S, 121º 48' 16" E, Lagrange 1:250,000 Topographical Sheet.|16-MAY-23
74632|Lagrange Calcilutite Member|Description at type locality|30 cm bioturbated cream mud; 50 cm bioturbated and root-structured grey mud to mottled grey/orange mud; 250 cm bioturbated and root-structured grey mud to mottled grey/cream mud with wood fragments, and shell fragments; 30 cm muddy sand resting on grey sand of the Port Smith Sand.|16-MAY-23
74632|Lagrange Calcilutite Member|Extent|The unit is widespread along the Canning Coast, occurring from Beagle Bay to Pardoo Creek. It also has been intersected in numerous cores throughout the coastal region.|16-MAY-23
74632|Lagrange Calcilutite Member|Thickness range|At the type section, 3.6 m; outside the type section, up to 4 m thick.|16-MAY-23
74632|Lagrange Calcilutite Member|Lithology|White/cream/grey bioturbated (locally laminated) and root-structured calcilutite with mangorove wood and mangrove-habitat molluscs; underlies salt flats, samphire flats, and mangrove flats.|16-MAY-23
74632|Lagrange Calcilutite Member|Depositional environment|Under mangrove vegetated and samphire-vegetated mid-high tidal flat environments.|16-MAY-23
74632|Lagrange Calcilutite Member|Fossils|Molluscan shell remains in this member include the bivalves Dosinia sp., Pitar sp, Saccostrea cucullata, Venus lamellaris, and the gastropods Cassidula angulifera, Cerithidea anticipata, Cerithidea cingulata, Ellobium aurisjudae, Nerita undata, Telescopium telescopium, Terebralia palustris and Terebralia sulcata, and remains of Teredinidae ("shipworm"). Plant remains include in situ and fallen trunks and wood fragments of Avicennia marina, Rhizophora stylosa and Ceriops tagal.|16-MAY-23
74632|Lagrange Calcilutite Member|Relationships and boundaries|Grades laterally into Djugun Member of the Sandfire Calcilutite and vertically downwards into Crab Creek Calcilutite Member of the Sandfire Calcilutite.|16-MAY-23
74632|Lagrange Calcilutite Member|Age reasons|Contemporary sedimentation and radiocarbon ages (Semeniuk 2008) place this unit in the Holocene.|16-MAY-23
74632|Lagrange Calcilutite Member|Correlations|The unit is equivalent to the Djugun Member, and laterally equivalent to the Cable Beach Sand and its members, and the Eighty Mile Beach Coquina.|16-MAY-23
74632|Lagrange Calcilutite Member|Comments|In situ mangrove stumps and mangrove-habitat mollusc fauna in bioturbated to structureless mud.|16-MAY-23
74632|Lagrange Calcilutite Member|References|Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.|16-MAY-23
74632|Lagrange Calcilutite Member|Parent|Member of the Sandfire Calcilutite.|16-MAY-23
28108|Lalla Rookh Sandstone|Name source|Lalla Rookh mining centre (Military Grid Reference 204 368), Marble Bar 1:250 000 Sheet area|16-MAY-23
28108|Lalla Rookh Sandstone|Type section locality|In the Lalla Rookh Syncline, southeastwards from near the Lalla Rookh mining centre.|16-MAY-23
28108|Lalla Rookh Sandstone|Extent|The Lalla Rookh Sandstone occurs in the centre of the Lalla Rookh Syncline, the Pilgangoora Syncline and at Shaw Gorge.|16-MAY-23
28108|Lalla Rookh Sandstone|Thickness range|Maximum 2-3 km|16-MAY-23
28108|Lalla Rookh Sandstone|Lithology|Sandstone and conglomerate, usually well bedded and locally showing cross-stratification and ripple marks.|16-MAY-23
28108|Lalla Rookh Sandstone|Relationships and boundaries|The Lalla Rookh Sandstone forms the upper part of the Gorge Creek Group. It conformably overlies the Honeyeater Formation and is unconformably overlain by Lower Proterozoic Fortescue Group rocks. Relationships with adjacent rocks of the Warrawoona Group are often obscured by regional slides, however, some local unconformities have been recognised. Equivalent to the Budjan Creek Formation.|24-JUN-23
28108|Lalla Rookh Sandstone|Age reasons|Archaean|16-MAY-23
28108|Lalla Rookh Sandstone|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan. Note|16-MAY-23
73328|Larranganni Formation|Name source|Named after Larranganni Bluff in Western Australia.|16-MAY-23
73328|Larranganni Formation|Unit history|Larranganni Beds|16-MAY-23
73328|Larranganni Formation|Geomorphic expression|Commonly forms silicified and ferruginized caps on Proterozoic rocks.|16-MAY-23
73328|Larranganni Formation|Type section locality|Type locality- around 4.5km ESE of Larranganni Bluff (128o59'45"E, 19o34'S). Reference locality - around 7km ENE of Supplejack Downs homestead.|16-MAY-23
73328|Larranganni Formation|Description at type locality|South of the Late Palaeoproterozoic Gardiner Sandstone, the Larranganni Formation forms a cap on an outcrop of the Late Palaeoproterozoic Pargee Sandstone.|16-MAY-23
73328|Larranganni Formation|Extent|On the BILLILUNA, BIRRINDUDU and TANAMI 1:250 000 sheet areas.|16-MAY-23
73328|Larranganni Formation|Thickness range|Around 8m thick.|16-MAY-23
73328|Larranganni Formation|Lithology|Sandstone: poorly sorted, medium-bedded, medium- to coarse-grained, locally ripple-marked, locally minor cross-bedded, conglomeratic; commonly silicified resembling silcrete. Minor siltstone. Minor conglomerate: with matrix-supported, rounded to angular pebbles and cobbles of locally derived rocks.|16-MAY-23
73328|Larranganni Formation|Depositional environment|Fluvial.|16-MAY-23
73328|Larranganni Formation|Relationships and boundaries|Unconformable on the Pargee Sandstone and silicified and ferruginized during the Cainozoic (Blake et al, 1975).|16-MAY-23
73328|Larranganni Formation|Age reasons|Mesozoic (Cretaceous) age indirectly inferred by Blake et al (1975) from: they are flat-lying and unconformably overlie Late Palaeoproterozoic rocks, and contain pebbles derived from the Cambrian Antrim Plateau Basalt; the formation is less indurated than lithologically similar Palaeozoic units in the region, and are commonly capped by Cainozoic ferricrete, silicified and ferruginized during the Cainozoic (Blake et al 1975).|16-MAY-23
73328|Larranganni Formation|References|Blake, D.H., Hodgson, I.M., Smith, P.A. 1975.  Geology of the Birrindudu and Tanami 1:250,000 sheet areas, Northern Territory. Bureau of Mineral Resources Report 174.|16-MAY-23
25727|Laurel Formation|Name source|Laurel Downs' research station; Noonkanbah 1:250 000 Sheet area.|16-MAY-23
25727|Laurel Formation|Unit history|Included by Playford & Lowry (1966) in their Fairfield Formation|16-MAY-23
25727|Laurel Formation|Type section locality|Defined by Thomas (1959) who nominated two complementary type sections in the area of Twelve Mile Bore (125o16'E, 17o55'S); thickness about 334 m.|16-MAY-23
25727|Laurel Formation|Extent|The unit is exposed as a 2-10 km belt along the southerly side of the Oscar and Napier Ranges for about 150 km.|16-MAY-23
25727|Laurel Formation|Thickness range|Range 357-800 m|16-MAY-23
25727|Laurel Formation|Lithology|Interbedded limestone, shale, siltstone and sandstone. The limestone is mainly white to yellow brown skeletal grainstones; the shales are grey and calcareous.|16-MAY-23
25727|Laurel Formation|Relationships and boundaries|Overlies the Yellow Drum Sandstone and is conformably overlain by the Anderson Formation in the subsurface and unconformably overlain by Grant Formation near the northerly basin margin.|16-MAY-23
25727|Laurel Formation|Age reasons|Contains a rich and varied biota including algae, brachiopods, bryozoans, conodonts, corals, fish, pelecypods, nautiloids, ammonoids, ostracods and a microflora.  The age is Early Carboniferous (Tournaisian).|16-MAY-23
25727|Laurel Formation|First Reference|98/29007|16-MAY-23
25727|Laurel Formation|Name first published by|BMR 1960 Rep. 41 & 41a|16-MAY-23
39661|Leo Member|Name source|Leo 1, 19deg 14' 50.17"S, 122deg 20' 44.31" E|16-MAY-23
39661|Leo Member|Type section locality|Fully cored CRA Exploration P/L mineral exploration hole DD87SS7, 19deg12' 56.03" S 122deg19' 25.70"  E, from 1482.9m to 1545.5 m. Reference section with limited core, cuttings, and wireline logs in petroleum exploration hole Leo 1 (1565-1642 m).|16-MAY-23
39661|Leo Member|Defn author|McCracken, S. (1994)|16-MAY-23
10365|Lewis Range Sandstone|Name source|Lewis Range, northeast part of Lucas 1:250 000 Sheet area, WA|16-MAY-23
10365|Lewis Range Sandstone|Unit history|Previously mapped as part of the Phillipson Beds (Casey & Wells, 1964)|16-MAY-23
10365|Lewis Range Sandstone|Type section locality|1.5 km southwest of Point Nelligan, Lewis Range, at 20o13'00"S, 128o38'00"E, where a sequence about 20 m thick is exposed up the side of a cuesta. At the base about 3 m of poorly sorted pebbly quartz arenite with grit and conglomerate lenses lies unconformably on Lewis Granite. It is overlain by about 17 m of flaggy, medium-grained, mostly well sorted quartz arenite showing low angle cross bedding.|16-MAY-23
10365|Lewis Range Sandstone|Extent|Northeast part of Lucas and central part of Billiluna 1:250 000 Sheet area, WA|16-MAY-23
10365|Lewis Range Sandstone|Thickness range|Maximum exposed is about 400 m|16-MAY-23
10365|Lewis Range Sandstone|Lithology|Predominantly sandstone-medium bedded, medium to fine-grained quartz arenite, minor sublithic arenite. Conglomerate commonly present at base. Cross-bedding very common, pellety bedding planes uncommon (cf. Murial Range Sandstone).|16-MAY-23
10365|Lewis Range Sandstone|Relationships and boundaries|Unconformably on probably Lower Proterozoic Lewis Granite and unnamed granite, on Archaean or Lower Proterozoic Killi Killi Beds of the Tanami complex, and Gardiner Sandstone of the Carpentarian Birrindudu Group. Inferred to be overlain conformably by Murraba Formation, but the contact between these two units is concealed beneath Quaternary sand.|16-MAY-23
10365|Lewis Range Sandstone|Age reasons|Probably Adelaidean|16-MAY-23
10365|Lewis Range Sandstone|Defn approved by|Taken from xerox copy of approved def. sent by Western Australian Sub-Committee|16-MAY-23
22208|Loadstone Monzogranite|Name source|Loadstone Hill, at GR CE231554, Angelo 1:100 000 Sheet areas, Mount Ramsay 1:250 000 Sheet area.|16-MAY-23
22208|Loadstone Monzogranite|Unit history|previously mapped as Bow River Granite (e.g., Gemuts & Smith 1968).|16-MAY-23
22208|Loadstone Monzogranite|Geomorphic expression|flat-topped low hills with scattered piles of granite boulders; some laterite cappings.|16-MAY-23
22208|Loadstone Monzogranite|Type section locality|GSWA|16-MAY-23
22208|Loadstone Monzogranite|Extent|Angelo and Dockrell 1:100 000 Sheet areas, Mount Ramsay 1:250 000 Sheet area, and Halls Creek 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area, WA.|16-MAY-23
22208|Loadstone Monzogranite|Lithology|homogeneous medium to coarse-grained monzogranite consisting of slightly strained quartz, perthitic microcline, subhedral oligoclase/andesine, subordinate biotite, and minor apatite, allanite, chlorite, epidote, muscovite and zircon; feldspars commonly slightly megacrystic; also syenogranite.|16-MAY-23
22208|Loadstone Monzogranite|Relationships and boundaries|Part of Sally Downs supersuite of Bow River Batholith (Sheppard et al. 1997). Intrudes Koongie Park Formation.|16-MAY-23
22208|Loadstone Monzogranite|Age reasons|Isotopically dated (U-Pb zircon) by R.W. Page at 1827 ? Ma (AGSO?s OZCHRON database).|16-MAY-23
22208|Loadstone Monzogranite|Correlations|some other intrusions of Sally Downs Supersuite (e.g., McHale Granodiorite).|16-MAY-23
22208|Loadstone Monzogranite|Comments|postdates main deformation of Koongie Park Formation|16-MAY-23
22208|Loadstone Monzogranite|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. **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.**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.**Griffin, T.J. & Tyler, I.M., 1994. Angelo, Western Australia, 1:100 000 geological map (sheet 4361). Geological Survey of Western Australia, Perth. **Tyler, I.M. & Griffin, T.J., 1994. Dockrell, Western Australia, 1:100 000 geological map sheet (4360). Geological Survey of Western Australia, Perth.|16-MAY-23
74630|Lombadina Conglomerate Member|Name source|The Lombadina area, northern Dampier Peninsula, 16º 30' S, 123º 45'E, Pender 1:250,000 Topographical Sheet.|16-MAY-23
74630|Lombadina Conglomerate Member|Geomorphic expression|As a high tidal boulder deposits.|16-MAY-23
74630|Lombadina Conglomerate Member|Type section locality|Lombadina region coastal region: 16º 21' 38" S, 123º 01' 47" E, Pender 1:250,000 Topographical Sheet.|16-MAY-23
74630|Lombadina Conglomerate Member|Description at type locality|1 m thick conglomerate deposit of rounded to angular slabs and boulders, cobbles and pebbles of calcarenite (reworked beachrock), with interstitial matrix of shelly beach sand in the lower part.|16-MAY-23
74630|Lombadina Conglomerate Member|Extent|In ribbons and patches in extensive strips discontinuously along the high tidal zone of the Canning Coast from about Cape Frezier to Cape Leveque.|16-MAY-23
74630|Lombadina Conglomerate Member|Thickness range|Thickness at type locality is 1 m.|16-MAY-23
74630|Lombadina Conglomerate Member|Lithology|Deposits of reworked beachrock forming rounded slabs and breccia, pebble to boulder sized; these fragments of beach rock are embedded in laminated sand, bubble sand, and cross-laminated shelly sand and sand, or form a sand-free deposit resting on beachrock pavement; ribbon deposit formed along upper tidal beach face.|16-MAY-23
74630|Lombadina Conglomerate Member|Depositional environment|Upper tidal to storm level of the beach environment; conglomearates deposited during storms.|16-MAY-23
74630|Lombadina Conglomerate Member|Fossils|Molluscs accumulated on the beach that are embedded in the interstitial matrix or in the beachrock intraclasts.|16-MAY-23
74630|Lombadina Conglomerate Member|Relationships and boundaries|The member lies with sharp contact on the Cape Boileau Calcarenite Member, with vertical sharp to gradational contact on the main sands of the Cable Beach Sand, or interfingers with the main sands of the Cable Beach Sand.  The unit is overlain with sharp contact by Shoonta Hill Sand.|16-MAY-23
74630|Lombadina Conglomerate Member|Age reasons|Contemporary nature of the unit, and its stratigraphic relationship with Cable Beach Sand indicates it is a Holocene unit .|16-MAY-23
74630|Lombadina Conglomerate Member|Correlations|The units is laterally equivalent to the main body of Cable Beach Sand and to the Cape Boileau Calcarenite Member.|16-MAY-23
74630|Lombadina Conglomerate Member|Comments|Conglomeratic unit of reworked beachrock.|16-MAY-23
74630|Lombadina Conglomerate Member|References|Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.|16-MAY-23
74630|Lombadina Conglomerate Member|Parent|Member of the Cable Beach Sand.|16-MAY-23
24365|Louden Volcanics|Name source|Louden Creek (Lat. 20deg52'40" S, Long. 117deg50'20" E), 4 km south of Whim Creek mine.|16-MAY-23
24365|Louden Volcanics|Name source|Louden Creek (20o54'S, 117o48'E) Roebourne 1:250 000 Sheet area.|16-MAY-23
24365|Louden Volcanics|Unit history|Included in the Negri Volcanics by (1) but see new definition of Negri Volcanics by Hickman and comments by (2). The two formations are separated on grounds of probable unconformable relations and different lithology.|16-MAY-23
24365|Louden Volcanics|Unit history|First defined as Louden Volcanics (Hickman, 1983), subsequently renamed as Louden Volcanic Member (Van Kranendonk et al., 2006)|16-MAY-23
24365|Louden Volcanics|Geomorphic expression|The Louden Volcanics outcrop in low hills and strike-controlled ridges.|16-MAY-23
24365|Louden Volcanics|Type section locality|6 km south-southwest of Mons Cupri (20o53'S, 117o48'E) around the headwaters of Louden Creek|16-MAY-23
24365|Louden Volcanics|Description at type locality|In the type area, the Louden Volcanics is a southeast dipping succussion of aphyric basalt, komatiitic basalt, and komatiite intruded by sills of peridotite, pyroxenite, and gabbro. The lower and upper contacts of the formation are faulted.|16-MAY-23
24365|Louden Volcanics|Extent|The formation occupies a large part of the Whim Creek greenstone belt which, prior to erosion, extended across a fault-bounded area of 1200 km2 (Hickman, 2016).|16-MAY-23
24365|Louden Volcanics|Extent|150 km2 between Peawah Hill (20o38'S, 117o55') and Mountain Well (20o57'S, 117o40'E). Corresponds to unit labelled "Abu" on Fig 28 of (2).|16-MAY-23
24365|Louden Volcanics|General description|The Louden Volcanics are regionally extensive within the Whim Creek greenstone belt, and have been interpreted to be the product of a mantle plume (Arndt et al., 2001). In this scenario, the Louden Volcanics are likely to have been erupted over a very large area of the northwest Pilbara, and subvolcanic ultramafic-mafic intrusions would have been emplaced over a similar large area. However, no major c. 2945 Ma basaltic formations have been recognized elsewhere in the Pilbara Craton. An alternative origin for the Louden Volcanics, involving volcanism related to subduction, was suggested by Smithies et al. (2007), although juvenile sources are precluded by c. 3400 Ma Nd model ages (Arndt et al., 2001; Smithies et al., 2004).|16-MAY-23
24365|Louden Volcanics|Thickness range|Approximately 1500-3000 m. The thickest development occurs northeast of Mount Negri. Between the Sherlock River and Good Luck Well (20o56'S, 117o41'E) rocks correlated with the formation form a 1600 m succession, the bulk of which is spinifex-textured.|16-MAY-23
24365|Louden Volcanics|Thickness range|Maximum stratigraphic thickness approximately 2000 m (Hickman, 1983) but regionally variable due to syn-depositional normal faulting and local erosion prior to deposition of the Mount Negri Volcanics. The thickness of the Louden Volcanics varies between 2000 and 500 m.|16-MAY-23
24365|Louden Volcanics|Lithology|Ultramafic and mafic volcanic rocks including komatiite, komatiitic basalt, pillowed and massive aphyric tholeiite. Ultramafic and mafic sills interlayered with the volcanic rocks are included in the formation. In the northeast section of the Whim Creek greenstone belt the upper part of the formation contains discontinuous units of arkosic sandstone, polymictic conglomerate, shale, and chert (Smithies, 1998).|16-MAY-23
24365|Louden Volcanics|Lithology|Intermediate, basaltic and ultramafic extrusive and intrusive rocks. Spinifex texture is common and the basaltic units contain high magnesium (MgO, 8.0-12.0 percent). Further description in Refs (2) and (3)|16-MAY-23
24365|Louden Volcanics|Depositional environment|As a formation of the Bookingarra Group, the Louden Volcanics were deposited in a zone of continental rifting and strike-slip faulting near the northwest margin of the Pilbara Craton. Nd model ages from the Louden Volcanics (Arndt et al., 2001; Smithies et al., 2004) average c. 3400 Ma indicating involvement of Paleoarchean crust, or sedimentary material derived from Paleoarchean crust, in magma genesis. Trace element data (normalized to primitive mantle) support this conclusion, with significant enrichments in Th, Zr, and LREE (Smithies et al., 2007).|16-MAY-23
24365|Louden Volcanics|Relationships and boundaries|The Louden Volcanics are folded by the c. 2940 Ma Whim Creek Anticline and form the uppermost stratigraphic unit around the limbs of this fold, overlying the Whim Creek Group, over a southwest-northeast distance exceeding 100 km. The Mount Negri Volcanics are far more restricted in outcrop and are not visibly folded by the Whim Creek Anticline. In contrast to the Louden Volcanics, the Mount Negri Volcanics are relatively flat-lying, and outcrop on upland areas of the Whim Creek greenstone belt. Where the Louden Volcanics and Mount Negri Volcanics are exposed in contact the Louden Volcanics are overlain by the Mount Negri Volcanics. The large-scale structural features combine to suggest an unconformable relationship between the Louden Volcanics and the Mount Negri Volcanics but geochemical evidence indicates a transition between the two formations (Smithies et al., 2007). The Louden Volcanics overlie the Rushall Slate and Cistern Formation conformably to unconformably, and overlie the Whim Creek Group unconformably throughout the Whim Creek greenstone belt. The Louden Volcanics are overlain by the c. 2943 Ma Kialrah Rhyolite, parts of which locally intrude the Louden Volcanics (Smithies et al., 2001). The Louden Volcanics are unconformably overlain by the c. 2775 Ma Mount Roe Basalt of the Fortescue Group.|16-MAY-23
24365|Louden Volcanics|Relationships and boundaries|Unconformably overlain by the Mount Roe Basalt (4) east of Mount Negri.  Differences in attitude of bedding at Mount Negri indicate that the formation unconformably underlies the Negri Volcanics (3). The formation is generally in faulted contact with the Whim Creek Group (1) and the Gorge Creek Group (5) but the succession (correlated) east of the Sherlock River unconformably overlies the Whim Creek Group.|16-MAY-23
24365|Louden Volcanics|Identifying features|Olivine- and pyroxene-spinifex textures are distinguishing features of the komatiitic units of the Louden Volcanics.|16-MAY-23
24365|Louden Volcanics|Structure and Metamorphism|The Louden Volcanics were folded by the c. 2940 Ma Whim Creek Anticline and faulted by the Sholl Shear Zone and Loudens Fault, and by minor normal and strike-slip faults of the Central Pilbara Tectonic Zone (Hickman, 2016). The metamorphic grade of the formation varies from prehnite-pumpellyite to greenschist facies.|16-MAY-23
24365|Louden Volcanics|Age reasons|A maximum eruptive age of c. 2948 Ma is indicated by dating of syndepositional VMS mineralization in the underlying Rushall Slate (Huston et al., 2002). Additionally, the formation is younger than a c. 2955 Ma regional unconformity that separates the Bookingarra Group from the underlying Whim Creek Group (Hickman, 2016). A minimum eruptive age of 2943 +/- 7 Ma is indicated by a zircon U-Pb date on the overlying Kialrah Rhyolite (Nelson, 1998).|16-MAY-23
24365|Louden Volcanics|Correlations|The Louden Volcanics may be related to basaltic units that stratigraphically overlie the c. 2955 Ma regional unconformity in the Mallina Basin (Hickman, 2016). These units are the South Mallina Basalt Member of the Mallina Formation (Croydon Group) and the Salt Well Member of the Lalla Rookh Sandstone (Croydon Group). The Louden Volcanics are also interpreted to be comagmatic with certain ultramafic-mafic layered intrusions of the northwest Pilbara Craton, including the Sherlock and Opaline Well Intrusions, both of which underlie the Louden Volcanics and are likely to be subvolcanic intrusions (Hickman, 2016).|16-MAY-23
24365|Louden Volcanics|Alteration and Mineralisation|Varying degrees of silicification, epidote-chlorite alteration, and carbonation affect the Louden Volcanics.|16-MAY-23
24365|Louden Volcanics|Geophysical Expression|Linear zones of high and low TMI anomalies corresponding to outcrops of ultramafic, mafic, and sedimentary units.|16-MAY-23
24365|Louden Volcanics|Geochemistry|The geochemistry of the formation has been documented by Glikson et al. (1986a, b), Arndt (2001), and Smithies et al. (2007).|16-MAY-23
24365|Louden Volcanics|Defn author|A.H. Hickman, Geological Survey of Western Australia 25-OCT-2017.|16-MAY-23
24365|Louden Volcanics|Proposed publication|Geology of the Pilbara Block and its environs, GSWA Bull.|16-MAY-23
24365|Louden Volcanics|References|Arndt, N, Bruzak, G and Reischmann, T 2001, The oldest continental and oceanic plateaus: geochemistry of basalts and komatiites of the Pilbara Craton Australia, in Mantle Plumes: Their Identification Through Time edited by RE Ernst and KL Buchan: Geological Society of America Special Publication 352, Boulder, Colorado, USA, p.359-387. **Glikson, AY, Davy, R, Hickman, AH 1986a, Geochemical data files of Archaean volcanic rocks, Pilbara Craton, Western Australia: Australia BMR, Record 1986/14, 12p. **Glikson, AY, Pride, C, Jahn, B-M, Davy, R and Hickman AH 1986b, RE and HFS (Ti, Zr, Nb, P, Y) element evolution of Archaean mafic-ultramafic volcanic suites, Pilbara Block, Western Australia: Australia BMR, Record 1986/6, 85p. **Hickman, AH 1983, Geology of the Pilbara Block and its environs: Geological Survey of Western Australia, Bulletin 127, 268p.  **Hickman, AH 2016, Northwest Pilbara Craton: a record of 450 million years in the growth of Archean continental crust: Geological Survey of Western Australia, Report 160, 104p. **Huston, DL, Sun, S -S, Blewett, R, Hickman, A, Van Kranendonk, M, Phillips, D, Baker, D, and Brauhart, C 2002, The timing of mineralisation in the Archaean Pilbara Craton, Western Australia: Economic Geology, v. 97, p. 733-755. **Nelson, DR 1998, 144261: rhyolite, Bradley Well, Geochronology Record 272: Geological Survey of Western Australia, 4p. **Pike, G and Cas, RAF 2002, Stratigraphic evolution of Archaean volcanic rock-dominated rift basins from the Whim Creek Belt, west Pilbara Craton, Western Australia, in Precambrian Sedimentary Environments: A Modern Approach to Depositional Systems edited by W Altermann and P Corcoran: International Association of Sedimentologists, Special Publication 33, Blackwell Science, Oxford, UK, p. 213-234. **Smithies, RH 1998, Geology of the Sherlock 1:100 000 sheet: Geological Survey of Western Australia, 1:100 000 Geological Series Explanatory Notes, 29p. **Smithies, RH, Nelson, DR and Pike, G 2001, Detrital and inherited zircon age distributions - implications for the evolution of the Archaean Mallina Basin, Pilbara Craton, northwestern Australia: Sedimentary Geology, v. 141-142, p. 79-94. **Smithies, RH, Champion, DC and Sun, S-S 2004, Evidence for Early LREE-enriched Mantle Source Regions: Diverse Magmas from the ca. 3.0 Ga Mallina Basin, Pilbara Craton, NW Australia: Journal of Petrology, v. 45, p. 1515-1537. **Smithies, RH, Champion, DC, Van Kranendonk, MJ and Hickman, AH 2007, Geochemistry of volcanic units of the northern Pilbara Craton: Geological Survey of Western Australia, Report 104, 47p. **Van Kranendonk, MJ, Hickman, AH, Smithies, RH, Williams, IR, Bagas, L and Farrell, TR 2006, Revised lithostratigraphy of Archean supracrustal and intrusive rocks in the northern Pilbara Craton, Western Australia: Geological Survey of Western Australia, Record 2006/15, 57p.|16-MAY-23
24365|Louden Volcanics|Proposer|Hickman A.H.|16-MAY-23
10840|Lucas Formation|Name source|Lake Lucas, 20o56'S, 128o50'E, Lucas 1:250 000 Sheet area, WA|16-MAY-23
10840|Lucas Formation|Unit history|Previously named the Lucas Beds. Upgraded to formation status as both top and base of the unit are now defined.|16-MAY-23
10840|Lucas Formation|Type section locality|Cliff section on east side of Lake Dennis, at 205o3'30"S, 128o56'00"E, Lucas Sheet area.  The sequence exposed here, from top to bottom, is 2.5 cm calcrete overlying 3 m calcareous mudstone, 2 m sandstone, 2 m mudstone, 0.25 m sandstone, 2 m mudstone, 1.5 m sandstone and 1 m mudstone. Both the mudstone and sandstone are calcareous and predominantly greyish.|16-MAY-23
10840|Lucas Formation|Extent|Southeast part of Lucas and northeast part of Stansmore 1:250 000 Sheet areas, WA and southwest part of The Granites and northwest part of Highland Rocks 1:250 000 Sheet area, NT|16-MAY-23
10840|Lucas Formation|Thickness range|Calculated to be at least 1000 m, in the Lake Lucas-Lake Dennis area|16-MAY-23
10840|Lucas Formation|Lithology|Calcareous and non-calcareous highly lithic sandstone, siltstone and mudstone: minor limestone and dolomite|16-MAY-23
10840|Lucas Formation|Relationships and boundaries|Unconformable on Precambrian rocks. Overlain by Pedestal Beds, the contact probably being a low angle unconformity.|16-MAY-23
10840|Lucas Formation|Age reasons|Probably Palaeozoic|16-MAY-23
10840|Lucas Formation|Defn approved by|Taken from xerox copy of approved def. sent by Western Australian Sub-Committee|16-MAY-23
10840|Lucas Formation|State(s)|WA|16-MAY-23
29271|Mallina Formation|Name source|Mallina Homestead, grid reference 20o52'S 118o02'E on the Roebourne 1:250 000 Sheet.|16-MAY-23
29271|Mallina Formation|Type section locality|South-west of Mallina Homestead, between Egina and Kangan.|16-MAY-23
29271|Mallina Formation|Extent|Widely distributed between Whim Creek on the Roebourne 1:250 000 Sheet and Kangan on the Pyramid 1:250 000 Sheet.|16-MAY-23
29271|Mallina Formation|Thickness range|Up to 2.5 km|16-MAY-23
29271|Mallina Formation|Lithology|A sequence of argillites and greyhwackes which, in the Mons Cupri area, have intercalted tuffaceous units, some felsic flows and cherts.|16-MAY-23
29271|Mallina Formation|Relationships and boundaries|The unit is conformably underlain by Constantine sandstone or Mons Cupri volcanics.|16-MAY-23
29271|Mallina Formation|Age reasons|Upper Archaean|16-MAY-23
29271|Mallina Formation|Proposed publication|CSIRO, Minerals Research Laboratories, Report No. FP 11|16-MAY-23
29271|Mallina Formation|Name first published by|Fitton, M.J., Horwitz R.C., Sylvester G., 1975|16-MAY-23
37720|Marillana Formation|Name source|Local Aboriginal name for the creek and nearby homestead|16-MAY-23
37720|Marillana Formation|Unit history|Marillana Pisolite, Robe Pisolite|16-MAY-23
37720|Marillana Formation|Constituents|Munjina (base), Barimunya and Eastern (top) Members|16-MAY-23
37720|Marillana Formation|Geomorphic expression|The Formation crops out as low, sinuous mesas, usually alongside the present day creek line. Typically a diagnostic dark brown-purple in colour in natural outcrop.|16-MAY-23
37720|Marillana Formation|Type section locality|The type locality is in BHP Billiton's (BHPB) Eastern 2 (mined-out) final pit wall (AMG 7 17000E/74 83000N), where the Eastern and Barimunya Members are exposed. This will remain intact. A reference core for the Barimunya Member is Western Calibration Hole (AMG 7 06350E/74 85200N) between 0 - 79.1m - it is stored at the BHPB Yandi coreshed. A suitable section of the Munjina Member is in drillhole WD41 (AMG 7 05800E/ 74 84400N) between 74.2 - 100.9m (stored at the same coreshed). Note that other cored intersections of the Munjina Member are available from numerous holes throughout the BHPB lease.|16-MAY-23
37720|Marillana Formation|Extent|Primarily in the Marillana Creek valley, but also in adjoining catchments (Yandicoogina and Weeli Wolli creeks) within the eastern Hamersley Ranges, Pilbara, WA.|16-MAY-23
37720|Marillana Formation|Thickness range|some 90  - 120m in the centre of the 500-650m wide palaeochannel.|16-MAY-23
37720|Marillana Formation|Lithology|Munjina Member - conglomerates and clays. Barimunya Member - channel iron deposit (CID) ore. Eastern Member - clay and CID|16-MAY-23
37720|Marillana Formation|Depositional environment|Fluvial deposits within a palaeovalley environment.|16-MAY-23
37720|Marillana Formation|Relationships and boundaries|Unconformably overlies the Proterozoic Hamersley Group and is disconformably overlain by the Oakover Formation and various alluvium/colluvium materials.|16-MAY-23
37720|Marillana Formation|Age reasons|Data from fossil pollen and spores in the basal Munjina Member indicate a preferred early Oligocene age (McPhail and Stone, in prep)|16-MAY-23
37720|Marillana Formation|Correlations|Similar in age and general nature to the Robe Formation of the lowland/plain Robe River valley at the western end of the Hamersley Ranges, Pilbara, WA. Also correlated to the Poondano Formation of the Pilbara craton.|16-MAY-23
37720|Marillana Formation|Proposed publication|Australian Journal of Earth Sciences|16-MAY-23
37720|Marillana Formation|References|Hall G. C. and Kneeshaw M., 1990. Yandicoogina-Marillana Pisolitic Iron Deposits in Mongraph 14, Geology of the Mineral Deposits of Australia and Papua New Guinea, pp 1581 - 1586 (AusIMM, Melbourne). **Harms, J.E. and Morgan, B.D., 1964. Pisolitic limonite deposits in Northwest Australia : Australasian Institute of Mining and Metallurgy, Proceedings no 212, pp 91-124.  **00/30544 - Hocking, R.M. and Preston, W.A., 1998, Western Australia: Phanerozoic geology and mineral resources. AGSO Journal of Australian Geology and Geophysics, v17 (3), 245-260. **Kneeshaw, M., Kepert, D.A., Tehnas, I.J. and Pudovskis, M.A., 2002. From Mt Goldsworthy to Mining Area C - reflections on forty years of iron ore exploration in the Pilbara. Iron Ore 2002, AusIMM Conference, Perth, September 2002. **MacLeod, W.N., 1966. The geology and iron deposits of the Hamersley Range area, Western Australia, Geol. Surv.West.  Aust. Bull 117. **McPhail, M.K. and Stone, M.S., 2002  in prep. Age and palaeoenvironmental constraints on the formation of the Marillana Formation channel iron deposits, Pilbara region, North-West Australia.  **Morris, R.C., Ramanaidou, E.R. and Horwitz, R.C., 1993. Channel Iron Deposits of the Hamersley Province. AMIRA-CSIRO Iron Ores of the Hamersley Province Project P75G, report 399R. CSIRO Division of Exploration and Mining, Perth 1993. **Stone, M.S., George, A.D., Kneeshaw, M. and Barley, M.E., 2002. New insights into the Tertiary Yandi Channel Iron Deposits, Hamersley Province, Western Australia. Iron Ore 2002, AusIMM Conference, Perth, September 2002.|16-MAY-23
31884|Maude Headley Member|Name source|Maude Headley gold prospect, at GR CF895136, McIntosh 1:100 000 Sheet area, Dixon Range 1:250 000 Sheet area.|16-MAY-23
31884|Maude Headley Member|Unit history|Maude Headley Volcanic Member (e.g., Warren 1997).|16-MAY-23
31884|Maude Headley Member|Geomorphic expression|strike ridges and valleys.|16-MAY-23
31884|Maude Headley Member|Type section locality|Gorge along Panton River, from GR CF945201, Dixon 1:100 000 Sheet area, where member is overlain to east by Olympio Formation turbidites, to GR CF930200, McIntosh 1:100 000 Sheet area, where the member is in fault contact with Olympio Formation turbidite to west; Dixon Range 1:250 000 Sheet area. The characteristic rock types of the member are well exposed along this section: thick to thin bedded and laminated, variably calcareous, fine to coarse-grained volcaniclastic rocks; mafic to felsic alkaline lava flows and fragmental volcanics, massive debris flow deposits containing fragments of amygdaloidal lava, and minor interbanded turbiditic greywacke and siltstone. They show a weak to strong, subvertical north-south cleavage and are metamorphosed to greenschist facies. The thinly bedded rocks show tight to isoclinal minor folds and irregular contortions.|16-MAY-23
31884|Maude Headley Member|Extent|northern part of Halls Creek 1:100 000 Sheet area, Gordon Downs  1:250 000 Sheet area, and southern parts of McIntosh and Dixon 1:100 000 Sheet areas, Dixon Range 1:250 000 Sheet area, WA|16-MAY-23
31884|Maude Headley Member|Thickness range|probably exceeds 1000 m in places.|16-MAY-23
31884|Maude Headley Member|Lithology|variably calcareous, fine to coarse-grained volcaniclastic rocks ranging from thickly bedded to laminated; mafic to felsic alkaline lavas, thin sills and fragmental volcanics; debris flow deposits containing fragments of amygdaloidal lava; minor bands of chert, marble, and turbiditic greywacke and siltstone. Rocks range from weakly to strongly cleaved, and have been metamorphosed to mainly greenschist facies.|16-MAY-23
31884|Maude Headley Member|Depositional environment|marine.|16-MAY-23
31884|Maude Headley Member|Relationships and boundaries|Olympio Formation of Halls Creek Group. Overlain and underlain by turbiditic greywacke, siltstone and mudstone of Olympio Formation.|16-MAY-23
31884|Maude Headley Member|Age reasons|Palaeoproterozoic - Orosirian. Volcanic rocks from member have been isotopically dated (U-Pb zircon) at 1857 ? 2 Ma  and 1857 ? 5 Ma (see Blake et al. 1998).|16-MAY-23
31884|Maude Headley Member|Correlations|none known.|16-MAY-23
31884|Maude Headley Member|Comments|Separated from underlying Biscay Formation by up to 100 m of Olympio Formation turbidites. Thinly bedded rocks commonly show tight to isoclinal minor folds. Apparently mylonitic rocks present in places.|16-MAY-23
31884|Maude Headley 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. **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. **Warren, R.G., 1997. Reconnaissance geological mapping in Dixon, SE McIntosh and 	northernmost Halls Creek 1:100 000 Sheet areas, East Kimberley, W.A. 1992-3. Australian Geological Survey Organisation, Record 1997/26.|16-MAY-23
27276|Meteorite Bore Member|Name source|Meteorite Bore (Lat. -22.9250 Long. 117.0422) on the ROCKLEA 1:100 000 map sheet, about 1.5 km east-southeast of the type section.|16-MAY-23
27276|Meteorite Bore Member|Unit history|The Meteorite Bore Member was first proposed by Trendall (1976; 1981) who specified a type area but no type section. Previously correlated with the newly defined Cave Hill Member at the top of the Boolgeeda Iron Formation and also previously included the newly defined Calgra Member (e.g. Martin, 1999; van Kranendonk et.al., 2015; van Kranendonk and Mazumder, 2015)|16-MAY-23
27276|Meteorite Bore Member|Geomorphic expression|The Meteorite Bore Member is generally not extensively exposed, forming isolated low hills in the Hardey Syncline that have a very distinctive chaotic, non-bedded, airphoto pattern and slightly darker weathering colour than the enclosing Kungarra Formation.|16-MAY-23
