Stratno | Stratigraphic Name | Category | Contents | Last update 
28319|Agnes Banks Sand|Name source|Village of Agnes Banks (GR 708465, Windsor, 1:63 360).|16-MAY-23
28319|Agnes Banks Sand|Unit history|Included in the Richmond Formation of Bell (1966).|16-MAY-23
28319|Agnes Banks Sand|Type section locality|7 m of fine to medium grained, cream to buff coloured quartz sand exposed in a sand pit of Farley and Lewers Ltd (GR 70447, Windsor 1:63 360).|16-MAY-23
28319|Agnes Banks Sand|Extent|Formation exposed over approximately 9 km2 south of the village of Agnes Banks.|16-MAY-23
28319|Agnes Banks Sand|Thickness range|Range 1-8 m.|16-MAY-23
28319|Agnes Banks Sand|Lithology|Mottled orange-grey, clayey quartz sand grading upwards into buff and cream coloured, fine to medium grained sand with minor clay. Rare crossbedding and occasional pebbles.|16-MAY-23
28319|Agnes Banks Sand|Relationships and boundaries|Boundary between Londonderry Clay and Agnes Banks Sand is sharp and probable disconformable. Erosional upper surface.|16-MAY-23
28319|Agnes Banks Sand|Age reasons|No floral or faunal assemblages available for dating. Agnes Banks Sand overlies the Londonderry Clay, the latter affected by late Miocene or early Pliocene lateritisation (Gobert in press). Unit occurs on a higher river terrace than the Pleistocene Cranebrook Formation and hence Agnes Banks Sand is thought to be Pliocene in age (Gobert in press, Morgan 1976a).|16-MAY-23
28319|Agnes Banks Sand|Name first published by|Wallace I., 1976|16-MAY-23
25684|Anembo Granodiorite|Name source|The village of Anembo at GR 195314 (Michelago 1:100 000 Geological Sheet).|16-MAY-23
25684|Anembo Granodiorite|Unit history|Baker (1915) referred to the Jerangle Grey Granite but most later workers combined the references to the Anembo Granodiorite and the Towners Creek Adamellite under the one name until Richards (1967) introduced the name Round Hill Granodiorite (invalidated by Andrews' (1922) Round Hill Group).|16-MAY-23
25684|Anembo Granodiorite|Type section locality|South of Anembo at GR 192336 near the Queanbeyan River.|16-MAY-23
25684|Anembo Granodiorite|Description at type locality|The granodiorite is a texturally homogeneous, coarse-grained, xenolith-enriched biotite-hornblende granodiorite. It generally has a coarse, hypidiomorphic granular texture. It weathers to a creamy-grey colour. Xenoliths up to 20 cm2 in area are common.|16-MAY-23
25684|Anembo Granodiorite|Extent|It appears along the full length of the Jerangle Igneous Complex, mainly along the eastern side. Size: 220 km2.|16-MAY-23
25684|Anembo Granodiorite|Relationships and boundaries|The granodiorite is partially bounded by the minor phase of the Jerangle Igneous Complex (Towners Creek Adamellite) and Late Ordovician Foxlow Beds. Some contact metamorphism is present.|16-MAY-23
25684|Anembo Granodiorite|Age reasons|A revised age of 396 m.y. is suggested by J Richards (pers. comm.). This suggests a Siluro-Devonian time of intrusion.|16-MAY-23
25684|Anembo Granodiorite|References|79/03619 - old reference number for RefID 32820 Richardson, S.J. 1975. A summary of the geology of the Michelago 1:100 000 sheet. Geological Survey of New South Wales. Quarterly Notes 21, p1-7|24-JUN-23
24602|Angus Place Sandstone|Name source|Village of Angus Place, North of Lidsdale|16-MAY-23
24602|Angus Place Sandstone|Type section locality|(1) Location - Elecom Lithgow-Newnes DDH 31 (221925mE, 1310963mN, Lithgow 1:50 000 sheet, 8931-111). (2) Repository - Elecom core store, Lithgow. Reference Section: Blackmans Crown A, GR 795257, Sofala 8831 - I and IV.|16-MAY-23
24602|Angus Place Sandstone|Extent|Western Coal Field. Equivalent lithologies known in Ulan area, Singleton district and Southern Coalfield. Detailed correlations have yet to be established between these areas. Also occurs on parts of the Hampton, Katoomba, Glen Davis and Glen Alice sheets.|16-MAY-23
24602|Angus Place Sandstone|Thickness range|(1) Type Section: From 239.22 m to 244.91 m. Thickness, 5.69 m.  (2) Maximum recorded - 15.5. M.|16-MAY-23
24602|Angus Place Sandstone|Lithology|A fine grained, quartz-lithic sandstone; rarely medium grained; sporadic low angle planar cross beds.|16-MAY-23
24602|Angus Place Sandstone|Relationships and boundaries|Conformably overlain by the State Mine Creek Formation or the Gap Sandstone and underlain by the Baal Bone Formation.  Fines downward - distinguished by sharp or distinct top and gradational base. Sporadic burrows. In part carbonate cemented. Top of unit is marked by sharp transition from sandstone to (commonly) coal or argillaceous and carbonaceous sediments of the State Mine Creek Formation. Base of unit transitional from sandstone to laminated and interbedded argillaceous sediments. Base placed at point where these become dominant. Part of Charbon Sub-Group.|16-MAY-23
24602|Angus Place Sandstone|Proposer|Bembrick C.S., Robertson Research (Australia) Pty Limited|16-MAY-23
37907|Appleogue Dacite Member|Name source|After 'Appleogue' homestead GR473238 Plagyan 1:25 000 sheet.|16-MAY-23
37907|Appleogue Dacite Member|Type section locality|On the banks of Maules Creek at GR441224 Berrioye 1:25 000 sheet.|16-MAY-23
37907|Appleogue Dacite Member|Extent|On the western limb of the Maules Creek anticline west of `Kashmir' (GR449211 Berrioye 1:25 000 sheet), extending for about 2 km between the entrance road to `Kashmir' and Maules Creek.|16-MAY-23
37907|Appleogue Dacite Member|Thickness range|35m|16-MAY-23
37907|Appleogue Dacite Member|Lithology|Dark grey to black, hornblende dacite containing plagioclase, hornblende, altered biotite and opaque minerals. The groundmass is spherulitic to chloritic and zeolitic and contains small fragments of pumice and possible shards.|16-MAY-23
37907|Appleogue Dacite Member|Depositional environment|Ignimbrite.[?? sub-aerial volcanics?]|16-MAY-23
37907|Appleogue Dacite Member|Relationships and boundaries|The Appleogue Dacite lies stratigraphically above the Peri Rhyolite|16-MAY-23
37907|Appleogue Dacite Member|Age reasons|Carboniferous|16-MAY-23
24603|Baal Bone Formation|Name source|Baal Bone Gap, east of Ben Bullen|16-MAY-23
24603|Baal Bone Formation|Unit history|New name (C.S. Bembrick)|16-MAY-23
24603|Baal Bone Formation|Type section locality|(1) Location - Elecom Lithgow-Newnes DDH 31 (221925 mE, 1310965mN, Lithgow 1:50 000 sheet, 8931-111).  (2) Repository - Elecom core store, Lithgow. Reference Section: Blackmans Crown A, GR 795257, Sofala 8831 - I and IV.|16-MAY-23
24603|Baal Bone Formation|Extent|Western Coalfield. Equivalent lithologies known in the Ulan area, Putty area, Singleton district and Southern Coalfield. A unit which appears to be of basin-wide extent, but this has not yet been fully established by detailed correlation. Also occurs on parts of the Hampton, Katoomba, Glen Davis and Glen Alice sheets.|16-MAY-23
24603|Baal Bone Formation|Thickness range|(1) Type Section - from 244.91 - 269.18 m. Thickness, 24.27 m. (2) Maximum recorded - 53 m (base not penetrated).|16-MAY-23
24603|Baal Bone Formation|Lithology|Dominantly interbedded and laminated mudstone, siltstone and claystone, with very minor sandstone. Sporadic very thin coals and oil shales.|16-MAY-23
24603|Baal Bone Formation|Relationships and boundaries|Conformably overlain by the Angus Place Sandstone and underlain by the Glen Davis Formation. Part of Charbon Sub-Group. Distinguished by the interbedded, laminated and bioturbated nature of the sediments. Contains arenaceous foraminifera and acritarchs. Common "drop stones". Unit as a whole commonly fines downward on a broad scale. Top of unit recognised at the point where sandstone becomes the dominant lithology. Base marked by a change from argillaceous sediments (commonly laminated) to coal, siliceous claystone or sandstone of the Glen Davis Formation.|16-MAY-23
24168|Baan Baa Formation|Name source|Baan Baa township; grid reference GG 830110, Baan Baa 1:100 000 Sheet area.|16-MAY-23
24168|Baan Baa Formation|Unit history|Correlative of Leard Formation (Brownlow, 1981) and other Early Permian pelletoidal claystones recognised in the Sydney Basin (see Loughnan, 1975).|16-MAY-23
24168|Baan Baa Formation|Type section locality|54 metres of massive to finely pelletoidal claystone in DMR borehole DDH Turrawan 2, from 619 to 673 metres.|16-MAY-23
24168|Baan Baa Formation|Extent|The unit occurs in the subsurface throughout the western part of the Gunnedah Basin (approximately 300 km2).|16-MAY-23
24168|Baan Baa Formation|Thickness range|Range 0-54 m|16-MAY-23
24168|Baan Baa Formation|Lithology|Massive to finely pelletoidal claystone, rarely carbonaceous. Essentially an alluvial deposit, finely bedded. Minor interbeds of non-pelletoidal clastic detritus near upper boundary.|16-MAY-23
24168|Baan Baa Formation|Relationships and boundaries|Overlies the Boggabri Volcanics (Hanlon, 1949) unconformably. Is a weathering product of the Boggabri Volcanics. Lower boundary is transitional with the Boggabri Volcanics. Conformably overlain by Maules Creek Formation (Brownlow, 1981) equivalents.|16-MAY-23
24168|Baan Baa Formation|Age reasons|Overlies Boggabri Volcanics (Early Permian Stage 2 age; McPhie, 1984) and underlies Maules Creek Formation equivalents (Early Permian Stage 4 age; McMinn, 1981). Age of Baan Baa Formation probably Stage 3 to lower Stage 4 Early Permian.|16-MAY-23
24168|Baan Baa Formation|Proposed publication|Abstracts, 20th Newcastle Symposium; Bicentennial Volume|16-MAY-23
24168|Baan Baa Formation|Comments|The Baan Baa Formation occurs west of the Boggabri Ridge. It is a correlative of the Leard Formation but spatially separated and distinct. It tends to be more alluvial (rather than colluvial) in character and attains greater thickness than the Leard Formation.|16-MAY-23
24168|Baan Baa Formation|References|79/02627; 84/24458;|16-MAY-23
24178|Belowrie Formation|Name source|Belowrie Creek; grid reference 14309825 to 14759815 (Dubbo 1:250 000).|16-MAY-23
24178|Belowrie Formation|Unit history|The Belowrie Formation is proposed as a name for the unpublished and invalid "Meadows Formation" of Steggles (1961), which was presented by Offenberg et al. (1971) as the unnamed unit, "S.Dma".|16-MAY-23
24178|Belowrie Formation|Type section locality|Extending from GR 147979 to GR 147978 (Dubbo 1:250 000) (top to bottom).|16-MAY-23
24178|Belowrie Formation|Extent|The Belowrie Formation extends in an arcuate tract about 12 km long by 1 km wide from 24 km S to 30 km SW of Dubbo.|16-MAY-23
24178|Belowrie Formation|Thickness range|The unit thickens from 400 m in the west to 900 m in the east. The volcanic member is 400 m thick at the type section.|16-MAY-23
24178|Belowrie Formation|Lithology|Shales with a prominent andesitic to basaltic tuff and lava member near the middle of the formation.|16-MAY-23
24178|Belowrie Formation|Relationships and boundaries|The top of the unit conformably underlies the basal graded bedded greywackes of the Whylandra Formation, and the base of the unit conformably overlies the sandstone member of the Wambangalong Formation.|16-MAY-23
24178|Belowrie Formation|Age reasons|The only recorded fossils in the Toongi Group occur in the uppermost unit, the Glengeera Formation, which contains poorly preserved corals, crinoid stems, and a conodont fauna including jSpathagnothodus sp. Of Late Ludlovian to Early Devonian age (Pickett, 1974). The Belowrie Formation is approximately halfway from the Glengeera Formation to the base of the Toongi Group, and a Silurian age is probable.|16-MAY-23
24178|Belowrie Formation|References|79/03255|16-MAY-23
1444|Belubula Limestone|Name source|The name derives from the Belubula River, along the banks of which, between Limestone Creek and Copper Mine Creek, some of the best outcrop is found.|16-MAY-23
1444|Belubula Limestone|Unit history|The informal 'Middle Member' of Webby (1969) was named the Boonderoo Limestone Member by Osborne (1978). However, use of the name must be abandoned because the 'Boonderoo Beds' of the Lower Permian of the Hughenden area, Queensland (Vine & Paine, 1974) has priority. No type section was designated by Osborne (1978). Instead, it is proposed to reinstate Carne and Jones" (1919, p.177) name 'Belubula Limestone Belt', a name which has remained unused for more than 50 years. Carne & Jones originally indicated the name to apply to the 'extensive belt of limestone outcrops' exposed on both sides of the Belubula River from the junction with Limestone Creek downstream (west) for a distance of 2.5 miles (4 km). The most conspicuous outcrops along this sector are the massively-bedded, 290 m thick, middle part of the Cliefden Caves Limestone Group. It is therefore proposed to use their name, modified to 'Belubula Limestone', for the middle of the three constituent formations of the Cliefden Caves Limestone Group.|16-MAY-23
1444|Belubula Limestone|Constituents|No mappable subdivisions have yet been recognised as extending across the area.|16-MAY-23
1444|Belubula Limestone|Type section locality|The type section will be designated in forthcoming publication as composite, including the section on Dunhill Bluff (GR 753815*) through the lower half, and the section on the north-west flanks of Caves Hill (GR 753821*) through the upper half. In the composite type section a total of 290 m of Belubula Limestone is represented.    (*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978).|16-MAY-23
1444|Belubula Limestone|Extent|Extensive belt of limestone outcrops exposed on both sides of the Belubula River from the junction with Limestone Creek downstream (west) for a distance of 2.5 miles (4 km).|16-MAY-23
1444|Belubula Limestone|General description|Carne and Jones (1919, p.177) 'extensive belt of limestone outcrops' exposed on both sides of the Belubula River from the junction with Limestone Creek downstream (west) for a distance of 2.5 miles (4 km). The most conspicuous outcrops along this sector are the massively-bedded, 290 m thick, middle part of the Cliefden Caves Limestone Group. It is therefore proposed to use their name, modified to 'Belubula Limestone', for the middle of the three constituent formations of the Cliefden Caves Limestone Group.|16-MAY-23
1444|Belubula Limestone|Thickness range|290 m thick.|16-MAY-23
1466|Bendethera Limestone Member|Name source|Presumed to be after Bendethera Homestead, E GR 474179, Araluen sheet.|16-MAY-23
1466|Bendethera Limestone Member|Unit history|The name Bendethera Limestone, presumably of formational status, was introduced by Best et al. (1964, Canberra 1:250 000 Geological Map, 2nd ed.). No formal definition has ever been published. Our mapping on the Araluen 1:100 000 sheet has demonstrated that it is best regarded as a limestone lense developed in the De Drack Formation (defined on Braidwood 1:100 000 Sheet) and of member status. A formal definition is given below.|16-MAY-23
1466|Bendethera Limestone Member|Type section locality|On hillside near Bendethera Cave, GR 438208, Araluen sheet.|16-MAY-23
1466|Bendethera Limestone Member|Extent|Four separate but spatially close together, lenses in the headwaters of Con Creek, a tributary of the Deua River. Total area about 1.5 km2.|16-MAY-23
1466|Bendethera Limestone Member|Thickness range|Uncertain because of rarity of bedding. At least 100 m present.|16-MAY-23
1466|Bendethera Limestone Member|Lithology|Massive, white to grey, coarsely recrystallised limestone. Fossils very rare. Some thin tuff beds and nodular limestone horizons occur rarely.|16-MAY-23
1466|Bendethera Limestone Member|Relationships and boundaries|Passes laterally, overlain and underlain by terrigenous sediments of De Drack Formation.|16-MAY-23
1466|Bendethera Limestone Member|Age reasons|Conodonts indicate a Late Silurian age.|16-MAY-23
28365|Bethungra Formation|Name source|Bethungra (GR 5856 7055, Cootamundra 1:250 000).|16-MAY-23
28365|Bethungra Formation|Type section locality|GR 5795 7100 to GR 5762 6196, Cootamundra 1:250 000 sheet, though outcrop here is quite poor. A subsidiary section is nominated from GR 5800 7170 to GR 5795 7170.|16-MAY-23
28365|Bethungra Formation|Extent|The unit occurs in a north-northwesterly trending belt, of variable width up to 7500 m, extending from near Powder Horn Hill south to the southern boundary of the Cootamundra 1:250 000 Sheet.|16-MAY-23
28365|Bethungra Formation|Thickness range|500-1000 m(?)|16-MAY-23
28365|Bethungra Formation|Lithology|Tuffs, dacitic to rhyolitic, dominantly airfall, some very siliceous. Minor arkose-siltstone containing a brachiopod fauna.|16-MAY-23
28365|Bethungra Formation|Relationships and boundaries|Overlies Frampton Volcanics with local unconformities. Overlain by undifferentiated sequence of siltstone, conglomerate, and sandstone. Contains the Ironbong Dacite Member at the top.|16-MAY-23
28365|Bethungra Formation|Age reasons|Brachiopod fauna (schizophorid, strophoedontid, and rynchonellid species) identified from K.S.W. Campbell of Australian National University as Early Devonian in age (Schmidt 1972).|16-MAY-23
28365|Bethungra Formation|Defn author|Gilligan L.B., Scheibner E., 1978|16-MAY-23
37908|Bexley Rhyolite Member|Name source|Named after the property `Bexley' GR376680 Eulowrie 1:25,000 sheet.|16-MAY-23
37908|Bexley Rhyolite Member|Unit history|Bexley Rhyolite (Opdyke et al. 2000).|16-MAY-23
37908|Bexley Rhyolite Member|Geomorphic expression|Very low ridge.|16-MAY-23
37908|Bexley Rhyolite Member|Type section locality|At GR370666 Eulowrie 1:25,000 sheet, in a gully on the western bank of Back Creek.|16-MAY-23
37908|Bexley Rhyolite Member|Extent|Crops over a length of 2.5 km in low ridges west of Back Creek on the properties Bexley and Pine Cliffs.|16-MAY-23
37908|Bexley Rhyolite Member|Thickness range|>2m [greater than 2m? - not very helpful!]|16-MAY-23
37908|Bexley Rhyolite Member|Lithology|An unwelded, pink ignimbrite with quartz, feldspar and minor opaque minerals. Pumices are small and either scattered or in aggregates. The groundmass is fine, chloritic to zeolitic and contains shards and bubble walls. The crystal-rich nature of parts of the unit may indicate redeposition.|16-MAY-23
37908|Bexley Rhyolite Member|Depositional environment|Ignimbrite but with the possibility of fluvial redeposition.|16-MAY-23
37908|Bexley Rhyolite Member|Relationships and boundaries|Relationship with the Peri Rhyolite is indeterminable, but most likely younger than that unit.|16-MAY-23
37908|Bexley Rhyolite Member|Age reasons|Carboniferous (Namurian)|16-MAY-23
37908|Bexley Rhyolite Member|Comments|Named informally by Hocking (1973). Restricted to the Kathrose block west of the Rocky Creek Syncline.|16-MAY-23
37908|Bexley Rhyolite Member|References|*HOCKING R.M. 1973. The Carboniferous Back Creek-Pound Creek sequence, southwest of Caroda, New South Wales. BSc (Hons) thesis, University of new England, Armidale (unpubl.).*OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
79325|Bibblewindi Coal Member|Name source|Bibblewindi Creek in northern New South Wales. This river overlies the parent unit Maules Creek Formation in the Gunnedah Basin.|16-MAY-23
79325|Bibblewindi Coal Member|Unit history|Namoi and Bohena Lower seam identified informally in well completion reports submitted to government departments by Force energy, Eastern Star Gas and Santos.|16-MAY-23
79325|Bibblewindi Coal Member|Geomorphic expression|Concealed beneath 700-1100m of Permian-Cretaceous cover (Gunnedah and Surat Basins).|16-MAY-23
79325|Bibblewindi Coal Member|Type section locality|Coal Seam Gas Exploration Drillhole Dewhurst 11 (Eastern Star Gas). 149.725147°E / 30.50355°S (GDA94) depth (984.90-991.94m).|16-MAY-23
79325|Bibblewindi Coal Member|Extent|Occurs in three areas over the Mullaley Sub-basin where the Maules Creek Formation greater than 60m thick. The areas are: - 1/ north and south of Narrabri, 2/ west of Werris Creek, and; 3/ south of Mullaley (650 square kilometres).|16-MAY-23
79325|Bibblewindi Coal Member|Thickness range|0 to 10m (generally 4 to 7m thick). The thickest interval is in the Bohena trough south of Narrabri and to the south of Mullaley (ACM Bando1). 7.04 m in type section.|16-MAY-23
79325|Bibblewindi Coal Member|Lithology|Coal, dull with chonchoidal fractures near base to dull with minor bright bands towards the top. Comprises a single seam in type section. Coal is free from stone bands in type section.|16-MAY-23
79325|Bibblewindi Coal Member|Depositional environment|Coal swamp (dry-terrestrial becoming wet terrestrial).|16-MAY-23
79325|Bibblewindi Coal Member|Diastems or hiatuses|Nil.|16-MAY-23
79325|Bibblewindi Coal Member|Relationships and boundaries|Below the Bohena Coal Member and often immediately above the contact with the Leard/Goonbri Formations.|16-MAY-23
79325|Bibblewindi Coal Member|Structure and Metamorphism|Dips at <5 degrees, probable early normal faulting is expected to be developed as observed in mining of the Maules Creek Formation in the Maules Creek Sub-basin to the east. Vitrinite reflectance values of between 0.65 and 0.85 RoMax where not heat affected by igneous intrusions.|16-MAY-23
79325|Bibblewindi Coal Member|Age reasons|Permian - Cisuralian (Kungurian) part of Gunnedah Basin Bellata Group, contains Glossopteris and Gengamoptris (Cisuralian). Palynological Age of APP31 inferred from samples above and below this interval. No tuffs are confidently logged at present within this seam.|16-MAY-23
79325|Bibblewindi Coal Member|Correlations|Probable equivalent to the Glenara Coal Member at Werris Ck, The Templemore to Cranliegh seams within the Maules Creek Sub-Basin. The Lewis and Loder Coal Members in the Musswellbrook Anticline north and the Balmoral Coal Member in the Musswellbrook Anticline south.|16-MAY-23
79325|Bibblewindi Coal Member|Alteration and Mineralisation|Coal - Bituminous in rank.|16-MAY-23
79325|Bibblewindi Coal Member|Geophysical Expression|Probable seismic reflector, low downhole gamma (<50) and density (<1.50g/cc) response.|16-MAY-23
79325|Bibblewindi Coal Member|Defn author|Mark Dawson, 10-FEB-2016.|16-MAY-23
79325|Bibblewindi Coal Member|Comments|This seam may eventually be broken into more than one split with further drilling and detailed correlations.|16-MAY-23
40754|Bideroie Ignimbrite Member|Name source|The property Bideroie (0239120E 6619480N Berrioye 1: 25 000 sheet).|16-MAY-23
40754|Bideroie Ignimbrite Member|Type section locality|locality  Between localities 414-1 and 414-4 30o32'23"S,150o18'29"E to30o32'30"S,150o18'22"E (0241750E 6618300N to 0241550E 6618100N Berrioye 1: 25 000 sheet). Despite minor faulting, this locality is chosen as the type because it displays all of the lithologies incorporated within the member.|16-MAY-23
40754|Bideroie Ignimbrite Member|Extent|Extends between Mount Byar in the north, via the eastern part of the Carrol-Nandewar region to Dripping Rock. Dark dacitic ignimbrite is best exposed south of Connors Creek, where there are two flows, on a small rounded hill immediately south of The Calpe (0242000E 6620900N Berrioye 1: 25 000 sheet) and on the northern slope of Mount Byar. Other outcrops usually contain rhyodacitic ignimbrite. At the type locality the rhyodacitic ignimbrite is replaced by a rhyodacite breccia.|16-MAY-23
40754|Bideroie Ignimbrite Member|Thickness range|Rhyodacitic ignimbrite 35 m in section 416; dacitic ignimbrite up to 20 m thick.|16-MAY-23
40754|Bideroie Ignimbrite Member|Lithology|Three lithologies are represented in this composite member ; dacitic ignimbrite (sample G13 Table 1 Appendix 3) , rhyodacitic ignimbrite (sample G14 Table 1 Appendix 3) and rhyodacitic breccia (sample G12 Table 1 Appendix 3). The dacitic ignimbrite is unwelded, dark grey, with plagioclase, hornblende, ? pumice fragments in a shard-rich, glassy, micropoikilitic or spherulitic groundmass. The rhyodacitic ignimbritic is slightly welded, purple to red, with scattered feldspars and pumice fragments in a shard-rich matrix. The breccia, which is confined to the type area, is red to beige and contains sub-rounded to angular clasts of felsic ignimbrite up to 20 mm in diameter. In thin section the matrix is ferruginised and contains smaller angular fragments and shards. In the type area the breccia is separated from the succeeding dacite by conglomerate, siltstone and sandstone.|16-MAY-23
40754|Bideroie Ignimbrite Member|Age reasons|?Late Namurian.|16-MAY-23
24181|Big Hole Formation|Name source|After The Big Hole, GR 405428, Araluen 1:100 000 Sheet.|16-MAY-23
24181|Big Hole Formation|Unit history|Previous use of name: None, introduced here for first time.|16-MAY-23
24181|Big Hole Formation|Type section locality|In the Big Hole (GR 405428) a large collapse structure developed in the Gundillion Conglomerate and Big Hole Formation. About 100 m of the unit, including its contact with the Gundillion Conglomerate, are exposed.|16-MAY-23
24181|Big Hole Formation|Extent|A meridional belt from near Gundillion north to west of Majors Creek. Small outliers continue to the southern part of the Braidwood 1:100 000 sheet.|16-MAY-23
24181|Big Hole Formation|Thickness range|About 140 m preserved.|16-MAY-23
24181|Big Hole Formation|Lithology|Well-bedded, medium to coarse arenite with only minor shale in the type area. Shale increases northwards to form about a third of the unit near its northern limit. Arenite is a quartz-lithic arenite in beds generally less than 1 m thick and often cross-bedded.|16-MAY-23
24181|Big Hole Formation|Relationships and boundaries|Conformably on Gundillion Conglomerate, with a gradational contact, and where the Conglomerate is absent, unconformably on the Silurian Long Flat Volcanics. The Big Hole Formation passes laterally southwards into the Long Swamp Creek Formation, and differs from the latter by having a much higher arenite/shale ratio, and in the arenites being coarser. The top of the Big Hole Formation is formed by the present-day erosion surface.|16-MAY-23
24181|Big Hole Formation|Age reasons|Several fossil localities are known in the north of the area; poorly preserved brachiopods and bivalves indicatae a Late Devonian age.|16-MAY-23
21249|Billilingra Dacite Member|Name source|Billilingra siding, GR960125, Cooma 1:100 000 sheet.|16-MAY-23
21249|Billilingra Dacite Member|Type section locality|Along road east of 'Rothlyn' homestead Cooma 1:100 000 sheet 8725, from GR982074 (base) to GR975074 (top).|16-MAY-23
21249|Billilingra Dacite Member|Extent|Extends from 1km northwest of Billilingra siding for about 20km to south-southeast; also from 0.5km east to 6km north of Bredbo, in small outliers between Bredbo and Billilingra, and in areas 6km and 15km east of Cooma.|16-MAY-23
21249|Billilingra Dacite Member|Thickness range|Ranges to about 600m.|16-MAY-23
21249|Billilingra Dacite Member|Lithology|Hornblende dacitic crystal tuff.|16-MAY-23
21249|Billilingra Dacite Member|Relationships and boundaries|Lowermost extensive volcanic unit in Rothlyn Formation from Colinton south; mostly overlain and underlain by shale; member of Rothlyn Formation.|16-MAY-23
21249|Billilingra Dacite Member|Age reasons|Late Silurian from fossils in enclosing sedimentary rocks of Rothlyn Formation; K/Ar isotopic age determination of 407 +/- 3 Ma indicates possible early Devonian age.|16-MAY-23
21249|Billilingra Dacite Member|Defn author|G.A.M. Henderson, ?1989.|16-MAY-23
21249|Billilingra Dacite Member|Comments|Although this appears to be an adequate unit definition, no evidence is available to show that this definition went through the Stratigraphy Commission approval process. The original card was supplied  to ASUD manager C. Brown by R. S. Abell, on his departure from BMR, after the publication of BMR Bulletin 233 Geology of the Canberra 1:100 000 sheet.|16-MAY-23
21249|Billilingra Dacite Member|References|Henderson, G.A.M. 1987. Late Silurian geology of the Michelago-Cooma area; 1:100 000 preliminary edn map. Bur. Miner. Resour. Aust.|16-MAY-23
27107|Billys Lookout Granite|Name source|Billys Lookout Mountain, GR 534835, Forbes 1:250 000 Sheet.|16-MAY-23
27107|Billys Lookout Granite|Unit history|Previously named Wyalong Granite on Forbes 1:250 000 Geological Sheet (1972). Given a separate name because it is a granite while the Wyalong body is a granodiorite.|16-MAY-23
27107|Billys Lookout Granite|Type section locality|Billys Lookout Mountain, GR 534835, Forbes 1:250 000 Sheet.|16-MAY-23
27107|Billys Lookout Granite|Extent|About 10 km2 at above location.|16-MAY-23
27107|Billys Lookout Granite|Lithology|Granite (perthite, microcline, quartz, minor andesine, biotite).|16-MAY-23
27107|Billys Lookout Granite|Relationships and boundaries|Intrusive into Late Silurian sediments.|16-MAY-23
27107|Billys Lookout Granite|Age reasons|Early Devonian(?) by analogy with the Grenfell Granite.|16-MAY-23
28368|Bindogandri Granite|Name source|Named after Bindogandri Creek which flows immediately south of the granite.|16-MAY-23
28368|Bindogandri Granite|Type section locality|Rock crops out at GR 642905 on hillside.|16-MAY-23
28368|Bindogandri Granite|Extent|A body of about 20 km2 extent centered at GR 643905|16-MAY-23
28368|Bindogandri Granite|Lithology|Granite (graphic alkali perthite = quartz> albite, minor biotite).|16-MAY-23
28368|Bindogandri Granite|Relationships and boundaries|Intrudes Ordovician sediments and is overlain by Late Devonian sediments.|16-MAY-23
28368|Bindogandri Granite|Age reasons|Interpreted as Early Devonian by analogy with the Grenfell Granite.|16-MAY-23
69825|Bingara Volcanics|Name source|After the town of Bingara (BINGARA 1:100 000 map sheet area).|16-MAY-23
69825|Bingara Volcanics|Type section locality|The type section area covers a small area near the Bingara-Narrabri road from GR 256890mE 6688760mN (MGA94 Zone 56) towards the east-southeast for approximately 2.4km along a prominent east-striking ridgeline.|16-MAY-23
69825|Bingara Volcanics|Extent|Part of the Central Province (McDougal and Wilkinson 1967), this unit lies on top of a plateau, approximately 7km to 12km west and southwest of Bingara.|16-MAY-23
69825|Bingara Volcanics|Thickness range|The Bingara Volcanics is estimated to attain a thickness of 60m.|16-MAY-23
69825|Bingara Volcanics|Lithology|Alkali olivine basalt and basanite lavas with minor volcaniclastic rocks and diamond-bearing gravels make up the Bingara Volcanics.|16-MAY-23
69825|Bingara Volcanics|Depositional environment|A series of basanitic flows up to 20m thick, interbedded with volcaniclastic deposits. Minor diamond-bearing gravels were deposited in erosional channels carved into the volcaniclastic deposits.|16-MAY-23
69825|Bingara Volcanics|Relationships and boundaries|The Bingara Volcanics unconformably overlies the Devonian to Carboniferous Parry Group of the Tamworth Belt, southern New England Orogen. It unconformably overlies Palaeogene gravels and interfingers with the Derra Derra Volcanics.|16-MAY-23
69825|Bingara Volcanics|Age reasons|One sample yielded a K-Ar age of 24Ma (Late Oligocene to Early Miocene).|16-MAY-23
39258|Birken Head Volcanic Member|Name source|From Birken Head Rock (0245900E 6582000N Kelvin 1:25,000 sheet), a prominent bluff near Kelvin.|16-MAY-23
39258|Birken Head Volcanic Member|Type section locality|From 30o52'03"S 150o20'37"E to 30o52'08"S 150o20'29"E (0246000E 6582050N to 0245800E 6581900N) in section 510 at Birken Head Rock.|16-MAY-23
39258|Birken Head Volcanic Member|Extent|Along the length of Tulcumba Ridge and northern half of Gunnan Ridge.|16-MAY-23
39258|Birken Head Volcanic Member|Thickness range|220 m in the type section. On Tulcumba Ridge, ranges from 280m in the north (section 411), 650 m in the central part (section 578) to 295 m in the south (section 521). On Gunnan Ridge from 260 m (section 522) in the central part to 85 m in the south. Section numbers are those of Roberts et al. ms.|16-MAY-23
39258|Birken Head Volcanic Member|Lithology|Composite unit of dacitic ignimbrite, subordinate and localised dacite lava, and resedimented dacitic conglomerate and/or agglomerate and sandstone. Predominant rock-type beige, white, pink or grey, coarse to medium-grained, crystal-rich, unwelded to moderately welded ignimbrite with quartz, plagioclase, K-feldspar, biotite, opaque minerals and minor pumices; groundmass generally spherulitic to occasionally micropoikilitic. A flow unit in upper part of member in section 578 (578-21) contains scattered medium grained plagioclase within a fine groundmass of oriented plagioclase laths and minor quartz. Glass shards normally present in resedimented rocks. Pumiceous conglomerate overlies the ignimbrite west of Birken Head Rock. XRF analyses (Liang 1989, MU47992, MU47993; Geeve 1995, MU55267, MU55268 and MU55269) indicate compositions of rhyolite at the base to dacite throughout the remainder of the unit.|16-MAY-23
39258|Birken Head Volcanic Member|Relationships and boundaries|A thin tongue of dacitic ignimbrite and, at the northern end of Tulcumba, a dacite flow (unnamed unit Cw9 of Roberts et al. in press) projects northwards from the main body of the Birken Head Volcanic Member in the central part of Tulcumba Ridge. The dacitic ignimbrite and lava are separated from the main body of the member by a lens of volcanolithic sediments and minor  volcanics.|16-MAY-23
39258|Birken Head Volcanic Member|Age reasons|The SHRIMP AS3 age is 315.2+/-2.8 Ma (sample 511-2. Figure 10, Roberts et al. ms). Early Westphalian.|16-MAY-23
1865|Blackmans Flat Conglomerate|Name source|Village of Blackmans Flat, Western Coalfield|16-MAY-23
1865|Blackmans Flat Conglomerate|Unit history|McElroy (1957), Branagan (1960). Not previously defined.|16-MAY-23
1865|Blackmans Flat Conglomerate|Type section locality|(1) Location: Austen & Butta Hartley Valley DDH3 (224552.4E 1291973.0N Lithgow 1:50 000 Sheet, 8931-111). (2) Repository: Dept Mineral Resources Core Library, Londonderry. Reference Section: Lidsdale House, GR 138051, Lithgow 8931-111.|16-MAY-23
1865|Blackmans Flat Conglomerate|Extent|Generally restricted to the western margin of the Western Coalfield.|16-MAY-23
1865|Blackmans Flat Conglomerate|Thickness range|(1) Type section: From 243.99 m to 247.53; thickness 3.54 m. (2) Maximum recorded: 20.5 m.|16-MAY-23
1865|Blackmans Flat Conglomerate|Lithology|Quartz-lithic, pebbly sandstone, medium and coarse grained, locally conglomeratic (pebble and cobble conglomerate); minor fine grained clastics. Sporadic coaly stringers.|16-MAY-23
1865|Blackmans Flat Conglomerate|Relationships and boundaries|Stratigraphic limits: Overlain conformably by the Lidsdale Coal. Sharp erosive contact with underlying Lithgow Coal. Part of Cullen Bullen Sub-Group. General: Massive bedded to planar cross bedded: generally fines upward, often in several sub-units. Thickness highly variable along strike. Base of unit marked by sharp transition from sandstone or conglomerate to coal or carbonaceous shales of the Lithgow Coal. Top of unit recognised by change from dominantly sandstone to coal, carbonaceous claystone or mudstone. The term is synonymous with the Upper Marrangaroo Sandstone (Rayner, 1955), (Taylor, 1954) and the Blackmans Flat Conglomerate (McElroy, 1957), (Branagan, 1960). Occurs in Lithgow and parts of Hampton 1:50 000 sheets.|16-MAY-23
1865|Blackmans Flat Conglomerate|Proposed publication|Australian Coal Geology|16-MAY-23
25792|Bland Diorite|Name source|County of Bland|16-MAY-23
25792|Bland Diorite|Type section locality|GR 528808, Forbes 1:250 000, on roadside at top of hill.|16-MAY-23
25792|Bland Diorite|Extent|Small outcrops over area of 15 km2 immediately east of Wyalong.|16-MAY-23
25792|Bland Diorite|Lithology|Diorite|16-MAY-23
25792|Bland Diorite|Relationships and boundaries|Intrudes Late Ordovician sediments. Is itself intruded by the Late Silurian Wyalong Granodiorite.|16-MAY-23
25792|Bland Diorite|Age reasons|Late Ordovician to Early Silurian (age date potassium-argon 422 +/- 15 m.y. by Amdel - File Geol. Surv. NSW GS 1975/187).|16-MAY-23
25794|Blow Clear Member|Name source|Blow Clear Trig Station.|16-MAY-23
25794|Blow Clear Member|Type section locality|533884 (bottom) to 532844 (top) Forbes 1:250 000|16-MAY-23
25794|Blow Clear Member|Extent|Outcrops for about 6 km along strike.|16-MAY-23
25794|Blow Clear Member|Thickness range|About 400 m|16-MAY-23
25794|Blow Clear Member|Lithology|Sandstone and conglomerate|16-MAY-23
25794|Blow Clear Member|Relationships and boundaries|Lithologically distinct and usually sharp boundaries with Burcher Greywacke greywacke.|16-MAY-23
25794|Blow Clear Member|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (V.7 No. 1)|16-MAY-23
2046|Boambolo Formation|Name source|"Boambolo" property; GR 1891 6730 (Umburra 1:50 000 Sheet, 8627-I).|16-MAY-23
2046|Boambolo Formation|Unit history|The "Glen Bower Member" of Brunker & Offenberg (1970) and the "Glen Bower Beds" of Best et al. (1964) were subdivided by Moignard (1970) into the Boambolo Formation in the east and the Glen Bower Formation in the west.|16-MAY-23
2046|Boambolo Formation|Type section locality|Near GR 191677 (Goulburn 1:250 000).|16-MAY-23
2046|Boambolo Formation|Extent|The unit has been mapped along approx. 5 km strike length in a N-S-trending tract 0.5-1 km wide, and offset by numerous transverse faults, extending from near GR 19056725 (Umburra 1:50 0000) to near GR 1895 6790 (Goulburn 1:250 000).|16-MAY-23
2046|Boambolo Formation|Thickness range|The lower member ranges from 20  m to 40 m. The upper member is of uncertain thickness, but probably averages 100-120 m, thinning to about 20 m in the north.|16-MAY-23
2046|Boambolo Formation|Lithology|The lower member contains finely laminated shales and siltstones, and the upper member contains coarse to medium-grained well sorted and well rounded quartz sandstones with calcite cement and limestone clasts.|16-MAY-23
2046|Boambolo Formation|Relationships and boundaries|The sandstones at the top of the formation are overlain by coarse crystal tuffs of the Douro Group volcanics, which rest on the Boambolo Formation with disconformity in the north, and with progressively more pronounced unconformity towards the south. The shales and siltstones at the base of the Boambolo Formation overlie the interbedded sandstones, siltstones, detrital stromatolitic limestones and limestones of the Glen Bower Formation with low angle discordance in the north, ranging to high angle discordance in the south.|16-MAY-23
2046|Boambolo Formation|Age reasons|The underlying Glen Bower Formation contains a middle Wenlockian to early Ludlovian conodont fauna (Moignard, 1970) and Encrinurus cf. Mitchelli. The Boambolo Formation itself contains Lingula sp., ?Girvanella sp., gastropods, ostracods, dendroid tabulate corals, clasts of Favosites sp. and Heliolites sp., and Encrinurus cf. mitchelli. The latter is common in both the Boambolo Formation and the Glen Bower Formation and is used, together with the age of the Glen Bower Formation, as evidence that the time break between the two formations is relatively minor, and hence that the Boambolo Formation is of Late Silurian age.|16-MAY-23
2046|Boambolo Formation|References|79/00647|16-MAY-23
24189|Boat Harbour Breccia|Name source|Boat Harbour on the east coast of Lord Howe Island at 159o06.1'E longitude, 31o33.4'S latitude on map of Lord Howe Island (Department of Lands, Sydney, 1966, 1:15840).|16-MAY-23
24189|Boat Harbour Breccia|Type section locality|Coast line immediately southwest of Rocky Point over a few hundred metres, on the west side of Boat Harbour.|16-MAY-23
24189|Boat Harbour Breccia|Extent|Exposed over about 4 km2 in central parts of Lord Howe Island from northern slopes of Mount Lidgbird to waist of island between Prince William Henry Bay and Blinkenthorpe Bay.|16-MAY-23
24189|Boat Harbour Breccia|Thickness range|Possibly 250 m +|16-MAY-23
24189|Boat Harbour Breccia|Lithology|Massive, well indurated breccia composed of angular to subangular basaltic fragments ranging down in size from 1 m, but usually consisting of fragments less than 10 cm across, set in a fine grained matrix. No bedding visible.|16-MAY-23
24189|Boat Harbour Breccia|Relationships and boundaries|No base exposed, but suggest it is younger than North Ridge Basalt. Intruded by numerous basaltic dykes and sheets. Overlain by Mount Lidgbird Basalt.|16-MAY-23
24189|Boat Harbour Breccia|Age reasons|Thought to be Late Miocene as probably younger than North Ridge Basalt (age ~6.9 Ma), and clearly older than Mount Lidgbird Basalt (K-Ar age ~6.4 Ma).|16-MAY-23
24189|Boat Harbour Breccia|Comments|Interpret the Boat Harbour Breccia as an agglomerate, probably formed within the vent region of the large basalt shield volcano of which Lord Howe Island is the erosional remnant.|16-MAY-23
24189|Boat Harbour Breccia|References|79/01576|16-MAY-23
25796|Bobs Creek Formation|Name source|The name is derived from Bobs Creek where the unit is well exposed.|16-MAY-23
25796|Bobs Creek Formation|Unit history|Woolomin Series, Benson 1911; Woolomin Group, Voisey 1959; Woolomin beds (Crook 1961) in part; Bobs Creek beds (unpublished thesis name of Cuddy 1978).|16-MAY-23
25796|Bobs Creek Formation|Type section locality|Stratotype: A type area is nominated as Bobs Creek (Cobbadah 1:100 000 topographic map sheet 9037 GR 870470 to GR 856474).|16-MAY-23
25796|Bobs Creek Formation|Thickness range|Indeterminate due to deformation and poor exposure.|16-MAY-23
25796|Bobs Creek Formation|Lithology|Basal basalt (often removed by faulting) depositionally overlain by up to 100 m of ribbon-bedded, red, radiolarian chert. This chert is overlain by several hundred metres of greenish argillite in turn overlain by a distinctive yellow chert horizon (50 to 100 m thick) in turn overlain by ;more greenish argillite and rare ?olistostromal lenses. Metamorphism: Prehnite-pumpellyite facies.|16-MAY-23
25796|Bobs Creek Formation|Relationships and boundaries|Thrust contacts, structurally overlying Cara Formation and structurally overlain by Nangahrah Formation.|16-MAY-23
25796|Bobs Creek Formation|Age reasons|Radiolaria indicate a possible age range from Middle Devonian to Early Carboniferous.|16-MAY-23
25796|Bobs Creek Formation|Correlations|Possibly correlates with Cockburn Formation and restricted Woolomin Formation of Cawood 1982 both of which were introduced without definition.|16-MAY-23
79331|Bohena Coal Member|Name source|Bohena Creek in northern New South Wales. This creek overlies the parent unit Maules Creek Formation in the Gunnedah Basin.|16-MAY-23
79331|Bohena Coal Member|Unit history|Bohena seam identified informally in well completion reports submitted to government departments by Force energy, Eastern Star Gas and Santos.|16-MAY-23
79331|Bohena Coal Member|Geomorphic expression|Concealed beneath 400-1100m of Permian-Cretaceous cover (Gunnedah and Surat Basins).|16-MAY-23
79331|Bohena Coal Member|Type section locality|Coal Seam Gas Exploration Drillhole Dewhurst 11 (Eastern Star Gas). 149.725147°E / 30.50355°S (GDA94) depths (969.46-984.76m).|16-MAY-23
79331|Bohena Coal Member|Extent|Occurs over most of the Mullaley Sub-basin where the Maules Creek Formation is present. Extends north of Narrabri to west of Werris Creek to south of Mullaley (2200 square kilometres).|16-MAY-23
79331|Bohena Coal Member|Thickness range|15.30m in type section. Range 1 to 18m (generally 6 to 14m thick). The thickest interval is in the Bohena trough south of Narrabri.|16-MAY-23
79331|Bohena Coal Member|Lithology|Coal, dull to dull with minor bright bands. Comprises a single seam in the type section. Coal has four carbonaceous mudstone bands from (972.24-972.36m / 974.95-975.15 / 975.73-976.22m / 976.85-977.11m).|16-MAY-23
79331|Bohena Coal Member|Depositional environment|Coal swamp (dry-terrestrial).|16-MAY-23
79331|Bohena Coal Member|Fossils|Coal.|16-MAY-23
79331|Bohena Coal Member|Diastems or hiatuses|Nil.|16-MAY-23
79331|Bohena Coal Member|Relationships and boundaries|Above the Bibblewindi Coal Member and below the Collygra Coal Member.|16-MAY-23
79331|Bohena Coal Member|Identifying features|Thick dull coal interval usually overlain by 20-30 metres of upward coarsening sandstone and siltstone.|16-MAY-23
79331|Bohena Coal Member|Structure and Metamorphism|Dips at <5 degrees, probable early normal faulting is expected to be developed as observed in mining of the Maules Creek Formation in the Maules Creek Sub-basin to the east. Vitrinite reflectance values of between 0.65 and 0.85 RoMax where not heat affected by igneous intrusions.|16-MAY-23
79331|Bohena Coal Member|Age reasons|Permian - Cisuralian (Kungurian) part of Gunnedah Basin Bellata Group, contains Glossopteris and Gengamoptris (Cisuralian). Palynological Age of APP32 inferred from samples above, and APP31 below this interval. No tuffs are confidently logged at present within this seam|16-MAY-23
79331|Bohena Coal Member|Correlations|Probable equivalent to the Erunderee, Faithful and Friendly Coal Members at Werris Ck, The Braymont to Tarrawonga seams within the Maules Creek Sub-Basin. The Muswellbrook and St Helliers Coal Members in the Muswellbrook Anticline north and the Theiss and Puxtrees Coal Members in the Muswellbrook Anticline south.|16-MAY-23
79331|Bohena Coal Member|Alteration and Mineralisation|Coal - Bituminous in rank.|16-MAY-23
79331|Bohena Coal Member|Geophysical Expression|Probable seismic reflector, low downhole gamma (<50) and density (<1.50g/cc) geophysical response.|16-MAY-23
79331|Bohena Coal Member|Defn author|Mark Dawson, 10-FEB-2016.|16-MAY-23
79331|Bohena Coal Member|Comments|This seam may eventually be broken into more than one split with further drilling and detailed ply correlations.|16-MAY-23
24744|Bombay Volcanics|Name source|"Bombay" property, GR 413754, Braidwood 1:100 000 Sheet.|16-MAY-23
24744|Bombay Volcanics|Type section locality|In Bombay Creek between GR 409755 (faulted base) and GR 386744 (top) (Braidwood 1:100 000 Sheet).|16-MAY-23
24744|Bombay Volcanics|Extent|A strip averaging 3 km wide extends from the vicinity of "Borwood" property (GR 439937 Braidwood 1:100 000 Sheet) at least as far south as "Nundale" property (GR 265607 Canberra 1:250 000 metallogenic map, Gilligan, 1975).|16-MAY-23
24744|Bombay Volcanics|Thickness range|1745 m at the type section in Bombay Creek.|16-MAY-23
24744|Bombay Volcanics|Lithology|Grey-green medium-grained dacitic crystal tuff; rhyolite, rhyolitic ignimbrite. Minor shale, siltstone, lithic sandstone.|16-MAY-23
24744|Bombay Volcanics|Relationships and boundaries|In the northern area of their outcrop, the Bombay Volcanics are faulted against the Boro Granite and Palerang Formation in the west and against the Long Flat Volcanics in the east. Further south the volcanics are intruded by the Boro Granite and are overlain to the west with apparent conformity by Palerang Formation sediments. The top of the volcanics is defined as the top of the last massive outcrop of crystal tuff. No volcanics are included in the Palerang Formation. South of the Braidwood sheet area, the Bombay Volcanics appear to overlie the Long Flat Volcanics, possibly disconformably. In this area, a topographic break occurs between the softer, more weathered crystal tuffs of the Long Flat Volcanics and the compositionally similar, but more massive rocks of the Bombay Volcanics.|16-MAY-23
24744|Bombay Volcanics|Age reasons|The volcanics are intruded by the Boro Granite (mid-Early Devonian) which establishes a minimum age. No fossils have been found in the overlying Palerang Formation, or in the Bombay and Long Flat Volcanics. The Bombay Volcanics are tentatively correlated with the Woodlawn Volcanics further north, which interfinger with De Drack Formation sediments containing Monograptus cf. bohemicus, a late Silurian graptolite. The Long Flat Volcanics conformably overlie De Drack Formation sediments and limestone containing non-diagnostic fossils of Silurian age. A tentative age of Middle to Late Silurian is assumed.|16-MAY-23
24744|Bombay Volcanics|References|GOLD1391|16-MAY-23
27113|Bongalaby Formation|Name source|"Bongalaby" property, GR 412224 Braidwood 1:100 000 Sheet.|16-MAY-23
27113|Bongalaby Formation|Constituents|Lake Bathurst Limestone Member.|16-MAY-23
27113|Bongalaby Formation|Type section locality|The section in Bongaralaby Creek between GR 408218 and GR 406213 (Braidwood 1:100 000 Sheet).|16-MAY-23
27113|Bongalaby Formation|Extent|The unit is exposed in a north-trending belt about 1 km wide which lies 1 km west of Tarago (GR 420159 and Lake Bathurst (GR 417217) townships.|16-MAY-23
27113|Bongalaby Formation|Thickness range|About 200 m (est).|16-MAY-23
27113|Bongalaby Formation|Lithology|Cream to buff calcareous siltstone and arenite, limestone.|16-MAY-23
27113|Bongalaby Formation|Relationships and boundaries|Overlies with possible disconformity the Tarago Conglomerate (together with which it constitutes the Mulwaree Group). Top eroded.|16-MAY-23
27113|Bongalaby Formation|Age reasons|The Lake Bathurst Limestone Member contains Gephuropora duni Etheridge, Chalcidophyllum sp., Polygnathus linguiformis foreolata Philip & Jackson, Neoprioniodus bicurvatus (Brahnson & Mehl), Ozarkodina cf. Jaegeri Walliser (Philip, 1966) Spathognathodus linearis (Philip). Receptaculites sp. and Plasmophyllum sp. occur within the Bongalaby Formation. See Philip & Pedder, 1968; Strusz & Nicoll, 1973. An Emsian age is indicated.|16-MAY-23