27276|Meteorite Bore Member|Type section locality|About 1.5 km west-northwest of Meteorite Bore in the vicinity of Lat. 117.028 Long. -22.921 (Martin, 1999; Van Kranendonk and Mazumder, 2015; Van Kranendonket al., 2015). A thinner reference section is proposed on the northern limb of the Hardey Syncline, starting at Lat. -22.844 Long. 116.871 (Martin, 1999).|16-MAY-23
27276|Meteorite Bore Member|Extent|Outcrop of the Meteorite Bore Member is restricted to the Hardey Syncline, although it may be present under regolith cover in the Turee Creek Syncline. It is unlikely to be present in the Turner, Brockman or Duck Creek Synclines based on thickness estimates and lithofacies correlations.|16-MAY-23
27276|Meteorite Bore Member|Thickness range|Approximately 400 m-thick at the type locality (Martin, 1999; van Kranendonk et.al., 2015; van Kranendonk and Mazumder, 2015), but thins northwards to about 270 m in the vicinity of Lat. -22.845 Long. 116.871 on the northern limb of the Hardey Syncline, which is proposed as a reference section|16-MAY-23
27276|Meteorite Bore Member|Lithology|The Meteorite Bore Member is composed predominantly of glacigenic diamictite, with minor thin interbeds of planar laminated siltstone.|16-MAY-23
27276|Meteorite Bore Member|Depositional environment|Deep marine glacigenic diamictite and minor shale deposited below fair weather wave-base (Martin, 1999). Interpreted by van Kranendonk and Mazumder (2015) and van Kranendonk et al. (2015) to have been deposited in response to glacially-driven low-stand.|16-MAY-23
27276|Meteorite Bore Member|Relationships and boundaries|Conformably underlain and overlain by shales and sandstones of the enclosing Kungarra Formation|16-MAY-23
27276|Meteorite Bore Member|Identifying features|Contains distinctive striated glacial dropstones of Woongarra Rhyolite and other lithologies derived from the underlying Hamersley and Fortescue Groups. These clasts are commonly well-defined by strain shadows within the Ophthalmian cleavage which is pervasive within the Hardey Syncline.|16-MAY-23
27276|Meteorite Bore Member|Structure and Metamorphism|The Meteorite Bore Member has been strongly affected by the Ophthalmian cleavage in outcrop, but this is not as evident in drill core. Glacial dropstones are commonly preserved in strain shadows where this cleavage wraps around competent clasts in outcrop. The metamorphic grade is no higher than lower greenschist facies.|16-MAY-23
27276|Meteorite Bore Member|Age reasons|Maximum depositional age of 2340 +/- 22 Ma (Caquineau et al., 2016; 2018), but older than the c. 2208 Ma Balgara Dolerite (Muller et al., 2005) which locally intrudes it. Re-Os diagenetic age of 2312.7 +/- 5.6 Ma (Philippot et al. 2018).|16-MAY-23
27276|Meteorite Bore Member|Correlations|Previously considered to be a single glacigenic horizon throughout the Hamersley province and correlated with the new Calgra and Cave Hill Members, based solely on lithology (e.g. Martin, 1999; van Kranendonk et.al., 2015; van Kranendonk and Mazumder, 2015). Stratigraphic relationships now indicate at least four discrete glacigenic horizons in the Turee Creek Group.|16-MAY-23
27276|Meteorite Bore Member|Defn author|Originally proposed by Alec Trendall (Geological Survey of Western Australia), revised by David Martin 7-JUL-2012.|16-MAY-23
27276|Meteorite Bore Member|Proposed publication|Published in Trendall (1976; 1981)|16-MAY-23
27276|Meteorite Bore Member|References|Caquineau, T, Paquette, J-L and Philippot, P 2016, In situ U-Pb zircon dating of the Meteorite Bore Member diamictites: constraints on the Paleoproterozoic glaciations and the Great Oxidation Event, in Goldschmidt Conference Abstracts: Goldschmidt Conference, Yokohama, Japan, 26 June 2016-1 July 2016, p. 364.   **Caquineau, T, Paquette, J-L and Philippot, P 2018, U-Pb detrital zircon geochronology of the Turee Creek Group, Hamersley Basin, Western Australia: Timing and correlation of the Paleoproterozoic glaciations: Precambrian Research, v. 307, p. 34-50.   **Martin, DMcB 1999, Depositional setting and implications of Paleoproterozoic glaciomarine sedimentation in the Hamersley Province, Western Australia: Geological Society of America Bulletin, v. 111, p. 189-203.  **Muller, SG, Krapez, B, Barley, ME and Fletcher, IR 2005, Giant iron-ore deposits of the Hamersley province related to the breakup of Paleoproterozoic Australia: New insights from in situ SHRIMP dating of baddeleyite from mafic intrusions: Geology, v. 33, no. 7, p. 577-580.  **Philippot, P 2018, Avila, JN, Killingsworth, BA, Tessalina, S, Baton, F, Caquineau, T, Muller, E, Pecoits, E, Cartigny, P, Lalonde, SV, Ireland, TR, Thomazo, C, Van Kranendonk, MJ and Busigny, V, 2018, Globally asynchronous sulphur isotope signals require re-definition of the Great Oxidation Event: Nature Communications, v.9, Article number 2245, 10 p.  **Trendall, AF 1976, Striated and faceted boulders from the Turee Creek Formation?Evidence for a possible Huronian glaciation on the Australian continent: Geological Survey of Western Australia Annual Report 1975, p. 88-92.   **Trendall, AF 1981, The lower Proterozoic Meteorite Bore Member, Hamersley Basin, Western Australia, in Hambrey, MJ and Harland, WB eds, Earth's pre-Pleistocene glacial record: Cambridge, Cambridge University Press, p. 555-557.   **Van Kranendonk, MJ and Mazumder, R 2015, Two Paleoproterozoic glacio-eustatic cycles in the Turee Creek Group, Western Australia: Geological Society of America Bulletin, v. 127, no. 3?4, p. 596-607.  **Van Kranendonk, MJ, Mazumder, R, Yamaguchi, KE, Yamada, K and Ikehara, M 2015, Sedimentology of the Paleoproterozoic Kungarra Formation, Turee Creek Group, Western Australia: a conformable record of the transition from early to modern Earth: Precambrian Research, v. 256, p. 314-343.|16-MAY-23
30319|Milba Formation|Name source|Milba aboriginal settlement at GR CE679895, Halls Creek 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area, WA|16-MAY-23
30319|Milba Formation|Unit history|previously mapped as Olympio Formation of Halls Creek Group (Gemuts & Smith 1968)|16-MAY-23
30319|Milba Formation|Geomorphic expression|low hills and ridges.|16-MAY-23
30319|Milba Formation|Type section locality|between major NNE-trending faults at GR CF765090 and GR CF784078, in the north of Halls Creek 1:100 000 Sheet area. Here the formation is in fault contact with Koongie Park Formation to west and King Leopold Sandstone to east. From west to east it consists of a prominent ridge-forming band 200 m wide of contorted carbonates, a band 500 m wide of interlayered calcareous and noncalcareous metasediments, and a synform about 1500 m across of mainly metamorphosed greywacke, siltstone, and mudstone.|16-MAY-23
30319|Milba Formation|Extent|Halls Creek Fault Zone in Halls Creek and McIntosh 1:100 000 Sheet areas, in Gordon Downs and Dixon Range 1:250 000 Sheet areas, respectively, WA|16-MAY-23
30319|Milba Formation|Thickness range|more than 1000 m.|16-MAY-23
30319|Milba Formation|Lithology|turbiditic greywacke, siltstone and mudstone; lithic, feldspathic and quartz sandstone; calcareous rocks; chert; and minor mafic lavas and sills. Regionally metamorphosed to mainly greenschist facies; commonly strongly foliated|16-MAY-23
30319|Milba Formation|Depositional environment|presumed to be marine.|16-MAY-23
30319|Milba Formation|Relationships and boundaries|fault-bounded; no stratigraphic relationships seen.|16-MAY-23
30319|Milba Formation|Age reasons|Palaeoproterozoic - Orosirian. Inferred to predate major deformation event at ~1835 Ma (Blake et al. 1998)|16-MAY-23
30319|Milba Formation|Correlations|possibilities include parts of Halls Creek Group, Koongie Park Formation and Tickalara Metamorphics.|16-MAY-23
30319|Milba Formation|Comments|proportions of turbidites, carbonates and volcanics different from those of Koongie Park Formation, Olympio Formation, and Biscay Formation.|16-MAY-23
30319|Milba Formation|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. **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
26030|Millajiddee Member|Name source|Millajiddee Homestead (Lat. 18o49'00"S, long. 124o55'25"E) at the southwestern edge of St George Range.|16-MAY-23
26030|Millajiddee Member|Type section locality|Lat. 18o45'00"S, long 124o55'25"E in the western St George Range.|16-MAY-23
26030|Millajiddee Member|Extent|Crops out in the St George Range, in the Poole Range, in the Lauris Range and other isolated exposures on the Noonkanbah Sheet area. At Mt Thorlan and in the southwestern St George Range the member is cut out by the unconformity at the base of the Poole Sandstone.  It occurs on the Mt Ramsay Sheet area to the east.|16-MAY-23
26030|Millajiddee Member|Thickness range|70 m in the type section and estimated to be over 100 m in the southeastern St George Range.|16-MAY-23
26030|Millajiddee Member|Lithology|Mainly sandstone and minor siltstone and conglomerate. Grain size mainly fine though a medium to coarse-grained middle part is present. Large and small-scale cross-bedding is common and the upper part is slumped in many areas.|16-MAY-23
26030|Millajiddee Member|Relationships and boundaries|Conformably overlies the Wye Worry Member in the St George Range and Poole Range; disconformably in the Lauris Range. Conformably overlain by the Nura Nura Member of the Poole Sandstone though in some places, the contact is an unconformity|16-MAY-23
26030|Millajiddee Member|Age reasons|Fauna consists of trace fossils and indeterminate wood fragments. The underlying Wye Worry Member is dated as Sakmarian (Dickins, 1963), and the overlying Nura Nura Member has been dated as Sakmarian (Glenister and Furnish, 1961) so the Millajiddee Member is also of Sakmarian age.|16-MAY-23
81890|Minga Dolerite|Name source|The unit was named after Minga Well (Lat. -23.943 Long. 115.552), which is located about 8.5 km WSW of Mangaroon Homestead on the Mangaroon 100k mapsheet, Western Australia.|16-MAY-23
81890|Minga Dolerite|Unit history|None.|16-MAY-23
81890|Minga Dolerite|Geomorphic expression|Exposed typically as small, low, rubbly outcrops.|16-MAY-23
81890|Minga Dolerite|Type section locality|Type locality:  The Minga Dolerite dykes occur within the western part of the Capricorn Orogen and intrude Paleoproterozoic metamorphosed sedimentary rocks of the Gascoyne Province. The type locality (Lat. -23.944 Long. 115.532) is on the Mangaroon Station, Upper Gascoyne Shire, Western Australia, Australia. Access to the locality is by an unsealed road approximately 10.5 km WSW of the Mangaroon Station, then about 500 m NNW of the road. The Mangaroon Homestead is just off the Lyndon Minnie Creek road connected with the Ullawarra road; driving ~ 130 km NNE of Gascoyne Junction by the Ullawarra road, which is 174 km east of Carnarvon by the Carnarvon-Mullewa road|16-MAY-23
81890|Minga Dolerite|Extent|In Mangaroon and Eudamullah 100k mapsheet areas, Western Australia.|16-MAY-23
81890|Minga Dolerite|General description|Occur within the westernmost part of the Capricorn Orogen and intrudes Paleoproterozoic metamorphosed sedimentary and igneous rocks of the Gascoyne Province.|16-MAY-23
81890|Minga Dolerite|Thickness range|At type locality: 50m. Range: up to 70 m wide, with the strike length up to 25 km.|16-MAY-23
81890|Minga Dolerite|Lithology|igneous mafic intrusive: dolerite|16-MAY-23
81890|Minga Dolerite|Depositional environment|Genesis: The Minga Dolerite dykes represent mantle-derived magmas, possibly with compositions resembling E-MORB that were more or less continuously contaminated through assimilation of crustal material during emplacement.|16-MAY-23
81890|Minga Dolerite|Relationships and boundaries|The Minga Dolerite dykes intrude the 1820-1775 Ma Moorarie Supersuite (P_-MO-g) of the central Gascoyne Province, comprising mainly granodiorite and monzogranite, and their metamorphosed equivalents, with a conspicuous paucity of coeval mafic rocks (GSWA Explanatory Notes System), and are crosscut by the 755 Ma Mundine Well Dolerite dykes.|16-MAY-23
81890|Minga Dolerite|Identifying features|The Minga Dolerite dykes are typically highly altered and greenish, features that distinguish them from the younger Kulkatharra Dolerite and Mundine Well Dolerite dyke suites. Away from chilled margins, the dykes are typically equigranular, although they can vary from fine grained to very coarse grained.|16-MAY-23
81890|Minga Dolerite|Structure and Metamorphism|Metamorphosed under low- to medium-grade conditions, although primary subophitic to intergranular textures are generally well preserved.|16-MAY-23
81890|Minga Dolerite|Age reasons|No Minga Dolerite dykes have been dated directly. Samples processed by GSWA for SHRIMP U-Pb geochronology failed to yield dateable minerals such as zircon, baddeleyite, and zirconolite, despite Zr concentrations up to 231 ppm in some samples. This may suggest that Zr in these rocks resides in other minerals, such as titanite, amphibole, clinopyroxene, ilmenite, or magnetite. The age of the Minga Dolerite is inferred from relationships with other units: maximum 1670 Ma, minimum 1070 Ma (GSWA Explanatory Notes System).|16-MAY-23
81890|Minga Dolerite|Correlations|The current status of knowledge shows no correlation between the Minga Dolerite and other contemporaneous igneous units in the western Capricorn Orogen. The Minga Dolerite dykes and the Narimbunna Dolerite sills were initially presumed to be petrogenetically related based on cursory geochemical similarities and on similar primary and alteration mineralogy, however more detailed investigation revealed that they are geochemically and petrogenetically distinct.|16-MAY-23
81890|Minga Dolerite|Alteration and Mineralisation|Typically highly altered, secondary minerals include hornblende, greenish-blue amphibole, clinozoisite?epidote, and minor biotite, sericite, and iron hydroxide minerals; pyrite, chalcopyrite and bornite are common accessory minerals.|16-MAY-23
81890|Minga Dolerite|Geophysical Expression|Difficult to identify in aeromagnetic images because the dykes typically parallel the regional structural architecture and magnetic grain.|16-MAY-23
81890|Minga Dolerite|Geochemistry|Tholeiitic composition; enriched in all incompatible trace elements (REE, HFSE, LILE, Th, U), with weakly to moderately fractionated mantle-normalized trace element patterns ((La/Yb)N = 2.7 - 4.0) and small to moderate negative Nb anomalies. Show distinctive Nd isotope compositions, corresponding to depleted mantle model ages (TDM2) between 2.11 and 1.96 Ga.|16-MAY-23
81890|Minga Dolerite|Defn author|Blay, O.A., 20-DEC-2020 (submitted 24-DEC-2021)|16-MAY-23
81890|Minga Dolerite|Comments|A complex mixture of Na-rich calcic amphiboles, including edenite, Fe-edenite, and mineral phases such as ferrotschermakite, aluminoferrotshermakite, and tschermakite series may reflect postmagmatic metasomatism by alkali-rich fluids. Plagioclase is typically clouded by exsolved micron-scale, acicular magnetite, reflecting crystallization at high pressures and temperatures.|16-MAY-23
81890|Minga Dolerite|References|Blay, OA, Johnson, SP, Wingate, MTD, Thorne, AM, Kirkland, CL, Tessalina, SG, Verrall, MR and Cutten, HN 2020, Proterozoic dolerite dykes in the western Capricorn Orogen, Western Australia, Geological Survey of Western Australia Record, 2020/12, 34p.|16-MAY-23
24380|Mininer Turbidite Member|Name source|The name is derived from Mininer Station, north of the Ashburton Range, south region of Paraburdoo.|16-MAY-23
24380|Mininer Turbidite Member|Extent|The Mininer Turbidite is a new member of the Ashburton Formation (de la Hunty, 1965) of the redefined Wyloo Group (Trendall, 1979), south of the Hamersley Ranges of the Turee Creek Geological Sheet area (Daniels, 1968). It is thus a facies which, on the Turee Creek Sheet area, occurs north of the Capricorn Ranges and the Ashburton River and south of the foothills of the Hamersley Ranges.|16-MAY-23
24380|Mininer Turbidite Member|Thickness range|At its thickest, the Member is at least 6000 m.|16-MAY-23
24380|Mininer Turbidite Member|Lithology|It is largely composed of turbidites with a well developed cyclicity. Some very coarse members (pebbles up to 10 cm) and some shale intervals are present as well as rare foreign rafts which all three bridge the facies to the Capricorn Member. It contains rare, thin white flinty, tuffaceous bands (e.g. longitude 117o28.5'; latitude 23o21') which occur rarely in all members of the Ashburton Formation in the Sheet area.|16-MAY-23
24380|Mininer Turbidite Member|Relationships and boundaries|The Mininer Turbidite Member is in a synclinorium and overlies, to the north, the Duck Creek Dolomite with which it interfingers in places. To the south, it overlies and interfingers extensively with the Capricorn Member (redefined).|16-MAY-23
24380|Mininer Turbidite Member|Proposed publication|Aust. CSIRO Inst. Earth Res. Rept No. FP 22|16-MAY-23
24380|Mininer Turbidite Member|Defn approved by|Western Australia Sub-Committee|16-MAY-23
24380|Mininer Turbidite Member|Proposer|Horwitz R.C.|16-MAY-23
22396|Mount Aloysius Complex|Name source|Mount Aloysius, lat. 26.00076oS, long. 128.59631oE, Cooper 1:250 000 Sheet area, WA.|16-MAY-23
22396|Mount Aloysius Complex|Constituents|The following units have been mapped: fns - sillimanite-garnet granulite; crops out only in centre of massif.  fg - felsic garnet granulite; in central region of massif, and as thin bands in north and south.  fna - intermediate and felsic granites, weakly interlayered to massive; in east, and two bands in central region.  fn/m - thin to thick layered felsic granulite with numerous mafic granulite interlayers and rare calc-silicate and quartzite; the most distinctly layered unit, and forms the bulk of the massif.  fn - felsic granulite as a prominent disrupted layer in south, and another in the north.  mn - mafic granulite; mainly in northwest, but also as isolated layers in centre and east.  fnk - leucofelsic granulite as discrete bodies around margins of massif; weakly layered to massive.  No stratigraphic facing is preserved in the granulites, and so stratigraphic order is unknown.|16-MAY-23
22396|Mount Aloysius Complex|Type section locality|The range of hills around and including Mount Aloysius (982 m ASL) is the type area. A reference section from GR 570210 (lat. 26.02922o, long. 128.57023o) to 590225 (lat. 26.01573o, long. 128.59027o) is representative of much of the complex, and exposes (from southwest to northeast) leucofelsic granulite (unit fnk), interlayered felsic and mafic granulites (fn/m) and felsic granulite (fn), felsic garnet granulite (fg), and sillimanite-garnet granulite (fns); a second reference section from GR 628237 (lat. 26.005o, long. 128.62828o) to 610230 (lat. 26.01127o, long. 128.61027o) exposes weakly layered to massive intermediate granulite (fna), and a third reference section from GR 557258 (lat. 25.98583o, long. 1285574o) to 559250 (lat. 25.99306o, long. 128.55937o) exposes mafic granulite (mn).|16-MAY-23
22396|Mount Aloysius Complex|Extent|Revised (enlarged) Extent: Exposed over about 4000 km2 in the Tomkinson ranges of Western Australia and South Australia; extends from Mount Aloysius in the Bell Rock 1:100 000 Sheet (4645) in the west to Teizi Hill in the Davies 1:100 000 Sheet (4745) in the east, and south to Latitude Hill in the Bell Rock 1:100 000 Sheet; also extends into southwest of Bates 1:100 000 Sheet (4646).  Original Extent: Exposed over about 75 km2 in the northwest corner of Bell Rock (4645) and southeast corner of Bates (4646) 1:100 000 Sheet areas; forms a range of hills of which Mount Aloysius is the highest point (982 m ASL).|16-MAY-23
22396|Mount Aloysius Complex|Lithology|Felsic, intermediate, and mafic granulites interlayered on scales ranging from centimetres to hundreds of metres.|16-MAY-23
22396|Mount Aloysius Complex|Relationships and boundaries|No older rocks known. Intruded by small bodies of granite, syenite, granite pegmatite, and by innumerable mafic dykes.|16-MAY-23
22396|Mount Aloysius Complex|Age reasons|A pooled age of 1578 +/- 20 Ma (Gray 1978, Gray & Compston 1978) by Rb-Sr whole-rock isochron method on felsic granulites is interpreted as protolith age because individual isochrons: (1) describe large bodies of rock or entire lithological units; (2) possess a large spread in Rb/Sr ratio; and (3) most are precise. In addition, initial ratios of felsic granulite layers are quite distinct from those of interlayered mafic granulite units. Confirmed by SHRIMP U-Pb zircon date of about 1530 Ma on banded felsic granulite (Sun & Sheraton 1992). Time of granulite metamorphism 1222 +/- 39 Ma (Gray 1978, Gray & Compston 1978) by Rb-Sr whole-rock isochron method, confirmed by SHRIMP U-Pb zircon date of about 1200 Ma (Sun & Sheraton 1992).|16-MAY-23
22396|Mount Aloysius Complex|Proposed publication|AGSO Record: Glikson A.Y. et al (in prep), Geology of the Giles Complex Special 1:100 000 map, western Musgrave Block.|16-MAY-23
12767|Mount Gratwick Granodiorite|Name source|Mount Gratwick, Marble Bar 1:250 000 Sheet area (MGR 1293 2903).|16-MAY-23
12767|Mount Gratwick Granodiorite|Type section locality|The Granodiorite is exposed along the Yandeearra homestead - outcamp road, about 3-5 km northwest of the outcamp (at about MGR 119 302).|16-MAY-23
12767|Mount Gratwick Granodiorite|Extent|The Mount Gratwick Granodiorite occurs in the Yule Batholith and forms an ovoid mass on the western margin of the Marble Bar 1:250 000 Sheet area, northwest of Mount Gratwick. The limits of the pluton on the adjacent Pyramid 1:250 000 Sheet area have not been determined. The mass crops out over an area of about 110 km2 between latitudes 21o35'S and 21o41'S, and longitudes 118o30'E and 118o35'E (see Fig. 1). The mass is poorly exposed and is obscured by superficial Quaternary sand and gravel deposits.|16-MAY-23
12767|Mount Gratwick Granodiorite|Lithology|The Mount Gratwick Granodiorite is a medium, equigranular, allotriomorphic granular textured, poorly foliated granodiorite. In outcrop, the rock is cream-coloured and leucocratic and has an appearance resembling that of anorthosite. The rock contains some coarse pegmatite veins. Although poorly foliated, the rock contains some biotite schlieren and amphibolite xenoliths and there are local cataclastic zones with abundant epidote. The mineralogy consists of calcic oligoclase (An25) and minor quartz, accessory microcline, opaques and apatite, and secondary chlorite, epidote and muscovite. According to mineral proportions, the rock has a composition close to a leuco-diorite. (Type specimen GSWA 28488).|16-MAY-23
12767|Mount Gratwick Granodiorite|Relationships and boundaries|The relationship of the Mount Gratwick Granodiorite to the surrounding Archaean migmatites is uncertain because of poor outcrop. However, regional foliations of the migmatite conform to the margins of the granodiorite and possibly the latter is an associated phase which has undergone more complete assimilation of biotite schlieren and amphibolite and ultramafic xenoliths which are abundant in the enclosing migmatite. The southern part of the Granodiorite is unconformably overlain by Lower Proterozoic Kylena Basalt.|16-MAY-23
12767|Mount Gratwick Granodiorite|Age reasons|Archaean.|16-MAY-23
12767|Mount Gratwick 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
12767|Mount Gratwick Granodiorite|Name first published by|79/20350|16-MAY-23
12864|Mount Keith Granodiorite|Name source|After "Mt Keith" homestead, grid ref. 347615, Sir Samuel 1:250 000 Sheet SG51-13, which overlies the northern extension of the body. (Not named after the topographical feataure Mount Keith 7 km to the north).|16-MAY-23
12864|Mount Keith Granodiorite|Unit history|'Western granite' (D.W. Durney, 1972, J. Geol. Soc. Austr. 19, p251-259); 'Mt Keith granite' (Metals Exploration N.L.).|16-MAY-23
12864|Mount Keith Granodiorite|Type section locality|6 km foothill traverse from grid ref. 348597 to grid ref. 353595, at southern extremity of the outcrop, corresponding to 3 1/2 km across strike.|16-MAY-23
12864|Mount Keith Granodiorite|Extent|Continuous NNW trending outcrop along a prominent escarpment from 2 km north of Jones Creek crossing (352594) to "Mt Keith" homestead. Possible further extension (unexplored) along same escarpment northwestwards from Mail Box Well (346607).|16-MAY-23
12864|Mount Keith Granodiorite|Lithology|Prekinematic granodiorite. Generally medium grained and massive textured though grain size locally variable, not uncommonly with approximately 1 cm sized stubby K-felspar. Contains rare 'basic' xenoliths and various acid dykes. Post-emplacement recrystallization and metamorphic textures visible in thin sections.|16-MAY-23
12864|Mount Keith Granodiorite|Relationships and boundaries|Faces east along its eastern margin where it is unconformably overlain by Jones Creek Conglomerate (D.W. Durney, op. cit.). Base unknown.|16-MAY-23
12864|Mount Keith Granodiorite|Age reasons|Age of emplacement 2689 m.y.+/-17 m.y. (Rb/Sr biotite age); age of post-metamorphic pegmatite 2535 m.y. +/- 18 m.y.  (Rb/Sr whole rock). Analysts J.C. Roddick and W. Compston.|16-MAY-23
12864|Mount Keith Granodiorite|Proposed publication|Journal of Precambrian Research|16-MAY-23
12864|Mount Keith Granodiorite|Name first published by|Roddick J.C., Compston W., Durney D.W., 1976|16-MAY-23
75885|Mount Kenneth Suite|Name source|Mount Kenneth (28.982ºS 118.229ºE)|16-MAY-23
75885|Mount Kenneth Suite|Geomorphic expression|Typically these rocks form ridges and isolated hills 20-50 m above colluviums.|16-MAY-23
75885|Mount Kenneth Suite|Type section locality|Kirkalocka, (29.053°S 118.149°E)|16-MAY-23
75885|Mount Kenneth Suite|Description at type locality|Metatonalite and metagranodiorite intrude amphibolitized metagabbro of the Narndee Igneous Complex. This could be an example of back veining. Many xenoliths of metagabbro are present within the metatonalitic rocks|16-MAY-23
75885|Mount Kenneth Suite|Extent|The suite has currently been documented within the northern and eastern Murchison Domain. More specifically, the suite is always adjacent to Norie Group metavolcanic rocks and Boodanoo and Meeline Suite igneous complexes.|16-MAY-23
75885|Mount Kenneth Suite|General description|5-10 km sized plutons of this suite intrudes into the margins and roof zones of Boodanoo and Meeline Suite igneous complexes.|16-MAY-23
75885|Mount Kenneth Suite|Lithology|Metatonalitic rocks with lesser metagranodiorite and metamonzogranite|16-MAY-23
75885|Mount Kenneth Suite|Depositional environment|Genesis:  These rocks are probably generated by melting of country rocks due to intrusion of large gabbroic bodies.|16-MAY-23
75885|Mount Kenneth Suite|Relationships and boundaries|Intrusive into Meeline and Boodanoo Suite igneous complexes. Intruded by Tuckanarra Suite and Bald Rock Supersuite granitic rocks.|16-MAY-23
75885|Mount Kenneth Suite|Identifying features|Hornblende pheonocrysts are locally abundant and along with a tonalitic affinity, these features differentiate this suite from other granitic suites such as the Tuckanarra Suite and Bald Rock Supersuites|16-MAY-23
75885|Mount Kenneth Suite|Structure and Metamorphism|These rocks are typically weakly metamorphosed and foliated|16-MAY-23
75885|Mount Kenneth Suite|Age reasons| 2815-2800 Ma U/Pb SHRIMP dating (zircons) (Geological Survey of Western Australia samples 185995 & 193967, as yet unpublished)|16-MAY-23
75885|Mount Kenneth Suite|Geophysical Expression|weak mag and gravity lows accompany these plutons|16-MAY-23
75885|Mount Kenneth Suite|Geochemistry| High HFSE composition|16-MAY-23
75885|Mount Kenneth Suite|Defn author| Dr Tim Ivanic, GSWA   23-MAR-2011|16-MAY-23
75885|Mount Kenneth Suite|References|Ivanic, TJ, in prep, Coolamaninu, WA Sheet 2540, Geological Survey of Western Australia, 1: 100 000 Geological Series.|16-MAY-23
30208|Mount Kinahan Sandstone|Name source|Mount Kinahan, at GR DE008928, Antrim 1:100 000 Sheet area, Gordon Downs 1:250 000 sheet. The formation forms Mount Kinahan.|16-MAY-23
30208|Mount Kinahan Sandstone|Unit history|previously assigned to the Mount Parker Sandstone (Gemuts & Smith 1968) of the Mesoproterozoic Osmand Basin of Tyler et al. (1997b).|16-MAY-23
30208|Mount Kinahan Sandstone|Geomorphic expression|prominent cuestas, ridges and plateaus|16-MAY-23
30208|Mount Kinahan Sandstone|Type section locality|south side of gorge along Elvire River, at GR CE908771, Halls Creek 1:100 000 Sheet area. Here the formation consists of quartz sandstone about 100m thick dipping between 20? and 40? to the east, unconformably overlying folded Olympio Formation and overlain concordantly by Eliot Range Dolomite.|16-MAY-23
30208|Mount Kinahan Sandstone|Extent|Ruby Plains, Halls Creek and Antrim 1:100 000 Sheet areas, Gordon Downs 1:250 000 Sheet area, and Dixon 1:100 000 Sheet area, Dixon Range 1:250 000 Sheet area, WA.|16-MAY-23
30208|Mount Kinahan Sandstone|Thickness range|maximum about 150 m.|16-MAY-23
30208|Mount Kinahan Sandstone|Lithology|quartz sandstone: silicified to friable, poorly to well sorted; medium to coarse-grained, with grit on some bedding planes; thin to thick-bedded; commonly cross-bedded; ripple marks present in places; pebbles of vein quartz and quartzite present locally at base.|16-MAY-23
30208|Mount Kinahan Sandstone|Depositional environment|shallow marine shelf.|16-MAY-23
30208|Mount Kinahan Sandstone|Relationships and boundaries|Of Ruby Plains Group.  Unconformably on folded and cleaved metasediments of Olympio Formation (Halls Creek Group) and unnamed granite; overlain conformably or disconformably by Eliot Range Dolomite.|16-MAY-23
30208|Mount Kinahan Sandstone|Age reasons|Neoproterozoic - Tonian or Cryogenian. The Ruby Plains Group is correlated by Grey & Blake (in prep.) with Supersequence 1 of the Centralian basin of Walter et al. (1995).|16-MAY-23
30208|Mount Kinahan Sandstone|Correlations|Lewis Range Sandstone of Birrindudu Basin, Heavitree Quartzite of Amadeus Basin, Vaughan Springs Quartzite of Ngalia Basin, Townsend Quartzite of Officer Basin (Blake et al. 1979; Walter et al. 1995).|16-MAY-23
30208|Mount Kinahan Sandstone|References|Blake, D.H., Hodgson, I.M. & Muhling, P.C., 1979. Geology of The Granites?Tanami region, Northern Territory and Western Australia. Bureau of Mineral Resources, Australia, Bulletin 197. **Blake, D.H., Tyler, I.M. & Sheppard, S., 1997. Geology of the Ruby Plains 1:100 000 Sheet area (4460), Western Australia,. Australian Geological Survey Organisation, Canberra. **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. **Grey, K. & Blake, D.H., in press. **Tyler, I.M., Thorne, A.M., Hoatson, D.M. & Blake, D.H., 1997b.  Turkey Creek, Western Australia, 1:100 000 geological map (sheet 4563). Geological Survey of Western Australia. **Walter, M.J., Veevers, J.J., Calver, C.R. & Grey, K., 1995. Late Proterozoic stratigraphy of the Centralian Superbasin, Australia. Precambrian Research, 73, 173-195.|16-MAY-23
12923|Mount McGrath Formation|Name source|The Mount McGrath Formation is part of the Precambrian Wyloo Group (redefined, Trendall, 1979), south of the Hamersley Ranges (map ref. Geological 1:250 000 Sheets Wyloo, Mount Bruce and Turee Creek).|16-MAY-23
12923|Mount McGrath Formation|Extent|The Formation (de la Hunty, 1965) is here restricted in usage to the essentially clastic rocks that overlie, disconformably the Cheela Springs Basalt and overlap unconformably onto older formations. It is overlain, conformably by the Duck Creek Dolomite which, itself, overlaps onto older units. In the southwest corner of the Mount Bruce Sheet area (de la Hunty, 1965) this redefined Formation was subdivided into the Coolbye Shale Member (which contains basal conglomerates at about long. 117o03') and the overlying Karlathundra Conglomerate. At the foot of Mt McGrath (Horwitz, 1978) the basal clastic units of the Formation contain massive carbonate bands and it abuts at low angle onto Hamersley Group rocks; 100 m are exposed and it is estimated that a top 200 m are covered by alluvium. The name Mount McGrath Formation is here applied to all the predominantly arenaceous rocks that extend from around the Wyloo Dome, south of the Duck Creek to the Angelo River and which are overlain conformably by the Duck Creek Dolomite. The Formation contains defined shale bands and, locally, massive carbonate lenses. Coarse, mature conglomerates are conspicuous and, south of Paraburdoo, where the formation rests on Hamersley Group BIF, Morris (1980) has observed in these conglomerates some pebbles derived from hematite ore.|16-MAY-23
12923|Mount McGrath Formation|Relationships and boundaries|Overlies, disconformably the Cheela Springs Basalt and overlaps unconformably onto older formations. It is overlain, conformably by the Duck Creek Dolomite which, itself, overlaps onto older units.|16-MAY-23
12923|Mount McGrath Formation|Defn author|Horwitz, R.C., March 1980.|16-MAY-23
12923|Mount McGrath Formation|Proposed publication|Aust. CSIRO Inst. Earth Res. Rept No. FP 22|16-MAY-23
12923|Mount McGrath Formation|Resdate|12-FEB-1980|16-MAY-23
12967|Mount Negri Volcanics|Name source|Mount Negri (Lat. 20° 47' 09" S., Long. 117° 50' 46" E).|16-MAY-23
12967|Mount Negri Volcanics|Unit history|First defined as part of the Negri Volcanics (Fitton et al., 1975) which also included stratigraphy later distinguished as the Louden Volcanics by Hickman (1983). Then revised to Mount Negri Volcanics (Hickman, 1990) because the place name Negri had been used for another stratigraphic unit elsewhere in Australia. Included as a formation of the Bookingarra Group by Pike and Cas (2002) and Van Kranendonk et al. (2002). Then renamed as Mount Negri Volcanic Member (Van Kranendonk et al., 2006) when these authors changed the Bookingarra Group to a formation of the Croydon Group. On geochronological and structural evidence this change was reversed by Hickman (2016).|16-MAY-23
12967|Mount Negri Volcanics|Geomorphic expression|The formation outcrops on high plateau and hilly areas of the Whim Creek greenstone belt.|16-MAY-23
12967|Mount Negri Volcanics|Type section locality|Mount Negri (Lat. 20° 47' 09" S., Long. 117° 50' 46" E).|16-MAY-23
12967|Mount Negri Volcanics|Description at type locality|Almost horizontal succession of basaltic lavas on Mount Negri.|16-MAY-23
12967|Mount Negri Volcanics|Extent|Overlying older stratigraphic units in the Whim Creek greenstone belt, the Mount Negri Volcanics are exposed between Mount Negri and Hill Well (Lat. 20°55'48"S., Long. 117°45'27"E). Based on these remnant outcrops, the inferred original depositional extent of the Mount Negri Volcanics was at least 200 km2.|16-MAY-23
12967|Mount Negri Volcanics|General description|The Mount Negri Volcanics are exposed in isolated upland areas of the Whim Creek greenstone belt.|16-MAY-23
12967|Mount Negri Volcanics|Thickness range|The maximum stratigraphic thickness of the formation is approximately 500 m (Hickman, 1983) but in most areas the thickness is between 100 and 200 m.|16-MAY-23
12967|Mount Negri Volcanics|Lithology|The Mount Negri Volcanics are predominantly composed of variolitic and vesicular tholeiitic basalt, although fine-grained pyroxene-spinifex textures are rarely present.|16-MAY-23
12967|Mount Negri Volcanics|Depositional environment|As a formation of the Bookingarra Group, the Mount Negri Volcanics were erupted in a zone of continental rifting and strike-slip faulting near the northwest margin of the Pilbara Craton. Nd model ages from the Mount Negri Volcanics (Arndt et al., 2001; Smithies et al., 2004) average c. 3400 Ma indicating involvement of Paleoarchean crust, or sedimentary material derived from Paleoarchean crust, in magma genesis. Trace element data (normalized to primitive mantle) support this conclusion, with significant enrichments in Th, Zr, and LREE, and fractionated HREE (Smithies et al., 2007).|16-MAY-23
12967|Mount Negri Volcanics|Diastems or hiatuses|None recognized within the formation.|16-MAY-23
12967|Mount Negri Volcanics|Relationships and boundaries|The Mount Negri Volcanics are restricted to several outliers on older formations of the Whim Creek and Bookingarra Groups in the Whim Creek greenstone belt. The formation is relatively flat-lying and, in contrast to all other formations of the Bookingarra Group, was not significantly folded by the Whim Creek Anticline. Where the Louden Volcanics and Mount Negri Volcanics are in close contact the Louden Volcanics are interpreted to be overlain by the Mount Negri Volcanics (Hickman, 1983). The large-scale structural features suggest an unconformable relationship between the Louden Volcanics and the Mount Negri Volcanics but geochemical evidence indicates a transition between the two formations (Smithies et al., 2007). The Mount Negri Volcanics may have been erupted in a late phase of volcanism following deposition of the Louden Volcanics, and which occurred after the main development of the Whim Creek Anticline. Early mapping of the Whim Creek greenstone belt led to the interpretation that the main part of the belt, between Mount Negri and Sherlock River is a graben between the Louden and Kents Bore Faults (Hickman, 1977, Barley, 1987), and the Mount Negri Volcanics were probably erupted from extensional fissures within this structure.|16-MAY-23
12967|Mount Negri Volcanics|Structure and Metamorphism|The Mount Negri Volcanics contain metamorphic foliations that are absent from the adjacent c. 2775 Ma Mount Roe Basalt of the Fortescue Group. The metamorphic grade of the formation is prehnite-pumpellyite facies.|16-MAY-23
12967|Mount Negri Volcanics|Age reasons|A maximum eruptive age of c. 2940 Ma is indicated by the observation that the Mount Negri Volcanics are not significantly deformed by the Whim Creek Anticline. Isotopic evidence indicates a maximum eruptive age of 2948 - 2942 Ma based on the age of syndepositional mineralization in the underlying Rushall Slate and Cistern Formation (Richards and Blockley, 1984; Richards, 1986; Huston et al., 2002). Epigenetic galena mineralization in the Mount Negri Volcanics at Mount Negri was dated at c. 2922 Ma (Thorpe et al., 1992). This may provide a minimum eruptive age providing the galena does not include Pb derived from the Paleoarchean-Mesoarchaen continental crust underlying the formation.|16-MAY-23
12967|Mount Negri Volcanics|Correlations|The interpreted depositional age of the Mount Negri Volcanics (2940-2920 Ma) overlaps with the crystallization age (2930-2924 Ma) of major mafic and ultramafic intrusions (Radley Suite) emplaced in the northwest Pilbara Craton c. 50 km south of Dampier.|16-MAY-23
12967|Mount Negri Volcanics|Alteration and Mineralisation|Varying degrees of silicification, epidote-chlorite alteration, and carbonation affect the Mount Negri Volcanics.|16-MAY-23
12967|Mount Negri Volcanics|Geophysical Expression|Low TMI anomalies corresponding to the basaltic outcrops.|16-MAY-23
12967|Mount Negri Volcanics|Geochemistry|The geochemistry of the formation has been documented by Glikson et al. (1986a, b) and Smithies et al. (2007).|16-MAY-23
12967|Mount Negri Volcanics|Defn author|A.H. Hickman, Geological Survey of Western Australia 25-OCT-2017.|16-MAY-23
12967|Mount Negri Volcanics|References|continued...Van Kranendonk, MJ, Hickman, AH, Smithies, RH, Nelson, DR and Pike, G 2002, Geology and tectonic evolution of the Archean North Pilbara Terrain, Pilbara Craton, Western Australia: Economic Geology, v. 97, p. 695-732. **Van Kranendonk, MJ, Hickman, AH, Smithies, RH, Williams, IR, Bagas, L and Farrell, TR 2006, Revised lithostratigraphy of Archean supracrustal and intrusive rocks in the northern Pilbara Craton, Western Australia: Geological Survey of Western Australia, Record 2006/15, 57p.|16-MAY-23
12967|Mount Negri Volcanics|References|Arndt, N, Bruzak, G and Reischmann, T 2001, The oldest continental and oceanic plateaus: geochemistry of basalts and komatiites of the Pilbara Craton Australia, in Mantle Plumes: Their Identification Through Time edited by RE Ernst and KL Buchan: Geological Society of America Special Publication 352, Boulder, Colorado, USA, p.359-387. **Barley, ME 1987, The Archaean Whim Creek Belt, an ensialic fault-bounded basin in the Pilbara Block, Australia: Precambrian Research, v. 37, p. 199-215. **Fitton, MJ, Horwitz, RC and Sylvester, G 1975, Stratigraphy of the Early Precambrian in the West Pilbara: CSIRO Minerals Research Laboratories, Division of Mineralogy, Report FP 11, 41p. **Glikson, AY, Davy, R, Hickman, AH 1986a, Geochemical data files of Archaean volcanic rocks, Pilbara Craton, Western Australia: Australia BMR, Record 1986/14, 12p. **Glikson, AY, Pride, C, Jahn, B-M, Davy, R and Hickman AH 1986b, RE and HFS (Ti, Zr, Nb, P, Y) element evolution of Archaean mafic-ultramafic volcanic suites, Pilbara Block, Western Australia: Australia BMR, Record 1986/6, 85p. **Hickman, AH 1977, Stratigraphic relations of rocks within the Whim Creek Greenstone Belt: Geological Survey of Western Australia Annual Report 1976, p. 53-56.  **Hickman, AH 1983, Geology of the Pilbara Block and its environs: Geological Survey of Western Australia, Bulletin 127, 268p. **Hickman, AH 1990, Geology of the Pilbara Craton, in Excursion Guidebook No. 5, Pilbara and Hamersley Basin, Third International Archaean Symposium Perth W.A. 1990 edited by SE Ho, JE Glover, JS Myers and JR Muhling: University of Western Australia Geology Department and University Extension, Publication 21, p. 2-13. **Hickman, AH 2016, Northwest Pilbara Craton: a record of 450 million years in the growth of Archean continental crust: Geological Survey of Western Australia, Report 160, 104p. **Huston, DL, Sun, S -S, Blewett, R, Hickman, A, Van Kranendonk, M, Phillips, D, Baker, D, and Brauhart, C 2002, The timing of mineralisation in the Archaean Pilbara Craton, Western Australia: Economic Geology, v. 97, p. 733-755. **Pike, G and Cas, RAF 2002, Stratigraphic evolution of Archaean volcanic rock-dominated rift basins from the Whim Creek Belt, west Pilbara Craton, Western Australia, in Precambrian Sedimentary Environments: A Modern Approach to Depositional Systems edited by W Altermann and P Corcoran: International Association of Sedimentologists, Special Publication 33, Blackwell Science, Oxford, UK, p. 213-234. **Richards, JR and Blockley, JG 1984, The base of the Fortescue Group, Western Australia: Further galena lead isotopic evidence of its age: Australian Journal of Earth Sciences, v. 31, p. 257-268.**Richards, JR, 1986, Lead isotope signatures: Further examination of comparisons between South Africa and Western Australia: Geological Society of South Africa Transactions, v. 89, p. 285-304. **Smithies, RH, Champion, DC and Sun, S-S 2004, Evidence for Early LREE-enriched Mantle Source Regions: Diverse Magmas from the ca. 3.0 Ga Mallina Basin, Pilbara Craton, NW Australia: Journal of Petrology, v. 45, p. 1515-1537. **Smithies, RH, Champion, DC, Van Kranendonk, MJ and Hickman, AH 2007, Geochemistry of volcanic units of the northern Pilbara Craton: Geological Survey of Western Australia, Report 104, 47p. **Thorpe, RI, Hickman, AH, Davis, DW, Mortensen, JK and Trendall, AF 1992, Constraints to models for Archaean lead evolution from precise U-Pb geochronology from the Marble Bar region, Pilbara Craton, Western Australia, in The Archaean: Terrains, processes and metallogeny, edited by JE Glover and SE Ho: University of Western Australia, Geology Department and University Extension, Publication no. 22, p. 395-408.|16-MAY-23
78890|Mu Formation|Name source|Mu Hills (latitude 23degrees 53' S, longitude 128degrees 49' E)|16-MAY-23
78890|Mu Formation|Unit history|Most outcrops of Mu Formation were previously mapped as Ligertwood beds by Wells et al. (1964) and Wells (1968). However, these outcrops are now inferred to be distinct from, and significantly older than the unit exposed at the Ligertwood beds type locality in the NT (Ligertwood beds at type area is inferred to be upper Paleozoic, post-dating the Alice Springs Orogeny: Edgoose, 2013). Some outcrops previously mapped as Ligertwood beds in WA are now assigned to Bitter Springs Formation diapiric carbonate breccia and Sir Frederick Conglomerate.|16-MAY-23
78890|Mu Formation|Geomorphic expression|Low hills and rubbly rises.|16-MAY-23
78890|Mu Formation|Type section locality|Northern edge of the Mu Hills in the vicinity of the Sandy Blight Junction Track. Outcrop is generally poor and discontinuous, so no single type section can be nominated. The conglomeratic facies is best exposed around lat 23degrees52'16"S, long 128degrees52'2"E, where it unconformable overlies poorly exposed and silicified Bitter Springs Formation to the south. This location is also the basal stratotype. The sandstone facies is best exposed in a small cluster of hills around lat 23degrees51'1"S, long 128degrees53'11"E. Access to the type area is via the Sandy Blight Junction Track.|16-MAY-23
78890|Mu Formation|Extent|Most confirmed outcrops are distributed along the northern edge of the Mu Hills. Isolated outcrops of conglomerate up to 20 km northeast of the type area may belong to the Mu Formation. Outcrops previously mapped as Ligertwood beds near the western edge of the Mount Rennie 1:250 000 map sheet area in the NT are probably Mu Formation (but the Ligertwood beds type area is excluded). Outcrops of cobble and boulder conglomerate near lat 24degrees27'S, long 128degrees23'E south of Wallace Hills are inferred to overlie the Maurice Formation and are tentatively included in the Mu Formation.|16-MAY-23
78890|Mu Formation|General description|The conglomeratic facies, as described for the type area is the most regionally widespread expression. The sandstone facies is only well developed around the type area.|16-MAY-23
78890|Mu Formation|Thickness range|The thickest exposure of at least 600 m is inferred in the type area. Significant thickness variations are expected due to the tectonic setting, but cannot be quantified due to poor and discontinuous outcrop.|16-MAY-23
78890|Mu Formation|Thickness range|At least 600 m estimated in the type area; top not exposed.|16-MAY-23
78890|Mu Formation|Lithology|Cobble and boulder conglomerate is the dominant lithofacies. Sandstone with interbeds of conglomeratic sandstone is locally present, and siltstone is a minor component. Conglomerate clasts are well rounded and are mostly sedimentary and metasedimentary including quartzite, silicified sandstone, metasandstone, with minor chert and vein quartz. Many of the conglomerate clasts may be reworked from the locally underlying Sir Frederick Conglomerate. The sandy matrix is often ferruginous and is typically very friable, with many exposures dominated by loose rounded cobbles and boulders at surface. The sandstone is typically red-brown, medium grained and lithic. Beds are typically massive, with current lineations common on bedding surfaces.|16-MAY-23
78890|Mu Formation|Depositional environment|Alluvial fan and fluvial environments based on sedimentary facies. Deposition in the Mu Hills area was controlled by local uplift and subsidence likely related to diapiric movement of Bitter Springs Formation salt, probably during a late phase of the Petermann Orogeny. The Mu Formation appears to fill local mini-basins related to salt withdrawal. The formation was tilted by continuing salt movements during deposition. The sediment was ultimately derived from uplift of the Petermann Orogen, but was at least in part recycled from earlier syn-Petermann deposits.|16-MAY-23
78890|Mu Formation|Fossils|None observed.|16-MAY-23
78890|Mu Formation|Diastems or hiatuses|None observed, but this may be a function of poor outcrop. Local hiatuses are possible, based on tectonic setting.|16-MAY-23
78890|Mu Formation|Relationships and boundaries|Unconformably overlies Maurice Formation, Sir Frederick Conglomerate, Carnegie Formation and Bitter Springs Formation. No top contact exposed.|16-MAY-23
78890|Mu Formation|Identifying features|In isolation the conglomeratic facies is difficult to distinguish from the older Sir Frederick Conglomerate (although the Mu Formation conglomerate matrix is often more ferruginous), while the sandstone facies resembles sandstone units in the Maurice Formation and Sir Frederick Conglomerate. It is only possible to confidently distinguish the Mu Formation where the pronounced basal angular unconformity over the older units can be recognised.|16-MAY-23
78890|Mu Formation|Structure and Metamorphism|Outcrops at and near the type locality mostly dip north at around 20 degrees, or steeper close to the basal unconformity. No metamorphism.|16-MAY-23
78890|Mu Formation|Age reasons|Younger than the Maurice Formation, which is probably lower Cambrian (Haines et al., 2012). Probably deformed prior to the middle Ordovician because nearly flat-lying middle Ordovician limestone is exposed nearby (Haines et al., 2012). Detrital zircon geochronology (Wingate et al., 2014a,b) is consistent with sediment derivation from the Petermann Orogen during or after the late Ediacaran to early Cambrian Petermann Orogeny. Probably lower Cambrian but could be somewhat younger.|16-MAY-23
78890|Mu Formation|Correlations|Correlative of lower Pertaoorrta Group in NT.|16-MAY-23
78890|Mu Formation|Alteration and Mineralisation|None observed.|16-MAY-23
78890|Mu Formation|Geophysical Expression|Not distinguished on geophysical datasets.|16-MAY-23
78890|Mu Formation|Geochemistry|No data.|16-MAY-23
78890|Mu Formation|Defn author|Peter Haines and Heidi Allen (Geological Survey of Western Australia) 18-MAR-2015|16-MAY-23
78890|Mu Formation|References|Edgoose, CJ 2013, Chapter 23: Amadeus Basin, in Ahmad, M and Munson, TJ (compilers), Geology and mineral resources of the Northern Territory: Northern Territory Geological Survey, Special Publication 5, p. 23.1-23.70. **Haines, PW, Allen, HJ, Grey, K and Edgoose, C 2012, The western Amadeus Basin: revised stratigraphy and correlations, in Central Australian Basin Symposium III, edited by GJ Ambrose and J Scott: Petroleum Exploration Society of Australia, Special Publication, CD-ROM, 6p. **Wells, AT, Forman, DJ and Ranford, LC 1964, Geological reconnaissance of the Rawlinson and MacDonald 1:250 000 sheet areas: Australia BMR, Report 65, 35p. **Wells, AT 1968, Macdonald, W.A.: Australia BMR, 1:250 000 Geological Series Explanatory Notes, 10p. **Wingate, MTD, Kirkland, CL and Haines, PW 2014a, 199419: silty sandstone, Mu Hills; Geochronology Record 1192: Geological Survey of Western Australia, 5p. **Wingate, MTD, Kirkland, CL and Haines, PW 2014b, 199420: sandstone, Mu Hills; Geochronology Record 1193: Geological Survey of Western Australia, 5p.|16-MAY-23
27510|Mulgine Granite|Name source|Mulgine Hill, BA 8, Perenjori 1:250 000 Sheet area, Lat. 29o11'S, Long. 116o59'E. In some reports known at Mt Mulgine.|16-MAY-23
27510|Mulgine Granite|Type section locality|The type locality for the Granite is in the vicinity of Mulgine Hill, where exposure is fair.|16-MAY-23
27510|Mulgine Granite|Extent|The Mulgine Granite is a roughly circular complex pluton approximately 2 km in diameter in the vicinity of the trig station.|16-MAY-23
27510|Mulgine Granite|Lithology|The Mulgine Granite is a complex pluton consisting of separate lithofacies of medium-fine even grained granite with foliated and porphyritic variants. The medium even grained granite is a leuco-granite composed of quartz, microcline, sericitized plagioclase and muscovite with lesser amounts of fluorite and pyrite. It contains numerous quartz veins with scheelite and molybdenite mineralisation. The granite encloses old molybdenite mines which produced a small amount of ore in 1915.|16-MAY-23
27510|Mulgine Granite|Age reasons|Archaean|16-MAY-23
27510|Mulgine Granite|Proposed publication|West. Australia Geol. Survey Min. Res. Bull.|16-MAY-23
27510|Mulgine Granite|Status|1|16-MAY-23
81973|Munder Formation|Name source|Named after Munder Spring (Lat. -22.97146 Long. 117.18025), about 30 km southwest of the proposed type locality, on the ROCKLEA 1:100 000 mapsheet.|16-MAY-23
81973|Munder Formation|Unit history|Locally equivalent to the lower part of Trendall's (1979) 'unnamed quartzite unit 3', all of 'quartzite 2' of Krapez et al. (2017) and the siliciclastic 'middle Kazput Formation' of Martin et al. (2000) and Martin and Morris (2010).|16-MAY-23
81973|Munder Formation|Geomorphic expression|The Munder Formation is more resistant to weathering than the underlying Kazput and overlying Anthiby Formations, and forms moderate hills.|16-MAY-23
81973|Munder Formation|Type section locality|6 km south of the mouth of Kungarra Gorge (Lat. -22.81230 Long. 116.93386) on ROCKLEA 1:100 000 sheet. An incomplete section has been measured at Lat. -22.8652 Long. 116.9107, but this does not reflect the full thickness of the formation.|16-MAY-23
81973|Munder Formation|Extent|The Munder Formation is confined to the core of the Hardey Syncline.|16-MAY-23
81973|Munder Formation|Thickness range|The thickness of the Munder Formation is highly variable due to truncation beneath the unconformity at the base of the overlying, newly defined, Anthiby Formation. The formation is at least 125 m thick at the type locality, and thickens to the east. The maximum thickness is estimated to be about 300m in the vicinity of Lat. -22.853 Long 116.932.|16-MAY-23
81973|Munder Formation|Lithology|The Munder Formation consists predominantly of medium to very coarse-grained, trough cross-stratified ferruginous sandstone and minor conglomerate that forms a broadly upward-coarsening succession in the type area.|16-MAY-23
81973|Munder Formation|Depositional environment|The Munder Formation is interpreted as a progradational fluvial deposit that formed during the filled stage of the Turee Creek Basin (formerly McGrath Trough, Martin et al., 2000; Martin and Morris, 2010).|16-MAY-23
81973|Munder Formation|Relationships and boundaries|The Munder Formation unconformably overlies the redefined Kazput Formation, and is in turn unconformably overlain by the newly defined Anthiby Formation.|16-MAY-23
81973|Munder Formation|Identifying features|Sandstones and conglomerates of the Munder Formation are characterised by the abundance of jaspilitic fragments, interpreted to have been derived from the upper parts of the underlying Hamersley Group, especially the Weeli Wolli Formation.|16-MAY-23
81973|Munder Formation|Structure and Metamorphism|The Munder Formation is preserved in the core of the Hardey Syncline, but is not significantly affected by the Ophthalmian cleavage due to its high competency. Metamorphic grade is lower greenschist facies.|16-MAY-23
81973|Munder Formation|Age reasons|The Munder Formation is younger than the 2.34 Ga maximum depositional age of the Meteorite Bore Member (Caquineau et al., 2016), and older than the 2208 Ma Balgara Dolerite (Muller et al., 2005) that intrudes the overlying Beasley River Quartzite.|16-MAY-23
81973|Munder Formation|Defn author|D. McB. Martin, Geological Survey of Western Australia 7-JUL-2020.|16-MAY-23
81973|Munder Formation|Proposed publication|GSWA Report 203|16-MAY-23
81973|Munder Formation|Comments|The Beasley River Quartzite has been mapped as 'unnamed quartzite unit 3', a partial equivalent of the Munder Formation, in the Turee Creek Syncline by Krapez et al. (2017), but this correlation is disputed based on regional stratigraphic relationships (Martin and Morris, 2010).|16-MAY-23
81973|Munder Formation|References|Caquineau, T, Paquette, J-L and Philippot, P 2016, In situ U-Pb zircon dating of the Meteorite Bore Member diamictites: constraints on the Paleoproterozoic glaciations and the Great Oxidation Event, in Goldschmidt Conference Abstracts: Goldschmidt Conference, Yokohama, Japan, 26 June 2016-1 July 2016, p. 364.    **Krapez, B, Muller, SG, Fletcher, IR and Rasmussen, B 2017, A tale of two basins?  Stratigraphy and detrital zircon provenance of the Paleoproterozoic Turee Creek and Horseshoe Basins of Western Australia: Precambrian Research, v. 294, p. 67-90.  **Martin, DMcB and Morris, PA 2010, Tectonic setting and regional implications of ca. 2.2 Ga mafic magmatism in the southern Hamersley Province, Western Australia: Australian Journal of Earth Sciences, v. 57, no. 7, p. 911-931.  **Martin, DMcB, Powell, CMcA and George, AD 2000, Stratigraphic architecture and evolution of the early Paleoproterozoic McGrath Trough, Western Australia: Precambrian Research, v. 99, p. 33-64.  **Muller, SG, Krapez, B, Barley, ME and Fletcher, IR 2005, Giant iron-ore deposits of the Hamersley province related to the breakup of Paleoproterozoic Australia: New insights from in situ SHRIMP dating of baddeleyite from mafic intrusions: Geology, v. 33, no. 7, p. 577-580.  **Trendall, AF 1979, A revision of the Mount Bruce Supergroup, in Annual Report for the year 1978: Geological Survey of Western Australia, Perth, Western Australia, p. 63-71.|16-MAY-23
13494|Munyu Sandstone|Name source|Munyu Hills, 21o47'S, 129o08'E, Highland Rocks 1:250 000 Sheet NT.|16-MAY-23
13494|Munyu Sandstone|Unit history|Outcrops in Stansmore 1:250 000 Sheet area were previously mapped as Gardiner Beds (Wells, 1962).|16-MAY-23
13494|Munyu Sandstone|Type section locality|Across strike ridge in southeast Stansmore 1:250 000 Sheet area, at 21o55'S, 128o55'E, where some 400 m of medium bedded, poorly sorted, medium to very coarse-grained and gritty quartz arenite dip 45o north.|16-MAY-23
13494|Munyu Sandstone|Extent|West part of Highland Rocks and southeast part of Stansmore 1:250 000 Sheet areas, NT and WA respectively.|16-MAY-23
13494|Munyu Sandstone|Thickness range|Maximum exposed is 400 m, in type section.|16-MAY-23
13494|Munyu Sandstone|Lithology|Predominantly sandstone - medium-bedded, poorly sorted, medium to very coarse-grained and gritty quartz arenite: minor well sorted quartz arenite. Also micaceous sandstone, conglomerate, and rare limestone lenses.|16-MAY-23
13494|Munyu Sandstone|Relationships and boundaries|Unconformable on Archaean or Lower Proterozoic Tanami complex and on probably Lower Proterozoic unnamed granite. Overlain, possibly conformably, by probably Adelaidean Redcliff Pound Group but contact is not exposed.|16-MAY-23
13494|Munyu Sandstone|Age reasons|Carpentarian or Adelaidean|16-MAY-23
13494|Munyu Sandstone|Defn approved by|Taken from xerox copy of approved def. sent by WA Sub-Committee.|16-MAY-23
13529|Murraba Formation|Name source|Murraba Ranges, 21o15'S, 128o45'E, Stansmore 1:250 000 Sheet area.|16-MAY-23
13529|Murraba Formation|Unit history|Mapped as Gardiner Beds and Phillipson Beds by Casey & Wells (1964).|16-MAY-23
13529|Murraba Formation|Type section locality|East side of Redcliff Pound, Stansmore Sheet area, at 21o36'30"S, 128o45'30"E. Here a succession 350 m thick dips 20-30oW, beneath conformably overlying Erica Sandstone. The section consists of 160 m flaggy, thin bedded to laminated sublithic arenite overlain successively by 110 m thin bedded, pellety, sublithic arenite, 10 m medium bedded quartz arenite and 70 m of thinly interbedded sublithic arenite and chert granule conglomerate.|16-MAY-23
13529|Murraba Formation|Extent|Eastern parts of Lucas and Stansmore 1:250 000 Sheet areas, WA.|16-MAY-23
13529|Murraba Formation|Thickness range|Maximum exposed about 800 m, at Redcliff Pound.|16-MAY-23
13529|Murraba Formation|Lithology|Sandstone-sublithic and quartz arenite and thin interbeds of chert granule to pebble conglomerate; minor siltstone, shale and dolomite.|16-MAY-23
13529|Murraba Formation|Relationships and boundaries|Part of Redcliff Pound Group. Conformably overlain by Erica Sandstone and inferred to be conformably on Lewis Range Sandstone, though this contact is concealed by Quaternary sand. Overlain unconformably by Palaeozoic and Cretaceous beds.|16-MAY-23
13529|Murraba Formation|Age reasons|Probably Adelaidean.|16-MAY-23
13529|Murraba Formation|Defn approved by|taken from xerox copy of approved def. Sent by WA Sub-Committee|16-MAY-23
13529|Murraba Formation|Name first published by|Blake D.H., Yeates A.N., Walton D.G. 1976|16-MAY-23
26070|Nambeet Formation|Name source|Nambeet well, near Samphire Marsh No. 1 (19.520 deg S, 121.183 deg E).|16-MAY-23
26070|Nambeet Formation|Unit history|Formally defined by Playford & others (1975). Johnstone (1961) described the section. Koop (1966) first published the name Nambeet Formation for this sequence but did not define the formation. Previously included in the Thangoo Limestone in Thangoo No. 1A and Edgar Range No. 1, and in the Willara Formation in Munro No. 1.  Redundant Synonyms: WAPET used the informal names 'Lower Formation' in the Kidson Sub-basin, the 'Unnamed Sandstone Formation' in McLarty No. 1, and  the 'Nambeet Formation Equivalent' in Willara No. 1.|16-MAY-23
26070|Nambeet Formation|Constituents|Although the sequences of the Nambeet Formation in Samphire Marsh No. 1, Tappers Inlet No. 1, and Munro No. 1 are similar - basal sandstone, middle interbedded limestone or carbonate and sandstone and/or shale, and upper shale mainly - it has not been formally subdivided.|16-MAY-23
26070|Nambeet Formation|Type section locality|4069-6610 feet (1240-2015 m) in Samphire Marsh No. 1 (233 in Table 6, BMR Bull 210 (1981) p80).|16-MAY-23
26070|Nambeet Formation|Extent|Only known from drill core. Samphire Marsh No. 1, Willara No. 1, McLarty No.1, Thangoo Nos. 1A and 2, Tappers Inlet No. 1, Munro No. 1, Edgar Range No. 1, Wilson Cliffs No. 1, and Contention Heights No. 1. Its widespread distribution suggests that it extends over most of the Canning Basin south of the Fenton Fault; it probably covers much of the Fitzroy Graben too, where - however - only Tappers Inlet No. 1 on the Pender Terrace has penetrated it. Its northern limit is the Lennard Shelf. Its eastern limit in the graben cannot be estimated. South of the Fenton Fault, it is missing from part of the Broome Arch.|16-MAY-23
26070|Nambeet Formation|Thickness range|Six wells intersected complete sections of the formation: Edgar Range No. 1 (161 m), Thangoo No.1A (49 m), Thangoo No. 2 (71 m), Munro No. 1 (93 m), Tappers Inlet No. 1 (632 m), and Wilson Cliffs No. 1 (540 m). The thickest section is 775 m - the incomplete type section eroded at the top in Samphire Marsh No. 1. Willara No. 1 penetrated 761 m of Nambeet Formation before it reached total depth still in Nambeet Formation. Isopach mapping of the Ordovician suggests that the Nambeet Formation may be more than 1000 m thick south of the Admiral Bay Hingeline; thus the thickest accumulation of the formation would be in the Willara Sub-basin. Isopach thicknesses may be greater in the centre of the Kidson Sub-basin but cannot be substantiated owing to the lack of seismic and drilling data. The thickness at Tappers Inlet No. 1 and isopach contours suggest that the Nambeet Formation is thicker to the south in the Fitzroy Graben than on the Pender Terrace. The thinnest accumulation is on the Broome Arch. This is supported by the absence of the formation in areas of thinnest Ordovician isopach contouring.|16-MAY-23
26070|Nambeet Formation|Lithology|Mainly grey to green shale with interbedded limestone and a basal fine-grained sandstone. In the Kid son Sub-basin and on parts of the Broome Arch the formation is wholly sandstone. Samphire Marsh No. 1 encountered the following sequence: 262 m Shale; fossiliferous grey-green micaceous lenses of fine crystalline limestone and fine sandstone constitute 20-30% of the rock. 145 m Shale and limestone as above. Limestone content is up to 40% in the lower part. Sandstone is absent. 231 m Micaceous, fossiliferous reddish brown to grey fine sandstone interbedded with grey green shale, limestone, and micaceous siltstone. The proportion of siltstone to shale increases with depth giving a coarser texture to the rock. Reddish brown colour in the shale and siltstone becomes more common with depth. 26 m Grey-green to white micaceous dolomitic sandstone grading into sandy dolomite. Fossiliferous with lenses of siltstone. 111 m Hard, well-cemented, siliceous, calcareous sandstone. Grainsize varies from fine to coarse. Colour ranges from grey-green to white and reddish brown.|16-MAY-23
26070|Nambeet Formation|Relationships and boundaries|The formation is everywhere unconformable on Precambrian rocks, which are granite in Samphire Marsh No. 1 and Munro No.1; schist in Edgar Range No. 1; gneiss in Thangoo No. 2; phyllite in Thangoo No. 1A; metabasalt in Tappers Inlet No. 1; and weakly metamorphosed ?Upper Proterozoic ferruginous shale in Wilson Cliffs No. 1 in the Kidson Sub-basin. Except in Samphire Marsh No. 1, the formation is conformably overlain by Ordovician limestone: Willara Formation south of and possibly·in the Fitzroy Graben; Gap Creek Formation on the Pender Terrace; and 'Middle Formation' in the Kidson Sub-basin. The top of the Nambeet Formation is diachronous within the Lower Ordovician (Arenigian). In Samphire Marsh No. 1, the top of the Nambeet Formation is eroded, and unconformably overlain by the Permian Grant Formation. The formation is equivalent to the Carranya beds on both lithology and age. Apart from its basal Ordovician sandstone in BMR Prices Creek No. 3, the Emanuel Formation is a time equivalent of the Nambeet Formation. The 'Lower Formation' (of WAPET) is included as part of the Nambeet Formation because of its lithological similarity, stratigraphic position, and relative age. Creevey (1969) noted a resemblance between the Nambeet Formation and the Pacoota Sandstone of the Amadeus Basin.|16-MAY-23
26070|Nambeet Formation|Age reasons|Early Ordovician (Tremadocian-Arenigian). The Nambeet Formation has a faunal assemblage including trilobites, graptolites, brachiopods, gastropods, and conodonts, .and contains the oldest dated Phanerozoic rocks in the Canning Basin. The Nambeet Formation is known to extend into the Tremadocian only in Samphire Marsh No. 1, where J. Gilbert-Tomlinson (in Johnstone, 1961) suggested the fauna may be as old as latest Cambrian. Veevers (1967 ) has excluded the possibility of Cambrian rocks. The formation is intensely diachronous south of the Fenton Fault; it becomes younger southeast and northeast of Samphire Marsh No. 1. The youngest section is in Tappers Inlet No. 1, on the Pender Terrace. The age of the Nambeet Formation in the Fitzroy Graben is unknown, but is probably older than that on the Pender Terrace. The age of the Emanuel Formation, its equivalent to the east, suggests that the Nambeet Formation in the graben may be as old as the section in Samphire Marsh No. 1.|16-MAY-23
26070|Nambeet Formation|Defn author|Formally defined by Playford & others (1975).  This information copied from BMR Bull 210 (1981), as compiled by R.V. Burne, J.D. Gorter and V.L. Passmore.|16-MAY-23
26070|Nambeet Formation|References|JOHNSTONE, M.H., 1961 - Samphire Marsh No. 1 well, Western Australia, of West Australian Petroleum Pty Ltd. Bureau of Mineral Resources, Australia, Petroleum Search Subsidy Acts Publication 5. ** KOOP, W.J., 1966 - Recent contributions to Palaeozoic geology in the south Canning Basin, Western Australia. APEA Journal, 1966, 105-9  .**PLAYFORD, P.E., COPE, R.N., COCKBAIN, A.E., LOW, G.H., & LOWRY, D.C., 1975 - Phanerozoic. In Geology of Western Australia. Geological Survey of Western Australia, Memoir 2. ** VEEVERS, J.J., 1967b - The Phanerozoic geological history of northwest Australia. Journal of the Geological Society of Australia, 14, 253-71.|16-MAY-23
36770|Nandingarra Granodiorite|Name source|Nandingarra Pool in the northern part of the Split Rock 1:100 000 sheet, in the eastern part of the Pilbara Craton, W.A.|16-MAY-23
36770|Nandingarra Granodiorite|Constituents|Archaean granodiorite to tonalite, and minor monzogranite|16-MAY-23
36770|Nandingarra Granodiorite|Geomorphic expression|forms low rocky relief|16-MAY-23
36770|Nandingarra Granodiorite|Type section locality|7 km north of Nandingarra Pool around MGA 785000E 7618000N|16-MAY-23
36770|Nandingarra Granodiorite|Extent|northwestern part of the Corunna Downs Granitoid Complex|16-MAY-23
36770|Nandingarra Granodiorite|Lithology|Fine- to coarse-grained biotite, hornblende granodiorite to tonalite; minor monzogranite|16-MAY-23
36770|Nandingarra Granodiorite|Relationships and boundaries|Part of the Corunna Downs Granitoid Complex.  Igneous rock intruding the c. 3433 Ma Panorama Formation (Nelson, 2000) in the Warrawoona Group and is intruded by the c. 3317+/-2 Ma (Barley and Pickard, 1999) Carbana Pool Monzogranite (Bagas and Van Kranendonk, in prep.)|16-MAY-23
36770|Nandingarra Granodiorite|Age reasons|between 3433 and 3317 Ma based on relationships outlined above|16-MAY-23
36770|Nandingarra Granodiorite|Proposed publication|GSWA Explanatory notes for the SPLIT ROCK 1:100 000 sheet area|16-MAY-23
36770|Nandingarra Granodiorite|References|Bagas, L., and Van Kranendonk, M. J., in prep., Geology of the Split Rock 1:100 000 sheet: Western Australia Geological Survey, 1:100 000 Geological Series Explanatory Notes. **BARLEY, M. E., and PICKARD, A. L., 1999, An extensive, crustally-derived, 3325 to 3310 Ma silicic volcanoplutonic suite in the eastern Pilbara Craton: evidence from the Kelly Belt, McPhee Dome and Corunna Downs Batholith: Precambrian Research, v. 60, p. 185-241. **NELSON, D. R., 2000, Compilation of geochronology data, 1999: Western Australia Geological Survey, Record 2000/2, 251p.|16-MAY-23
13856|Nardoopiquithanna Adamellite|Name source|Nardoopiquithanna Pool, Marble Bar 1:250 000 Sheet area (MGR 1425 3405).|16-MAY-23
13856|Nardoopiquithanna Adamellite|Type section locality|Although the Adamellite is well exposed over most of its area, access is most readily attained via station and mining tracks from the Wittenoom-Port Hedland road (from a point near Kunagunarrina Pool) extending northwest towards Wodgina and west towards Round Hummock.|16-MAY-23
13856|Nardoopiquithanna Adamellite|Extent|The Nardoopiquithanna Adamellite occurs northwest of Abydos in the Yule Batholith (see Fig. 1) as an arcuate mass, concave towards the south, between laltitudes 21o21'S and 21o19'S, and longitudes 118o40'E and 118o51'E. The pluton has an area of about 125 km2.|16-MAY-23
13856|Nardoopiquithanna Adamellite|Lithology|The Nardoopiquithanna Adamellite is a massive to poorly foliated biotite adamellite. It is fine to medium-grained in the northern portion becoming medium-grained towards the south. The mass is strongly jointed and has almost total outcrop as low rocky ridges and large rounded tors. Pegmatites are sparse.|16-MAY-23
13856|Nardoopiquithanna Adamellite|Relationships and boundaries|The pluton clearly cuts the strong foliation of older banded migmatite in the north and is intruded in the south by Numbana Granite which contains abundant xenoliths of the Adamellite. Relationships with porphyritic rocks to the east (Pincunah Adamellite) and west (Kangan Granite) are uncertain. Possibly the Nardoopiquithanna Adamellite intrudes both the Kangan Granite and Pincunah Adamellite since these exhibit a strong metamorphic foliation not observed in the Nardoopiquithanna Adamellite.|16-MAY-23
13856|Nardoopiquithanna Adamellite|Age reasons|Archaean|16-MAY-23
13856|Nardoopiquithanna 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
13856|Nardoopiquithanna Adamellite|First Reference|79/20350|16-MAY-23
14193|Nita Formation|Name source|Nita Downs homestead, 22 km southeast of Cape Missiessy|16-MAY-23
14193|Nita Formation|Unit history|'E Member' of Carribuddy Formation; 'Evaporite Sequence' of Carribuddy Foramtion (lower part) in Willara No.1; 'Unit A' in Blackstone No.1. Roebuck Dolomite considered a synonym. The sequence 3821 - 4165 feet  in Parda No.1 has been removed from the Goldwyer Formation and 'Red and Green Claystone' and defined as the type section of the Nita Formation. The 'E Member has been removed from the Carribuddy Formation in Edgar Range No. 1, Matches Springs No.1, and McLarty No.1, and is now considered to be Nita Formation.|16-MAY-23
14193|Nita Formation|Constituents|Formation not formally subdivided, though an in formal threefold subdivision is evident in many of the wells and the type section. The lower unit is interbedded shale and limestone in equal proportions or with limestone slightly more predominant. The middle unit is limestone (dolomite in Barbwire No. 1) with minor thin shale interbeds. The upper unit is a dolomite, often massive, interbedded with shale; the shale content may increase up to or exceed 50% at the top. The relative thickness of each member varies.|16-MAY-23
14193|Nita Formation|Type section locality|3821 - 4165 feet (1165 - 1269 m) in Parda No.1 (18deg 56'08" S, 122deg 00' 34'' E.|16-MAY-23
14193|Nita Formation|Description at type locality|In Parda No.1: 33 m Dolomite, light to dark grey, finely massive, crystalline, argillaceous, calcareous, and anhydritic. Thin beds of grey shale and light grey crystalline limestone are interbedded with the dolomite. Traces of quartz and anhydrite are common; ghosts of marofossils are less common. 51 m Limestone, pale grey, finely crystalline, dolomitic in part, fossiliferous, and massive.Interbedded with thin dark beds of grey shale. 20 m Limestone and shale interbedded. The limestoneis light grey and crystalline; the shale is dark grey and thin bedded.|16-MAY-23
14193|Nita Formation|Extent|No  outcrop. McLarty No.1, Barbwire No.1, Munro No.1, Willara No.1, Parda No.1, Edgar Range No.1, Matches Springs No.1, Blackstone No. 1; Broome Arch, Barwire and Margaret Terraces, and Willara Sub-basin. The eastern limit is uncertain. The formation was not identified in any of the wells in the Kidson Sub-basin, but it may be present in the western part of the sub-basin where the wells did not penetrate the Ordovician rocks. The formation is assumed to be present on the Jurgurra Terrace abnd possibly  in the Fitzroy Graben.|16-MAY-23