27113|Bongalaby Formation|References|97/28484; 73/015.|16-MAY-23
37903|Boomi Rhyolite Member|Name source|Boomi Creek, a major tributary of the Horton River west of Upper Horton, NSW.|16-MAY-23
37903|Boomi Rhyolite Member|Unit history|Boomi Rhyodacite (Opdyke et al. 2000)|16-MAY-23
37903|Boomi Rhyolite Member|Geomorphic expression|Low ridge.|16-MAY-23
37903|Boomi Rhyolite Member|Type section locality|On Boomi Creek at GR379565 Horton 1:25,000 sheet.|16-MAY-23
37903|Boomi Rhyolite Member|Extent|On the western limb and southern closure of the Maules Creek Anticline adjacent to Boomi Creek.|16-MAY-23
37903|Boomi Rhyolite Member|Thickness range|25m|16-MAY-23
37903|Boomi Rhyolite Member|Lithology|Poorly to moderately welded beige rhyolitic ignimbrite containing quartz, feldspars, possible biotite and rare volcanic rock fragments. Groundmass micropoikilitic and having shards, rare bubble walls and small pumices.|16-MAY-23
37903|Boomi Rhyolite Member|Depositional environment|Ignimbrite.|16-MAY-23
37903|Boomi Rhyolite Member|Age reasons|Carboniferous (Visean)|16-MAY-23
37903|Boomi Rhyolite Member|Comments|Named informally by Hocking (1973). Klootwijk (2002) used palaeomagnetic evidence to suggest the Boomi Rhyodacite is an equivalent of the Peri Rhyolite. Current mapping does not support this proposal.|16-MAY-23
37903|Boomi Rhyolite Member|References|HOCKING R.M. 1973. The Carboniferous Back Creek-Pound Creek sequence, southwest of Caroda, New South Wales. BSc (Hons) thesis, University of new England, Armidale (unpubl.).02/32155 - KLOOTWIJK C.T. 2002. Carboniferous palaeomagnetism of the Rocky Creek Block, northern Tamworth Belt, and the New England pole path. Australian Journal of Earth Sciences 49, 375-405.OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
39259|Boorabil Ignimbrite Member|Name source|After the Parish of Boorabil (Gunnedah 1: 25, 000 sheet).|16-MAY-23
39259|Boorabil Ignimbrite Member|Type section locality|The type section taken between 30o52'00"S 150o20'54"E to 30o52'03"S 150o20'47"E (0246459E 6582164N and 0246275E 6582064N Kelvin 1: 25,000 sheet) within section 510, northern Gunnan Ridge.|16-MAY-23
39259|Boorabil Ignimbrite Member|Extent|Western slope of the northern end of Gunnan Ridge.|16-MAY-23
39259|Boorabil Ignimbrite Member|Thickness range|75 m in type section; exceeds 310 m in mid-part of Gunnan Ridge (section 574 of Roberts et al. ms).|16-MAY-23
39259|Boorabil Ignimbrite Member|Lithology|Beige, pink or brown, unwelded to slightly welded ignimbrite, with quartz, plagioclase, K-feldspar, biotite, opaque minerals and rare pumices; groundmass micropoikilitic or spherulitic. Lithologically close to dacitic ignimbrites in the Birken Head Volcanic Member.|16-MAY-23
39259|Boorabil Ignimbrite Member|Relationships and boundaries|A possible equivalent of the lower part of the Birken Head Volcanic Member.|16-MAY-23
39259|Boorabil Ignimbrite Member|Age reasons|Probably early Westphalian.|16-MAY-23
2344|Boro Granite|Name source|Boro village, GR 424078, Braidwood 1:100 000 sheet.|16-MAY-23
2344|Boro Granite|Type section locality|Fresh pink granite is exposed by the roadside on the Goulburn-Braidwood road 3 km south of Boro. Texture is coarse grained equigranular, with mafic minerals occurring as small aggregates 5 mm in diameter, slightly streaked into cleavage. Xenoliths are rare at this locality but can be seen in the tor-like outcrops in the vicinity of Reedy Creek where it is crossed by the road (GR 425995, Braidwood 1:100 000 sheet).|16-MAY-23
2344|Boro Granite|Extent|The Boro Granite is batholithic in character. Disconnected bodies extend from just north of Lake Bathurst (GR 455180, Braidwood 1:100 000 sheet) to the southern edge of the Canberra 1:250 000 sheet and beyond, where it becomes part of the Bega Batholith, an undifferentiated, composite granitic intrusion. The area in which it crops out is at least 120 km long and 20 km wide.|16-MAY-23
2344|Boro Granite|Lithology|The Boro Granite consists of hornblende biotite granodiorite and adamellite, pink to grey in colour. It is intruded by basic dykes, particularly near Reedy Creek (GR 425995, Braidwood 1:100 000 sheet) and by bodies of microgranite with quartz phenocrysts (exposed by the roadside 5 km south of Boro).|16-MAY-23
2344|Boro Granite|Relationships and boundaries|The Boro Granite intrudes Ordovician metasediments, Middle to Late Silurian volcanics and sediments (Long Flat and Bombay Volcanics; De Drack Formation, Palerang Formation) and is unconformably overlain by the Early Devonian Tarago Conglomerate and Cainozoic sediments. Faulted against the Long Flat and Bombay Volcanics. Intrudes the ?Early Silurian Lockhart igneous complex.|16-MAY-23
2344|Boro Granite|Age reasons|The granite is of earliest Devonian age (based on stratigraphic evidence cited above). It has been dated at 390 m.y. (Evernden and Richards, 1962) (Early Devonian).|16-MAY-23
27117|Boyd Volcanic Complex|Name source|Prominent forested hill in the parish of Boyd; GR 58984 7465, Eden 1:25 000 topographic sheet (8823-1-N)|16-MAY-23
27117|Boyd Volcanic Complex|Type section locality|There is no type section, as the unit is a complex of interdigitating facies. Ten sections through the unit have been measured and will be published to illustrate the variations.|16-MAY-23
27117|Boyd Volcanic Complex|Extent|The unit is exposed over approximately 300 km2 parallel to the Pacific Coastline in the Bega 1:250 000 Metallogenic map (1975) from Bunga Head to the Victorian Border.|16-MAY-23
27117|Boyd Volcanic Complex|Thickness range|Variable: measured sections vary from 120 m to 1500 m.|16-MAY-23
27117|Boyd Volcanic Complex|Lithology|Eight facies have been identified: (1) Sedolithic breccia-conglomerate-sandstone facies, (2) Flyschoid facies, (3) Arkosic-volcolithic conglomerate-sandstone mudstone facies, (4) Banded rhyolite facies, (5) Lenticle-tuff facies, (6) Massive rhyolite facies, (7) Basalt facies, and (8) Massive, granular rhyolite-aplite facies.|16-MAY-23
27117|Boyd Volcanic Complex|Relationships and boundaries|Overlies Ordovician (?) Mallacoota Beds (Steiner, 1972) with high angle unconformity, and is non-conformable on the Bega granitoids. The top is a low-angle unconformity with the base of the Upper Devonian Merrimbula Group (Steiner, 1972). The Gabo Island Granite is intrusive into, and comagmatic with the rhyolitic facies. Revision of old terms: The Boyd Volcanic Complex includes all the rocks formerly sub-divided into the "Eden Rhyolite" and "Lochiel Formation" (Hall, 1960), which two formations are rejected as being invalid because they are not mappable units.|16-MAY-23
27117|Boyd Volcanic Complex|Age reasons|Probably Upper Devonian. Upper Devonian fish fossils have been found in mudstones within the complex (G. Young, pers. comm.), Upper Devonian plant fossils have been recovered from the overlying Merrimbula Group. A K/Ar date from the Gabo Island Granite (356 +/- 12 m.y., Thompson, 1974) is also Upper Devonian. No Middle or Lower Devonian fossils have been found, but the older time bracket can be established no more precisely than post-Bega Granitoids from which a K/Ar date of 376 m.y. (Evernden & Richards, 1962) has been obtained.|16-MAY-23
27117|Boyd Volcanic Complex|References|GOLD1667; 79/04091; |16-MAY-23
40188|Brawlin Formation|Type section locality|GR 595800 mE, 6156200 mN east to GR600400 mE, 6154900 mN, AMG datum AGD 66. Western end of the section is at the sharp bend from southerly to easterly in the Cootamundra to Coolac road. See GSNSW Quarterly Notes 117 for conversion to MGA GDA 94.|16-MAY-23
40188|Brawlin Formation|Proposed publication|NSW Geological Survey Quarterly Notes.|16-MAY-23
25809|Breckin Ignimbrite Member|Name source|including grid co-ordinates: Mt Breckin (Paterson 45829707).|16-MAY-23
25809|Breckin Ignimbrite Member|Unit history|Subdivision of the Gilmore Volcanics.|16-MAY-23
25809|Breckin Ignimbrite Member|Type section locality|North of Vacy. Mt Breckin (Paterson 45829707) located approximately mid-way between Breckin and North Breckin.|16-MAY-23
25809|Breckin Ignimbrite Member|Extent|Forms a band in the vicinity Martin's Creek, Vacy, Lambs Valley, Mt Breckin.|16-MAY-23
25809|Breckin Ignimbrite Member|Thickness range|a) At type section: 40 metres.  B) Maximum known:|16-MAY-23
25809|Breckin Ignimbrite Member|Lithology|Basal porphyritic grey, andesitic ignimbrite overlain by a red, porphyritic, andesitic ignimbrite.|16-MAY-23
25809|Breckin Ignimbrite Member|Relationships and boundaries|The unit overlies the Newton Formation (purple lithic sandstones) and is overlain by sandstones of the Mowbray Formation. It occurs as the basal lmember of the Mowbray Formation.|16-MAY-23
25809|Breckin Ignimbrite Member|Age reasons|Lower Namirian, correlations by Campbell & McKelvey.|16-MAY-23
2778|Buckburraga Slate|Name source|Buckburraga Creek.|16-MAY-23
2778|Buckburraga Slate|Unit history|Name first proposed in unpubl. BSc. Hons. Thesis by D Dunnell and I Gemuts, Sydney Uni. 1961.|16-MAY-23
2778|Buckburraga Slate|Type section locality|Type area: Village of Burraga. Location of type section: Excelsior Copper Mine, Burraga GR 519035 Burraga 1:31680.|16-MAY-23
2778|Buckburraga Slate|Extent|Burraga area.|16-MAY-23
2778|Buckburraga Slate|Thickness range|a) At type section 200 m approx.  b) Maximum known: 200 m approx.|16-MAY-23
2778|Buckburraga Slate|Lithology|Grey-blue to grey-green and black slates.|16-MAY-23
2778|Buckburraga Slate|Fossils|Not known|16-MAY-23
2778|Buckburraga Slate|Relationships and boundaries|Base is top of Dunchurch Formation. Top is base of Excelsior Porphyry Member of the Lovetts Formation or chlorite schist of the Lovetts Formation.|16-MAY-23
2778|Buckburraga Slate|Age reasons|Silurian - Stratigraphic position.|16-MAY-23
80755|Buckingbong Granite|Type section locality|The most extensive exposure of the Buckingbong Granite is in a borrow pit in the Buckingbong State Forest (Photograph 17). Although the exposed granite is very weathered, given the amount of exposure and access, this site is here suggested as the type locality for the pluton (At ERIVSJT1548, GR 451890 613910; 146.473268E, -34.9181533S; YANCO).|16-MAY-23
80755|Buckingbong Granite|Defn author|Trigg (2018) in GSNSW report GS2018/0253 p40-43.|16-MAY-23
2885|Bullanamang Porphyry|Name source|Parish of Bullanamang in the County of Beresford|16-MAY-23
2885|Bullanamang Porphyry|Unit history|The unit has been mapped and/or described but unnamed by Browne (1944), Joplin (1943), Joplin et al. (1953) and Best et al. (1964).|16-MAY-23
2885|Bullanamang Porphyry|Type section locality|In creek bed at GR 914212 (Michelago 1:100 000 Geological Slheet).|16-MAY-23
2885|Bullanamang Porphyry|Description at type locality|The porphyry is more a mass of thin lenses or sills rather than one mass. It contains large bipyramidal phenocrysts of quartz up to 9 mm in length with plagioclase, biotite and minor hornblende in a finely altered granular groundmass. There are associated small intrusions of aplites and alaskite.|16-MAY-23
2885|Bullanamang Porphyry|Extent|Northwest of Bredbo and north of the Murrumbidgee River.  Size: 0.4 km2.|16-MAY-23
2885|Bullanamang Porphyry|Relationships and boundaries|The porphyry is intrusive into the Bransby Beds. Shearing related to the Murrumbidgee Shear Zone is developed along the eastern margin as well as parts of the western margin.|16-MAY-23
2885|Bullanamang Porphyry|Age reasons|Late Silurian to Early Devonian.|16-MAY-23
2885|Bullanamang Porphyry|References|01/31570; 01/31571; 85/24687; 79/03619.|16-MAY-23
27121|Bundaburrah Granodiorite|Name source|Bundaburrah GR 574855, Forbes 1:250 000|16-MAY-23
27121|Bundaburrah Granodiorite|Unit history|Previously named Grenfell Granite (Forbes 1:250 000 Geological Sheet 1972). As it is more basic than the Grenfell Granite at Grenfell it warrants a separate name.|16-MAY-23
27121|Bundaburrah Granodiorite|Type section locality|GR 578857, Forbes 1:250 000, on side of hill.|16-MAY-23
27121|Bundaburrah Granodiorite|Extent|Small outcrops over area of 1 km2 3 km northeast of Bundaburrah.|16-MAY-23
27121|Bundaburrah Granodiorite|Lithology|Granodiorite (andesine>orthoclase>quartz, minor amphibole).|16-MAY-23
27121|Bundaburrah Granodiorite|Relationships and boundaries|Intrusive into Late Ordovician sediments|16-MAY-23
27121|Bundaburrah Granodiorite|Age reasons|Early Devonian (?) by analogy with the Grenfell Granite.|16-MAY-23
24203|Bungendore Formation|Name source|Named after Bungendore, south of Lake George.|16-MAY-23
24203|Bungendore Formation|Unit history|None.|16-MAY-23
24203|Bungendore Formation|Type section locality|Designated from core in BMR stratigraphic hole C354 (Abell 1985a). From the surface 54m of clay and silt was recovered (mostly in excess of 90%) from the greatest thickness of the formation so far drilled in the Lake George Basin.  The base is defined by thin beds of dark-greenish-grey to medium-grained sand and silt at the top of the Ondyong Point Formation. Representative outcrops of clay occur at the drier northern and southern extremities of Lake George.|16-MAY-23
24203|Bungendore Formation|Extent|Lake George drainage basin (Canberra 1:100 000 sheet 8727). The unit immediately underlies the present lake bed.|16-MAY-23
24203|Bungendore Formation|Thickness range|Maximum known is 54m in BMR stratigraphic hole C354.|16-MAY-23
24203|Bungendore Formation|Lithology|Consists of three lithotypes: mottled clay; gravelly clay with quartz and lithic clasts; clay with colour, carbonaceous or silty laminations.  Reddish-brown ferriginous weathering profiles occur intermittently throughout.  The unit is characterised by montmorillonite, montmorillonitic mixed clays and detrital kaolinite (Abell, 1985b).|16-MAY-23
24203|Bungendore Formation|Depositional environment|Lacustrine.|16-MAY-23
24203|Bungendore Formation|Relationships and boundaries|The base is not exposed but is taken at the top of the highest and most persistent sandbed of the Ondyong Point Formation. The top of the formation is the lake bed which is exposed when Lake George dries out. The upper part of the formation grades laterally into coarse alluvium in embayments at the southern and eastern margin of the basin. Westward it grades laterally into colluvium and alluvial fans at the base of the Lake George escarpment.|16-MAY-23
24203|Bungendore Formation|Age reasons|A study of palaeomagnetic reversals through the upper 36m of the formation in ANU hole LG4 gives a Pliocene age of 3.5Ma (Singh and other 1981). A similar and probably greater age can be extrapolated to the thicker lacustrine sequence in BMR stratigraphic hole C354.|16-MAY-23
24203|Bungendore Formation|Correlations|The upper part of the formation presumably correlates with the Late Quarternary colluvial, alluvial strandline and lagoonal sediments in marginal areas of the Lake George drainage basin; also with fluviolacustrine sediments on the Carwoola Flats: perched drainage basin associated with the Murrumbidgee River on the Tuggeranong and Lanyon areas south of Canberra, and Plio-Pleistocene sediments in the Lake Bathurst drainage basin.|16-MAY-23
3060|Burcher Greywacke|Name source|Village of Buracher.|16-MAY-23
3060|Burcher Greywacke|Type section locality|Type Section and Lithology: This unit is about 4000 m thick and consists, except for the Blow Clear Member, of a very uniform massive medium grained grey quartz-feldspar-biotite greywacke. It is silicified in many places and forms hills with extensive outcrops. Bedding is generally not prominent in the greywacke but there is overall variation in grain size from dark slate to grit. In places it is calcareous or dolomitic, and a few rare crinoid stems have been found within the massive greywacke. The type section for the formation, including the Blow Clear Member, is along an east-west line through Lake View homestead. Here the succession is as follows: a. The basal 1500 m of the formation is generally fine grained and slaty.  b. Blow Clear Member - Immediately to the west of Lake View there is a hill subsurface, about 200 m thick and lenses out to the north. Overlying the sandstone but separated from it by alluvium and soil, there is a 50 m thick unit of cobble and pebble conglomerate. The cobbles and pebbles are well rounded and consist of quartzite. The conglomerate lenses out to the north. To the south it grades into sandstones and shales.  c. To the west, i.e. stratigraphically above, of the conglomerate there is a wide interval of soil and alluvium. However it is marked as a magnetic ridge on aeromagnetic maps and probably indicates an andesitic volcanic rock in the subsurface. d. Further west, towards the Burcher-West Wyalong road, there is almost continuous outcrop of the monotonous quartz greywacke. Although the Blow Clear Member is a prominent part of the Burcher Formation in the south, towards the north the Member sharply lenses out. The contact between the Burcher Greywacke and the overlying Sandal Formation is nowhere exposed; the two formations are separated by soil and alluvium.  534844 (bottom) to 527845 (top) Forbes 1:250 000.|16-MAY-23
3060|Burcher Greywacke|Extent|For about 20 km along strike between Billy's Lookout and Burcher.|16-MAY-23
3060|Burcher Greywacke|Thickness range|About 4000 m.|16-MAY-23
3060|Burcher Greywacke|Relationships and boundaries|Lithologically distinct. Conformable above Corringle Formation. Possibly unconformable under Sandal Formation.|16-MAY-23
3060|Burcher Greywacke|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (V.7 No. 1)|16-MAY-23
26295|Burragundy Formation|Name source|Burragundy Property|16-MAY-23
26295|Burragundy Formation|Unit history|Unpublished "Back Creek Formation" of Maggs (1963) (UNSW MSc Thesis) and published on Dubbo 1:250 000 as unnamed formation letter coded Sbk on legend.|16-MAY-23
26295|Burragundy Formation|Type section locality|Along "Back Creek".  Location of Type Section: Dubbo 1:250 000 GR 171941|16-MAY-23
26295|Burragundy Formation|Extent|Extends in a tract about 15 km long and 1-2 km wide from about 16 km SW of Wellington to about 14 km north of Cumnock.|16-MAY-23
26295|Burragundy Formation|Thickness range|a) at type section: 730 m.  b) Maximum known: approximately 1500 m.|16-MAY-23
26295|Burragundy Formation|Lithology|Predominately shales with lesser jasper chert and detrital limestone horizons.|16-MAY-23
26295|Burragundy Formation|Fossils|Abundant crinoid ossicles, favositids, heliotids.|16-MAY-23
26295|Burragundy Formation|Relationships and boundaries|Conformably overlies the Canowindra porphyry and is fault-bounded at the top.|16-MAY-23
26295|Burragundy Formation|Age reasons|Upper Wenlockian to Ludlovian age based on correlation along strike with Cary Beds (Upper Wenlock) and Burrawong Limestone (Lower Ludlovian).|16-MAY-23
24205|Calamia Member|Name source|"Calamia" property; GR 515006 6705955, Pillar Valley 1:25 000 map sheet 9538-III-N|16-MAY-23
24205|Calamia Member|Name source|From Calamia Parish in the Pillar Valley area, southeast of Grafton, in New South Wales.|16-MAY-23
24205|Calamia Member|Unit history|First published by Etheridge et al., 1985|16-MAY-23
24205|Calamia Member|Geomorphic expression|The member weathers recessively and outcrop is fragmentary. A few poor exposures are present in the Coast Range, the best being in a quarry on the Grafton-Wooli Road, NN 171.047 on the Bare Point 1:100 000 Sheet. Here shale of the Calamia Member crops out beneath bluffs of the Gatton Sandstone.|16-MAY-23
24205|Calamia Member|Type section locality|92 m (926-1018 m) in DM Pillar Valley DDH2. The top is identified by a grey to dark grey claystone, 5.35 m thick; the base by the occurrence of coarse grained sandstone.|16-MAY-23
24205|Calamia Member|Type section locality|The type section nominated is the interval 881-1018 m in the DM Pillar Valley DDH No. 2 based on the lithological log (Etheridge et al., 1985).|16-MAY-23
24205|Calamia Member|Description at type locality|The detailed sequence in the member is given in the Department of Mines descriptive log of Pillar Valley DDH 2, and on a graphic log compiled by Wells and O'Brien from this description. The member is composed of siltstone and mudrocks, and fine to medium grained sandstone. It is 137 m thick in Pillar Valley DDH No. 2. No palynomorphs were recovered from one sample collected from the member and there is no record of diastems or hiatuses.|16-MAY-23
24205|Calamia Member|Description at type locality|92 m (926-1018 m) of light grey to grey sandstone and grey to dark grey siltstone and claystone in DM Pillar Valley DDH2. The top is identified by a grey to dark grey claystone, 5.35 m thick; the base by the occurrence of coarse grained sandstone.|16-MAY-23
24205|Calamia Member|Extent|RDEF: The member was first identified in the DM Pillar Valley DDH 2 drillhole and was thereafter extended to neighbouring well sections.|16-MAY-23
24205|Calamia Member|Extent|The unit is defined in DM Pillar Valley DDH2 and has been identified and correlated tentatively in Kyogle-1, Sextonville-1, Shannon-1 and Tullymorgan-1 using lithological descriptions, gamma ray and sonic log responses. These wells are distributed over approximately 3168 km2 on the eastern side of the Grafton 1:250 000 map sheet (SH56-6) and the western side of the Maclean 1:250 000 map sheet (SH56-7).|16-MAY-23
24205|Calamia Member|General description|REGIONAL ASPECTS: The member is widespread in the subsurface but does not outcrop well and has only been observed in fragmentary exposures in the Coast Range.|16-MAY-23
24205|Calamia Member|Thickness range|Range 42-120 m.|16-MAY-23
24205|Calamia Member|Lithology|SANDSTONE, light grey, fine to coarse (generally fine) grained, quartzose, low to medium angle crossbedding, siliceous matrix, occasionally carbonaceous interbedded with SILTSTONE (grey to dark grey, partly carbonaceous) and CLAYSTONE (grey to dark grey, partly carbonaceous, common root traces).|16-MAY-23
24205|Calamia Member|Depositional environment|Predominantly overbank and minor channel depositional facies of a fluvial environment.|16-MAY-23
24205|Calamia Member|Relationships and boundaries|RDEF: The member is apparently conformable with bounding units. It separates the Gatton Sandstone of the Marburg Subgroup from the Ripley Road Sandstone.  The member is lithologically similar to the Gatton Sandstone but contains a higher proportion of siltstone and claystone units and the channel sandstones are finer grained, quartzose and have a siliceous matrix.|16-MAY-23
24205|Calamia Member|Relationships and boundaries|Conformably overlies the Ripley Road Sandstone. Conformably overlain by the remainder of the lower Marburg Formation. Top and base readily distinguished by the gamma ray log response. Refer to Type Section.|16-MAY-23
24205|Calamia Member|Identifying features|The lithology of the member and its gamma ray log response distinguish it from neighbouring units.|16-MAY-23
24205|Calamia Member|Age reasons|The member contains no internal evidence of age. The Marburg Subgroup is Early Jurassic in age and the basal parts of the Subgroup, probably including strata equivalent to the Calamia Member, contain the upper limit of the basal Early Jurassic P. crenulatus zone. The Ripley Road Sandstone beneath is Upper Triassic in NS 272 Ipswich, and in GSQ Ipswich 1 the uppermost part of the sandstone is in the lower part of Assemblage C, and thus is probably latest Triassic.|16-MAY-23
24205|Calamia Member|Correlations|Etheridge et al. (1985) consider that it may represent a distal facies of the lower Evergreen Formation from the Surat Basin.   A correlateable unit with a similar gamma ray response and lithology has been identified in Tullymorgan 1 and Sectonville 1 wells, and as far north as the Laidley Sub-basin (Ipswich 19-22R and Beef City Water Bore). The interval in Ipswich 19-22R falls within Assemblage D.|16-MAY-23
24205|Calamia Member|References|Etheridge et al. (1985) - REFID 39907 Etheridge et al , in prep 1988 - ?Willis 1989 - REFID 41631|16-MAY-23
3385|Camden Head Claystone|Name source|Camden Head 31deg38' 48.56"S, 152deg50' 24.81"E. The Camden Head Claystone is named after Camden Head where the first outcrop of Triassic rocks in the Lorne Basin was identified by Carne (1897).|16-MAY-23
3385|Camden Head Claystone|Name source|Camden Head 911834 Camden Haven 1:63 360|16-MAY-23
3385|Camden Head Claystone|Unit history|Named by Pratt & Herbert 1973.|16-MAY-23
3385|Camden Head Claystone|Unit history|Previously included in the Camden Haven Series of Voisey (1939),  then the Camden Haven Group of Packham (1969). The formation was formally named by Pratt and Herbert (1973) who nominated, with a single grid reference, the Bago Road exposure south from Kings Creek as the type section because more of the unit was exposed there than at Camden Head. They also noted that the unit 'usually, although not always, has a thin basal conglomerate' and the 'conglomerate is identical in composition to the overlying Laurieton Conglomerate'. The latter part of this observation is now shown herein to be incorrect.|16-MAY-23
3385|Camden Head Claystone|Geomorphic expression|The presence of the Camden Head Claystone is usually suggested by undulating terrain without outcrop and the deep, usually rich red soil developed over it. There is often a noticeable change of slope and change in soil colour at the boundary of the formation and the overlying, more-resistant, Coorabakh Conglomerate. The Coopernook Conglomerate Member has a different geomorphic expression as described in that unit's definition.|16-MAY-23
3385|Camden Head Claystone|Type section locality|Kings Creek. Location of Type Section: Kings Creek 795 995 Camden Haven 1:63 360.|16-MAY-23
3385|Camden Head Claystone|Type section locality|E side of Bago Road from 31.52058 deg S 152.72916 deg E,  to 31.52705 deg S 152.72216 deg E. The type section now proposed for this formation is located more precisely than the original site nominated by Pratt and Herbert (1973). The Camden Head Claystone type section is now specified as along Bago Road from GR 474286 6512671 (1:25 000 map sheet 9434-4-N, Byabarra; location 26) to GR 473623 6511952 (1:25 000 map sheet 9434-4-N, Byabarra; location 23). The lower and sand- to pebble-dominated part of the section, herein defined as the Coopernook Conglomerate Member, constitutes the lower part of the section from GR 474286 6512671 (1:25 000 map sheet 9434-4-N, Byabarra; location 26) to GR 474108 6512416 (1:25 000 map sheet 9434-4-N, Byabarra; location 24).|16-MAY-23
3385|Camden Head Claystone|Description at type locality|The type section for the Camden Head Claystone is exposed in road cuttings on the eastern side of the Bago Road southwards up the hill from near the Kings Creek Bridge. The Camden Head Claystone is an upward-fining sequence from pebble and granule conglomerate at the base, through sandstone to siltstone and claystone at the top. While these lithologies are interbedded in various proportions, the conglomerates are confined to the lower part of the formation. To provide more precise locations for the top and base of the section, the exposure was reassessed and measured. Bed lithology analysis of the 82 m thick Bago Road section has indicated an overall lithological composition of: conglomerate 16%; sandstone 21%; mudstone 63%. The sequence fines upward, with rudaceous sedimentary rocks dominating the basal 32 m, where the components are: conglomerate 41%; sandstone 17%; mudstone 42%. This basal 32 m unit contains a variety of interbedded lithologies from pebble (occasional cobble bands in some locations) conglomerate through sandstone to mudstone - although the unit is dominated by conglomerate and sandstone. This basal unit has both a lithology and topographic expression distinctly different to the upper part of the formation and so, as a mappable unit, is separated as a new member It is herein defined as the Coopernook Conglomerate Member of the Camden Head Claystone. The base of the Camden Head Claystone, being the base of its Coopernook Conglomerate Member, is defined as the bed which rests on the Jolly Nose Conglomerate, as at location 21 or the Palaeozoic rocks of the basin floor as at location 202. The top of the unit is the top of the reddish purple mudstone on which the Laurieton Conglomerate rests. A graphical reference for the lithology of measured sections are presented in Figure 4. The graphical representation for the lithology of the type section of the Camden Head Claystone (location 26 to location 23), is presented in Figure 5.|16-MAY-23
3385|Camden Head Claystone|Extent|The Camden Head Claystone is the most widely distributed formation throughout the Lorne Basin but, apart from the Coopernook Conglomerate Member, exposures are not common because it is generally deeply weathered and recessive.|16-MAY-23
3385|Camden Head Claystone|Extent|Lorne Basin.|16-MAY-23
3385|Camden Head Claystone|Thickness range|While a complete section has not been located, 82 m and 74 m sections have been measured at the Bago Road type section and the Rock Creek sections respectively. Maximum is greater than this. Minimum not known.|16-MAY-23
3385|Camden Head Claystone|Thickness range|a) At type section: 75 m.  b) Maximum known: 75 m.|16-MAY-23
3385|Camden Head Claystone|Lithology|The Camden Head Claystone is dominated by grey and reddish purple mudstone. The formation is readily identified by that reddish purple mudstone, which is absent from the other Triassic units. Some of the reddish purple mudstone weathers to grey while the grey mudstone may weather to, or be stained, reddish purple. The reddish purple mudstone is very well-developed in the upper part of the sequence and well-exposed in the coastal cliffs of Camden Head and Grants Head. Carbonaceous mudstones are not common but are exposed on the Pacific Highway 5 km north of Herons Creek (location 51). Thin 'coaly' beds, no longer exposed, were recorded by Morrison (1922), south of Johns River Railway station (location 116). Below the mudstone-dominated top of the unit, as exposed at Camden Head and Grants Head, there is a horizon with more frequent thin- and medium-bedded sandstone beds. That horizon forms gently rounded hills throughout the outcrop area and can be seen in the cutting on the Pacific Highway 2 km south of Moorland, between Two Mile Creek and the North Coast Railway bridge (location 203). Mudstone dominates the unit between that horizon and the Coopernook Conglomerate Member. Lithology plots of measured sections of the Coopernook Conglomerate Member at other exposures - Cowarra Quarry (location 22); Rock Creek, Langley Vale (location 72 to location 74); Hannam Vale (location 87 to 88); and Sapling Creek (location 20 to location 139) - are presented in figures 6, 7, 8 and 9 respectively. Lithology plots of measured sections at the top of the sequence exposed at Camden Head (after Voisey, 1939) and at Grants Head (after Holmes & Ash 1979) are presented in figures 10 and 11, respectively.|16-MAY-23
3385|Camden Head Claystone|Lithology|Red-brown claystone and siltstone with minor grey siltstone, sandstone and conglomerate.|16-MAY-23
3385|Camden Head Claystone|Depositional environment|The sedimentary sequence derived from sheet sands and channel sands incised into muddy overbank deposits together with the laminated reddish and grey terrestrial plant-bearing silts and clays, indicates a fluviatile depositional environment for the Camden Head Claystone. From the identified megaflora, Holmes and Ash (1979 p. 68) concluded that 'The localities from which the bulk of our flora was collected all represent a single environment, that of back-swamps bordering streams and filled by overbank flooding.'|16-MAY-23
3385|Camden Head Claystone|Fossils|Plant fossils.|16-MAY-23
3385|Camden Head Claystone|Fossils|Lower Triassic plant and palynological fossils have been recorded by several authors.|16-MAY-23
3385|Camden Head Claystone|Relationships and boundaries|Of Camden Haven Group (Packham 1969). Rocks of the Camden Head Claystone and, in particular, its basal Coopernook Conglomerate Member, unconformably overlie the Palaeozoic rocks of the basin floor. East of the North Coast Railway the formation overlies the Jolly Nose Conglomerate (where present) - except for a small area in the immediate vicinity of Jolly Nose Hill where the Camden Head Claystone is not present. The Camden Head Claystone is in turn overlain, generally with an erosional contact, by the Laurieton Conglomerate east of the Pacific Highway and by its lateral equivalent, the Coorabakh Conglomerate west of the Pacific Highway. The basal boundary of the Camden Head Claystone is chert-quartz-jasper pebble conglomerate or the reddish purple mudstone overlying the Jolly Nose Conglomerate or the Palaeozoic sedimentary rocks of the basin floor. The top of the formation is the reddish purple mudstone overlain by the cobble and pebble chert-jasper-quartz conglomerate of the Laurieton Conglomerate or more quartz-rich pebble conglomerate of the Coorabakh Conglomerate. Includes Coopernook Conglomerate Member. Unit overlies the Palaeozoic rocks of the Basin floor or the Jolly Nose Conglomerate. Top of unit is reddish-purple mudstone overlain by Laurieton or Coorabakh Conglomerate.|16-MAY-23
3385|Camden Head Claystone|Relationships and boundaries|Unconformable on Palaeozoic basement. Overlain by and laterally equivalent to Laurieton Conglomerate.|16-MAY-23
3385|Camden Head Claystone|Identifying features|The Camden Head Claystone is characterised by the presence of reddish purple mudstone. Reddish purple mudstone is also sparsely interbedded with the sandstone and conglomerate of its Coopernook Conglomerate Member. However, mudstone is far more strongly developed in the upper part of the formation. This upper part is predominantly (about 80%) mudstone (grey or, commonly and distinctively, reddish purple). The formation is usually highly weathered and outcrops are not common. However, its presence is indicated by the red-brown clayey soil which develops over it. Clays of similar colour are also developed from weathering of some of the late Triassic to Jurassic igneous rocks. Sheet sandstone is also present, having been deposited adjacent to channels incised into the underlying mudstone.|16-MAY-23
3385|Camden Head Claystone|Structure and Metamorphism|Generally the Camden Head Claystone dips slightly towards the centre of the basin. (Map 1 and Figure 2).|16-MAY-23
3385|Camden Head Claystone|Age reasons|Lower Triassic - Palynological data.|16-MAY-23
3385|Camden Head Claystone|Age reasons|Megaflora fossils were collected by Carne (1897), Voisey (1939) and Pratt (1970), and were identified by W.S.Dun, A.B.Walkom and J.W. Pickett, respectively. Retallack (1977) and Holmes and Ash (1979) also collected and identified material from the Camden Head and Grants Head exposures. The megaflora is found in the grey mudstone while the reddish purple mudstone is deplete of plant fossils. Four of the five locations in the Holmes and Ash (1979) study work are at the top of the Camden Head Claystone - on the southern side of Camden Head (location 66) and in a thin bed of grey siltstone exposed at the base of sea cliffs on the northern side of Perpendicular Point. The third and fourth locations were in the Camden Head Claystone at Grants Head, 8 m and 13 m (see Holmes & Ash 1979, figure 2, p. 48) below the Laurieton Conglomerate (figures 10 and 11). The fifth location was 63 m above the base of the Grants Head Formation at Bartletts Beach (location 104). Palynological samples from the Camden Head and Grants Head exposures were studied by Helby who reported 'A probable upper Early Triassic age was suggested for these assemblages on the basis of comparison with Sydney Basin assemblages' (1973 p. 146).|16-MAY-23
3385|Camden Head Claystone|Correlations|There are no units in the Lorne Basin with which the Camden Head Claystone correlates.|16-MAY-23
3385|Camden Head Claystone|Defn author|G. Winston Pratt 7-JUL-2010.|16-MAY-23
3385|Camden Head Claystone|Defn author|G.W. Pratt & C. Herbert 11-Dec-1972.|16-MAY-23
3385|Camden Head Claystone|Comments|Redefined to more accurately locate the type section and its Coopernook Conglomerate Member.|16-MAY-23
3385|Camden Head Claystone|References|Carne J.E. 1897. Report on the geology and mineral resources of the coast between Port Macquarie and Cape Hawke. New South Wales Department of Mines Annual Report for 1896. **Helby R.J. 1973. Review of Late Permian and Triassic palynology of New South Wales. Geological Society of Australia Special Publication 4, pp. 141-155. **Holmes W.B.K. & Ash S.R. 1979. An early Triassic megafossilflora from the Lorne Basin, New South Wales. Proceedings of the Linnean Society of New South Wales, 103, 47-70. **Packham G.H. 1969. The New England region. Triassic System, pp. 270¿271. In: Packham G.H. ed. The Geology of New South Wales. Journal of the Geological Society of Australia. 16 (1), 1-654. **Pratt, G.W. 2010. A revised Triassic stratigraphy for the Lorne Basin, NSW. Quarterly Notes of the Geological Survey of New South Wales 126. **Pratt G.W. & Herbert C. 1973. A reappraisal of the Lorne Triassic Basin. Geological Survey of New South.Wales, Records 15, 205-212. **Voisey A.H. 1939. The Lorne Triassic Basin and associated rocks. Proceedings of the Linnean Society of New South Wales 64, 225-265. **Helby (1972) GS NSW Report Palynology 1972/3|16-MAY-23
3563|Captains Flat Formation|Name source|Named after the township of Captains Flat on the Michelago 1:100 000 sheet area (Richardson 1979).|16-MAY-23
3563|Captains Flat Formation|Unit history|Captains Flat Beds (Glasson and Paine, 1965)|16-MAY-23
3563|Captains Flat Formation|Type section locality|Within the township of Captains Flat (Michelago 1:100 000 sheet 8726), the formation is well-exposed on Town Hill (GR 216/593). Here the sequence consists of dark grey shale, lithic and crystal tuff, dacite and basalt in a tight north-plunging syncline (Oldershaw 1965). Top and bottom are not exposed.|16-MAY-23
3563|Captains Flat Formation|Extent|It outcrops as two meridional belts along the eastern and western margins of the Captains Flat Graben. The eastern belt, up to 2km wide, stretches from 'Woodbine' homestead (GR 333/849) on the Canberra 1:100 000 sheet, southwards to Captains Flat on the Michelago 1:100 000 sheet. The western belt of similar width follows the Lake George Range from the Bungendore-Gundaroo road south for 30km onto the Michelago sheet area.  Continuity of this belt is broken by quartz turbidite units of the Carwoola Formation cropping out in the Molonglo River valley.|16-MAY-23
3563|Captains Flat Formation|Thickness range|In the vicinity of Captains Flat, Oldershaw (1965) estimated 800-1220 m while west of Hoskinstown, Wilson (1964) gave 1100m.|16-MAY-23
3563|Captains Flat Formation|Lithology|A heterogeneous sequence of shale, siltstone, dacite, tuff and minor basalt, limestone, chert and conglomerate.|16-MAY-23
3563|Captains Flat Formation|Depositional environment|Shallow marine.|16-MAY-23
3563|Captains Flat Formation|Relationships and boundaries|The Captains Flat Formation in part conformably overlies the Carwoola Formation. However south of Hoskinstown the Carwoola Formation thins out to leave the Captains Flat Formation apparently conformable with the underlying Kohinoor Volcanics.  North of Hoskinstown the base of the Captains Flat Formation appears to progressively overlap the Copper Creek Shale as the Kohinoor Volcanics thin out northwards.|16-MAY-23
3563|Captains Flat Formation|Age reasons|By stratigraphical relationships with the Kohinoor Volcanics and the Carwoola Formation, a Late Silurian age (Ludlow or younger) has been proposed by Strusz (1971) and Robinson (1979).|16-MAY-23
3563|Captains Flat Formation|Correlations|Basaltic units in the formation tentatively suggest a correlation in part with the Currawang Basalt. The upper part may be the same age as quartz turbidite sediments of the Covan Creek Formation and Palerang beds. The Captains Flat formation may in part be a facies equivalent of the Carwoola Formation.|16-MAY-23
28435|Cara Formation|Name source|The name is derived from the property "Cara" (Bingara 9038-111-N) where typical Cara Formation lithologies are well exposed.|16-MAY-23
28435|Cara Formation|Unit history|Previously mapped as undifferentiated Palaeozoic (Chestnut et al. 1968, 1969).|16-MAY-23
28435|Cara Formation|Type section locality|Stratotype: The unit is not well exposed and a type area (instead of type section) is therefore nominated. The type area is along the length of Tea Tree Creek (Bingara 9038-111-N 1:25 000 topographic map sheet) from GR 703017 to GR 750502.|16-MAY-23
28435|Cara Formation|Extent|The unit is well exposed over at least 50 km2 west of Copeton Dam between Gwydir River and Sheep Station Creek.|16-MAY-23
28435|Cara Formation|Thickness range|Indeterminate due to faulting and poor exposure.|16-MAY-23
28435|Cara Formation|Lithology|Cara Formation is dominated by fine-grained, siliceous, commonly tuffaceous argillites. Subordinate volcaniclastic sandstones and pebble conglomerates are also present. Tuffaceous argillites are typically thin bedded and often weather to massive, grey blue outcrops. Where not bleached tuffaceous argillite and chert range in colours from moderate red through reddish and yellowish brown to white. Tuffaceous argillite is observed in depositional contact upon altered basalt at some localities. Radiolaria are often abundant in tuffaceous argillites. Well developed axial planar cleavage indicates mesoscopic folding in some areas.|16-MAY-23
28435|Cara Formation|Relationships and boundaries|Cara Formation is poorly exposed and intensely faulted. The base of the formation is always faulted and an unconformable contact with overlying Whitlow Formation is inferred. In places the formation has been overthrust by Woolomin Group.|16-MAY-23
28435|Cara Formation|Age reasons|Radiolaria indicate a Famnenian-Tournaisian age.|16-MAY-23
28435|Cara Formation|Comments|Metamorphism: Prehnite-pumpellyite facies.|16-MAY-23
3566|Caragabal Granite|Name source|Caragabal GR 578817 Forbes 1:250 000|16-MAY-23
3566|Caragabal Granite|Unit history|Previously named Grenfell Granite (Forbes 1:250 000 Geological Sheet 1972). It is more basic than the granite at Grenfell and thus has been separately named.|16-MAY-23
3566|Caragabal Granite|Type section locality|GR 590825 on sides of hills|16-MAY-23
3566|Caragabal Granite|Extent|About 30 km2 7 km east of Caragabal|16-MAY-23
3566|Caragabal Granite|Lithology|Leucogranite (quartz>alkali perthite>albite, minor biotite).|16-MAY-23
3566|Caragabal Granite|Relationships and boundaries|Intrusive into Late Ordovician sediments.|16-MAY-23
3566|Caragabal Granite|Age reasons|Early Devonian (?) by analogy with the Grenfell Granite.|16-MAY-23
40759|Carramundra Member|Name source|From the property Carramundra (0242760 6602540 Willuri 1:25 000 sheet).|16-MAY-23
40759|Carramundra Member|Type section locality|Section 297 between localities 297-17 at 30040?20?S,150019?11?E (0243202E 6603632N) and 297-22 at 30039?15?S,150018?34?E (0242164E 6605636N Willuri 1:25 000 sheet).|16-MAY-23
40759|Carramundra Member|Extent|The Carramundra Member contains three beige ignimbrites (a-c) separated by volcanolithic sandstone and conglomerate (Figure 5). The member extends from the base of ignimbrite bed a to the top of ignimbrite c. All three ignimbrites extend northwards from Barneys Springs Creek at Wean Gap, curve abruptly westwards around the southern margin of the Bunaleer Dacite Member and then trend northwards parallel with the Mooki Thrust. Ignimbrite bed a terminates near the southwestern corner of the dacite whilst beds b and c extend northwards to a splay fault from the Mooki Thrust 4 km south-southwest of Dripping Rock.|16-MAY-23
40759|Carramundra Member|Thickness range|The member ranges in thickness from 320 m in section 297 to 260 m in section 298 (Figure 5). The range of thickness of the ignimbrite beds is : a 30-35 m; b up to 37 m; c 7-20 m.|16-MAY-23
40759|Carramundra Member|Lithology|Beige to brown, welded ignimbrites with phenocrysts of plagioclase, K-feldspar, opaque minerals, pumice fragments and well oriented shards. Ignimbrite beds b and c have minor biotite and quartz; rare hornblende is present in ignimbrite bed a. Some basal parts of ignimbrite beds a and b are vitric. An XRF analysis of ignimbrite bed b indicates a dacitic composition (sample 492-2 Table 2 Appendix2).|16-MAY-23
40759|Carramundra Member|Age reasons|The SHRIMP AS3 age of ignimbrite bed b is 309.6?4.3 Ma (sample 429-2, Figure 10d).  Late Westphalian.|16-MAY-23
3716|Carwoola Formation|Name source|Richardson (1979) cites the origin of the name as Carwoola Trig. Station at GR 193/766 on the Canberra 1:100 000 sheet area.|16-MAY-23
3716|Carwoola Formation|Unit history|Carwoola Beds (Best and others, 1964 and Oldershaw, 1965)|16-MAY-23
3716|Carwoola Formation|Type section locality|West of Hoskinstown in the vicinity of Carwoola Trig. Station where interbeds of sandstone, siltstone and shale are folded into open north-plunging anticlines and synclines (Canberra 1:100 000 sheet 8727). The formation appears to rest conformably on the Kohinoor Volcanics, while the top is not exposed.|16-MAY-23
3716|Carwoola Formation|Extent|Occurs over much of the central portion of the Captains Flat Graben. There are two main outcrop areas: a southern area forming hilly country west of Hoskintown and also a broad low ridge extending south along Primrose Valley; a northern area forming a low rise in the vicinity of Halfway Hill (GR 199/855) and tapering northwards as scattered outcrops towards Bungendore. The formation is also exposed along the western margin of the Captains Flat Graben between Kings Highway and Widgeewah Estate.|16-MAY-23
3716|Carwoola Formation|Thickness range|Oldershaw (1965) gives an estimate of 1200 m west of Hoskinstown.|16-MAY-23
3716|Carwoola Formation|Lithology|A quartz turbidite sequence of lithic and quartz sandstone with siltstone and shale. Volcanics are absent.|16-MAY-23
3716|Carwoola Formation|Depositional environment|The Carwoola Formation is a proximal quartz turbidite sequence of local derivation which indicates marine conditions and rapid subsidence in the axis of the Captains Flat Graben.|16-MAY-23
3716|Carwoola Formation|Relationships and boundaries|The Carwoola Formatio conformably overlies the Kohinoor Volcanics. Along Primrose Valley where the Kohinoor Volcanics are missing, the Carwoola Formation appears to rest on the Copper Creek Shale. East of Hoskinstown and along Primrose Valley the Carwoola Formation dips beneath and appears to be overlain conformably by the Captains Flat Formation. The Carwoola Formation is probably in part a lateral facies equivalent of the Captains Flat Formation since it appears to lens out southwards onto the Michelago 1:100 000 sheet area leaving the Captains Flat Formation to overlap onto the Kohinoor Volcanics.|16-MAY-23
3716|Carwoola Formation|Age reasons|Unfossiliferous. a late Silurian age (possibly Pridoli) deduced from stratigraphic relationships with the Kohinoor Volcanics and Captains Flat Formation.|16-MAY-23
3716|Carwoola Formation|Correlations|Tentatively with quartz turbidite sediments of the Covan Creek Formation and the Palerang Beds which also overlie Late Silurian shallow marine and felsic volcanic sequences on the Braidwood and Araluen 1:100 000 sheet areas.|16-MAY-23
24605|Chalk Mountain Formation|Name source|Chalk Mountain; GR 199148, Gilgandra Sheet 1:250 000.|16-MAY-23
24605|Chalk Mountain Formation|Type section locality|Approximately 15-18 m of lacustrine sediments of siltstone, mudstone, clay, tuff, diatomite and lignite exposed in Quarry A on the western side of Chalk Mountain - GR as above. The top is bounded by thick flows of olivine basalt; the rarely exposed base rests on basalt, andesite and trachyte.|16-MAY-23
24605|Chalk Mountain Formation|Extent|The unit is exposed in quarries around the upper escarpment of Chalk Mountain, 6 km south of the village of Bugaldie. The present area of the unit is approximately 38 hectares. The relationship of this unit to the diatomite deposits at Paddy McCulloch's Mountain and at Yearinan is not known.|16-MAY-23
24605|Chalk Mountain Formation|Thickness range|Approximately 15-18 m.|16-MAY-23
24605|Chalk Mountain Formation|Lithology|Lacustrine sediments of white to pale grey siltstone, mudstone and clay with interbedded diatomite, tuff and one lignite band near the top. Siltstone and mudstone show occasional current bedding; the diatomite exhibits (?)seasonal varves. The diatomite contains a vertebrate and invertebrate fauna and a macroflora of leaves, fruit and flowers. The diatomite and lignite contains preserved pollen and spores. Bivalves occur in a white siltstone.|16-MAY-23
24605|Chalk Mountain Formation|Relationships and boundaries|Overlies and is overlain by igneous rocks associated with the Warrumbungle Volcano. The top of the unit is a white siltstone above a thin band of lignite. This is overlain by a thick basalt flow. The base is mudstone resting on basalt, andesite and trachyte which in turn overlie the soft sandstones of the Pilliga Sandstone.|16-MAY-23