14193|Nita Formation|General description|The type section  in Parda No. 1 is typical of the formation. The upper unit is missing in McLarty No.1, where the formation is thin (57 m); its absence may be due to postdepositional erosion. Only dolomite was recorded from the section in Barbwire No. 1. Whether this represents local development or postdepositional alteration is uncertian. This section is also abmormally thin although no direct relationship between the lithology and the thickness of this section is established.  Anhydrite is most abundant in association with the dolomite near the top of the formation, and comprises up to 25% of the upper unit is Willara No. 1, but is absent in Edgar Range No. 1. In Blackstone No. 1, the formation is much more argillaceous than in the southern part of the basin, but, although it has a similar sequence of dolomite overlying limestone, anhydrite is again absent from the upper unit. Dolomitisation of the limestone is probably secondary, or even tertiary. In Edgar Range No. 1, successive periods of dolomitisation are evident in some zones. Generally the porosity is low and the permeability is very low or not developed. the middle and lower untis are uniformly tight, and show little of no signs of porosity or permeability. but vugs in the upper dolomite give some porosity to the formation. In Edgar Range No. 1 the vugular porosity in less argillaceous zones in which dolomite has replaced fossils of almost pure limestone is up to 12%. Porosity is best developed  at former shell bed levels, where, however, permeability is low to non-existent.|16-MAY-23
14193|Nita Formation|Thickness range|The thickest section is 250 m in Matches Springs No.1. Alll other wells that encountered the formation intersected more complete sections ranging in thickness from 52 m to 239 m; McLarty No.1 (52 m), Barbwire No.1 (52 m), Munro No.1 (84 m), Willara No.1 (137 m), Parda No.1 (106 m), Edgar Range No.1 (172 m), Blackstone No. 1 (239 m). The Nita Formation appears to thicken to the north and thin to the east. It has not been identified in on the western onshore Broome Arch, though the Roebuck Dolomite, a lithological and time correlative, is present in both Dampier Downs No. 1 and Roebuck Bay No. 1. Any inferences made from its thickness variations can only be tentative due to the effects of erosion, particularly on the eastern Broome Arch, and the absence of data in the Fitzroy Graben.|16-MAY-23
14193|Nita Formation|Lithology|Chiefly a grey massive crystalline carbonate containing both limestone and dolomite in different proportions from well to well. Subordinate amounts of grey shale are interbedded with carbonate, and are most abumdant at the base and at the top of the formation.|16-MAY-23
14193|Nita Formation|Relationships and boundaries|Conformably overlies the Goldwyer Formation. Their contact is gradational in several of the wells, and more sharply defined wher ethe basal lithology of the Nita Formation is a relavelty clean limestone, as in McLarty  No. 1. In Blackstone No. 1 their contact is difficult ot pick owing to the relatively high proportion of shale in the Nita Formation. South of the Fitzroy Graben, their contact is gradational; it si picked at the base of a dominantly dolomite sequence; below this contact the lithology if wholly more than 50% shale.  The Carribuddy Formation unconformably overlies the Nita Formation south of the Fitzroy Graben. North of the graben, only Blackstone No. 1 intersected the Nita Formation, which is unconformably overlain by the Devonian Poulton Formation. The unconformity between the Carribuddy and Nita Formations is based on meagre dating of Carribuddy Formation, which suggests a hatus encompassing the Late Ordovician and the Silurian; lithologically the contact appears to be conformable and , in places, gradational.  The formation is botha  lithological and time correlative of the Roebuck Dolomite, which should perhaps be considered part of the formation. In the Kidson Sub-basin, and in Balckstone No. 1 on the Margaret Terrace, the top of the Goldwyer Formation is a time correlative of the Nita Formation south of the Fitzroy Graben. The Nita Formation in Blackstones No. 1 has no known time equivalents in the Canning Basin.|16-MAY-23
14193|Nita Formation|Age reasons|Llanvirnian to Llandeilian (middle Ordovician). Conodont studies by R.A. McTavish (Browd, 1973) restrict the Nita Formation to the middle Ordovician. Conodonts include Phragmodus sp. cf. P inflexus, Ozarkodina spp., Chirognathus spp., Amorphognathus, and Panderodus gracilis (Playford & others, 1975). A miiddle Ordovician age is supported by a microflora which yeilds a similar age. Bivalves from the Nita Formation including Ctenodonta suggst a slightly younger age - middle to early Late Ordovician.|16-MAY-23
14193|Nita Formation|Defn author|R.A. McTavish (in Playford et al. , 1975). GSWA Memoir 2. Reported in BMR Bulletin 210, Appendix 1 (1981).|16-MAY-23
14193|Nita Formation|References|BMR Bull 210, Appendix 1 p10-13.|16-MAY-23
14208|Noingara Siltstone|Name source|Noingara well, 3-2 km north-northwest of the type section (30o14'S, 116o00'E). Moora 1:250 000 Sheet area.|16-MAY-23
14208|Noingara Siltstone|Type section locality|790 m of siltstone and minor interbedded chert and orthoquartzite. This is a discontinuous composite section, which commences 1-8 km west-southwest of Longreach Homestead and extends east to near the homestead.|16-MAY-23
14208|Noingara Siltstone|Extent|The formation is known only in the area extending from 8 km northwest of Watheroo to just west of Coorow.|16-MAY-23
14208|Noingara Siltstone|Thickness range|The type section is the only section measured.|16-MAY-23
14208|Noingara Siltstone|Lithology|Siltstone, red-brown, light-grey, white, and pale-yellow, massive to thin-bedded: thin interbeds of white and grey chert, and some orthoquartzite.|16-MAY-23
14208|Noingara Siltstone|Relationships and boundaries|The lower limit of the unit is not exposed, but stratigraphic evidence suggests that the formation overlies the Coomberdale Chert. It is overlain conformably by the Winemaya Quartzite. The top of the formation is defined by a predominantly red-brown, also light-grey to white and pale-yellow, mostly massive, micaceous and highly ferruginous siltstone 581 m thick.|16-MAY-23
14208|Noingara Siltstone|Age reasons|No fossils have so far been found in the formation but it is believed to be of Proterozoic age because of its relationship with underlying formations of the Moora Group.|16-MAY-23
14208|Noingara Siltstone|Proposed publication|Geology of Western Australia; West Aust. Geol. Survey, Memoir 2; in press.|16-MAY-23
14208|Noingara Siltstone|Name first published by|Lipple S.L., 1976|16-MAY-23
24433|North Shaw Tonalite|Name source|North Shaw Well, Marble Bar 1:250 000 Sheet area (MGR 216 335).|16-MAY-23
24433|North Shaw Tonalite|Type section locality|The pluton is well exposed near the North Shaw Well.|16-MAY-23
24433|North Shaw Tonalite|Extent|The North Shaw Tonalite occurs as a small pluton (area of 35 km2) in the northern part of the Shaw Batholith (see Fig. 1), between latitudes 21o19'S and 21o23'S, and longitudes 119o23'E and 119o28'E.|16-MAY-23
24433|North Shaw Tonalite|Lithology|The North Shaw Tonalite is an equigranular, poorly foliated biotite tonalite. The composition is variable due to assimilation of Archaean greenstone material from the enclosing country rock. The pluton is notable for the preservation of igneous textures. Near the North Shaw Well, the pluton is a fine-grained biotite tonalite with euhedral sericitized oligoclase, quartz, chlorite after biotite, opaque iron oxide; minor microcline, common accessory apatite and sphene, rare zircon and allanite; and secondary carbonate, epidote and sericite. Other varieties in the pluton occurring to the south and east of North Shaw Well are medium to coarse-grained biotite granodiorite, and medium-grained hornblende biotite granofiorite with hornblende phenocrysts. Accessory minerals are similar for these varieties except that sphene is more abundant in the latter type.|16-MAY-23
24433|North Shaw Tonalite|Relationships and boundaries|The pluton intrudes mafic and felsic volcanic rocks of the Archaean Warrawoona Group. The pluton is intruded by Lower Proterozoic dolerite dykes and is unconformably overlain by Mount Roe Basalt. The relationship with gneissose and migmatitic granodiorite to the south is not known but the preservation of primary textures in the North Shaw Tonalite contrasted with the strong metamorphic foliation of the migmatitic rocks suggest that the Tonalite is younger and intrudes the migmatitic granodiorite.  The tonalite may be the source of numerous thin quartz-feldspar porphyry dykes which intrude the Archaean basalt around the North Shaw mining centre. Several quartz veins cut the pluton. Exposure is generally not good since it is obscured by extensive but thin Quaternary gravel and sand deposits.|16-MAY-23
24433|North Shaw Tonalite|Age reasons|Archaean|16-MAY-23
24433|North Shaw Tonalite|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
24433|North Shaw Tonalite|First Reference|83/23412|16-MAY-23
24433|North Shaw Tonalite|Proposer|Lipple S.L. and Hickman A.H.|16-MAY-23
24433|North Shaw Tonalite|Resdate|15-JAN-1975|16-MAY-23
14360|Nullara Limestone|Name source|Nullara Spring, near northeast end of Oscar Range (17o38'24"S, 124o54'20"E).|16-MAY-23
14360|Nullara Limestone|Unit history|The Nullara Limestone previously formed the upper part of the Pillara Limestone of Playford and Lowry (1966). The name "Nullara Oolite" was first used for the lower part of the present formation in an unpublished Wapet report. The name "Nullara Formation" was shown on a stratigraphic chart by Read (1973).|16-MAY-23
14360|Nullara Limestone|Type section locality|Northeast end of Oscar Range, from 17o39'15"S, 124o56'12"E to 17o38'45"S, 124o54'20"E.|16-MAY-23
14360|Nullara Limestone|Extent|Exposed in the Oscar Range, Napier Range, Horeshoe Range and Red Bluffs areas.  Encountered in severl wells on the Lennard Shelf.|16-MAY-23
14360|Nullara Limestone|Thickness range|About 400 m thick in the type section.  Up to 320 m thick in several wells on the Lennard Shelf.|16-MAY-23
14360|Nullara Limestone|Lithology|Dominantly well-bedded fenestral (cryptalgal) calcarenite and oolite, with some interbeds of sandstone and siltstone.|16-MAY-23
14360|Nullara Limestone|Fossils|Most of unit consists of cryptalgal limestone and oolite with few skeletal fossils other than thick-shelled gastropods and bivalves. Incriodid conodonts occur rarely, and there are also some stromatoporoids and brachiopods. They indicate a Famennian age. The lower limit is uncertain, but the formation probably extends up into the latest Famennian (do VI).|16-MAY-23
14360|Nullara Limestone|Relationships and boundaries|Overlies and interfingers with the Windjana Limestone; interfingers with or is abutted by the Piker Hills and Virgin Hills Formations. Overlain conformably by the Fairfield Formation.|16-MAY-23
14360|Nullara Limestone|Defn author|Playford P.E., Cockbain A.E., 1976  |16-MAY-23
14360|Nullara Limestone|Proposed publication|Geological Survey of WA Annual Rept|16-MAY-23
14360|Nullara Limestone|Defn Reference|83/23481|16-MAY-23
30595|Onedin Member|Name source|Onedin Prospect, GR CE454734.|16-MAY-23
30595|Onedin Member|Geomorphic expression|low narrow ridges.|16-MAY-23
30595|Onedin Member|Type section locality|southeastern flank of syncline at GR CE460738, near Onedin prospect (Zn-Cu-Pb), Halls Creek 1:100 000 Sheet area. Here the member is about 30 m thick and consists of red shale with limonitic chert (carbonate at depth), gossan and ironstone; it is underlain by sandstone and overlain and intruded by rhyolite (Orth 1997).|16-MAY-23
30595|Onedin Member|Extent|SW of Halls Creek, in Halls Creek 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area, WA|16-MAY-23
30595|Onedin Member|Thickness range|maximum about 150 m.|16-MAY-23
30595|Onedin Member|Lithology|red shale with interlayered ironstone, chert, carbonate and gossan; also chloritic, talc-rich, and carbonaceous shale, calc-silicate rocks, iron-rich dolomite and tremolite-talc schist in drill core.|16-MAY-23
30595|Onedin Member|Depositional environment|marine.|16-MAY-23
30595|Onedin Member|Relationships and boundaries|Of Koongie Park Formation. Conformable band within Koongie Park Formation.|16-MAY-23
30595|Onedin Member|Age reasons|Palaeoproterozoic - Orosirian, as part of Koongie Park Formation, which is dated at 1843 Ma (Page et al. 1995).|16-MAY-23
30595|Onedin Member|Correlations|as for Koongie Park Formation|16-MAY-23
30595|Onedin 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. **Orth, K.,1997. Notes on the geology of the Koongie Park Formation southwest of  Halls Creek, Western Australia. Australian Geological Survey Organisation, Record 1997/25.|16-MAY-23
27093|Padbury Group|Name source|Revision of Definition of Barnett 1975 so as to include new formation (Wilthorpe Conglomerate) and to exclude the Labouchere Formation.|16-MAY-23
27093|Padbury Group|Constituents|Wilthorpe Conglomerate (Gee 1979) Robinson Range Formation and Millidie Formation (Barnett 1975).|16-MAY-23
27093|Padbury Group|Relationships and boundaries|Unconformably overlies Glengarry Group; probably correlates with Earaheedy Group in eastern part of Nabberu Basin (Hall and others 1977).|16-MAY-23
27093|Padbury Group|Age reasons|Proterozoic, probably about 1.8-1.7 b.y.|16-MAY-23
27093|Padbury Group|Defn author|Denis Gee, 1978.|16-MAY-23
27093|Padbury Group|Proposed publication|Western Australia Geological Survey Annual Report for 1978 (Pub. 1979)|16-MAY-23
14753|Paddy Market Formation|Name source|Paddy Market Creek (Military Grid 202 328), Marble Bar 1:250 000 Sheet area.|16-MAY-23
14753|Paddy Market Formation|Type section locality|The unit is well exposed in a gorge cut by Paddy Market Creek through a prominent ridge at 202 328. It is also well exposed east of Split Rock homestead and north of Honeyeater Creek (201 347). Ferruginous shales are prominent in the area north of Honeyeater Creek.|16-MAY-23
14753|Paddy Market Formation|Extent|The Paddy Market Formation occurs in the North Shaw Belt and Pilgangoora, Lalla Rookh and Coongan Belt Synclines.|16-MAY-23
14753|Paddy Market Formation|Thickness range|Maximum thickness about 1 km|16-MAY-23
14753|Paddy Market Formation|Lithology|Banded iron formation, shales and ferruginous sandstones and siltstones.|16-MAY-23
14753|Paddy Market Formation|Relationships and boundaries|Conformably underlies the Honeyeater Formation and conformably overlies the Corboy Formation and a thick unassigned sequence of sandstones and siltstones of the Soanesville Subgroup.|16-MAY-23
14753|Paddy Market Formation|Age reasons|Archaean because of tectonic style and conformity with other divisions of the greenstone sequence intruded by Archaean granitic rocks.|16-MAY-23
14753|Paddy Market Formation|Defn author|Lipple S.L., 1975|16-MAY-23
14753|Paddy Market Formation|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
80587|Panhandle Dolerite|Name source|Named after the Panhandle Syncline (Lat. -22.7842 Long. 117.6283) on the MOUNT LIONEL 1:100 000 mapsheet, which makes up the southern part of the Turner Syncline in the vicinity of Tom Price, and trends parallel to the trend of the Panhandle Dolerite dykes. Numerous well-exposed Panhandle dykes are also present in this area.|16-MAY-23
80587|Panhandle Dolerite|Unit history|Synonymous with the P_d5 dolerite dyke suite of Tyler (1990), and the c. 2008 Ma dolerite dykes dated by Muller et al. (2005).|16-MAY-23
80587|Panhandle Dolerite|Geomorphic expression|Narrow, steep-sided gullies in BIF or discontinuous, linear, rubbly outcrops in other lithologies (especially Fortescue Group basalts).|16-MAY-23
80587|Panhandle Dolerite|Type section locality|Panhandle Syncline (Lat. -22.7842 Long. 117.6283) on the MOUNT LIONEL 1:100 000 mapsheet.|16-MAY-23
80587|Panhandle Dolerite|Extent|Panhandle Dolerite dykes are present throughout the Hamersley province, southwest of a line between Newman and Pannawonica in units that are older than the Wooly Formation.|16-MAY-23
80587|Panhandle Dolerite|Thickness range|Generally a few tens of metres wide, or less.|16-MAY-23
80587|Panhandle Dolerite|Lithology|Medium-grained dolerite.|16-MAY-23
80587|Panhandle Dolerite|Relationships and boundaries|All Panhandle Dolerite dykes trend broadly northwest and commonly form narrow gullies within exposed Hamersley Group BIF. The dykes also post-date all regional folding of the Hamersley Group. Intrudes all units up to and including the Cheela Springs Basalt. Although the Panhandle Dolerite is supposedly younger than the Wooly Formation (Muller et al., 2005), no dykes are known to intrude this unit.|16-MAY-23
80587|Panhandle Dolerite|Identifying features|Narrow, steep-sided, northwest-trending gullies in BIF, particularly well-developed on the southwest flank of Mount Nameless.|16-MAY-23
80587|Panhandle Dolerite|Structure and Metamorphism|Intrusion likely controlled by the axial planar fabric of northwest-trending folds, and post-dates this folding. Responsible for mild thermal metamorphism of country rocks, especially in BIF where secondary magnetite enhances the aeromagnetic response.|16-MAY-23
80587|Panhandle Dolerite|Age reasons|Muller et al. (2005) dated baddeleyite in Panhandle Dolerite dykes in the Hardey Syncline (2007 +/- 16 Ma) and at the Paraburdoo mine site (2009 +/- 16 Ma), but the age of intrusion is commonly assumed to be c. 2008 Ma.|16-MAY-23
80587|Panhandle Dolerite|Geophysical Expression|Dykes themselves do not appear to be very magnetic, but are well-expressed in aeromagnetic data where they cross-cut BIF, producing magnetite in the wall-rocks.|16-MAY-23
80587|Panhandle Dolerite|Geochemistry|Relatively flat, unenriched REE patterns, distinctive from all other dyke suites in the region which tend to be LREE-enriched.|16-MAY-23
80587|Panhandle Dolerite|Defn author|D. McB. Martin, Geological Survey of Western Australia 7-JUL-2020.|16-MAY-23
80587|Panhandle Dolerite|Proposed publication|GSWA Report 203|16-MAY-23
80587|Panhandle Dolerite|Comments|Tyler (1990) interpreted that Panhandle Dolerite dykes post-dated an earlier west-northwest trending dyke suite (Pd_4), but this relationship has not yet been validated. All dykes of this trend in the Rocklea Anticline are younger than the Panhandle Dolerite and probably belong to the Round Hummock Dolerite.|16-MAY-23
80587|Panhandle Dolerite|References|Muller, SG, Krapez, B, Barley, ME and Fletcher, IR 2005, Giant iron-ore deposits of the Hamersley province related to the breakup of Paleoproterozoic Australia: New insights from in situ SHRIMP dating of baddeleyite from mafic intrusions: Geology, v. 33, no. 7, p. 577-580.  **Tyler, IM 1990, Pilbara Craton  -  Mafic dyke swarms, in Geology and mineral resources of Western Australia: Geological Survey of Western Australia, Memoir 3, p. 191-194.|16-MAY-23
14834|Panorama Formation|Name source|From Panorama Ridge, which is a prominent ridge extending about 22 km west from Military Grid Reference 230 344 to 206 342, Marble Bar 1:250 000 Sheet area.|16-MAY-23
14834|Panorama Formation|Type section locality|Panorama ridge in the area 6 km northeast from North Shaw mining centre.|16-MAY-23
14834|Panorama Formation|Extent|The Panorama Formation occurs along Panorama Ridge in the North Pole Dome and as inliers within the Proterozoic cover of the North Pole Dome.|16-MAY-23
14834|Panorama Formation|Thickness range|Maximum 1 km.|16-MAY-23
14834|Panorama Formation|Lithology|Dacite lava, tuff and agglomerate are dominant in the western portion. The lava is generally massive and may be vesicular or porphyritic. Minor sedimentary rocks including shale, sandstone and conglomerate are intercalated within the volcanic sequence. Banded cherts including red and white, grey and white, black and white and green coloured varieties are prominent. In the eastern portion of the Formation, sandstones, grits and conglomerates become dominant. The conglomerates contain abundant clasts of chert, dacite, vein quartz and rare basalt. Current stratification is common in sandstone and grit units.|16-MAY-23
14834|Panorama Formation|Relationships and boundaries|The Panorama Formation is a lensoid volcanic-sedimentary rock sequence conformably within the unassigned pillow basalt of the Salgash Subgroup. The volcanic and sedimentary rocks exhibit an interfingering contemporary facies relationship with some contribution from the volcanic pile to the adjacent sedimentary deposits. Equivalent to the Kelly Formation.|16-MAY-23
14834|Panorama Formation|Age reasons|Archaean|16-MAY-23
14834|Panorama Formation|Defn author|Lipple S.L. 1975|16-MAY-23
14834|Panorama Formation|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
26833|Paringa Basalt|Name source|From the Paringa Gold Mining Lease 5782E which is situated at the northern extremity of the Golden Mile|16-MAY-23
26833|Paringa Basalt|Type section locality|Chloritic types are exposed in the underground workings on the Golden Mile, centred about the Fimiston Post Office (30deg46'40''S, 121deg 27'50''E). Amphibolitic varieties outcrop immediately north of the Kalgoorlie Golf Course (30deg 43'20''S, 121deg27'10'').|16-MAY-23
26833|Paringa Basalt|Extent|Several belts, the result of repetition by folding, trend north-north-west and south-south-east from the Golden Mile|16-MAY-23
26833|Paringa Basalt|General description|Outcrop pattern: this rock rarely crops out. Outcrops of the chloritic varieties are invariably oxidised, whereas outcrops of the amphibolitic varieties are usually fresh. Representative specimens are kept by the Geological Survey of Western Australia.|16-MAY-23
26833|Paringa Basalt|Thickness range|1,500 - 2,500 feet. [~458 - 763 m]|16-MAY-23
26833|Paringa Basalt|Lithology|Meta-basaltic lavas, in part pillow lavas, with minor thin interbedded pyroclastics and slates. The lavas are typically fine grained amphibolitic rocks, altered in some areas to chlorite-carbonate rocks. The chloritic varieties are locally termed "fine grained greenstones" and bleached, chloritic types "calc schist".|16-MAY-23
26833|Paringa Basalt|Relationships and boundaries|Conformably overlies the Williamstown Dolerite and is conformably overlain by the Golden Mile Dolerite. The upper contact is usually marked by a thin slate band; the lower contact may also be marked by slate.|16-MAY-23
26833|Paringa Basalt|Age reasons|Archaean.|16-MAY-23
26833|Paringa Basalt|Geochemistry|Analysed specimens recorded in GSWA Bulletin Nos. 6, 41, 51, 67, 69 and 94 are:  (a) amphibolitic varieties - 11033. (b) chloritic varieties - 13773, 13451.|16-MAY-23
26833|Paringa Basalt|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
26833|Paringa Basalt|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
26833|Paringa Basalt|References|GSWA Bulletin Nos. 6, 41, 51, 67, 69 and 94.  **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
74168|Pegasus Dolomite Member|Name source|Pegasus 1 petroleum exploration well (20degrees 5' 45.60"S 123degrees 57' 8.83"E, Joanna Spring 1:250 000 map sheet), in which the member is intersected close to the centre of its known distribution.|16-MAY-23
74168|Pegasus Dolomite Member|Constituents|None.|16-MAY-23
74168|Pegasus Dolomite Member|Geomorphic expression|Sub-surface only.|16-MAY-23
74168|Pegasus Dolomite Member|Type section locality|The fully cored interval 550.45 - 552.6 m in petroleum exploration well Acacia 1 (19degrees 19' 44.95"S 124degrees 59' 43.66"E; Crossland 1:250 000 map sheet). Reference locality for western area: Fully cored interval 971.75 - 975.5 m in mineral exploration drill hole Brooke 1 (19degrees 44' 52.17"S 122degrees 55' 3.60"E). Both cores are stored in Geological Survey of Western Australia Perth core library. DESCRIPTION AT TYPE :LOCALITY:  Light grey, hard, massive dolomite; stylolitic, with infilled subvertical fractures, microfaults, calcite filled veins and minor vuggy porosity.|16-MAY-23
74168|Pegasus Dolomite Member|Description at type locality|Light grey, hard, massive dolomite; stylolitic, with infilled subvertical fractures, microfaults, calcite filled veins and minor vuggy porosity.|16-MAY-23
74168|Pegasus Dolomite Member|Extent|Widespread in the Canning Basin in wells south of the Fenton Fault Zone, although apparently absent (or thin) in the southern and eastern Kidson Sub-basin. Commonly removed by pre-Permian erosion in wells near the west coast. Only known from the sub-surface.|16-MAY-23
74168|Pegasus Dolomite Member|Thickness range|Thickness at type section 2.15 m. Average thickness estimated at 2 m. Maximum thickness 4 m in petroleum explorations wells Dodonea 2 and Sally May 1.|16-MAY-23
74168|Pegasus Dolomite Member|Lithology|Typically hard, massive to nodular and laminated, fine grained, cream to pale grey and brown dolomite and argillaceous dolomite. Locally includes, or is dominated by dolomitic limestone. Local anhydrite. The member has a distinctive signature on wireline logs (a sharp and often double spike on gamma and sonic logs) allowing it to be easily recognised in numerous petroleum exploration wells.|16-MAY-23
74168|Pegasus Dolomite Member|Depositional environment|Shallow or marginal marine incursion.|16-MAY-23
74168|Pegasus Dolomite Member|Fossils|None known.|16-MAY-23
74168|Pegasus Dolomite Member|Diastems or hiatuses|None known.|16-MAY-23
74168|Pegasus Dolomite Member|Relationships and boundaries| A conformable member within or occasionally at the base the Sahara Formation of the Carribuddy Group. Boundaries are relatively sharp with mudstone below and above. Although this thin marker was probably deposited approximately synchronously across the basin, its position relative to the base of the Sahara Formation varies because of the diachronous nature of the salt-defined lower boundary of the formation. In several wells it lies at the base of the Sahara Formation|16-MAY-23
74168|Pegasus Dolomite Member|Age reasons|No internal evidence for age. The age is inferred to be Late Ordovician to Early Silurian based on biostratigraphic ages from the underlying Mallowa Salt (Foster and Williams, 1991) and overlying basal Worral Formation (Nicoll et al., 1994).|16-MAY-23
74168|Pegasus Dolomite Member|Defn author|Haines, P.W. 2008|16-MAY-23
74168|Pegasus Dolomite Member|Comments|A valuable stratigraphic marker aiding well correlations across the basin|16-MAY-23
74168|Pegasus Dolomite Member|References|Foster, CB, and Williams, GE, 1991, Late Ordovician - Early Silurian age for the Mallowa Salt of the Carribuddy Group, Canning Basin, Western Australia, based on occurrences of Tetrahedraletes medinensis Strother & Traverse 1979: Australian Journal of Earth Sciences, v. 38, p. 223-228.***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.|16-MAY-23
31962|Pimbyana Granite|Name source|Pimbyana Creek at MGA Zone 50, 434000E 7350000N|16-MAY-23
31962|Pimbyana Granite|Unit history|The name "Pimbyana Granite" was first used by Pearson et al. (1996; AJES v.43, p.299-309). A brief description was provided, along with two whole-rock chemical analyses. The synonym "Pimbyana Granitoid" was introduced by Krapez (1999; AJES v 46(1), p.71-89) but no justification is given for the name change. The synonym is only mentioned in the paper, and the unit was not studied by the author.|16-MAY-23
31962|Pimbyana Granite|Geomorphic expression|Low rounded hills covered in boulders and tors. Whalebacks with reddish weathered surfaces are common.|16-MAY-23
31962|Pimbyana Granite|Type section locality|About 0.5 km NW of the Frasers-Yangibana REE prospect on the Edmund 100k sheet area (MGA Zone 50 429500E 7351500N). Access is via a station track from Gifford Creek Homestead via Fraser Bore.|16-MAY-23
31962|Pimbyana Granite|Extent|The Pimbyana Granite forms a NW trending belt at least 90 km long comprising numerous intrusions extending from just north of Gifford Creek Homestead to near Maroonah Homestead. The most abundant rock type is a coarse-grained porphyritic to megacrystic biotite(-muscovite) monzogranite to syenogranite. The vast bulk of the intrusion contains squat tabular megacrysts or phenocrysts of microperthite, although between Bald Hill North and Henderson Bore on the Edmund 100K sheet, round K-feldspar megacrysts with graphic textures predominate. A fine- to medium-grained, even-textured tonalite or granodiorite that is comingled with the megacrystic phase is also included within the Pimbyana Granite.|16-MAY-23
31962|Pimbyana Granite|Lithology|The most abundant rock type is a coarse-grained porphyritic to megacrystic biotite(-muscovite) monzogranite to syenogranite. Fine- to medium-grained biotite tonalite and granodiorite comprises an un-named member. It is only abundant in the area east and southeast of the Star of Mangaroon mine on the Mangaroon 100K sheet, and around the Frasers-Yangibana REE prospect on the Edmund 100K sheet. Between the Yangibana South and Frasers-Yangibana REE prospects, the Pimbyana Granite contains abundant inclusions metasedimentary and mafic meta-igneous rocks it is mapped as a separate, un-named member.|16-MAY-23
31962|Pimbyana Granite|Relationships and boundaries|The Pimbyana Granite intrudes foliated porphyritic granodiorite and augen gneiss of the Gooche Gneiss, and metasedimentary rocks of the Pooranoo Metamorphics. The megacrystic monzogranite to syenogranite phase is intruded by various other units of the Durlacher Supersuite: namely the Dingo Creek Granite and the Yangibana Granite, and by extensive veins and dykes of muscovite-biotite granite, and tourmaline-bearing granite and pegmatite.|16-MAY-23
31962|Pimbyana Granite|Age reasons|Two samples of porphyritic biotite-muscovite syenogranite have been dated at 1673 ? 15 Ma (GSWA 169060; D.R. Nelson, 2002, GSWA Record 2002/2) and 1673 ? 11 Ma (GSWA 178029; D.R. Nelson, in prep., GSWA Record 2004/2). A sample of fine-to medium-grained, even-textured biotite tonalite from about 500 m northwest of the Frasers-Yangibana prospect (GSWA sample 169054) has an indistinguishable SHRIMP U-Pb zircon age of 1674 ? 8 Ma (D.R. Nelson, 2002, GSWA Record 2002/2).|16-MAY-23
31962|Pimbyana Granite|Comments|The name "Pimbyana Granite" was first used by Pearson et al. (1996; AJES v.43, p.299-309). A brief description was provided, along with two whole-rock chemical analyses.|16-MAY-23
31962|Pimbyana Granite|References|Martin, D.M., Thorne, A.M. and Occhipinti, S.A., 2002, Edmund, W.A. Sheet 2150. Western Australia Geological Survey, 1:100 000 Geological Series.|16-MAY-23
72985|Pirrilyungka Formation|Unit history|The Pirrilyungka Formation is a succession of diamictite, sandstone, mudstone and pebble conglomerate between 779.2 and 2017 m (total depth) in Vines 1. It was previously included in the Vines Formation, and is named after Pirrilyungka Outstation (26°31'48''S 128°25'47''E, Cooper 1:250 000 map sheet).|16-MAY-23
72985|Pirrilyungka Formation|Type section locality|Between 779.2 and 2017 m (total depth) in GSWA Vines 1 stratigraphic drillhole. The base was not intersected, and the unit extends for an unknown depth below the total depth of Vines 1. This interval is continuously cored.|16-MAY-23
72985|Pirrilyungka Formation|Extent|Vines 1 is the only known occurrence. Similar successions with comparable or greater thicknesses are known from the Adelaide Rift Complex (Sturt Tillite and equivalents), eastern Officer Basin in South Australia and the Amadeus Basin.|16-MAY-23
72985|Pirrilyungka Formation|Lithology|Dark-grey diamictite with local reddish-brown horizons, sandstone, mudstone and pebble conglomerate. Deposited in marine and possibly continental, glacially influenced settings.|16-MAY-23
72985|Pirrilyungka Formation|Relationships and boundaries|Overlain, apparently unconformably, by Wahlgu Formation. Probably overlies equivalents of the upper Buldya Group (based on probably reworked palynomorphs and stromatolites), but the contact is not observed.|16-MAY-23
72985|Pirrilyungka Formation|Age reasons|Poorly preserved Cerebrosphaera buickii were recovered throughout the formation. These are most probably reworked, but it is possible that slightly better preserved specimens in the lower 200 m are in situ. If so, they may imply a Cryogenian age, and possible correlation with the uppermost Steptoe Formation of the Buldya Group. The youngest extent of C. buickii is uncertain, but it has not so far been recorded in situ in rocks equivalent to the Sturtian glaciation or younger elsewhere in Australia. Evidence for glacial influence and other lithological characteristics suggest correlation with the Sturtian glacial succession of central and South Australia.|16-MAY-23
72985|Pirrilyungka Formation|Defn Reference|Haines, PW, Hocking, RM, Grey, K and Stevens, MK, 2008, 'Vines 1 revisited: are older Neoproterozoic glacial deposits preserved in Western Australia?', Australian Journal of Earth Sciences, vol. 55(3), p. 397-406.|16-MAY-23
24461|Point Torment Sand|Name source|Point Torment grid reference 117853 Derby 1:250 000 Sheet.|16-MAY-23
24461|Point Torment Sand|Type section locality|Point Torment Light tower (grid reference 120847, Derby 1:250 000 Sheet)|16-MAY-23
24461|Point Torment Sand|Extent|Discontinuous shoreline depsoit on both east and west shores of King Sound.|16-MAY-23
24461|Point Torment Sand|Thickness range|<1 m up to 3 m.|16-MAY-23
24461|Point Torment Sand|Lithology|Cross laminated cross bedded and bioturbated medium and coarse quartz skeletal sand, shelly sand and lithoclastic sand; generally white or cream colour.|16-MAY-23
24461|Point Torment Sand|Relationships and boundaries|The Point Torment Sand unconformably abuts Mowanjum Sand; locally the formation rests unconformably on Christine Point Clay. The formation more typically overlies and interfingers with Doctors Creek Formation.|16-MAY-23
24461|Point Torment Sand|Age reasons|The Point Torment Sand is being deposited today and is obviously Holocene.|16-MAY-23
24461|Point Torment Sand|Proposed publication|Journal of the Royal Society of WA|16-MAY-23
24461|Point Torment Sand|Proposer|Semeniuk V.|16-MAY-23
37649|Pooranoo Metamorphics|Name source|Pooranoo Well (382300E 7363400N MGA 94) on the Mangaroon 100K sheet|16-MAY-23
37649|Pooranoo Metamorphics|Geomorphic expression|Metamorphosed cobble and pebble conglomerate forms low ridges. Metamorphosed feldspathic sandstone and pelitic gneiss form low, undulating countryside dissected by numerous creeks.|16-MAY-23
37649|Pooranoo Metamorphics|Type section locality|Between Maroonah Homestead, Red Rock Well and East Paddock Hill on the southern edge of the Maroonah 100K sheet. The area contains a well-defined contact between the two main units (pelitic gneiss and metamorphosed feldspathic sandstone). Also present are layers of metamorphosed cobble and granule conglomerate and quartz sandstone, and calc-silicate gneiss and schist. The pelitic gneiss is accessible from a station track and N-S fenceline east of Maroonah Homestead. Good exposures of metamorphosed feldspathic sandstone are located 2.75km SSW of Red Rock Well on the east side of a dolerite dyke. Metamorphosed cobble and pebble conglomerate and quartz sandstone are well exposed at East Paddock Hill.|16-MAY-23
37649|Pooranoo Metamorphics|Extent|Confined to a southeasterly trending, fault-bounded terrane about 50 km wide in the northern Gascoyne Complex. The unit is in faulted contact with, or ?overlies, granites of the 1830-1780 Ma Moorarie Supersuite, which contrasts with older metamorphic units that are intruded by the supersuite.|16-MAY-23
37649|Pooranoo Metamorphics|Lithology|Pooranoo Metamorphics comprises two main units in roughly equal proportions: metamorphosed feldspathic sandstone and pelitic gneiss. The metamorphosed feldspathic sandstone is interlayered with minor pelitic rock and granule conglomerate. Graded bedding is preserved in places in the metamorphosed feldspathic sandstone. Pelitic gneiss and granofels are mainly non-migmatitic, but in the area around the Star of Mangaroon Mine, migmatitic pelitic gneiss is abundant. The migmatites include both diatexites and metatexites. Interlayered metamorphosed cobble and pebble conglomerate, granule sandstone, calc-silicate gneiss and schist, and amphibolite and actinolite schist are minor rock types.|16-MAY-23
37649|Pooranoo Metamorphics|Relationships and boundaries|Rocks of the Pooranoo Metamorphics are confined to a fault-bounded terrane. The metamorphics are separated from inliers of the c. 1770 Ma Gooche Gneiss by layer-parallel faults, and are intruded extensively by granites of the c. 1685-1620 Ma Durlacher Supersuite. The Pooranoo Metamorphics are unconformably overlain by sedimentary rocks of the Edmund Group (Bangemall Supergroup).|16-MAY-23
37649|Pooranoo Metamorphics|Age reasons|The youngest population of detrital zircons from a sample of pelitic gneiss from southeast of Maroonah Homestead provide a maximum depositional age of 1680 ? 13 Ma (GSWA 169094; D.R. Nelson in press, GSWA Record 2003/2). Two samples of metamorphosed feldspathic sandstone provide maximum ages of 1800 ? 4 Ma (GSWA 169091; D.R. Nelson in press, GSWA Record 2003/2) and 1808 ? 11 Ma (GSWA 169056; D.R. Nelson 2002, GSWA Record 2002/2). However, these rock types are interbedded with pelitic gneiss and, therefore, the whole succession must have a maximum age of 1680 ? 13 Ma. The metamorphic rocks are intruded by granites of the 1685-1620 Ma Durlacher Supersuite, thus providing a minimum depositional age.|16-MAY-23
37649|Pooranoo Metamorphics|References|Sheppard S., Martin D. M., & Thorne A. M. 2004. Mangaroon, W.A. Sheet 2050. Western Australia Geological Survey,1:100 000 Geological Series. **Martin D. M. 2004. Maroonah, W.A. Sheet 2051. Western Australia Geological Survey,1:100 000 Geological Series. **Nelson D. R. 2002. Compilation of geochronology data 2001. Western Australia Geological Survey, Record 2002/2. **Nelson D. R. in press. Compilation of geochronology data 2002. Western Australia Geological Survey, Record 2003/2.|16-MAY-23
29880|Port Smith Sand|Name source|Port Smith, latitude/longitude coordinates 18º 30' 16" S, 121º 47' 51" E, LaGrange 1:250,000 Topographical Sheet.|16-MAY-23
29880|Port Smith Sand|Geomorphic expression|In its contemporary mid to low tidal flat setting its geomorphic expression is as a plane to hummocky tidal flat surface that irself is plane to rippled surface to megarippled surface.|16-MAY-23
29880|Port Smith Sand|Type section locality|Coastal zone of Port Smith, latitude/longitude coordinates 18º 30' 51" S, 121º 48' 06" E, LaGrange 1:250,000 Topographical Sheet.|16-MAY-23
29880|Port Smith Sand|Description at type locality|FROM TOP TO:30 cm grey sand, bioturbated, scattered shell; 2 cm shell layer in grey sand; 75 cm grey, slightly shelly sand, structureless; 5 cm shell bed in grey sand; and 30 cm grey, slightly shelly sand, structureless.......BASE|16-MAY-23
29880|Port Smith Sand|Extent|The unit occurs along almost the entire length of the Canning Coast. Additionally, it has been intersected, underlying other Holocene units, in numerous cores throughout the region (Semeniuk 2008).|16-MAY-23
29880|Port Smith Sand|Thickness range|At type locality 1.42 m thick.  Additionally, where intersected in cores and trenches, the Formation has been recorded as 1-2 m thick. Geomorphic considerations, i.e., slope of the exposure of the Formation, suggests that it may be up to 3 m thick. Regionally, the unit is a ribbon, some hundreds of kilometres long, but only up to 10 km wide and 1-3 m thick.|16-MAY-23
29880|Port Smith Sand|Lithology|Mostly grey, bioturbated to structureless, fine and very fine sand and shelly sand ranging to coarse sand and shelly sand. Sand grains are quartz, or quartz and bioclasts, and locally ooids. Locally there are thin layers of oriented shell. Where reworked by tides into megaripples, there is a facies variant within the Formation, and sediments may consist of brown/tan/buff to grey layered and cross-laminated sand and shelly sand in addition to the dominant grey structureless to bioturbated sand.|16-MAY-23
29880|Port Smith Sand|Depositional environment|Sandy (mid to)  low tidal flat environments.|16-MAY-23
29880|Port Smith Sand|Fossils|Bivalves: Anadara crebricostata, Anomalocardia squamosa, Antigona cf. chemnitzii, Antigona chemnitzii, Arca avellana, Arca ventricosa, Asaphis violascens, Asaphis sp., Austriella sordida, Barbatia coma, Callista impar, Cardita cf. preissii, Dosinia incisa, Dosinia scalaris, Exotica assimilis, Hemidonax arafurensis, Irus sp., Mactra abbreviata cf. meretriciformis, Mactra westralis, Meropesta nicobarica, Paphies striata, Placamen gravescens, Saccostrea cucullata, Septifer bilocularis, Sunetta perexcavata, Tellina rostrata, Trachycardium flavum, Trisidos tortuosa, and an unidentified Mesodesmatid. Gastropods Amalda elongata, Astraea rotularia, Calthalotia strigata, Cerithidea reidi, Chicoreus permestus, Conus victoriae, Cronia aurantiaca, Cymatium vespaceum, Cypraea gracilis, Nerita undata, Phalium areola, Phasianella australis, Pyrene varians, Pythia cf. scarabaeus, Strombus campbelli, Syrinx aruanus, Tectus fenestratus, Trochus maculatus, and Turbo bruneus.|16-MAY-23
29880|Port Smith Sand|Relationships and boundaries|The unit is overlain, with gradational contact, by the Eighty Mile Beach Coquina, or Cable Beach Sand, or passes vertically upwards sharply or through a series of thin muddy interlayers over an interval of 50 cm, into the Sandfire Calcilutite.|16-MAY-23
29880|Port Smith Sand|Age reasons|Radiocarbon dating of shells within the Formation places it in the Holocene, viz., 3520 +/- 200 yrs BP, 3680 +/- 210 yrs BP, and 4320 +/-220 yrs BP.|16-MAY-23
29880|Port Smith Sand|Correlations|The formation is laterally equivalent to the Cable Beach Sand, the Eighty Mile Beach Coquina, and the Sandfire Calcilutite.|16-MAY-23
29880|Port Smith Sand|Comments|Grey bioturbated to structureless sand and shelly sand.|16-MAY-23
29880|Port Smith Sand|References|Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.|16-MAY-23
22722|Race Course Plains Coquina|Name source|Race Course Plains, on the Thangoo Station, latitude/longitude coordinates 18º 13' 06" S, 122º 14' 22" E, Lagrange 1:250,000 Topographical Sheet.|16-MAY-23
22722|Race Course Plains Coquina|Geomorphic expression|As cheniers and shelly sand ridges on tidal flats situated at mid to high tidal zones and supratidal zones.|16-MAY-23
22722|Race Course Plains Coquina|Type section locality|Quarry Pit on Thangoo Station, latitude/longitude coordinates 18º 13' 07" S, 122º 15' 31" E, Lagrange 1:250,000 Topographical Sheet.|16-MAY-23
22722|Race Course Plains Coquina|Description at type locality|150 cm shell gravel, layered shell hash and sand; sharp contact with underlying Sandfire Calcilutite.|16-MAY-23
22722|Race Course Plains Coquina|Extent|The unit is widespread along the Canning Coast as a semi-continuous to scattered shoe-string deposit.|16-MAY-23
22722|Race Course Plains Coquina|Thickness range|At type locality 1.50 m thick.  Additionally, where intersected in cores and trenches, the Formation has been recorded as 2 m thick. Regionally, the unit will appear as discontinuous shoe-string deposits, individually, some tens of metres to several kilometres long, but only up to tens of metres wide and 2 m thick.|16-MAY-23
22722|Race Course Plains Coquina|Lithology|In general, light-coloured, shell gravel, shelly sand, and some sand that is variable in structure from bedded, to laminated, to cross-laminated, to locally bioturbated, to structureless. It is biostratigraphically distinct in that it is dominated by shells of Anadara, Terebralia, Saccostrea cucullata, and Cerithidea.|16-MAY-23
22722|Race Course Plains Coquina|Depositional environment|Storm and wave deposits on high-tidal to supra-tidal flats.|16-MAY-23
22722|Race Course Plains Coquina|Fossils|The diversity of molluscan shells in the Formation is variable and depends on location, and on whether storm/wave processes have been dominant in accumulating the shells or whether Indigenous people have been dominant in generating middens, or both processes have occurred.  For instance, cheniers may be dominated by bivalves deposited by storms/waves, with lesser input by Indigenous people, and are composed of bivalves Anadara granosa, Anadara crebricostata, Anadara secticostata, Asaphis violascens, Dosinia deshayesii, Dosinia incisa, Gafrarium dispar, Mactra incarnata, Paphia crassisula, and Saccostrea cucullata, and gastropods Cantharus cf. erythrostoma, Cerithidea anticipata, Cerithidea cf. cingulata, Cerithidea cingulata, Chicoreus cornucervi, Cymatium waterhousei, Epitonium imperialis, Littoraria cf. cingulata, Nassarius dorsatus, Nerita squamulata, Neritina cf. violacea, Phalium areola, Polinices sp., Stramonita javanica, Terebralia palustris, Turbo laminiferus, and unidentified Marginellids, cheniers may contain shells accumulated by storms/waves, with some input by Indigenous people contributing bivalves Anadara granosa, Dosinia incisa, and Tellina cf. piratica, cheniers may be dominated by shells deposited by storms/waves, again with Indigenous people contributing bivalves Anadara granosa, Dosinia incisa, and Saccostrea cucullata, or cheniers may be dominated by entire shells and fragments of Saccostrea cucullata that have been transported and deposited by storms/waves.|16-MAY-23
22722|Race Course Plains Coquina|Diastems or hiatuses|Hiatuses are present within the stratigraphic pile of the Race Course Plains Coquina separating changes in shell composition, and often marked by thin humic layers, and zones of bioturbation.|16-MAY-23
22722|Race Course Plains Coquina|Relationships and boundaries|The unit passes downwards, with sharp contact, into the underlying Sandfire Calcilutite. It interfingers locally with Sandfire Calcilutite on its margins.|16-MAY-23
22722|Race Course Plains Coquina|Age reasons|Radiocarbon dating of shells within the Formation places it in the Holocene, viz., 1285 +/- 150 yrs BP, 2290 +/-180 yrs BP, 1510 +/- 210 yrs BP, 2350 +/- 225 yrs BP, 3625 +/- 260 yrs BP.|16-MAY-23
22722|Race Course Plains Coquina|Correlations|In its contemporary environment, and its lithosome, the Formation is equivalent to the Sandfire Calcilutite, the Cable Beach Sand, the Eight Mile Beach Coquina, and the Shoonta Hill Sand.|16-MAY-23
22722|Race Course Plains Coquina|Comments|Shell gravel to shelly sand as a mid tidal to supratidal shoe-string deposit.|16-MAY-23
22722|Race Course Plains Coquina|References|Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.|16-MAY-23
15929|Red Bull Member|Name source|Red Bull Bore, Napier Range. The use of the geographic name Red Bull, a common geographic name in Australia, reflects the scarcity of place names in the northern Canning Basin.|16-MAY-23
15929|Red Bull Member|Unit history|Informally named Red Bull Member by Read (1973b).|16-MAY-23
15929|Red Bull Member|Type section locality|Partial section (top not exposed) approximately five km southwest of Red Bull Bore, Napier Range area (N 2840000 yds; E 244500 yds to N 2840300 yds; E243500 yds). A second reference section (base and top not exposed) is located immediately north of Windjana Gorge, Napier Range (N 2810200 yds; E 27900 yds to N 281020 yds; E 277700 yds); for detailed stratigraphic section see Read (1973b; Fig. 5).|16-MAY-23
15929|Red Bull Member|Thickness range|Maximum thicknesses (270 m) occur in Napier Range - east Oscar Plateau area. Thins rapidly to south and west; it is approximately 100 m thick in the Geikie Range, 6 m in the Oscar Range and less than 15 m thick in the Pillara Range.|16-MAY-23
15929|Red Bull Member|Lithology|Interbedded terrigenous sediments (sandstone, siltstone and shale) and limestone (stromatoporoid limestone, pellet limestone).|16-MAY-23
15929|Red Bull Member|Relationships and boundaries|Conformably overlies Big Spring Member and is conformably overlain by the Menyous Limestone Member.  The top is placed at the top of the uppermost terrigenous horizon below the Menyous Limestone Member, which lacks terrigenous interbeds.|16-MAY-23
15929|Red Bull Member|Age reasons|Givetian to lowermost Frasnian.|16-MAY-23
15929|Red Bull Member|Proposed publication|Bull. Can. Petrol. Geol. V.21, p.344-394|16-MAY-23
15929|Red Bull Member|Name first published by|Logan B.W., Semeniuk V., 1976.|16-MAY-23
15980|Redbank Yard Formation|Name source|Redbank Yard on Wolf Creek, at 19o04'00"S, 127o47'00"E, Billiluna 1:250 000 Sheet area, WA.|16-MAY-23
15980|Redbank Yard Formation|Unit history|Outcrops of Redbank Yard Conglomerate were previously mapped as part of the Kearney Beds (Casey & Wells, 1964).|16-MAY-23
15980|Redbank Yard Formation|Type section locality|15 km west-northwest of Redbank Yard. Here a sequence 330 m thick, dipping 20o south, consists of 200 m of polymictic conglomerate overlain by 130 m of medium to very coarse sublithic arenite.|16-MAY-23
15980|Redbank Yard Formation|Extent|Northwest corner of the Billiluna 1:250 000 Sheet area.|16-MAY-23
15980|Redbank Yard Formation|Thickness range|At least 330 m (maximum exposed, in type section).|16-MAY-23
15980|Redbank Yard Formation|Lithology|Conglomerate, sublithic arenite, minor dolomite.|16-MAY-23
15980|Redbank Yard Formation|Relationships and boundaries|Stratigraphic equivalent of the Moonlight Valley Tillite in the Gordon Downs Sheet area (Gemuts & Smith, 1968). Inferred to be unconformable on Wade Creek Sandstone, which it overlies to the west, and to be conformably overlain by Ranford Formation to the east. Hence it is a constituent formation of the Duerdin Group, East Kimberley succession (Gemuts & Smith, 1968; Dow & Gemuts, 1969). |16-MAY-23
15980|Redbank Yard Formation|Age reasons|Adelaidean|16-MAY-23
15980|Redbank Yard Formation|Defn approved by|taken from xerox copy of approved definitions from WA Sub-Committee acc.to Dr Blake|16-MAY-23
15980|Redbank Yard Formation|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
15983|Redcliff Pound Group|Name source|Redcliff Pound, WA (21deg 35'S, 128deg 45'E)|16-MAY-23
15983|Redcliff Pound Group|Name source|Redcliff Pound, 21o35'S, 128o45'E. Stansmore 1:250 000 Sheet area, NT.|16-MAY-23
15983|Redcliff Pound Group|Unit history|The term Redcliff Pound Group was first used by Blake et al. (1973), and defined and described in more detail by Blake et al. (1979). The group was originally part of the Birrindudu Basin succession, but later moved to the Centralian Superbasin by Tyler and Hocking (2001). This part of the Centralian Superbasin was given the name Murraba Basin by Tyler (2005) and Grey et al. (2005). As originally conceived, the group comprised the correlative Lewis Range, Muriel Range and Munyu Sandstones at the base, overlain successively by the Murraba Formation and Erica Sandstone. The original correlations to the Amadeus Basin suggested by Blake et al. (1979), if correct, would restrict the original Redcliff Pound Group to Supersequence 1 of the Centralian Superbasin (supersequence terminology after Walter et al., 1995). The correlation of this succession to the rest of the Centralian Superbasin was substantially revised by Haines and Allen (2016, in prep.), who assigned the Lewis Range, Muriel Range and Munyu Sandstones to lower Supersequence 1, and the Murraba Formation and Erica Sandstone to Supersequence 3-4. The base of the exposed Murraba Formation is inferred to be an unconformity over a mostly concealed succession (inferred from regolith) likely belonging to upper Supersequence 1 and Supersequence 2. The original Redcliff Pound Group no longer fits the lithostratigraphic definition of a group ("a succession of two or more contiguous or associated formations with significant and diagnostic lithologic properties in common") as it contains significant unconformities and hiatuses in deposition, and was deposited episodically over much of the Neoproterozoic. The definition of the Redcliff Pound Group is herein revised to include only the conformable Murraba Formation and Erica Sandstone, and exclude all lower units of the Murraba Basin. It includes all of the units exposed in the Redcliff Pound area where the name was derived.|16-MAY-23
15983|Redcliff Pound Group|Constituents|Lewis Range Sandstone, Muriel Range Sandstone, Murraba Formation, Erica Sandstone.|16-MAY-23
15983|Redcliff Pound Group|Constituents|Murraba Formation and Erica Sandstone.|16-MAY-23
15983|Redcliff Pound Group|Geomorphic expression|Low strike ridges and strike valleys.|16-MAY-23
15983|Redcliff Pound Group|Type section locality|Not required for groups. Type localities of constituent units are near Redcliff Pound (Murraba Formation) and Erica Range (Erica Sandstone), as nominated by Blake et al. (1979). The Redcliff Pound area (centred around 21º 35'S, 128º 45'E) forms a useful Reference Locality for the group as a whole.|16-MAY-23
15983|Redcliff Pound Group|Extent|Billiluna, Lucas and Stansmore 1:250 000 Sheet areas, WA, and The Granites 1:250 000 Sheet area, NT.|16-MAY-23
15983|Redcliff Pound Group|Extent|Outcrops are restricted to the eastern STANSMORE and southeastern LUCAS 1:250 000 map sheet areas in WA, and western HIGHLAND ROCKS in the NT.|16-MAY-23
15983|Redcliff Pound Group|Thickness range|Maximum exposed is about 1000 m, at Redcliff Pound in the southeast part of the Stansmore 1:250 000 Sheet area. Maximum aggregate thickness of the constituent formation is about 2000 m.|16-MAY-23
15983|Redcliff Pound Group|Thickness range|Not well constrained due to poor outcrop; c. 1500 m in the Redcliff Pound area (Blake et al., 1979).|16-MAY-23
15983|Redcliff Pound Group|Lithology|Murraba Formation: Sandstone, siltstone, and minor carbonate and conglomerate deposited in shallow marine to deltaic environments. Erica Sandstone: predominantly sandstone deposited in deltaic, fluvial and eolian environments.|16-MAY-23
15983|Redcliff Pound Group|Lithology|Lithologic affinities of constituent formations: All consist mainly of two types of sandstone - sublithic and quartz arenite.|16-MAY-23
15983|Redcliff Pound Group|Depositional environment|Changes up-section from shallow marine, to deltaic and fluvial, with eolian facies near the top.|16-MAY-23
15983|Redcliff Pound Group|Fossils|Arumberia and probable tubular body fossils are present in the lower part of the group.|16-MAY-23
15983|Redcliff Pound Group|Diastems or hiatuses|None observed.|16-MAY-23
15983|Redcliff Pound Group|Relationships and boundaries|Unconformable over mostly concealed unnamed units (likely Supersequence 1-2 of Centralian Superbasin). Top (Erica Sandstone) is youngest unit of the Murraba Basin and is unconformably overlain by Paleozoic outliers of the Canning Basin in WA and the Antrim Plateau Volcanics in NT.|16-MAY-23
15983|Redcliff Pound Group|Relationships and boundaries|Unconformable on Archean or Lower Proterozoic Tanami Complex, on probably Lower Proterozoic Lewis Granite and unnamed granite, and on Carpentarian Birrindudu Group. Overlies, possibly conformably, Munyu Sandstone. Overlain possibly conformably by Hidden Basin Beds and unconformably by Palaeozoic units.|16-MAY-23
15983|Redcliff Pound Group|Identifying features|More resistant than underlying succession presumably due to dominant sandstone lithologies in Redcliff Pound Group. Underlying succession inferred to be mainly diamictite, siltstone and carbonates, which are either absent (diamictite) or subordinate in the Redcliff Pound Group.|16-MAY-23
15983|Redcliff Pound Group|Structure and Metamorphism|Gently to tightly folded and faulted, but not metamorphosed.|16-MAY-23
15983|Redcliff Pound Group|Age reasons|Probably Adelaidean.|16-MAY-23
15983|Redcliff Pound Group|Age reasons|Inferred to be mainly of Ediacaran age, but the age could potentially extend from the late Cyrogenian to early Cambrian. The age is inferred from regional correlations to the Amadeus and Georgina Basins. The problematical fossil Arumberia and probable tubular body fossils, both present in the late Ediacaran of the Amadeus and Georgina Basins, are present in the middle of the group. The age of the top is older than the c. 510 Ma Antrim Plateau Volcanics, which are inferred to locally overlie the Erica Sandstone in the NT (Ahmed, 2013).|16-MAY-23
15983|Redcliff Pound Group|Correlations|Regionally correlated with Supersequence 3 and 4 of the Centralian Superbasin (supersequence scheme of Walter et al., 1995).|16-MAY-23
15983|Redcliff Pound Group|Geophysical Expression|Not distinguished on geophysical datasets.|16-MAY-23
15983|Redcliff Pound Group|Defn author|Peter Haines and Heidi Allen (GSWA); originally Blake et al. (1979). 23-JAN-2017. Approved by Milo Barham 27-JAN-2017.|16-MAY-23
15983|Redcliff Pound Group|Defn author|D. H. Blake, probably reserved 1973. Definition likely written before 1978.|16-MAY-23
15983|Redcliff Pound Group|References|Ahmad, M 2013, Chapter 25: Murraba Basin, in Geology and mineral resources of the Northern Territory compiled by M Ahmad and TJ Munson: Northern Territory Geological Survey, Darwin, Northern Territory, Special Publication 5, p. 25.1-25.3. **Blake, DH, Hodgson, IM and Muhling, PC 1973, Geology of The Granites and Precambrian parts of Billiluna, Lucas and Stansmore 1:250 000 sheet areas, Northern Territory and Western Australia: Bureau of Mineral Resources, Geology and Geophysics, Record 1973/171, 96p. **Blake, DH, Hodgson, LM and Muhling, PC 1979, Geology of the Granites-Tanami Region, Northern Territory And Western Australia: Bureau of Mineral Resources, Australia, Bulletin 197, 91p. **Grey, K, Hocking, RM, Stevens, MK, Bagas, L, Carlsen, GM, Irimies, F, Pirajno, F, Haines, PW and Apak, SN 2005, Lithostratigraphic nomenclature of the Officer Basin and correlative parts of the Paterson Orogen, Western Australia: Geological Survey of Western Australia, Report 93, 89p. **Haines, PW and Allen HJ 2016, The Murraba Basin: another piece of the Centralian Superbasin jigsaw puzzle falls into place, in GSWA 2016 extended abstracts: promoting the prospectivity of Western Australia: Geological Survey of Western Australia, Record 2016/2, p. 31-35. **Haines, PW and Allen HJ in prep., Geological reconnaissance of the southern Murraba Basin, Western Australia: revised stratigraphic position within the Centralian Superbasin and hydrocarbon potential: Geological Survey of Western Australia, Record. **Tyler, IM 2005, Australia: Proterozoic, in Encyclopedia of Geology edited by RC Selley, LRM Cocks and IR Plimer: Elsevier, Oxford, UK, Volume 1, p. 208-221. **Tyler, IM and Hocking, RM 2001, A revision of the tectonic units of Western Australia: Geological Survey of Western Australia, 2000-01 Annual Review, p. 33-44. **Walter, MR, Veevers, JJ, Calver, CR and Grey, K 1995, Neoproterozoic stratigraphy of the Centralian Superbasin, Australia: Precambrian Research, v. 73, p. 173-195.|16-MAY-23
15983|Redcliff Pound Group|Defn approved by|Taken from xerox copy of approved definitions sent by WA Sub-Committee. Likely approved in 1978  but maybe as early as 1975.|16-MAY-23
30278|Ruby Plains Group|Name source|Ruby Plains 1:100 000 map sheet (4460) and homestead (at GR CE565432), Gordon Downs 1:250 000 Sheet area.|16-MAY-23
30278|Ruby Plains Group|Unit history|previously mapped as part of the Osmond Range succession (Dow & Gemuts 1969) and Wade Creek Sandstone (Blake et al. 1979), which are Mesoproterozoic.|16-MAY-23
30278|Ruby Plains Group|Constituents|from bottom to top, Mount Kinahan Sandstone, Eliot Range Dolomite, and Illjarra Sandstone.|16-MAY-23
30278|Ruby Plains Group|Geomorphic expression|ridges, cuestas and valleys.|16-MAY-23
30278|Ruby Plains Group|Type section locality|across prominent ridges, from base at GR CE703578  to top at GR CE718570, Halls Creek 1:100 000 Sheet area, where all three constituent formations of the group are exposed, unconformably overlying Olympio Formation to west and overlain by Duerdin Group to east.|16-MAY-23
30278|Ruby Plains Group|Extent|Ruby Plains, Halls Creek and Antrim 1:100 000 Sheet areas, Gordon Downs 1:250 000 Sheet area, and Dixon 1:100 000 Sheet area, Dixon Range 1:250 000 Sheet area; extends southwest into, but not distinguished in, Billiluna and Mount Bannerman 1:250 000 Sheet areas.|16-MAY-23
30278|Ruby Plains Group|Thickness range|from about 500 m to more than 1000 m.|16-MAY-23
30278|Ruby Plains Group|Lithology|sedimentary rocks, dominated by quartz sandstone, dolomite, and lithic sandstone.|16-MAY-23
30278|Ruby Plains Group|Depositional environment|marine shelf?|16-MAY-23
30278|Ruby Plains Group|Relationships and boundaries|Ruby Plains Group is unconformable on Olympio Formation of Palaeoproterozoic Halls Creek Group and on undated granite, and is overlain unconformably by Neoproterozoic Duerdin Group. Stratigraphic contacts between the three formations of the group are conformable or disconformable.|16-MAY-23
30278|Ruby Plains Group|Age reasons|Neoproterozoic - Tonian or Cryogenian.|16-MAY-23
30278|Ruby Plains Group|Correlations|Supersequence 1 of Centralian Superbasin of Walter et al. (1995).|16-MAY-23
30278|Ruby Plains Group|References|Blake, D.H., Hodgson, I.M. & Muhling, P.C., 1979. Geology of The Granites-Tanami region, Northern Territory and Western Australia. Bureau of Mineral Resources, Australia, Bulletin 197. **Blake, D.H., Tyler, I.M. & Sheppard, S., 1997. Geology of the Ruby Plains 1:100 000 Sheet area (4460), Western Australia,. Australian Geological Survey Organisation, Canberra. **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.**Walter, M.J., Veevers, J.J., Calver, C.R. & Grey, K., 1995. Late Proterozoic stratigraphy of the Centralian Superbasin, Australia. Precambrian Research, 73, 173-195.|16-MAY-23
27300|Rushall Slate|Name source|Rushall mine (Lat. 20deg 51' S., Long. 117deg 50' E.) Roebourne 1:250 000 Sheet area.|16-MAY-23
27300|Rushall Slate|Name source|Rushall mine (20o51'S, 117o50'E) Roebourne 1:250 000 Sheet area.|16-MAY-23
27300|Rushall Slate|Unit history|Published as Rushall Slate of the Whim Creek Group (Hickman, 1981, 1983). Following recognition of an unconformity between the Whim Creek and Bookingarra Groups, the Rushall Slate was assigned to the Bookingarra Group by Pike and Cas (2002). Redefined as a formation of the Croydon Group by Van Kranendonk et al. (2006) based on interpreted correlations between the Whim Creek greenstone belt and the Mallina Basin. Re-assigned to the Bookingarra Group by Hickman (2016) based on geochronological and structural evidence against correlation with units of the Mallina Basin.|16-MAY-23
27300|Rushall Slate|Unit history|Whim Creek slate (3) informally used. The name 'Whim Creek' is applied to the Whim Creek Group|16-MAY-23
27300|Rushall Slate|Geomorphic expression|The Rushall Slate outcrops in valleys and on low-lying ground.|16-MAY-23
27300|Rushall Slate|Type section locality|Whim Creek mine area (Lat. 20deg 52' S., Long. 117deg 50' E.) Roebourne 1:250 000 sheet area.|16-MAY-23
27300|Rushall Slate|Type section locality|Whim Creek mine (20o52'S, 117o50'E).|16-MAY-23
27300|Rushall Slate|Description at type locality|Predominantly grey slate (metamorphosed shale) with graded bedding indicating deposition from turbidity currents. Locally contains thin units of felsic tuff and chert (Marston, 1979; Barley, 1987).|16-MAY-23
27300|Rushall Slate|Extent|The Rushall Slate is confined to the Whim Creek greenstone belt, within which it is restricted to small outcrops between Mount Negri (Lat. 20deg 47' S., Long. 117deg 51' E.) and Good Luck Well (Lat. 20deg 57' S., Long. 117deg 41' E.).|16-MAY-23
27300|Rushall Slate|Extent|30 km2 around Whim Creek centre and also immediately southwest of Mons Cupri (20o53'S, 117o48'E) and near Good Luck Well (20o56'S, 117o41'E).|16-MAY-23
27300|Rushall Slate|General description|Several lines of evidence indicate that deposition of the Cistern Formation and Rushall Slate was restricted to small sections of the Whim Creek greenstone belt. Thin units of felsic tuff within the Rushall Slate are consistent with deposition during felsic volcanism of the Cistern Formation; however, the Rushall Slate was deposited farther away from the felsic volcanic centres.|16-MAY-23
27300|Rushall Slate|Thickness range|Up to 200 m thick (Hickman, 1983). The stratigraphic thickness of the Rushall Slate varies up to 200 m. In some sections it is absent between the Cistern Formation and the Louden Volcanics.|16-MAY-23
27300|Rushall Slate|Thickness range|200 m.|16-MAY-23
27300|Rushall Slate|Lithology|Grey slate and phyllite, very subordinate flows of andesite and dacite, local beds of quartzite and thin lenses of felsic tuff. Basal conglomerate (2m) south of Whim Creek centre. At Mons Cupri the formation includes an andesite unit (informally referred to as the Comstock andesite by (3).|16-MAY-23
27300|Rushall Slate|Lithology|Grey slate and phyllite, very subordinate flows of andesite and dacite; local beds of quartzite and thin lenses of felsic tuff. At Mons Cupri (Lat. 20deg 53' S., Long. 117deg 48' E.) the Rushall Slate includes the Comstock Member (basalt and dolerite).|16-MAY-23
27300|Rushall Slate|Depositional environment|The regional setting was a zone of continental rifting and strike-slip faulting near the northwest margin of the Pilbara Craton. The Rushall Slate and the Cistern Formation were deposited within the Whim Creek greenstone belt close to c. 2950 Ma volcanic centres (Barley, 1987). These centres were located above intrusions of the Sisters Supersuite. The Cistern Formation comprises proximal facies including volcaniclastic breccia and conglomerate and sandstone whereas the Rushall Slate was deposited in slightly deeper water in one or more adjacent basins, possibly including caldera lakes with hydrothermal activity. Low Boron contents indicate lacustrine rather than marine deposition. Detrital zircon ages in metasandstone of the Cistern Formation (Nelson, 2000) indicate derivation from 3006¿2982 Ma felsic igneous rocks such as the Red Hill Volcanics (Whim Creek Group) or Maitland River Supersuite. Less common younger detrital zircons (2980¿2960 Ma) in the Cistern Formation suggest an additional source not yet identified in the northwest Pilbara Craton.|16-MAY-23
27300|Rushall Slate|Relationships and boundaries|Top formation of the Whim Creek Group (1) Unconformably overlain by the Negri Volcanics; (2) at Mount Negri and by the rocks correlated with the Louden Volcanics (new name) at Good Luck Well.|16-MAY-23
27300|Rushall Slate|Relationships and boundaries|Conformably overlies the Cistern Formation in some areas, although regionally the Cistern Formation and Rushall Slate are vertically and laterally transitional. Locally unconformably overlain by both the Louden Volcanics and the Mount Negri Volcanics. Constituents include: Comstock Member (basalt and dolerite). Parent: Bookingarra Group.|16-MAY-23
27300|Rushall Slate|Identifying features|Compared to shale units in other formations of the Bookingarra Group, the Rushall Slate is an exceptionally thick metamorphosed shale containing a strong slaty cleavage.|16-MAY-23
27300|Rushall Slate|Structure and Metamorphism|Local thrusting and folding of the Rushall Slate and Cistern Formation were reported by Krapez and Eisenlohr (1998). These structures might be related to folding of the c. 2940 Ma Whim Creek Anticline rather than belonging to a separate phase of deformation. The metamorphic grade of the Rushall Slate is prehnite-pumpellyite to lower greenschist facies.|16-MAY-23
27300|Rushall Slate|Age reasons|Late Archaean.|16-MAY-23
27300|Rushall Slate|Age reasons|Pb isotope data from syn-depositional VMS mineralization in the Rushall Slate were interpreted by Huston et al. (2002) to indicate an age of c. 2948 Ma. The maximum depositional age of the Rushall Slate is c. 2955 Ma, which is the age of the unconformity that separates the Bookingarra Group from the underlying Whim Creek Group (Pike and Cas, 2002; Hickman, 2016). Detrital zircon U-Pb dating establishes that the underlying Cistern Formation is younger than 2964 +/- 6 Ma (Huston et al., 2002) and stratiform Pb-Zn mineralization within the Cistern Formation, interpreted to be syndepositional, has been dated at 2950 Ma (Richards and Blockley, 1984; Richards, 1986). The minimum age of the Rushall Slate is constrained by a date of 2943 +/- 7 Ma on the Kialrah Rhyolite (Nelson, 1998) which overlies and intrudes the overlying Louden Volcanics.|16-MAY-23
27300|Rushall Slate|Correlations|The Rushall Slate is partly laterally equivalent to the Cistern Formation, both units containing lateral facies variations.|16-MAY-23
27300|Rushall Slate|Alteration and Mineralisation|Varying degrees of silicification, epidote¿chlorite alteration, and carbonate alteration affect the formation. The Rushall Slate contains economically important copper mineralization at Whim Creek (reviewed by Hickman, 2016). The Whim Creek Cu-Zn VMS deposit is stratabound within a particular stratigraphic horizon of the Rushall Slate. Primary minerals are pyrite, pyrrhotite, chalcopyrite, and sphalerite with minor galena, magnetite, and arsenopyrite, whereas supergene alteration minerals are chalcocite, covellite, and malachite, with minor azurite and chrysocolla (Collins and Marshall, 1999). Between 1891 and 2009 total production from the Whim Creek mine was approximately 46 500 t Cu (Hickman, 2016).|16-MAY-23
27300|Rushall Slate|Geophysical Expression|Low TMI anomalies correspond to outcrops of metamorphosed shale.|16-MAY-23
27300|Rushall Slate|Geochemistry|Two samples of the Rushall Slate from Whim Creek were analysed by McLennan et al. (1983). REE patterns show LREE enrichment and little or no Eu depletion (Eu/Eu* = 0.86-0.90). McLennan et al. (1983) interpreted these data to indicate a detrital source without large negative Eu anomalies (e.g. TTG or compositionally similar felsic volcanics). Elevated Ni and Cr contents relative to average shales suggest involvement of mafic sources. Low Boron contents indicate lacustrine rather than marine deposition.|16-MAY-23
27300|Rushall Slate|Defn author|A.H. Hickman, Geological Survey of Western Australia|16-MAY-23
27300|Rushall Slate|Proposed publication|Name published by Hickman (1980) and used in many later publications to refer to a formation of either the Whim Creek Group or the Bookingarra Group. Redefinition published in Hickman, AH, 2016, Northwest Pilbara Craton: a record of 450 million years in the growth of Archean continental crust: Geological Survey of Western Australia, Report 160, 104p.|16-MAY-23
27300|Rushall Slate|Proposed publication|Geology of the Pilbara Block and its environs, GSWA Bull.|16-MAY-23
27300|Rushall Slate|References|Barley, ME 1987, The Archaean Whim Creek Belt, an ensialic fault-bounded basin in the Pilbara Block, Australia: Precambrian Research, v. 37, p. 199-215. **Collins and Collins, PLF and Marshall, AE 1999, Volcanic-hosted massive sulfide deposits at Whundo-Yannery in the Sholl belt, in Lead, zinc and silver deposits of Western Australia by KM Ferguson: Geological Survey of Western Australia, Mineral Resources Bulletin 15, p. 73-79. **Hickman, AH 1980, Lithological and Stratigraphic Interpretation of the Pilbara Block (1:1 000 000 scale): Geological Survey of Western Australia, Bulletin 127, Plate 1. **Hickman, AH 1981, Crustal evolution of the Pilbara Block, in Archaean Geology, Second International Archaean Symposium Perth 1980 edited by JE Glover and DI Groves: Geological Society of Australia, Special Publication 7, Perth, Australia, p. 57-69.  **Hickman, AH 1983, Geology of the Pilbara Block and its environs: Geological Survey of Western Australia, Bulletin 127, 268p.**Hickman, AH 2016, Northwest Pilbara Craton: a record of 450 million years in the growth of Archean continental crust: Geological Survey of Western Australia, Report 160, 104p. **Huston, DL, Sun, S -S, Blewett, R, Hickman, A, Van Kranendonk, M, Phillips, D, Baker, D, and Brauhart, C 2002, The timing of mineralisation in the Archaean Pilbara Craton, Western Australia: Economic Geology, v. 97, p. 733-755. **Krapez, B and Eisenlohr, B 1998, Tectonic settings of Archaean (3325¿2775 Ma) crustal-supracrustal belts in the West Pilbara Block: Precambrian Research, v. 88, p. 173-205. **Marston, RJ 1979, Copper mineralisation in Western Australia: Geological Survey of Western Australia, Mineral Resources Bulletin 13 208p. **McLennan, SM, Taylor, SR and Eriksson, KA 1983, Geochemistry of Archean shales from the Pilbara Supergroup, Western Australia: Geochimica et Cosmochimica Acta, v. 47, p. 1211-1222. **Nelson, DR 1998, 144261: rhyolite, Bradley Well, Geochronology Record 272: Geological Survey of Western Australia, 4p. **Nelson, DR 2000m, 142949: metasandstone, Whim Creek, Geochronology Record 299: Geological Survey of Western Australia, 4p. **  Pike, G and Cas, RAF 2002, Stratigraphic evolution of Archaean volcanic rock-dominated rift basins from the Whim Creek Belt, west Pilbara Craton, Western Australia, in Precambrian Sedimentary Environments: A Modern Approach to Depositional Systems edited by W Altermann and P Corcoran: International Association of Sedimentologists, Special Publication 33, Blackwell Science, Oxford, UK, p. 213-234. **Richards, JR and Blockley, JG 1984, The base of the Fortescue Group, Western Australia: Further galena lead isotopic evidence of its age: Australian Journal of Earth Sciences, v. 31, p. 257-268. **Richards, JR, 1986, Lead isotope signatures: Further examination of comparisons between South Africa and Western Australia: Geological Society of South Africa Transactions, v. 89, p. 285-304.|16-MAY-23
27300|Rushall Slate|Proposer|Hickman A.H.|16-MAY-23
16559|Salgash Subgroup|Name source|Salgash mining centre (Military Grid 263 341). Mable Bar 1:250 000 Sheet area.|16-MAY-23
16559|Salgash Subgroup|Type section locality|The type area is between Camel Creek and Salgash. The Subgroup is also well exposed along Chinaman Creek, west of Marble Bar and in the North Pole Dome, southwest of North Pole.|16-MAY-23
16559|Salgash Subgroup|Extent|The Salgash Subgroup is distributed over most of the greenstone areas of the Marble Bar Sheet, including the Warrawoona, Coongan and Pilganoora Synclines, the North Shaw, Western Shaw, Marble Bar, Kelly Belts, and the North Pole Dome.|16-MAY-23