24605|Chalk Mountain Formation|Age reasons|The unit is interbedded between basalt flows from the Warrumbungle Volcano. Bands of tuff are included in the sediments. Therefore deposition of the unit took place during the active period of the Warrumbungle Volcano. K/Ar dating of igneous rocks around the volcanic complex range from 17 to 14 million years (Wellman and McDougall 1974) i.e. Middle Miocene. Fossil fish (Hills 1946), a bird (Rich and McEvey 1977) and diatoms (Griffin 1961; Thomas and Gould 1981 a and b) do not provide reliable evidence of age. The microflora described by Martin (in Holmes et al. 1983), differs from and appears to be younger than the Middle Miocene assemblages from the Gippsland Basin (Stover and Partridge, 1973). Because of its geographical location it is reasonable to assume that the Chalk Mountain locality was in a much lower rainfall area than south-eastern Australian coastal regions. Therefore the flora at Chalk Mountain would have shown adaptation to drier conditions earlier in the Miocene than floras in areas of higher rainfall. Hence the dissimilarities between the Chalk Mountain and Gippsland Basin microfloral assemblages reflect the differing environment and not time differences. Radiometric dating of the associated igneous rocks is being undertaken by Dr Ewart at the University of Queensland.|16-MAY-23
24605|Chalk Mountain Formation|References|83/23562; 79/03613; 79/04146; 81/22184; 81/22182; 79/04604.|16-MAY-23
28449|Cheitmore Limestone Member|Name source|Presumed to be after Cheitmore Caves, developed in the main mass of limestone.|16-MAY-23
28449|Cheitmore Limestone Member|Unit history|The name Cheitmore Limestone was introduced by Best et al. (1964, Canberra 1:250 000 Geological Map, 2nd edition). No formal definition has been published. Our mapping on the Araluen 1:100 000 sheet has demonstrated that it is best regarded as limestone lenses developed in the De Drack Formation and of member status. A formal definition is given for the first time.|16-MAY-23
28449|Cheitmore Limestone Member|Type section locality|On the eastern edge of the more northerly lense at GR 433462, Araluen 1:100 000 sheet.|16-MAY-23
28449|Cheitmore Limestone Member|Extent|Two small lenses, with a total area of less than 0.1 km2 in the headwaters of Neringla Creek.|16-MAY-23
28449|Cheitmore Limestone Member|Thickness range|Unknown, at least 50 m.|16-MAY-23
28449|Cheitmore Limestone Member|Lithology|Grey, strongly recrystallised massive sporite, rare patches of crinoid ossicles present. Recrystallisation caused by the Braidwood Granodiorite, which crops out close by.|16-MAY-23
28449|Cheitmore Limestone Member|Relationships and boundaries|Both lenses are surrounded by Long Flat Volcanics, which overlies the limestone. Since the Long Flat Volcanics are known elsewhere to overly the De Drack Formation conformably, and since terrigenous sediments of the De Drack Formation crop out close by, underlying the Volcanics, it is considered that the Cheitmore Limestone is best regarded as a limestone lense at the top of the De Drack Formation. It is therefore regarded as of member status, comparable with the Wyanbene, Marble Arch and Bendethera Limestone Members.|16-MAY-23
28449|Cheitmore Limestone Member|Age reasons|Conodonts indicate a Late Silurian age.|16-MAY-23
24219|Chichester Formation|Name source|Chichester is a smalll hamlet situated on the Chichester River approximately 35 km north of Dungog. Grid 46400185.|16-MAY-23
24219|Chichester Formation|Unit history|Previous nomenclature: The Copeland Road Formation of McDonald (1972) is now believed to be Chichester Formation.|16-MAY-23
24219|Chichester Formation|Type section locality|North, approximately 2 km, of Chichester. From the Upper Chichester Road down across the Chichester River in a SW direction. Grid 46200196 to 46350202.|16-MAY-23
24219|Chichester Formation|Extent|From Upper Chichester in the North to the Blackcamp Creek area east of Allyn Brook in the south. From Salisbury in the west to Brownmore in the east.|16-MAY-23
24219|Chichester Formation|Thickness range|1006 m.|16-MAY-23
24219|Chichester Formation|Lithology|Consists of 2 units; a basal Williams River Member consisting of volcanics and associated conglomerates; and a sequence of interbedded mudstone, siltstone and sandstone with minor conglomerate.|16-MAY-23
24219|Chichester Formation|Fossils|Rhipidomella fortimuscula Cvancara, Productina sp.|16-MAY-23
24219|Chichester Formation|Relationships and boundaries|Conformably overlies the Flagstaff Sandstone and is conformably overlain by the Salisbury Sandstone. It is probably contiguous with the Copeland Road Formation.|16-MAY-23
24219|Chichester Formation|Age reasons|Late Visean (CuIII B - X) - based on fossil assemblage plus dating of the approximately equivalent Martins Creek Ignimbrite Member.|16-MAY-23
4098|Clarendon Formation|Name source|Original name proposed by Walker and Hawkings (1957) from Clarendon Village (GR 785473, Windsor 1:63 360).|16-MAY-23
4098|Clarendon Formation|Unit history|First called the Clarendon Formation by Walker and Hawkins (1957). Described by Bell (1966) as Richmond Formation.|16-MAY-23
4098|Clarendon Formation|Type section locality|6 m of fine grained red-brown clayey sand and loam exposed in a road cutting on the Richmond-Bell road (GR 741419, Windsor 1:63 360).|16-MAY-23
4098|Clarendon Formation|Extent|The unit is exposed over 35 km2 as a sheet deposit underlying the villages of Richmond and Clarendon, and the Hawkesbury Agricultural College.|16-MAY-23
4098|Clarendon Formation|Thickness range|Range 4-8 m.|16-MAY-23
4098|Clarendon Formation|Lithology|Sand, clayey loam, clay content increases with depth. Transported ironstone pisolites concentrated towards top of unit.|16-MAY-23
4098|Clarendon Formation|Relationships and boundaries|Erosive into Londonderry Clay and hence overlies this unit with a probable disconformity. Erosional upper surface.|16-MAY-23
4098|Clarendon Formation|Age reasons|No floral or faunal assemblages available for dating. Unit is erosive into the Londonderry Clay. Occurs on a higher river terrace than the Cranebrook formation of Pleistocene age. The Clarendon Formation is thought to be Pliocene in age (Gobert in press).|16-MAY-23
4098|Clarendon Formation|References|01/31632|16-MAY-23
21515|Coco Range Sandstone|Name source|Coco Range which lies on Nundooka Station.|16-MAY-23
21515|Coco Range Sandstone|Unit history|Coco Range Wbeds, Ward et al. 1969.|16-MAY-23
21515|Coco Range Sandstone|Type section locality|The type section trends north eastwards from 4662 1808 (base) to 1725 1844. (GR 1:250 000, Cobham lake).|16-MAY-23
21515|Coco Range Sandstone|Extent|The formation extends 24 km northwards from Sandstone Tank in the south to northeast of "The Veldt" in the north. It probably extends subsurface NNW to the South Australian border. It also crops out south of the Silver City Highway near Gap, 323 Trig.|16-MAY-23
21515|Coco Range Sandstone|Thickness range|The formation is ~1320 m thick t the type section.|16-MAY-23
21515|Coco Range Sandstone|Lithology|The formation is composed of the following units: 1. Lower fine arenite, ~300 m thick; 2. The Valley Tank member, coarse grained arenite ~150 m thick; 3. Central fine arenite ~160 m thick; 4. Copi Dam member, coarse grained arenite, 38 m thick, and 5.  Upper fine arenite, at least 670 m thick.|16-MAY-23
21515|Coco Range Sandstone|Relationships and boundaries|The formation is unconformable on the late Precambrian Fowlers Gap Formation - its upper part is faulted out by the Nundooka Creek Fault.|16-MAY-23
21515|Coco Range Sandstone|Age reasons|Basal beds of the lower fine arenite contains Wuttagoonaspis Sp., and "Mulgaspis minor" and other species indicating an Emsian-Eifilian age (latest Early Devonian to early Mid Devonian).  The upper part of the formation could be Givetian in age.|16-MAY-23
21515|Coco Range Sandstone|References|97/28342; 79/05433;79/19200|16-MAY-23
4334|Colinton Volcanics|Name source|Village of Colinton, GR947294, Michelago 1:100 000 sheet.|16-MAY-23
4334|Colinton Volcanics|Unit history|Modified from Richardson (1979) to include the original Bransby Beds of Joplin (1943) and exclude rocks in the Tharwa-Williamsdale area now mapped as Deakin Volcanics.|16-MAY-23
4334|Colinton Volcanics|Type section locality|4km south of Colinton, Michelago 1:100 000 sheet 8726, from GR968255 (base) to GR03424 (top); rock types exposed along section include from the base going southwest-0-140m tuff; 140-270m cleaved siltstone; 270-600m dacite and tuff; 600-1780m dacitic crystal tuff; 1780-2180 m rhyolite and dacite; 2180-3300 m rhyolite; 3300-3500m ashsstone (Ingalara Ashstone Member); 3500-3600m tuff.|16-MAY-23
4334|Colinton Volcanics|Extent|Narrow meridional belt extending Queanbeyan in the north to Cooma in the south.|16-MAY-23
4334|Colinton Volcanics|Thickness range|About 4000m along type section; thicker to north, lenses out to south.|16-MAY-23
4334|Colinton Volcanics|Lithology|Dacitic and rhyolitic crystal tuff; rhyolite; dacite; tuff; ashstone; sedimentary lenses including shale, sandstone and limestone.|16-MAY-23
4334|Colinton Volcanics|Relationships and boundaries|Conformably overlies the Cappanana Formation, conformably overlain by the Rothlyn Formation; base is first major volcanic unit above sedimentary rocks of Cappanana Formation, top is first major sedimentary unit overlying volcanics or base of Billilingra Dacite Member of Rothlyn Formation.|16-MAY-23
4334|Colinton Volcanics|Age reasons|Late Silurian, from fossils in sedimentary lenses and in overlying and underlying formations, and from isotopic age determinations on Williamsdale Dacite Member.|16-MAY-23
4334|Colinton Volcanics|Defn author|G.A.M.Henderson ?1989.|16-MAY-23
4334|Colinton Volcanics|Comments|Although this appears to be an adequate draft unit definition (albeit with location issues), no evidence is available to show that this definition went through the Stratigraphy Commission approval process. The original card was supplied  to ASUD manager C. Brown by R. S. Abell, on his departure from BMR, after the publication of BMR Bulletin 233 Geology of the Canberra 1:100 000 sheet.|16-MAY-23
4334|Colinton Volcanics|References|Henderson, G.A.M., 1987. Late Silurian geology of the Michelago-Cooma area: 1:100 000 preliminary edn map. Bur. Miner. Resour. Aust. **Joplin, G.a., 1943. Petrological studies in the Ordovician of New South Wales. 2 the northern extension of the Cooma Complex. Proc. Linn. Soc. NSW, 68 (5-6), 159-83. **Richardson, S.J., 1979. Geology of the Michelago 1:100 000 sheet 8726. Geol. Surv. NSW, Sydney.|16-MAY-23
79332|Collygra Coal Member|Name source|Colygra Creek in northern New South Wales. This creek overlies the parent unit Maules Creek Formation in the Gunnedah Basin.|16-MAY-23
79332|Collygra Coal Member|Unit history|Bohena upper split or unnamed thin coal seams identified informally in well completion reports submitted to government departments by Force energy, Eastern Star Gas and Santos.|16-MAY-23
79332|Collygra Coal Member|Geomorphic expression|Concealed beneath 500-1000m of Permian-Cretaceous cover (Gunnedah and Surat Basins)|16-MAY-23
79332|Collygra Coal Member|Type section locality|Coal Seam Gas Exploration Drillhole Dewhurst 11 (Eastern Star Gas). 149.725147°E / 30.50355°S (GDA94) depths (925.69-926.81m upper split / 938.78-939.60m lower split).|16-MAY-23
79332|Collygra Coal Member|Extent|Occurs over most of the Mullaley Sub-basin where the Maules Creek Formation is present. Extends north of Narrabri to west of Werris Creek to south of Mullaley (2400 square kilometres).|16-MAY-23
79332|Collygra Coal Member|Thickness range|1.12m upper split, 0.82m lower split (2.04m combined), in type section. Range: 1 to 3m (2-3 splits ranging from 0.6-1.2m thick).|16-MAY-23
79332|Collygra Coal Member|Lithology|Coal, dull (upper split) and dull with minor bright bands (lower split). Comprises 2 splits in type section. Coal is free of stone bands.|16-MAY-23
79332|Collygra Coal Member|Depositional environment|Coal swamp (dry-terrestrial)|16-MAY-23
79332|Collygra Coal Member|Fossils|Coal.|16-MAY-23
79332|Collygra Coal Member|Diastems or hiatuses|Nil.|16-MAY-23
79332|Collygra Coal Member|Relationships and boundaries|Below the Coxs Coal Member and above the Bohena Coal Member in the Maules Creek Formation. Coalesces with the Coxs and Bohena Coal Members in Yallambee 1 drillhole north of the type section.|16-MAY-23
79332|Collygra Coal Member|Identifying features|Both splits of coal are free of stone bands and are dull. A coarse sandstone occurs between the upper split of the Collygra Coal Member and the Coxs Coal Member.|16-MAY-23
79332|Collygra Coal Member|Structure and Metamorphism|Dips at <5 degrees, probable early normal faulting is expected to be developed as observed in mining of the Maules Creek Formation in the Maules Creek Sub-basin to the east. Vitrinite reflectance values of between 0.65 and 0.85 RoMax where not heat affected by igneous intrusions.|16-MAY-23
79332|Collygra Coal Member|Age reasons|Permian - Cisuralian (Kungurian) part of Gunnedah Basin Bellata Group, contains Glossopteris and Gengamoptris (Cisuralian). Palynological age of APP32 inferred from samples above and below this interval. No tuffs are present within this seam.|16-MAY-23
79332|Collygra Coal Member|Correlations|Probable equivalent to the Doyles Hill Coal Member at Werris Ck and Thornfield seam within the Maules Creek Sub-Basin.|16-MAY-23
79332|Collygra Coal Member|Alteration and Mineralisation|Coal - Bituminous in rank.|16-MAY-23
79332|Collygra Coal Member|Geophysical Expression|Unlikely seismic reflector, low downhole gamma (<50) and density (<1.50g/cc) geophysical response.|16-MAY-23
79332|Collygra Coal Member|Defn author|Mark Dawson, 10-FEB-2016.|16-MAY-23
24223|Cookeys Plains Formation|Name source|Parish of Cookeys Plains, County Cunningham|16-MAY-23
24223|Cookeys Plains Formation|Type section locality|Thinly bedded quartzose sandstone, calcaraeous (usually leached) in part, with occasional limestone lenses, and grey mudstone/shale, approximately 1300 m thick, exposed in low outcrops between the Black Range (Forbes 1:250 000 GR 5665 9165) and the Byong Range (do., GR 5710 9125).|16-MAY-23
24223|Cookeys Plains Formation|Extent|Scattered outcrops, very poor where shales are dominant, extend for some 40 km from just west of Byong Range (Forbes 1:250 000 to GR 570913) to about Gobondery (Narromine 1:250 000 GR 5635 9575).|16-MAY-23
24223|Cookeys Plains Formation|Thickness range|1100 m approximately, east of Black Range.|16-MAY-23
24223|Cookeys Plains Formation|Lithology|The iron stained blocky sandstones are the dominant rock type, but this possibly reflects their better outcrops. These grade laterally and vertically into calcareous sandstones (usually skeletal because of leaching) and marls. The limestones are thickly bedded, and consist principally of coralline and algal debris. Near Kadungle there are thick crossbedded units of quartzose sandstone.|16-MAY-23
24223|Cookeys Plains Formation|Relationships and boundaries|Within the Derriwong Group, overlies the Edols Conglomerate, and is overlain in turn by the Byong Volcanics. North of Trundle the contact with the Yarrabandai Formation is yet unclear. Contact with the Edols Conglomerate is believed to be conformable, but contact with the overlying Byong Volcanics is uncertain. North of Trundle, where the Byong Volcanics are absent, trends observed suggest conformity with the overlying Yarrabandai Formation.|16-MAY-23
24223|Cookeys Plains Formation|Age reasons|Earlymost Devonian - fossils include Encrinurus, Shaleria cf. Armaghensis, Molongia elegans capricornae, Warburgella jelli, Iridostrophia sp., Howellella spp., Pleurodictyum sp.|16-MAY-23
24224|Cookopie Monzonite|Name source|Parish Cookopie, County Kennedy, Narromine 1:250 000 sheet.|16-MAY-23
24224|Cookopie Monzonite|Type section locality|Two small outcrops at GR 62109465 and GR 62159442. Narromine 1:250 000 sheet.|16-MAY-23
24224|Cookopie Monzonite|Extent|Two small outcrops occur, some 2.5 km apart and at a distance of 7.5 km and 5.5 km SW of Peak Hill.|16-MAY-23
24224|Cookopie Monzonite|Lithology|Hornblende monzonite.|16-MAY-23
24224|Cookopie Monzonite|Relationships and boundaries|Isolated outcrops in Quaternary alluvium and probably intrudes Late Ordovician, Goonumbla Volcanics.|16-MAY-23
24224|Cookopie Monzonite|Age reasons|Siluro Devonian because of stratigraphic relationships.|16-MAY-23
25856|Coolamine Igneous Complex|Name source|Coolamine homestead; GR 507580, Tantangara 1:100 000 Sheet area.|16-MAY-23
25856|Coolamine Igneous Complex|Type section locality|No type localaity is given in view of the wide compositional variation shown by the bodies forming the complex.|16-MAY-23
25856|Coolamine Igneous Complex|Extent|Ten individual intrusions form the Complex. They all occur in the Cooleman Plains area northeast of Kiandra.|16-MAY-23
25856|Coolamine Igneous Complex|Lithology|Porphyritic, two pyroxene granodiorite, pyroxene and hornblende adamellite, hornblende quartz gabbro, pyroxenite, quartz monzogabbro, quartzmonzodiorite.|16-MAY-23
25856|Coolamine Igneous Complex|Relationships and boundaries|The bodies intrude the Cooleman Limestone, Kellys Plain Volcanics, Gurrangorambla Granophyre and Blue Waterhole Beds and are intruded by the Jackson Granite. Some of the bodies are the intrusive equivalent of the Rolling Grounds Latite.|16-MAY-23
25856|Coolamine Igneous Complex|Age reasons|Early Devonian as the bodies intrude the Late Silurian Cooleman Limestone and Kellys Plain Volcanics and they are in part equivalent to the Early Devonian Rolling Grounds Latite. The Latite conformably underlies the Early Devonian Mountain Creek Volcanics.   Note: The distribution is given on the Tantangara 1:100 000 preliminary geological sheet (1974).|16-MAY-23
29939|Coomber Formation|Name source|"Coomber" homestead GR 750627, Mudgee 1:100 000 Sheet area (8832).|16-MAY-23
29939|Coomber Formation|Unit history|Much of the Coomber Formation was previously included in the Lue beds, Gulgamree beds and the Dungeree Volcanics (Offenberg et al. 1971; Pemberton et al. 1994).|16-MAY-23
29939|Coomber Formation|Type section locality|1750 m of mainly lithic sandstone with minor radiolarian chert at the top of the section and rare andesite lava occur between GR 746652 and GR 728652 (Mudgee) along the Cudgegong River, although the lower contact of the unit is not exposed here but occurs at GR 586900 (Mudgee). Another representative section occurs along Pipe Clay Creek between GR 584962 and GR 528965 (Mudgee).|16-MAY-23
29939|Coomber Formation|Extent|The unit is exposed over 100 km2 in the Botobolar-Havilah-Lue district, in three areas totalling approximately 10 km2 5 km west of Rylstone and in an 5 km2 area 8 km northwest of Rylstone.|16-MAY-23
29939|Coomber Formation|Thickness range|A minimum thickness of 850 m occurs west of Bara Creek (GR 580900 Mudgee) and over 1750 m in the type section.|16-MAY-23
29939|Coomber Formation|Lithology|The unit consists of seven facies: (I) massive lithic sandstone, rare conglomerate: (ii) thin-bedded sandstone and mudstone; (iii) siliceous mudstone and chert; (iv) limestone blocks and calcareous mudstone; (v) basalt-andesite lavas; (vi) mafic-intermediate intrusions; and (vii) quartz-feldspar porphyry.|16-MAY-23
29939|Coomber Formation|Relationships and boundaries|Conformably overlies the Early Ordovician Adaminaby Group which contain quartz-rich sandstones, mudstones and chert. Disconformably overlain by the Late Silurian Dungeree Volcanics with a basal conglomerate containing clasts derived from the underlying Coomber Formation at the top of the type section (Fergusson and Colquhoun in prep.). Intruded by the Pyangle Pass Granite of presumed Carboniferous age and angularly unconformably overlain by the Late Carboniferous-Early Permian Rylstone Volcanics and the basal Permian Shoalhaven Group (Pemberton et al. 1994).|16-MAY-23
29939|Coomber Formation|Age reasons|The unit contains no age-diagnostic fossils but is constrained to the Late Ordovician-Early Silurian from boundary relationships.|16-MAY-23
29939|Coomber Formation|Comments|The Coomber Formation was formally named by Pemberton et al. (1994). A more complete description of the unit and its extent will be given by Fergusson & Colquhoun (in prep.).|16-MAY-23
29939|Coomber Formation|References|79/03255; 94/28015.|16-MAY-23
4616|Coonigan Formation|Name source|Coonigan Creek, northeastern Broken Hill 1:250 000 sheet area|16-MAY-23
4616|Coonigan Formation|Type section locality|31o10.3'S 142o19.3'E (base) to 31o10.2'S 142o19.4'E (top), western flank of syncline.|16-MAY-23
4616|Coonigan Formation|Extent|Northeastern Broken Hill 1:250 000 sheet area, in syncline on western side of valley drained by Mount Wright Creek; small area immediately south of Mount Wright Tank.|16-MAY-23
4616|Coonigan Formation|Thickness range|115 m in type section (Warris 1967, unpubl.).|16-MAY-23
4616|Coonigan Formation|Lithology|Light grey limestones overlain by white shales in type section; white shales (time equivalent of limestones) immediately south of Mount Wright Tank.|16-MAY-23
4616|Coonigan Formation|Relationships and boundaries|Irregular, apparently conformable relationship with underlying Cymbrie Vale Formation. Separated from overlying Nootumbulla Sandstone (basal unit of Mootwingee Group) by regional disconformity.|16-MAY-23
4616|Coonigan Formation|Age reasons|Middle Cambrian. Trilobites indicate an Ordian age for lower (limestone) part, Templetonian age for upper (shale) part (Opik 1968; Runnegar & Jell 1976).|16-MAY-23
4616|Coonigan Formation|Proposed publication|Palaeontographica A.177 p.129-212.|16-MAY-23
76918|Coopernook Conglomerate Member|Name source|The name Coopernook Conglomerate Member is derived from the village of Coopernook, near which the unit crops out extensively.  31deg49' 34.41"S, 152deg36' 35.81"E.|16-MAY-23
76918|Coopernook Conglomerate Member|Unit history|This member was previously the lower part of the (then undifferentiated) Camden Head Claystone.|16-MAY-23
76918|Coopernook Conglomerate Member|Geomorphic expression|Where conglomerate dominates, the Coopernook Conglomerate Member is often cliff-forming while the upper part of the member - with a finer component - forms a more rounded topography. Where the upper part has been eroded fully and the conglomerate has been deeply weathered, such as in the Coopernook to Coralville area, the unit forms a gently undulating topography.|16-MAY-23
76918|Coopernook Conglomerate Member|Type section locality|The type section for the Coopernook Conglomerate Member is nominated as from Tunnel Road GR 474286 6512671(1:25 000 map sheet 9434-4-N, Byabarra; location 26) next to the Kings Creek Bridge southwards along the Bago Road to GR 474108 6512416 (1:25 000 map sheet 9434-4-N, Byabarra; location 24).|16-MAY-23
76918|Coopernook Conglomerate Member|Description at type locality|The top of the member is defined as the top of the uppermost conglomerate bed in this section and is conformably overlain by the remainder of the Camden Head Claystone. The base of the formation is not exposed in this section, although the lowest exposure is thought to be only a few metres above the Palaeozoic basin floor rocks. Elsewhere, the base of the Coopernook Conglomerate Member, is defined as the bed which rests on the Jolly Nose Conglomerate, as at location 21 or the Palaeozoic rocks of the basin floor, as at location 202. A lithology plot of the type section is shown as part of the lithology graphic for the Camden Head Claystone in Figure 5. In its type section the Coopernook Conglomerate Member is an upward-fining sequence of interbedded pebble and granule lithic quartzose conglomerate and sandstone with minor, generally grey, mudstone, although some mudstone has a distinctive reddish purple colour. Bedding thickness in the conglomerates ranges from very thick to thin bedded, the thicker beds becoming less frequent upwards in the section. Conglomerate beds in the basal 10 m to 20 m may contain cobble- and jasper-rich bands up to 1 m in thickness. However, these bands are rarely repeated and are often interbedded with reddish purple mudstone. These features, together with different jasper and quartz clast percentages (of total clasts), distinguish the unit from the Laurieton Conglomerate.|16-MAY-23
76918|Coopernook Conglomerate Member|Extent|The Coopernook Conglomerate Member is a widespread unit in the Triassic sequence of the Lorne Basin. It is present around the perimeter of the basin from Coralville in the southeast then westward and northwestward along the Lansdowne Escarpment, where it forms the cliff line, to the Lorne-Comboyne Road in the west of the basin and then to 5 km northeast of Mount Comboyne (Map 1). In the north of the basin the Coopernook Conglomerate Member is developed along the Broken Bago Range and east from the Bago Road to the Pacific Highway and Kew. The member crops out west of Bonny Hills both north of the Jolly Nose Hill and south towards Queeens Lake. A further outcrop of the Coopernook Conglomerate Member occurs around the perimeter of a circular, 7 km diameter exposure of Carboniferous basin floor rocks between Hannam Vale and Moorland, the Holey Flat Uplift. Another exposure crops out around part of the perimeter of the Black Creek Uplift, from the Lorne Road between Lorne and Upsalls Creek to near Mount Comboyne (location 101). A further, near-vertical outcrop strata occurs adjacent to the Bagnoo Fault on Old School Road, 5 km northwest of Herons Creek at location 43 (Map 1).|16-MAY-23
76918|Coopernook Conglomerate Member|General description|Reddish purple mudstone occurs at or very close to the base of the unit in several other exposures throughout the basin. In some places, channel deposits rest on the basin floor and these often contain cobbles and an elevated proportion of jasper clasts as seen in Taylors Quarry, Kew at Locations 54 and 55 or in the west at Locations 100, 101 and 197. Towards the centre of the basin the conglomerate tends to be finer grained.|16-MAY-23
76918|Coopernook Conglomerate Member|Thickness range|Although most measured sections do not expose both the top and base of the member, most are considered to start within a few metres of the base. The member has an estimated thickness throughout the basin of between 30 m and 50 m. The greatest thickness (estimated maximum 50 m) is developed in the west of the basin in the Mount Comboyne area.|16-MAY-23
76918|Coopernook Conglomerate Member|Lithology|The type section of the Coopernook Conglomerate (Figure 5) consists of conglomerate 41%; sandstone 17%; and mudstone (siltstone, claystone) 42%. The general bed thinning and upward-fining trend can be seen in outcrop in Photograph 2. At the type section, jasper clasts constitute 16% and quartz clasts 37% of the total clasts while the average of 51 samples (each of 100 pebbles) throughout the basin was jasper 15% and quartz 36% of total clasts. In conglomerate exposures throughout the basin, there are less than 3 cobbles per 0.5 m × 0.5 m square. Table 2 presents the jasper and quartz clast percentages of total clasts measured in 46 locations. (At some locations two separate samples were taken.) The significant proportion of chert and jasper clasts is typical of the New England Orogen provenance which is also commonly the provenance of Triassic strata in the Gunnedah Basin and northern Sydney Basin. The input of quartz as clasts into the Gunnedah Basin and Sydney Basin is considered to be from Lachlan Orogen (to the west) but the source of quartz clasts for the Lorne Basin is uncertain. It may have been from the Lord Howe Island Rise to the east. Chert and jasper are also common in the Watonga Formation, immediately northeast of the Lorne Basin.|16-MAY-23
76918|Coopernook Conglomerate Member|Depositional environment|Interbedded sheet sands and muddy overbank deposits with incised channel sands indicate a fluviatile environment for deposition of the member. A good example is seen at location 75 (Photograph 3).|16-MAY-23
76918|Coopernook Conglomerate Member|Relationships and boundaries|The member conformably overlies the Jolly Nose Conglomerate in the northeastern part of the Lorne Basin, as at Cowarra Quarry (location 21). Elsewhere it unconformably overlies the Palaeozoic basement as at Taylors Quarry, Kew (locations 54 and 55). This exposure has been destroyed by recent roadworks. The Coopernook Conglomerate Member is conformably overlain by the remainder of the Camden Head Claystone as in the type sections for both units at location 24.|16-MAY-23
76918|Coopernook Conglomerate Member|Identifying features|The member is predominantly (about 60%) conglomerate and sandstone. Cobbles are rare, and there are few very thick (>100 cm) beds. The very thick beds usually occur as individual layers rather than stacks of several very thick beds. Thin interbedded reddish purple mudstone is common, enabling the unit to be readily distinguished from the Grants Head Formation and the otherwise very similar Coorabakh Conglomerate - in both of which reddish purple mudstones are very rare or absent. Jasper clasts are usually <20% and quartz clasts usually >25%.  The base of the Coopernook Conglomerate Member coincides with that of the Camden Head Claystone and the top of the member is the uppermost bed of pebble conglomerate overlain by sandstone or reddish purple mudstone.|16-MAY-23
76918|Coopernook Conglomerate Member|Structure and Metamorphism|Outcrops around the basin perimeter generally have a slight dip towards the basin centre, usually less than 10 degrees. Within the basin the Coopernook Conglomerate Member has been folded to very steep dips around two circular zones in which the basement rocks have been uplifted through the Triassic cover. On the Old School Road, at location 43, the member has been tilted to a near vertical position adjacent to the Bagnoo Fault.|16-MAY-23
76918|Coopernook Conglomerate Member|Age reasons|Although fossils have not been recovered from the member, an Early Triassic age is indicated by the conformable stratigraphic position of the Coopernook Conglomerate Member at the base of the Camden Head Claystone, the top part of which contains megaflora fossils of probable late Early Triassic age (Holmes & Ash 1979).|16-MAY-23
76918|Coopernook Conglomerate Member|Correlations|There are no units in the Lorne Basin with which this member correlates.|16-MAY-23
76918|Coopernook Conglomerate Member|Defn author|Winston Pratt 7-JUL-2010.|16-MAY-23
76918|Coopernook Conglomerate Member|References|Holmes W.B.K. & Ash S.R. 1979. An early Triassic megafossil flora from the Lorne Basin, New South Wales. Proceedings of the Linnean Society of New South Wales, 103, 47-70. **Pratt, G.W. 2010. A revised Triassic stratigraphy for the Lorne Basin, NSW. Quarterly Notes of the Geological Survey of New South Wales 126.|16-MAY-23
75739|Coorabakh Conglomerate|Name source|The Coorabakh Conglomerate is named after the Coorabakh National Park where the formation is exposed in the cliffs forming part of the Lansdowne Escarpment. Coorabakh National Park Lat 31deg 42min 43.85sec S, Long 152deg 31min 20.59sec E.|16-MAY-23
75739|Coorabakh Conglomerate|Unit history|The conglomerate was earlier mapped as part of the Laurieton Conglomerate (Pratt & Herbert 1973).|16-MAY-23
75739|Coorabakh Conglomerate|Geomorphic expression|The conglomerate is cliff-forming, with both west-facing and northeast-facing cliffs between the Nellies Flat Fault and Dellward Fault (as can be seen from location 273; Photograph 7) and north-facing cliffs along the top of the Broken Bago Range. There is often a noticeable change of slope and change in soil colour at the boundary of the formation and the underlying less-resistant Camden Head Claystone.|16-MAY-23
75739|Coorabakh Conglomerate|Type section locality|Along Oskies Trail from Lat 31.67830deg S, Long 152.51521deg E to Lat 31.67953deg S, Long 152.50896 E. An exposure of the Coorabakh Conglomerate measurable as a type section has not been located. However, good exposures suitable for, and designated as, a type location are present along Oskies Trail from GR 54050 6495119 (1:25 000 map sheet 9434-4-S, Lorne; location 331) to GR 453458 6494980 (1:25 000 map sheet 9434-4-S, Lorne; location 328).|16-MAY-23
75739|Coorabakh Conglomerate|Description at type locality|Loose boulders and outcrop are exposed along Oskies Trail from location 331 westwards to the junction with the Coopernook Forest Way where, about 100 m to the south, the unit is exposed at the cliff top of the Lansdowne Escarpment at location 228. The Coorabakh Conglomerate is a dominantly pebble to granule conglomerate with interbedded sandstone and minor cobble conglomerate bands. Beds of reddish purple mudstone are absent. The formation frequently changes from thick to medium bedding although thick beds form the majority. The bed contacts are often gradational. The base of the unit is defined as the bed resting on the uppermost reddish purple mudstone of the Camden Head Claystone. The top of the unit is not constrained by other exposed overlying units.|16-MAY-23
75739|Coorabakh Conglomerate|Extent|Between the Nellies Flat Fault and Dellward Fault the conglomerate is exposed along the Lansdowne Escarpment (in the southwestern part of the Lorne Basin). It extends northeastwards to terminate in a northeast-facing cliff line overlooking Stewarts River, and also forms the capping along the top of the Broken Bago Range in the north. The formation is not preserved in the central part of the basin.|16-MAY-23
75739|Coorabakh Conglomerate|Thickness range|No strata overlie the Coorabakh Conglomerate, so the true thickness is not known. However, an estimated minimum thickness of approximately 30 m is suggested from exposures on both the Lansdowne Escarpment and the Broken Bago Range.|16-MAY-23
75739|Coorabakh Conglomerate|Lithology|At the type location, jasper clasts in the Coorabakh Conglomerate made up 11% and quartz clasts 54% of the total clasts (the average of the two samples, each 100 pebbles), while the average of nine samples (each 100 pebbles) throughout the Lorne Basin was jasper 16% and quartz 39% of total. Quartz clasts dominate (usually >25%) over jasper clasts (usually <20%). However there is a slight increase in the proportion of jasper clasts eastwards along the Broken Bago Range. Table 4 presents the jasper and quartz clast percentages of total clasts measured at seven locations. The significant proportion of chert and jasper clasts is typical of a New England Orogen provenance. A possible source of the high proportion of quartz was mentioned under the Coopernook Conglomerate Member of the Camden Head Claystone.|16-MAY-23
75739|Coorabakh Conglomerate|Depositional environment|The rapid variation from poorly sorted cobble conglomerates to moderately well-sorted sandstones, the rapid and alternating bed thicknesses, and the absence of overbank deposits with incised channel deposits suggest a fluvial braid plain environment for deposition of the Coorabakh Conglomerate. The coarser beds suggest rapid deposition in the deeper major channels. Such an environment would feature rapid deposition from a range of probably shortlived and variable flows with an abundant supply of clast material.|16-MAY-23
75739|Coorabakh Conglomerate|Relationships and boundaries|Of Camden Haven Group. This conglomerate conformably overlies the Camden Head Claystone throughout the Lorne Basin. No overlying strata have been located. The base of the formation is the top of the uppermost bed of reddish purple mudstone of the Camden Head Claystone. The top of the formation is not defined.|16-MAY-23
75739|Coorabakh Conglomerate|Identifying features|The conglomerate is distinguished by its stratigraphic position, the relative proportion of quartz and jasper clasts, its bedding geometry and the absence of interbedded reddish purple mudstone. While the Coorabakh Conglomerate is very similar to the Coopernook Conglomerate Member of the Camden Head Claystone in terms of the relative proportion quartz and jasper clasts and its bedding geometry, it is differentiated from the Coopernook Conglomerate Member by its stratigraphic position and the absence of beds of reddish purple mudstone.|16-MAY-23
75739|Coorabakh Conglomerate|Structure and Metamorphism|The Coorabakh Conglomerate dips towards the basin centre, at angles of between 6° and 10°.|16-MAY-23
75739|Coorabakh Conglomerate|Age reasons|Fossils have not been recovered from the Coorabakh Conglomerate. However being the lateral equivalent of the Laurieton Conglomerate - which is constrained above and below by palynological evidence suggesting a late Early Triassic age (Helby 1970, 1971, 1972) - the Coorabakh Conglomerate is also considered to be of that age.|16-MAY-23
75739|Coorabakh Conglomerate|Correlations|The conglomerate is considered to be the lateral equivalent of the Laurieton Conglomerate.|16-MAY-23
75739|Coorabakh Conglomerate|Defn author|G. Winston Pratt , 7-JUL-2010.|16-MAY-23
75739|Coorabakh Conglomerate|Comments|Separated from the Laurieton Conglomerate on lithological grounds. Coorabakh is more quartz rich than the Laurieton.|16-MAY-23
75739|Coorabakh Conglomerate|References|Helby R.J. 1970. Plant microfloras from the Lorne Basin. Geological Survey of New South Wales, Palynology Report 1970/07. ** Helby R.J. 1971. Review of Late Permian and Triassic palynology of New South Wales. Geological Survey of New South Wales Palynology Report 1971/06. Geological Survey of New South Wales, Report GS 1971/595. **Helby (1972) GS NSW Report Palynology 1972/3. **Helby R.J. 1973. Review of Late Permian and Triassic palynology of New South Wales. Geological Society of Australia Special Publication 4, pp. 141-155. **Pratt, G.W. 2010. A revised Triassic stratigraphy for the Lorne Basin, NSW. Quarterly Notes of the Geological Survey of New South Wales 126.|16-MAY-23
34357|Copi Dam Arenite Member|Name source|Copi Dam lies ~10 km NNW of Nundooka Station.|16-MAY-23
34357|Copi Dam Arenite Member|Type section locality|The type section is made in the northeast trending creek which lies 1 km south of Copi Dam (c.f. GR 4718 1877, 1:250 000 Cobham Lake).|16-MAY-23
34357|Copi Dam Arenite Member|Extent|The member extends northwards for 25 km from south of Sandstone Dam to east of The Veldt.|16-MAY-23
34357|Copi Dam Arenite Member|Thickness range|The member is 38 m thick at the type section.|16-MAY-23
34357|Copi Dam Arenite Member|Lithology|At the type section the member is composed of a basal pebbly coarse and very coarse arenite 17 m thick, overlain by fine grained arenite 10 m thick and followed by an upper coarse grained pebbly arenite 11 m thick.|16-MAY-23
34357|Copi Dam Arenite Member|Relationships and boundaries|The member is conformable with the Central fine arenite (below) and the Upper fine arenite (above), Coco Range Sandstone.|16-MAY-23
34357|Copi Dam Arenite Member|Age reasons|The member is most likely to be Emsian-Eifelian in age - it could, however, be Givetian, based on fossils in basal beds of Coco Range Sandstone.|16-MAY-23
34357|Copi Dam Arenite Member|References|79/05433|16-MAY-23
4677|Copper Creek Shale|Name source|Derived from Copper Creek, a small tributary of the Molonglo River at Captains Flat (GR 206/584) on the Michelago 1:100 000 sheet area (Richardson 1979).|16-MAY-23
4677|Copper Creek Shale|Unit history|Copper Creek beds (Glasson and Paine, 1965).|16-MAY-23
4677|Copper Creek Shale|Type section locality|Designated as Copper Creek and an adjacent road cutting near Captains Flat Railway Station (GR 207/586) on the Michelago 1:100 000 sheet 8726 (Oldershaw 1965 and Richardson 1979).  Here the formation crops out as tightly folded beds of dark grey shale and siltstone with subordinate sandstone. On the Canberra 1:100 000 sheet 8727, a representative section is exposed in a road cutting at GR 160/710. Here similar rock types show sedimentary structures but the thickness is unclear as beds may be repeated in isoclinal folds.|16-MAY-23
4677|Copper Creek Shale|Extent|Crops out poorly along the eastern edge of the Captains Flat Graben. Good exposures occur in the road and rail cuttings north of Captains Flat Mine. A few outcrops are found in Primose Valley (western limb of Captains Flat Graben).|16-MAY-23
4677|Copper Creek Shale|Thickness range|Estimated as 60-150 m (Richardson 1979).|16-MAY-23
4677|Copper Creek Shale|Lithology|Thin-bedded greyish-black shale, siltstone and sandstone with minor limestone and tuff. Discontinuous beds of quartzite and conglomerate at the base are representative of the Rutledge Quartzite Member.|16-MAY-23
4677|Copper Creek Shale|Depositional environment|Marine turbidite facies - presence of limestone suggests locally shallow marine conditions.|16-MAY-23
4677|Copper Creek Shale|Relationships and boundaries|The basal unit of the Copper Creek Shale (Rutledge Quartzite Member) rest unconformably on Late Ordovician rocks. Where this basal unit is absent the lower boundary is conjectural since the Copper Creek Shale is lithologically similar to the Ordovician rocks. Near Captains Flat on the Michelago 1:100 000 sheet the Copper Creek Shale passes gradationally up into the Kohinoor Volcanics (Richardson 1979).  Along Primrose Valley the Kohinoor Volcanics are absent and the Copper Creek Shale appears to dip disconformably beneath the Carwoola Formation. Along the eastern margin of the Captains Flat Graben the Copper Creek Shale is in contact with the Captains Flat Formation but the nature of this contact is conjectural.|16-MAY-23
4677|Copper Creek Shale|Age reasons|Late Silurian (Ludlow?) based on rugose corals (Oldershaw 1965 and Talent and others, 1975).|16-MAY-23
4677|Copper Creek Shale|Correlations|De Drack Formation (Huleatt 1971) and Cappannana Formation (Richardson 1979).|16-MAY-23
24228|Coradgery Monzonite|Name source|Coradgery Homestead (GR 60939300 Narromine 1:250 000 sheet).|16-MAY-23
24228|Coradgery Monzonite|Type section locality|Coradgery mine, GR 61839300|16-MAY-23
24228|Coradgery Monzonite|Extent|One small area exposed by auger drilling.  Size: 150 m x 150 m.|16-MAY-23
24228|Coradgery Monzonite|Lithology|Mafic quartz monzonite.|16-MAY-23
24228|Coradgery Monzonite|Relationships and boundaries|Intrusive into the Wombin Volcanics of Late Silurian age.|16-MAY-23
24228|Coradgery Monzonite|Age reasons|Intrusion probably of Middle Devonian age.|16-MAY-23
4718|Coreen Creek Coal Member|Name source|Coreen Creek; 4 km NE of D.M. Oaklands R.D.H. 1 (GR DA 095597) and 6 m S of D.M. Oaklands R.D.H. 3 (GR DA 215587), Buraja 1:100 000 sheet, where the coal member was first observed.|16-MAY-23
4718|Coreen Creek Coal Member|Type section locality|1.39 m thick coal seam with sharp erosive top and distinct base. The top is identified by mudstone or sandstone, medium, grey with brown tint, cross bedded with coaly lamellae. The bottom is identified by a claystone or siltstone dark brown, micaceous with coaly lamellae. Found in D.M. Oaklands R.D.H. 4 (GR DA 952638) from 218.29 m to 219.68 m.|16-MAY-23
4718|Coreen Creek Coal Member|Extent|The unit occurs only in the subsurface. Its subcrop extends over about 500 km2 in the central portion of Jerilderie 1:250 000 sheet and probably further north.|16-MAY-23
4718|Coreen Creek Coal Member|Thickness range|Range about 0.50 m to 1.50 m.|16-MAY-23
4718|Coreen Creek Coal Member|Lithology|Coal dull, tends to coal inferior, clayey; sporadic bright coal lamellae; becomes very clayey towards its base; it can deteriorate locally into black, carbonaceous mudstone (D.M. Oaklands R.D.H. 17; GR DA 162740).|16-MAY-23
4718|Coreen Creek Coal Member|Relationships and boundaries|Top part of the Loughmore Formation (Palese and Morgan, in prep.). Conformably overlies the non-coal bearing sequence of the Formation. It is unconformably overlain by the Nowranie Creek Formation (Palese and Morgan, in prep.)|16-MAY-23
4718|Coreen Creek Coal Member|Age reasons|Minor Glossopteris remains. Microflora is dominated by bisaccate grains, as in the remainder of the Loughmore Formation (Palese and Morgan, in prep.), especially by Luekisporites. Rare Monosaccates, with Bascanisporites undosus mainly represented. Diagnostic forms include Marsupipollenites sinuous, Didecitriletes ericianus, Dulhuntyispora parvicula, Microreticulatisporites bitriangulatus, Peltacystia spp. and Quadrisporites horridus. This microflora is assigned to the Upper Stage 5 of Paten (1969), which identifies the Upper Permian age (Guadalupian).|16-MAY-23
4718|Coreen Creek Coal Member|Comments|The roof and floor of the coal seam are preserved in the NSW Department of Mines Core Library in Londonderry, near Penrith. The coal seam was destroyed for sampling purposes and the resulting analyses are available in the bore logs (GS 1974/090).|16-MAY-23
4718|Coreen Creek Coal Member|References|79/05280; ? R003|16-MAY-23
4751|Corringle Formation|Name source|Corringle railway siding.|16-MAY-23
4751|Corringle Formation|Type section locality|Along east-west road, 3.5 km north of Lake View homestead. 533847 (bottom) to 532847 (top) Forbes 1:250 000.|16-MAY-23
4751|Corringle Formation|Extent|Outcrops for about 10 km along strike between Corringle and Burcher.|16-MAY-23
4751|Corringle Formation|Thickness range|About 100 m.|16-MAY-23
4751|Corringle Formation|Lithology|Greenish-brown sericitic quartz-feldspar rock with breccia texture. Probably tuffaceous breccia or paraconglomerate. Fragments about 1 cm average.|16-MAY-23
4751|Corringle Formation|Relationships and boundaries|Lithologically distinct and conformable with overlying Burcher greywacke. Slight interbedding with underlying Banar Formation.|16-MAY-23
4751|Corringle Formation|Age reasons|Probably Silurian, from stratigraphic position.|16-MAY-23
4751|Corringle Formation|Proposed publication|Bulletin Aust. Soc. Exploration Geophysicists (v.7, No. 1)|16-MAY-23
4789|Covan Creek Formation|Name source|"Covan Creek" property, GR 259678, Goulburn 1:250 000 sheet.|16-MAY-23
4789|Covan Creek Formation|Unit history|The Covan Creek Formation is shown on the Canberra 1:250 000 metallogenic map (Gilligan, 1974) as Late Silurian De Drack Formation.|16-MAY-23
4789|Covan Creek Formation|Type section locality|In a creek between GR 395151 (bottom) and GR 386150 (top) Braidwood 1:100 0000 sheet. About 800 m area exposed in this section.|16-MAY-23
4789|Covan Creek Formation|Extent|Extends over an area of approximately 450 km2 centred on Currawang village, GR 252680, Goulburn 1:250 000 sheet.|16-MAY-23
4789|Covan Creek Formation|Thickness range|About 1200 m (maximum)|16-MAY-23
4789|Covan Creek Formation|Lithology|Medium-grained, thick-bedded quartz-lithic arenite and greywacke, occasionally graded or laminated; quartzite; siltstone, often cross-bedded on a small scale or laminated; shale.|16-MAY-23
4789|Covan Creek Formation|Relationships and boundaries|The top of the Covan Creek Formation is not exposed and appears to have been removed by erosion. It is unconformably overlain by the late Early Devonian Tarago Conglomerate at one locality (GR 398163, BRAIDWOOD 1:100 000 sheet). Its relationship with underlying Late Silurian rocks is variable and appears to be conformable with the Currawang Basalt in the Currawang area (GR 25206780, Goulburn 1:250 000 geological sheet) and disconformable with the Woodlawn Volcanics and De Drack Formation elsewhere. Marked unconformity is unlikely because the Covan Creek Formation is structurally continuous with the Late Silurian rocks.|16-MAY-23
4789|Covan Creek Formation|Age reasons|On stratigraphic and structural grounds the Covan Ceek Formation appears to be of Late Silurian to early Early Devonian age. Possible plant fragments from a locality at GR 329235 (BRAIDWOOD 1:100 000 sheet) may indicate an age of earliest Devonian (Sherwin, 1973).|16-MAY-23
79333|Coxs Coal Member|Name source|Cox's Creek in northern New South Wales. This creek overlies the parent unit Maules Creek Formation in the Gunnedah Basin.|16-MAY-23
79333|Coxs Coal Member|Unit history|Upper Maules Creek seam or Parkes seam used informally in well completion reports submitted to government departments by Force energy, Eastern Star Gas and Santos.|16-MAY-23
79333|Coxs Coal Member|Geomorphic expression|Concealed beneath 500-1000m of Permian-Cretaceous cover (Gunnedah and Surat Basins).|16-MAY-23
79333|Coxs Coal Member|Type section locality|Coal Seam Gas Exploration Drillhole Dewhurst 11 (Eastern Star Gas). 149.725147°E / 30.50355°S (GDA94) depth (913.85-916.80m).|16-MAY-23
79333|Coxs Coal Member|Extent|Occurs over most of the Mullaley Sub-basin where the Maules Creek Formation is present. Extends north of Narrabri to west of Werris Creek to south of Mullaley (1800 square kilometres).|16-MAY-23
79333|Coxs Coal Member|Thickness range|2.95 m in type section. Range : 1 to 4m.|16-MAY-23