16559|Salgash Subgroup|Thickness range|The unit has variable thickness between 1-8 km due partly to variation in original depositonal thickness and partly to tectonic thinning.|16-MAY-23
16559|Salgash Subgroup|Lithology|Approx. 2 km lower basalt lavas, commonly pillowed with intercalated chert horizons, 1 km dacite lava tuff and agglomerate with local sedimentary rocks (Panorama Formation and Kelly Formation), and about 0.5-1 km of upper basalt lavas, commonly pillowed with intercalated chert horizons, and minor felsic volcanic and ultramafic units.|16-MAY-23
16559|Salgash Subgroup|Relationships and boundaries|Conformably overlies the Duffer Volcanics and underlies the Wyman Formation. The upper margin is locally unconformable, such as in the Kelly Belt. The Marble Bar Chert lies at or near the base of the Subgroup in the Marble Bar Belt and the Warrawoona Syncline. The informally named "Chinaman Pool chert", occurring near Marble Bar, locally forms the base of the Subgroup.|16-MAY-23
16559|Salgash Subgroup|Age reasons|Archaean because of tectonic style and intrusion and Archaean granitic rocks.|16-MAY-23
16559|Salgash Subgroup|Defn author|Lipple S.L., 1975|16-MAY-23
16559|Salgash Subgroup|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
16559|Salgash Subgroup|Name first published by|Lipple S.L., 1975|16-MAY-23
79800|Samphire Marsh Member|Name source|Samphire Marsh 1, petroleum exploration well where the original Nambeet Formation type section is designated. Location: Lat: -19.520 S, Long: 121.183 E.|16-MAY-23
79800|Samphire Marsh Member|Unit history|This member has previously just been included in the overall definition of the Nambeet Formation.|16-MAY-23
79800|Samphire Marsh Member|Constituents|N/A|16-MAY-23
79800|Samphire Marsh Member|Geomorphic expression|The Samphire Marsh Member has been recorded only in the subsurface.|16-MAY-23
79800|Samphire Marsh Member|Type section locality|Olympic 1 well (-18deg17'57.60"S, 122deg38'23.40"E) between 1170.00 and 1383.57 m depth (213.57 m thick; continuous drill core). Drill core archived in Geological Survey of Western Australia Perth Core Library.|16-MAY-23
79800|Samphire Marsh Member|Extent|The Samphire Marsh Member is recorded across the central-western parts of the Canning Basin, although confident identification is restricted to locations where the Nambeet Formation has been intersected by drilling. It has been drilled on the following tectonic sub-divisions: Broome Platform, Willara Sub-basin, Barbwire Terrace, Munro Arch, and Kidson Sub-basin and recently identified in the Waukarlycarly Embayment.|16-MAY-23
79800|Samphire Marsh Member|General description|The Samphire Marsh Member is identified as a thick carbonate-mudstone sequence, overlying a siliciclastic package and transitioning into carbonate-dominated sediments of the overlying Willara Formation.|16-MAY-23
79800|Samphire Marsh Member|Thickness range|~ 213.57 m thick at the type locality, with a transitional upper contact. Whole section recovered. Thickness of the Samphire Marsh Member varies from as thin as an estimated ~50 m to almost 640 m in Samphire Marsh 1.|16-MAY-23
79800|Samphire Marsh Member|Lithology|Samphire Marsh Member consists of interbedded and nodular carbonate-mudstone sequences. Limestone bed textures range from grainstone to lime mudstone and nodule textures vary from wackestone to lime mudstone. Transitions between interbedded and nodular sections and coarser to finer carbonate fabrics are gradational throughout the sequence. Mudstones in both interbedded and nodular sections are calcareous. X-ray diffraction indicates a quartz content of 4.1 - 29.8%, a total clay content between 3.8 - 43.8 %, a calcite content of between 9.9 - 85.9 %, and a dolomite content between 0 - 12.2 % across the Samphire Marsh Member at the type section.|16-MAY-23
79800|Samphire Marsh Member|Depositional environment|At the type section, the Samphire Marsh Member was deposited on an epeiric platform or very low-angle epeiric ramp environment (restricted inner-ramp to outer-ramp settings).|16-MAY-23
79800|Samphire Marsh Member|Fossils|Conodonts, trilobites, graptolites, brachiopods, bivalves, nautiloids sensus lato, echinoderms. Minor taxa include gastropods, macheridians, bryozoans, scolecodonts, and the incertae sedis cyanobacteria, Nuia.|16-MAY-23
79800|Samphire Marsh Member|Diastems or hiatuses|Bored hardgrounds are observed in the lower-middle parts of the member at the type locality. The lower contact of the member with the underlying Fly Flat Member is represented by an abrupt sequence boundary which may represent a disconformity at this locality.|16-MAY-23
79800|Samphire Marsh Member|Relationships and boundaries|At the type section the Samphire Marsh Member lies stratigraphically between the Fly Flat Member (below) and the Willara Formation (above). Although the depositional sequence from Fly Flat to Samphire March Member is continuous elsewhere, the contact at the type section is likely a disconformity. In the Samphire Marsh 1 well the Samphire Marsh Member is atypically and unconformably overlain by the Permo-carboniferous Grant Group.|16-MAY-23
79800|Samphire Marsh Member|Identifying features|Distinguished from the underlying Fly Flat Member by the abrupt change from dominantly sandy siliciclastic to carbonate-mudstone lithologies.|16-MAY-23
79800|Samphire Marsh Member|Structure and Metamorphism|Flat-lying to gently dipping depending on structural position. Locally affected by faulting (Zhan 2019). No metamorphism.|16-MAY-23
79800|Samphire Marsh Member|Age reasons|At the type section, the Samphire Marsh Member is assigned a Lower - Middle Ordovician, Tremadocian to possible earliest Dapingian age. This is based on the presence of the Jumudontus gananda, Oepikodus communis, Prioniodus oepiki - Serratognathus bilobatus and Paroistodus proteus conodont biozones (Zhen et al. 2017). Six U-Pb radiometric dates are recorded from bentonite beds. Derived ages range from 479.37 +/- 0.16 Ma at 1383.27 m (30 cm above the base of the member) to 470.18 +/- 0.13 Ma at 1165.44 m (just above the interpreted Samphire Marsh Member - Willara Formation contact) (Normore et al., 2017).|16-MAY-23
79800|Samphire Marsh Member|Correlations|The basal section of the Samphire Marsh Member may be equivalent to the uppermost deposits of the Wilson Cliffs Sandstone which is recorded in the south eastern sections of the Canning Basin (wells Contention Heights 1, Kidson 1, Patience 2 and Wilson Cliffs 1 [type section]). Based on conodont biostratigraphy, the lower parts of the Samphire Marsh Member are considered equivalent to the Kudata Dolomite as described by Nicoll et al. (1993), and the Emanuel Formation, while the upper parts of the member may be equivalent to the lower parts of the Gap Creek Formation (all Prices Creek Group) as described by Nicoll and Ethington, (2004) and Zhen and Nicoll (2009).|16-MAY-23
79800|Samphire Marsh Member|Alteration and Mineralisation|N/A|16-MAY-23
79800|Samphire Marsh Member|Geophysical Expression|This member is not differentiated from the Fly Flat Member on seismic work completed to date.|16-MAY-23
79800|Samphire Marsh Member|Defn author|L Dent and L Normore 18-JAN-2021.|16-MAY-23
79800|Samphire Marsh Member|Proposed publication|Dent, LM, Normore, LS, and Martin, SK 2021, Reference section, revised stratigraphy and facies analysis of the Ordovician Nambeet Formation, Canning Basin, Western Australia, Geological Survey of Western Australia, Report in press.|16-MAY-23
79800|Samphire Marsh Member|References|Nicoll, RS, Laurie, JR and Roche, MT 1993, Revised stratigraphy of the Ordovician (late Tremadoc-Arenig) Prices Creek Group and Devonian Poulton Formation, Lennard Shelf, Canning Basin, Western Australia: Journal of Australian Geology and Geophysics, v. 14, p. 65-76.  **Nicoll, RS and Ethington, RL 2004, Lissoepikodus nudus gen. et sp. nov. and Oepikodus cleftus sp. nov., new septimembrate conodont taxa from the Early Ordovician of Australia and Nevada: Courier Forschungsinstitut Senckenberg, v. 245, p. 427-461.  **Normore, LS, Zhen, YY, Dent, LM, Crowley, JL, Percival, IG and Wingate, MTD 2018, Early Ordovician CA-IDTIMS U-Pb zircon dating and conodont biostratigraphy, Canning Basin, Western Australia: Australian Journal of Earth Sciences, v. 65, p. 61-73.  **Zhan, Y 2019, A seismic interpretation of the Broome Platform, Willara Sub-basin and Munro Arch of the Canning Basin, Western Australia: Geological Survey of Western Australia, Report 193, 43p.  **Zhen, Y, Percival, IG, Normore, LS and Dent, LM 2017, Floian (Early Ordovician) Conodonts of the Canning Basin, Western Australia ? Biostratigraphy and Palaeobiogeographic Affinities with Chinese Faunas, in Proceedings of the International Geoscience Programme (IGCP) Project 653 Annual Meeting, p. 235-241.  **Zhen, YY and Nicoll, RS 2009, Biogeographic and biostratigraphic implications of the Serratognathus bilobatus fauna (Conodonta) from the Emanuel Formation (Early Ordovician) of the Canning Basin, Western Australia: The Australian Museum, Sydney, NSW, Records of the Australian Museum 61, 30p.|16-MAY-23
74623|Sandfire Calcilutite|Name source|Sandfire, a location south of Broome, latitude/longitude coordinates 19º 43' 54" S, 121º 12' 31" E, Mandora 1:250,000 Topographical Sheet, where the Formation is well developed. ¿Sandfire¿ is a literary degradation of the term "samphire", as in the locally named Samphire Marsh, so named because the lowlands in this region are inhabited by samphire vegetation. Samphire Marsh is also known as Mandora Marsh, the latter name being used in the listing of the marsh as a Ramsar site.|16-MAY-23
74623|Sandfire Calcilutite|Constituents|While the main part of the calcilutite unit is referred to the Sandfire Calcilutite as a Formation, three members are formally recognised within it: the Lagrange Calcilutite Member, the Crab Creek Calcilutite Member, and the Djugun Member.|16-MAY-23
74623|Sandfire Calcilutite|Geomorphic expression|As contiguous supratidal coastal flats, high intertidal flats, and mid-low tidal flats.|16-MAY-23
74623|Sandfire Calcilutite|Type section locality|The Sandfire region, latitude/longitude coordinates 19º 43' 54" S, 121º 12' 31" E, Mandora 1:250,000 Topographical Sheet.|16-MAY-23
74623|Sandfire Calcilutite|Description at type locality|7 m cream structureless calcilutite, with grey root-structured calcilutite in the upper 30 cm.|16-MAY-23
74623|Sandfire Calcilutite|Extent|The unit is widespread along the Canning Coast, occurring from Beagle Bay to Pardoo Creek. It also has been intersected in numerous cores throughout the coastal region.|16-MAY-23
74623|Sandfire Calcilutite|Thickness range|At type locality 7 m thick.  Additionally, generally as the lithotope for this Formation occurs between MSL and HAT, in northern areas where the tidal range is 8 m, the Formation has been intersected in cores and trenches and has been recorded at 5 m thick. In southern areas where the tidal range is 6 m, the Formation is 2-3 m thick.  In Crab Creek it is 10 m thick.  Regionally, the unit will appear as discontinuous ribbons and lenses, some kilometres to tens of kilometres in length and kilometres to tens of kilometres width, but only 2-7 m thick, increasing in general thickness in response to increasing tidal amplitude, from south to north.|16-MAY-23
74623|Sandfire Calcilutite|Lithology|Light-coloured to white, cream to grey bioturbated to structureless to locally root-structured to laminated calcilutite and shelly calcilutite. XRD analyses show the mud to be dominantly calcite, with some Mg-calcite and aragonite, and generally minor quartz silt and kaolinite.   In mangrove environments, there is a local scattered shell content, composed of mangrove-associated molluscs; in this lithotope, in some areas exposed to periodic wave action and storms, low tidal molluscs have been transported into the environment, and form a shelly calcilutite. Where the Formation extends as a depositional lithosome to low tidal levels, the sediment is more commonly laminated, and has a molluscan shell content (indicative of mid-low tidal settings) different to those of mangrove environments.|16-MAY-23
74623|Sandfire Calcilutite|Depositional environment|Coastal mud flat environments.|16-MAY-23
74623|Sandfire Calcilutite|Fossils|Molluscan shells in this member include the bivalves Dosinia sp., Pitar sp, Saccostrea cucullata, Venus lamellaris, and the gastropods Cassidula angulifera, Cerithidea anticipata, Cerithidea cingulata, Ellobium aurisjudae, Nerita undata, Telescopium telescopium, Terebralia palustris and Terebralia sulcata, and remains of Teredinidae ("shipworm"). Plant remains include in situ and fallen trunks and wood fragments of Avicennia marina, Rhizophora stylosa and Ceriops tagal.  Lower parts of the formation contain molluscan shell such as the bivalves Anadara granosa, Anomalocardium squamosa, Paphies striata, Tellina capsoides, Tellina piratica, Tellina spp, and the gastropod Nassarius dorsatus.|16-MAY-23
74623|Sandfire Calcilutite|Relationships and boundaries|Stratigraphic relations have been determined from a number of locations.  The unit passes downwards, with gradational contact, through a series of muddy interlayers over an interval of 30 cm, into the underlying Port Smith Sand. Where it is juxtaposed against the Race Course Plains Coquina, the basal contact is sharp. Locally, there is an erosional contact with the laterally equivalent Eighty Mile Beach Coquina, with the Eighty Mile Beach Coquina cutting into the calcilutite.  The Formation passes laterally and basally into red sand of the Mowanjum Sand via a muddy sand zone (the Djugun Member).|16-MAY-23
74623|Sandfire Calcilutite|Age reasons|Radiocarbon dating of shells and sediment within the Formation places it in the Holocene, viz., 1390 +/-170 yrs BP, 3170 ± 180 yrs BP, 3170 ± 130 yrs BP, 3415 +/- 260 yrs BP, 4070 +/- 220 yrs BP, 4470 +/- 120 yrs BP, 5070 +/-270 yrs BP, 7280 +/- 290 yrs BP, 7450 ± 190 yrs BP.|16-MAY-23
74623|Sandfire Calcilutite|Correlations|In the contemporary and sub-recent setting, the Sandfire Calcilutite is temporally equivalent to the Port Smith Sand, the Cable Beach Sand, the Eighty Mile Beach Coquina, the Shoonta Hill Sand, the Church Hill Sand, and the Barn Hill Formation; at the level of the lithosome, the formation is laterally equivalent to Port Smith Sand, the Cable Beach Sand, the Eighty Mile Beach Coquina; earlier in the Holocene (circa 5000 years BP), the Sandfire Calcilutite is stratigraphically equivalent to the Willie Creek Calcarenite.|16-MAY-23
74623|Sandfire Calcilutite|Comments|Generally a cream toned calcilutite.|16-MAY-23
74623|Sandfire Calcilutite|References|For Canning Coast units: Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.For Mowanjum Sand: Semeniuk V 1980 Quaternary stratigraphy of the tidal flats King Sound, WA. Journal of the Royal Society of Western Australia 63: 65-78.|16-MAY-23
80524|Searle Hills Conglomerate|Name source|Searle Hills in the Western Australian Amadeus Basin (RAWLINSON 1:250 000 sheet, centred around 24deg 04'S 127deg 49'E).|16-MAY-23
80524|Searle Hills Conglomerate|Unit history|The unit currently recognised as Searle Hills Conglomerate was previously included in the Sir Frederick Conglomerate by Wells et al. (1964) and Forman (1965), however the stratigraphic relationships are different to the Sir Frederick Conglomerate elsewhere, and suggest that it is older than that unit.|16-MAY-23
80524|Searle Hills Conglomerate|Geomorphic expression|Low rubbly strike ridges and discontinuous low hills and rises.|16-MAY-23
80524|Searle Hills Conglomerate|Type section locality|The type locality is in a low strike ridge the centre of the Searle Hills (24deg 04'S 127deg 49'E; RAWLINSON 1:250 000 map sheet; GILLESPIE 1:100 000 map sheet).|16-MAY-23
80524|Searle Hills Conglomerate|Extent|Exposure of the Searle Hills Conglomerate is limited to the Searle Hills area of the Western Australian Amadeus Basin (northwest RAWLINSON 1:250 000 sheet), where it outcrops over a strike length of about 16 km around the nose of northeast plunging anticline. Its extent under cover is unknown.|16-MAY-23
80524|Searle Hills Conglomerate|Thickness range|Approximately 300 m thick at the type locality. The variation in thickness beyond the estimated 300 m in the type area is unknown.|16-MAY-23
80524|Searle Hills Conglomerate|Lithology|The Searle Hills Conglomerate is composed of conglomerate consisting of rounded pebble-, cobble- and boulder-sized clasts in a very friable, coarse, sandy matrix. At most outcrops the matrix has largely or totally disintegrated, leaving low hills and ridges of loose clasts. The larger clasts are mainly of quartzite, sandstone and metasandstone, with pebble clasts including minor chert and white quartz. Boulder clasts reach 85 cm in diameter. Cobble and boulder clasts may display pressure solution pits indicating clast support. The siliciclastic clasts were probably derived from the Dean Quartzite, Kulail Sandstone and Dixon Range Formation, which were uplifted along the southern margin of the Amadeus Basin during the Petermann Orogeny. The chert clasts are likely derived from silicified carbonate units lower in the Amadeus Basin succession.|16-MAY-23
80524|Searle Hills Conglomerate|Depositional environment|The Searle Hills Conglomerate was deposited by high-energy streams in an alluvial setting, possibly as fans. Although there is no paleocurrent data, the clasts are inferred to have been derived from uplift and erosion along the southern margin of the Amadeus Basin during the Petermann Orogeny.|16-MAY-23
80524|Searle Hills Conglomerate|Fossils|None observed.|16-MAY-23
80524|Searle Hills Conglomerate|Diastems or hiatuses|None observed.|16-MAY-23
80524|Searle Hills Conglomerate|Relationships and boundaries|The Searle Hills Conglomerate lies stratigraphically between the Carnegie Formation (below) and the Ellis Sandstone (above), however the contacts are not exposed and thus their nature is uncertain. The unit is also locally overlain unconformably by the Carboniferous-Permian Grant Group of the onlapping Canning Basin.|16-MAY-23
80524|Searle Hills Conglomerate|Identifying features|The dominant lithology of cobble- to boulder conglomerate distinguishes the Searle Hills Conglomerate from the enclosing Carnegie Formation and the Ellis Sandstone, which are both dominated by sandstone. The Searle Hills Conglomerate is lithologically indistinguishable from the Sir Frederick Conglomerate, but has different stratigraphic relationships that implies that it is somewhat older.|16-MAY-23
80524|Searle Hills Conglomerate|Structure and Metamorphism|Folded and moderately to steeply dipping, but not metamorphosed.|16-MAY-23
80524|Searle Hills Conglomerate|Age reasons|The Searle Hills Conglomerate has not been directly dated, but stratigraphic relationships indicate that it was deposited during the Petermann Orogeny, either during the late Ediacaran or early Cambrian.|16-MAY-23
80524|Searle Hills Conglomerate|Correlations|As the nature of contacts are uncertain it is possible that the Searle Hills Conglomerate is at least partly a lateral equivalent of either the Carnegie Formation or the Ellis Sandstone. Stratigraphic relationships suggest that the Searle Hills Conglomerate is older than the similar Sir Frederick Conglomerate, which overlies and apparently cuts down through the Ellis Sandstone.|16-MAY-23
80524|Searle Hills Conglomerate|Alteration and Mineralisation|None observed.|16-MAY-23
80524|Searle Hills Conglomerate|Geophysical Expression|Not distinguished on geophysical datasets.|16-MAY-23
80524|Searle Hills Conglomerate|Geochemistry|No data.|16-MAY-23
80524|Searle Hills Conglomerate|Defn author|P.W. Haines and H-J. Allen 17-DEC-2020.|16-MAY-23
80524|Searle Hills Conglomerate|Proposed publication|Geological Survey of Western Australia Report. The unit is currently indicated on the 1:500 000 Interpreted Bedrock Geology, 2020 GIS layer available through GeoVIEW.WA (www.dmirs.wa.gov.au/geoview) and published in the GSWA Explanatory Notes System (www.dmirs.wa.gov.au/ENS).|16-MAY-23
80524|Searle Hills Conglomerate|References|Forman, DJ (compilers) 1965, Rawlinson, WA: Bureau of Mineral Resources, Geology and Geophysics, 1:250 000 Geological Series Explanatory Notes, 7p.  **Wells, AT, Forman, DJ and Ranford, LC 1964, Geological reconnaissance of the Rawlinson and MacDonald 1:250 000 sheet areas: Bureau of Mineral Resources, Geology and Geophysics, Report 65, 35p.|16-MAY-23
79382|Shingle Creek Group|Name source|Named after Shingle Creek on the HARDEY 1:100 000 mapsheet, which crosses the Nanutarra-Paraburdoo road at Lat. -22.8951 Long. 116.8571.|16-MAY-23
79382|Shingle Creek Group|Unit history|The Shingle Creek Group is synonymous with the bulk of the informally named 'lower Wyloo Group', which was generally regarded to extend from the base of the Beasley River Quartzite to the base of the Mount McGrath Formation (Horwitz, 1982; Powell and Horwitz, 1994), but excludes the Wooly Dolomite.|16-MAY-23
79382|Shingle Creek Group|Geomorphic expression|The basal sedimentary portion of the group forms prominent hills with a distinctive pattern on aerial photographs. The upper volcanic part is best exposed in the type area as low rounded hills, but is not well-exposed in most other areas.|16-MAY-23
79382|Shingle Creek Group|Type section locality|The type locality for the Shingle Creek Group is along Shingle Creek on the HARDEY 1:100 000 mapsheet, between Lat. -22.8576 Long. 116.8803 and Lat. -22.8893 Long. 116.8629.|16-MAY-23
79382|Shingle Creek Group|Extent|The Shingle Creek Group is preserved throughout the southern margin of the Hamersley province, primarily in synclines formed during the Ophthalmia Orogeny.|16-MAY-23
79382|Shingle Creek Group|Thickness range|The total thickness of the Shingle Creek Group in the type area is estimated to be about 3.2 km, although this estimate includes Balgara Dolerite sills that intrude the base of the group. The thickness of the Shingle Creek Group is highly variable on account of it being bound by unconformities. The maximum thickness of about 3.2 km is present in the type area, but thins to zero around the Wyloo Anticline.|16-MAY-23
79382|Shingle Creek Group|Lithology|The Shingle Creek Group consists of quartz sandstone, conglomerate, siltstone, and mudstone at the base, overlain by about 2 km of massive to amygdaloidal and vesicular basalt.|16-MAY-23
79382|Shingle Creek Group|Depositional environment|The sedimentary component of the group was deposited in a fluvial to shallow marine environment, and the volcanic component is entirely shallow marine (Thorne and Seymour, 1991, Muller, 2005).|16-MAY-23
79382|Shingle Creek Group|Diastems or hiatuses|The Nummana Member, at the base of the Cheela Springs Basalt is locally absent around the Wyloo Anticline, where the Cheela Springs Basalt onlaps the Beasley River Quartzite.|16-MAY-23
79382|Shingle Creek Group|Relationships and boundaries|The Shingle Creek Group overlies the Turee Creek, Hamersley and Fortescue Groups on a locally pronounced angular unconformity. The contact with the overlying Wooly Formation is largely paraconformable, but there is local evidence for several metres to hundreds of metres of relief as well as low angularity. The Shingle Creek Group is intruded by the c. 2208 Ma Balgara Dolerite|16-MAY-23
79382|Shingle Creek Group|Identifying features|The lower 500 m of the Shingle Creek Group is dominated by siliciclastic rocks that form an overall upward-fining succession from pebble to cobble conglomerate, to siltstone and mudstone. The upper 2.7 km consists of thick basalt flows. The basal Beasley River Quartzite is a distinctive cliff-forming unit that can be correlated throughout the region, and displays a consistent stratigraphic relationship to the overlying Cheela Springs Basalt via the Nummana member which forms a lithological gradation between the two.|16-MAY-23
79382|Shingle Creek Group|Structure and Metamorphism|The Shingle Creek Group has been folded by the Ophthalmia Orogeny, producing east-west to west-northwest and east-southeast trending folds that have a strong control on the preservation of the unit. It has been metamorphosed to lower greenschist facies, and is also displaced by a series of younger normal and strike-slip faults along the southern margin of the Hamersley province.|16-MAY-23
79382|Shingle Creek Group|Age reasons|The Shingle Creek Group is younger than the Meteorite Bore Member in the underlying Turee Creek Group, which has a maximum depositional age of 2340 +/- 22 Ma (Caquineau et al., 2016; 2018), and a diagenetic age of 2312.7 +/- 5.6 Ma (Philippot et al. 2018). It is also older than the c 2208 Ma Balgara Dolerite which intrudes the lower part throughout the region (Muller et al. 2005; Martin and Morris, 2010).|16-MAY-23
79382|Shingle Creek Group|Defn author|D. McB. Martin, Geological Survey of Western Australia 7-JUL-2020.|16-MAY-23
79382|Shingle Creek Group|Proposed publication|GSWA Report 203|16-MAY-23
79382|Shingle Creek Group|Comments|The Wooly Formation (formerly Wooly Dolomite) is excluded from the Shingle Creek Group on account of the presence of a basal disconformity to angular unconformity, despite being included in the former ?lower Wyloo Group? by some authors.|16-MAY-23
79382|Shingle Creek Group|References|Caquineau, T, Paquette, J-L and Philippot, P 2016, In situ U-Pb zircon dating of the Meteorite Bore Member diamictites: constraints on the Paleoproterozoic glaciations and the Great Oxidation Event, in Goldschmidt Conference Abstracts: Goldschmidt Conference, Yokohama, Japan, 26 June 2016-1 July 2016, p. 364.   **Caquineau, T, Paquette, J-L and Philippot, P 2018, U-Pb detrital zircon geochronology of the Turee Creek Group, Hamersley Basin, Western Australia: Timing and correlation of the Paleoproterozoic glaciations: Precambrian Research, v. 307, p. 34-50.   **Horwitz, RC 1982, Geological History of the Early Proterozoic Paraburdoo Hinge Zone, Western Australia: Precambrian Research, v. 19, p. 191-200.   **Philippot, P 2018, Avila, JN, Killingsworth, BA, Tessalina, S, Baton, F, Caquineau, T, Muller, E, Pecoits, E, Cartigny, P, Lalonde, SV, Ireland, TR, Thomazo, C, Van Kranendonk, MJ and Busigny, V, 2018, Globally asynchronous sulphur isotope signals require re-definition of the Great Oxidation Event: Nature Communications, v.9, Article number 2245, 10 p.  **Martin, DMcB and Morris, PA 2010, Tectonic setting and regional implications of ca. 2.2 Ga mafic magmatism in the southern Hamersley Province, Western Australia: Australian Journal of Earth Sciences, v. 57, no. 7, p. 911-931.  **Muller, SG, 2005, The tectonic evolution and volcanism of the Lower Wyloo Group, Ashburton Province, with timing implications for giant iron-ore deposits of the Hamersley Province, Western Australia: Unpublished PhD Thesis, University of Western Australia, 156p.  **Muller, SG, Krapez, B, Barley, ME and Fletcher, IR 2005, Giant iron-ore deposits of the Hamersley province related to the breakup of Paleoproterozoic Australia: New insights from in situ SHRIMP dating of baddeleyite from mafic intrusions: Geology, v. 33, no. 7, p. 577-580.  **Powell, CMcA and Horwitz, RC 1994, Late Archaean and Early Proterozoic tectonics and basin formation of the Hamersley Ranges: 12th Australian Geological Convention, Geological Society of Australia (WA Division), Excursion Guidebook 4, 53p.  **Thorne, AM and Seymour, DB 1991, The geology of the Ashburton Basin, Western Australia: Geological Survey of Western Australia, Bulletin 139, 141p.|16-MAY-23
22841|Shoonta Hill Sand|Name source|Shoonta Hill area, a region of well developed coastal sand dunes, latitude/longitude coordinates 19º 55' 51" S, 120º 10' 43" E, Mandora 1:250,000 Topographical Sheet.|16-MAY-23
22841|Shoonta Hill Sand|Geomorphic expression|As white coastal dunes.|16-MAY-23
22841|Shoonta Hill Sand|Type section locality|Shoonta Hill, latitude/longitude coordinates 19º 55' 02" S, 120º 11' 20" E, Mandora 1:250,000 Topographical Sheet.|16-MAY-23
22841|Shoonta Hill Sand|Description at type locality|Cream to light coloured fine/medium quartzose and calcareous sand; large-scale cross-bedding and cross-lamination, with local shell horizons; thickness 8 m.|16-MAY-23
22841|Shoonta Hill Sand|Extent|The unit is widespread as a shoe-string to lensoid deposit along the Canning Coast.|16-MAY-23
22841|Shoonta Hill Sand|Thickness range|Thickness at type locality is 8 m.  In addition, regionally, the unit will appear as a continuous to locally discontinuous shoe-string to lensoid deposit of variable thickness and width, some tens to hundreds of kilometres long, but only up to 500 m wide and up to 8 m thick.|16-MAY-23
22841|Shoonta Hill Sand|Lithology|In general, light-coloured to white, laminated, cross-laminated to bedded, to structureless and root-structured quartzose calcareous fine to medium sand. Calcareous sand grains are bioclasts, foraminifera, intraclasts, some lithoclasts, and locally ooids.  Locally humic soil layers are developed.|16-MAY-23
22841|Shoonta Hill Sand|Depositional environment|Coastal dune environments.|16-MAY-23
22841|Shoonta Hill Sand|Fossils|Mollusc shells occur in the lower part of the Formation, near its contact with Eighty Mile Beach Coquina and Cable Beach Sand, also in horizons within the Formation, representing wind lag deposits (that include Donax faba and Sepia spp), and as midden deposits.|16-MAY-23
22841|Shoonta Hill Sand|Diastems or hiatuses|Largely, not applicable, but elsewhere from the type locality there are locally developed thin humic soil layers (hiatuses).|16-MAY-23
22841|Shoonta Hill Sand|Relationships and boundaries|The unit passes downwards, with gradational contact into Cable Beach Sand.  Depending on setting, it overlies with sharp contact the Mowanjum Sand (Semeniuk 1980), or Church Hill Sand, or Barn Hill Formation, or Eighty Mile Beach Coquina. Locally, the unit overlies with sharp contact the Sandfire Calcilutite or the Eighty Mile Beach Coquina.|16-MAY-23
22841|Shoonta Hill Sand|Age reasons|Radiocarbon dating of shells and soil within the Formation places it in the Holocene, viz., 1190 +/-170 yrs BP, 2440+/-190 yrs BP.|16-MAY-23
22841|Shoonta Hill Sand|Correlations|The unit is temporally and laterally equivalent to the Barn Hill Formation, the Church Hill Sand, in the coastal dune settings, and to the Sandfire Calcilutite, Port Smith Sand, and Eighty Mile Beach Coquina in the tidal settings.|16-MAY-23
22841|Shoonta Hill Sand|Comments|Large scale cross bedded; white fine to medium sand.|16-MAY-23
22841|Shoonta Hill Sand|References|For Canning Coast units: Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.For Mowanjum Sand: Semeniuk V 1980 Quaternary stratigraphy of the tidal flats King Sound, WA. Journal of the Royal Society of Western Australia 63: 65-78.|16-MAY-23
26900|Slatey Creek Granite|Name source|Slatey Creek, lat. 19o19'S, long. 128o45'E, Billiluna 1:250 000 Sheet area (SE/52-14).|16-MAY-23
26900|Slatey Creek Granite|Unit history|Included by Casey & Wells (1964) in the Lewis Granite, which is now restricted to the Lewis Range area in the Lucas Sheet area to the south. The Lewis Granite is dated isotopically by R.W. Page at 1715 +/- 15 m.y.|16-MAY-23
26900|Slatey Creek Granite|Type section locality|Scarp face 60 m high 16 km NNW of Tent Hill and 3 km S of Slatey Creek, at lat. 19o22'S, long. 128o41'30"E. Here unweathered medium grained mainly non porphyritic pale muscovite and muscovite-biotite adamellite is exposed intruding Killi Killi Beds and overlain by 30 m of Lewis Range Sandstone.|16-MAY-23
26900|Slatey Creek Granite|Extent|Scattered exposures in eastern part of the Billiluna Sheet area southwest of the Gardner Range and mainly south of Slatey Creek.|16-MAY-23
26900|Slatey Creek Granite|Lithology|Porphyritic and non-porphyritic mainly medium to fine muscovite, biotite-muscovite, and biotite adamellite; minor biotite granodiorite. Some pegmatite and aplite veins.|16-MAY-23
26900|Slatey Creek Granite|Relationships and boundaries|Intrudes low grade metamorphics of the Killi Killi Beds, part of the Archaean? Tanami complex (Blake et al., in press). Overlian by Carpentarian Gardiner Sandstone (Blake et al., in press) and Adelaidean Lewis Range Sandstone (Blake & Hodgson, in prep.).|16-MAY-23
26900|Slatey Creek Granite|Age reasons|Dated isotopically by R.W. Page, using the whole rock Rb-Sr method, at 1770 +/- 62 my i.e., early Carpentarian.|16-MAY-23
26900|Slatey Creek Granite|Proposed publication|Bureau of Mineral Resources Report|16-MAY-23
78697|Stockyard Gully Member|Name source|The name of the caves and national park where it outcrops: The Stockyard Gully System / Stockyard Gully National Park: 29°56'23" S; 115°05'55" E.|16-MAY-23
78697|Stockyard Gully Member|Unit history|None. [presumably not previously distinguished from the rest of the Tamala Limestone?]|16-MAY-23
78697|Stockyard Gully Member|Geomorphic expression|It appears as a intermediate member/unit on exposed rocks (walls), delimited by palaeosoil and calcrete horizons.|16-MAY-23
78697|Stockyard Gully Member|Type section locality|The exposed wall at the entrance of the Beekeepers Cave in Stockyard Gully National Park, accessible with 4WD vehicles. Co-ordinates available to researchers, but location is confidential to protect from vandalism. Apply to National Convenor, Stratigraphy Commission.|16-MAY-23
78697|Stockyard Gully Member|Confidential_type_locality|Yes.|16-MAY-23
78697|Stockyard Gully Member|Extent|It occurs in Stockyard Gully National Park and Beekeepers Nature Reserve. However, it also occurs (mostly as calcrete) in Nambung National Park as part of the pinnacles, but its distinctive features there are obscured by a calcrete formation.|16-MAY-23
78697|Stockyard Gully Member|General description|Cross-bedded poorly to well cemented aeolian calcarenite, deposited in Pleistocene.|16-MAY-23
78697|Stockyard Gully Member|Thickness range|Its thickness in the Pinnacles Desert ranges from 0.5 m to 2 m, whilst in Eneabba region it ranges from 3 m to 10 m.|16-MAY-23
78697|Stockyard Gully Member|Lithology|It is yellow coloured, poorly to well cemented, fine to coarse grained, well sorted limestone (calcarenite) with distinctive aeolian cross-bedding (inclined up to 45° towards the north to north-east). The porosity ranges between 10% and 20%. It is mainly composed of carbonates (27% - 79%; low-Mg-calcite) and quartz (21% - 71%) with minor amounts of feldspar (1% - 2%). Feldspar is mostly orthoclase (~75% of feldspar), followed by microcline (~25% of feldspar). The carbonate cement is sparry meniscus, rim and pore-filling cement, and on the echinoderm fragments, syntaxial rims have formed. Overlying the calcarenite is a case-hardened calcrete layer and then a mostly cemented reddish palaeosoil.|16-MAY-23
78697|Stockyard Gully Member|Depositional environment|Aeolian cross-bedding indicates that it was deposited as coastal dunes with bioclasts derived from the ocean (marine bioclasts). Development of calcrete and palaeosoil followed.|16-MAY-23
78697|Stockyard Gully Member|Fossils|The bioclasts include foraminifera, echinoderms, red-algae, bryozoans, and molluscs.|16-MAY-23
78697|Stockyard Gully Member|Diastems or hiatuses|None.|16-MAY-23
78697|Stockyard Gully Member|Relationships and boundaries|The Stockyard Gully Member is underlain by the older Nambung Member. It is overlain by the Pinnacles Desert Member.|16-MAY-23
78697|Stockyard Gully Member|Identifying features|It appears as the `middle¿ unit (out of 3), well visible in front of the big exposed walls at the cave entrances in Stockyard Gully National Park and Beekeepers Nature Reserve, delimited by palaeosoil horizons. The overlying Pinnacles Desert Member and underlying Nambung Member have both some karst (palaeo)surface, whilst the Stockyard Gully Member only has a horizontal calcrete layer. The other difference between these members is the age, the alteration of bioclasts when compared to the overlying Pinnacles Desert Member which still has some percentage of aragonite, and isotopic signatures when compared to the overlying Pinnacles Desert Member (see the range of isotopic signatures for each member).|16-MAY-23
78697|Stockyard Gully Member|Structure and Metamorphism|Undeformed.|16-MAY-23
78697|Stockyard Gully Member|Age reasons|No samples of the Eneabba [typo for Stockyard Gully?]  Member were dated, but the presence of thick palaeosoil units between this member and the higher Pinnacles Desert (MIS 7) and lower Nambung (MIS 11) Members suggest a most probable deposition in the MIS 9 period.|16-MAY-23
78697|Stockyard Gully Member|Correlations|None.|16-MAY-23
78697|Stockyard Gully Member|Alteration and Mineralisation|None.|16-MAY-23
78697|Stockyard Gully Member|Geophysical Expression|Not known.|16-MAY-23
78697|Stockyard Gully Member|Geochemistry|Whole rock isotopic values for delta18O range between -3.28ppt and -3.84ppt, and delta13C between -7.07ppt and -7.50ppt.|16-MAY-23
78697|Stockyard Gully Member|Defn author|Matej Lipar & John A. Webb, La Trobe University 14-Mar-2014|16-MAY-23
74062|Strelley Pool Formation|Name source|Strelley Pool (21o 06' 41"S       119o 08' 25"E)|16-MAY-23
74062|Strelley Pool Formation|Unit history|Strelley Pool Chert.   Previously named as the Strelley Pool Chert (Lowe, 1983; Van Kranendonk et al., 2006).|16-MAY-23
74062|Strelley Pool Formation|Constituents|Three informally named members in type area.|16-MAY-23
74062|Strelley Pool Formation|Geomorphic expression|Positive relief, generally forms ridges.|16-MAY-23
74062|Strelley Pool Formation|Type section locality|21o 06' 41"S 119o 08' 25"E Ridge section immediately to east of Strelley Pool; also west of Strelley Pool.|16-MAY-23
74062|Strelley Pool Formation|Description at type locality|Basal sandstone (5 m), overlain by secondary grey-white chert representing silicified carbonate rocks (13 m), overlain by silicified volcanic ash (2 m), overlain by matrix-supported polymictic breccia and conglomerate (3 m)|16-MAY-23
74062|Strelley Pool Formation|Extent|30,000 km2 in the East Pilbara Terrane of the Pilbara Craton, Western Australia.Outcrops in eleven greenstone belts of the East Pilbara Terranes in the Pilbra Craton, Western Australia.|16-MAY-23
74062|Strelley Pool Formation|Thickness range|5-1000m.  Extremely variable thickness and lithological composition on a regional scale, and rapid lateral variations over distances of 500 m to 1000 m.THICKNESS FOR TYPE AREA:  Averages 20 m in type area, but laterally variable between 10m and 30m.THICKNESS IN EAST PILBARA TERRANE:  0-1000 m|16-MAY-23
74062|Strelley Pool Formation|Lithology|Regionally dominated by siliciclastic and volcaniclastic assemblages, laminated grey-white chert, representing silicified carbonate rocks, carbonate rocks with only minor silicification, and minor primary black, white, and jaspilitic chert with crystal fans (pseudomorphs after aragonite, gypsum, or barite).LITHOLOGY FOR TYPE AREA:  Sandstone, conglomerate, silicified carbonate rocks (laminated chert), and evaporite deposits.LITHOLOGY IN EAST PILBARA TERRANE:  Regionally dominated by siliciclastic assemblages, carbonate rocks, and laminated grey-wgite chert (slicified carbonate rocks). Minor primar black, white, and jaspilitic chert with crystal fans (pseudomorphs after aragonite, gypsum, or barite).|16-MAY-23
74062|Strelley Pool Formation|Depositional environment|Continental, including fluviatile, deltaic, and shallow-water marine environments.IN TYPE SECTION:  Shallow-water marine, including tidal and supratidal.IN EAST PILBARA TERRANE:  Shallow-water marine, esturine, deltaic, beach, fluviatile, lacustrine, and sabkha environments.|16-MAY-23
74062|Strelley Pool Formation|Fossils|Coniform stromatolites and trace fossils (microtubular structures).IN TYPE AREA:  Coniform stromatolites and trace fossils (microtabular structures).|16-MAY-23
74062|Strelley Pool Formation|Diastems or hiatuses|Formation spans 75 million years based on dating of immediately underlying and overlying volcanic formations. More detailed mapping and internal geochronology on a regional scale is expected to reveal local breaks.IN TYPE AREA:   Indicated by lateral thickness variations of facies, evaporite deposits repeated at several stratigraphic levels, and horizons showing erosional freatures.|16-MAY-23
74062|Strelley Pool Formation|Relationships and boundaries|Paraconformable to disconformable on the 3450-3427 Ma Panorama Formation (upper Warrawoona Group), and disconformably to paraconformably underlies the 3350-3315 Ma Euro Basalt (lower Kelly Group). Currently assigned to the Kelly Group (dominated by mafic volcanic rocks) based on apparent conformity and the presence of mafic volcaniclastic rocks in the upper part of the formation. However, conglomerate at the top of the formation in several areas indicates local erosional breaks between this formation and the overlying Euro Basalt.Unconformably to paraconformably overlies formations of the Warrawoona Group.|16-MAY-23
74062|Strelley Pool Formation|Age reasons|Paleoarchean, 3427-3350 Ma, based on the youngest precise zircon U-Pb age obtained from the underlying Panorama Formation (3427 Ma; Nelson, 2001) and the oldest zircon U-Pb age from the Euro Basalt (3350 Ma: Geological Survey of Western Australia, 2005).|16-MAY-23
74062|Strelley Pool Formation|Comments|Name change from Strelley Pool Chert proposed because (a) the formation contains a wide range of lithologies, in which chert is commonly absent or minor, and (b) most of the chert in the formation is a seconadary replacement (partly Cenozoic) of primary carbonate rocks.Includes most of the succession previously informally named as the Strelley Pool Chert (Lowe, 1983), and formally named as the Strelley Pool Chert (Van Kranendonk and Morant, 1998). The name is amended because 'chert' does not reflect the lithological diversity of the unit as mapped.|16-MAY-23
74062|Strelley Pool Formation|References|Hickman, AH, 2008, Regional review of the 3426-3350 Ma Strelley Pool Formation, Pilbara Craton, Western Australia, Record 2008/15, 27p.Lowe, D.R., 1983, Restricted shallow-water sedimentation of early Archaean stromatolitic and evaporitic strata of the Strelley Pool Chert, Pilbara Block, Western Australia. Precambrian Research 19(3) p239-283.Nelson, D.R., 2001, Compilation of geochronology data, 2000, Geological Survey of Western Australia, Record 2001/2, 205p.Van Kranendonk, MJ, and Morant, P, 1998, Revised Archaean stratigraphy of the North Shaw 1:100 000 sheet, Pilbara Craton: Geological Survey of Western Australia, Annual Review 1997-98, p. 55-62.Van Kranendonk, M.J., Hickman, A.H., Smithies, R.H., Williams, I.R., Bagas, L., and Farrell, T.R., 2004, Event stratigraphy applied to 700 million years of Archaean crustal evolution, Pilbara Craton, Western Australia: Geological Survey of Western Australia, Annual Review 2003-04, p. 49-61.Van Kranendonk, M.J., Hickman, A.H., Smithies, R.H., Williams, I.R., Bagas, L., and Farrell, T.R., 2006, Revised lithostratigraphy of Archaean supracrustal and intrusive rocks in the northern Pilbara Craton, Western Australia. Western Australia Geological Survey, Record 2006/15, 75p.Geological Survey of Western Australia, 2005, Compilation of geochronological data, June 2005 update. Western Australia Geological Survey (DVD).|16-MAY-23
74062|Strelley Pool Formation|Parent|Pilbara Supergroup. The formation is not assigned to a group.|16-MAY-23
74062|Strelley Pool Formation|Reserved? Yes/No|Yes - will supersede Strelley Pool Chert when the definition is formally published in a GSWA Record (probably March 2008).|16-MAY-23
74062|Strelley Pool Formation|State(s)|W.A.|16-MAY-23
24538|Tuckfield Member|Name source|Mt Tuckfield 18o42'S, 124o53'E)|16-MAY-23
24538|Tuckfield Member|Unit history|Forms main part of Poole Sandstone (Guppy et al., 1952). Previously termed "middle Poole Sandstone" by Crowe & Towner (1976a).|16-MAY-23
24538|Tuckfield Member|Type section locality|Mt Tuckfield (18o42'15"S, 124o53'35"E)|16-MAY-23
24538|Tuckfield Member|Extent|Exposed in and between the Poole, St George and Grant Ranges in the Fitzroy Trough of the Canning Basin. Molre isolated exposures also occur on the Lennard Shelf. Correlatives elsewhere in the basin are indefinite.|16-MAY-23
24538|Tuckfield Member|Thickness range|245 m at the type section, but the top is not exposed. 25 m thick in the southern Poole Range.|16-MAY-23
24538|Tuckfield Member|Lithology|Mainly thinly bedded and laminated very fine and fine-grained quartz and lithic wacke with minor quartz arenite and clay pellet conglomerate. Wave-formed ripple marks and bedding-surface trace fossils are common.|16-MAY-23
24538|Tuckfield Member|Relationships and boundaries|Conformably and disconformably overlies Nura Nura Member (Guppy et al., 1952). Disconformably overlain by Christmas Creek Member (Crowe & Towner, 1976b) and where the Christmas Creek Member is absent the Tuckfield Member is overlain by the Noonkanbah Formation, possibly disconformably.|16-MAY-23
24538|Tuckfield Member|Age reasons|Probably Artinskian as it overlies latest Sakmarian Nura Nura Member and is overlain by Artinskian Noonkanbah Formation.|16-MAY-23
24538|Tuckfield Member|Proposed publication|Annual Report Geological Survey of WA for 1976|16-MAY-23
24538|Tuckfield Member|First Reference|80/20975|16-MAY-23
24538|Tuckfield Member|Proposer|Towner R.R., Crowe R.W.A.|16-MAY-23
24538|Tuckfield Member|Reserved? Yes/No|Yes|16-MAY-23
18668|Tumbiana Formation|Name source|Tumbiana Pool on the Nullagine River (MGR 342 346).|16-MAY-23
18668|Tumbiana Formation|Unit history|Original name "Tumbiana Pisolite" (Noldart and Wyatt, 1962).|16-MAY-23
18668|Tumbiana Formation|Type section locality|Meentheena Basin, south of Tumbiana Pool on the Nullagine River.|16-MAY-23
18668|Tumbiana Formation|Extent|Southern part Marble Bar 1:250 000 Sheet; Meentheena Basin Nullagine 1:250 000 Sheet, Roy Hill 1:250 000 Sheet etc.|16-MAY-23
18668|Tumbiana Formation|Thickness range|At Meentheena, about 200 metres. On Marble Bar Sheet, about 50 metres.|16-MAY-23
18668|Tumbiana Formation|Lithology|Upper carbonate member, Lower tuff member.|16-MAY-23
18668|Tumbiana Formation|Relationships and boundaries|Part of the Fortescue Group. Conformably overlies Kylena Basalt. Conformably overlain by Nymerina Basalt. Consists of Meentheena carbonate and Mingah tuff members.|16-MAY-23
18668|Tumbiana Formation|Age reasons|Lower Proterozoic.|16-MAY-23
18668|Tumbiana Formation|Defn author|Lipple S.L., 1975|16-MAY-23
18668|Tumbiana Formation|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
18668|Tumbiana Formation|Status|1|16-MAY-23
35793|Vines Formation|Unit history|The Vines Formation, as originally defined by Stevens et al. (2002), comprised the entire section intersected below 4 m in Vines 1. The formation is here restricted to the interval between 4 and 124.5 m of Vines 1, after the recognition of a significant unconformity at 124.5 m.|16-MAY-23
35793|Vines Formation|Type section locality|Between 4 and 124.5 m in GSWA Vines 1 stratigraphic drillhole. The interval is continuously cored below 44.5 m. Core from Vines 1 can be viewed at the Geological Survey of Western Australia's Perth Core Library, and electric logs are available online from the Department of Industry and Resources (http://www.doir.wa.gov.au) and in Apak et al. (2002).|16-MAY-23
35793|Vines Formation|Extent|Vines 1 is the only known occurrence.|16-MAY-23
35793|Vines Formation|Lithology|Clast-supported, relatively well-rounded and sorted, dark-brown to reddish, pebble conglomerate, with lesser quartz sandstone.|16-MAY-23
35793|Vines Formation|Relationships and boundaries|Unconformably overlies the Lungkarta Formation, and is unconformably overlain by sand and calcrete of assumed Cenozoic age in Vines 1.|16-MAY-23
35793|Vines Formation|Age reasons|Non-fossiliferous. A late Ediacaran to Cambrian age is inferred because it overlies a succession containing reworked Cryogenian palynomorphs, and because of the absence of any younger fossils, the lack of apparent glacial imprint (which would suggest correlation with the Carboniferous - Permian Paterson Formation), and the red-brown colour, which is similar to other upper Ediacaran to Lower Cambrian units in central and South Australia. The depositional facies are consistent with synorogenic deposition, allowing tentative correlation with the Ediacaran to earliest Cambrian Petermann Orogeny.|16-MAY-23
35793|Vines Formation|Defn Reference|Haines, PW, Hocking, RM, Grey, K and Stevens, MK, 2008, 'Vines 1 revisited: are older Neoproterozoic glacial deposits preserved in Western Australia?', Australian Journal of Earth Sciences, vol. 55(3), p. 397-406.|16-MAY-23
79111|Waldburg Dolerite|Name source|The unit was named after Waldburg Homestead (Lat. - 24.742 Long. 117.358), which is located on the Candolle 100k mapsheet, Western Australia.|16-MAY-23
79111|Waldburg Dolerite|Unit history|In some localities the unit was previously mapped as the 1465-1450 Ma Narimbunna Dolerite, but the Waldburg Dolerite is now shown to be 1514-1505 Ma. Before 2014, it was presumed that dolerite sills that were emplaced within the 1679-1455 Ma Edmund Basin of the Capricorn Orogen belong to the Narimbunna Dolerite whereas dolerite sills intruded into the rocks of the younger 1298-1067 Ma Collier Croup were assigned to the 1083-1075 Ma Kulkatharra Dolerite. However, in 2013 GSWA geologist O Blay was puzzled by astonishing similarities in the geochemical signature of two presumably Narimbunna Dolerite samples located more than 200 km apart. Furthermore the samples were analysed in different years and by different laboratories. The dolerite sill located on the CANDOLLE 100k map sheet was analysed in 2012. It yielded zircons that gave a crystallization age of c. 1505 Ma. However, at that time it was suggested that the significantly older age, presumably, represented a separate episode of dolerite intrusion. The sample from another dolerite sill on the MANGAROON 100k mapsheet collected back in 2002 did not yield datable minerals. However in 2013, based on the geochemical similarities of these two dolerite samples the dolerite sill on MANGAROON was re-sampled and successfully dated: a crystallization age of c. 1514 Ma was obtained from combined analyses of zircon and baddeleyite extracted from very coarse-grained leucogabbro. Both sills were emplaced into the base of the Edmund Group. These encouraging results enabled further investigation with more dolerite sills on the MOUNT AUGUSTUS 100k map sheet, previously assigned to the Narimbunna Dolerite, being dated with significantly older ages. Therefore, geochronology, field observation, petrography and distinct geochemistry of dolerite sills in the Capricorn Orogen revealed a new suite of sills: the 1514-1505 Ma Waldburg Dolerite (GSWA Explanatory Notes System).|16-MAY-23
79111|Waldburg Dolerite|Geomorphic expression|Generally outcrops as brownish-black rounded boulders, with thick colluvial scree at the top of low hills and ridges, within small creeks, or at the bases of low slopes; but appear to be laterally continuous.|16-MAY-23
79111|Waldburg Dolerite|Type section locality|The Waldburg Dolerite sills occur within the Western Capricorn Orogen and intrude Paleoproterozoic and Mesoproterozoic mixed siliciclastic and carbonate sedimentary rocks, and chert from Depositional packages 1, 2 and 3 of the 1673-1455 Ma Edmund Group in the Western Capricorn Orogen. The type locality (Lat. -24.256 Long 116.619) is on Mount Augustus Station, Shire of Upper Gascoyne, Western Australia, Australia. Access to the locality is about 30 km west-northwest of the Mount Augustus Station by an unsealed Cobra-Mount Augustus road, then about 3.3 km southwest of the road. The Mount Augustus Station is a homestead just off the Landor-Mount Augustus road. It is located about 360 km northwest of Meekatharra via Landor-Meekatharra road and Landor-Mount Augustus road. The Mount Augustus Station is about 1000 km north of Perth.|16-MAY-23
79111|Waldburg Dolerite|Extent|On MANGAROON, MOUNT PHILLIPS, MOUNT AUGUSTUS, and CANDOLLE 1: 100 000 scale map sheets, Western Australia.|16-MAY-23
79111|Waldburg Dolerite|General description|The Waldburg Dolerite sills were emplaced in a structural corridor between two major fault structures, the Lyons River Fault and the Ti Tree Shear Zone within the Western Capricorn Orogen. The sills intrude Paleoproterozoic and Mesoproterozoic metasedimentary rocks of the middle and lower parts of the Edmund Group.|16-MAY-23
79111|Waldburg Dolerite|Thickness range|Thickness in type area 100-150 m. Range in thickness from 100 to 500 m, with the strike length up to 36 km.|16-MAY-23
79111|Waldburg Dolerite|Lithology|The mafic rocks are massive medium- to very-coarse grained moderately- to distinctly-weathered dolerite and/or a very coarse-grained leucogabbro. At some localities the dolerites are intruded by a network of thin (1-4 cm) felsic quartz -feldspar veinlets interpreted as the final phase of magmatic crystallization. Plagioclase and pyroxene are the main primary minerals but are extensively altered to low- to medium-grade metamorphic minerals including epidote, clinozoisite, amphibole, actinolite, tremolite, chlorite, albite, sericite, sauccurite, and lesser amount of hornblende, biotite and pleonaste.|16-MAY-23
79111|Waldburg Dolerite|Depositional environment|Melt source and depth of melting estimated from TiO2/Yb, Th/Yb, and Nb/Yb contents show that the Waldburg Dolerite has a narrow range of compositions intermediate to OIB and N-MORB, generally equivalent to those of E-MORB, suggesting that they were derived from relatively shallow?mantle melting depths. The dolerite samples show a very narrow trend parallel to the MORB-OIB array, which may indicate derivation from a mildly heterogeneous mantle source.|16-MAY-23
79111|Waldburg Dolerite|Relationships and boundaries|On MOUNT AUGUSTUS the Waldburg Dolerite dolerite sills intruded into silicified siltstone and sandstone of the 1590-1514 Ma Kiangi Creek Formation at, or near, a fault contact with dolostone of the 1673-1610 Ma Irregully Formation of the 1673-1455 Ma Edmund Group (GSWA Explanatory Notes System).|16-MAY-23
79111|Waldburg Dolerite|Identifying features|The Waldburg Dolerite sills are highly altered, strongly fractured, and exhibit spheroidal weathering. The sills consist mainly of medium- to coarse-grained dolerite with rare felsic veins of predominantly granophyric quartz-plagioclase composition, up to 4 cm thick. In most cases, these felsic veins are interpreted as late-magmatic fractionates that filled cooling fractures in dolerite host.|16-MAY-23
79111|Waldburg Dolerite|Structure and Metamorphism|Metamorphosed under low- to medium-grade conditions, although primary ophitic to allotriomorphic-granular textures are typically well-preserved.|16-MAY-23
79111|Waldburg Dolerite|Age reasons|Four samples of Waldburg Dolerite sills yielded U-Pb zircon and/or baddeleyite crystallization ages of 1517-1505 Ma. Two sills, sampled near Mount Augustus Station, intruded Depositional Package 3 (Kiangi Creek Formation). These are dated at 1517 +/- 8 and 1513 +/- 5 Ma using zircons recovered from granophyric quartz-plagioclase veinlets interpreted as late-magmatic fractionates. A similar crystallization age of 1514 +/- 5 Ma was obtained from combined analyses of zircon and baddeleyite extracted from very coarse-grained leucogabbro within mainly medium-grained dolerite in a sill intruded at the base of Depositional Package 1 (Yilgatherra Formation) on MANGAROON 100k mapsheet. Medium- to coarse-grained dolerite of the fourth sill, which also intruded Depositional Package 1 (Irregully Formation), was sampled on CANDOLLE 100k mapsheet, and yielded zircons that indicated a crystallization age of 1505 +/-  3 Ma (GSWA Explanatory Notes System).|16-MAY-23
79111|Waldburg Dolerite|Correlations|The current status of knowledge shows no correlation between the Waldburg Dolerite and other contemporaneous igneous units in the western Capricorn Orogen.|16-MAY-23
79111|Waldburg Dolerite|Alteration and Mineralisation|Typically highly altered; secondary minerals include epidote, actinolite, tremolite, amphibole, chlorite, clinozoisite group minerals, saussurite, and minor biotite, titanite, and iron-titanium oxide minerals.|16-MAY-23
79111|Waldburg Dolerite|Geophysical Expression|Difficult to identify in aeromagnetic images because the sills typically parallel the regional structural architecture and magnetic grain.|16-MAY-23
79111|Waldburg Dolerite|Geochemistry|High-Fe tholeiitic composition; relatively high MgO-Cr contents and notably low concentrations in most REE and HFSE. The mafic rocks show weak REE fractionation in both light REE and heavy REE with very slight light-REE enrichment, weak negative Nb anomalies and a relatively low average La/Nb ratio of 1.36. Distinctive Nd and Hf isotope compositions correspond respectively to two-stage depleted mantle model ages (TDM2) between 1.94 and 1.80 Ga, and depleted mantle model ages (TDM) between 1.84 and 1.71 Ga.|16-MAY-23
79111|Waldburg Dolerite|Defn author|Olga Blay 5-APR-2022.|16-MAY-23
79111|Waldburg Dolerite|Comments|The Waldburg Dolerite can be distinguished geochemically and isotopically from the Narimbunna and Kulkatharra Dolerites in the Western Capricorn Orogen. Insignificant Nb anomalies, minor REE (particularly heavy REE) fractionation, uniformly positive epsilonNd(i) values, and the least variation in Th/Yb indicate that the Waldburg Dolerite is the most primitive in composition compared with the other dolerites in the region and did not have significant interaction with evolved crustal material during its transport and emplacement history.|16-MAY-23
79111|Waldburg Dolerite|References|Blay, OA, Johnson, SP, Wingate, MTD, Thorne, AM, Kirkland, CL, Tessalina, SG and Cutten, HN 2018, A new Mesoproterozoic mafic intrusive event in the Capricorn Orogen, Western Australia, Geological Survey of Western Australia Record, 2018/4, 41p.|16-MAY-23
73257|Warakurna Supersuite|Name source|Named for the community of Warakurna, adjacent to the Giles Meteorological Station, in central Australia.  The name is also an Aboriginal word that refers to 'long, dark ridges' in the region.|16-MAY-23
73257|Warakurna Supersuite|Unit history|None; but name also used in Warakurna Large Igneous Province|16-MAY-23
73257|Warakurna Supersuite|Extent|Extends for approx. 1.7 million square kilometres in central and Western Australia.|16-MAY-23
73257|Warakurna Supersuite|Age reasons|Numerous U-Pb and other dates:  c. 1078 - 1050 Ma.|16-MAY-23
73257|Warakurna Supersuite|Defn Reference|Howard, H.M., Smithies, R.H., Pirajno, F., Skwarnecki, M.S., 2006. Bates, W.A., Sheet 4646, Geological Survey of Western Australia, 1:100,000 Geological Series.|16-MAY-23
29116|Warambie Basalt|Name source|Warambie Homestead; grid reference 20o57', 117o22', Roebourne 1:250 000 Sheet area.|16-MAY-23
29116|Warambie Basalt|Type section locality|200 metres of massive basalt in close proximity to Warambie Homestead.|16-MAY-23
29116|Warambie Basalt|Extent|The unit is exposed in an arcuate belt between Warambie Homestead and Whim Creek, on the Roebourne 1:250 000 Sheet.|16-MAY-23
29116|Warambie Basalt|Thickness range|Range 100-200 metres.|16-MAY-23
29116|Warambie Basalt|Lithology|A fine-grained grey-green amygdaloidal mafic volcanic, ranging in composition from andesite to basalt. Rare glomeroporphyritic plagioclase has been observed. Minor pyroclastic horizons and ultramafic flows occur near the base of the unit locally.|16-MAY-23
29116|Warambie Basalt|Relationships and boundaries|Appears to unconformably overlie either rocks of the Teichmans Group or Caines Well granite. It is conformably overlain by the Mons Cupri Volcananics.|16-MAY-23
29116|Warambie Basalt|Age reasons|Structural complexity and stratigraphic position suggest an Upper Archaean age. Geochronology on a unit within the Mons Cupri Volcanics has been published (Compston & Ariens, 1967) at an age of 3050 m.y. but more recently Ariens has revised this date to an age approximately in the range between 2 500 and 2 300 m.y.; the Warambie Basalt is thus older.|16-MAY-23
29116|Warambie Basalt|Defn author|Fitton M.J., Horwitz R.C., Sylvester G., 1975|16-MAY-23
29116|Warambie Basalt|Proposed publication|CSIRO, Minerals Research Laboratories, Report No. FP 11|16-MAY-23
29116|Warambie Basalt|State(s)|Warambie Basalt|16-MAY-23
78850|Weerianna Basalt|Name source|Weerianna Hill (Lat. 20°45'56" S, Long. 117°07'11" E), 2 km west of Roebourne|16-MAY-23
78850|Weerianna Basalt|Type section locality|Weerianna Hill (Lat. 20°45'56" S, Long. 117°07'11" E), 2 km west of Roebourne|16-MAY-23
78850|Weerianna Basalt|Extent|From Mount Wangee, through Roebourne, southwest to Nickol River, outcropping over an area of 100 km2|16-MAY-23
78850|Weerianna Basalt|Thickness range|Approximately 1000 m at Weerianna Hill and Mount Wangee, becoming thinner southwest towards Nickol River. Southwest thinning is attributed to deformation beneath the Regal Thrust|16-MAY-23
78850|Weerianna Basalt|Lithology|Metamorphosed basalt, including fine-grained komatiitic basalt.|16-MAY-23
78850|Weerianna Basalt|Relationships and boundaries|Formation of the Roebourne Group and conformably overlies the Ruth Well Formation. Overlain, across a faulted unconformity, by the c. 3220 Ma Nickol River Formation. Intruded by irregular sills and dykes of gabbro and dolerite related to the c. 3015 Ma Andover Intrusion. Intruded by rhyolite and dacite sills and stocks of the c. 3015 Ma Orpheus Supersuite.|16-MAY-23
78850|Weerianna Basalt|Age reasons|Minimum age c. 3270 Ma.  The Ruth Well Formation, conformably underlying the Weerianna Basalt, is intruded by the 3270-3261 Ma Karratha Granodiorite. Maximum age c. 3330 Ma based on unpublished Nd isotopic data from the Ruth Well Formation.|16-MAY-23
26211|Whim Creek Group|Name source|Whim Creek centre (20o52'S, 117o50'E) Roebourne 1:250 000 Sheet areas.|16-MAY-23
26211|Whim Creek Group|Name source|Whim Creek Townsite and Mine; 20o51'S and 117o51'E on the Roebourne Sheet.|16-MAY-23
26211|Whim Creek Group|Unit history|Whim Creek Group of (1). Reasons for redefinition of the Whim Creek Group were published in (2). As defined by (1) the group includes the Mosquito Creek Formation (Mallina Formation of (1)) and the Lalla Rookh Sandstone (Constantine Sandstone of (1)) but these formations are currently regarded as forming part of the Gorge Creek Group (as originally defined in (4)). As stated in (2) the Mons Cupri Volcanics overlies the Mallina Formation (Mosquito Creek Formation) 15 km southeast of Sherlock. Also, the Whim Creek Group is less deformed than the Gorge Creek Group, lying immediately adjacent to the south.|16-MAY-23
26211|Whim Creek Group|Type section locality|Between Whim Creek centre and Mons Cupri (20o53'S, 117o48'E), but no single section affords a complete succession of the entire group.|16-MAY-23
26211|Whim Creek Group|Type section locality|The lower part of the sequence is well exposed 2.5 km east of Mons Cupri while the upper part is well exposed in the immediate vicinity of Whim Creek Mine.|16-MAY-23
26211|Whim Creek Group|Extent|Approx. 100 km2 between Mount Negri (20o53'S, 117o48'E), but no single section affords a complete succession of the entire group.|16-MAY-23
26211|Whim Creek Group|Extent|Rocks of this unit are widely exposed between Whim Creek, Warambie Station, Kangan and to the west of Kangan some 80 km.|16-MAY-23
26211|Whim Creek Group|Thickness range|Approx. 900 m|16-MAY-23
26211|Whim Creek Group|Lithology|The unit is composed of four named formations: (1) The Warambie Basalt, (2) The ;Mons Cupri Volcanics, (3) The Constantine Sandstone, (4) The Mallina Formation.|16-MAY-23
26211|Whim Creek Group|Relationships and boundaries|Unconformably overlies the Warrawoona Group (equivalent to Teichmans Group of (1)) 4 km west of Mount Fraser (20o56'S, 117o33'E). See (1) and (2). Conformably or disconformably overlies the Gorge Creek Group (4) 15 km south east of Sherlock homestead (20o53'S, 117o38'E). See (2). Unconformably overlain by the Negri Volcanics (1), and newly redefined to appear in (3)) at Mount Negri and southwest of Mons Cupri. Unconformably overlain by the Fortescue Group (Lower Proterozoic) 3 km west-northwest of Warambie. Low angle unconformity separates the group from rocks correlated with the overlying Louden Volcanics (newly defined and to appear in (3) approx. 10 km south-southeast of Sherlock homestead.|16-MAY-23
26211|Whim Creek Group|Relationships and boundaries|The unit is underlain unconformably by the Caines Well Granite or the Teichmans Group and overlain (probably disconformably by the Negri Volcanics).|16-MAY-23
26211|Whim Creek Group|Age reasons|Late Archaean. Unpublished geochronology indicates an age of approx. 2700-2600 my.|16-MAY-23
26211|Whim Creek Group|Age reasons|Upper Archaean|16-MAY-23
26211|Whim Creek Group|Proposed publication|Geology of the Pilbara Block and its environs GSWA Bull.|16-MAY-23
26211|Whim Creek Group|Proposed publication|CSIRO, Minerals Research Laboratories, Report No. FP 11|16-MAY-23
26211|Whim Creek Group|Apprdate|14-SEP-1979|16-MAY-23
26211|Whim Creek Group|Defn approved by|Western Australia|16-MAY-23
26211|Whim Creek Group|Defn approved by|Western Australia|16-MAY-23
26211|Whim Creek Group|Proposer|Hickman A.H.|16-MAY-23
26211|Whim Creek Group|Proposer|Fitton M.J. Horwitz R.C., Sylvester G.|16-MAY-23
26211|Whim Creek Group|Status|1|16-MAY-23
20090|Williamstown Dolerite|Name source|From Williamstown, a suburban area immediately east of the Kalgoorlie townsite.|16-MAY-23
20090|Williamstown Dolerite|Type section locality|Outcrops and old shaft dumps one mile north of Williamstown, near the Transcontinental Railway cutting (30deg44'00"S, 121deg28'45"E)|16-MAY-23
20090|Williamstown Dolerite|Extent|In several belts trending north-north-west and south-south-east, the repetition being due to folding. One belt runs north-north-west from Williamstown for at least 3 miles; another runs from the western limits of the Golden Mile northwards through the Kalgoorlie-Boulder townsites and south-south-west [?east] for four miles before lensing out.|16-MAY-23
20090|Williamstown Dolerite|General description|Outcrop pattern: Rare isolated rises, in either a fresh or oxidised state. Specimens collected and analysed by the Geological Survey of Western Auatralia illustrate the variation in the sill. Numbers 1745, 11003, 11029, 11105, 13424 and 13454 have analyses published in Bulletin Nos. 6, 42, 51, 67, 69 and 94.|16-MAY-23
20090|Williamstown Dolerite|Thickness range|Approximately 1000 ft thick [305 m)|16-MAY-23
20090|Williamstown Dolerite|Lithology|A differentiated sill, the lower half being ultrabasic (hornblendite) transitional through meta-gabbro or meta-dolerite to meta-quartz-dolerite in the upper portion. Some altered chloritic varieties occur, which, in the ultrabasic section of the sill, contain talc and/or phlogopitic mica.|16-MAY-23
20090|Williamstown Dolerite|Relationships and boundaries|Conformably overlies the Devon Consols Basalt and is conformably overlain by the Paringa Basalt, but some minor discordance is probable, as indicated by inliers of basalt in some areas. The lower contact is usually marked by the Kapai Slate.|16-MAY-23
20090|Williamstown Dolerite|Age reasons|Archaean.|16-MAY-23
20090|Williamstown Dolerite|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
20090|Williamstown Dolerite|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
20090|Williamstown Dolerite|References|GSWA Bulletin Nos. 6, 42, 51, 67, 69 and 94.  **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
74629|Willie Creek Calcarenite|Name source|Willie Creek, latitude/longitude coordinates 17º 45' 54" S, 122º 12' 56" E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
74629|Willie Creek Calcarenite|Geomorphic expression|Exposed as cliffs along tidal creel banks and along open coast that are cut into the calcarenite.|16-MAY-23
74629|Willie Creek Calcarenite|Type section locality|Cliff exposure on shores of Willie Creek, latitude/longitude coordinates 17º 46' 07" S, 122º 12' 55" E, Broome 1:250,000 Topographical Sheet.|16-MAY-23
74629|Willie Creek Calcarenite|Description at type locality|300 cm low-angle cross-layered to cross-bedded and laminated burrow-structured to bioturbated fine-grained to medium grained calcarenite and shelly calcarenite; base not exposed.|16-MAY-23
74629|Willie Creek Calcarenite|Extent|The unit is widespread along the Canning Coast as a semi-continuous to scattered ribbon deposit.|16-MAY-23
74629|Willie Creek Calcarenite|Thickness range|Thickness at type locality is 3 m.  Additionally, where exposed along the coast the Formation has been recorded 3-5 m thick, but can be up to 7 m thick.  Regionally, the unit will appear as a discontinuous ribbon deposit, individually, some tens of metres to several hundred of metres long, but only up to 100 m wide and generally 3-5 m thick.|16-MAY-23
74629|Willie Creek Calcarenite|Lithology|A fine to medium to coarse sand-sized bioclastic and quartzose calcarenite, with layers of shells. Sand grains are quartz, lithoclasts, intraclasts, molluscs fragments, and oolitically coated grains.  The cementing agent is sparry calcite. It is burrow-structured to bioturbated to laminated and bedded.|16-MAY-23
74629|Willie Creek Calcarenite|Depositional environment|Mid-Holocene mid-low tidal sand flat  environment.|16-MAY-23
74629|Willie Creek Calcarenite|Fossils|Bivalves: Acrosterigma fultoni, Acrosterigma vlamingi, Anadara crebricostata, Anomalocardia squamosa, Barbatia coma, Barbatia foliata, Callista impar, Donax faba, Donax cf. faba, Dosinia scalaris, Gafrarium tumidum, Saccostrea cucullata, Semele jukesii, Tellina virgata, an unidentified Cardiid, and an unidentified Venerid.  Gastropods: Conus sp. and Strombus campbelli.|16-MAY-23
74629|Willie Creek Calcarenite|Relationships and boundaries|Mostly the Formation is overlain by the Kennedys Cottage Limestone, but locally it may be overlain directly with sharp contact by the Horsewater Soak Calcarenite.  At the type location, indurated beach deposits of the Kennedys Cottage Limestone overlie the formation. Where cut by more recent channels, the Formation is overlain by channel-fills composed of Christine Point Clay and/or Sandfire Calcilutite.  Where exposed, the Formation rests with sharp contact on pre-Holocene Formations such as Mowanjum Sand (Semeniuk), or red ironstone gravel, or palaeosol developed on Pleistocene limestone.|16-MAY-23
74629|Willie Creek Calcarenite|Age reasons|Radiocarbon dating of shells within the Formation places it in the Holocene, viz., 3060 ± 600 yrs BP and 6910 +/-180 yrs BP.|16-MAY-23
74629|Willie Creek Calcarenite|Correlations|The formation is laterally equivalent to older parts of the Sandfire Calcilutite in the region.|16-MAY-23
74629|Willie Creek Calcarenite|Comments|Low-angle cross-layered to cross-bedded and laminated burrow-structured to bioturbated fine-grained to medium grained calcarenite and shelly calcarenite.|16-MAY-23
74629|Willie Creek Calcarenite|References|For Canning Coast units: Semeniuk, V. 2008. Holocene sedimentation, stratigraphy, biostratigraphy and history of the Canning Coast, north-western Australia. Journal of the Royal Society of Western Australia, Volume 91 Part 1 (Supplement): 53-148.For Mowanjum Sand: Semeniuk V 1980 Quaternary stratigraphy of the tidal flats King Sound, WA. Journal of the Royal Society of Western Australia 63: 65-78.|16-MAY-23
30320|Windoo Sandstone|Name source|Windoo Hill, GR , Nicholson 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area.|16-MAY-23
30320|Windoo Sandstone|Unit history|( No synonymy given)|16-MAY-23
30320|Windoo Sandstone|Geomorphic expression|Low hills and small mesas.|16-MAY-23
30320|Windoo Sandstone|Type section locality|At GR DE733765, Nicholson 1:100 000 Sheet area, where Cambrian Antrim Plateau Volcanics are overlain by 20 m of flat-lying sandstone, mapped as Windoo Sandstone, forming a small mesa.|16-MAY-23
30320|Windoo Sandstone|Extent| Nicholson 1:100 000 Sheet area, Gordon Downs 1:250 000 Sheet area, W.A.|16-MAY-23
30320|Windoo Sandstone|Thickness range|Maximum probably less than 50 m.|16-MAY-23
30320|Windoo Sandstone|Lithology|Thin to thick bedded, variably lithic quartz sandstone, ripple marks and  large-scale convolute bedding common; thinly bedded claystone and dolomitic mudstone present locally at base and stromatolitic chert present locally near top.|16-MAY-23
30320|Windoo Sandstone|Depositional environment|Shallow marine?|16-MAY-23
30320|Windoo Sandstone|Relationships and boundaries|Overlies, probably disconformably, Antrim Plateau Volcanics; top not seen.|16-MAY-23
30320|Windoo Sandstone|Age reasons|Palaeozoic - Cambrian or younger.|16-MAY-23
30320|Windoo Sandstone|Correlations|May be similar in age to sandstone in the Elder Subgroup of the Cambrian Goose Hole Group or in the Devonian Mahony Group of the Ord Basin succession.|16-MAY-23
30320|Windoo Sandstone|Comments| Previously mapped as Gardiner beds (Gemuts & Smith 1968).|16-MAY-23
30320|Windoo Sandstone|References|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
24577|Winemaya Quartzite|Name source|Winemaya Spring, 10.5 km north of the type section (30o14'S; 115o59'E). Moora 1:250 000 Sheet area.|16-MAY-23
24577|Winemaya Quartzite|Type section locality|1 365 m of bedded light grey orthoquartzites, with minor red-brown and grey siltstone and chert. The section commences about 4 km west of Longreach Homestead and extends for some 2.2 km to the east-northeast.|16-MAY-23
24577|Winemaya Quartzite|Extent|Scattered exposures over a belt 5 km wide extending from 9 km northwest of Watheroo to 13 km northwest of Marchagee.|16-MAY-23