79333|Coxs Coal Member|Lithology|Coal, dull with bright bands. Comprises a single split in type section. One stone band of carbonaceous mudstone (19cm thick) occurs within the seam. Generally, occurs as a single seam with a sandstone/mudstone parting 10-30cm thick, 60cm from the top of the seam.|16-MAY-23
79333|Coxs Coal Member|Depositional environment|Coal swamp (wet-terrestrial).|16-MAY-23
79333|Coxs Coal Member|Fossils|Coal.|16-MAY-23
79333|Coxs Coal Member|Diastems or hiatuses|Nil.|16-MAY-23
79333|Coxs Coal Member|Relationships and boundaries|Located below the Tullamullen Coal Member and above the Collygra Coal Member in the Maules Creek Formation. Coalesces with the Collygra and Bohena Coal Members in Yallambee 1 drillhole to the north of the type section.|16-MAY-23
79333|Coxs Coal Member|Identifying features|A sandstone/mudstone parting 10-30cm thick, 60cm from the top of the seam is a common distinguishing feature using downhole geophysics. Occurs above a conglomerate/coarse sandstone unit of the Maules Creek Formation.|16-MAY-23
79333|Coxs Coal Member|Structure and Metamorphism|Dips at <5 degrees, probable early normal faulting is expected to be developed as observed in mining of the Maules Creek Formation in the Maules Creek Sub-basin to the east. Vitrinite reflectance values of between 0.65 and 0.85 RoMax where not heat affected by igneous intrusions.|16-MAY-23
79333|Coxs Coal Member|Age reasons|Permian - Cisuralian (Kungurian) part of Gunnedah Basin Bellata Group, contains Glossopteris and Gengamoptris (Cisuralian). Palynological Age of APP32 inferred from samples above and below this interval. No tuffs are present within this seam.|16-MAY-23
79333|Coxs Coal Member|Correlations|Probable equivalent to the Britton and Cintra Coal Members at Werris Ck, Halett Coal Member at Muswellbrook Anticline north and Grasstrees Coal Member Muswellbrook Anticline south, Teston seam at Maules Creek Sub-Basin.|16-MAY-23
79333|Coxs Coal Member|Alteration and Mineralisation|Coal - Bituminous in rank.|16-MAY-23
79333|Coxs Coal Member|Geophysical Expression|Possible seismic reflector, low downhole gamma (<50) and density (<1.50g/cc) response. Stone band 80cm above floor of seam can be used to correlate this seam in places.|16-MAY-23
79333|Coxs Coal Member|Defn author|Mark Dawson, 10-FEB-2016.|16-MAY-23
4846|Cranebrook Formation|Name source|Village of Cranebrook (GR 695346, Windsor 1:63 360).|16-MAY-23
4846|Cranebrook Formation|Unit history|First called Cranebrook Formation by Walker and Hawkins (1957). Described by Bell (1966) as " Undifferentiated Young Alluvium".|16-MAY-23
4846|Cranebrook Formation|Type section locality|Section 8.8 m thick consisting of coarse polymictic gravel (5 m thick) overlain by red-yellow medium grained sandy silt (3.8 m thick). Exposed in a gravel pit of Farley and Lewers Ltd, (GR 678355, Windsor 1:63 360).|16-MAY-23
4846|Cranebrook Formation|Extent|Outcrops over an area of approximately 25 km2 in the vicinity of Penrith adjacent to the Nepean River.|16-MAY-23
4846|Cranebrook Formation|Thickness range|Range 8-15 m.|16-MAY-23
4846|Cranebrook Formation|Lithology|Polymictic gravel, sand, silt and clay. Gravel clasts consist of relatively fresh porphyry, granite, quartzite, silcrete, chert, hornfels and sandstone. Occasional sand lenses occur within the gravel unit. Scattered pebbles occur throughout the overlying silt.|16-MAY-23
4846|Cranebrook Formation|Relationships and boundaries|Erosive into, and hence disconformably overlies the Wianamatta Group. Erosional upper surface.|16-MAY-23
4846|Cranebrook Formation|Age reasons|Pleistocene based on palynological evidence Morgan (1976). Diagnostic Spores identified were Nothofagidites emarcidus, (Cookson), Phyllocladidites Mawsonii Cookson, and Cingulatisporis bifurcatus (Couper).|16-MAY-23
4846|Cranebrook Formation|References|01/31632|16-MAY-23
24607|Cullen Bullen Subgroup|Name source|Town of Cullen Bullen, Western Coal Field|16-MAY-23
24607|Cullen Bullen Subgroup|Constituents|Comprises the Marrangaroo Conglomerate (at the base) and also includes the Lithgow Coal, Blackmans Flat Conglomerate and Lidsdale Coal where these units are developed. Commonly comprises only the Marrangaroo Conglomerate and Lithgow Coal.|16-MAY-23
24607|Cullen Bullen Subgroup|Type section locality|(1) Type section: From 21.53 m to 34.31 m. Thickness 12.78 m.  (2) Maximum recorded: 25.5 m.  Reference Section: Browns Gap, GR 158600, Hampton 8930-IV|16-MAY-23
24607|Cullen Bullen Subgroup|Extent|Western Coalfield-Lithgow and Bungleboori 1:50 000 sheets. Lithological equivalents of the Marrangaroo Conglomerate and Lithgow Coal are known from the Burragorang Valley almost to Ulan. Also occurs on parts of Hampton, Katoomba, Glen Davis and Glen Alice sheets.|16-MAY-23
24607|Cullen Bullen Subgroup|Relationships and boundaries|Within the Illawarra Coal Measures. Conformably underlies the Charbon Sub-Group; overlies the Nile Sub-Group of the Illawarra Coal Measures or the Berry Siltstone of the Shoalhaven Group.|16-MAY-23
24607|Cullen Bullen Subgroup|Proposed publication|Australian Coal Geology|16-MAY-23
24607|Cullen Bullen Subgroup|Proposer|Bembrick C.S., Robertson Research (Australia) Pty Limited|16-MAY-23
5030|Cunglebung Creek beds|Name source|Cunglebung Creek, GR 4800 1210 Mount Wellington 1:25 000 Topographic Sheet.|16-MAY-23
5030|Cunglebung Creek beds|Unit history|Previously I included these beds in the "Mann River sequence" (Fergusson, 1982).|16-MAY-23
5030|Cunglebung Creek beds|Type section locality|Representative section: Cunglebung Creek between GR 4665 1190 and GR 5115 1322 (Mount Wellington), monotonous exposure of silicified argillite.|16-MAY-23
5030|Cunglebung Creek beds|Extent|The unit is exposed over 200 km2 in an arcuate belt between the Mann and Nymboida rivers on the southeast portion of the Grafton 1:250 000 Sheet area (SH 56-6).|16-MAY-23
5030|Cunglebung Creek beds|Thickness range|The monotonous lithology and lack of structural control do not enable resolution of a true stratigraphic thickness.|16-MAY-23
5030|Cunglebung Creek beds|Lithology|Indurated massive and laminated argillite with rare chert and greywacke.|16-MAY-23
5030|Cunglebung Creek beds|Relationships and boundaries|Unconformably overlain to the southeast by the Mesozoic Clarence-Moreton Basin. To the northwest the unit is intruded by the Dandahra Creek Granite (Brunker et al., 1976). To the northeast the unit is in probable fault contact with the Gundahl Complex and to the southwest it is abruptly juxtaposed to the Coffs Harbour beds suggestive of a faulted contact. Both the Coffs Harbour beds and Gundahl Complex are distinguished from the unit by their abundance of greywackes.|16-MAY-23
5030|Cunglebung Creek beds|Age reasons|No fossils have been found. The unit is older than the Dandahra Creek Granite of probable Late Permian or Early Triassic age. Adjacent units are of probable Carboniferous age and this may also apply to the Cunglebung Creek beds.|16-MAY-23
5030|Cunglebung Creek beds|References|79/00646; |16-MAY-23
24235|Cupala Creek Formation|Name source|The formation is named after Cupala Creek, which runs southeastwards to Cootawundi Station (see Kayrunnera 1:100 000 orthophoto map 7436).|16-MAY-23
24235|Cupala Creek Formation|Unit history|Revision of old terms: The Cupala Creek Formation was formerly equated with rocks near Mt Daubney and Old Gnalta Homestead, reported to contain plant remains (Rose, 1974).|16-MAY-23
24235|Cupala Creek Formation|Type section locality|On a tributary of Cupala Creek from GR 6594E 5778N to GR 6589E 5769N.|16-MAY-23
24235|Cupala Creek Formation|Extent|About 4.5 km2 in the headwaters of Cupala Creek.|16-MAY-23
24235|Cupala Creek Formation|Thickness range|Type section 1020 m - the uppermost 190 m being unexposed. Conglomeratic unit approx. 90 m, lower red sandstone 170 m, pale-grey sandstone 235 m, upper red sandstone 125 m, olive-grey siltstone and fine sandstone 210 m, unexposed 190 m.|16-MAY-23
24235|Cupala Creek Formation|Lithology|The unit is grossly a fining-upward succession with a basal lithic, conglomeratic unit overlain by a lower red sandstone, then a pale-grey sandstone, an upper red sandstone and a fossiliferous olive-grey siltstone with very fine sandstone interbeds. The sandstones become texturally and chemically more mature upward. Sandstones from the middle part of the formation contain angular to rounded grains, and sorting ranges from poor to good. Seven sandstone samples point-counted cluster in the feldspathic-litharenite field of Folk (1974) with quartz comprising from 45% to 57% of framework grains. Plagioclase grains are present, and rock fragments are most commonly volcanogenic, with lesser amounts of sedimentary and tectonite grains. Much of the original porosity is infilled by quartz overgrowths, and some feldspar overgrowths are present. Carbonate and ferruginous cement also occur. There appears to be no petrological difference between the framework components of the red- and grey-coloured sandstone beds - the colour difference being caused by a ferruginous cement or coating on the grains in the red sandstone.|16-MAY-23
24235|Cupala Creek Formation|Relationships and boundaries|Overlies the Copper Mine Range Beds (Pogson and Scheibner, 1971) with marked angular unconformity, and is in turn overlain with moderate-angle unconformity by the quartzose sandstone and silt of the Mulga Downs Group.|16-MAY-23
24235|Cupala Creek Formation|Age reasons|Trilobites and brachiopods from the olive-grey fine sandstone and siltstone are Idamean (Late Cambrian). No fossils have been found in the underlying Copper Mine Range Beds, and Skolithos worm tubes are the only known fossils from the overlying Mulga Downs Group in this area, although elsewhere (near Cobar) basal Mulga Downs Group contains late Early to early Middle Devonian fish plates (Ritchie, 1973). The Kandie Tank Limestone, reported to contain Upper Cambrian to Tremadocian fossils (Warris, 1967, in Pogson and Scheibner, 1971), is probably considerably younger than the exposed Cupala Creek Formation. |16-MAY-23
24235|Cupala Creek Formation|References|79/03467; 79/03654; 79/03727; |16-MAY-23
24238|Curmulee Conglomerate|Name source|After Curmulee Creek, which drains the eastern side of the Minuma Range and joins the Deua River at GR 472297 Araluen 1:100 000 sheet.|16-MAY-23
24238|Curmulee Conglomerate|Unit history|The name Curmulee Conglomerate has not previously been used. Johnson (1964, unpublished M.Sc. Thesis, ANU) used the name "Grieg Creek Conglomerate" for this unit, however the name has previously been used in NSW and hence is unavailable for publication, the name Curmulee Conglomerate being introduced as a replacement.|16-MAY-23
24238|Curmulee Conglomerate|Type section locality|In a small, steep gully on eastern side of Minuma Range at GR 424258; all of the unit, here about 20 m thick, is exposed.|16-MAY-23
24238|Curmulee Conglomerate|Extent|Mainly on the western slopes of the Minuma Range.|16-MAY-23
24238|Curmulee Conglomerate|Thickness range|A maximum of 20 m at the type locality. About 10 m at its northernmost outcrop, where faulted out, at GR 398377. Thins southwards and is absent south of GR 412233.|16-MAY-23
24238|Curmulee Conglomerate|Lithology|Typically massive, reddish-brown, well rounded conglomerate with clasts normally <5 cm across. Minor pebbly arenite, coarse arenite and siltstone.|16-MAY-23
24238|Curmulee Conglomerate|Relationships and boundaries|Overlies conformably but abruptly the Long Swamp Creek Formation and is overlain conformably by Deua Formation, the contact being gradational over 2 to 5 m. The upper contact is taken at the top of the highest conglomerate or pebbly arenite bed.|16-MAY-23
24238|Curmulee Conglomerate|Age reasons|The unit is unfossiliferous. A Late Devonian age is suggested by its relationship with overlying Deua Formation.|16-MAY-23
38099|Currangandi Group|Name source|From Currangandi, elevation 882 m, (0243300E 6668370N, Eulowrie 8937-1-N, 1:25,000 sheet) a mountain mid-way between Rocky Creek and Boomi Creek, 12 km northwest of Upper Horton.|16-MAY-23
38099|Currangandi Group|Constituents|Rocky Creek region: Spion Kop Conglomerate, Ermelo Pyroclastics, Clifden Formation, Rocky Creek Conglomerate and Lark Hill Formation. Carroll-Nandewar block and tentatively the Clifton-Carroll block: Willuri Formation. Werrie Syncline: Currabubula Formation.|16-MAY-23
38099|Currangandi Group|Extent|Extends from the northern closure of the Rocky Creek Syncline east of Terry Hie Hie to the Waverley Fault north of Gundy. Main outcrops in the north are in the Rocky Creek Syncline, Kathrose and Darthula blocks; south of the Nandewar Range throughout the remainder of the Rocky Creek Syncline, Carroll-Nandewar and possibly Clifton-Carroll blocks; in the Werrie Syncline from the northern closure of the Currabubula Formation southwards to the Waverley Fault via the eastern limb of the syncline, Quirindi and Castle Mountain Domes and Kankool Anticline.|16-MAY-23
38099|Currangandi Group|Lithology|Continental, volcanogenic sandstone, conglomerate and siltstone with interbedded  ignimbrites, rare lavas and in some cases glacigene features including varved shales, dropped pebbles and tillite. The Spion Kop Conglomerate, which contains evidence of a glacial origin (White 1968), lacks interbedded ignimbrites and contains a greater proportion of metamorphic and igneous clasts than conglomerates in other constituent formations. The Ermelo Pyroclastics contain rare resedimented pebbles.|16-MAY-23
38099|Currangandi Group|Age reasons|Largely Namurian to Westphalian. A single rhyolite flow from the upper part of the Willuri Formation on Tulcumba Ridge has a SHRIMP AS3 age of between 297 and 287 Ma (?latest Carboniferous to Early Permian). The next youngest dated ignimbrite is 307.8+/-3.7 Ma old (Westphalian). The rhyolite appears to be in sequence with the Willuri Formation but, because of a possible hiatus between this and underlying units, could belong to the Early Permian Boggabri Volcanics. Resolution of conflicting SHRIMP SL13 and AS3 ages for the Kiaman Reversal (Opdyke et al. 2000; Roberts et al. in press; Figure 6) is required to clarify the age of the Clifden Formation, the oldest unit of the group containing ignimbrites. The age of the underlying Spion Kop Conglomerate is not determinable, but its glacigene origin (White 1968) may suggest a Namurian age.|16-MAY-23
27138|Currawang Basalt|Name source|Currawang village, GR 252679, Goulburn 1:250 000 sheet.|16-MAY-23
27138|Currawang Basalt|Type section locality|In a creek east of Currawang village, between GR 300253 (bottom) and GR 305253 (top) Goulburn 1:100 000 sheet.|16-MAY-23
27138|Currawang Basalt|Extent|The unit's extent is indicated on the Canberra and Goulburn 1:250 000 metallogenic maps (Gilligan, 1974; Felton, 1974a). On the Canberra metallogenic map, the unit is shown as B7L4 (basalt, pillow lavas and dolerite dykes) and on the Goulburn metallogenic map as B7L4 (undifferentiated spilite, amphibolite, quartzite, claystone). Only the outcrops in the area of Currawang village are included in the unit as defined here. It covers about 60 km2.|16-MAY-23
27138|Currawang Basalt|Thickness range|Variable; estimated maximum 1000 m.|16-MAY-23
27138|Currawang Basalt|Lithology|Pillowed basalt flows, basaltic and andesitic tuffs, minor keratophyre, chert.|16-MAY-23
27138|Currawang Basalt|Relationships and boundaries|The Currawang Basalt interfingers with and overlies the Woodlawn Volcanics, and is conformably overlain by the Covan Creek Formation. It is intruded by dolerite masses and dykes of unknown age.|16-MAY-23
27138|Currawang Basalt|Age reasons|On stratigraphic and structural grounds the unit is of Late Silurian age.|16-MAY-23
27138|Currawang Basalt|References|79/01437; 79/01733.|16-MAY-23
27385|Cymbric Vale Formation|Name source|"Cymbric Vale" property, northeastern Broken Hill 1:250 000 sheet area.|16-MAY-23
27385|Cymbric Vale Formation|Type section locality|Lower part 31o10.7'S 142o24.3'E (base) to 31o10.0'S 142o23.7'E. Middle part (partially or entirely overlaps top of previous part) 31o9.4'S 142o24.2'E to 31o9.4'S 142o23.9'E. Upper part (partially or entirely overlaps top of previous part ) 31o10.3'S 142o19.3'E.|16-MAY-23
27385|Cymbric Vale Formation|Extent|Northeastern Broken Hill 1:250 000 sheet area, on eastern side of valley drained by Mount Wright Creek; small area on western flank of syncline on western side of same valley.|16-MAY-23
27385|Cymbric Vale Formation|Thickness range|1500-1900 m.|16-MAY-23
27385|Cymbric Vale Formation|Lithology|Interbedded blue, green and grey-white cherts and green and brown tuffs. Lithic and feldspathic sandstones and impure iron rich carbonates in uppermost parts.|16-MAY-23
27385|Cymbric Vale Formation|Relationships and boundaries|Faulted contact with underlying Mount Wright Volcanics. Irregular, apparently conformable relationship with overlying Coonigan Formation, as seen in upper part of composite type section.|16-MAY-23
27385|Cymbric Vale Formation|Age reasons|Early Cambrian (later Atdabanian to early Lenian), as indicated by archaeocyaths at localities L98-L101 and trilobites in uppermost levels of unit (Opik 1976).|16-MAY-23
27385|Cymbric Vale Formation|Proposed publication|Palaeontographica A177 p.129-212|16-MAY-23
5150|Dalmally Basalt Member|Name source|After Dalmally Homestead, near where Copes Creek flows into the Nymboida River.|16-MAY-23
5150|Dalmally Basalt Member|Type section locality|The basalt is about 15 m thick outside the meander bend on the true right bank of Copes Creek ("Nymboida" 1:63,360 military map, GR 808877).|16-MAY-23
5150|Dalmally Basalt Member|Description at type locality|McElroy (1963, pp.49, 59) has described the outcrop, petrography and chemistry of this unit. The CIPW norm calculated from McElroy's analysis indicates a sub-alkaline (non-alkaline) basaltic composition. Several specimens illustrating the textural variation in this rock have been placed in the collections of the Geology Department, University of New England (UNER 34382, 35367-35370).|16-MAY-23
5150|Dalmally Basalt Member|Relationships and boundaries|Bardool Conglomerate of the Nymboida Coal Measures, underlying the far southwestern Moreton Basin (McElroy, 1963).|16-MAY-23
5150|Dalmally Basalt Member|Age reasons|Why the Dalmally Basalt Member is a Triassic Flow: The elongate outcrop of the basalt is concordant with the strike of the surrounding Triassic sedimentary rocks and completely within the outcrop of the Bardool Conglomerate. The dip of the bench-forming top of the basalt is also the same as the dip of overlying conglomerate, sandstone and tuff. Concordance is also supported by the outcrop pattern of vertical texture variation in the basalt at the type locality. The basalt has a glassy, block-jointed base, and a more massive central portion containing feldspar phenocrysts. Amygdales and vesicles increase in abundance and size towards the top of the flow. The vesicles are up to 3 cm in diameter and may be partly or completely filled with calcite, zeolites and quartz. Some rounded basalt floaters found on the hillside above the top of the basalt are very strongly vesicular and resemble basaltic scoria. In the creek bank exposure at "Nymboida" grid. ref. 808873, coarsely vesicular basalt with lenticular flow structure appears to cut a shallow channel into the underlying well-jointed basalt. The Cope's Creek Tuff, only 15 to 30 m above Dalmally Basalt Member, is evidence of associated Triassic pyroclastic activity in this area. The Dalmally Basalt Member is chemically more similar to some Triassic basalts in south-eastern Queensland than to subalkaline Tertiary basalts in northeastern New South Wales (McElroy, 1963, p.63; Wilkinson, pers. comm).   Geological age: Homotaxial megafossil floras found both stratigraphically above and below the Dalmally Basalt Member indicate that it is Late Anisian to Ladinian in age.  Isotopic age:  Unweathered plagioclase from near the base of the basalt yielded a 40K/40Ar isotopic age of 211 +/- 5 million years.  Isotopic Age: Unweathered plagiaoclase from near the base of the basalt yielded a 40K/40Ar isotopic age of 211 +/- 5 million years.|16-MAY-23
5150|Dalmally Basalt Member|Proposed publication|Proc. Linn. Soc. NSW 101, pp.79-80.|16-MAY-23
5150|Dalmally Basalt Member|References|97/28843|16-MAY-23
25714|Dangarfield Formation|Name source|Named after the Settlement of Dangarfield, 996244 Aberdeen 1:31,680.|16-MAY-23
25714|Dangarfield Formation|Unit history|Incorporates the Bushy Hill Limestone as a Member.|16-MAY-23
25714|Dangarfield Formation|Type section locality|Glenbawn area, particularly east of Lake Glenbawn. Location of Type Section: Measured from a short distance downstream from Glenbawn Dam (998280 Scone 1:31 680 Sheet), eastwards to the contact with the overlying Isismurra Formation located just below the top of Trig. 2290 (030289, Woolooma 1:63 360 Sheet).|16-MAY-23
25714|Dangarfield Formation|Extent|Outcrops over an area of about 70 km2 on the eastern and western flanks of the Brushy Hill anticline (Brushy Hill), between Rouchel Springs in the south and the Pages River in the north.|16-MAY-23
25714|Dangarfield Formation|Thickness range|a) At type section: 511 m.  B) Maximum known: 511 m.|16-MAY-23
25714|Dangarfield Formation|Lithology|Mudstone with subordinate medium to thickly-bedded green lithic sandstone, and oolitic and  crinoidal limestone. The Brushy Hill Limestone, previously named by Osborne (1950) is a member in the lower part of the formation.|16-MAY-23
25714|Dangarfield Formation|Fossils|Brachiopods, corals, bivalves, polyzoans, crinoids, conodonts, ammonoids.|16-MAY-23
25714|Dangarfield Formation|Relationships and boundaries|Lower boundary - see Kingsfield Beds. The Dangarfield Formation is overlain by the Isismurra Formation (Manser, 1968, Wingen 1:100 000 sheet, University of New England Map Series). In the type section, the boundary is taken at the transition from brown lithic sandstones to pink cross-bedded lithic sandstones; the pink sandstone is lithologically typical of the Isismurra Formation, and is succeeded by the Ayr Conglomerate Member. Elsewhere, the Dangarfield Formation is overlain by Ayr Conglomerate.|16-MAY-23
25714|Dangarfield Formation|Age reasons|Lower Carboniferous (early Tournaisian to early Visean). Contains brachiopods of the Spirifer sol, Schellwienella cf. Burlingtonensis and Pustula gracilis Zones.|16-MAY-23
25714|Dangarfield Formation|Defn approved by|Approved. Copied from xerox sent by NSW Stratigaraphic Nomenclature Sub-Committee.|16-MAY-23
25714|Dangarfield Formation|Reserved? Yes/No|Roberts J., Oversby B.S.|16-MAY-23
24240|Danswell Creek Granodiorite|Name source|After Danswell Creek which lies close to the granodiorite's western margin at GR 108334, Michelago 1:100 000 Geological Sheet.|16-MAY-23
24240|Danswell Creek Granodiorite|Unit history|The granodiorite was previously included under the name Sapling Flat Granite (Joplin et al. 1953). Richards (1967) introduced the name Limekiln Granodiorite (invalid).|16-MAY-23
24240|Danswell Creek Granodiorite|Type section locality|The granodiorite is well represented at GR 118334.|16-MAY-23
24240|Danswell Creek Granodiorite|Description at type locality|Coarse-grained hypidiomorphic granular texture, becoming finer grained to porphyritic along the margins. It typically consists of bluish quartz crystals, pink K-feldspar, plagioclase, and clusters of medium-grained biotite and hornblende. Xenoliths of ?sedimentary origin are most common towards the margin of the granodiorite.|16-MAY-23
24240|Danswell Creek Granodiorite|Extent|The granodiorite constitutes the northern part of the Sapling Flat Igneous Complex and lies to the northwest of Jerangle.  Size: 8 km2.|16-MAY-23
24240|Danswell Creek Granodiorite|Relationships and boundaries|The Danswell Creek Granodiorite is the minor phase of the Sapling Flat Igneous Complex; it intrudes Late Ordovician metasediments (Foxlow Beds) and is bounded on its eastern side by the Narongo Fault and the Kohinoor Volcanics of Late Silurian age. Contact metamorphism leading to the development of andalusite has taken place adjacent to the granodiorite.|16-MAY-23
24240|Danswell Creek Granodiorite|Age reasons|K-Ar age dating by AMDEL give an age of 356 +/- 7 m.y. (Biotite) and 353 +/- 7 m.y. (Hornblende). However, as the specimens were collected in proximity to the Narongo Fault it is more likely that the granodiorite has a greater age I.e. intruded at the close of the Silurian Period-beginning of Devonian Period.|16-MAY-23
24240|Danswell Creek Granodiorite|Proposed publication|Geological Survey of NSW 1:100 000 Note Series.|16-MAY-23
37914|Darthula Rhyodacite Member|Name source|Named after the property `Darthula', GR286583 Coryah 1:25,000 sheet.|16-MAY-23
37914|Darthula Rhyodacite Member|Unit history|Darthula Rhyodacite (Opdyke et al. 2000). Originally informally named by Hocking (1973).|16-MAY-23
37914|Darthula Rhyodacite Member|Geomorphic expression|Ridge-forming.|16-MAY-23
37914|Darthula Rhyodacite Member|Type section locality|Within an unnamed tributary of Pound Creek between GR286566 and 287562 Coryah 1:25,000 sheet.|16-MAY-23
37914|Darthula Rhyodacite Member|Extent|Outcrops are restricted to low hills 2 km south of Darthula.|16-MAY-23
37914|Darthula Rhyodacite Member|Thickness range|50 m|16-MAY-23
37914|Darthula Rhyodacite Member|Lithology|Purple, moderately welded ignimbrite having large  (up to 5 mm) embayed quartz, feldspar, minor opaque minerals, volcanic rock fragments and pumice fiamme (up to 12 mm); the groundmass is micropoikilitic.|16-MAY-23
37914|Darthula Rhyodacite Member|Depositional environment|Ignimbrite.|16-MAY-23
37914|Darthula Rhyodacite Member|Relationships and boundaries|Underlain by two unnamed ignimbrites within the upper part of the Rocky Creek Conglomerate.|16-MAY-23
37914|Darthula Rhyodacite Member|Age reasons|Carboniferous (Namurian).|16-MAY-23
37914|Darthula Rhyodacite Member|References|HOCKING R.M. 1973. The Carboniferous Back Creek-Pound Creek sequence, southwest of Caroda, New South Wales. BSc (Hons) thesis, University of new England, Armidale (unpubl.).OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
5292|De Drack Formation|Name source|De Drack trig. Station, GR 363997 Braidwood 1:100 000 sheet.|16-MAY-23
5292|De Drack Formation|Unit history|The term De Drack Formation was used by Huleatt (1971) when briefly describing a sequence of shale, tuffaceous and calcareous shale, arenite, tuffaceous arenite, chert and limestone in the Braidwood district. Large areas in the northeast of the Canberra 1:150 000 metallogenic map (Gilligan, 1974) and the southeast of the Goulburn 1:250 000 metallogenic map (Felton, 1974a) are shown as De Drack Formation (B7L2). The term is here defined as above.|16-MAY-23
5292|De Drack Formation|Constituents|Sandhills Creek Limestone Member (Felton and Huleatt, 1975).|16-MAY-23
5292|De Drack Formation|Type section locality|In Fairy Meadow Creek between GR 373027 and GR 369029, Braidwood 1:100 000 sheet.|16-MAY-23
5292|De Drack Formation|Extent|The unit crops out in two belts: in the vicinity of Boro mine (GR 441091) and Mayfield (GR 541008), and between Lake Bathurst town (GR 417217) and "Bengwen" property (GR 353915). All grid references refer to the Braidwood 1:100 000 sheet. Total area of outcrop of the unit is about 150 km2.|16-MAY-23
5292|De Drack Formation|Thickness range|Estimated minimum 300 m.|16-MAY-23
5292|De Drack Formation|Lithology|Mainly tuffaceous siltstone and shale; also minor shale, silttone, tuffaceous arenite, quartzite, limestone, dolomite and conglomerate.|16-MAY-23
5292|De Drack Formation|Relationships and boundaries|The De Drack Formation unconformably overlies the Birkenburn Beds and undifferentiated Ordovician metasediments. It interfingers with and is overlain by the Woodlawn Volcanics. It is overlain, probably disconformably, by the Covan Creek Formation and unconformably overlain by the Tarago Conglomerate. It is faulted against the Birkenburn Beds and probably also against undifferentiated Ordovician metasediments. Its relationship with the Long Flat Volcanics is obscure. It is intruded by the Boro Granite. The base of the De Drack Formation is marked in places by a chert-rich conglomerate-arenite unit whose thickness does not exceed 5 m. Elsewhere the base of the unit is faulted against Ordovician rocks.|16-MAY-23
5292|De Drack Formation|Age reasons|Strusz and Nicoll (1973) have identified Monograptus bohemicus from the De Drack Formation, indicating a Late Silurian age.|16-MAY-23
5292|De Drack Formation|Proposed publication|Felton E.A., Huleatt M.B., 1975. Geology of the Braidwood 1:100 000 Sheet. Geological Survey NSW, Sydney.|16-MAY-23
5292|De Drack Formation|References|79/01437; 79/01436; 73/015.|16-MAY-23
5292|De Drack Formation|Status|1|16-MAY-23
69824|Delungra Volcanic Suite|Name source|After the township of Delungra (BINGARA 1:100 000 map sheet area).|16-MAY-23
69824|Delungra Volcanic Suite|Constituents|Four formations constitute the Delungra Volcanic Suite. These are the Mount Russell Volcanics, Derra Derra Volcanics, the Inverell Volcnaics and the Bingara Volcanics.|16-MAY-23
69824|Delungra Volcanic Suite|Extent|This suite is widespread and extends from Copeton Dam and Inverell in the south and east, respectively, west to Gravesend and north to North Star to have dimensions of approximately 150km north-south by 100km east-west.|16-MAY-23
69824|Delungra Volcanic Suite|Lithology|Lithologies include mafic flows, intrusikons and volcaniclastic rocks of tholeiitic and alkaline composition.|16-MAY-23
69824|Delungra Volcanic Suite|Age reasons|Published K-Ar ages extend from Late Oligocene (24Ma) to Early Miocene (19Ma).|16-MAY-23
69826|Derra Derra Volcanics|Name source|After the Parish of Derra Derra (BINGARA and GRAVESND 1:100 000 map sheet areas).|16-MAY-23
69826|Derra Derra Volcanics|Type section locality|A north to south section from above the basal Palaeogene gravels at the Monte Christo mine (GR 257250mE 6690690mN, MGA94 Zone 56) to the top of a hill to the south-southeast (GR 258660mE 6688900mN, MGA94 zone 56) is proposed. This is a vertical section up the hill to the south of the Monte Christo mine.|16-MAY-23
69826|Derra Derra Volcanics|Extent|This unit forms part of the Central Province of McDougall and Wilkinson (1967) and occurs 5km to 20 km west and southwest of Bingara.|16-MAY-23
69826|Derra Derra Volcanics|Thickness range|In the type section, the Derra Derra Volcanics is estimated to have a cumulative thickness of 80m. a maximum thickness is reached further to the west where the Derra Derra Volcanics attains a thickenss of 150m.|16-MAY-23
69826|Derra Derra Volcanics|Lithology|The main rock types of the Derra Derra Volcanics are tholeiitic basalts with minor volcaniclastic rocks and diamond-bearing gravels.|16-MAY-23
69826|Derra Derra Volcanics|Depositional environment|A series of mafic lave flows up to 20m thick with interbedded diamond-bearing fluvial sedimnets in a lacustrine environment.|16-MAY-23
69826|Derra Derra Volcanics|Relationships and boundaries|The Derra Derra Volcanics unconformably overlies the Devonian to Carboniferous Parry Group of the Tamworth Belt, southern New England Orogen. It unconformably overlies Palaeogene gravels and interfingers with the Bingara Volcanics.|16-MAY-23
69826|Derra Derra Volcanics|Age reasons|One sample yielded a K-Ar age of 23 Ma (Early Miocene). Other unpublished ages are 28 Ma (Late Oligocene).|16-MAY-23
5426|Deua Formation|Name source|Deua Trig. GR 424257, Araluen 1:100 000 Sheet.|16-MAY-23
5426|Deua Formation|Unit history|The name was first used in Johnson's (1964) unpublished M.Sc thesis, from ANU. It was mentioned by McIlveen (1975, Rec. geol. Survey NSW 16(3), p.268) but was not defined.|16-MAY-23
5426|Deua Formation|Type section locality|Along a tributary creek and the Shoalhaven River from GR 403290 (base) to 393280 (top). Good but not continuous exposure through about 350 m of the unit.|16-MAY-23
5426|Deua Formation|Extent|Extensive along the Minuma Range from Wyanbene south to the southern edge of the Araluen sheet. A small area occurs in the north of Cobargo 1:100 000 sheet.|16-MAY-23
5426|Deua Formation|Thickness range|Generally 300 to 350 m, but thins to 200 m in south.|16-MAY-23
5426|Deua Formation|Lithology|Typically reddish-purple to reddish brown, medium to fine grained lithic quartzo-feldspathic arenite with minor shale. Arenite is generally well-bedded, in units 10 to 50 cm thick, and often contains shale "rip-up" clasts. Cross-bedding is common.|16-MAY-23
5426|Deua Formation|Relationships and boundaries|Rests conformably on the Curmulee Conglomerate, or where the Conglomerate is absent, on the Long Swamp Creek Formation; in both cases the contact is gradational over several metres. The Deua Formation is overlain conformably by the Khan Yunis Formation, again with a gradational contact. The top of the Deua Formation is placed at the base of the first coarse arenite or pebbly arenite in the sequence.|16-MAY-23
5426|Deua Formation|Age reasons|Poorly preserved brachiopods and bivalves are known from four localities. They indicate a Late Devonian age.|16-MAY-23
5426|Deua Formation|Reserved? Yes/No|Yes|16-MAY-23
29267|Dinoga Formation|Name source|The name is derived from a peak named Dinoga (Dinoga 1:25 000 topographic map sheet 9038-111-S grid reference 704796) near where the unit is well exposed.|16-MAY-23
29267|Dinoga Formation|Unit history|Spring Ridge Formation (informal thesis name of Rodgers 1986).|16-MAY-23
29267|Dinoga Formation|Type section locality|Stratotype: Type area is nominated as the small hill on the west side of Spring Creek (Bingara 1:100 000 topographic map sheet 9038 GR 675900).|16-MAY-23
29267|Dinoga Formation|Extent|Discontinuous lenses of Dinoga Formation have been traced from Bingara to east of Barraba.|16-MAY-23
29267|Dinoga Formation|Thickness range|Unknown|16-MAY-23
29267|Dinoga Formation|Lithology|Volcaniclastic sandstones, argillite sand conglomerates which contain blocks of coralline limestone of Devonian age. Metamorphism: Burial grade only.|16-MAY-23
29267|Dinoga Formation|Relationships and boundaries|Structurally overlies Woodsreef Ophiolitic Melange.|16-MAY-23
29267|Dinoga Formation|Age reasons|Younger than the Early to Middle Devonian limestone blocks in Dinoga Formation conglomerates.|16-MAY-23
29267|Dinoga Formation|Category|2|16-MAY-23
29267|Dinoga Formation|Defn approved by|NSW Stratigraphic Nomenclature Sub-Committee|16-MAY-23
24250|Donovan Basic Complex|Name source|Mount Donovan, GR 608281, on which the complex is centred.|16-MAY-23
24250|Donovan Basic Complex|Type section locality|No type locality is given as the complex is zoned from bottom to top. Representative rock types are best examined on the ridge between the top of Mount Donovan and the saddle at GR 603282.|16-MAY-23
24250|Donovan Basic Complex|Extent|A roughly circular stock of about 2.3 km2 centred on Mount Donovan (GR 608281).|16-MAY-23
24250|Donovan Basic Complex|Lithology|The body is compositionally zoned from bottom to top ranging from fine grained two pyroxene gabbro at the bottom through two pyroxene magnetite gabbro, quartz gabbro quartz monzogabbro to pyroxene granophyre of granodiorite composition at the top. At GR 606281 the pyroxene granophyre is intruded by a 2 m thick leucocratic granophyre dyke.|16-MAY-23
24250|Donovan Basic Complex|Age reasons|A Rb/Sr whole rock isochron gives an age of 355 +/- 13 Ma and initial ratio of 0.7066 +/- 0.0008. The date is in accord with the Complex being part of the Mid to Late Devonian Comerong Rift Zone magmatism.|16-MAY-23
24250|Donovan Basic Complex|Resdate|21-JUN-1982|16-MAY-23
24250|Donovan Basic Complex|Reserved? Yes/No|Yes|16-MAY-23
24252|Dooralong Shale|Name source|"Dooralong" township, GR 360985 Morisset 1:63 360 sheet.|16-MAY-23
24252|Dooralong Shale|Type section locality|DM Dooralong DDHI, GR 355979 Morisset 1:63 360 sheet, from depths 334.80 m to 371.39 m. Fully cored section is stored at NSW Mines Department core library at Londonderry, NSW.|16-MAY-23
24252|Dooralong Shale|Extent|Poor outcrop in Lake Macquarie area, intersected in boreholes in the Gosford-Lake Macquarie area, to Windeyers Hawkesbury River Bore in the south, and to MIH St Albans DDHI in the west.|16-MAY-23
24252|Dooralong Shale|Thickness range|From 8 m thick in Lake Macquarie area, to maximum of 201 m thick in Longley DDH at Somersby.|16-MAY-23
24252|Dooralong Shale|Lithology|Interbedded grey to grey-green siltstone and claystone, and white to light grey fine and medium sandstone.|16-MAY-23
24252|Dooralong Shale|Relationships and boundaries|Unconformably overlies Newcastle Coal Measures, laterally equivalent in part to and overlain by Munmorah Conglomerate, Clifton Sub-Group, Narrabeen Group.|16-MAY-23
24252|Dooralong Shale|Age reasons|Possibly late Late Permian, characterised by Protohaploxypinus reticulatis microfloral assemblage zone, of Helby (1973), Morgan (1976, 1977).|16-MAY-23
24252|Dooralong Shale|Proposed publication|The Geology of the Gosford and Lake Macquarie 1:100 000 sheets.|16-MAY-23
24252|Dooralong Shale|References|96/28292.|16-MAY-23
37910|Downs Rhyodacite Member|Name source|Named after the property `The Downs' GR284662 Grattai 1:25,000 sheet.|16-MAY-23
37910|Downs Rhyodacite Member|Unit history|Downs Rhyodacite (Opdyke et al. 2000)|16-MAY-23
37910|Downs Rhyodacite Member|Type section locality|On a ridge crest at GR303621 Coryah 1:25,000 sheet, 4 km southeast of `Locheil Downs'.|16-MAY-23
37910|Downs Rhyodacite Member|Extent|On the western limb and closure of the Berrygil Anticline, and on the faulted eastern limb of the same structure, 4 km southeast of Lochiel Downs (formerly Panpanboolala) homestead  at GR281651 Grattai 1:25,000 sheet.|16-MAY-23
37910|Downs Rhyodacite Member|Thickness range|5 m|16-MAY-23
37910|Downs Rhyodacite Member|Lithology|Unwelded red ignimbrite with quartz, feldspar and pumice fragments. The groundmass is vitric and contains shards and bubble walls.|16-MAY-23
37910|Downs Rhyodacite Member|Depositional environment|Ignimbrite.|16-MAY-23
37910|Downs Rhyodacite Member|Relationships and boundaries|70 m from the top of the Clifden Formation in the Darthula block.|16-MAY-23
37910|Downs Rhyodacite Member|Age reasons|Carboniferous (Namurian).|16-MAY-23
37910|Downs Rhyodacite Member|Comments|Named informally by Hocking (1973). Restricted to the Darthula block.|16-MAY-23
37910|Downs Rhyodacite Member|References|HOCKING R.M. 1973. The Carboniferous Back Creek-Pound Creek sequence, southwest of Caroda, New South Wales. BSc (Hons) thesis, University of new England, Armidale (unpubl.).OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
24931|Drysdale Conglomerate Member|Name source|Mount Drysdale, GR 385142 Cobar 1:250 000 sheet. (SH55-14).|16-MAY-23
24931|Drysdale Conglomerate Member|Unit history|Andrews (1913) referred to the conglomerates as the Drysdale Conglomerates (page vi) and Mount Drysdale Conglomerates (page 42). Longman and Meares (1972) included these beds in their Mt Drysdale Conglomerate.|16-MAY-23
24931|Drysdale Conglomerate Member|Type section locality|No type section of this member has been measured due to the deformation in the member. A good section through part of the member crops out on NW/SE trending spurs near Mount Drysdale trigonometrical station. The base of the member is near the foot of the spurs on the western side of the Mount Drysdale range but the boundary itself is not exposed. The top of the member can be observed in outcrops just east of Cougar trig. station.|16-MAY-23
24931|Drysdale Conglomerate Member|Extent|The Member is exposed in a series of isolated outcrops on ridges between Cougar (GR 385131) and Mooka (GR 383160) Trigonometrical Stations in the northwest part of the Cobar 1:250 000 sheet.|16-MAY-23
24931|Drysdale Conglomerate Member|Thickness range|No measurement of the thickness has been made but a maximum of 300-400 m seems likely.|16-MAY-23
24931|Drysdale Conglomerate Member|Lithology|Conglomerate, pebbly sandstone, sandstone and sandstone with minor siltstone and claystone. The pebbles and cobbles in the conglomerate are mainly quartzite, chert, sandstone and vein quartz with minor siltstone and claystone.|16-MAY-23
24931|Drysdale Conglomerate Member|Relationships and boundaries|The member unconformably overlies the Ballast Beds. A basal conglomerate is normally present. The member is overlain by and laterally equivalent to undifferentiated Chesney Formation. This boundary is marked by a gradational decrease in grain size of the sediments.|16-MAY-23
24931|Drysdale Conglomerate Member|Age reasons|Fossils from one locality near Mooka Trig. Station (GR 3822 1590) included Molongia capricornae McKellar and Howellella sp. Sherwin (1974b). This suggests a Late Silurian to Early Devonian age. This is in agreement with the age suggested from fossils found elsewhere in the Cobar Group. Sherwin (1974a).|16-MAY-23
24931|Drysdale Conglomerate Member|Proposed publication|Quarterly Notes of the Geological Survey of New South Wales|16-MAY-23
24931|Drysdale Conglomerate Member|References|GOLD0014;|16-MAY-23
5806|Dunchurch Formation|Name source|Dunchurch property, Burraga 1:31 680|16-MAY-23
5806|Dunchurch Formation|Unit history|Name first proposed by D. Dunnett and I. Gemuts in unpublished BSc Hons. Thesis for Sydney University in 1961.|16-MAY-23
5806|Dunchurch Formation|Type section locality|Thompsons Creek, Burraga. Location of Type Section: Not known|16-MAY-23
5806|Dunchurch Formation|Extent|Barraga area.|16-MAY-23
5806|Dunchurch Formation|Thickness range|Not known|16-MAY-23
5806|Dunchurch Formation|Lithology|Grey-green felspathic greywacke with partings of slate and chert common.|16-MAY-23
5806|Dunchurch Formation|Fossils|Poorly preserved crinoids and brochropads.|16-MAY-23
5806|Dunchurch Formation|Relationships and boundaries|Base - undefined, Top-base of thick grey-green slates.|16-MAY-23
5806|Dunchurch Formation|Age reasons|Silurian-stratigraphic position.|16-MAY-23
5806|Dunchurch Formation|Proposed publication|The Geology of the Burraga Copper Mine. Records of the Geological Survey of NSW|16-MAY-23
5806|Dunchurch Formation|Defn approved by|Approved - copied from xerox sent by NSW Stratigraphic Nomenclature Sub-Committee|16-MAY-23
5806|Dunchurch Formation|Name first published by|Scheibner E., 1970|16-MAY-23
5806|Dunchurch Formation|Proposer|Bowman H.N. (after I. Gemuts)|16-MAY-23
24937|Dundurrabin Granodiorite|Name source|Village of Dundurrabin GR 5622 2605 (Dorrigo 1:250 000).|16-MAY-23
24937|Dundurrabin Granodiorite|Unit history|Named by Binns and others (1967) and Leitch et al (1971) but not defined.|16-MAY-23
24937|Dundurrabin Granodiorite|Type section locality|Road cuttings on the Grafton to Ebor road just to the east of Dundurrabin, and outcrops in the Blicks River, where the road cuts the river. GR 5622 2603 Dorrigo 1:250 000.|16-MAY-23
24937|Dundurrabin Granodiorite|Extent|A west-north-west trending body of about 45 km2 occurring 10 km northwest of Dorrigo.|16-MAY-23
24937|Dundurrabin Granodiorite|Lithology|Predominantly coarse- to medium-grained granodiorite and adamellite which is frequently porphyritic in K-feldspar. Rare dioritic phases. Xenoliths are abundant in the coarse granodiorite and adamellite phases.|16-MAY-23
24937|Dundurrabin Granodiorite|Relationships and boundaries|Intruded into the Moombil Beds and Brooklana Beds producing biotite-cordierite hornfels adjacent to the contacts.|16-MAY-23
24937|Dundurrabin Granodiorite|Age reasons|Unknown but intrudes the Moombil Beds and Brooklana Beds, both of which are postulated to be Late Palaeozoic.|16-MAY-23
24256|Dungay Group|Identifying features|The group consists of the Kullatine Formation, Majors Creek Formation and Boonanghi beds. The name is taken from Dungay Creek which drains a large portion of the northern part of the Parrabel Anticline. It is a tributary of the Mackay River at 31o07'S, 152o35'E, west of Kempsey. There are excellent exposures in the creek and in cuttings on the road beside the creek. The base of the Boonanghi beds is not exposed. According to Northcott (1973), in an unpublished thesis (in the University of New England library), the top of Kullatine Formation is an erosion surface which he called the Sebastopol Disconformity. That name has been used by Korsch and Harrington (1981) in their Figure 5 (Column 7) and their page 215 (Column 1). The Yessabah Limestone is above the disconformity and is of Early Permian age. The Dungay Group is thought to be entirely Late Carboniferous, but the Boonanghi beds might be older. The Majors Creek and Kullatine formations both contain Levipustula levis which is Late Carboniferous. The group makes up most of the sequence in the Parrabel Anticline as shown on the 1:500 000 and 1:250 000 geological maps published by the NSW Geological Survey.|16-MAY-23
24256|Dungay Group|Proposed publication|Was named informally by R.J. Korsch and H.J. Harrington in a paper entitled "Stratigraphic and structural synthesis of the New England Orogen", J. Geol. Soc. Aust., Vol. 28, page 215 column 1, 1981.|16-MAY-23
24256|Dungay Group|First Reference|81/21750|16-MAY-23
24256|Dungay Group|Proposer|Harrington H.J., Korsch R.J.|16-MAY-23
24258|Dunhill Bluff Limestone Member|Unit history|The Dunhill Bluff Limestone Member was known previously as the 'mixed fauna' unit (Webby 1969).|16-MAY-23
24258|Dunhill Bluff Limestone Member|Type section locality|Type section on Dunhill Bluff (GR 753814*) (*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978).|16-MAY-23
24258|Dunhill Bluff Limestone Member|Description at type locality|Above the gradational contact with the underlying Taplow Limestone Member, the sequence is thin-bedded, and comprises some 6 m of grey skeletal wackestones with thin shale partings. A small fault in the type section disrupts the top of this sequence but is unlikely to be responsible for loss of more than 1 m of beds.  The 12 m thick succession above the fault exhibits marked colour change from grey to orange-brown, and increase in calcareous siltstone content. The beds are thin bedded alternating skeletal packstones, wackestones and calcareous siltstones with a varied shelly fauna. The succeeding 4 m of sequence contains a small bioherm and a varied coral and stromatoporoid fauna. The remaining, uppermost 4.5 m of the Dunhill Bluff Limestone Member comprises alternating thin bedded 'platy' skeletal wackestones with shally partings and thicker trilobite-rich packstones. The thinner bedded skeletal wackestones at the top are in relatively sharp contact with overlying, massive bedded lime mudstones and fine grainstones of basal Transmission Limestone Member.|16-MAY-23
24258|Dunhill Bluff Limestone Member|General description|Like the other subdivisions of the Fossill Hill Limestone, the Dunhill Bluff Limestone Member has been mapped as a continuous thin-bedded unit with rich and varied faunal and floral associations.|16-MAY-23
24258|Dunhill Bluff Limestone Member|Thickness range|24.5 m thick in type section.|16-MAY-23
24258|Dunhill Bluff Limestone Member|Proposed publication|Stratigraphy of the Cliefden Caves Limestone Group (Upper Ordovician) central NSW. J. geol. Soc. Aust.|16-MAY-23
24258|Dunhill Bluff Limestone Member|Proposer|Webby B.D., Packham G.H.|16-MAY-23
39340|Edithvale Formation|Name source|Edithvale homestead, 10km ESE of Weethalle.|16-MAY-23
39340|Edithvale Formation|Unit history|Synomyn: Part of the Cocoparra Group.|16-MAY-23
39340|Edithvale Formation|Constituents|None.|16-MAY-23
39340|Edithvale Formation|Geomorphic expression|Forms low ridges.|16-MAY-23
39340|Edithvale Formation|Type section locality|In low-lying hills, west of Weja Rd between Edithvale HS and Mountain View HS between AMG473790,6247566 and 474305,6246279.|16-MAY-23
39340|Edithvale Formation|Description at type locality|Medium-thick bedded, poorly sorted pebbly sandstone with minor thick beds of pebble-cobble polymictic conglomerate.|16-MAY-23
39340|Edithvale Formation|Extent|In core of Narriah Syncline.|16-MAY-23
39340|Edithvale Formation|Thickness range|>200m.   The top of the unit isn't exposed so thickness can't be accurately estimated.|16-MAY-23
39340|Edithvale Formation|Lithology|Medium-thick bedded, poorly sorted pebbly sandstone with minor thick beds of pebble-cobble polymictic conglomerate. Pebbles of vein quartz, quartzite, siltstone, chert and ?volcanics often show imbrication.|16-MAY-23
39340|Edithvale Formation|Depositional environment|High energy braided fluvial system.|16-MAY-23
39340|Edithvale Formation|Fossils|None found.|16-MAY-23
39340|Edithvale Formation|Relationships and boundaries|Conformably overlies the Hazeldene Sandstone (nov.). No overlying units, as it forms the core of a syncline.|16-MAY-23
39340|Edithvale Formation|Age reasons|Late Devonian, based on similarity with better-dated sequences elsewhere in NSW.|16-MAY-23
39340|Edithvale Formation|Correlations|Possibly Rankin Formation (Mailman Gap Member?).|16-MAY-23
39340|Edithvale Formation|Proposed publication|Explanatory Notes to accompany the Cargelligo 1:250 000 geological sheet|16-MAY-23