24577|Winemaya Quartzite|Thickness range|The type section is the only section that has been measured. The top is not exposed and it is likely that a considerable additional thickness is obscured by Quaternary deposits.|16-MAY-23
24577|Winemaya Quartzite|Lithology|Orthoquartzite, light grey to medium grey, fine- to coarse-grained with some pebble conglomerate with chert and orthoquartzite clasts: with minor red-brown and grey micaceous siltstone and chert.|16-MAY-23
24577|Winemaya Quartzite|Relationships and boundaries|The Winemaya Quartzite rests with apparent conformity on the Noingara Siltstone. The top of the formation is not exposed. The base of the formation is defined by a unit, 245 m thick, consisting of light-grey, coarse-grained, orthoquartzite, well bedded towards the top, with occasional thin beds of pebble conglomerate.|16-MAY-23
24577|Winemaya Quartzite|Age reasons|No fossils have so far been found in the Winemaya Quartzite. However, the unit is believed to be of Proterozoic age because of its relationship with underlying formations of the Moora Group.|16-MAY-23
24577|Winemaya Quartzite|Proposed publication|Geology of Western Australia; West. Aust. Geol. Survey, Memoir 2; in press.|16-MAY-23
24577|Winemaya Quartzite|Proposer|Low G.H.|16-MAY-23
24577|Winemaya Quartzite|Resdate|15-JAN-1975|16-MAY-23
27255|Winifred Formation|Name source|Lake Winifred (22o45'S, 123o30'E)|16-MAY-23
27255|Winifred Formation|Unit history|Middle part of Grant Formation (Guppy et al., 1952) now termed Grant Group. Referred to as Dora Shale by Koop (1966) and as "middle shale unit" by Crowe & Towner (1976).|16-MAY-23
27255|Winifred Formation|Type section locality|Section at 22o52'40"S, 123o36'20"E near Well 26 on the Tabletop Sheet area. A subsurface reference section between 814-1069 m in Kidson No. 1 (22o36'59"S, 125o00'16"E) is also designated.|16-MAY-23
27255|Winifred Formation|Extent|Only exposures so far identified occur in Well 26-27 area near L. Winifred, Canning Basin. In subsurface the unit has been traced throughout the basin.|16-MAY-23
27255|Winifred Formation|Thickness range|Up to 100 m thick in Fitzroy Trough-Lennard Shelf area; up to 190 m thick in Gregory Sub-basin; up to 256 m in Kidson Sub-basin.|16-MAY-23
27255|Winifred Formation|Lithology|On the surface the unit is composed of mudstone with minor very fine-grained quartz wacke. Subsurface sections contain a similar lithology.|16-MAY-23
27255|Winifred Formation|Relationships and boundaries|Conformably overlain by Carolyn Formation except where overlapped. Conformably overlies Betty Formation and probably interfingers laterally with the Paterson Formation.|16-MAY-23
27255|Winifred Formation|Age reasons|Sakmarian sensu lato based on palynological evidence (Broad & McDermott, 1974).B8|16-MAY-23
27255|Winifred Formation|Proposed publication|Annual Report Geological Survey of Western Australia for 1976|16-MAY-23
27255|Winifred Formation|Reserved? Yes/No|Yes|16-MAY-23
80380|Wonangara Member|Name source|Named after Wonangara Well (Lat. -22.89035 Long. 116.61525) about 30 km west-southwest of the proposed type section, on the HARDEY 1:100 000 mapsheet|16-MAY-23
80380|Wonangara Member|Unit history|Equivalent to part of the lower Kazput Formation as originally defined by Thorne and Tyler (1996), as well as the lower part of all previous equivalent informal units. The unit has been named in recognition of the fact that it contains diamictite of potential glacial origin that may be important in global correlation of Paleoproterozoic glaciations.|16-MAY-23
80380|Wonangara Member|Geomorphic expression|Poorly exposed and generally extensively weathered.|16-MAY-23
80380|Wonangara Member|Type section locality|The Wonangara Member is not well exposed, but the best outcrops, especially of the characteristic diamictites, can be found in the vicinity of Lat. -22.86489 Long. 116.91078 in the core of the Hardey Syncline. It is also well exposed in a small creek in the vicinity of Lat. -22.87330 Long. 116.95397.|16-MAY-23
80380|Wonangara Member|Extent|Only present in the Hardey Syncline|16-MAY-23
80380|Wonangara Member|Thickness range|The total thickness in the type area is about 108 m, with the exposed diamictite component about 5-10 m thick. Thickness variations unknown due to poor exposure and access, as well as truncation by unconformities and faults. However, the measured thickness ranges from about 100-500 m. The diamictite component is about 15-20 m thick.|16-MAY-23
80380|Wonangara Member|Lithology|The diagnostic lithology is a matrix supported conglomerate with a muddy sandstone matrix, interpreted as a glacigenic diamictite, that has been found in three localities in the core of the Hardey Syncline. The diamictite is intensely weathered wherever it is in close proximity to the Munder Formation basal unconformity. However, the bulk of the Wonangara Member consists of planar-laminated siltstone with minor interbedded fine-grained sandstone, commonly with hummocky and swaley cross-lamination.|16-MAY-23
80380|Wonangara Member|Depositional environment|Deep-marine glacigenic diamictite deposited below storm wave-base and most likely reworked by mass flow.|16-MAY-23
80380|Wonangara Member|Relationships and boundaries|The basal contact with interbedded dolomites and shales in the basal Kazput Formation is poorly exposed and commonly covered by scree, but appears to be abrupt and conformable. The Wonangara Member is unconformably overlain by the Munder Formation on an irregular contact at the type locality. Further east, a similar lithology is present below the Munder Formation unconformity (Lat. ?22.873 Long. 116.954) but appears from aerial photographic interpretation to be at a similar stratigraphic level.|16-MAY-23
80380|Wonangara Member|Identifying features|The diamictite component of the Wonangara Member is commonly strongly weathered and saprolitic. Elsewhere in the type area it could easily be mistaken for regolith if contact relationships are not well preserved or exposed.|16-MAY-23
80380|Wonangara Member|Age reasons|The Wonangara Member is older than the 2208 Ma Balgara Dolerite (Muller et al., 2005) which post-dates the Turee Creek and Shingle Creek Groups (Martin and Morris, 2010), and is younger than the 2340 +/- 22 Ma maximum depositional age (Caquineau et al., 2016; 2018) and 2312.7 +/- 5.6 Ma diagenetic age (Philippot et al. 2018) of the Meteorite Bore Member in the underlying Kungarra Formation.|16-MAY-23
80380|Wonangara Member|Defn author|D. McB. Martin, Geological Survey of Western Australia 7-JUL-2020.|16-MAY-23
80380|Wonangara Member|Proposed publication|GSWA Report 203|16-MAY-23
80380|Wonangara Member|References|Caquineau, T, Paquette, J-L and Philippot, P 2016, In situ U-Pb zircon dating of the Meteorite Bore Member diamictites: constraints on the Paleoproterozoic glaciations and the Great Oxidation Event, in Goldschmidt Conference Abstracts: Goldschmidt Conference, Yokohama, Japan, 26 June 2016-1 July 2016, p. 364.   **Caquineau, T, Paquette, J-L and Philippot, P 2018, U-Pb detrital zircon geochronology of the Turee Creek Group, Hamersley Basin, Western Australia: Timing and correlation of the Paleoproterozoic glaciations: Precambrian Research, v. 307, p. 34-50.   **Martin, DMcB and Morris, PA 2010, Tectonic setting and regional implications of ca. 2.2 Ga mafic magmatism in the southern Hamersley Province, Western Australia: Australian Journal of Earth Sciences, v. 57, no. 7, p. 911-931.  **Muller, SG, Krapez, B, Barley, ME and Fletcher, IR 2005, Giant iron-ore deposits of the Hamersley province related to the breakup of Paleoproterozoic Australia: New insights from in situ SHRIMP dating of baddeleyite from mafic intrusions: Geology, v. 33, no. 7, p. 577-580.   **Philippot, P 2018, Avila, JN, Killingsworth, BA, Tessalina, S, Baton, F, Caquineau, T, Muller, E, Pecoits, E, Cartigny, P, Lalonde, SV, Ireland, TR, Thomazo, C, Van Kranendonk, MJ and Busigny, V, 2018, Globally asynchronous sulphur isotope signals require re-definition of the Great Oxidation Event: Nature Communications, v.9, Article number 2245, 10 p.  **Thorne AM and Tyler IM 1996, Geology of the Rocklea 1:100 000 sheet: Western Australia Geological Survey, 1:100 000 Geological Series Explanatory Notes, 15p.|16-MAY-23
81974|Wooly Formation|Name source|The original definition by Seymour et al. (1988) did not specify the origin of the name, but it is assumed to be derived from Wooly Bore (Lat. -22.8699 Long. 116.5243) about 12 km southwest of the type area on the WYLOO 1:100 000 map sheet.|16-MAY-23
81974|Wooly Formation|Unit history|The Wooly Formation (formerly Wooly Dolomite) occupies the same relative stratigraphic position as the Mount McGrath Beds of MacLeod et al. (1963) and the Coolbye Shale Member of Halligan and Daniels (1964) and De La Hunty (1965). However, it was mapped as part of the obsolete Turee Creek Formation by Daniels (1970). The Wooly Dolomite was first recognised by Seymour et al. (1988) as a distinct lithological unit that conformably overlies the Cheela Springs Basalt and is unconformably overlain by the Mount McGrath Formation. The revised name reflects the fact that new mapping has shown that it is much more extensive than originally mapped (Krapez et al., 2015), and dolomite is a subordinate component of this stratigraphic interval which consists of a larger proportion of fine-grained siliciclastic rocks.|16-MAY-23
81974|Wooly Formation|Geomorphic expression|The Wooly Formation is generally poorly exposed, mostly forming regolith-covered flats with occasional small outcrops. Where it is well-exposed, it consists of steep-sided low hills of dolomite, usually in close proximity to the Mount McGrath Formation basal unconformity.|16-MAY-23
81974|Wooly Formation|Type section locality|The original type area is on the southern limb of the Wyloo Anticline, between Lat. -22.7855 Long. 116.42 and Lat. -22.8043 Long. 116.4892 on the WYLOO 1:100 000 mapsheet (Seymour et al., 1988; Thorne and Seymour, 1991) where the unit is exceptionally well exposed. Reference localities where the lithological variability of the revised unit is well developed are proposed in the headwaters of Urandy Creek at Lat. -22.2401 Long. 116.2952, in the vicinity of Urandy Creek Outcamp (centred on Lat. -22.2744 Long. 116.2727), and on Duck Creek (at Lat. -22.4742 Long. 116.3518), all on the MOUNT STUART 1:100 000 mapsheet.|16-MAY-23
81974|Wooly Formation|Extent|The redefined Wooly Formation is considerably more extensive that the original Wooly Dolomite, with the currently mapped distribution extending discontinuously over about 300 km of strike from about 20 km west of Pannawonica in the northwest, to the Mount Olympus area in the southeast. This greater extent is due to the fact that it was previously included in the Mount McGrath Formation outside of the original type area.|16-MAY-23
81974|Wooly Formation|General description|Outside of the original type area, shale, carbonaceous shale, and medium- to coarse-grained siliciclastic rocks constitute a larger proportion of the unit, but are interbedded with carbonates which is a distinguishing feature. Thin vesicular to amygdaloidal basaltic flows are also present locally, especially in the vicinity of the Red Hill copper prospect. The basal contact is either an erosional contact with significant relief or a low-angle unconformity. The upper contact is an angular unconformity with the Mount McGrath Formation.|16-MAY-23
81974|Wooly Formation|Thickness range|325 m in the original type area on the southern margin of the Wyloo Anticline. The Wooly Formation has a maximum thickness of 325 m in the original type area. According to Krapez et al. (2015) it is thinner and much more variable outside of this area, where it attains a maximum thickness of about 175 m. However, poor exposure and extensive faulting outside of the original type area make accurate thickness estimation difficult.|16-MAY-23
81974|Wooly Formation|Lithology|In the original type area, the Wooly Formation comprises dolomite and dolomitic mudstone, with local stromatolites, and minor clastic intervals.|16-MAY-23
81974|Wooly Formation|Depositional environment|The Wooly Formation was predominantly deposited in a marine environment below storm wave-base, although high-energy shallow marine and shoreline deposits are locally developed. The base of the formation consists locally of high-energy terrigenous clastic sedimentary rocks.|16-MAY-23
81974|Wooly Formation|Fossils|Stromatolites are present but not common in the dolomitic portions of the Wooly Formation.|16-MAY-23
81974|Wooly Formation|Relationships and boundaries|Originally considered to conformably overlie the Cheela Springs Basalt, and to be unconformably overlain by the Mount McGrath Formation (Seymour et al., 1988). However, the basal contact can now be shown to be an erosional surface with hundreds of metres of relief, that is onlapped by the Wooly Formation.|16-MAY-23
81974|Wooly Formation|Structure and Metamorphism|The Wooly Formation is cut by numerous normal faults, some of which have also been reactivated by dextral strike-slip motion. These faults make up what has previously been referred to as either the Nanjilgardy Fault or Menindee Fault Zone|16-MAY-23
81974|Wooly Formation|Age reasons|The Wooly Formation has a maximum depositional age of 2031 +/- 6 Ma (Muller et al., 2005) determined from a volcaniclastic sandstone near the base of the formation in the Mount Olympus area, and is older than the unconformably overlying Capricorn Group that has a maximum depositional age of 1801 +/- 6 Ma (Wingate et al., 2017).|16-MAY-23
81974|Wooly Formation|Alteration and Mineralisation|Mapping of the extent of the revised Wooly Formation shows that it hosts the Mount Olympus gold deposit.|16-MAY-23
81974|Wooly Formation|Defn author|D. McB. Martin, Geological Survey of Western Australia 7-JUL-2020.|16-MAY-23
81974|Wooly Formation|Proposed publication|GSWA Report 203|16-MAY-23
81974|Wooly Formation|References|Daniels, JL 1970, Wyloo, Western Australia: Geological Survey of Western Australia, 1:250 000 Explanatory Notes, 19p.  **de La Hunty, LE 1965, Mount Bruce, Western Australia: Bureau of Mineral Resources, Geology and Geophysics, 1:250 000 Geological Series Explanatory Notes, 28p.  **Halligan, R and Daniels, JL 1964, Precambrian geology of the Ashburton valley region, northwest Division: Western Australia Geological Survey, Annual Report 1963, p. 38-46.  **Krapez, B, Muller, SG and Bekker, A 2015, Stratigraphy of the Late Palaeoproterozoic (~2.03 Ga) Wooly Dolomite, Ashburton Province, Western Australia: A carbonate platform developed in a failed rift basin: Precambrian Research, v. 271, p. 1-19.  **MacLeod, WN, de la Hunty, LE, Jones, WR and Halligan, R 1963, Preliminary report on the Hamersley Iron Province, North West Division: Western Australia Geological Survey, Annual Report 1962, p. 44-54.   **Muller, SG, Krapez, B, Barley, ME and Fletcher, IR 2005, Giant iron-ore deposits of the Hamersley province related to the breakup of Paleoproterozoic Australia: New insights from in situ SHRIMP dating of baddeleyite from mafic intrusions: Geology, v. 33, no. 7, p. 577-580.  **Seymour, DB, Thorne, AM and Blight, DF 1988, Explanatory Notes on the Wyloo 1:250 000 geological sheet, Western Australia (2nd edition): Geological Survey of Western Australia, Record 1987/3, 69p.  **Wingate, MTD, Lu, Y, Fielding, IO and Johnson, SP 2017, 219526: felsic volcanic rock, Bali Lo deposit; Geochronology Record 1370: Geological Survey of Western Australia, 4p.|16-MAY-23
20708|Wye Worry Member|Name source|Wye Worry Bore, lat. 18o42'25"S, long. 125o15'20"E, on Cherrabun Station in the St George Range, Noonkanbah 1:250 000 Sheet area.|16-MAY-23
20708|Wye Worry Member|Type section locality|Latitude 18o46'25"S, longitude 125o18'50"E in the eastern St George Range.|16-MAY-23
20708|Wye Worry Member|Extent|The member crops out in the St George Range, the Poole Range, in the Lauris Range and in isolated hills around Fitzroy Crossing on the Noonkanbah Sheet area. It extends onto the Mt Ramsay 1:250 000 Sheet area to the east.|16-MAY-23
20708|Wye Worry Member|Thickness range|Range from 25 m in central St George Range to at least 95 m in type section.|16-MAY-23
20708|Wye Worry Member|Lithology|Mainly sandy siltstone and shale with calcareous concretions and striated and facetted glacial dropstones. Contains varves of graded silt and clay at the base. Contains lenses of tillitic conglomerate and is snady towards the top. In the Poole Range the member is slumped and deformed.|16-MAY-23
20708|Wye Worry Member|Relationships and boundaries|Overlies undivided Grant Formation probably disconformably. Conformably overlain by the Millajiddee Member in most of the St George Range and in the Poole Range; at Mt Thorlan and southwestern St George Range the Nura Nura Member of the Poole Sandstone rests unconformably on the Wye Worry Member.|16-MAY-23
20708|Wye Worry Member|Age reasons|Fauna consists of pelecypods, bryozoans, gastropods and brachiopods. The fauna has much in common with that of the upper part of the Lyons Group in the Carnarvon Basin. The age is Sakmarian.|16-MAY-23
20715|Wyloo Group|Name source|The derivation of the name was never specified in the original definition (MacLeod et al. 1963), but it most likely is taken from Wyloo Station (Lat. -22.6899 Long. 116.2330) on the WYLOO 1:250 000 map sheet (which may also be the origin of the name)|16-MAY-23
20715|Wyloo Group|Unit history|The Wyloo Group was originally defined by MacLeod et al. (1963) to include all strata in the combined Turee Creek, Shingle Creek and Wyloo Groups as currently defined. This definition persisted until it was revised by Trendall (1979), who recognised a major unconformity at the base of the Beasley River Quartzite, and consequently excluded the Turee Creek Group strata from the original definition. Following this, the Wyloo Group has commonly been further informally subdivided into lower and upper units, with the base of the latter defined by an unconformity at the base of the Mount McGrath Formation (Horwitz, 1980, 1982). This informal subdivision is hereby formalised by retaining the Wooly Formation (formerly Wooly Dolomite) as a separate unit, and renaming the remainder of the lower Wyloo Group as the Shingle Creek Group. The Wyloo Group now refers to all units above the base of the Mount McGrath Formation that formerly constituted the informal upper Wyloo Group.|16-MAY-23
20715|Wyloo Group|Constituents|Mount McGrath Formation, Duck Creek Dolomite, June Hill Volcanics, Ashburton Formation|16-MAY-23
20715|Wyloo Group|Geomorphic expression|The bulk of the Wyloo Group is poorly exposed, forming low hills that make up the Ashburton River valley. Locally it comprises some higher hills such as Mount Boggola, Mount Mortimer, Mount Clement, and Mount Stuart|16-MAY-23
20715|Wyloo Group|Type section locality|No type locality was specified in the original definition of MacLeod et al. (1963), or in the subsequent incomplete formal definition of Halligan and Daniels (1964) although the latter authors did recognize that the Wyloo Group occupies most of the Ashburton Valley and western margin of the Hamersley Range. For the purposes of this redefinition, the type area is considered to be the area between Mount DeCourcy (Lat. -22.7219 Long. 116.3042) and the Capricorn Range (Lat. -23.2498 Long. 116.6361).|16-MAY-23
20715|Wyloo Group|Extent|The Wyloo Group is the dominant unit exposed in the Ashburton River valley, between the top of the Shingle Creek Group and the base of the Bangemall Supergroup.|16-MAY-23
20715|Wyloo Group|Thickness range|The maximum thickness of the Wyloo Group is estimated to be about 12000 m, although the total thickness of the Wyloo Group is difficult to estimate because of the poor outcrop and stratigraphic repetition by folding and faulting (especially within the Ashburton Formation).|16-MAY-23
20715|Wyloo Group|Lithology|The Wyloo Group comprises conglomerate, sandstone, stromatolitic dolomite, shale and mafic and felsic volcanic rocks. The bulk of the group is represented by the turbidite sandstones and shales of the Ashburton Formation|16-MAY-23
20715|Wyloo Group|Fossils|Stromatolites are abundant in the Duck Creek Dolomite, and also locally within the Mount McGrath Formation. The Duck Creek Dolomite also contains an assemblage of filamentous microfossils that have been correlated with the Gunflint assemblage (Knoll and Barghoorn, 1976).|16-MAY-23
20715|Wyloo Group|Diastems or hiatuses|The Duck Creek Dolomite onlaps the Wyloo Anticline, and sparse geochronological data suggest that other hiatuses probably exist within the succession, but these have not yet been accurately identified.|16-MAY-23
20715|Wyloo Group|Relationships and boundaries|The base of the Wyloo Group is marked by an angular unconformity with all underlying units, and it is unconformably overlain by the Capricorn, Mount Minnie, Bresnahan, and Edmund Groups, as well as Phanerozoic rocks.|16-MAY-23
20715|Wyloo Group|Identifying features|Throughout much of the outcrop area, the Wyloo Group is characterised by the presence of two cleavages, whereas younger Proterozoic units tend to only have one cleavage.|16-MAY-23
20715|Wyloo Group|Structure and Metamorphism|The Wyloo Group has been deformed by two deformation events related to the Capricorn Orogeny, and has undergone greenschist facies metamorphism that increases in grade towards the southwest. There is local contact metamorphism around the Boolaloo Granodiorite|16-MAY-23
20715|Wyloo Group|Age reasons|The Wyloo Group is younger than the 2031 +/- 6 Ma maximum depositional age of the underlying Wooly Formation (Muller et al., 2005) and older than the unconformably overlying Capricorn Group that has a maximum depositional age of 1801 +/- 6 Ma (Wingate et al., 2017)|16-MAY-23
20715|Wyloo Group|Alteration and Mineralisation|Gold at Mt McGrath, Dead Finish, Star of the West, Top Camp, Soldier's Secret, Mount Mortimer, Gorge Creek. Base metals at Kooline (Pb), Bali Hi and Bali Low (Cu, Pb, Ag)|16-MAY-23
20715|Wyloo Group|Defn author|D. McB. Martin, Geological Survey of Western Australia 7-JUL-2020.|16-MAY-23
20715|Wyloo Group|Proposed publication|GSWA Report 203|16-MAY-23
20715|Wyloo Group|References|Halligan, R and Daniels, JL 1964, Precambrian geology of the Ashburton valley region, northwest Division: Western Australia Geological Survey, Annual Report 1963, p. 38-46.  **Horwitz, RC 1980, The Lower Proterozoic succession south of the Hamersley Iron Province between the Angelo and the Beasley Rivers. CSIRO Institute of Earth Resources Division of Mineralogy, Report FP 22, 19 p.  **Horwitz, RC 1982, Geological History of the Early Proterozoic Paraburdoo Hinge Zone, Western Australia: Precambrian Research, v. 19, p. 191-200.  **Knoll, AH and Barghoorn, ES 1976, A gunflint-type microbiota from the Duck Creek Dolomite, Western Australia. Origins of Life, v. 7, p. 417-423.  **MacLeod, WN, de la Hunty, LE, Jones, WR and Halligan, R 1963, Preliminary report on the Hamersley Iron Province, North West Division: Western Australia Geological Survey, Annual Report 1962, p. 44-54.   **Muller, SG, Krapez, B, Barley, ME and Fletcher, IR 2005, Giant iron-ore deposits of the Hamersley province related to the breakup of Paleoproterozoic Australia: New insights from in situ SHRIMP dating of baddeleyite from mafic intrusions: Geology, v. 33, no. 7, p. 577-580.  **Trendall, AF 1979, A revision of the Mount Bruce Supergroup, in Annual Report for the year 1978: Geological Survey of Western Australia, Perth, Western Australia, p. 63-71.  **Wingate, MTD, Lu, Y, Fielding, IO and Johnson, SP 2017. 219526. felsic volcanic rock, Bali Lo deposit. Geochronology Record 1370, Geological Survey of Western Australia, 4p.|16-MAY-23
26238|Wyman Formation|Name source|Wyman's Well (Military Grid 262 339), Marble Bar 1:250 000 Sheet area.|16-MAY-23
26238|Wyman Formation|Unit history|Rocks now assigned to this formation in the Wymans Well and Upper Budjan Creek areas were described by Noldart and Wyatt (1962, p.108-109) as belonging to the "Copper Hills porphyry".|16-MAY-23
26238|Wyman Formation|Type section locality|The type area is along Camel Creek south of Wyman's Well and near Fieldings Gully. The unit is also well exposed in the upper reaches of Budjan Creek.|16-MAY-23
26238|Wyman Formation|Extent|The Wyman Formation occurs in the central portion of the Warrawoona Syncline, south of Wyman's Well, in an arcuate belt near the eastern margin of Strelley Granite, north of Soanesville, in the Coongan Syncline and south of Kelly.|16-MAY-23
26238|Wyman Formation|Thickness range|The formation has a maximum thickness of about 1 km.|16-MAY-23
26238|Wyman Formation|Lithology|The formation typically consists of massive to schistose, flow banded, porphyritic and locally strikingly columnar jointed rhyolite. Further description of the rhyolite is given by Hickman and Lipple (in prep.) and chemical analyses of the rock are presented in their Table 14B. The formation also contains felsic tuff and agglomerate and minor basalt lava and agglomerate in the belt east of Strelley Granite. The columnar-jointing is well illustrated by photographs in Noldart and Wyatt (1962, p.108-109).|16-MAY-23
26238|Wyman Formation|Relationships and boundaries|The formation is conformable with the underlying Salgash Subgroup in the Warrawoona Syncline but unconformably overlies the Salgash Subgroup in the Kelly Belt and is there unconformably overlain by the Budjan Creek Formation. It is locally overlain unconformably by the Soanesville Subgroup in the Soanesville Belt.|16-MAY-23
26238|Wyman Formation|Proposed publication|West. Australia Geol. Survey 1:250 000 Geol. Series Explan. Notes|16-MAY-23
35993|Yangibana Granite|Name source|Yangibana Creek (411500E 7356300N, Zone 50, MGA 94) on the Edmund 100K sheet area|16-MAY-23
35993|Yangibana Granite|Unit history|Named and described by Pearson (1996) and mentioned by Pearson et al (1996). The definition expands on the distribution of the unit as described by Pearson (1996).|16-MAY-23
35993|Yangibana Granite|Geomorphic expression|Typically, low rounded hills covered in tors and boulders.|16-MAY-23
35993|Yangibana Granite|Type section locality|About 1.5km south of the Yangibana-Frasers REE prospect near the southern edge of the Edmund 100k sheet area, centred at 430100E 7349400N (Zone 50 MGA94). The locality can be accessed via station tracks from Gifford Creek Homestead to the prospect, then south off road. The locality is centred on a GSWA geochronology samples site (GSWA 169055). North of the site, toward the edge of the pluton, the granite contains numerous thin schlieren of biotite. About 500m north of the sample site, there is a contact with a phase of the Yangibana Granite that is rich in inclusions of metasedimentary rock.|16-MAY-23
35993|Yangibana Granite|Extent|The Yangibana Granite forms two plutons on the southern half of the Edmund 100k sheet area, as well as dykes and veins in the surrounding metasedimentary rocks.|16-MAY-23
35993|Yangibana Granite|Lithology|The Yangibana Granite is a massive, leucocratic, medium-grained biotite-muscovite syenogranite to monzogranite, which ranges from being equigranular to slightly porphyritic. Locally the granite contains clots of tourmaline. Large areas of the unit that are rich in inclusions of metasedimentary rock have been assigned to an un-named member of the unit.|16-MAY-23
35993|Yangibana Granite|Relationships and boundaries|Dykes and veins of the Yangibana Granite extensively intrude metasedimentary rocks of the Pooranoo Metamorphics. Dykes and veins of the granite intrude the Pimbyana Granite. The Dingo Creek Granite is unconformably overlain by sedimentary rocks of the Edmund Group (Bangemall Supergroup) in the southeastern corner of the Edmund 100K sheet.|16-MAY-23
35993|Yangibana Granite|Age reasons|The granite has been dated at two localities on the Edmund 100k sheet area: 4 km southeast of Fraser Well (GSWA sample 169055; Nelson, 2002) and 4 km southeast of Yangibana Bore (GSWA sample 169059; Nelson, 2002).  The two samples gave U-Pb SHRIMP ages of, respectively, 1659 +/-10 Ma and 1660 +/-9 Ma. These ages are comparable to other units of the Durlacher Supersuite.|16-MAY-23
35993|Yangibana Granite|Correlations|The Yangibana Granite is lithologically similar to, and probably coeval with, other leucocratic muscovite-biotite(-tourmaline) granites of the Durlacher Supersuite farther to the west and northwest on the Mangaroon and southern Maroonah 100k sheet areas.|16-MAY-23
35993|Yangibana Granite|References|Nelson D. R. 2002. Compilation of geochronology data 2001. Western Australia Geological Survey, Record 2002/2.**Pearson J. M. 1996. Alkaline rocks of the Gifford Creek Complex, Gascoyne Province, Western Australia - their petrogenetic and tectonic significance. PhD thesis (unpublished), University of Western Australia. **Pearson J. M. Taylor W. R. & Barley M. E. 1996. Geology of the alkaline Gifford Creek Complex, Gascoyne Complex, Western Australia. Australian Journal of Earth Sciences 43, 299-309.|16-MAY-23
82206|Yapukarninjarra Formation|Name source|The name Yapukarninjarra, meaning 'rocks underground', was provided by the Martu traditional owners of the land surrounding the type locality at Barnicarndy 1.|16-MAY-23
82206|Yapukarninjarra Formation|Unit history|This unit has not been previously distinguished as a separate formation, however it is inferred to equivalent to an interval of reddish, slightly arkosic, kaolinitic sandstone that overlies basement in Samphire Marsh 1. This interval was previously included in the Nambeet Formation, but can be distinguished from the overlying marine Fly Flat Member of that Formation in a similar way to the succession in Barnicarndy 1. It may also be equivalent to a red sandstone interval overlying basement in mineral drillhole PHD1 on the Lennard Shelf, currently included in the basal Kunian Sandstone of the Prices Creek Group.|16-MAY-23
82206|Yapukarninjarra Formation|Geomorphic expression|The Yapukarninjarra Formation has been recorded only in the subsurface.|16-MAY-23
82206|Yapukarninjarra Formation|Type section locality|Barnicarndy 1 well (-21.4785 degreesS, 121.7823E) between 2443 - 2585 m depth (142 m thick).|16-MAY-23
82206|Yapukarninjarra Formation|Extent|The Yapukarninjarra Formation, or likely equivalents, are recorded on both the western (Barnicarndy 1 and Samphire Marsh 1) and northeastern margins of the Canning Basin (tentative equivalent in PHD1) but has not been identified on the basement highs within the central Canning Basin. This formation likely exists in the main Canning Basin depocentres but has not been penetrated by drilling due to excessive depths.|16-MAY-23
82206|Yapukarninjarra Formation|General description|The Yapukarninjarra Formation has been identified in 3 subsurface locations: 1) Barnicarndy 1; stratigraphic drillhole in the Barnicarndy Graben in the southwest Canning Basin, underlying the Fly Flat Member, Nambeet Formation, 2) Samphire Marsh 1; petroleum exploration well in the Samphire Graben in the northwest Canning Basin, underlying the Fly Flat member, Nambeet Formation, 3) PHD1; mineral exploration drillhole in the Lennard Shelf, eastern Canning Basin|16-MAY-23
82206|Yapukarninjarra Formation|Thickness range|142 m thick at the type locality. The Yapukarninjarra Formation ranges from 142 m thick in Barnicarndy-1 to 112 m in PHD 1|16-MAY-23
82206|Yapukarninjarra Formation|Lithology|The Yapukarninjarra Formation is composed of red and grey, fine to coarse-grained quartz arenites with rare mottled bioturbation and local argillaceous sandy siltstone interbeds. Thin green claystone beds, most abundant near the base, are interpreted as bentonites.|16-MAY-23
82206|Yapukarninjarra Formation|Depositional environment|At the type section, the Yapukarninjarra Formation was deposited in an early rift, alluvial fan setting, with minor evidence of marine influence (bioturbation).|16-MAY-23
82206|Yapukarninjarra Formation|Fossils|No body fossils known. Rare bioturbation.|16-MAY-23
82206|Yapukarninjarra Formation|Relationships and boundaries|At the type section the Yapukarninjarra Formation lies stratigraphically between the Fly Flat Member of the Nambeet Formation (above) and the Yeneena Basin representing basement to the Canning Basin (below). The lower contact of the Yapukarninjarra Formation with the Yeneena Basin is an angular unconformity, while the upper contact with the Fly Flat Member is gradational.|16-MAY-23
82206|Yapukarninjarra Formation|Identifying features|Grain size, colour, diagenesis and proposed depositional environments, distinguish the alluvial fan deposited Yapukarninjarra Formation from the overlying shallow marine shoreface deposited Fly Flat Member. The unit is easily distinguished from the underlying Yeneena Basin basement which is steeply dipping and comprises weakly metamorphosed dolomites and weathered siltstone.|16-MAY-23
82206|Yapukarninjarra Formation|Structure and Metamorphism|Flat-lying to slightly dipping to the north in Barnicarndy 1. No metamorphism.|16-MAY-23
82206|Yapukarninjarra Formation|Age reasons|At the type section, the Yapukarninjarra Formation is assigned a maximum depositional age of 510 +/- 5 Ma based on the youngest dated detrital zircon from GSWA sample 237995 at 2577.05 - 2577.12 m depth in Barnicarndy 1 (Wingate et al., 2021). A minimum age constraint is provided by the late Tremadocian to early Floian biostratigraphic age of the upper part of the overlying Fly Flat Member.|16-MAY-23
82206|Yapukarninjarra Formation|Correlations|The Yapukarninjarra Formation is potentially the oldest sedimentary unit in the Canning Basin and has no formal equivalents.|16-MAY-23
82206|Yapukarninjarra Formation|Alteration and Mineralisation|None observed.|16-MAY-23
82206|Yapukarninjarra Formation|Geophysical Expression|The Yapukarninjarra Formation is seismically identifiable on the Kidson Sub-basin seismic line (18GA-KB1).|16-MAY-23
82206|Yapukarninjarra Formation|Geochemistry|X-ray diffraction of Yapukarninjarra Formation samples at the type section indicates a composition consisting of quartz (38.2 - 98.5%), k-feldspar (0- 6.8 %) and clay (1.3 - 53.7%).|16-MAY-23
82206|Yapukarninjarra Formation|Defn author|L Normore and P. Haines, 2-FEB-2022.|16-MAY-23
82206|Yapukarninjarra Formation|Comments|Ongoing biostratigraphic analysis may help better define the age of the Yapukarninjarra Formation.|16-MAY-23
82206|Yapukarninjarra Formation|References|Nicoll, RS, Laurie, JR and Roche, MT 1993, Revised stratigraphy of the Ordovician (late Tremadoc-Arenig) Prices Creek Group and Devonian Poulton Formation, Lennard Shelf, Canning Basin, Western Australia: Journal of Australian Geology and Geophysics, v. 14, p. 65-76.  **Normore, LS, Haines, PW, Carr, LK, Henson, P, Zhan, Y, Wingate, M, Zhen, YY, Lu, Y, Martin, S, Kelsey, D, Allen, H, and Fielding, I. 2021, Barnicarndy Graben, southern Canning Basin: stratigraphy defined by the Barnicarndy-1 stratigraphic well: The APPEA Journal, 61, 224-235, APPEA Conference June 2021 https://doi.org/10.1071/AJ20160  **Wingate, MTD, Lu, Y, Fielding, IOH, Normore, LS and Haines, PW 2021, 237995: siltstone, Barnicarndy-1: Geochronology Record 1740: Geological Survey of Western Australia, 8p.|16-MAY-23
20935|Yellow Drum Sandstone|Name source|Yellow Drum Bore; 125o23'45"E, 18o05'S, Noonkanbah 1:250 000 Sheet area.|16-MAY-23
20935|Yellow Drum Sandstone|Unit history|Thomas (1959) included the uppermost part in his Laurel Formation.|16-MAY-23
20935|Yellow Drum Sandstone|Type section locality|(WCB 004) 14 m of dolomite with shale and sandstone complemented by 68.9 m of sandstone and dolomite with minor shale from BMR Noonkanbah No. 4 which spudded in at the top of the type section. The bottom is recognised by the incoming of sandstone and dolomite, the top by the incoming of pellital limestone.|16-MAY-23
20935|Yellow Drum Sandstone|Extent|Southwest of the Oscar Range and in Station Creek. Outcrop is poor but the unit is known from boreholes to the south of the Oscar and Napier Ranges.|16-MAY-23
20935|Yellow Drum Sandstone|Thickness range|Range 50-300 m|16-MAY-23
20935|Yellow Drum Sandstone|Lithology|The dominant rock types are sandstone, dolomite and siltstone together with minor shale and limestone. The sandstones are white to yellow brown or grey, calcareous and quartzose; the dolomites are porous, greyish yellow to dark grey; the siltstones are brown.|16-MAY-23
20935|Yellow Drum Sandstone|Relationships and boundaries|Conformably overlies and interfingers with the Gumhole Formation. Conformably overlain and interfingers with the Laurel Formation.|16-MAY-23
20935|Yellow Drum Sandstone|Age reasons|Contains a sparse microbiota of spores and conodonts which show that the unit is diachronous and was deposited during the latest Late Devonian and earliest Early Carboniferous (do VI - tnla-tn-lb of the European sequence).|16-MAY-23
20935|Yellow Drum Sandstone|Defn Reference|79/20374; 83/23481|16-MAY-23