39340|Edithvale Formation|Comments|Has a moderate and speckled U,Th,K radiometric response. The magnetic response is slightly elevated near its base.|16-MAY-23
24260|Ednas Gneiss|Name source|Taken from Ednas Tank (GR 6000 4040 Redan 1:25 000 sheet).|16-MAY-23
24260|Ednas Gneiss|Unit history|Incorporated in undifferentiated Thackaringa Group by Willis et al. (1983). Part of "Redan gneiss" of Rayner (1949) and part of "Redan rock unit association" of Corbett (1981).|16-MAY-23
24260|Ednas Gneiss|Type section locality|No continuous section is available, but an incomplete type section is nominated between GR 550362 (near base) and GR 568405 (top) (Redan 1:25 000 sheet). Reference sections are nominated between GR 635358 and GR 660362 (Redan 1:25 000 sheet) and between GR 731435 and GR 725443 (Kinalung 1:25 000 sheet).|16-MAY-23
24260|Ednas Gneiss|Description at type locality|Ednas Gneiss consists mostly of albite rich rock types. The most distinctive type is an albite-quartz-magnetite rock or gneiss. This rock exhibits layering on a scale of several cm to several 10's of cm. The layering is mainly defined by concentrations of magnetite and was interpreted by Corbett (1981) as bedding. This mineralogical layering imparts a gneissic appearance to the rock, hence the term "Gneiss". The rock consists of albite and quartz in various proportions, plus 5-10% magnetite. In outcrop the rock is typically stained reddish by secondary iron oxides. Ednas Gneiss also contains substantial amounts of more leucocratic albite-quartz (+/- magnetite) rocks, gradational in character to the gneissic rock described above. Also present are small amounts of albite-quartz-amphibole-magnetite rock, identical with that which characterises Redan Gneiss. Minor metasedimentary composite gneiss and very minor amphibolite are present. Quartz-magnetite rocks are known only north of Menindee Tank (GR 739420 Kinalung 1:25 000 sheet).|16-MAY-23
24260|Ednas Gneiss|Extent|The formation crops out very poorly, but is inferred to extend across the central part of the Redan 1:25 000 sheet, from west to east, and onto the lower part of the Kinalung 1:25 000 sheet. This formation wraps around the Redan Gneiss in the Redan Antiform.|16-MAY-23
24260|Ednas Gneiss|Thickness range|Outcrop width ranges from about 2 to 2.5 km on the northern side of the Redan Antiform, where magnetic trends imply no major structural reversals. Allowing for non-vertical dip and small scale internal folding, true width might be about 1 km.|16-MAY-23
24260|Ednas Gneiss|Relationships and boundaries|The base is defined by a change from a predominance of amphibole-bearing albite rich rocks (Redan Gneiss) to a predominance of magnetite bearing albite rich rocks (Ednas Gneiss). The basal part of Ednas Gneiss corresponds with a linear magnetic high, on the northern limb of the Redan Antiform. The top of Ednas Gneiss is defined by an increase in the abundance of metasediments or metasedimentary composite gneiss and/or a decrease in the  abundance of albite-quartz-magnetite gneiss. The upper part of Ednas Gneiss corresponds with a particularly strong linear magnetic high.|16-MAY-23
24260|Ednas Gneiss|Age reasons|Part of Proterozoic Willyama Supergroup - similarity of rock types, no observed unconformtiy.|16-MAY-23
24260|Ednas Gneiss|References|83/23842|16-MAY-23
25893|Ellenden Granite|Name source|Mount Ellenden, GR 249661 (Canberra 1:250 000 sheet).|16-MAY-23
25893|Ellenden Granite|Type section locality|The Ellenden Granite crops out along the Bungendore-Tarago road, characterised by rounded tor-like outcrops. Fresh grey granite is exposed in a cutting about 100 m north of the bridge over Deep Creek 10 km northeast of Bungendore. Fresh pink granite occurs by the roadside about 15 km from Bungendore (at GR 310028, Braidwood 1:100 000 sheet). Both equigranular and porphyritic phases are present, but not in situ.|16-MAY-23
25893|Ellenden Granite|Extent|The main mass of granite crops out over about 150 km2 in the vicinity of Mount Ellenden. A few smaller bodies, separate from the main part of the intrusion, crop out around the margins of the intrusion.|16-MAY-23
25893|Ellenden Granite|Lithology|Pink and grey medium to coarse hornblende biotite adamellite and granodiorite. Satellitic bodies of porphyritic granite occur near the eastern margin of the main mass. Aplite and dolerite dykes occur within the intrusion near its margins. Aplite dykes and phyllite inclusions in weathered coarse "granite" are well exposed in a railway cutting at GR 318026. Dolerite dykes can be seen in Emu Flat Creek, close to the railway line, at GR 337024.|16-MAY-23
25893|Ellenden Granite|Relationships and boundaries|The granite intrudes Ordovician metasediments.|16-MAY-23
25893|Ellenden Granite|Age reasons|It is regarded (Felton and Huleatt, 1975) as being the same age as the nearby Boro and Braidwood Granites, which have similar field and petrographic characteristics. The Boro Granite has been dated at 390 m.y. and the Braidwood Granite at 385 m.y. (Evernden and Richards, 1962) (Early Devonian).|16-MAY-23
25893|Ellenden Granite|Proposer|First used on Canberra 1:250 000 geological sheet (2nd edition) (Best et al. 1964); not defined.|16-MAY-23
82205|Elura Limestone Member|Name source|Named after the Elura mine (now Endeavor mine) where the subsurface unit is intersected.|16-MAY-23
82205|Elura Limestone Member|Unit history|Elura Limestone was first used by Lorrigan, A.N. (2005) (Zinifex Ltd., 380 St Kilda Rd., Melbourne, Vic 3004) and more comprehensively studied by David in his PhD thesis (2005).The informal stratigraphic name Elura limestone was introduced into the literature and has been widely used to describe a prominent subsurface reef limestone unit intersected in drill core immediately beneath the Endeavor-Zn-Pb-Ag massive sulphide deposit, located 43 km NNW of Cobar in central-western New South Wales (Lorrigan 2005; David 2005, 2008).|16-MAY-23
82205|Elura Limestone Member|Type section locality|Drill core section NP1047 (31.161464degS, 145.654392degE) from the Endeavor mine. The type core section is housed at the Londonderry Core Library of the Geological Survey of NSW and can be accessed by companies, researchers and general public.|16-MAY-23
82205|Elura Limestone Member|Description at type locality|>533.5 m of apparent total thickness of fossiliferous limestone.|16-MAY-23
82205|Elura Limestone Member|Extent|The limestone unit is known to be 50-70 m wide and 700 m long, with a maximum vertical thickness of over 500 m in the Endeavor mine district (David 2008). Its known spatial distribution is restricted to along the NE side of the Elura Thrust Fault Zone in the Endeavor mine district. The unit does not crop out.|16-MAY-23
82205|Elura Limestone Member|Thickness range|>533.5 m of apparent total thickness at type locality/type section.  Maximum over 500 m. Total thickness and distribution of the Elura Limestone Member observed in several drill core sections suggest that the carbonate build-up distally and laterally interfingers and pinches out into the surrounding fine-grained siliciclastics (dominantly mudstone and siltstone) of the Brookong Formation (Kopjye Group).|16-MAY-23
82205|Elura Limestone Member|Lithology|It consists of limestone with minor intercalated dark calcareous mudstone and siltstone of reefal, back reefal and out-shelf facies. The limestone is dominated by rudstone, boundstone, packstone, floatstone with minor grainstone.|16-MAY-23
82205|Elura Limestone Member|Depositional environment|The Elura Limestone Member represents a major carbonate build-up with a considerable relief above the seafloor, developed in shallow water shelf and reefal settings on the eastern margin of the northern Cobar Superbasin. Due to a rapid increase of sea-level, the reef structure (Elura Limestone Member) was drowned and acted as a underwater high ground before it was buried into the deep water mud and silt of the CSA Siltstone, but details of its nature and duration is unclear and no confirmative palaeontological and other age dating evidence is available.|16-MAY-23
82205|Elura Limestone Member|Fossils|At type locality, the recovered fauna include three species of rugose corals (Aphyllum sp., Nardophyllum sp. cf. N. lonense and Neomphyma karpinskiense), six species of tabulate corals (Favosites allani, Favosites goldfussi, Favosites grandipora, Heliolites daintreei, Heliolites porosa? and Syringopora sp.) and 10 identifiable species of conodonts (Caudicriodus woschmidti, Caudicriodus sp. indet, Cypricriodus hesperius, Genus & sp. indet., Oulodus sp., Panderodus unicostatus, Panderodus sp., Pandorinellina camelfordensis, Wurmiella excavata and Zieglerodina remscheidensis).|16-MAY-23
82205|Elura Limestone Member|Diastems or hiatuses|.|16-MAY-23
82205|Elura Limestone Member|Relationships and boundaries|At the type locality, conformable (or likely disconformable) contact with siltstone of the CSA Siltstone, but base of the limestone unit was not intersected in this drilling. However, in drill core DE522 (31.158759degS, 145.654118degE), the Elura Limestone Member consists of fossiliferous limestone of ~170 m in apparent thickness and conformably overlies mudstone and siltstone of 130 m penetrated thickness of the Brookong Formation (Kopyje Group).|16-MAY-23
82205|Elura Limestone Member|Identifying features|Subsurface unit and only detected in drilling. [???]|16-MAY-23
82205|Elura Limestone Member|Structure and Metamorphism|Moderate-intense recrystallization.|16-MAY-23
82205|Elura Limestone Member|Age reasons|Corals (both Rugosa and Tabulata) and conodonts from the middle part of the Elura Limestone Member can precisely date this prominent carbonate build-up within the Kopyje Group as latest Silurian to early Lochkovian (Early Devonian) age.|16-MAY-23
82205|Elura Limestone Member|Correlations|Based on the conodonts recovered, the Elura Limestone Member can correlate with several other basal Devonian units or horizons recognized in NSW, such as the White Tank Limestone Member of the Meryula Formation in the Cobar Superbasin, a unnamed carbonate unit in the southern Thomson Orogen, the Windellama Limestone Member of the Tangerang Formation of the Windellama region, the Elmside Formation in the Yass area and the Clandulla Limestone near Mudgee.|16-MAY-23
82205|Elura Limestone Member|Alteration and Mineralisation|Minor limestone hosted mineralisation occurs in veins and fractures and replaces calcite in the Elura Limestone Member.|16-MAY-23
82205|Elura Limestone Member|Geophysical Expression|Observed subsurface only. [???]|16-MAY-23
82205|Elura Limestone Member|Geochemistry|Carbonates.|16-MAY-23
82205|Elura Limestone Member|Defn author|Zhen,Y.Y. 29-JAN-2021.|16-MAY-23
82205|Elura Limestone Member|Proposed publication|Zhen, Y.Y. & Fitzherbert, J., 2021. Lochkovian (Early Devonian) corals and conodonts from the Elura limestone Member, north of Cobar in central-western New South Wales. Quarterly Notes of the Geological Survey of New South Wales, in press.|16-MAY-23
82205|Elura Limestone Member|References|CAROLAN P.M. 1999. Geology of Shelf Strata and Carbonate Hosted Mineralisation at the Elura Mine, Cobar, NSW. BSc (Honours) thesis, University of Wollongong, Wollongong (unpublished).  **DAVID V. 2005. Structural setting of mineral deposits in the Cobar Basin. PhD thesis, University of New England, Armidale (unpublished).  **DAVID V. 2008. Structural-geological setting of the Elura Zn-Pb-Ag massive sulphide deposit, Australia. Ore Geology Reviews 34, 428-444.  **DAVID V. 2018. Cobar Deposits - Structural control. ASEG Extended Abstracts, 2018:1, 1-9. DOI: 10.1071/ASEG2018abT6_2G  **LORRIGAN, A.N. 2005. Elura Zn-Pb-Ag deposit, Cobar District, NSW In Butt, C.R.M. et al. (eds.), "Regolith expression of Australia ore systems: a compilation of exploration case histories with conceptual dispersion, process and exploration models", CRC LEME (Cooperative Research Centre for Landscape Environments and Mineral Exploration), 1v, 143-145.  **Zhen, Y.Y. & Fitzherbert, J., 2021. Lochkovian (Early Devonian) corals and conodonts from the Elura limestone Member, north of Cobar in central-western New South Wales. Quarterly Notes of the Geological Survey of New South Wales, in press.|16-MAY-23
37298|Ermelo Pyroclastics|Name source|Ermelo homestead GR431895 Terry Hei Hei 1:50,000 sheet|16-MAY-23
37298|Ermelo Pyroclastics|Unit history|Ermelo Andesite Tuff (McKelvey & White 1964)Ermelo Dacite Tuff (Chesnut 1971)Ermelo Pyroclastics (Opdyke et al. 2000)|16-MAY-23
37298|Ermelo Pyroclastics|Geomorphic expression|Cliff-forming in thicker parts of the unit.|16-MAY-23
37298|Ermelo Pyroclastics|Type section locality|The type section was designated 'in rocky bluffs 2 miles [2.5 km] west of Ermelo homestead' (McKelvey 1968), 2 km north-northeast of Derra Gap (GR398874 Terry Hei Hei 1:50,000 sheet).|16-MAY-23
37298|Ermelo Pyroclastics|Extent|The main outcrops are within fault blocks on the eastern limb of the Rocky Creek Syncline around Caroda, and in a belt extending northwards to the closure of the syncline; extensive outcrops are present in the vicinity of Derra Gap (GR398874 Terry Hie Hie 1:50,000 sheet). Others are between Caroda (GR458759 Eulowrie) and Slaughterhouse Pinnacle (GR389072 Gravesend 1:50,000 sheet) ; in a northwest-trending belt between GR342866 and 326888 (Terry Hie Hie 1:50,000 sheet) north of Montrose state Forest (McKelvey 1968); and in two belts on the faulted northwestern limb of the syncline near Moorabool (GR345091 Gravesend 1:50,000 sheet).|16-MAY-23
37298|Ermelo Pyroclastics|Thickness range|30 m in type area but greater than 160 m  between GR402881 to 392888 Terry Hie Hie 1: 50,000 sheet|16-MAY-23
37298|Ermelo Pyroclastics|Lithology|Crystal-rich, coarse to occasionally fine, andesitic to dacitic pyroclastic. It contains occasional lapillae, ash-rich siltstone. Minor cross bedding and rounded clasts up to cobble size are present in some localities. Constituents include abundant zoned and slightly abraded feldspar, less abundant, resorbed to angular quartz, hornblende, biotite, rare augite and opaque minerals.|16-MAY-23
37298|Ermelo Pyroclastics|Depositional environment|Ignimbritic to partially resedimented.|16-MAY-23
37298|Ermelo Pyroclastics|Relationships and boundaries|Conformably overlies the Spion Kop Conglomerate and in a few areas disconformably overlies the Caroda Formation. It is probably conformably overlain by the Clifden Formation.|16-MAY-23
37298|Ermelo Pyroclastics|Age reasons|Carboniferous (Namurian)  SHRIMP U-Pb (SL13) 321.3 +/- 3.2 Ma (SL13) (Opdyke et al. 2000); K-Ar hornblende 319 +/- 5 Ma (J. Roberts unpublished data).|16-MAY-23
37298|Ermelo Pyroclastics|Comments|The term pyroclastics is substituted because geochemical work (Wang 1999) indicates a composition varying from predominantly andesitic to dacitic and because the unit is partly resedimented.|16-MAY-23
37298|Ermelo Pyroclastics|References|CHESNUT W.S. 1971. Inverell 1:250,000 Geological Series Sheet SH 56-5. Geological Survey of NSW, Sydney.MCKELVEY B.C. 1968. Geological Map of New England 1:100,000, Bangheet Sheet (No. 280) with marginal text. The University of New England, Armidale, NSW, Australia.MCKELVEY B.C. & WHITE A.H. 1964. Geological Map of New England 1:100,000 Horton Sheet (No. 290), with marginal text. The University of New England, Armidale, NSW, Australia.OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
6437|Excelsior Porphyry Member|Name source|Synonym for Burraga Copper Mine.|16-MAY-23
6437|Excelsior Porphyry Member|Unit history|Member of the Lovetts Form.|16-MAY-23
6437|Excelsior Porphyry Member|Type section locality|Type area: Burraga Copper Mine. Location of Type Section: Burraga Copper Mine, Burraga 1:31680  517032.|16-MAY-23
6437|Excelsior Porphyry Member|Extent|East of Burraga. Restricted to lens in Burraga Copper Mine.|16-MAY-23
6437|Excelsior Porphyry Member|Thickness range|a) At type section: 20 m.  B) Maximum known: 40m.|16-MAY-23
6437|Excelsior Porphyry Member|Lithology|Quartz-feldspar porphyry.|16-MAY-23
6437|Excelsior Porphyry Member|Relationships and boundaries|Basal lithology of the Lovetts Formation in the Burraga Copper Mine.|16-MAY-23
6437|Excelsior Porphyry Member|Age reasons|Silurian - Stratigraphic position.|16-MAY-23
6437|Excelsior Porphyry Member|Defn approved by|copied from xerox sent by NSW Stratigraphic Nomenclature Committee|16-MAY-23
6504|Fairy Meadow Limestone Member|Name source|Fairy Meadow Creek, GR 367035 Braidwood 1:100 000 sheet.|16-MAY-23
6504|Fairy Meadow Limestone Member|Unit history|The limestones at Mount Fairy were referred to collectively by Carne and Jones (1919) as the "Fairy Meadow limestones". These limestones are now subdivided on lithological grounds, the name Sandhills Creek Limestone Member (Felton and Huleatt, 1975) being applied to the principal limestone/dolomite outcrops along Sandhills Creek and Fairy  Meadow Creek. The term Fairy Meadow Limestone Member is here applied to the smaller unit described above.|16-MAY-23
6504|Fairy Meadow Limestone Member|Type section locality|In Fairy Meadow Creek as above. 10 m of limestone is exposed.|16-MAY-23
6504|Fairy Meadow Limestone Member|Extent|The main outcrop of the unit is in Fairy Meadow Creek at GR 367044, Braidwood 1:100 000 sheet. Two small outcrops 500 m to the east may also belong to the unit.|16-MAY-23
6504|Fairy Meadow Limestone Member|Thickness range|10 m at the type section.|16-MAY-23
6504|Fairy Meadow Limestone Member|Lithology|Finely laminated micrite.|16-MAY-23
6504|Fairy Meadow Limestone Member|Relationships and boundaries|The unit appears to be a lens or discontinuous horizon of limestone enclosed by siltstone and tuffaceous arenite. Boundaries of the units, where exposed, are sharp.|16-MAY-23
6504|Fairy Meadow Limestone Member|Age reasons|The age of the De Drack Formation is Late Silurian, based on the identification of Monograptus(?)bohemicus by Strusz and Nicoll (1973). The Fairy Meadow Limestone is therefore also Late Silurian. The limestone itself is unfossiliferous.|16-MAY-23
6504|Fairy Meadow Limestone Member|Proposed publication|Felton E.A. and Huleatt M.B. 1975. Geology of the Braidwood 1:100 000 Sheet. Geological Survey NSW, Sydney.|16-MAY-23
6504|Fairy Meadow Limestone Member|References|01/31634; 73/015.|16-MAY-23
6504|Fairy Meadow Limestone Member|Parent|De Drack Formation|16-MAY-23
35525|Farmcote Gneiss|Name source|Farmcote homestead is situated very close to the main outcrops.|16-MAY-23
35525|Farmcote Gneiss|Unit history|The name Farmcote Gneiss is applied to an area of rocks that were previously interpreted as part of the Lady Brassey Formation. The change has been made because neither the association of lithologies nor the magnetic character is typical of Lady Brassey Formation, and because the stratigraphic position relative to the Thackaringa Group is uncertain.|16-MAY-23
35525|Farmcote Gneiss|Type section locality|No exposed section fulfils the ideal criteria for a type section. The type section nominated between GRs 570250E 6454800N and 569500E 6450000N (Zone 54 AGD1966) (southeast of Farmcote homestead) exhibits the upper contact with the Cues Formation, and shows all of the component rock types. However, structural complications could mean that the southern half of the section is a partial repetition of the northern half. A reference section is nominated south of Huonville homestead, between GRs 553600E 6447100N and 556850E 6445850N, showing good outcrop of the upper half of the Farmcote Gneiss.|16-MAY-23
35525|Farmcote Gneiss|General description|The component rock types were described by Stevens & Corbett (1993) as Association A: leucocratic albite - quartz-rich metasediments (Pl symbol on published maps), leucocratic quartz - K-feldspar - plagioclase (±biotite, magnetite) gneiss (leucogneiss Lf), amphibolite/basic granulite (although it is believed that granulite-facies metamorphic grade was attained, most of the basic gneisses have retrogressed to amphibolite). The amphibolite/basic granulite bodies were probably dolerite sills/dykes (Stevens 1998) intruded before or during Broken Hill Group time. They are therefore not part of this stratigraphic unit, although sills tend to cluster at certain levels of the stratigraphy. Nutman & Ehlers (1998a) noted that one of the leucogneiss bodies is discordant to layering in the enclosing albitic rocks (altered metasediments) and interpreted it as a deformed leucogranite. However, low-angle discordance between massive and layered rock units in a highly deformed terrain could result from rheological differences. Page et al. (2005a) and this paper showed that the age of the leucogneiss and the host metasediments are within error, permitting the leucogneiss to have been volcanic in origin, although more likely a granitic or subvolcanic intrusion. Hence, it is uncertain whether the leucogneisses should be considered part of the stratigraphic unit.|16-MAY-23
35525|Farmcote Gneiss|Thickness range|It is difficult to estimate the true thickness of the Farmcote Gneiss; outcrop width varies from about 1 to 5 km. True thickness may be of the order of 1 - 2 km.|16-MAY-23
35525|Farmcote Gneiss|Lithology|See the above 'General description'.|16-MAY-23
35525|Farmcote Gneiss|Relationships and boundaries|Relationships to apparently underlying and overlying units are unclear, largely as a result of the scarcity of outcrop. The Farmcote Gneiss forms the uppermost part of the very magnetic Redan geophysical zone, apparently overlain by the Cues Formation of the Thackaringa Group. It is unclear whether the upper boundary is a stratigraphic boundary, or a folded fault, but the age of 1705 ± 5 Ma is consistent with the Farmcote Gneiss correlating with the lower Thackaringa Group. Stevens (2006a) introduced the name Rantyga (pronounced ran-teega) Group to include the four formations comprising the Redan geophysical zone, from base to top: Redan Gneiss, Ednas Gneiss, Mulculca Formation, Farmcote Gneiss. There is no outcrop of the lower contact of the Farmcote Gneiss with the Mulculca Formation, but on a regional scale the two are conformable.|16-MAY-23
35525|Farmcote Gneiss|Age reasons|Maximum 1705 ± 5 Ma (this paper), minimum 1703 ± 3 Ma, 1705 ± 3 Ma (Page et al. 2005a). SHRIMP U - Pb zircon dating.|16-MAY-23
35525|Farmcote Gneiss|Defn Reference|Stevens B.P.J., Page R.W. and Crooks A. 2008, 'Geochronology of Willyama Supergroup metavolcanics, metasediments and contemporaneous intrusions, Broken Hill, Australia' , Australian Journal of Earth Sciences, vol. 55(3) p328.|16-MAY-23
24609|Farmers Creek Formation|Name source|Farmers Creek, Lithgow Valley|16-MAY-23
24609|Farmers Creek Formation|Constituents|Katoomba Coal Member, the Burragorang Claystone Member and the Middle River Coal Member (at the base).|16-MAY-23
24609|Farmers Creek Formation|Type section locality|(1) Location - Elecom Lithgow-Newnes DDH31 (221925m E, 1310965 m N, Lithgow 1:50 000 sheet, 8931-111).  (2) Repository - Elecom core store, Lithgow.  Reference Section: Brown Gap, GR 158600, Hampton 8930-IV.|16-MAY-23
24609|Farmers Creek Formation|Extent|Western Coalfield. Lithgow and Bungleboori 1:50 000 sheets. Equivalent lithological unit known in the Ulan and Putty area. Also, occurs on parts of the Hampton, Katoomba, Glen Davis and Glen Alice sheets.|16-MAY-23
24609|Farmers Creek Formation|General description|The Katoomba Coal Member is not always the topmost coal. The unit outcrops in the Lithgow Brickpit and at Browns Gap.|16-MAY-23
24609|Farmers Creek Formation|Thickness range|(1) Type section - from 202.24 m to 222.30 m. Thickness 20.06 m.  (2) Maximum recorded - 97 m.|16-MAY-23
24609|Farmers Creek Formation|Lithology|Claystone, carbonaceous shale, coal, mudstone, siltstone, sandstone, siliceous claystone, oil shale.|16-MAY-23
24609|Farmers Creek Formation|Relationships and boundaries|Overlain with regional unconformity by the Caley Formation of the Narrabeen Group. Conformably underlain by the Gap Sandstone. In the Ulan area this unit is in places almost completely eroded by the overlying Narrabeen Group sandstones.|16-MAY-23
24609|Farmers Creek Formation|Proposed publication|Australian Coal Geology|16-MAY-23
24609|Farmers Creek Formation|Proposer|Bembrick C.S.|16-MAY-23
6862|Fossil Hill Limestone|Name source|The name derives from Fossil Hill where the lower part of the formation is exceptionally well exposed.|16-MAY-23
6862|Fossil Hill Limestone|Unit history|The informal 'Lower Member' of Webby (1969) was named the Fossil Hill Limestone Member by Osborne (1978); this latter is now redefined as a formation. It is probably equivalent to both 'Davy's Creek limestone' and 'Large Flat limestone' of Opik (MS) as quoted by Stevens (in Hill, 1957, p.100). Use of 'Davy's Creek limestone', however, must be abandoned as it duplicates the earlier established Davies Creek Granite (Stanton, 1956).  The change in rank is necessitated by the recent geological mapping of the limestone by Webby and Packham and the recognition of six mappable subdivisions (members) of the Fossil Hill Limestone.|16-MAY-23
6862|Fossil Hill Limestone|Type section locality|The type section was not designated by Osborne (1978). It will be designated in forthcoming publication as composite including section through lower part on Fossil Hill (GR 752812*) and section of upper part on immediately adjacent Dunhill Bluff (GR 753814*). This is consistent with Osborne's original description. (*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978).|16-MAY-23
6862|Fossil Hill Limestone|Thickness range|In the type area, the Fossil Hill Limestone is 110 m thick.|16-MAY-23
6862|Fossil Hill Limestone|Relationships and boundaries|The Fossil Hill Limestone is the lower of the three constituent formations of the Cliefden Caves Limestone  Group.|16-MAY-23
6862|Fossil Hill Limestone|Proposed publication|Stratigraphy of the Cliefden Caves Limestone Group (Upper Ordovician) - J. geol. Soc. Aust.|16-MAY-23
6993|Gap Sandstone|Name source|Browns Gap between Vale of Clywdd and Hartley Valley|16-MAY-23
6993|Gap Sandstone|Unit history|New name|16-MAY-23
6993|Gap Sandstone|Type section locality|(1) Location - Browns Gap, GR 158600, Hampton 1:50 000 sheet (8930-IV). See also Elecom Lithgow-Newnes DDH31 (221925 m E, 1310965 m N, Lithgow 1:50 000 sheet, 8931-111) Elecom core store, Lithgow.|16-MAY-23
6993|Gap Sandstone|Extent|Western Coalfield. Lithgow and Bungleboori 1:50 000 sheets. Equivalent lithological unit in Southern Coalfield, Ulan and Putty areas. Also occurs on parts of Hampton, Katoomba, Glen Davis and Glen Alice sheets.|16-MAY-23
6993|Gap Sandstone|General description|Sharp, erosive base, fines upward, planar and trough cross beds. In places erodes the entire State Mine Creek Formation and part or all of the Angus Place Sandstone. Top of unit recognised by transition to coal or argillaceous sediments of Farmers Creek Formation. Base of unit marked by abrupt transition from sandstone to (commonly) argillaceous and carbonaceous sediments of the State Mine Creek Formation, or (rarely) to a fining downward sandstone (Angus Place Sandstone).|16-MAY-23
6993|Gap Sandstone|Thickness range|(1) Type Section: 5.95 M. (In DDH31, from 222.30 m to 229.86 m. Thickness 6.56 m).   (2) Maximum recorded - 13.5 m.|16-MAY-23
6993|Gap Sandstone|Lithology|A medium and fine grained quartz-lithic sandstone, rarely coarse grained and pebbly. Minor mudstone.|16-MAY-23
6993|Gap Sandstone|Relationships and boundaries|Conformably underlies the Farmers Creek Formation. Overlies the State Mine Creek Formation or the Angus Place Sandstone (rarely the Baal Bone Formation), and is locally erosive into these units. Part of Wallerawang Sub-Group.|16-MAY-23
6993|Gap Sandstone|Proposed publication|Australian Coal Geology|16-MAY-23
26305|Gearys Gap Formation|Name source|Named after Gearys Gap (GR 165/133), a low saddle on the Lake George escarpment.|16-MAY-23
26305|Gearys Gap Formation|Unit history|None.|16-MAY-23
26305|Gearys Gap Formation|Type section locality|A fully cored type section is unavailable because drillcore recovery in this formation is generally poor.  A representative section is designated from BMR drillhole C354, over the intervals 116.5-132.0m; 135.5-149.5m; and 160.0-164.5m. Deeply weathered sand and gravel with minor clay and silt have been cored at recovery levels mostly in excess of 90%.|16-MAY-23
26305|Gearys Gap Formation|Extent|Lake George drainage base (Canberra 1:100 000 sheet 8727). The unit is represented by patches of ferruginous quartz gravel on the escarpment near Gearys Gap (GR 159/122) and silcrete on the western shore of Lake George (GR 170/113). Subsurface distribution is in palaeodrainage lines beneath Lake George.|16-MAY-23
26305|Gearys Gap Formation|Thickness range|A maximum thickness of 58m has been recorded in BMR drillhole C354 (Abell 1985a).|16-MAY-23
26305|Gearys Gap Formation|Lithology|Deeply weathered sand and gravel with minor silt and clay interbeds.  Lithological contrasts within the unit are apparent on downhole gamma and neutron logs (Abell 1985a).  The unit is characterised by illite, illitic mixed clays and residual kaolinite (Abell 1985b).|16-MAY-23
26305|Gearys Gap Formation|Depositional environment|Fluvial.|16-MAY-23
26305|Gearys Gap Formation|Relationships and boundaries|Base unconformable on an irregular bedrock surface of Late Ordovician and Late Silurian rocks. The unit passes upwards into finer sand and clay of the overlying Ondyong Point Formation. The top is also arbitarily taken at the top of a deeply weathered profile suggesting a disconformable relationship with the Ondyong Point Formation.|16-MAY-23
26305|Gearys Gap Formation|Age reasons|Unfossiliferous. An Early Miocene or older age is likely because of the probable Late Miocene age of the overlying Ondyong Point Formation and the Mid to Late Tertiary age placed on the the deep weathering profile (Ruxton and Taylor, 1982).|16-MAY-23
26305|Gearys Gap Formation|Correlations|Beyond the limits of the Lake George Basin the formation correlates with unnamed indurated quartz gravels along the eastern and southern margins of the Carwoola Flats (near Hoskinstown) and in the Yass River basin. In the Goulburn-Crookwell area the formation may be co-eval with quartzose sediments in the Hollymount Formation (Bishop 1984).|16-MAY-23
70111|Georges Bore Granite Gneiss|Name source|Georges Bore is about 2 km northeast of the geochronology sample site from this body.|16-MAY-23
70111|Georges Bore Granite Gneiss|Type section locality|The irregular shape of the body makes it difficult to specify a representative type section. The section from GR 512900E 6430750N to GR 515300E 6427850N (Zone 54 AGD 1966) is chosen because it exhibits most of the lithological variation in the gneiss, incorporates areas of intervening metasediments, and passes through the geochronology sample site.|16-MAY-23
70111|Georges Bore Granite Gneiss|Extent|A large, irregular body or bodies extending about 17 km in northeast strike length, and up to 4 km outcrop width. Located between Oakdale and Montana homesteads (both currently unoccupied), and enclosing the hill known as the Sentinel.|16-MAY-23
70111|Georges Bore Granite Gneiss|Lithology|Consists of apparently irregular areas of megacryst-rich and megacryst-poor quartz - feldspar - biotite gneiss, and minor garnet-bearing gneiss (Stroud 1986).|16-MAY-23
70111|Georges Bore Granite Gneiss|Relationships and boundaries|Intrusive into Thackaringa Group composite gneiss and albitised metasediments, and into Broken Hill Group metasediments.|16-MAY-23
70111|Georges Bore Granite Gneiss|Age reasons|1695 ± 4 Ma. SHRIMP U - Pb zircon dating, this paper.|16-MAY-23
70111|Georges Bore Granite Gneiss|Defn Reference|Stevens B.P.J., Page R.W. and Crooks A. 2008, 'Geochronology of Willyama Supergroup metavolcanics, metasediments and contemporaneous intrusions, Broken Hill, Australia' , Australian Journal of Earth Sciences, vol. 55(3) p330.|16-MAY-23
7133|Georgica Rhyolite Member|Name source|Georgica village; GR 169297, Nimbin 1:50 000 sheet 9540-IV.|16-MAY-23
7133|Georgica Rhyolite Member|Unit history|McElroy (1962) included this flow in the Nimbin Rhyolite.|16-MAY-23
7133|Georgica Rhyolite Member|Type section locality|Immediately west of the Nimbin Rocks from 194344 (base) to 196343 (top). 100 m of porphyritic rhyolite of which the lowermost 10 m is vitrophyric. The type area was described by Relph (1958).|16-MAY-23
7133|Georgica Rhyolite Member|Extent|The unit occurs over an area of 40 km2 south and south-west of Nimbin (217366).|16-MAY-23
7133|Georgica Rhyolite Member|Lithology|Two-feldspar rhyolite, either vitrophyric or porphyritic with a microcrystalline groundmass.|16-MAY-23
7133|Georgica Rhyolite Member|Relationships and boundaries|A member unit of the Kyogle Basalt. Conformably overlies the Homeleigh Agglomerate Member. The top is everywhere eroded to an unknown degree. The base is marked by a glassy zone of variable thickness (up to 10 m) representing the chilled base to the flow.|16-MAY-23
7133|Georgica Rhyolite Member|Age reasons|The Lamington Volcanics as a whole have been dated at 23-20 m.y. by :K-Ar methods (Wellman and McDougall, 1974, and references therein).|16-MAY-23
7133|Georgica Rhyolite Member|Defn author|Duggan M.B., Mason D.R., 1978|16-MAY-23
7133|Georgica Rhyolite Member|Proposed publication|Journal of the Geological Society of Australia.|16-MAY-23
7133|Georgica Rhyolite Member|References|97/28843; 79/04604.|16-MAY-23
7133|Georgica Rhyolite Member|Reserved? Yes/No|Yes|16-MAY-23
35899|Gibsonvale Formation|Name source|The unit is named after the hamlet of Gibsonvale, which is in turn named after Jack Gibson, a prospector who discovered alluvial tin deposits in the area in 1938.|16-MAY-23
35899|Gibsonvale Formation|Geomorphic expression|Large areas of the unit have been redistributed and artificially sorted by mining operations and the unit is now best exposed in pits.|16-MAY-23
35899|Gibsonvale Formation|Type section locality|In situ deposits occur in a scraping (469483 MGAE, 6275868 MGAN) 400 m east south east of Kikoira, where they unconformably overlie Ordovician metasedimentary rock. A weathering profile is developed in coarse sandstone in the northern bank of Contessa's Open Cut Mine (470833 MGAE, 6276363 MGAN).|16-MAY-23
35899|Gibsonvale Formation|Extent|Exposed mainly in pits and open cut mines which are scattered over approximately 10km southeast from Kikoira to Gibsonvale, it continues as deep leads which have been partially mapped by mining companies extending towards the east.|16-MAY-23
35899|Gibsonvale Formation|Thickness range|Company drilling suggests that the basal gravel deposits are typically up to 3 m thick and overlain by 6 m of unconsolidated, well-sorted fine- to medium-grained quartz sand passing up into 15 m of clayey sand and brown clay. A mottled ferruginous weathering profile is sometimes observable and is overlain by up to 3 m of red soil.|16-MAY-23
35899|Gibsonvale Formation|Lithology|The unit consists of quartzose conglomerate, pebbly sandstone and sandstone which contain common detrital cassiterite. Clasts are sub-rounded to rounded and consist of dominant white vein quartz  with minor cassiterite and metasedimentary lithics. Typically, the coarse-grained sandy matrix consists of angular to sun-angular grains of quartz, cassiterite (some quartz veined), altered feldspar, tourmaline and chert with interstitial kaolinite and sporadically developed limonitic cement.|16-MAY-23
35899|Gibsonvale Formation|Depositional environment|The gravels were deposited by high energy braided streams which dissected the weathered landscape and followed a course defined by the (partly faulted) boundary between the Kikoira Granite and Ordovician metasedimentary rocks, and joints and fractures within these terrains.|16-MAY-23
35899|Gibsonvale Formation|Fossils|None found.|16-MAY-23
35899|Gibsonvale Formation|Diastems or hiatuses|Sporadically developed weathering profiles at the top of the Gibsonvale Formation reflect depositional hiatuses.|16-MAY-23
35899|Gibsonvale Formation|Relationships and boundaries|The unit unconformably overlies a range of Palaeozoic rocks and is overlain by mixed alluvial and aeolian Quaternary deposits.|16-MAY-23
35899|Gibsonvale Formation|Age reasons|Tertiary (-?Quaternary). Though not directly dated, comparison with coarse alluvial deposits dated by palynology elsewhere in NSW (eg H Martin for DLWC), suggests likely to be Neogene (Miocene?) in age.|16-MAY-23
35899|Gibsonvale Formation|Correlations|May correlate with the Calavil Formation in the Murray Basin.|16-MAY-23
35899|Gibsonvale Formation|Comments|Hosts placer tin deposits.|16-MAY-23
7306|Gladstone Formation|Name source|Unknown.|16-MAY-23
7306|Gladstone Formation|Unit history|Toll Bar Group (Hanlon, in Hill, 1954). Toll Bar Formation (Rasmus, 1964).|16-MAY-23
7306|Gladstone Formation|Type section locality|Alliance, Quirindi No. 1 well. Location of Type Section: Not defined by Hanlon (1949). Here designated 3127 ft to 36582 ft (Packham, 1970) in Alliance Quirindi No. 1 well. Core stored Department of Mines, Core Library, Londonderry).|16-MAY-23
7306|Gladstone Formation|Extent|West of Willow Tree.|16-MAY-23
7306|Gladstone Formation|Thickness range|a) At type section: 555 ft.  B) Maximum known: 800 ft at Willow Tree in Tributary of Borambil Creek 715838 to 710837 (Quirindi A-G 1:31,680 topographic sheets).|16-MAY-23
7306|Gladstone Formation|Lithology|Finely bedded carbonaceous shales and claystones and minor interbedded pebbly sandstones. Limestones have been noted high in the unit also.|16-MAY-23
7306|Gladstone Formation|Fossils|Glossopterid leaves.|16-MAY-23
7306|Gladstone Formation|Relationships and boundaries|The Gladstone Formation conformably overlies Porcupine Formation. The Digby Formation of assumed Triassic age overlies the Gladstone Formation with a high angle unconformity at Willow Tree.|16-MAY-23
7306|Gladstone Formation|Age reasons|Late Permian due to stratigraphic position.|16-MAY-23
7306|Gladstone Formation|Proposed publication|Journal Proc. of Royal Soc. Of NSW|16-MAY-23
7306|Gladstone Formation|Defn approved by|Approved. Copied from xerox sent by NSW Stratigraphic Nomenclature Sub-Committee.|16-MAY-23
7306|Gladstone Formation|Proposer|Lowe S.P.|16-MAY-23
7306|Gladstone Formation|Status|1|16-MAY-23
24286|Gleesons Limestone Member|Name source|The name is derived from Gleesons Creek (GR 759829*) a tributary of the Belubula River, some 2 km north-north-east of Fossil Hill.  (*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978)).|16-MAY-23
24286|Gleesons Limestone Member|Unit history|The Gleesons Limestone Member was previously known informally as the 'lower big shell' unit (Webby 1969).|16-MAY-23
24286|Gleesons Limestone Member|Type section locality|Type section on the north-east slopes of Fossil Hill (GR. 752812*)(*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978)).|16-MAY-23
24286|Gleesons Limestone Member|Description at type locality|In the type section it comprises 6 m of volcanic breccia, calcareous siltstones and shales (a 'lithic' unit); 4.5 m of a lime-mud and wackestone-supported Eodinobolus shell bank; 2 m of gastropod, algal (Hedstroemia) and coral (Tetradium)-dominated wackestones; 4.5 m of skeletal wackestones with bryozoans at two horizons; 1.5 m of platy bedded, pelloidal packstones; and 1.5 m of Eodinobolus-dominated wackestones.|16-MAY-23
24286|Gleesons Limestone Member|Thickness range|In the type section it is 20 m thick.|16-MAY-23
24286|Gleesons Limestone Member|Relationships and boundaries|It represents the lowest of the six constituent members of the Fossil Hill Limestone. Despite being affected by a number of small folds and faults in the type section on the north-east slopes of Fossil Hill (GR. 752812*), the order of succession and thickness of the Gleesons Limestone Member can be firmly established. It rests with apparent disconformity on the Walli Andesite and is succeeded by the Kalimna Limestone Member (new name) of the Fossil Hill Limestone|16-MAY-23
24286|Gleesons Limestone Member|Identifying features|The Gleesons Limestone Member has been mapped as an independent unit throughout the Cliefden Caves area.|16-MAY-23
24286|Gleesons Limestone Member|Proposer|Webby B.D., Packham G.H.|16-MAY-23
24286|Gleesons Limestone Member|Resdate|12-MAY-1981.  Ref. 80/1569|16-MAY-23
24286|Gleesons Limestone Member|Reserved? Yes/No|Central Register, BMR, Canberra|16-MAY-23
40761|Glen Allyn Ignimbrite Member|Name source|From the property Glen Allyn (0248290E 6582680N Kelvin 1:25 000 sheet).|16-MAY-23
40761|Glen Allyn Ignimbrite Member|Type section locality|Locality 510-5 30051?54?S, 150021?16?E (0247043E 6582343N) on the northeastern part of Gunnan Ridge.|16-MAY-23
40761|Glen Allyn Ignimbrite Member|Extent|Restricted to Gunnan Ridge. Crops out along the eastern margin of the ridge in the north, around closures of a syncline and anticline in the central part, and possibly on the ridge crest in the south.|16-MAY-23
40761|Glen Allyn Ignimbrite Member|Thickness range|Between 5 and 35 m.|16-MAY-23
40761|Glen Allyn Ignimbrite Member|Lithology|The lower part of the member has small plagioclase and K-feldspar phenocrysts and small oriented, elongate pumice fragments; lapillae are present at locality 519-18 (0248335E 6580430N Gunnedah 1:25 000 sheet); the upper part has coarser shards and slightly larger and more abundant phenocrysts and pumice fragments. A sample analysed by XRF (Geeve 1995 MU55262), with a dacitic composition, may be from this unit.|16-MAY-23
40761|Glen Allyn Ignimbrite Member|Age reasons|Namurian.|16-MAY-23
24610|Glen Davis Formation|Name source|Village of Glen Davis, Capertee Valley.|16-MAY-23
24610|Glen Davis Formation|Unit history|New name|16-MAY-23
24610|Glen Davis Formation|Type section locality|(1) Location - Placer Wolgan DDH 2 (231121 m E, 1319262 m N Bungleboori 1:50 000 sheet, 8931-11);  (2) Repository - NSW Dept of Mineral Resources Core Library, Londonderry. Reference Section: Browns Gap, GR 158600, Hampton 8930 - IV.|16-MAY-23
24610|Glen Davis Formation|Extent|Western Coalfield; Lithgow and Bungleboori 1:50 000 sheets. Also on part of Glen Davis and Glen Alice sheets.|16-MAY-23
24610|Glen Davis Formation|General description|A unit of variable thickness and lithology, commonly containing oil shale horizons. The sandstone units, where present, commonly fine downwards. Acritarchs present. Bioturbated in part. Near the western outcrop the coal at the base becomes thick enough to have been called (Carne, 1908 and Hall, 1956) the "Upper Irondale Seam". Top of unit recognised by a change to dark grey argillaceous sediments, commonly bioturbated and laminated. Base of unit marked by sharp contact with sandstone of Newnes Formation.|16-MAY-23
24610|Glen Davis Formation|Thickness range|(1) Type Section - from 366.28 m to 372.68 m; thickness 6.40 m.  (2) Maximum recorded - 13 m.|16-MAY-23
24610|Glen Davis Formation|Lithology|Claystone, minor siltstone mudstone, thin coal, carbonaceous claystones and sandstone. Sporadic development of siliceous claystones and oil shale.|16-MAY-23
24610|Glen Davis Formation|Relationships and boundaries|Conformably overlain by the Baal Bone Formation and underlain by the Newnes Formation. Part of Charbon Sub-Group.|16-MAY-23
24610|Glen Davis Formation|Proposed publication|Australian Coal Geology|16-MAY-23
24610|Glen Davis Formation|References|01/31626|16-MAY-23
24610|Glen Davis Formation|Proposer|Bembrick C.S.|16-MAY-23
7460|Gnalta Group|Name source|"Gnalta" property, northeastern Broken Hill 1:250 000 sheet area.|16-MAY-23
7460|Gnalta Group|Extent|Northeastern Broken Hill 1:250 000 sheet area, in valley drained by Mount Wright Creek.|16-MAY-23
7460|Gnalta Group|Thickness range|4050-4450 m.|16-MAY-23
7460|Gnalta Group|Identifying features|Definition: Gnalta Group (Rose 1968 following Warris 1967, unpubl.). Includes Mount Wright Volcanics, Cymbric Vale Formation and Coonigan Formation.|16-MAY-23
7460|Gnalta Group|Age reasons|Early to early Middle Cambrian.|16-MAY-23
7460|Gnalta Group|Proposed publication|Palaeontographica A177 p.129-212|16-MAY-23
7460|Gnalta Group|Defn approved by|Approved by NSW Sub-Committee. See file 82/86 folios 209 and 195.|16-MAY-23
24296|Goonbri Formation|Name source|Goonbri' Mountain; GR KM334092, Boggabri 1:100 000 Sheet area.|16-MAY-23
24296|Goonbri Formation|Unit history|Not previously recognised. Time equivalent to the Dalwood Group of the Hunter Valley.|16-MAY-23
24296|Goonbri Formation|Type section locality|Intersected in Kembla Coal & Coke Pty. Limited borehole DDH MAC 44 from 145.04m to 340.73 m. When corrected for apparent dip, a true thickness in excess of 150 m is postulated. Top is identified by a massive fine to medium grained massive sandstone. Drilling terminated within the unit so a lower boundary cannot be determined.|16-MAY-23
24296|Goonbri Formation|Extent|The unit exists in the subsurface over 12 km2 in the central northern portion of the Boggabri 1:100 000 Sheet area around longitude 150o12', latitude 30o34', north of Goonbri Mountain.|16-MAY-23
24296|Goonbri Formation|Thickness range|Range 0-150 m. It is likely that maximum thickness is significantly greater than 150 m.|16-MAY-23
24296|Goonbri Formation|Lithology|A coarsening upward sequence. Basal section is a dark, massive siltstone. Central part is interbedded fine grained sandstone and siltstone with evidence of bioturbation. Top is characterised by a massive, fine to medium grained sandstone.|16-MAY-23
24296|Goonbri Formation|Relationships and boundaries|Suggest unconformably overlies the Boggabri Volcanics (Hanlon, 1949) and the Leard Formation (Brownlow, 1981), if present. Goonbri Formation onlaps the Boggabri Volcanics. The Leard Formation is a weathering product of the Boggabri Volcanics so it is likely that the Goonbri also onlaps the Beard Formation in a similar manner. Conformably overlain by the Maules Creek Formation (Brownlow, 1981). First appearance of coal marks top of the Goonbri Formation.|16-MAY-23
24296|Goonbri Formation|Age reasons|Microflora is fairly restricted but can be assigned to Early Permian Stage 3 of Price, 1976 (McMinn, 1981) viz interval between first occurrence of g. trisinus and thymospora cicatricosus. Abundance of monosaccate pollen (I.e. plicatipollenites spp.) also indicates Early Permian age.|16-MAY-23
24296|Goonbri Formation|Defn author|Etheridge L.T., 1986|16-MAY-23
24296|Goonbri Formation|Proposed publication|Abstracts, 20th Newcastle Symposium; Bicentennial Volume|16-MAY-23
24296|Goonbri Formation|Comments|Notes: The Goonbri Formation onlaps the Boggabri Volcanics to the west. It is truncated to the east by the Mooki Thrust. It is suggested that the Goonbri Formation is a lake deposit.|16-MAY-23
24296|Goonbri Formation|References|01/31265|16-MAY-23
24296|Goonbri Formation|Defn Reference|87/25681. Described p.2.|16-MAY-23
24296|Goonbri Formation|Resdate|24-JUN-1986|16-MAY-23
24297|Goonigal Group|Name source|Goonigal Creek between GR 1575 9110 and GR 16709020 (Bathurst 1:250 000).|16-MAY-23
24297|Goonigal Group|Unit history|The Goonigal Group is equivalent to the invalid "Fairhill Formation" of Savage (1968). The equivalent strata further to the north was subdivided by Maggs (1963) and the original formation of Savage was elevated to group status by work presented in the NSW Geological Survey's Silurian Lexicon.|16-MAY-23
24297|Goonigal Group|Type section locality|The group as a whole has no specific type section, and the component formations and lithologies are described elsewhere.|16-MAY-23
24297|Goonigal Group|Extent|The unit is exposed in several north-south trendings tracts - two undifferentiated tracts, one up to 6 km wide extending from about 13 km S to 6 km N of Manildra, and the other extending from about 11 km SSE to 18 km NNE of Manildra and about 2 km wide (both on Bathurst 1:250 000 sheet); and two differentiated tracts, the first composed of the Wansey Tuff, Geneffe Shale, Burgoon Formation and Jews Creek Volcanics and extending from 16 km N of Manildra (Bathurst 1:250 000 sheet) to 22 km SSE of Yeoval (Dubbo 1:250 000 sheet); and the second consisting of the Myrangle Formation and the Buckinbah Volcanics, extending from about 22 km SSE of Yeoval to 14 km SE of Yeoval. The latter two tracts are up to about 3 km wide.|16-MAY-23
24297|Goonigal Group|Thickness range|The group is about 1100 m thick in the south, and increases to about 1250 m in the north. Details of thicknesses of individual formations are given elsewhere.|16-MAY-23
24297|Goonigal Group|Lithology|Predominantly andesitic to dacitic volcanic sandstones, greywackes, siltstones and shales with lesser amounts of non-tuffaceous sediments and intermediate to acid lavas.|16-MAY-23
24297|Goonigal Group|Relationships and boundaries|A brachiopod fauna in the uppermost horizons of the group indicate a Pridolian or early Gedinnian age (Savage, 1973), and underlying formations limit the lower parts of the group to the late Silurian. The group underlies the Early Devonian Gregra Group (Savage, 1968) with conformity, and conformably overlies the Mackeys Creek shale (Savage, 1968).|16-MAY-23
24297|Goonigal Group|Proposed publication|NSW Geological Slurvey's Silurian Lexicon to be published as a Record of the Geological Survey of NSW|16-MAY-23
24297|Goonigal Group|References|79/03796|16-MAY-23
24297|Goonigal Group|Proposer|Bradley G.M.|16-MAY-23
24297|Goonigal Group|Resdate|08-JUL-1974|16-MAY-23
24297|Goonigal Group|Status|1|16-MAY-23
24298|Gospel Oak Shale|Name source|Gospel Oak Public School Site, GR 168848, Bathurst 1:250 000 sheet.|16-MAY-23
24298|Gospel Oak Shale|Unit history|Lower Avoca Valley Lshale (Ryall 1966).|16-MAY-23
24298|Gospel Oak Shale|Type section locality|Locking Hole Creek, south of Liscombe Pools homestead, at GR 178852, Bathurst 1:250 000 sheet.|16-MAY-23
24298|Gospel Oak Shale|Extent|A 9-mile long belt in the Cranky Rock Anticline and a meridional strip ca. 5 miles long between the Canangle and Columbine Mountain Thrusts, east of Canowindra.|16-MAY-23
24298|Gospel Oak Shale|Thickness range|110 m.|16-MAY-23
24298|Gospel Oak Shale|Lithology|Red, green and brown shales which contain a proiminent buff siltstone bed which is graptolitic. Immediately below the contact with the Porphyry in the red-brown shales occur numerous spherical concretions which are up to 10" across. Where this unit crops out around the Cranky Rock Anticline exactly the same units are present.|16-MAY-23
24298|Gospel Oak Shale|Relationships and boundaries|Overlies the Liscombe Pools Limestone (Percival 1976) with apparent conformity. Base defined by transition from limestone to shale. Overlain by Canowindra Porphyry (Ryall 1966) with apparent conformity. Sharp contact with Porphyry marks the top of the formation.|16-MAY-23
24298|Gospel Oak Shale|Age reasons|Silurian; Late Llandovery to Early Wenlock. Graptolite assemblage with Monograptus priodon, M. aff. vomerinus, M. ? spiralis and Retiolites geinitzianus. Upper limit not certain.|16-MAY-23
24298|Gospel Oak Shale|Defn author|Pickett J., 1982|16-MAY-23
24298|Gospel Oak Shale|Proposed publication|"Silurian System of NSW", Geological Survey of NSW|16-MAY-23
24298|Gospel Oak Shale|Comments|Notes: The name is introduced to replace the name "Lower Avoca Valley Lshale" (Ryall 1966), which is in contravention of the Code as it is everywhere separated from the "(Upper) Avoca Valley Shale" by the Canowindra Porphyry.|16-MAY-23
24298|Gospel Oak Shale|References|79/03373; 01/31575.|16-MAY-23
24298|Gospel Oak Shale|Defn Reference|86/25236  Defined P.79|16-MAY-23
24298|Gospel Oak Shale|Proposer|Pickett J.W.|16-MAY-23
24298|Gospel Oak Shale|Status|1|16-MAY-23
24299|Gourock Granodiorite|Name source|Gourock Range on the western margin of the Araluen 1:100 000 sheet area.|16-MAY-23
24299|Gourock Granodiorite|Type section locality|Head of Jarrabattgulla Creek at GR 272335.|16-MAY-23
24299|Gourock Granodiorite|Extent|Near the axis of the Gourock Range in the Crow Valley Creek valley on the western side and the Jerrabattgulla Creek valley on the eastern side. The granodiorite is composed of two separate elongate masses each of about 7 km2.|16-MAY-23
24299|Gourock Granodiorite|Lithology|Everywhere the granodiorite is strongly foliated. It is mainly medium grained hornblende granodiorite but in the southern parts of the two separate masses medium grained leucogranite predominates. At the head of Crow Valley Creek the leucogranite forms meridional trending dyke-like bodies.|16-MAY-23
24299|Gourock Granodiorite|Age reasons|The granodiorite is probably Early Devonian and has been deformed in the Carboniferous. A sample from GR 261410 yielded a biotite K/Ar age of 373 +/- 6 m.y. and a biotite-whole rock Rb/Sr age of 380 +/- 6 m.y. with initial ratio 0.7103. These results are probably partly reset by the Carboniferous deformation.|16-MAY-23
24299|Gourock Granodiorite|Resdate|26-MAY-1982|16-MAY-23
24299|Gourock Granodiorite|Reserved? Yes/No|Yes|16-MAY-23
7665|Gragin Conglomerate|Name source|County of Gragin, east of Warialda.|16-MAY-23
7665|Gragin Conglomerate|Type section locality|About five kilometres along Spring Gully and Warialda Creek from GR 758285 to GR 731271 (Bingara 1:100 000, 9038).|16-MAY-23
7665|Gragin Conglomerate|Extent|The unit is exposed over 140 km2 in Warialda Creek area and The Darling Plain area southeast of Warialda.|16-MAY-23
7665|Gragin Conglomerate|Thickness range|At least 60 m. Maybe up to 100 m thick.|16-MAY-23
7665|Gragin Conglomerate|Lithology|Conglomerate, composed of well rounded, almost spherical cobbles of quartz-feldspar porphyry including tuff, ignimbrite and flow banded rhyolites with some granites. Chert, jasper, metamorphosed basic volcanic rock and metamorphosed sediment is less abundant. The matrix is composed of coarse to medium-grained feldspathic to sublabile sandstone.|16-MAY-23
7665|Gragin Conglomerate|Relationships and boundaries|Conformably overlies Cunnee Formation. The basal contact of the Gragin Conglomerate is erosive at some sites and grades into Cunnee Formation at other sites. Unconformably overlain by E-Middle Jurassic Hutton Sandstone.|16-MAY-23
7665|Gragin Conglomerate|Age reasons|Presence of Dicroidium eskense (Walkom) a mid Triassic fern. Also presence of Falcisporites australis and Falcisporites (or Artisporites) similis.|16-MAY-23
7665|Gragin Conglomerate|Proposed publication|Records, Geological Survey of NSW|16-MAY-23
7665|Gragin Conglomerate|References|01/31576;|16-MAY-23
7665|Gragin Conglomerate|Status|1|16-MAY-23
7702|Grants Head Formation|Name source|Grants Head 915898 Camden Haven 1:63 360.|16-MAY-23
7702|Grants Head Formation|Name source|Grants Head: Lat 31deg 36min 05.8sec S, 152deg 50min, 49.3sec E. The Grants Head Formation was described and formally named by Pratt and Herbert (1973), after Grants Head where, on the northern side, the formation is best exposed in the coastal cliffs and adjacent rock platform.|16-MAY-23
7702|Grants Head Formation|Unit history|Named by Pratt & Herbert (1973). [RefID 32719].|16-MAY-23
7702|Grants Head Formation|Geomorphic expression|The Grants Head Formation forms low coastal cliffs and crops out poorly in the gently undulating lowlands in a shallow syncline in the immediate vicinity of Bonny Hills.|16-MAY-23
7702|Grants Head Formation|Type section locality|Grants Head, from Lat 31.59803deg S, Long 152.84719deg E to Lat 31.58994deg S, Long 152.84004deg E. The type section is exposed in cliffs and along the rock platform from the northern side of Grants Head to the southern end of Rainbow Beach at Bonny Hills. Pratt and Herbert (1973) nominated the exposure at Grants Head as the type section. A precise location at Grants Head, between GR 485504 6504108 (1:25 000 map sheet 9434-1-N, Grants Head; location 31; Photograph 5), and GR 484824 6505004 (1:25 000 map sheet 9434-1-N, Grants Head; location 33) is now specified as the location of the type section. A lithology plot of the measured section is presented in Figure 13.|16-MAY-23
7702|Grants Head Formation|Type section locality|Grants Head. Location of Type Section: Grants Head 915898 Camden Haven 1:63 360.|16-MAY-23
7702|Grants Head Formation|Description at type locality|The formation is an overall upward-fining sequence grading from minor pebble and granule conglomerate interbedded with lithic-quartz sandstone and siltstone near the base, passing upwards into interbedded quartz-lithic and quartz sandstone and grey mudstone. The unit contains a wide variety of bedding thicknesses and sedimentary structures. Bedding thicknesses range from thick beds of granule conglomerate and sandstone to very thinly laminated beds of mudstone. Sedimentary structures include cross stratification, parallel laminations, flaser bedding, ripple laminations, occasional palaeosols, and upward-fining sequences.|16-MAY-23
7702|Grants Head Formation|Extent|The formation is only exposed on the northeastern edge of the Lorne Basin. The author has not identified the formation west of the Jolly Nose Hill.|16-MAY-23
7702|Grants Head Formation|Extent|Lorne Basin.|16-MAY-23
7702|Grants Head Formation|Thickness range|a) at type section: 75 m.  b) maximum known: 75 m.|16-MAY-23
7702|Grants Head Formation|Thickness range|The Grants Head Formation at the type section is 155 m in thickness. However, the top of the section is faulted out so the true thickness may exceed that figure.|16-MAY-23
7702|Grants Head Formation|Lithology|Interbedded sandstone and laminated fine sandstone and shale.|16-MAY-23
7702|Grants Head Formation|Lithology|Analysis of the type section (Figure 13), indicated lithological composition of: conglomerate 1%; sandstone 40%; and siltstone and claystone 59%. The formation fines upwards with rudaceous rocks dominating the basal 45 m (conglomerate 3%; sandstone 66%; and siltstone and claystone 31%). Siltstone and claystone dominate the upper 110 m, with sandstone (30%) and siltstone and claystone (70%).|16-MAY-23
7702|Grants Head Formation|Depositional environment|A fluviatile depositional environment for the Grants Head Formation is indicated by the presence of cross-stratified sheet and channel sandstone deposits, levee deposits, ripple lamination, flasar bedding, laminated grey siltstones with root casts and occasional palaeosol horizons. Megafossil floral material was collected and examined by Holmes and Ash (1979) from the Grants Head Formation and they also suggested a depositional environment of backswamps bordering streams and filled by overbank flooding for the plant-bearing strata.|16-MAY-23
7702|Grants Head Formation|Fossils|Plant Spores and fragmentary plants.|16-MAY-23
7702|Grants Head Formation|Fossils|Lower Triassic plant fossils recorded by several authors including Holmes and Ash (1979)|16-MAY-23
7702|Grants Head Formation|Relationships and boundaries|Of Camden Haven Group. The Grants Head Formation conformably overlies the top pebble conglomerate bed of Laurieton Conglomerate (Figure 13) at its type section. However, the top of the section is faulted so that its overlying stratigraphic relationships are unknown. Along most of the type section, the Grants Head Formation is unconformably overlain by beds up to 3 m thick of ferricrete-containing clasts of Grants Head Formation, grading in size from granule to boulders, set in a ferruginised matrix of mud to pebble conglomerate and well exposed at Boat Ramp Beach (location 32). These ferruginised beds are probably of Quaternary age.|16-MAY-23
7702|Grants Head Formation|Relationships and boundaries|Conformably overlies the Laurieton Conglomerate.|16-MAY-23
7702|Grants Head Formation|Identifying features|The distinguishing features for the Grants Head Formation are the absence of reddish purple interbedded mudstone and the absence of cobbles in the conglomerates of the lower, coarser part of the formation. Near the top of the cliff at the northern end of Bartletts Beach at Bonny Hills (location 104) a reddish purple hue is imparted to grey mudstones by a veneer of flakey ferruginised float from ferruginised horizons above. Close examination revealed the horizon to contain plant remains. Also absent from the Grants Head Formation are the tuff beds and poor coaly horizons characteristic of the younger Milligans Road Formation.|16-MAY-23
7702|Grants Head Formation|Structure and Metamorphism|The Grants Head Formation has an average dip of 10° towards 320°.|16-MAY-23
7702|Grants Head Formation|Age reasons|Helby (1972) examined a sample which yielded 10 species of palynomorphs from the northern end of Bartletts Beach (location 104), 63 m from the base of the formation. Bocking (1977) also collected samples from this location and identified Dicroidium dubium var. australe (Jacob & Jacob) Retallack. Holmes and Ash (1979) collected and identified more species from the same location. Both the palynology and megaflora samples suggest a late Early Triassic age for the Grants Head Formation.|16-MAY-23
7702|Grants Head Formation|Age reasons|Lower Triassic - Aratrisporites tenuispinosus Assemblage.|16-MAY-23
7702|Grants Head Formation|Correlations|There are no units in the Lorne Basin which correlate to the Grants Head Formation.|16-MAY-23
7702|Grants Head Formation|Defn author|G. Winston Pratt, 7-JUL-2010.|16-MAY-23
7702|Grants Head Formation|Proposed publication|Rec. geological Survey NSW.|16-MAY-23
7702|Grants Head Formation|Comments|Described.|16-MAY-23
7702|Grants Head Formation|Comments|Redefined to more accurately locate the type section and to note the absence of reddish-purple mudstones. [thickness has significantly changed too]|16-MAY-23
7702|Grants Head Formation|References|Bocking M.A. 1977. The geology of the Lorne Basin and underlying lithologies in the region of Grants Head. MSc Preliminary thesis. University of Sydney. (unpublished). **Helby (1972), Geol Survey NSW Report Palynology 1972/3 (unpub).  **Helby R.J. 1973. Review of Late Permian and Triassic palynology of New South Wales. Geological Society of Australia Special Publication 4, pp. 141-155.   **Holmes W.B.K. & Ash S.R. 1979. An early Triassic megafossil flora from the Lorne Basin, New South Wales. Proceedings of the Linnean Society of New South Wales, 103, 47-70. **Pratt, G.W. 2010. A revised Triassic stratigraphy for the Lorne Basin, NSW. Quarterly Notes of the Geological Survey of New South Wales 126. **Pratt G.W. & Herbert C. 1973. A reappraisal of the Lorne Triassic Basin. Geological Survey of New South.Wales, Records 15, 205-212. **Retallack G.J. 1977. Reconstructing Triassic vegetation of eastern Australasia: a new approach for the biostratigraphy of Gondwanaland. Alcheringa 1(3), 247-277.|16-MAY-23
7702|Grants Head Formation|Defn approved by|Copied from xerox sent by NSW Stratigraphic Nomenclature Committee|16-MAY-23
7702|Grants Head Formation|Name first published by|Pratt G.W., Herbert C., 1973|16-MAY-23
27162|Gundagai Serpentinite|Name source|Gundagai Township 611668 (yds) Wagga Wagga 1:250 000 Sheet SI/55-15.|16-MAY-23
27162|Gundagai Serpentinite|Unit history|Would form part of a general ultramafic belt described by Rayner (1969) known as the Gundagai Serpentine Belt.|16-MAY-23
27162|Gundagai Serpentinite|Type section locality|North of Gundagai.  Type Section: 1.5 km north of Gundagai 609670 to 610670 (yds) (Wagga Wagga 1:250 000 Sheet).|16-MAY-23
27162|Gundagai Serpentinite|Extent|Comprises two bodies trending 330o, extending over a distance of 15.5 km between 607676 and 613663 (Wagga Wagga 1:250 000 sheet - extending 0.25 km into southern part Cootamundra 1:250 000 Sheet).|16-MAY-23
27162|Gundagai Serpentinite|Thickness range|a) At Type Section: 0.7 km.  b) Maximum known: 1 km.|16-MAY-23
27162|Gundagai Serpentinite|Lithology|Serpentinited, talc-carbonate rocks. Pyroxenite, Gabbro Pegmatite.|16-MAY-23
27162|Gundagai Serpentinite|Relationships and boundaries|Intrusive into Blowering Beds (tuffaceous sediments, phyllites) and the Jones Creek Porphyrite (Winward 1972 - BSc. Thesis. "The Geology of the Gundagai District).|16-MAY-23
27162|Gundagai Serpentinite|Age reasons|Cambrian to Early Ordovician - Part of the Jindalee Beds which are assigned this age on analogy to Girilambone Beds, Scheibner - Tectonic Map of NSW.|16-MAY-23
27162|Gundagai Serpentinite|Defn author|Basden H., Adrian J., Clift D.LS.L., Winchester R.E., 1978|16-MAY-23
27162|Gundagai Serpentinite|Proposed publication|Geology of the Cootamundra 1:100 000 Sheet (Geological Survey of NSW in prep.)|16-MAY-23
27162|Gundagai Serpentinite|Defn approved by|Copied from xerox from NSW Sub-Committee|16-MAY-23
7886|Gundahl Complex|Name source|Gundahl Creek, GR 6250 1800 Gundahl 1:25 000 Topographic Sheet.|16-MAY-23
7886|Gundahl Complex|Unit history|Previously included this unit in the "Mann River sequence" (Fergusson, 1982).|16-MAY-23
7886|Gundahl Complex|Type section locality|Representative Section: Along the Nymboida and Mann rivers (GR 5900 0900 to GR 5385 1662 Gundahl and GR 5475 2040 Gundahl to GR 4790 3710 Coombadjha) there are abundant and in places near continuous exposures.|16-MAY-23
7886|Gundahl Complex|Extent|The unit is exposed over 500 km2 in the eastern part of the Grafton 1:250 000 Sheet area (SH 56-6) along the Mann River to the northwest and south of Jackadgery.|16-MAY-23
7886|Gundahl Complex|Thickness range|The style of deformation precludes any reliable estimate of thickness. The Gundahl Complex is a tectonic melange with blocks embedded in a sheared matrix. Similar lithofacies and lithofacies sequences are found within blocks repeated throughout the unit implying an imbricate fault structure. Individual blocks may contain coherent sequences up to hundreds of metres thick.|16-MAY-23
7886|Gundahl Complex|Lithology|Six main lithofacies of the unit include: massive greywacke, greywacke-argillite, argillite, interbedded argillite-tuff, bedded cherts and greenstones (I.e. alteread basic volcanics).|16-MAY-23
7886|Gundahl Complex|Relationships and boundaries|Unconformably overlain by the Mesozoic Clarence-Moreton Basin. Intruded by the Dandahra Creek Granite and in part faulted against or intruded by a ring pluton of the Coombadjha Volcanic Complex (McPhie, 1982). Northeast contact with the Willowie Creek beds is a major fault. Contact with the Cunglebung Creek beds to the southwest is marked by large blocks of greywacke and chert of the Gundahl Complex and is probably faulted.|16-MAY-23
7886|Gundahl Complex|Age reasons|Day et al. (1978, p.345) reported ooliths in greywackes from the Gundahl Complex near Jackadgery and suggested a correlation with similar greywackes in the Neranleigh-Fernvale beds and the Curtis Island Group of eastern Queensland. This implies a possible Early Carboniferous age for greywacke-bearing lithologies of the Gundahl Complex.|16-MAY-23
7886|Gundahl Complex|Proposed publication|Journal of the Geological Society of Australia|16-MAY-23
7886|Gundahl Complex|Proposer|Fergusson, C.L.|16-MAY-23
7886|Gundahl Complex|Reserved? Yes/No|Yes|16-MAY-23
24302|Gundillion Conglomerate|Name source|After Gundillion Homestead (GR 386396, Araluen 1:100 000 map).|16-MAY-23
24302|Gundillion Conglomerate|Unit history|The name was introduced by Johnson (1964, ANU M.Sc. Thesis) but has never been published.|16-MAY-23
24302|Gundillion Conglomerate|Type section locality|On ridge just south of stream, from GR 390402 (base) to 386401 (top) on Araluen sheet. Exposes about 150 m of coarse massive conglomerate at base becoming finer upwards, into pebbly arenite and coarse arenite.|16-MAY-23
24302|Gundillion Conglomerate|Extent|Widespread in a longitudinal zone on Araluen 1:100 000 sheet from west of Majors Creek to southern border of map. Also present in north of Cobargo sheet, to the south of Araluen sheet.|16-MAY-23
24302|Gundillion Conglomerate|Thickness range|Very variable from 0 m to 150 m, often over short distances.|16-MAY-23
24302|Gundillion Conglomerate|Lithology|Typically a massive to very poorly bedded, reddish-purple poorly sorted, coarse polymict conglomerate. Clasts can be up to 1 m across, but usually 30 cm or less. Has a tendency to become finer upwards, with coarse arenite and pebbly arenite common at top of unit. Locally it may have a basal breccia which appears to represent a fossil soil or scree deposit.|16-MAY-23
24302|Gundillion Conglomerate|Relationships and boundaries|Rests unconformably on Late Silurian De Drack Formation and Long Flat Volcanics. Overlain conformably by Long Swamp Creek Formation. The gradational contact with the Long Swamp Creek Formation is taken at the top of the highest conglomerate or pebbly arenite in the section. It also overlies unconformably the Braidwood Granite.|16-MAY-23
24302|Gundillion Conglomerate|Age reasons|The unit is unfossiliferous. From relationships with other units, and regional considerations, a Late Devonian age is likely.|16-MAY-23
24302|Gundillion Conglomerate|Resdate|18-APR-1981|16-MAY-23
24302|Gundillion Conglomerate|Reserved? Yes/No|Yes|16-MAY-23
7913|Gunnee Formation|Name source|County Gunnee, north of Delungra.|16-MAY-23
7913|Gunnee Formation|Type section locality|Along an unnamed tributary of Pine Creek from GR 802139 to GR 783143 (Bingara 1:100 000, 9038).|16-MAY-23
7913|Gunnee Formation|Extent|About 75 km2 in the Darling Plain area and some parts of Warialda Creek southeast of Warialda.|16-MAY-23
7913|Gunnee Formation|Thickness range|Approximately 2 to 30 m.|16-MAY-23
7913|Gunnee Formation|Lithology|Interbedded, conglomerate, breccia, arkose, feldspatholithic sandstone, siltstone, mudstone and minor coal. The unit grades from coarse at the base to fine at the top.|16-MAY-23
7913|Gunnee Formation|Relationships and boundaries|Non conformably overlies rocks of the central part of the New England Fold Belt. It is overlain by the Gragin Conglomerate which in places has a very erosive base.|16-MAY-23
7913|Gunnee Formation|Age reasons|Middle Triassic. This is supported by the presence of plant remains including Cladophlebis, Cobifolia (Walkom), Johstonia coriacea (Johnson) Xylopteris elongata. (carruthers), also spore such as artisporites, parvispinosus.|16-MAY-23
7913|Gunnee Formation|Proposed publication|Records, Geological Survey of NSW|16-MAY-23
7913|Gunnee Formation|Status|1|16-MAY-23
8051|Hanrahan Agglomerate Member|Name source|Main road of Burraga Hanrahan Drive Burraga 1: 31 680 GR 510052|16-MAY-23
8051|Hanrahan Agglomerate Member|Unit history|Member of the Lovetts Formation|16-MAY-23
8051|Hanrahan Agglomerate Member|Type section locality|Burraga Copper Mine. Location of Type Section: Burraga Copper Mine Burraga 1:31 680 GR 518032.|16-MAY-23
8051|Hanrahan Agglomerate Member|Extent|East of Burraga|16-MAY-23
8051|Hanrahan Agglomerate Member|Thickness range|a) At type section: 40 m.  b) Maximum known:  70 m.|16-MAY-23
8051|Hanrahan Agglomerate Member|Lithology|Interbedded dark grey agglomerate and coarse tuffs.|16-MAY-23
8051|Hanrahan Agglomerate Member|Relationships and boundaries|Overlies Excelsior Porphyry Member.|16-MAY-23
8051|Hanrahan Agglomerate Member|Age reasons|Silurian - Stratigraphic position.|16-MAY-23
8051|Hanrahan Agglomerate Member|Proposed publication|"The geology of the Burraga Copper Mine". Records of the Geological Slurvey of NSW.|16-MAY-23
8051|Hanrahan Agglomerate Member|Defn approved by|Copied from xerox sent by NSW Stratigraphic Nomenclature Committee|16-MAY-23
8051|Hanrahan Agglomerate Member|Name first published by|Bowman N.H., 1975|16-MAY-23
8051|Hanrahan Agglomerate Member|Reserved? Yes/No|Bowman H.N.|16-MAY-23
37334|Hazeldene Sandstone|Name source|The name is derived from Hazeldene Homestead a property on the Weja Road at AMG 475500-6248200.|16-MAY-23
37334|Hazeldene Sandstone|Unit history|None.|16-MAY-23
37334|Hazeldene Sandstone|Constituents|None.|16-MAY-23
37334|Hazeldene Sandstone|Geomorphic expression|Outcrop is recessive throughout.|16-MAY-23
37334|Hazeldene Sandstone|Type section locality|The proposed type locality is just south of the Mid Western Highway at AMG 472564-6250695 where there is subcrop of well sorted red micaceous sandstone on a low rise in a ploughed field.|16-MAY-23
37334|Hazeldene Sandstone|Extent|Outcrop is limited to a small rise near the type locality.|16-MAY-23
37334|Hazeldene Sandstone|Thickness range|The inferred thickness is 200 m.|16-MAY-23
37334|Hazeldene Sandstone|Lithology|The formation comprises medium to fine grained, moderately sorted, maroon sandstone with a significant component of detrital mica. Pebbly sandstone (eg at AMG 473244-6247790) makes up a minor component.|16-MAY-23
37334|Hazeldene Sandstone|Fossils|None found.|16-MAY-23
37334|Hazeldene Sandstone|Relationships and boundaries|The lower contact with Barrat Conglomerate and upper contact with Edithvale Formation are not exposed but the formation is inferred to be conformable with both.|16-MAY-23
37334|Hazeldene Sandstone|Age reasons|Upper Devonian age is inferred.|16-MAY-23
37334|Hazeldene Sandstone|Correlations|The unit may be equivalent to the Naradhan Sandstone.|16-MAY-23
37334|Hazeldene Sandstone|Comments|The formation has a moderate K, Th, U radiometric response and this gives it a speckled appearance in RGB images. It has a higher response than the underlying Barrat Conglomerate. It has a uniformly low magnetic response and measured magnetic susceptibilities do not exceed 10x10-5 SI units.|16-MAY-23
37912|Hazelvale Rhyodacite Member|Name source|Named after the property Hazelvale, now renamed Strathdownie, GR272621 Coryah 1:25,000 sheet.|16-MAY-23
37912|Hazelvale Rhyodacite Member|Unit history|Hazelvale Rhyodacite (Opdyke et al. 2000).  Named informally by Hocking (1973).|16-MAY-23
37912|Hazelvale Rhyodacite Member|Type section locality|On a ridge crest at GR296598 Coryah 1:25,000 sheet.|16-MAY-23
37912|Hazelvale Rhyodacite Member|Extent|On the western and eastern limbs and area of southern closure of the Berrygil Anticline; in the hills northeast of 'Darthula' (GR286584 Coryah 1:25,000 sheet). Possible outcrops of the unit occur on the eastern limb of the anticline southeast from Locheil Downs and on the western limb of the anticline at Locheil Downs (GR281651 Grattai 1:25,000 sheet).|16-MAY-23
37912|Hazelvale Rhyodacite Member|Thickness range|<5m|16-MAY-23
37912|Hazelvale Rhyodacite Member|Lithology|South of the type locality the rhyodacite is a red to pink, unwelded ignimbrite. It contains feldspars, quartz, minor pyroxene, opaque minerals, pumices and minor brown to grey volcanic rock fragments. The groundmass is vitric and rich in shards and bubble walls. Towards 'The Downs' (GR284662 Grattai 1:25,000 sheet) outcrops consist mainly of fine to coarse red, resedimented sandstone. The sandstone contains the same minerals and groundmass as the ignimbrite as well as abundant andesite, dacite and pumice fragments.|16-MAY-23
37912|Hazelvale Rhyodacite Member|Depositional environment|Ignimbrite to fluvially resedimented sandstone.|16-MAY-23
37912|Hazelvale Rhyodacite Member|Relationships and boundaries|Lowermost ignimbrite within the Rocky Creek Conglomerate within the Darthula block.|16-MAY-23
37912|Hazelvale Rhyodacite Member|Age reasons|Carboniferous (Namurian).|16-MAY-23
37912|Hazelvale Rhyodacite Member|References|HOCKING R.M. 1973. The Carboniferous Back Creek-Pound Creek sequence, southwest of Caroda, New South Wales. BSc (Hons) thesis, University of new England, Armidale (unpubl.).OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
24312|Hollymount Formation|Name source|Hollymount' property; GR 9695 7865, Goulburn 1:250 000 Sheet area (SI 55-12).|16-MAY-23
24312|Hollymount Formation|Unit history|Williamson (1969) assigned a Miocene age to the Glen Logan Gravel, a high level quartzose gravel around Cowra, NSW.|16-MAY-23
24312|Hollymount Formation|Type section locality|10 metres of semi-lithified quartzose sand, granules and gravel exposed beneath the Bevendale Basalt in a cutting on Paddys Creek at GR 9725 7945. The base is identified by very coarse quartz cobbles (up to 30 cm intermed. Axis) and the top by medium to fine sands abruptly overlain by Bevendale Basalt.|16-MAY-23
24312|Hollymount Formation|Extent|Unit is exposed discontinuously between Gunning and Narrawa, NSW, in the upper Lachlan Valley, in association with the overlying Bevendale Basalt.|16-MAY-23
24312|Hollymount Formation|Thickness range|Range 1 to 15 m.|16-MAY-23
24312|Hollymount Formation|Lithology|Fine sand to coarse cobbles; white quartz in orange-brown clayey sand matrix; massive to cross-bedded. Also occurs in a silicified form as benches of massive sand and cobble silcrete, some of which contains silicified wood and leaf fragments.|16-MAY-23
24312|Hollymount Formation|Relationships and boundaries|Disconformably overlies undifferentiated Ordovician phyllites as a channel-fill. Conformably overlain by Bevendale Basalt.|16-MAY-23
24312|Hollymount Formation|Age reasons|Early Miocene on basis of K-Ar ages of overlying Bevendale Basalt (Wellman & McDougall, 1974; Young & Bishop, 1980).|16-MAY-23
24312|Hollymount Formation|Comments|Notes: The Hollymount Formation crops out beneath, * topographically above the Bevendale Basalt and represents quartzose fluvial sediment which was deposited immediately prior to *extrusion of the lavas of the Bevendale Basalt. The outcrops of the Hollymount Formation now found topographically above the Bevendale Basalt were probably originally covered by the basalt which has since been removed by erosion.  (*Amendments 16/10/84 file 82/86).|16-MAY-23
8440|Homeleigh Agglomerate Member|Name source|Homeleigh settlement, 6 km north-west of Kyogle, GR 040390, Nimbin 1:50 000 sheet 9540-IV.|16-MAY-23
8440|Homeleigh Agglomerate Member|Unit history|Included in the Nimbin Rhyolite by McElroy (1962).|16-MAY-23
8440|Homeleigh Agglomerate Member|Type section locality|On the Homeleigh road (048371) 5 km north-east of Kyogle.  30 m of volcanic agglomerate.|16-MAY-23
8440|Homeleigh Agglomerate Member|Extent|The unit is exposed over an area of 200 km2 mainly within the triangle bounded by Wiangaree (865455), Kyogle (003336) and Nimbin (217366) with sporadic outcrops farther south in the McKellar Range.|16-MAY-23
8440|Homeleigh Agglomerate Member|Thickness range|Range 5-30 m.|16-MAY-23
8440|Homeleigh Agglomerate Member|Lithology|Volcanic agglomerate containing blocks up to 1 m in diameter in a rhyolitic matrix. Blocks include subalkaline rhyolites and rhyolitic pitchstones and minor mugearite, benmoreite and trachyte.|16-MAY-23
8440|Homeleigh Agglomerate Member|Relationships and boundaries|A Member unit of the Kyogle Basalt. Occurs within the Kyogle Basalt and is clearly recognisable as an acid pyroclastic unit within a sequence of alkaline basaltic flows. In the east (west and south of Nimbin) it is conformably overlain by the Georgica Rhyolite Member. Here the top of the unit is recognised by the passage into the lower glassy portion of the rhyolite flow comprising the Georgica Rhyolite Member.|16-MAY-23
8440|Homeleigh Agglomerate Member|Age reasons|The Lamington Volcanics as a whole have been dated at 23-20 m.y. by K-Ar methods (Wellman and McDougall 1974 and refereances therein). An age of 22.2 m.y. on a specimen from the Hillview Rhyolite (now Mt Gillies Rhyolite; Ross, 1974), which may be a correlative, is given by Wellman and McDougall (1974).|16-MAY-23
8440|Homeleigh Agglomerate Member|Defn author|Duggan M.B., Mason D.R., 1978|16-MAY-23
8440|Homeleigh Agglomerate Member|Proposed publication|Journal of the Geological Society of Australia|16-MAY-23
8440|Homeleigh Agglomerate Member|Comments|Notes: May be a correlative of the Mt Gillies Rhyolite in south-eastern Queensland (Ross, 1974) although the Mt Gillies Rhyolite is directly overlain by sub-alkaline basalts akin to the Lismore Basalt.|16-MAY-23
8440|Homeleigh Agglomerate Member|Reserved? Yes/No|Yes|16-MAY-23
8512|Hoskinstown Group|Name source|Named after the village of Hoskinstown at GR 225/775.|16-MAY-23
8512|Hoskinstown Group|Unit history|Captains Flat Group (Glasson and Paine, 1965).|16-MAY-23
8512|Hoskinstown Group|Constituents|Copper Creek Shale, Kohinoor Volcanics, Carwoola Formation, Captains Flat Formation.|16-MAY-23
8512|Hoskinstown Group|Extent|The Hoskinstown Group underlies a broad topographic depression coinciding with the Captains Flat Graben. Formations within the group separate into two limbs southwest of Hoskinstown. In the western limb the sediments persist along the Primrose Valley Creek towards the Queanbeyan River while in the eastern limb they reach Captains Flat and contract as fault-bounded remnants as far south as the Bredbo River (Canberra and Michelage 1:100 000 sheets 8727 and 8726 respectively).|16-MAY-23
8512|Hoskinstown Group|General description|Formations within the Hoskinstown Group have been described on the Michelago 1:100 000 sheet by Richardson (1979).|16-MAY-23
8512|Hoskinstown Group|Thickness range|A minimum thickness of 4,000 m is given by  Oldershaw (1965) but this may reach 5,000m in the deeper axial portions of the Captains Flat Graben.|16-MAY-23
8512|Hoskinstown Group|Depositional environment|Quiet, relatively shallow-water marine conditions.|16-MAY-23
8512|Hoskinstown Group|Relationships and boundaries|The lower boundary is obscured by strong deformation, however conglomeratic beds at the base of the Copper Creek Shale (Rutledge Quartzite Member) are taken as evidence of a stratigraphic break with the underlying Ordovician rocks. The group is otherwise faulted against Ordovician rocks mainly along the Whiskers and Ballallaba Faults. The topmost units are truncated by the present erosion surface and by Cainozoic alluvium.|16-MAY-23
8512|Hoskinstown Group|Age reasons|Late Silurian (Ludlow to Pridoli) - fossils are scarce.|16-MAY-23
8512|Hoskinstown Group|Correlations|Facies equivalent of Mount Fairy Group - a shallow marine volcano-sedimentary sequences at the western edge of the Capertee Shelf. In part coeval with the Late Silurian Laidlow Volcanic Suite on the Canberra-Yass Shelf.|16-MAY-23
8512|Hoskinstown Group|Defn author|Probably R.S. Abell circa 1990.|16-MAY-23
8630|Hylea Intrusive Complex|Name source|Name derived from the Hylea Homestead which is near the intrusive.|16-MAY-23
8630|Hylea Intrusive Complex|Unit history|No previous published description. The BMR first detected on aeromagnetic anomaly in 1961.|16-MAY-23
8630|Hylea Intrusive Complex|Type section locality|Immediately south of Hylea Homestead Narromine 1:250 000 SI-55/3 GR.  Type Section: Drill core, drilled by Lomadec Exploration, DDP Lomadec B, 750 ft Narromine 1:250 000 SI 55/3, 1:50 000 833 No. 3 GR 524500 998800|16-MAY-23
8630|Hylea Intrusive Complex|Extent|Size: a) At type section: Its area is at least 11 km2 but may be larger with several isolated intrusions.  b) Maximum known:|16-MAY-23
8630|Hylea Intrusive Complex|Lithology|An intrusive complex of intermediate to basic composition. Dominant lithology is hornblende monzonite. There are phases of hornblendites including aegerine augite hornblendite, biotite hornblendite. Some phases of syenodiorite, biotite augite diorite of hypersthene augite syenodiorite.|16-MAY-23
8630|Hylea Intrusive Complex|Relationships and boundaries|The boundaries are discordant and the body is intrusive into the metasediments of the Girilambone Beds of Cambro-Ordovidian age.|16-MAY-23
8630|Hylea Intrusive Complex|Age reasons|397 +/- 162 m.y. K-Ar dating. Lower Devonian.|16-MAY-23
8630|Hylea Intrusive Complex|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982.|16-MAY-23
8630|Hylea Intrusive Complex|Proposed publication|Notes to accompany Narromine 1:250 000 Metallogenic Map|16-MAY-23
8630|Hylea Intrusive Complex|Defn approved by|Copies from xerox from Nsw Sub-Committee|16-MAY-23
8630|Hylea Intrusive Complex|Name first published by|Thomson J., 1975|16-MAY-23
8630|Hylea Intrusive Complex|Reserved? Yes/No|Stroud J.|16-MAY-23
24315|Ina Volcanics|Name source|Parish of Ina, County Gipps.|16-MAY-23
24315|Ina Volcanics|Type section locality|Along east-west Burcher-Forbes road between 8.5 km and 5.5 km east of Burcher. Bottom contact with Manna Conglomerate does not outcrop. Top contact with Banar Formation sharply defined on the ground. 537857 (bottom) to 533857 (top) Forbes 1:250 000.|16-MAY-23
24315|Ina Volcanics|Description at type locality|Along the type section N of the road, the contact between the Manna Conglomerate and the overlying rhyolite tuff porphyry of the Cowal Member of the Ina Volcanics is obscured by a few hundred metres of soil. Going westward and up-dip the section is as follows: a. Cowal Member - A massive coarse rhyolite tuff porphyry about 1000 thick. It consists of phenocrysts of quartz and feldspar in a sericitic groundmass. A small lens of tuff breccia containing angular dark grey aphanitic fragments occurs south of the road. b. Andesite - Between the rhyolite tuff to the east and fine clastics to the west along the type section and elsewhere, there is a soil covered area which the BMR aeromagnetic map shows to be a long magnetic ridge. From evidence mentioned later, this part of the section probably contains a very persistent andesite flow or flows. This andesitic horizon is evident from the magnetic maps as far south as east of West Wyalong and even Barmedman, and northwards it appears to finish at the northern boundary of the geological map as shown in Fig. 1. c. Overlying the interpreted andesite, and outcropping continuously to the north of the road, is a section of cherty shales, greenish tuffaceous rocks, silts and sands, and finally a thick sequence of siliceous shales. They are sharply overlain by the Banar Formation and the contact is exposed. This part of the sequence is about 1000 m thick. The topmost siliceous shales laterally along strike contain and grade into rhyolite tuff porphyry. These tuff bodies are in places very thin, but are up to about 100 m in thickness and 1000 m in strike length in max. size. They consist of quartz and feldspar phenocrysts set in a sericitic groundmass. They are characterised by fairly abundant irregular angular fragments of greyish shale or perhaps devitrified glass or pumice. These fragments are up to about 10 cm in size.  Along the horizon of the tuff there are also lenses of calcarenites, calcareous shales and sandstones with abundant crinoid stem remains. There are also dolerite sills. Along the type section the siliceous shales are overlain sharply by the Banar Formation.|16-MAY-23
24315|Ina Volcanics|Extent|The unit is exposed for about 16 km along strike between Corringle and Burcher.|16-MAY-23
24315|Ina Volcanics|Thickness range|About 2000 m.|16-MAY-23
24315|Ina Volcanics|Lithology|The Ina Volcanics consist of a succession of rhyolite tuff porphyries, sandstones, andesites, shales and minor conglomerates which overlie the Weelah Formation in the north and the Manna Conglomerate in the south. There is considerable lateral facies variation in the Ina Volcanics. Notable along these are a number of andesite flows outcropping in the Nerang-Cowal State Forest and also shown up by aeromagnetics to occur in a few other places along strike.  The andesites in the forest are greenish, calcareous and generally fragmental. They contain small feldspar lath phenocrysts. There are abundant dark fine fragments up to 1 cm in size. Also in the Nerang Cowal State Forest, the sandstones overlying the Cowal Member in places grade into conglomerate. It is clear that the Ina Volcanics contain a complex of lithological types: shales, mudstones, acid volcanics, andesitic volcanics, sandstones, conglomerates and carbonates.|16-MAY-23
24315|Ina Volcanics|Fossils|Within the silts and sands, a sheared trilobite resembling Encrinurus has been found.|16-MAY-23
24315|Ina Volcanics|Relationships and boundaries|Perhaps partly unconformable on Weelah Formation and Manna Conglomerate.|16-MAY-23
24315|Ina Volcanics|Age reasons|Probably Silurian. Encrinurus sp. found within formation.|16-MAY-23
24315|Ina Volcanics|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (v.7 No. 1)|16-MAY-23
21998|Ingalara Ashstone Member|Name source|Ingalara Creek, 5km north of Colinton. Michelago 1:100 000 sheet (alternative spelling Ingelara).|16-MAY-23
21998|Ingalara Ashstone Member|Unit history|Conforms in part with a unit previously mapped as 'Sva" within the Colinton Volcanics (Richardson, 1979).|16-MAY-23
21998|Ingalara Ashstone Member|Type section locality|Along Ingalara Creek Michelago 1:100 000 sheet 8726, from GR931350 (base) to GR928353 (top).|16-MAY-23
21998|Ingalara Ashstone Member|Extent|Extends discontinuously along a narrow belt from about 1km north of Ingalara Creek near its confluence with the Murrimbidgee River south to a point near the Monaro Highway about 4km north of Bredbo.|16-MAY-23
21998|Ingalara Ashstone Member|Thickness range|Ranges to about 250m.|16-MAY-23
21998|Ingalara Ashstone Member|Lithology|White to very pale grey, fine-grained, massive to faintly banded rhyolitic tuff or ashstone.|16-MAY-23
21998|Ingalara Ashstone Member|Relationships and boundaries|Overlies white rhyolite and medium to coarse rhyolitic tuff to east; overlain to west by cleaved shale (at base of Rothlyn Formation); member at top of Colinton Volcanics.|16-MAY-23
21998|Ingalara Ashstone Member|Age reasons|Late Silurian, from relationship to fossiliferous sediments in Colinton Volcanics and overlying Rothlyn Formation.|16-MAY-23
21998|Ingalara Ashstone Member|Defn author|G.A.M. Henderson ?1989.|16-MAY-23
21998|Ingalara Ashstone Member|Comments|Although this appears to be an adequate unit definition, no evidence is available to show that this definition went through the Stratigraphy Commission approval process. The original card was supplied  to ASUD manager C. Brown by R. S. Abell, on his departure from BMR, after the publication of BMR Bulletin 233 Geology of the Canberra 1:100 000 sheet.|16-MAY-23
21998|Ingalara Ashstone Member|References|Henderson, G.A.M., 1987. Late Silurian geology of the Michelago-Cooma area: 1:100 000 preliminary edn. map. Bur. Miner. Resour. Aust. **Richardson, S.J., 1979. Geology of the Michelgo 1:100 000 sheet 8726. Geol. Surv. NSW Sydney.|16-MAY-23
24317|Inverary Tonalite|Name source|Inverary Creek, a north flowing tributary which joins Bungonia Creek 4 km NE of Bungonia; GR 724415 - Bungonia 1:25 000 Topographic Sheet (8828-II-N).|16-MAY-23
24317|Inverary Tonalite|Type section locality|An east flowing tributary of Inverary Creek 2 km ESE of Bungonia GR 711380 - Bungonia 1:25 000 Topographic Sheet (8828-II-N).|16-MAY-23
24317|Inverary Tonalite|Extent|The unit extends over 4 km2 as a 0.3 to 1 km wide belt extending from 2 km east of Bungonia to 6 km SSW of Bungonia.|16-MAY-23
24317|Inverary Tonalite|Lithology|Porphyritic tonalite.|16-MAY-23
24317|Inverary Tonalite|Relationships and boundaries|A pluton of the Marulan Batholith (Naylor, 1939). It intrudes the Tangerang Volcanics and the Lumley Adamellite. It is overlain by Tertiary basalt and surficial deposits.|16-MAY-23
24317|Inverary Tonalite|Age reasons|Lower Devonian since it intrudes the Tangerang Volcanics of Lower Devonian age (Carr, Jones & Wright, 1980) and is intruded by the Lower Devonian Lumley Adamellite I.e. between 393 m.y. and 410 m.y.|16-MAY-23
24317|Inverary Tonalite|Proposer|Carr P.F., Jones B.G., Kantsler A.J., Moore P.S., Cook A.C.|16-MAY-23
69820|Inverell Volcanics|Name source|After the town of Inverell (INVERELL 1:100 000 map sheet area).|16-MAY-23
69820|Inverell Volcanics|Type section locality|The type area is nominated at the Inverell lookout (GR 314100mE 6704000mN, MGA94 Zone 56).|16-MAY-23
69820|Inverell Volcanics|Extent|This unit forms part of the Central Province of McDougall and Wilkinson (1967). Outcrop of the Inverell Volcanics is limited to two areas: on the top of a plateau in the Inverell lookout area (GR 314100mE 6704000mN, MGA94 Zone 56) that continues to the west; and the tops of a line of hills striking 030o, 15km east of Delungra.|16-MAY-23
69820|Inverell Volcanics|Thickness range|In the type area the Inverell Volcanics is less than 20m thick. A maximum thickness of approximately 80m is attained to the north of the Copeton Dam Road at GR 308900mE 6705200mN (MGA94 Zone 56).|16-MAY-23
69820|Inverell Volcanics|Lithology|Basanite and weathered volcaniclastic rocks.|16-MAY-23
69820|Inverell Volcanics|Depositional environment|A series of basanite volcanic flows each no more than 5m thick, interbedded with volcaniclastic horizons.|16-MAY-23
69820|Inverell Volcanics|Relationships and boundaries|The Inverell Volcanics conformably overlies the Mount Russell Volcanics.|16-MAY-23
69820|Inverell Volcanics|Age reasons|One sample yielded a K-Ar age of 20Ma (Early Miocene).|16-MAY-23
27165|Ironbong Dacite Member|Name source|Ironbong Trig. Station (GR 5750 7164, Cootamundra 1:250 000).|16-MAY-23
27165|Ironbong Dacite Member|Type section locality|GR 5765 7168 to GR 5742 7161, Cootamundra 1:250 000 sheet.|16-MAY-23
27165|Ironbong Dacite Member|Extent|The unit occurs over an area of about 1 km2, located 6 km southwesterly from Ironbong Trig Station (GR 5750 7163 Cootamundra 1:250 000).|16-MAY-23
27165|Ironbong Dacite Member|Thickness range|Up to 200 m(?)|16-MAY-23
27165|Ironbong Dacite Member|Lithology|Dacite, altered; pyrite common; contains conglomerate beds.|16-MAY-23
27165|Ironbong Dacite Member|Relationships and boundaries|Occurs within and at the top of the Bethungra Formation. Overlain by undifferentiated sequence of siltstone, conglomerate, and sandstone.|16-MAY-23
27165|Ironbong Dacite Member|Age reasons|Early Devonian based on brachiopods found in the Bethungra Formation.|16-MAY-23
27165|Ironbong Dacite Member|Proposed publication|A Metallogenic study of the Cootamundra 1:250 000 sheet.|16-MAY-23
27165|Ironbong Dacite Member|Defn Reference|79/20317|16-MAY-23
8780|Irondale Coal|Name source|Irondale Colliery, Piper's Flat.|16-MAY-23
8780|Irondale Coal|Unit history|Irondale Seam of Branagan (1960) and McElroy (1957).|16-MAY-23
8780|Irondale Coal|Type section locality|(1) Location: Placer Wolgan DDH 2 (231121 m E  1319262 m N Bungleboori 1:50 000 sheet, 8931-11).  (2) Repository: NSW Dept of Mineral Resources, Core Library, Londonderry.|16-MAY-23
8780|Irondale Coal|Extent|A persistent, widespread unit over most of the Western Coalfield - particularly the Lithgow and Bungleboori 1:50 000 sheets.|16-MAY-23
8780|Irondale Coal|General description|A commonly thin (1.3 to 1.4 m) but persistent coal horizon characterised by two or three stone bands giving it a distinctive seam section and density log profile. Coal bands tend to be brighter and thicker at top of unit. The unit is commonly distinguished by a pallid claystone bed at its base, containing root traces (cf Vertebraria). It is subject to rapid lateral facies variations near the basin margin where sandstone bands are locally prominent. In localised areas, also near the basin margin, it may be overlain by a thin, pebbly sandstone unit (the Ivanhoe Sandstone Member of the Newnes Formation) which in places has an erosive base.|16-MAY-23
8780|Irondale Coal|Thickness range|(1) Type section: from 380.75 m to 382.98 m; thickness 2.23 m.  (2) Maximum recorded: 3.5 m.|16-MAY-23
8780|Irondale Coal|Lithology|Coal, mainly bright, claystone, black carbonaceous and also buff.|16-MAY-23
8780|Irondale Coal|Relationships and boundaries|Conformably overlies the Bunnyong Sandstone Member of the Long Swamp Formation. Base of unit recognised by sharp transition to fining down sandstone. Unit overlain by sandstones of the Newnes Formation.|16-MAY-23
8780|Irondale Coal|Proposed publication|Australian Coal Geology|16-MAY-23
8926|Jerilderie Formation|Name source|AOG Jerilderie No. 1 bore, GR 397645 Jerilderie 1:250 000 (SI 55-14).|16-MAY-23
8926|Jerilderie Formation|Unit history|New name (C.S. Bembrick).|16-MAY-23
8926|Jerilderie Formation|Type section locality|1. In A.O.G. Jerilderie No. 1 between 468' (142.7 m) and 1187' (362.3 m).  2. In D.M. Oaklands RDH 5 between 111.13 m (366 ft) and 282.55 m (927 ft). Repository - Department of Mines Core Library, Londonderry.|16-MAY-23
8926|Jerilderie Formation|Extent|Restricted to the subsurface. Unit occurs over an area of approximately 1000 km2 in the southern Oaklands Basin, west of Oaklands, and probably extends northwards along the basin axis.|16-MAY-23
8926|Jerilderie Formation|Thickness range|Range 0-719' (219.15 m).|16-MAY-23
8926|Jerilderie Formation|Lithology|Sandstone, pebbly to conglomeratic, medium to very coarse grained, white to light grey, quartzose, white clay matrix; minor claystone and mudstone; sporadic crossbedding lowermost 50 m (approximately) in D.M. drillholes contains common white claystone beds to 9 m thick. Uppermost 60 m Jerilderie No. 1 in dominantly silty sandstone and mudstone.|16-MAY-23
8926|Jerilderie Formation|Relationships and boundaries|Unit rests with regional angular unconformity on Early and Late Permian sediments, including the Corrabin Coal Measures. It is unconformably overlain by Tertiary sediments of the Renmark Group.|16-MAY-23
8926|Jerilderie Formation|Identifying features|Geoohysical Log Characteristics: The unit has a low, "quiet" log response, which is similar to the overlying Tertiary sands. It has a much more uniform response than the underlying Permian sediments. It displays a moderate Neutron - Neutron log count with a relatively "quiet" response compared to units above and below. The Resistivity log is relatively uniform in response, but shows gradually decreasing resistivity towards the base of the unit. S.P. and Density logs are of uniform response.|16-MAY-23
8926|Jerilderie Formation|Age reasons|Identified by palynology in A.O.G. Jerilderie No. 1 and Urana No. 1 Mid-Triassic - palynological unit Tr 3B of Evans (1966) which is equivalent to the Aratrisporites parvispinosus Assemblage Zone of Helby (1973).|16-MAY-23
8926|Jerilderie Formation|Proposed publication|Records of the Geological Survey of New South Wales Vo. 18(2).|16-MAY-23
8926|Jerilderie Formation|First Reference|79/20208|16-MAY-23
26269|Jolly Nose Conglomerate|Name source|The Jolly Nose Conglomerate was first identified and mapped by Bocking (1977), then formally named and described by Leitch and Bocking (1980). It is named after the Jolly Nose Hill, a prominent peak in the immediate area of the type section.|16-MAY-23
26269|Jolly Nose Conglomerate|Geomorphic expression|The Jolly Nose Conglomerate crops out poorly; most outcrops are moderately to highly weathered.|16-MAY-23
26269|Jolly Nose Conglomerate|Type section locality|Leitch and Bocking (1980) nominated the type section to be on the south side of Jolly Nose Hill between GR 480537 6505540 and GR 480433 6505873 (1:25 000 map sheet 9434-1-N, Grants Head) (locations 79 and 76; all locations are listed in Appendix 1). They also indicated more accessible exposures on the former Pacific Highway (location 20) and at Cowarra quarry (location 21). There was insufficient exposure at the type section to construct a measured section.|16-MAY-23
26269|Jolly Nose Conglomerate|Description at type locality|Leitch and Bocking (1980 p.93) comprehensively described the Jolly Nose Conglomerate. 'Massive and rudaceous rocks dominate the Jolly Nose Conglomerate. These are mainly well rounded cobble conglomerates with an open framework and a coarse quartz sandstone matrix. The unit is characterised by the presence of mainly poorly-indurated quartz sandstone clasts, in contrast with the Laurieton Conglomerate in which most clasts are composed of chert, jasper and vein quartz. Frequently pebbly and sometimes cross-stratified quartz sandstones occur in the Jolly Nose Conglomerate.'|16-MAY-23
26269|Jolly Nose Conglomerate|Extent|The Jolly Nose Conglomerate has a limited extent occurring only in the northeastern part of the Lorne Basin, east of the North Coast Railway line and north of Herons Creek and Queens Lake.|16-MAY-23
26269|Jolly Nose Conglomerate|Thickness range|Leitch and Bocking (1980) estimated a thickness of 100 m for the Jolly Nose Conglomerate at the type section while the author estimates a thickness of over 140 m at a nearby section (locations 38 to 78). However the formation thins rapidly to the northwest, with a total thickness of 5 m at Cowarra Quarry (location 21) and an observed thickness of 2 m and estimated thickness of about 8 m at the former Pacific Highway (location 20).|16-MAY-23
26269|Jolly Nose Conglomerate|Lithology|The author examined about 30 thin sections from the former Pacific Highway location (location 20) where the clasts are least weathered. The clast lithology of the Jolly Nose Conglomerate was found to be very varied, being dominated (about 80%) by lithic and quartzofeldspathic sandstone comparable with those of the Carboniferous Pappinbarra Formation and Mingaletta Formation. Although other lithologies present include granitoids, quartzite and acid volcanic rocks, sources for all clasts can be found in basin floor rocks within the basin perimeter. The more exotic clasts may have been reworked from the Carboniferous conglomerates. This localised provenance is markedly different from the provenance of the Triassic strata higher in the sequence where chert, quartz and jasper dominate. The conglomerates are cobble-rich as shown at the type section (location 79), east of Jolly Nose Hill (location 38), Pacific Park (location 20) and at Cowarra Quarry (location 21).|16-MAY-23
26269|Jolly Nose Conglomerate|Relationships and boundaries|The Jolly Nose Conglomerate is the lowest Triassic formation in the Lorne Basin and, where present, unconformably overlies the Palaeozoic basement rocks, as at location 20 (on the former Pacific Highway), where the formation can be seen directly overlying Palaeozoic serpentinite. In the Jolly Nose Hill area, the formation is overlain by the Laurieton Conglomerate, as at locations 76 and 78 (Photograph 1). Further south, at location 147; and west, as at locations 20 and 21, the formation is overlain by the Coopernook Conglomerate Member of the Camden Head Claystone.|16-MAY-23
26269|Jolly Nose Conglomerate|Identifying features|The Jolly Nose Conglomerate is readily identified by its cobble clast lithology of predominantly (about 80%) lithic and quartzo-feldspathic sandstones and the rarity or absence of quartz, jasper or chert clasts. The formation crops out poorly and immediately overlies the Palaeozoic basin floor.|16-MAY-23
26269|Jolly Nose Conglomerate|Structure and Metamorphism|The formation appears to fill a graben in the eastern floor of the basin and thins rapidly westwards beyond this depression.|16-MAY-23
26269|Jolly Nose Conglomerate|Age reasons|The age of the Jolly Nose Conglomerate is uncertain as no fossils have been recovered from the formation although shelly fossils were recovered from a constituent cobble. Thin section analysis of these fossils indicated that they were bivalves (rather than brachiopods) and of similar shape and size to the bivalves of the `Merismopteria'  horizon in the Late Carboniferous Mingaletta Formation from which it is thought the cobble was derived. The formation is assumed to unconformably overlie the Middle Ordovician to Late Carboniferous Watonga Formation, and is observed to overlie Palaeozoic serpentinite. The formation is overlain, in part, by the Laurieton Conglomerate which is constrained by macroflora to an Early Triassic age. The Jolly Nose Conglomerate is probably Early Triassic or perhaps Late Permian in age.|16-MAY-23
26269|Jolly Nose Conglomerate|Correlations|There are no other units in the Lorne Basin that can be correlated with the Jolly Nose Conglomerate.|16-MAY-23
24324|Kadoona Dacite Member|Name source|Kadoona Homestead GR 383361.|16-MAY-23
24324|Kadoona Dacite Member|Unit history|Probably equal to the Bombay Volcanics in the Braidwood 1:100 000 sheet.|16-MAY-23
24324|Kadoona Dacite Member|Type section locality|Outcrops in the grassy field at GR 392373.|16-MAY-23
24324|Kadoona Dacite Member|Extent|Narrow fault blocks along the Shoalhaven River south of Gundillion and larger areas near Gundillion, Cleatmore Caves, Moodong and north of Mt Elrington where it extends onto the Braidwood 1:100 000 sheet area.|16-MAY-23
24324|Kadoona Dacite Member|Lithology|Porphyritic dacite variably altered by low grade burial metamorphism. The freshest samples came from the type locality, and apart from degree of alteration are typical of much of the unit. Here the rock is grey-green and contains about 60% phenocrysts in a fine structureless groundmass of possibly devitrified glass. Plagioclase (An50-60) is the dominant phenocryst followed by, in order of abundance, quartz, orthopyroxene, clinopyroxene, biotite, hornblende, magnetite, allanite, apatite and zircon. Quartz is most commonly the largest phenocryst and is up to 5 mm across.|16-MAY-23
24324|Kadoona Dacite Member|Age reasons|Late Silurian or possibly Early Devonian as it overlies the De Drack Formation and underlies the Toggannoggra Rhyolite Member.|16-MAY-23
24324|Kadoona Dacite Member|Resdate|21-JUN-1982|16-MAY-23
24325|Kadungle Volcanics|Name source|Township Kadungle (GR 5661 9488 Narromine 1:250 000 sheet).|16-MAY-23
24325|Kadungle Volcanics|Type section locality|Near Kadungle GR 569950 (whole section).|16-MAY-23
24325|Kadungle Volcanics|Extent|The unit is exposed around Trundle in the southern central part of the Narromine 1:250 000 sheet.|16-MAY-23
24325|Kadungle Volcanics|Thickness range|Range 100-700 m.|16-MAY-23
24325|Kadungle Volcanics|Lithology|Dacite, tuff, shale and sandstone.|16-MAY-23
24325|Kadungle Volcanics|Relationships and boundaries|Overlies the Derriwong Group and underlies silicified marls and limestone of the Trundle Group. The unit is deeply weathered.|16-MAY-23
24325|Kadungle Volcanics|Age reasons|Thought to be Early Devonian from age dating of the Derriwong Group and Tarundle Group by Sherwin 1979 (unpubl.)|16-MAY-23
24325|Kadungle Volcanics|Proposer|Sherwin L.|16-MAY-23
24325|Kadungle Volcanics|Reserved? Yes/No|Yes|16-MAY-23
24328|Kalimna Limestone Member|Name source|The name derives from the property of Kalimna (GR 737812*), some 1.5 km north-west of the type locality.(Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978)).|16-MAY-23
24328|Kalimna Limestone Member|Unit history|Originally referred to informally as the 'lower coral' unit (Webby 1969).|16-MAY-23
24328|Kalimna Limestone Member|Type section locality|Type section on Fossil Hill (GR 752812*) (Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978)).|16-MAY-23
24328|Kalimna Limestone Member|Description at type locality|There is a relatively sharp contact in the section between topmost Gleesons Limestone Member (beds with large-shelled Eodinobolus) and the basal Kalimna Limestone Member (a 320 mm thick siltstone). The succeeding 7.5 m of sequence is thin bedded, and composed of skeletal wackestones and packstones with silty interbeds. A thin bed containing large Eodinobolus shells forms the top of this sequence, and is succeeded directly by distinctive 1.2 m thick coral/algal/stromatoporoid biostrome. The top of the Kalimna Limestone Member is taken 0.75 m above the biostrome at a significant lithological change from grey brown skeletal wackestones with abundant corals to greenish brown, volcaniclastic, fine sandstones of the overlying Wyoming Limestone Member.|16-MAY-23
24328|Kalimna Limestone Member|Thickness range|In the type section the Kalimna Limestone Member is 9 m thick.|16-MAY-23
24328|Kalimna Limestone Member|Identifying features|The Kalimna Limestone Member has been mapped as an independent unit throughtout the Cliefden Caves area, distinguished across less well-exposed ground by the prominence and continuity in its beds of large colonies of Tetradium cribriforme.|16-MAY-23
24328|Kalimna Limestone Member|Proposer|Webby B.D., Packham G.H.|16-MAY-23
24328|Kalimna Limestone Member|Resdate|12-MAY-1981|16-MAY-23
24328|Kalimna Limestone Member|Reserved? Yes/No|Central Register, BMR, Canberra (Ref. 80/1569)|16-MAY-23
25970|Khan Yunis Formation|Name source|Khan Yunis property, GR 382279, Araluen.|16-MAY-23
25970|Khan Yunis Formation|Unit history|The name was first used by Johnson (1964, M.Sc. Thesis ANU) but the only published use of the name was by McIlveen (1975, Rec. geol. Survey NSW 16(3) p.268) who briefly mentioned it without description.|16-MAY-23
25970|Khan Yunis Formation|Type section locality|To the southeast of Khan Yunis homestead from GR 400245 (base) to 382245 (top). Outcrop along the section is only fair, however the unit as a whole forms poor outcrop. About 500 m of sediment is present in the type section.|16-MAY-23
25970|Khan Yunis Formation|Extent|In a meridional belt some 17 km long and up to 2 km wide on the western side of the Shoalhaven valley from the southern edge of the Araluen sheet. A small area is present in the north of the Cobargo sheet.|16-MAY-23
25970|Khan Yunis Formation|Thickness range|A maximum of 550 m.|16-MAY-23
25970|Khan Yunis Formation|Lithology|Interbedded yellowish-brown to reddish-brown medium to coarse arenite, reddish-brown siltstone and red shale. Conglomeratic and pebbly arenite horizons fairly common. Cross-bedding is common. Beds organised into fining-upwards cycles typical of fluviatile environments.|16-MAY-23
25970|Khan Yunis Formation|Relationships and boundaries|The unit rests conformably, with gradational contact, on the Deua Formation. The top of the unit is everywhere a faulted contact against the Devonian Jinden Granite and the Silurian Long Flat Volcanics.|16-MAY-23
25970|Khan Yunis Formation|Age reasons|A rich fish fauna is known from one locality near the base of the Khan Yunis Formation. It indicates a Fammenian (Late Devonian) age for the unit.|16-MAY-23
25970|Khan Yunis Formation|Defn author|Wyborn D., Owen M., 1986|16-MAY-23
25970|Khan Yunis Formation|Proposed publication|BMR map commentary - Araluen 1:100 000 Sheet.|16-MAY-23
25970|Khan Yunis Formation|Reserved? Yes/No|Yes|16-MAY-23
24337|Kingsland Conglomerate Member|Name source|Kingsland homestead 2 km north of the type section.|16-MAY-23
24337|Kingsland Conglomerate Member|Type section locality|Road cutting on the upper Horton-Narrabri road at GR 345766 Eulowrie 8937-1-N. 40 m of conglomerate, sandstone and minor siltstone in an otherwise mudstone sequence.|16-MAY-23
24337|Kingsland Conglomerate Member|Extent|The unit is distribuated over a distance of 25 km from the NE corner of the Horton 1:100 000 geological series (McKelvey & White 1964) and the E margin of the Bangheet 1:100 000  series (McKelvey, 1968).|16-MAY-23
24337|Kingsland Conglomerate Member|Thickness range|Range 40-60 m.|16-MAY-23
24337|Kingsland Conglomerate Member|Lithology|Orthoconglomerate, sandstone, siltstone and pebbly mudstone with minor lithographic limestone and mudstone.|16-MAY-23
24337|Kingsland Conglomerate Member|Relationships and boundaries|Lies within the Mandowa Mudstone - previously this conglomerate was referred to the Keepit Conglomerate by McKelvey & White (1964) and McKelvey (1968). The upper contact is at the highest coarse sandstone, conglomerate or pebbly mudstone. The lower contact is defined in a similar manner but may have an abrupt as well as gradational lower contact.|16-MAY-23
24337|Kingsland Conglomerate Member|Age reasons|Siphonodella duplicata, an early Tournaisian conodont species is present in a limestone boulder 6.5 m below the top of the type section. Siphonodella sp. Is also present 20 cm below this unit 3 km SW of the type section on the southern side of the Horton Road. No other macro or microfauna is known from this unit.|16-MAY-23
24337|Kingsland Conglomerate Member|Comments|Remarks: This conglomerate has been renamed for the following reasons:  1) The underlying Eungai Mudstone cannot be lithologically distinguished from the overlying Mandowa Mudstone (and is hence placed into synonomy with the Mandowa).  2) There is a significant age difference between the Keepit Conglomerate (latae Devonian) and the newly named Kingsland Conglomerate (early Carboniferous) as well as lack of outcrop of both conglomerate units between Burindi and Horton (a distance of 47 km).|16-MAY-23
24337|Kingsland Conglomerate Member|Proposer|Mory, Arthur J.|16-MAY-23
24337|Kingsland Conglomerate Member|Reserved? Yes/No|Yes|16-MAY-23
27175|Kohinoor Volcanics|Name source|Named after Kohinoor Trig. Station on the Michelago 1:100 000 sheet area (Richardson 1979).|16-MAY-23
27175|Kohinoor Volcanics|Unit history|None.|16-MAY-23
27175|Kohinoor Volcanics|Type section locality|The mine workings at Captains Flat (Michelago 1:100 000 sheet 8728) where the Kohinoor Volcanics have been studied in detail (Glasson and Paine, 1965, Davis 1975 and Richardson, 1979). The formation acts as a host for base metal mineralisation in the Captains Flat Graben.|16-MAY-23
27175|Kohinoor Volcanics|Extent|The volcanics are well developed south of Captains Flat in the Michelago 1:100 000 sheet area (Richardson 1979).  The formation is poorly exposed on the Canberra 1:100 000 sheet where it appears to lens out northwards in to the medial portion of the Captains Flat Graben. The Kohinoor Volcanics have not been recognised along the western margin of the the Captains Flat Graben.|16-MAY-23
27175|Kohinoor Volcanics|Thickness range|Glasson and Paine (1965) give a maximum thickness of about 1300m in the Captains Flat area. Oldershaw (1965) gives 800m in the same area. The volcanics thin northwards and Wilson (1964) gives 300m east of Hoskinstown.|16-MAY-23
27175|Kohinoor Volcanics|Lithology|Dacitic to rhyodacite ignimbrite and lava with minor breccia, chert and shale ("Keatings Shale Member").|16-MAY-23
27175|Kohinoor Volcanics|Depositional environment|Subaerial south of Captains Flat becoming shallow marine northwards to Hoskinstown where the volcanics are brecciated and interbedded with the shale.|16-MAY-23
27175|Kohinoor Volcanics|Relationships and boundaries|The Kohinoor Volcanics appear to overlie the Copper Creek Shale conformably.  The upper boundary is complex. The volcanics are overlain by the Carwoola Formation on the Canberra 1:100 000 sheet but southwards are apparently conformable with the Captains Flat Formation on the Michelago 1:100 000 sheet.|16-MAY-23
27175|Kohinoor Volcanics|Age reasons|Unfossiliferous.  Probably Ludlow (Talent and other 1975) based on its stratigraphic position relative to the Copper Creek Shale.|16-MAY-23
27175|Kohinoor Volcanics|Correlations|Woodlawn Volcanics (Huleatt 1971) and Colinton Volcanics (Richardson 1979).|16-MAY-23
24342|Koonburra Creek Quartzite Member|Name source|Koonburra Creek, a south flowing tributary of Prospectors Creek, which is present south of Woolshed Tank (see Grassmere 7435, First Ed. 1:100 000 orthomap Series).|16-MAY-23
24342|Koonburra Creek Quartzite Member|Type section locality|Is made 2 km west of Mt Daubeny Outstation at GR 5719 1577 (1:250 000 Wilcannia).|16-MAY-23
24342|Koonburra Creek Quartzite Member|Extent|The member extends northwestwards for 12 km from Prospectors Creek (Wilson, 1967).|16-MAY-23
24342|Koonburra Creek Quartzite Member|Thickness range|It is thickest, 75 m, 500 m NW of the intersection of the member and Koonburra Creek. Elsewhere it ranges from 14-36 m, generally thinning northwards.|16-MAY-23
24342|Koonburra Creek Quartzite Member|Lithology|The member, fine grained, is composed of uniform, fine grained planar cross bedded quartzite containing very rare clasts of vein quartz.|16-MAY-23
24342|Koonburra Creek Quartzite Member|Relationships and boundaries|It is unconformable on Wonaminta Beds and is overlain by medium and coarse red coloured arenite.|16-MAY-23
24342|Koonburra Creek Quartzite Member|Age reasons|The member lacks fossils and is considered to be somewhat older (perhaps only 1 m.y.) than the Baragwanathia Flora Fossils present in Gnalta Creek.|16-MAY-23
24342|Koonburra Creek Quartzite Member|Proposer|Neef G., Edwards A.C., Bottrill R.S., Holzberger I., Kelly R., Hatty J., Vaughan J.|16-MAY-23
24342|Koonburra Creek Quartzite Member|Reserved? Yes/No|Yes|16-MAY-23
37902|Kooringal Dacite Member|Name source|The property `Kooringal' on Boomi Creek GR426571 Horton 1:25,000 sheet|16-MAY-23
37902|Kooringal Dacite Member|Unit history|Kooringal Andesite (Opdyke et al. 2000).  Name was first used informally by Hocking (1973).|16-MAY-23
37902|Kooringal Dacite Member|Type section locality|On the banks of Boomi Creek at GR380565 Horton 1:25,000 sheet.|16-MAY-23
37902|Kooringal Dacite Member|Extent|Crops out over a length of 2 km on the western limb of the Maules Creek Anticline north and south of Boomi Creek.|16-MAY-23
37902|Kooringal Dacite Member|Thickness range|50m|16-MAY-23
37902|Kooringal Dacite Member|Lithology|Dark grey dacitic ignimbrite containing elongate feldspar (largely plagioclase), biotite and opaque minerals. The groundmass is vitric and contains traces of shards and bubble walls.|16-MAY-23
37902|Kooringal Dacite Member|Depositional environment|Ignimbrite|16-MAY-23
37902|Kooringal Dacite Member|Relationships and boundaries|Trace element abundances are similar to those in the Barney Springs Andesite (Wang 1999).|16-MAY-23
37902|Kooringal Dacite Member|Age reasons|Carboniferous (Visean)|16-MAY-23
37902|Kooringal Dacite Member|References|HOCKING R.M. 1973. The Carboniferous Back Creek-Pound Creek sequence, southwest of Caroda, New South Wales. BSc (Hons) thesis, University of new England, Armidale (unpubl.).OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.WANG X. 1999. Carboniferous volcanic rocks of the Rocky Creek region, northern Tamworth Belt, Southern New England Orogen. PhD thesis, University of New South Wales, Sydney (unpubl.).|16-MAY-23
24343|Koreelah Conglomerate Member|Name source|The name is derived from the small settlement of old Koreelah in north-eastern NSW (GR MP 435.585 Warwick 1:100 000 Sheet).|16-MAY-23
24343|Koreelah Conglomerate Member|Unit history|The Koreelah Conglomerate Member has been previously included in either the Marburg 'Formation' or the Laytons Range Conglomerate.|16-MAY-23
24343|Koreelah Conglomerate Member|Geomorphic expression|Mostly poorly exposed in low mounds or in road cuttings.|16-MAY-23
24343|Koreelah Conglomerate Member|Type section locality|The type section lies in an area about 10 km to the southwest of Warwick along the New England Highway, at GR LP 978.702, on the Allora 1:100 0000 Sheet. There are no continuous complete sections of the Koreelah Conglomerate Member and the best outcrops are those along road cuttings on the New England and Bruxner Highways. The base of the Member in the type section is present in outliers and at the basin margin east and southeast of the Leslie Hall Dam such as outcrops at LP 963.784 and outcrops on the Cunningham Highway 15-17 km west of Warwick. The top of the member grades into the Gatton Sandstone between the exposures on the New England Highway and a quarry in the Gatton Sandstone at MP 002.708.|16-MAY-23
24343|Koreelah Conglomerate Member|Description at type locality|The member is composed of conglomerate, sandstone, siltstone and shale. Pebble to cobble conglomerate is the dominant lithology in most outcrops but the relative proportion of rock types varies considerably from one outcrop to another. The predominantly clast supported conglomerate is polymict with mostly subrounded and a few angular and rounded clasts mostly in the range 3-5 cm across, and a maximum of 16 cm, composed of predominantly mudstone metasediments, with subordinate black chert, felsic volcanics, fine grained sandstone, slatey metasediaments and reef quartz in a matrix of coarse grained sandstone containing fresh angular feldspar grains. The conglomerate is both matrix anda clast supported, has poorly defined bedding, including trough crossbeds, and in a few places the clasts show a slight imbrication. Fine and coarse grained lithic and feldspathic sandstone occurs as interbeds of variable thickness. Red and grey siltstone is interbedded in some of the conglomerate exposures. In places the mudstone encloses lenses of conglomerate and coarse grained sandstone up to 2 to 3 m thick.|16-MAY-23
24343|Koreelah Conglomerate Member|Extent|The member is found chiefly in narrow strips along the western and parts of the southern margin of the Clarence Moreton Basin. The Koreelah Conglomerate Member is distributed along the western and southern margins of the basin on the Cunningham and New England Highways, west and south of Warwick, on the Bruxner Highway west of Tabulam, Gwydir Highway west of Main Creek and probably also on the Pacific Highway at the Dirty Creek Range.  The known maximum exposed thickness is about 20-30 m in the area west of Tabulam on the Bruxner Highway.|16-MAY-23
24343|Koreelah Conglomerate Member|General description|The proportion of conglomerate, sandstone, and fine grained rocks varies from locality to locality and in places shales and fine sandstones are present in the sequence. Ferruginised and siliceous fossil wood, logs and fragments are common. The formation typically occurs as a pebble-cobble conglomerate, with abundant coarse sandstone interbeds and a similar sandy matrix. The lithology of the clasts in the conglomerate is controlled largely by the composition of the underlying basement. The known maximum exposed thickness is about 20-30 m in the area west of Tabulam on the Bruxner Highway.|16-MAY-23
24343|Koreelah Conglomerate Member|Thickness range|Only incomplete sections are present in outcrop and about 20-30 m on the Bruxner Highway (GR 470.030 Drake 1:100 000 Sheet) is the maximum known exposed thickness. About 5 m of conglomerate penetrated in GSQ Ipswich RM2 at Leyburn probably equates with the Koreelah Conglomerate Member.  The true thickness is probably much greater but exposure is discontinuous.|16-MAY-23
24343|Koreelah Conglomerate Member|Depositional environment|Probably deposited as a series of alluvial fans and braided stream deposits along the western and southern margins of the Clarence Moreton Basin.|16-MAY-23
24343|Koreelah Conglomerate Member|Fossils|The member has no internal evidence for depositional age. Superposition and lateral relationships indicate that the member has approximately the same age as the Early Jurassic Gatton Sandstone of the Marburg Subgroup.|16-MAY-23
24343|Koreelah Conglomerate Member|Diastems or hiatuses|Evidence for minor hiatusus and diastems is present.|16-MAY-23
24343|Koreelah Conglomerate Member|Relationships and boundaries|The member unconformably overlies Palaeozoic and Early Triassic basement rocks, and is inferred to overlie Late Triassic sediments of the Bundamba Group. The member occurs at the local base of the Marburg Sub-group and is interpreted to grade laterally into the Gatton Sandstone, and doubtfully into the Heifer Creek Sandstone of the Marburg Sub-group. Precise boundaries are not readily defined due to lateral and vertical facies transitions. Lateral and vertical boundaries may be defined by the last significant beds of pebble conglomerate in the unit. Contacts are rarely observed and are typically gradational.|16-MAY-23
24343|Koreelah Conglomerate Member|Identifying features|The combination of pebble-cobble conglomerate and coarse grained arenitic assemblage in the member distinguishes it from the bulk of the basin sequence. The Late Triassic basal conglomerates of the basin (Laytons Range, Corindi and Aberdare Conglomerates) are superficially similar to the Koreelah Conglomerate Member; however there is usually a higher proportion of sandstone interbedded in the Koreelah Conglomerate Member, and it is distinguished in many places by the abundance of fossil wood. The sandstone interbeds are lithologically similar to those of the Gatton Sandstone. It is not always easy to distinguish the basal Late Triassic conglomerates from those in the Early Jurassic, and in some instances a demonstration of lateral transition to the Marburg Subgroup is the surest way of distinguishing the two.|16-MAY-23
24343|Koreelah Conglomerate Member|Structure and Metamorphism|The Koreelah Conglomerate Member generally dips at low angles into the basin.|16-MAY-23
24343|Koreelah Conglomerate Member|Correlations|There are no units that can be correlated lithologically and temporally with the Koreelah Conglomerate Member. The Koreelah Conglomerate Member is laterally continuous with the Gatton Sandstone of the Marburg Subgroup.|16-MAY-23
24343|Koreelah Conglomerate Member|Proposed publication|Wells A.T. et al. BMR Journal of Geology and Geophysics|16-MAY-23
24343|Koreelah Conglomerate Member|Comments|Discussion:  The evidence for the existence of the younger conglomerate and the reasons for proposing a new member name may be summarised as follows. (1) The conglomerate occurs in the exposed base of the Marburg Subgroup along the western and southern margins of the basin. In this area the Subgroup ovelaps the older formations in the basin and unconformably overlies Palaeozoic and Early Triassic basement rocks.  (2) The Marburg Subgroup shows evidence of general coarsening towards the basin margin and the proportion and thickness of conglomerate interbeds increase towards the margin.  (3) The clast composition is noticeably different in some areas to that found in the Laytons Range, Aberdare, and Corindi Conglomerates, and fossil wood commonly constitutes a large percentage of these clasts.  (4) The sandstone interbeds found in the conglomerate are similar in composition to those found in the Marburg Subgroup.  (5) The basal conglomerate member is apparently continuous with the Marburg Subgroup; no unconformity is apparent between the Marburg Subgroup and the conglomerate member which would be expected if an overlapping relationship existed.  (6) The suggested identification of the conglomerate present locally at the base of the Marburg Subgroup in contact with the Raceview Formation in the southeast provides additional evidence for the age and stratigraphic position of the member.|16-MAY-23
24343|Koreelah Conglomerate Member|Resdate|01-MAR-1988|16-MAY-23
24343|Koreelah Conglomerate Member|State(s)|NSW and Qld|16-MAY-23
9979|Kyndalyn Mudstone Member|Name source|'Kyndalyn' property at Babbinboon; GR 569639, Somerton 1:31 680 Sheet area.|16-MAY-23
9979|Kyndalyn Mudstone Member|Type section locality|170 m of interbedded mudstone, siltstone and minor lithic sandstone from 591594 (bottom) to 595595 (top of section), Winton 1:31 680 Sheet. The base is gradational with the underlying terrestrial Merlewood Formation, but at the top there is an abrupt change from marine mudstone to pink lithic sandstone and conglomerate.|16-MAY-23
9979|Kyndalyn Mudstone Member|Extent|The member is exposed over 5 km2 around 'Kyndalyn' and on either side of the Werrie Syncline, outcropping for about 12 km on the eastern limb and 7 km on the western limb.|16-MAY-23
9979|Kyndalyn Mudstone Member|Thickness range|Range 0-170 m.|16-MAY-23
9979|Kyndalyn Mudstone Member|Lithology|Mudstone, siltstone and minor lithic sandstone, all of which are buff to brownish green in colour. The silty beds contain a rich marine invertebrate fauna. The member contains interbedded oolitic and bioclastic limestone up to 30 m in thickness north and west of the type section, and contains or is represented by oolitic limestone conglomerate and polymictic conglomerate up to 60 m thick south and west of the type section.|16-MAY-23
9979|Kyndalyn Mudstone Member|Relationships and boundaries|Gradational contact with underlying terrestrial sediments but an abrupt change, probably a disconformity, with the overlying lithic sandstone and conglomerate of the Merlewood Formation.|16-MAY-23
9979|Kyndalyn Mudstone Member|Age reasons|Late Visean. See Roberts, J., 1975. Early Carboniferous Brachiopod Zones of Eastern Australia. J. geol. Soc. Aust., 22, 1-32.|16-MAY-23
9979|Kyndalyn Mudstone Member|Proposed publication|Royal Society of NSW|16-MAY-23
9979|Kyndalyn Mudstone Member|Comments|Notes: The Kyndalyn Member represents a marine transgression into the essentially terrestrial Merlewood Formation. The member is diverse lithologically and consists of beach (oolitic limestone conglomerate), bank (oolitic and bioclastic limestone) and offshore sediments (mudstone and siltstone). The Hill 60 Member of Voisey and Williams (1964) comprises one of the bioclastic limestones within the Kyndalyn Member, and should be relegated to a lower status.|16-MAY-23
9979|Kyndalyn Mudstone Member|References|01/31622; 01/31623; 01/31624|16-MAY-23
25142|Kyogle Basalt|Name source|Kyogle' township; GR 003335, Nimbin 1:50 000 Sheet 9540-IV.|16-MAY-23
25142|Kyogle Basalt|Unit history|McElroy (1962) included these rocks in the Lismore Basalt.|16-MAY-23
25142|Kyogle Basalt|Type section locality|On east side of Hermits Peak from 010452 (base) to 000459 (top). Some 330 m of alkaline volcanics. The Homeleigh Agglomerate Member occurs 60 m above the base of the section. The base is not exposed in the type section, but is exposed nearby at a similar elevation. The top is identified by the sudden predominance of tholeiitic lavas which constitute the base of the overlying Lismore Basalt.|16-MAY-23
25142|Kyogle Basalt|Extent|The unit is exposed over an area of 1500 km2 mainly to the east of Kyogle comprising most of the Nimbin (9540-IV) and Rosebank (9540-I) 1:50 000 sheets.|16-MAY-23
25142|Kyogle Basalt|Thickness range|Range <50 m up to 330 m. Thins eastward and south-eastward. East and south of Nimbin the thickness rarely exceeds 100 m.|16-MAY-23
25142|Kyogle Basalt|Lithology|Predominantly hawaiite with minor alkali olivine basalt and basanite and rare tholeiitic volcanics. Many hawaiites, especially those near the base of the sequence, approach mugearite in composition. Groundmass mineraloids impart a greenish colour to hand specimens.|16-MAY-23
25142|Kyogle Basalt|Relationships and boundaries|Unconformably overlies the Mesozoic sediments of the Clarence-Moreton Basin. Relief on the Mesozoic basement varies from 0 to 250 m. New basal "formation" of Lamington Volcanics (Gp). Overlain by the predominantly tholeiitic lavas of the Lismore Basalt.|16-MAY-23
25142|Kyogle Basalt|Age reasons|No age data available. However, K-Ar ages reported by Wellman and McDougall (1974) indicate an age range 23-20 m.y. for the Lamington Volcanics as a whole and, more specifically, about 22.5 m.y. for the Albert Basalt which may correlate with the Kyogle Basalt.|16-MAY-23
25142|Kyogle Basalt|Defn author|Duggan M.B., Mason D.R., 1978.|16-MAY-23
25142|Kyogle Basalt|Proposed publication|Journal of the Geological Society of Australia|16-MAY-23
25142|Kyogle Basalt|Comments|Notes: The name Kyogle Basalt was first used but not defined by Duggan and Wilkinson (1973). Petrologically similar to and may correlate with the Albert Basalt in south-eastern Queensland (McTaggart 1962).|16-MAY-23
25142|Kyogle Basalt|Reserved? Yes/No|Yes|16-MAY-23
24349|Kyong Formation|Name source|From Kyong Tank, GR 59851063 Gairdners Tank 1:25 000 sheet.|16-MAY-23
24349|Kyong Formation|Unit history|Previously regarded as undifferentiated Willyama Supergroup.|16-MAY-23
24349|Kyong Formation|Type section locality|Designated between GRs 5945 1059 (base) and 59201050 (top), Gairdners Tank 1:25 000 sheet area. Comprises approximately 850 m of psammitic to pelitic metasediments with abundant persistant beds and some lenses of leucocratic quartzofeldspathic gneiss, and very minor beds of ferruginous quartz rock and basic gneiss. The base is defined by a body of laterally persistent, very thick quartzofeldspathic gneiss (Alma Gneiss), and the top by a persistent body of quartzofeldspathic gneiss (Rasp Ridge Gneiss).|16-MAY-23
24349|Kyong Formation|Extent|Widely distributed in the central Euriowie Block, and particularly in the Gairdners Tank 1:25 000 sheet area.|16-MAY-23
24349|Kyong Formation|Thickness range|Ranges between 180 m and 860 m.|16-MAY-23
24349|Kyong Formation|Lithology|Comprises psammitic to pelitic metasediments with various amounts (but greater than 10%) of quartzofeldspathic gneisses as an essential component. The quartzofeldspathic gneisses include leucocratic and biotite rich varieties, and sillimanite- and feldspar megacryst-bearing types. Minor beds of basic gneiss, stratiform, granular feruginous and cupriferous quartz rock, garnet quartz rock, and poorly layered calc-silicate rock occur sparsely throughout.|16-MAY-23
24349|Kyong Formation|Relationships and boundaries|The base is defined by a broad interval of metasediment in sharp contact with a persistent body of quartzofeldspathic gneiss (Alma Gneiss). The top is defined by a sharp contact with a laterally persistant body of quartzofeldspathic gneiss in excess of 70 m thick (Rasp Ridge Gneiss), or by an interval rich in leucocratic plagioclase-quartz rocks (Himalaya Formation). Is laterally transitional to metasediment rich Cues Formation in places, and is locally underlain by same. Locally interfingers with Alma Gneiss and Broken Hill Group. Is locally vertically transitional to Allandale Metasediments.|16-MAY-23
24349|Kyong Formation|Age reasons|Structurally and lithologically part of the Willyama Supergroup of Early Proterozoic age, approximately 1820 Ma (Shaw 1968).|16-MAY-23
24349|Kyong Formation|Proposed publication|NSWGS Quarterly Note and NSWGS Record.|16-MAY-23
24349|Kyong Formation|Comments|NOTE: All stratigraphic names used above are after Willis et al., 1983.|16-MAY-23
27457|Lake Bathurst Limestone Member|Name source|Lake Bathurst township, GR 417217, Braidwood 1:100 000 sheet.|16-MAY-23
27457|Lake Bathurst Limestone Member|Unit history|Philip and Pedder (1968) referred informally to the "Lake Bathurst Limestone". Pogson (1972) also used the name but did not define the unit.|16-MAY-23
27457|Lake Bathurst Limestone Member|Type section locality|In Bongaralaby Creek between GR 408216 and GR 408217, Braidwood 1:100 000 Sheet.|16-MAY-23
27457|Lake Bathurst Limestone Member|Extent|Discontinuous outcrops occur in a north-trending belt west of Tarago and Lake Bathurst townships. The most southerly outcrop occurs at GR 410141, the most northerly at GR 415222 (both GR's refer to Braidwood 1:100 000 sheet).|16-MAY-23
27457|Lake Bathurst Limestone Member|Thickness range|In any one outcrop, 80 m maximum.|16-MAY-23
27457|Lake Bathurst Limestone Member|Lithology|Mainly light to dark grey micrite and biomicrite. A coarse pinkish-grey bioclastic sparite was noted in one outcrop. Only texturally compact limestones are included in the Lake Bathurst Limestone Member: associated calcareous sediments are regarded as belonging to the Bongalaby Formation (Felton and Huleatt, 1975).|16-MAY-23
27457|Lake Bathurst Limestone Member|Relationships and boundaries|One or more discontinuous limestone horizons occur within the Bongalaby Formation. As noted above, only texturally compact limestones are included in the unit as defined here: this is the principal criterion for identifying the unit.|16-MAY-23
27457|Lake Bathurst Limestone Member|Age reasons|The Lake Bathurst Limestone Member contains Gephuropora duni Etheridge; Chalcidophyllum sp. Polygnathus linguiformis foreolata Philip and Jackson; Neoprioniodus bicurvatus (Brahnson and Mehl); Ozarkodina cf. Jaegeri Walliser (Philip, 1966); Spathognathodus linearis (Philip). See Philip and Pedder, 1968. An Emsian age is indicated.|16-MAY-23
10073|Lake Victoria Sand|Name source|Formation named after Lake & 3 members after the 3 stations where the lunette occurs.|16-MAY-23
10073|Lake Victoria Sand|Unit history|Not previously named.|16-MAY-23
10073|Lake Victoria Sand|Type section locality|E. shore Lake Victoria.  Location of Type Section: Nulla/Talgarry fence longitude 141o21'E, latitude 34o1'S.|16-MAY-23
10073|Lake Victoria Sand|Extent|Down E. shore on L. Victoria (c. 9 mile). Extends 1-1.5 ml inland.|16-MAY-23
10073|Lake Victoria Sand|Thickness range|a) At type section: 120 ft.  B) Maximum known: 145 ft.|16-MAY-23
10073|Lake Victoria Sand|Lithology|Fine dune sand with some clay.|16-MAY-23
10073|Lake Victoria Sand|Fossils|Dunedin Park - no fossils, Talgarry Sand - living spp. Marsupials and reptiles, Nulla Sand - extinct giant marsupials. List provided by paper by L Marshall in Mem. 34.|16-MAY-23
10073|Lake Victoria Sand|Relationships and boundaries|The three members are superposed and comprise the whole dune system which overlies Blanchetown and onlaps Rufus Alluvium relicts.|16-MAY-23
10073|Lake Victoria Sand|Age reasons|C14 and marsupial fossils.|16-MAY-23
10073|Lake Victoria Sand|Comments|Defined as Lake Victoria Sand.  1. Dunedin Park Sand Member  2. Talgarry Sand with 3 members.  3. Nulla Sand Member (reserved and published as Nulla Nulla Sand Member)|16-MAY-23
10073|Lake Victoria Sand|Defn approved by|Copied from xerox sent by NSW Stratigraphic Nomenclature Committee.|16-MAY-23
25987|Lambs Valley Ignimbrite Member|Name source|Lambs Valley Creek (Singleton 44809752).|16-MAY-23
25987|Lambs Valley Ignimbrite Member|Unit history|Subdivision of the Gilmore Volcanics Group.|16-MAY-23
25987|Lambs Valley Ignimbrite Member|Type section locality|Lambs Valley. Location of Type Section: Singleton 44829752. From the Lambs Valley Creek west along the Lambs Valley Creek Road.|16-MAY-23
25987|Lambs Valley Ignimbrite Member|Extent|Forms a band in the vicinity of Peterson-Vacy, Lambs Valley and Kealeys Bight.|16-MAY-23
25987|Lambs Valley Ignimbrite Member|Thickness range|a) At type section: 40 m.  B) Maximum known:|16-MAY-23
25987|Lambs Valley Ignimbrite Member|Lithology|Basal, white, porphyritic, dellenitic, tuff; overlain by a purple porphyritic dellenitic tuff. The upper tuff weathers to a lime green colour.|16-MAY-23
25987|Lambs Valley Ignimbrite Member|Relationships and boundaries|Overlies the Newton Formation conformably and is overlain disconformably by the Mount Johnstone Formation. Within the Mowbray Formation.|16-MAY-23
25987|Lambs Valley Ignimbrite Member|Age reasons|Lower Westphalian from correlations based on Campbell and McKelvey.|16-MAY-23
25987|Lambs Valley Ignimbrite Member|Defn approved by|Copied from xerox sent by NSW Stratigraphic Nomenclature Committee|16-MAY-23
25987|Lambs Valley Ignimbrite Member|Reserved? Yes/No|Grahame Hamilton|16-MAY-23
25988|Lanes Shaft Coal Member|Name source|Lane's Shaft; sunk by T.J. Lane, in his property, for water (1916); coal was discovered at a depth of 67 m; GR DA 294706, Buraja 1:100 0000.|16-MAY-23
25988|Lanes Shaft Coal Member|Type section locality|13.97 m thick coal seam with sharp, erosive top and base; the coal grades into a mudstone dark brown to black, towards base; occurs in bore D.M. Coorabin R.D.H. 2 (GR DA 266567) Buraja 1:100 000 from 69.42 m to 83.39 m.|16-MAY-23
25988|Lanes Shaft Coal Member|Extent|The unit occurs only in the subsurface. Its subcrop extends over 570 km2 in the central portion of the Jerilderie 1:250 000 sheet, and probably further north.|16-MAY-23
25988|Lanes Shaft Coal Member|Thickness range|3.50 m to 19.00 m.|16-MAY-23
25988|Lanes Shaft Coal Member|Lithology|Coal dull, very uniform; common fusain lenses; clayey in part; two claystone buff to grey, possibly tuffaceous bands, a few centimetres thick occur in upper half of unit; one mudstone band, buff to grey, possibly tuffaceous, 0.91 m thick, in lower half of unit; coal becomes very clayey towards base, where it grades into mudstone or claystone, dark brown to black, carbonaceous.|16-MAY-23
25988|Lanes Shaft Coal Member|Relationships and boundaries|Top part of the Narrow Plain Formation (Palese and Morgan, in prep.); it conformably overlies claystones and sandstones of the Formation. The base is defined by the gradational change from coal to carbonaceous mudstone or claystone. It is unconformably overlain by the Loughmore Formation (Palese and Morgan, in prep.).|16-MAY-23
25988|Lanes Shaft Coal Member|Age reasons|Impressions of Vertebraria and Glossopteris are common on the coal bedding planes. The microflora, as identified in the thin claystone buff bands, consists mainly of Luekisporites and Parasaccites. Elements such as Didecitriletes ericianus, Marsupipollensis sinuosus and Dulhuntyispora dulhuntyi, identify the Lower Stage 5 microflora of Late Permian age (? Roadian).|16-MAY-23
25988|Lanes Shaft Coal Member|First Reference|79/20208|16-MAY-23
10240|Laurieton Conglomerate|Name source|Town of Laurieton 31deg39' 00.71"S, 152deg47' 53.44"E. The Laurieton Conglomerate was noted by Carne (1897) and Voisey (1939) and formally named by Pratt and Herbert (1973) after Laurieton, the nearest town to the major outcrops.|16-MAY-23
10240|Laurieton Conglomerate|Name source|Laurieton Trig 910835 Camden Haven 1:63 360.|16-MAY-23
10240|Laurieton Conglomerate|Geomorphic expression|The Laurieton Conglomerate is a resistant, cliff-forming unit well-exposed along the coast between Camden Head and Grants Head and on the eastern and southern sides of Jolly Nose Hill.|16-MAY-23
10240|Laurieton Conglomerate|Type section locality|Grants Head - Bonny Hills.  Location of Type Section: Grants Head-Bonny Hills 915895 Camden Haven 1:63 360.|16-MAY-23
10240|Laurieton Conglomerate|Type section locality|Grants Head from 31.61034deg S, 152.84715deg E to 31.59803deg S, 152.84719deg E. Pratt and Herbert (1973) nominated the exposure at Grants Head as the type section for the Laurieton Conglomerate. A precise location at Grants Head, between GR 485501 6503744 (1:25 000 map sheet 9434-1-N, Grants Head, location 90, Photograph 4), and GR 485504 6504108 (1:25 000 map sheet), 9434-1-N, Grants Head, location 31) is now specified as the location of the type section. This is a complete and unbroken section with exposures of both the base and the top of the formation. The base of the formation is exposed at the foot of the cliff at GR 485501 6503744 (location 90). The section then offsets along the bed to GR 485567 6503949 (location 117) from where the section continues up-dip along the rock platform to the base of the overlying Grants Head Formation at GR 485504 6504108 (location 31, Photograph 5). A lithology plot of the Laurieton Conglomerate measured section is presented in Figure 12.|16-MAY-23
10240|Laurieton Conglomerate|Description at type locality|The type section for the conglomerate is exposed in cliffs and then along the rock platform on the northern side of Grants Head. Pratt and Herbert's (1973) original description has been revised to: the Laurieton Conglomerate is dominated by reddish to grey, poorly to moderately sorted pebble to cobble conglomerate usually with very thick (>100 cm) beds, as exposed on the southern side of Grants Head (location 342); (Photograph 6). Pebble and minor granule conglomerate and sandstone interbeds are uncommon and beds of reddish purple mudstone are absent. The subrounded to subangular clasts are predominantly chert with lesser jasper and quartz. The fabric is clast-supported and the matrix is poorly sorted sandstone to claystone. Bedding is generally very thick with some minor thick-bedded strata.|16-MAY-23
10240|Laurieton Conglomerate|Extent|The Laurieton Conglomerate is developed as isolated headlands around the northeastern perimeter of the Lorne Basin, as well as an upfolded exposure at the Jolly Nose Hill.|16-MAY-23
10240|Laurieton Conglomerate|Extent|Crops out around basin perimeter in the east of the basin and around Jolly Nose Hill, also in the east.|16-MAY-23
10240|Laurieton Conglomerate|General description|While the type section description for the Laurieton Conglomerate is consistent with most other exposures, at Little Grants Head, 800 m southwest of the type section, there is a distinct decrease in clast size with pebble and granule conglomerate dominating. There is also a change in the relative proportions of quartz to jasper clasts, although jasper clasts still predominate over quartz clasts, a characteristic of the Laurieton Conglomerate.|16-MAY-23
10240|Laurieton Conglomerate|Thickness range|At the type section the Laurieton Conglomerate is almost 47 m thick. There is an observed thickness of approximately 60 m at Jolly Nose Trigonometric Station but at that location the top of the unit is not exposed and hence the true thickness is greater.|16-MAY-23
10240|Laurieton Conglomerate|Lithology|Pebble to cobble conglomerate with minor granule conglomerate, sandstone and red-brown claystone.|16-MAY-23
10240|Laurieton Conglomerate|Lithology|At the type section, jasper clasts comprise 33% and quartz clasts 20% of the total clasts and 12 cobbles per 0.5 m × 0.5m square, while the average of 15 samples (100 pebbles each) throughout the basin was jasper 30% and quartz 20% of total clasts and 6 cobbles per 0.5 m × 0.5 m square. Jasper clasts usually comprise >25% of total clasts while quartz clasts are usually <25% and there are usually more than 3 cobbles per 0.5 × 0.5 m square. Table 3 presents the jasper and quartz clast percentages of total clasts measured at 11 locations. The significant proportion of chert and jasper clasts is typical of the New England Orogen provenance and is also typical of the Triassic strata in the Gunnedah Basin (Digby Conglomerate) and northern Sydney Basin (Munmorah Conglomerate).|16-MAY-23
10240|Laurieton Conglomerate|Depositional environment|For the Laurieton Conglomerate the very thick bedding, crude cross stratification, clast-supported framework; poor to moderate sorting, and the subrounded to subangular clasts and their pebble to cobble size, indicate rapid deposition in a high-energy environment from a source of abundant supply. These features would suggest deposition in the main channel areas of a braided stream subject to periods of major flooding. Parisotto (1989, p.116) noted that sheetflood deposits and braided streams are most common in the mid-alluvial fan region. He concluded that 'the Laurieton Conglomerate was deposited in a mid-alluvial fan environment that was relatively flat and dominated by water-laid deposits, in particular those by sheetfloods'.|16-MAY-23
10240|Laurieton Conglomerate|Relationships and boundaries|Of Camden Haven Group. Overlies and in part laterally equivalent to the Camden Head Claystone. In some areas rests unconformably on Palaeozoic basement. Overlain by the Grants Head Formation.|16-MAY-23
10240|Laurieton Conglomerate|Relationships and boundaries|Of the Camden Haven Group (Packham, 1969). The Laurieton Conglomerate overlies the Camden Head Claystone with an erosive contact. However, in the Jolly Nose Hill area, the Camden Head Claystone and Coopernook Conglomerate Member are (locally) absent and there the Laurieton Conglomerate overlies the Jolly Nose Conglomerate (Map 1 and Figure 2). Poorly developed bedding in both units and their coarse cobble grainsize rendered the nature of the contact indeterrminate, but it is presumed to be paraconformable. The Laurieton Conglomerate is conformably overlain by the Grants Head Formation. The basal boundary of the Laurieton Conglomerate is the contact between the chert-jasper and quartz cobble and pebble conglomerate of the Laurieton Conglomerate and the reddish purple mudstone of the underlying Camden Head Claystone or, in the immediate vicinity of Jolly Nose Hill, the lithofeldspathic sandstone cobble conglomerate of the Jolly Nose Conglomerate. The top of the formation is the top of the uppermost bed of chert-jasper-quartz pebble conglomerate underlying the pebbly sandstone of the Grants Head Formation.|16-MAY-23
10240|Laurieton Conglomerate|Identifying features|The distinguishing features of the Laurieton Conglomerate are the abundant cobbles, poor sorting and dominantly very thick (>100 cm) beds. Jasper clasts usually constitute >30% and quartz clasts usually <25%. There are generally more than 5 cobbles per 0.5 m × 0.5 m square. Beds of reddish purple mudstone are absent. The formation crops out strongly; is often cliff-forming; and is characterised by the very thick beds of the dominating conglomerate so well exposed in the coastal cliffs and at Jolly Nose Hill.|16-MAY-23
10240|Laurieton Conglomerate|Structure and Metamorphism|The Laurieton Conglomerate has been folded into north-south-trending open folds with a final basinward dip from the westernmost anticline (Map 1 and Figure 2).|16-MAY-23
10240|Laurieton Conglomerate|Age reasons|Lower Triassic - age data from surrounding formations.|16-MAY-23
10240|Laurieton Conglomerate|Age reasons|Although fossils have not been recovered from the Laurieton Conglomerate, palynological samples from the Camden Head Claystone, 9 m below the Laurieton Conglomerate and from the Grants Head Formation at Bartletts Beach, 63 m above the Laurieton Conglomerate (location 104) place the formation in a transitional zone between the underlying Protohaploxypinus samoilovichii Assemblage and the Aratrisporites tenuispinosus Assemblage (Helby 1970, 1971, 1972). These floras are found in the Terrigal Formation, and underlying Clifton Subgroup, of the Sydney Basin and suggest an upper Early Triassic age for the Laurieton Conglomerate.|16-MAY-23
10240|Laurieton Conglomerate|Correlations|Pratt and Herbert (1973) considered the Laurieton Conglomerate to include the conglomerates of the Lansdowne Escarpment, Mount Comboyne and Broken Bago Range. However, those conglomerates are shown herein to be the Coopernook Conglomerate Member of the Camden Head Claystone. The conglomerates overlying the Camden Head Claystone are sufficiently different from the Laurieton Conglomerate to warrant their description as a separate new formation, the Coorabakh Conglomerate, albeit laterally equivalent to the former.|16-MAY-23
10240|Laurieton Conglomerate|Defn author|W. Pratt, 7-JUL-2010.|16-MAY-23
10240|Laurieton Conglomerate|Proposed publication|Record of Geological Survey NSW.|16-MAY-23
10240|Laurieton Conglomerate|Comments|Described.|16-MAY-23
10240|Laurieton Conglomerate|Comments|Redefined to precisely locate type section and to slightly modify the lithology description.|16-MAY-23
10240|Laurieton Conglomerate|References|Carne J.E. 1897. Report on the geology and mineral resources of the coast between Port Macquarie and Cape Hawke. New South Wales Department of Mines Annual Report for 1896. **Helby R.J. 1970. Plant microfloras from the Lorne Basin. Geological Survey of New South Wales, Palynology Report 1970/07. **Helby R.J. 1971. Review of Late Permian and Triassic palynology of New South Wales. Geological Survey of New South Wales Palynology Report 1971/06. Geological Survey of New South Wales, Report GS 1971/595. **Helby (1972) GS NSW Report Palynology 1972/3.  **Helby R.J. 1973. Review of Late Permian and Triassic palynology of New South Wales. Geological Society of Australia Special Publication 4, pp. 141-155. **Packham G.H. 1969. The New England region. Triassic System, pp. 270-271. In: Packham G.H. ed. The Geology of New South Wales. Journal of the Geological Society of Australia. 16 (1), 1-654. **Parisotto D.F. 1989. Appreciation of the geology in the southwest margin of the Lorne Basin. Field Project (62360), University of Technology, Sydney. (unpublished). **Pratt, G.W. 2010. A revised Triassic stratigraphy for the Lorne Basin, NSW. Quarterly Notes of the Geological Survey of New South Wales 126. **Pratt G.W. & Herbert C. 1973. A reappraisal of the Lorne Triassic Basin. Geological Survey of New South.Wales, Records 15, 205-212. **Voisey A.H. 1939. The Lorne Triassic Basin and associated rocks. Proceedings of the Linnean Society of New South Wales 64, 225-265.|16-MAY-23
10240|Laurieton Conglomerate|Defn approved by|Copied from xerox sent by NSW Stratigraphic Nomenclature Committee.|16-MAY-23
10268|Lawsons Gully Porphyry|Name source|Named after deep lead in township of Grenfell GR 619810, Forbes 1:250 0000.|16-MAY-23
10268|Lawsons Gully Porphyry|Type section locality|Hospital Hill, Grenfell (GR 619810).|16-MAY-23
10268|Lawsons Gully Porphyry|Extent|Crops out for 3 km in a north-south belt about 500 m wide immediately east of Grenfell.|16-MAY-23
10268|Lawsons Gully Porphyry|Lithology|Quartz-feldspar porphyry.|16-MAY-23
10268|Lawsons Gully Porphyry|Relationships and boundaries|Intrusive dyke (?) into Late Ordovician sediments. Intruded by the Early Devonian Grenfell Granite.|16-MAY-23
10268|Lawsons Gully Porphyry|Age reasons|Probably Early Devonian because of stratigraphic evidence.|16-MAY-23
10268|Lawsons Gully Porphyry|Name first published by|Borman H.N., 1977.|16-MAY-23
10280|Leard Formation|Name source|Leard State Forest, approximately 20 km north east of Boggabri, NSW.|16-MAY-23
10280|Leard Formation|Unit history|Relationship to Nandewar Group (Hanlon, 1949) not clear, owing to lack of specific record. The distinctive lithology was first explicitly recorded by Loughnan (1975). The present name was used informally and fully described (Brownlow, 1976 and 1977).|16-MAY-23
10280|Leard Formation|Type section locality|Between 460.93 m and 469.56 m in DM Maules Creek DDH 5 (GR 315 214 y on the Manilla 1:250 000 sheet).  Core Repository: Department of Mineral Resources Core Library, Londonderry, NSW).|16-MAY-23
10280|Leard Formation|Extent|In outcrops and in numerous drill holes between the Boggabri Ridge and Mooki Fault System.|16-MAY-23
10280|Leard Formation|Thickness range|Approximately 8.63 m in DM Maules Creek DDH 5. In outcrop and other bores it is generally thinner.|16-MAY-23
10280|Leard Formation|Relationships and boundaries|Overlies irregular, eroded and in part deeply weathered surfaces on the Boggabri Volcanics and Werrie Basalt. The upper boundary is taken at the lowermost occurrence of lithic sediments which constitute the overlying Maules Creek Formation.|16-MAY-23
10280|Leard Formation|Age reasons|Early Permian  Lower Stage 4 (Morgan, 1976b).|16-MAY-23
10280|Leard Formation|Proposed publication|Australian Coal Geology|16-MAY-23
10280|Leard Formation|References|?01/31625; 79/02627|16-MAY-23
10383|Lidsdale Coal|Name source|Village of Lidsdale, Western Coalfield|16-MAY-23
10383|Lidsdale Coal|Unit history|Taylor (1954), McElroy (1957), Branagan (1960). Not previously defined.|16-MAY-23
10383|Lidsdale Coal|Type section locality|(1) Location: Austen & Butta Hartley Valley DDH3 (224552.4E, 1291973.ON Lithgow 1:50 000 Sheet 8931-111).  (2) Repository: Dept of Mineral Resources Core Library, Londonderry.|16-MAY-23
10383|Lidsdale Coal|Extent|Generally restricted to the western margin of the Western Coalfield - Lithgow and parts of Hampton 1:50 000 sheets.|16-MAY-23
10383|Lidsdale Coal|Thickness range|(1) Type section: From 242.13 m to 243.99 m; thickness, 1.86 m.  (2) Maximum recorded: 5 m.|16-MAY-23
10383|Lidsdale Coal|Lithology|Dull coal, carbonaceous claystone, mudstone, ?oil shale.|16-MAY-23
10383|Lidsdale Coal|Relationships and boundaries|Conformably overlain by the Long Swamp Formation and underlain by the Blackmans Flat Conglomerate. Where the latter unit is absent, the lateral equivalents of the Lidsdale Coal are included with the Lithgow Coal. Top of unit marked by transition from coal or carbonaceous sediments to a dark grey mudstone, commonly laminated. Base recognised by transition from coal to sandstone and minor argillaceous sediments of the Blackmans Flat Conglomerate. The term is synonymous with Lidsdale Seam (Taylor, 1954), Lidsdale Seam (McElroy, 1957) and Lidsdale Seam (Branagan, 1960). Part of Cullen Bullen Sub-Group.|16-MAY-23
10383|Lidsdale Coal|Proposed publication|Australian Coal Geology|16-MAY-23
10455|Lismore Basalt|Name source|'Lismore' city; GR 268129, Lismore 1:50 000 sheet 9540-II.|16-MAY-23
10455|Lismore Basalt|Type section locality|Road section 3 km northeast of Nimbin from 254383 (base) to 256389 (top). 115 m of mafic lavas, predominantly tholeiitic andesites.|16-MAY-23
10455|Lismore Basalt|Extent|The unit is exposed over an area of 3000 km2 within a radius of 25 km of Lismore.|16-MAY-23
10455|Lismore Basalt|Thickness range|Range 50-150 m.|16-MAY-23
10455|Lismore Basalt|Lithology|Mafic lava flows, mainly transitional to tholeiitic but some alkaline variants. Tholeiitic types typically grey-black in hand specimen compared to the more greenish alkaline rocks of the underlying Kyogle Basalt.|16-MAY-23
10455|Lismore Basalt|Relationships and boundaries|Belongs to Lamington Volcanics (Gp). Overlies the Kyogle Basalt. Rests unconformably on Mesozoic and Palaeozoic basement in eastern areas where the Kyogle Basalt is absent. Where overlying the Kyogle Basalt the contact may be transitional. It is marked by a change from the alkaline basaltic rocks of the Kyogle Basalt to the more subalkaline (or transitional to tholeiitic) rocks of the Lismore Basalt.|16-MAY-23
10455|Lismore Basalt|Age reasons|No radiometric agaes are available for a rocks in the southern portion of the Tweed Shield Volcano. The Lamington Volcanics as a whole have been dated at 23-20 m.y. by K-Ar methods (Wellman and McDougall, 1974, and reference therein).|16-MAY-23
10470|Lithgow Coal|Name source|Town of Lithgow, Western Coalfield|16-MAY-23
10470|Lithgow Coal|Unit history|Carne (1908) Branagan (1960). Not previously defined.|16-MAY-23
10470|Lithgow Coal|Type section locality|(a) Location: Austen & Butta Hartley Valley DDH3 (224552.4E 1291973.0 N. Lithgow 1:50 000 sheet, 8931-111).  (2) Repository: Dept Mineral Resources Core Library, Londonderry.* (*Browns Gap, GR 158600, Hampton 8930 - IV).|16-MAY-23
10470|Lithgow Coal|Extent|Generally well developed and persistent in most of the Western Coalfield, but particularly along strike close to the western margin. Occurs on Lithgow, Bungleboori, parts of Hampton, Katoomba, Glen Davies and Glen Alice sheets.|16-MAY-23
10470|Lithgow Coal|General description|Part of Cullen Blullen Sub-Group. Stratigraphic equivalents recognised in the South Western Coalfield (Kooloo "Seam"), Southern Coalfield (Woonona) and Singleton area (Bayswater). Top of unit recognised by a change from coal and carbonaceous claystone to either sandstone and conglomerate of the Blackmans Flat Conglomerate or dark grey/mudstone of the Long Swamp Formation. Base of unit marked by transition from coal or carbonaceous claystone to sandstone, conglomerate and minor mudstone of the Marrangaroo Conglomerate. This term is synonymous with Lithgow Seam - Carne (1908) and most subsequent authors, including Branagan (1960).|16-MAY-23
10470|Lithgow Coal|Thickness range|(1) Type section: From 247.53 m to 250.12 m; thickness, 2.59 m.  (2) Maximum recorded: 9 m.|16-MAY-23
10470|Lithgow Coal|Lithology|Dull coal, carbonaceous claystone; minor mudstone, claystone, sandstone.|16-MAY-23
10470|Lithgow Coal|Relationships and boundaries|Conformably overlain by the Long Swamp Formation or, near the western margin, by the Blackmans Flat Conglomerate.|16-MAY-23
10470|Lithgow Coal|Proposed publication|Australian Coal Geology|16-MAY-23
10470|Lithgow Coal|References|01/31626|16-MAY-23
29940|Little Bay Shale|Name source|Little Bay, c. 2.5 km north of Cape Banks at the entrance to Botany Bay, GR 338500 6238600, Sydney 1:100 000 sheet; 33o58'50"S, 151o15'6"E.|16-MAY-23
29940|Little Bay Shale|Type section locality|DMR Little Bay DDH5, University of NSW campus, Little Bay, for precise location see Figure 1. Core is stored in the Core Library of the New South Wales Department of Mineral Resources, Londonderry, NSW.|16-MAY-23
29940|Little Bay Shale|Extent|Confined to part of Miocene palaeovalley; proved extent 350 m x 150 m; probable extent up to 1.5 km x 150 m.|16-MAY-23
29940|Little Bay Shale|Thickness range|Maximum known thickness is 27 m in DDH5.|16-MAY-23
29940|Little Bay Shale|Lithology|Chiefly pale buff to grey unconsolidated shale, plastic when wet, separating along bedding when dry, with sandy horizons, peat layers and horizonts with fossil leaves.|16-MAY-23
29940|Little Bay Shale|Relationships and boundaries|The base is unconformable on Triassic Hawkesbury Sandstone; the top most units are eroded.|16-MAY-23
29940|Little Bay Shale|Age reasons|Mid to Late Miocene; Triporopollenites bellus Zone.|16-MAY-23
29940|Little Bay Shale|Defn approved by|Approved by Chris Fergusson & Helena Basden|16-MAY-23
10511|Livingstone Porphyry|Name source|Livingstone trig. Station (932 m) at GR 943424 Michelago 1:100 000 Geological Sheet.|16-MAY-23
10511|Livingstone Porphyry|Unit history|Brown (1928), Sharp (1949) and Joplin et al. (1953) all described but did not name the porphyry.|16-MAY-23
10511|Livingstone Porphyry|Type section locality|Typical outcrop at GR 943424|16-MAY-23
10511|Livingstone Porphyry|Description at type locality|Greenish-grey colour; dacitic composition, containing quartz, plagioclase (oligoclase/andesite), biotite, apatite, sphene and alkali feldspar set in a matrix of plagioclase, quartz, alkali feldspar, chlorite and sericite plus granular epidote. Some xenoliths, fine-grained rhyodacitic composition. The porphyry ;may contain large xenocrysts of pink orthoclase feldspar up to 30 mm in length and present in a frequency of roughly 1 to 230 cm2. Minor aplites and alaskite are associated with the porphyry.|16-MAY-23
10511|Livingstone Porphyry|Extent|Extends in a narrow belt from north of Michelago to Colinton over 19 km. Main area of outcrop between the Murrumbidgee River and the Monaro Highway, although minor separated masses are found to the west of the river. Size: 19.5 km2.|16-MAY-23
10511|Livingstone Porphyry|Relationships and boundaries|The porphyry is a sill-like intrusive mass with its boundaries showing a crude parallelism to the eastern boundary of the Murrumbidgee Batholith. The porphyry intrudes the Colinton Volcanics and the Bransby Beds.|16-MAY-23
10511|Livingstone Porphyry|Age reasons|Late Silurian to Early Devonian as it intrudes the Late Silurian Colinton Volcanics.|16-MAY-23
10511|Livingstone Porphyry|Proposed publication|Geological Survey of NSW 1:100 000 Note Series.|16-MAY-23
10511|Livingstone Porphyry|References|01/31627|16-MAY-23
10608|Londonderry Clay|Name source|Village of Londonderry (GR 725398, Windsor 1:63 360).|16-MAY-23
10608|Londonderry Clay|Unit history|Included by Walker and Hawkins (1957) in the Londonderry Formation. Bell (1966) included the unit as part of his Windsor Formation.|16-MAY-23
10608|Londonderry Clay|Type section locality|5 m of mottled red-grey moderately to highly plastic clay. Sand "pockets" and iron cemented sand-clay aggregates occur throughout with abundant ironstone pisolites. Type section exposed in PGH Ceramics clay pit (GR 712438, Windsor 1:63 360).|16-MAY-23
10608|Londonderry Clay|Extent|Continuous clay sheet exposed over 140 km2 between Cranebrook and Windsor in the Cumberland Basin.|16-MAY-23
10608|Londonderry Clay|Thickness range|Range 1-9 m.|16-MAY-23
10608|Londonderry Clay|Lithology|Moderately to highly plastic clay, sand, ironstone pisolites, and aggregates of sand and clay.|16-MAY-23
10608|Londonderry Clay|Relationships and boundaries|Gradational boundary between underlying Rickabys Creek Gravel and Londonderry Clay. Top of unit defined by hard, semi-indurated zone of cemented ironstone pisolites.|16-MAY-23
10608|Londonderry Clay|Age reasons|No floral or faunal assemblages available for dating. The Londonderry Clay has been lateritised during a period of duricrusting thought to be Late Miocene or Early Pliocene in age (Gobert in press). The Londonderry Clay overlies Rickabys Creek Gravel, thought to be Miocene in age. Hence a Miocene age is suggested also for the Londonderry Clay.|16-MAY-23
10608|Londonderry Clay|Proposed publication|Gobert, Val, _______. Cumberland Basin Stratigraphy in The geology of the Penrich 1:100 000 sheet, by C. Herbert. Geol. Survey of NSW, Sydney (in press).|16-MAY-23
10619|Long Flat Volcanics|Name source|"Long Flat" property, GR 431604, Araluen 1:100 000 sheet.|16-MAY-23
10619|Long Flat Volcanics|Unit history|Anderson (1893) briefly described the "Long Flat Porphyry". Kennedy (1961) used the term "Manar Group" for the unit and divided it into four subunits (only one of which occurs on the Braidwood sheet. The term "Long Flat Volcanics" was used informally by Johnson (1964) to describe a sequence of volcanic rocks in the vicinity of Krawaree (GR 266577, Canberra 1:250 000 sheet).|16-MAY-23
10619|Long Flat Volcanics|Type section locality|The Long Flat Volcanics are exposed at intervals along the Boro-Bunnerong road between GR 447058 and GR 479032 (Braidwood 1:100 000 sheet). Outcrops in creeks are very weathered and are seen to be strongly cleaved, with phenocrysts of quartz standing out from a fine groundmass on the weathered surfaces. In areas of higher relief near GR 479032 fresh specimens of dark grey green porphyritic dacite and dacitic tuff can be obtained from outcrops above the left bank of Boro Creek.|16-MAY-23
10619|Long Flat Volcanics|Extent|The main part of the unit crops out over an area of 550 km2, between Boro (GR 424078, Braidwood 1:100 000 sheet) in the north and Kain (GR 324423, Araluen 1:100 000 sheet) in the south. Discontinuous outcrops continue south for about 10 km.|16-MAY-23
10619|Long Flat Volcanics|Thickness range|Not known; of the order of 2000 m.|16-MAY-23
10619|Long Flat Volcanics|Lithology|Porphyritic dacite and dacitic tuff; minor rhyolite.|16-MAY-23
10619|Long Flat Volcanics|Relationships and boundaries|The eastern margin of the Long Flat Volcanics is an intrusive contact with the Early Devonian Braidwood Granite. In the west the unit is faulted against the Bombay Volcanics and, further north, against the Boro Granite. The relationship of the unit with adjacent Silurian sediments is obscure, but the two sequences may be partly time-equivalent. The Bombay and Long Flat Volcanics have similar petrographic characteristics but are distinguished in the field by differences in weathering behaviour. The Long Flat Volcanics form a mature, low-relief topography which includes the Shoalhaven River flood-plain west of Braidwood (GR 540740). By contrast, the Bombay Volcanics occupy a range of deeply dissected hills of maximum relief 200 metres.|16-MAY-23
10619|Long Flat Volcanics|Age reasons|As indicated above, the relationship of the unit with the Silurian sediments (De Drack Formation of Middle to Late Silurian age) is obscure. The unit is no younger than mid-Early Devonian (the age of the Braidwood Granite). It is probably Middle to Late Silurian in age.|16-MAY-23
10619|Long Flat Volcanics|Defn author|Wyborn D., Owen M., 1986|16-MAY-23
10619|Long Flat Volcanics|Proposed publication|Felton E.A. and Huleatt M.B., 1975. Geology of the Braidwood 1:100 000 sheet. Geol. Survey NSW, Sydney.|16-MAY-23
10619|Long Flat Volcanics|Comments|Note: The term is proposed for use in the same sense as "Beds" due to insufficient knowledge of the sequence at this stage.|16-MAY-23
10619|Long Flat Volcanics|References|01/31628; GOLD1671|16-MAY-23
10619|Long Flat Volcanics|Proposer|Name used formally on Canberra 1:250 0000 geological sheet (2nd edn) (Best et al. 1964); not defined.|16-MAY-23
27292|Long Swamp Creek Formation|Name source|After Long Swamp Creek, which flows into the upper Shoalhaven River at GR 397283, Araluen 1:100 000 sheet.|16-MAY-23
27292|Long Swamp Creek Formation|Unit history|The name was previously used by Johnson (1964) in an unpublished ANU M.Sc. thesis.|16-MAY-23
27292|Long Swamp Creek Formation|Type section locality|On east bank of Shoalhaven River from GR 404265 (base) to GR 401263 (top). About 100 m of interbedded shale and lithic arenite exposed.|16-MAY-23
27292|Long Swamp Creek Formation|Extent|Extensive outcrops on the Minmurra Range, east of Shoalhaven River from Wyanbene to southern edge of Araluen Sheet.|16-MAY-23
27292|Long Swamp Creek Formation|General description|Generally bioturbated. Several fining downward sandstone units. Sporadic acritarchs. Some flaser bedding. Sporadic "dropstones". Contains the "Bunnyong Sandstone" of Branagan (1960) at or near the top. Base of unit marked by transition from dark grey, commonly laminated, mudstone to coal, carbonaceous shale or sandstone of the Cullen Bullen Sub-Group.|16-MAY-23
27292|Long Swamp Creek Formation|Thickness range|Varies from 50 m in south to 150 m locally to north.|16-MAY-23
27292|Long Swamp Creek Formation|Lithology|Typically interbedded grey-brown mudstone and shale with lithic (at times feldspathic) quartz arenite. Rare red siltstone in south. Proportion of arenite to shale increases upwards through the unit.|16-MAY-23
27292|Long Swamp Creek Formation|Relationships and boundaries|The Long Swamp Creek Formation rests conformably on the Gundillion Conglomerate, the contact being taken at the top of the highest conglomerate or pebbly arenite. It is overlain conformably, though with a sharp contact, by the Curmulee Conglomerate, or, when the Curmulee Conglomerate is absent, by the Deua Formation. The unit passes laterally to the north, about the latitude of Gundillion, into well bedded sandstone with only minor shale of the Big Hole Formation.|16-MAY-23
27292|Long Swamp Creek Formation|Age reasons|The only fauna so far found are poorly preserved brachiopods from GR 421286, Araluen sheet, which cannot be identified. The age, from relationships with other units in the area, is considered to be Late Devonian.|16-MAY-23
27292|Long Swamp Creek Formation|Defn author|Wyborn D., Owen M., 1986|16-MAY-23
27292|Long Swamp Creek Formation|Proposed publication|BMR Map Commentary - Araluen 1:100 000 Sheet|16-MAY-23
27292|Long Swamp Creek Formation|Proposer|Owen M.|16-MAY-23
27292|Long Swamp Creek Formation|Resdate|18-APR-1981|16-MAY-23
27292|Long Swamp Creek Formation|Reserved? Yes/No|Yes|16-MAY-23
25692|Looney Intrusive Complex|Name source|Looney trig. Station in Parish Fitzroy, County Kennedy.|16-MAY-23
25692|Looney Intrusive Complex|Type section locality|Ben Hur mine GR 55789495, Narromine 1:250 000|16-MAY-23
25692|Looney Intrusive Complex|Extent|An area 8 km west of Kadungle. Size: Approximately 1 km wide.|16-MAY-23
25692|Looney Intrusive Complex|Lithology|Hornblende metadiorite, hornblende metasyenite.|16-MAY-23
25692|Looney Intrusive Complex|Relationships and boundaries|Probably intrudes Cambro-Ordovician Girilambone Group.|16-MAY-23
25692|Looney Intrusive Complex|Age reasons|Probable Early Devonian, because of similarity with Tout Complex which has been dated using radioisotopes.|16-MAY-23
25692|Looney Intrusive Complex|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982.,|16-MAY-23
25692|Looney Intrusive Complex|Proposed publication|A metallogenic study of the Narromine 1:250 000 sheet.|16-MAY-23
25692|Looney Intrusive Complex|Defn Reference|86/25274 Defined p.326.|16-MAY-23
25692|Looney Intrusive Complex|Proposer|Bowman H., Richardson S., Dolanski J.|16-MAY-23
25692|Looney Intrusive Complex|Reserved? Yes/No|YES|16-MAY-23
27183|Loughmore Formation|Name source|"Loughmore" property, 4 km south of D.M. Oaklands R.D.H. 1 (GR DA 096599), Buraja 1:100 0000 sheet, in which the formation was first identified.|16-MAY-23
27183|Loughmore Formation|Type section locality|8.59 m thick sequence, consisting of sandstones and mudstones interbedded, and a coal seam at the top. The top of the formation identifies with the top of the coal seam. Its sharp and erosive base consists generally of sandstone and/or conglomerate. Found in D.M. Oaklands R.D.H. 1 from 193.34 m to 201.93 m.|16-MAY-23
27183|Loughmore Formation|Extent|The formation occurs only in the subsurface. Its subcrop extends over about 500 km2 in the central portion of the Jerilderie 1:250 0000 sheet (SI 55-14) and probably further north.|16-MAY-23
27183|Loughmore Formation|Thickness range|Range 7 m to 18 m.|16-MAY-23
27183|Loughmore Formation|Lithology|Coal dull, clayey, at the top of the formation. Sandstone generally well cemented, medium, light grey, micaceous; abundant coaly lamellae and laminae; abundant mudstone, mid grey and brown, micaceous, carbonaceous interbeds. Conglomerate, consisting of white quartz, well rounded pebbles, occurs at base of sequence.|16-MAY-23
27183|Loughmore Formation|Relationships and boundaries|The formation unconformably overlies the Narrow Plain Formation (Palese and Morgan, in prep.); unconformably overlain by the Nowranie Creek Formation (Palese and Morgan, in prep.). It includes the Coreen Creek Coal Member (Palese and Morgan, in prep.) at top.|16-MAY-23
27183|Loughmore Formation|Age reasons|Plant remains are very scarse and unidentifiable. The microflora is dominated by bisaccate grains, especially of Luekisporites. Palynomorphs include Marsupipollenites triradiatus, M. scutatus, Dulhunryispora parvithola, Didecitriletes uncinatus, D. ericianus, Granulatisporites trisinus, G. micronodosus, Indospora clara, Parasaccites, Luekisporites limpidus, L. amplus, Perotriletes spp. Acritarchs include Peltacystia venosa, P. monile, Circulisporites, Quadrisporites horridus, and Tetraporina sp. The Microflora is assigned to Upper Stage 5 of Paten (1969), which identifies the Upper Permian age (Guadalupian).|16-MAY-23
27183|Loughmore Formation|Proposed publication|Records of the Geological Survey of NSW|16-MAY-23
27183|Loughmore Formation|Comments|Notes: Core of the mentioned bores is preserved in the NSW Dept of Mines Core Library in Londonderry, near Penrith. The coal seam was destroyed for sampling purposes and the resulting analyses are available in the bore log (GS 1974/090).|16-MAY-23
27183|Loughmore Formation|First Reference|79/20208|16-MAY-23
27183|Loughmore Formation|Proposer|Palease G.W.|16-MAY-23
10687|Lovetts Formation|Name source|Refer I. Gemuts.|16-MAY-23
10687|Lovetts Formation|Unit history|Name first proposed in unpubl. BSc. Hons. Thesis by D. Dunnett and I. Gemuts, Sydney Univ. 1961. Synonomy with Kildrummie & Campbells Groups, on Bathurst 1:250 000 sheet.|16-MAY-23
10687|Lovetts Formation|Type section locality|Burraga. Location of Type section: Not defined.|16-MAY-23
10687|Lovetts Formation|Extent|Around Burraga.|16-MAY-23
10687|Lovetts Formation|Thickness range|a) At type section: not known.  B) Maximum known:|16-MAY-23
10687|Lovetts Formation|Lithology|Greenish slates, dark brown subgreywackes, quartz feldspar porphyry and tuffs.|16-MAY-23
10687|Lovetts Formation|Relationships and boundaries|Base is top of Buckburraga Slates. Top is undefined.|16-MAY-23
10687|Lovetts Formation|Age reasons|Stratigraphic position.|16-MAY-23
10687|Lovetts Formation|Proposed publication|"The Geology of the Burraga Copper Mine" in Records of the Geological Survey of NSW|16-MAY-23
10687|Lovetts Formation|Defn approved by|Approved. Copies from Xerox sent by NSW Stratigraphic Nomenclature Sub-Committee.|16-MAY-23
10687|Lovetts Formation|Name first published by|Bowman N.H., 1975.|16-MAY-23
10687|Lovetts Formation|Reserved? Yes/No|Reserved by I. Gemuts|16-MAY-23
26011|Manna Conglomerate|Name source|Parish of Manna, County Gipps.|16-MAY-23
26011|Manna Conglomerate|Unit history|The unit was named "Womboyne Conglomerate" by Brunker (1972) on the Forbes 1:250 000 geological sheet, but this name is invalid.|16-MAY-23
26011|Manna Conglomerate|Type section locality|537857 (top) to ? Eastwards Forbes 1:250 000.|16-MAY-23
26011|Manna Conglomerate|Description at type locality|Several hundred metres of conglomerate just north of Burcher-Forbes road, 8.5 km east of Burcher. Bottom nowhere exposed. Top has sharp contact with overlying Cowal Member rhyolitic tuff.|16-MAY-23
26011|Manna Conglomerate|Extent|The unit is exposed for at least 30 km strike on west side of Lake Cowal.|16-MAY-23
26011|Manna Conglomerate|Thickness range|The formation is about 5000 m thick.|16-MAY-23
26011|Manna Conglomerate|Lithology|The unit grades from coarse sandstone to a very coarse conglomerate with boulders 50 cm in diameter. It is generally massive and poorly bedded. The pebbles and boulders are very well rounded, consist of quartzite and quartz-sericite and are significantly flattened because of shearing. Although outcrops of conglomerate within the unit form visually impressive mountains, it seems that they constitute lenses of sheared and perhaps silicified rock within the formation. The poorly outcropping and non-outcropping areas within the boundaries of the formation are soft, recessive sandstones, non-resistant conglomerate and perhaps shales. Aeromagnetic maps of the area suggest that the Manna Conglomerate contains andesite flows and/or dolerite sills none of which are known to outcrop.|16-MAY-23
26011|Manna Conglomerate|Relationships and boundaries|Underlying unit unknown; aeromagnetics suggest an andesitic sequence. Overlain by Ina Volcanics and Weelah Formation suggesting some change in depositional conditions.|16-MAY-23
26011|Manna Conglomerate|Age reasons|Probably Silurian, from regional evidence.|16-MAY-23
26011|Manna Conglomerate|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (v.7 No. 1)|16-MAY-23
26013|Marble Arch Limestone Member|Name source|After Marble Arch Cave, a limestone arch through which Reedy Creek flows (GR 432248).|16-MAY-23
26013|Marble Arch Limestone Member|Unit history|The name Marble Arch Limestone was introduced by Best et al. (1964, Canberra 1:250 000 Geological Map, 2nd edition). No formal definition has been published. Our mapping on the Araluen 1:100 000 sheet has demonstrated that it is best regarded as a limestone lens developed in the De Drack Formation (defined on the Braidwood sheet) and is of member status. A formal definition is given for the first time.|16-MAY-23
26013|Marble Arch Limestone Member|Type section locality|Gorge of Reedy Creek for 200 m below Marble Arch Cave (GR 432248).|16-MAY-23
26013|Marble Arch Limestone Member|Extent|An area of less than 0.1 km2 in the headwaters of Reedy Creek, centred on GR 432248, Araluen sheet.|16-MAY-23
26013|Marble Arch Limestone Member|Thickness range|No bedding is present, but probably at least 100 m.|16-MAY-23
26013|Marble Arch Limestone Member|Lithology|Strongly recrystallised to coarse sporite, tending to marble. Locally a saccharoidal texture and cleavage developed. Alteration is due to thermal metamorphism by the Braidwood Granodiorite, which crops out within 50 m of the limestone.|16-MAY-23
26013|Marble Arch Limestone Member|Relationships and boundaries|A limestone lens surrounded by sediments of the De Drack Formation.|16-MAY-23
26013|Marble Arch Limestone Member|Age reasons|No fossils have been found. Its stratigraphic position indicates a Late Silurian age.|16-MAY-23
26013|Marble Arch Limestone Member|Reserved? Yes/No|by prior usage|16-MAY-23
26013|Marble Arch Limestone Member|Unit name|Marble Arch Limestone Member of De Drack Formation|16-MAY-23
11364|Marrangaroo Conglomerate|Name source|Marrangaroo railway station, Ph. Marrangaroo., Co. Cook.|16-MAY-23
11364|Marrangaroo Conglomerate|Unit history|Stephens (1883), Carne (1894 & 1908). Not previously defined.|16-MAY-23
11364|Marrangaroo Conglomerate|Type section locality|(1) Location: Austen & Butta Hartley Valley DDH3 (224552.4 E 1291973.0 N Lithgow 1:50 000 sheet 8931-111).  (2) Repository: Dept Mineral Resouraces Coal Library, Londonderry.*  (*Reference Section: Tanksley Hill, GR 325937, Lithgow 8931-111).|16-MAY-23
11364|Marrangaroo Conglomerate|Extent|Widespread and persistent unit in Western Coalfield and South-Western Coalfield (Higgins Ck Conglomerate) and in the Ulan area. Occurs on Lithgow, Bungleboori, Hampton, Katoomba, Jamison, Glen Davies and Glen Alice sheets.|16-MAY-23
11364|Marrangaroo Conglomerate|Thickness range|(1) Type section: From 250.12 m to 253.94 m; thickness 3.82 m.  (2) Maximum recorded: 16 m.|16-MAY-23
11364|Marrangaroo Conglomerate|Lithology|Quartz-lithic pebbly sandstone, medium and coarse grained, locally a pebble and cobble conglomerate: minor mudstone. Few coaly stringers.|16-MAY-23
11364|Marrangaroo Conglomerate|Relationships and boundaries|Conformably overlain by the Lithgow Coal. Commonly a sharp erosive basal contact with coaly sediments of Nile Sub-Group or sandy siltstones of the Berry Siltstone.|16-MAY-23
11364|Marrangaroo Conglomerate|Proposed publication|Australian Coal Geology|16-MAY-23
11472|Maules Creek Formation|Name source|Township of Maules Creek, northern NSW.|16-MAY-23
11472|Maules Creek Formation|Unit history|Previously the Nandewar Group (Hanlon, 1949, 1950). Recent drilling data has shown that group status is not justified as the simple division into Vickery Conglomerate and Wean Formation is not valid (Hanlon, 1975, unpubl. And 1977). The present name was used informally (Brownlow, 1976, 1977).|16-MAY-23
11472|Maules Creek Formation|Type section locality|A.B. Boggabri DDH 2 from top to 500.10 m. Core Repository: Amax/BHP Core Shed, Boggabri.|16-MAY-23
11472|Maules Creek Formation|Extent|Outcrops extensively between the Boggabri Ridge and Mooki Fault System. Laterally equivalent strata also recorded on the western side of the Boggabri Ridge, in DM Emerald Hill DDH 1 (McDonald, 1976) (unpubl.), in outcrops at Gunnible ;Mountain and possibly at Gunnedah (Brownlow, 1977). Possibly overlain conformably by equivalents of the Porcupine Formation, on Timor Mountain (Brownlow, 1977).|16-MAY-23
11472|Maules Creek Formation|Lithology|Lithic conglomerates and coarse sandstone (about 50% of the sequence), lithic fine to medium sandstone, siltstone and claystone (about 40%). Typically bright coal in seams up to 7 m thick (about 10% of the sequence) are irregularly interbedded throughout. A sequence of silicified, laminated siltstones, with recorded thicknesses up to 10-15 m commonly occurs at the base of the formation in the Leard State Forest.|16-MAY-23
11472|Maules Creek Formation|Relationships and boundaries|Overlies the Leard Formation (flint clay sediments) from which it is distinguished by distinctive clast petrology. The boundary is taken at the base of the lithic sediments. The top of the Maules Creek Formation has generally been eroded. Equivalents of the marine Porcupine Formation conformably overlies equivalents of the Maules Creek Formation in D.M. Erald Hill DDH 1 (McDonald, 1976, unpubl.), and probably overlies the Maules Creek Formation on Timor Mountain.|16-MAY-23
11472|Maules Creek Formation|Age reasons|Early Permian  Lower Stage 4 (Morgan, 1976a, b).|16-MAY-23
11472|Maules Creek Formation|Proposed publication|Australian Coal Geology|16-MAY-23
11472|Maules Creek Formation|References|01/31629|16-MAY-23
11472|Maules Creek Formation|Proposer|Brownlow J.W.|16-MAY-23
11472|Maules Creek Formation|Resdate|01-APR-1980|16-MAY-23
24377|Meloola Volcanics|Name source|Meloola homestead at GR 5284 9457 (Narromine 1:250 000 Sheet).|16-MAY-23
24377|Meloola Volcanics|Unit history|On Narromine 1:250 000 Geological Lsheet, it is described as the Ootha Beds. On Forbes 1:250 000 Metallogenic Sheet it is classified as Derriwong Beds.|16-MAY-23
24377|Meloola Volcanics|Type section locality|Near Meloola homestead, about 1.5 km to the northeast.|16-MAY-23
24377|Meloola Volcanics|Extent|Two main outcrop areas. The northern area extends between GR 5300 9510 and GR 5248 9386, the southern area from GR 5164 9276 southward onto Forbes 1:250 000 Sheet (on the latter it is classified as Derriwong Beds).|16-MAY-23
24377|Meloola Volcanics|Thickness range|Approximately 150 m.|16-MAY-23
24377|Meloola Volcanics|Lithology|Sequence of acid volcanics, sandstone, siltstone, conglomerate, limestone. The acid volcanics include rhyolitic lithic crystal tuffs, lavas and banded rhyolites.|16-MAY-23
24377|Meloola Volcanics|Relationships and boundaries|Unconformably overlies the Edols Conglomerate. Unconformably overlain by the Yarra Yarra Creek Group.|16-MAY-23
24377|Meloola Volcanics|Age reasons|Thought to be of Early Devonian age. Fossils present in limestones.|16-MAY-23
24377|Meloola Volcanics|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982|16-MAY-23
24377|Meloola Volcanics|Proposed publication|A Metallogenic Study of the Narromine 1:250 000 Sheet|16-MAY-23
24377|Meloola Volcanics|Defn Reference|86/25274 Defined P.326|16-MAY-23
24377|Meloola Volcanics|Proposer|Richardson S.J., Bowman H.N.|16-MAY-23
24377|Meloola Volcanics|Reserved? Yes/No|Yes|16-MAY-23
11678|Merigan Black Shale|Name source|"Merigan" property; GR 359052, Braidwood 1:100 000 sheet.|16-MAY-23
11678|Merigan Black Shale|Type section locality|30 metres of black shale and slate in Fairy Meadow Creek at GR 377026.|16-MAY-23
11678|Merigan Black Shale|Extent|The unit is present as disconnected linear outcrops within the Birkenburn Beds and occurs over about 50 km2 in the northwestern part of the Braidwood 1:100 0000 sheet.|16-MAY-23
11678|Merigan Black Shale|Thickness range|Variable, maximum 150 m.|16-MAY-23
11678|Merigan Black Shale|Lithology|Thin-bedded, often laminated, black shale and slate; micaceous, siliceous or pyritic in part. Rare beds of pale grey siltstone, not exceeding 2 cm thickness and showing small scale crossbedding, may be present. A graptolite fauna is present in the shale and slate.|16-MAY-23
11678|Merigan Black Shale|Relationships and boundaries|Upper and lower unit boundaries are shap and are defined by a colour change from black or grey to the buff shades which prevail in the Birkenburn Beds, in which the unit is usually encloded. Also overlain unconformably by and faulted against the Late Silurian Mount Fairy Group (Felton, 1974).|16-MAY-23
11678|Merigan Black Shale|Age reasons|Graptolites in the unit include the following species: Orthograptus truncatus (Lapworth), Orthograptus calcaratus cf basilicus (Lapworth) (possibly deformed O. quadrimucronatus), Orthograptus quadrimucronatus (J. Hall), Climacograptus sp., Dicellograptus cf. forchammeri flexuosus (LLapworth), Leptograptus cf. flaccidus (J. Hall) (Sherwin, 1070). This assemblage indicates an Eastonian (Late Ordovician) age, and probably the upper part of that stage.|16-MAY-23
11678|Merigan Black Shale|Proposed publication|Felton E.A. and Huyleatt M.B., 1975. Geology of the Braidwood 1:100 000 Sheet. Geological Survey NSW, Sydney|16-MAY-23
11678|Merigan Black Shale|Name first published by|Richardson S.J., 1975|16-MAY-23
27194|Micalong Swamp Basic Igneous Complex|Name source|Micalong Swamp, GR 380900 Brindabella 1:100 000 Sheet area.|16-MAY-23
27194|Micalong Swamp Basic Igneous Complex|Type section locality|No type locality has been given in view of the great aerial extent of outcrop and variety of rock types present.|16-MAY-23
27194|Micalong Swamp Basic Igneous Complex|Extent|A number of gabbroic stocks and associated dyke swarms in the western side of the Brindabella 1:100 000 sheet area. Stocks occur west of Burrinjuck Dam in the north and are distributed over a large area down to Goobarragandra River in the south, a distance of over 50 kms. See Brindabella 1:100 000 Geological Sheet Preliminary Edition 1975.|16-MAY-23
27194|Micalong Swamp Basic Igneous Complex|Lithology|Hornblende gabbro, hornblende dolerite, two pyroxene gabbro, olivine gabbro, leucogabbro, anorthosite, diorite, granodiorite granophyre, hornblendite.|16-MAY-23
27194|Micalong Swamp Basic Igneous Complex|Relationships and boundaries|The stocks intrude the Goobarragandra Beds and are intruded by the Young Granodiorite and Burrinjuck Adamellite.|16-MAY-23
27194|Micalong Swamp Basic Igneous Complex|Age reasons|The Complex has been dated by K/Ar at 430 +/- 9 m.y. and is probably Late Silurian.|16-MAY-23
27194|Micalong Swamp Basic Igneous Complex|Proposed publication|Bureau of Mineral Resources Bulletin|16-MAY-23
27194|Micalong Swamp Basic Igneous Complex|Comments|Note: The Pigeon Square Gabbro (name given on Tantangara 1:100 000 sheet preliminary geological edition (1974)) is included in the Micalong Swamp Basic Igneous Complex.|16-MAY-23
27194|Micalong Swamp Basic Igneous Complex|Defn Reference|83/24087|16-MAY-23
11773|Michelago Igneous Complex|Name source|The village of Michelago at GR 960460 (Michelago 1:100 000 Geological Sheet) on the Monaro Highway.|16-MAY-23
11773|Michelago Igneous Complex|Unit history|Brown (1928) was the first to describe and name the Michelago Granite but his remarks are relevant only to the northern body. Best et al. (1964) published the name in reference to both northern and southern bodies. Slepecki (1973) made reference to the Michelago Batholith|16-MAY-23
11773|Michelago Igneous Complex|Type section locality|Described under the different phase names i.e. Micaligo Adamellite, Koolambah Adamellite, Monkellan Granodiorite and Onslow Granodiorite.|16-MAY-23
11773|Michelago Igneous Complex|Description at type locality|Described under the different phase names.|16-MAY-23
11773|Michelago Igneous Complex|Extent|The complex lies to the east of the Monaro Highway and extends meridionally over some 32 km, from just north of the Bredbo River to near Mount Allan homestead at GR 001515. The mass has an average width of 4 km. In form the Michelago Complex actually consists of two distinct masses which have been subdivided into several phases. The Collingwood Fault separates the two bodies. Size: Southern body covers 32 km2 and the northern body covers 60 km2.|16-MAY-23
11773|Michelago Igneous Complex|Relationships and boundaries|The complex has intruded Late Ordovician metasediments (Foxlow Beds). Very little contact metamorphism has taken place. In the vicinity of Collingwood homestead and Colinton Trig. Station, the Early Silurian Ryrie Formation and Late Silurian Cappanana Formation and Colinton Volcanics are faulted against the complex.|16-MAY-23
11773|Michelago Igneous Complex|Age reasons|The Onslow Granodiorite has been successfully age dated by AMDEL. K-Ar analyses of biotite indicate an age of 395 +/- 8 m.y. This therefore indicates an age of intrusion of Late Silurian to Earliest Devonian for at least part of the complex.|16-MAY-23
11773|Michelago Igneous Complex|Proposed publication|Geological Survey of NSW 1:100 000 Note Series|16-MAY-23
11773|Michelago Igneous Complex|Status|1|16-MAY-23
40757|Mihi Rhyolite Member|Name source|Named after Mihi homestead (0245660 6609580 Berrioye 1:25 000 sheet).|16-MAY-23
40757|Mihi Rhyolite Member|Type section locality|Locality 297-1 on Well Gully adjacent to 30037?58?S, 150019?50?E (0244153E 6608055N Willuri 1:25 000 sheet).|16-MAY-23
40757|Mihi Rhyolite Member|Extent|Crops out over a distance of 10 km between Mihi and Nioka, adjacent to the Plagyan Thrust. An ignimbrite cropping out in Connors Creek, west of the Plagyan Thrust is tentatively referred to this member.|16-MAY-23
40757|Mihi Rhyolite Member|Thickness range|Commonly 20-25 m, but southwest of Mihi  reaches 90 m because of thick medial pumiceous and upper resedimented sandstone layers.|16-MAY-23
40757|Mihi Rhyolite Member|Lithology|Lithology  Red to green, unwelded, rhyolitic ignimbrite (sample 429-1 Table 2 Appendix 3). Medial parts highly pumiceous, the remainder contains quartz, plagioclase, minor K-feldspar, biotite and opaque minerals in a glassy, shard-rich; groundmass; shards are partially replaced by chlorite and zeolite.|16-MAY-23
40757|Mihi Rhyolite Member|Age reasons|Namurian. The SHRIMP AS3 age is 320.0?4.5 Ma (sample 429-1, Figure 10a); there is minor Pb loss.|16-MAY-23
74041|Milligans Road Formation|Name source|Milligans Road Latitude 31deg 31min 53.12sec South, Longitude 152deg 43min 8.95sec E. The Milligans Road Formation is named after Milligans Road, along which it crops out in several places, albeit poorly.|16-MAY-23
74041|Milligans Road Formation|Unit history|Not previously identified|16-MAY-23
74041|Milligans Road Formation|Geomorphic expression|The formation usually forms gently undulating terrain towards the centre of the Lorne Basin. However in the area between Waitui Falls and Lorne, resistant tuff beds form a prominent ridge north of Stewarts River.|16-MAY-23
74041|Milligans Road Formation|Type section locality|Milligans Road to small quarry. From Lat 31.52532deg S , Long 152.68386deg E to Lat 31.53236deg S, 152.71831deg E. The type section is designated to be from the base of the tuff exposed at the Bago Road-Milligans Road intersection GR 469986 6512134 (1:25 000 map sheet 9434-4-N, Byabarra; location 95) to the top of the airfall tuff beds exposed in a quarry 200 m to the southwest at GR 473259 6511362 (1:25 000 map sheet 9434-4-N, Byabarra; location 28). A lithology plot for the type section is presented in Figure 14. A lithology plot (Figure 15) for the measured section exposed in the Volcanic Resources Quarry (GR 470332 6512062, 1:25 000 map sheet 9434-4-N, Byabarra; location 45; Photograph 8) is presented for comparison.|16-MAY-23
74041|Milligans Road Formation|Description at type locality|The type section of the Milligans Road Formation is exposed in the roadside embankment at the intersection of the Bago Road and Milligans Road, southwestward along the gutters up a track leading to a quarry at the top of the rise. The beds are weathered and poorly exposed. However, the sequence of sedimentary and pyroclastic rocks of presumed Late Triassic age - and uniquely containing airfall tuff beds often associated with carbonaceous mudstone and thin poor 'coal' beds - occurs at several locations within the Lorne Basin. Thus the sequence warrants description as a new formation, the Milligans Road Formation. The tuffs are thickly bedded whereas the sandstones and mudstones are laminated to thinly bedded and the poor 'coal' beds are laminated or very thinly laminated.|16-MAY-23
74041|Milligans Road Formation|Extent|The formation is exposed at the intersection of Bago Road and Milligans Road (location 95) and extends westward, with few outcrops along Milligans Road to near the junction with Rollover Road. Separate outcrops also occur on the Pacific Highway 1 km north of the Camden Haven River Bridge and about 5 km north of Herons Creek (although the latter exposure has been destroyed by recent roadworks). A downfaulted block of the formation occurs between Lorne and Stewarts River, while further small downfaulted blocks occur from Swans Crossing southwest to the Lorne-Comboyne Road, and on the 'Camden Road 4WD' track 5 km west of Dellward.|16-MAY-23
74041|Milligans Road Formation|Thickness range|A thickness of 12 m is recorded at the type section while a thickness of 27 m is exposed in the Volcanic Resources Quarry (location 45).|16-MAY-23
74041|Milligans Road Formation|Lithology|The Milligans Road Formation, as at locations 45 and 95, consists of brown quartz-feldspathic sandstone with mica flakes, siltstone and grey mudstone with minor conglomerate. Also included are carbonaceous mudstone and thin, poor 'coal' beds up to 500 mm in thickness, together with diagnostic off-white airfall tuff up to 10 m in thickness. At location 45 the basal 300 mm of the more than 9 m-thick tuff bed contains accretionary lapilli up to 20 mm in diameter. In the southwest of the Lorne Basin, along Isaacs Road, tuff beds, each several metres thick, are exposed in several locations, including locations 170, 172 and 173. Those at location 170 are weathered, friable and blue-grey in colour while those at locations 172 and 173 are fresh, hard and range from pale buff to orange-brown.|16-MAY-23
74041|Milligans Road Formation|Depositional environment|The presence of carbonaceous mudstone with thin,'coal' beds suggests back swamps in an overbank fluviatile environment.|16-MAY-23
74041|Milligans Road Formation|Diastems or hiatuses|Probably hiatus after deposition of Camden Haven Group and prior to deposition of this unit.|16-MAY-23
74041|Milligans Road Formation|Relationships and boundaries|As the exposures of the formation appear to occur in fault-bounded blocks and neither the top nor the base of the formation is exposed boundary criteria cannot be determined. However, the inferred Late Triassic age suggests that this formation overlies the other Triassic formations after a presumed depositional hiatus. The unit is identified by its distinguishing features.|16-MAY-23
74041|Milligans Road Formation|Identifying features|The Milligans Road Formation is identified by the presence of airfall tuff often associated with carbonaceous mudstone and thin, poor 'coaly' beds.|16-MAY-23
74041|Milligans Road Formation|Structure and Metamorphism|The Milligans Road Formation occurs in fault-bounded blocks in the northeastern and southwestern parts of the Lorne Basin.|16-MAY-23
74041|Milligans Road Formation|Age reasons|While highly fragmented plant remains have been found at two locations, no identifiable material has yet been recovered from the Milligans Road Formation. These locations are on Milligans Road (GR 470918 6512474, 1:25 000 map sheet 9434-4-S) and North Branch Forest Road (GR 463189 6498582, 1:25 000 map sheet 9434-4-S, Lorne; location 243). The introduction of airfall tuff into this sequence suggests that it is associated with the emplacement of Late Triassic to Early Jurassic igneous rocks both within the Lorne Basin (Graham et al. 2006) and further northwest with the Werrikimbe Volcanics.|16-MAY-23
74041|Milligans Road Formation|Correlations|There are no units in the Lorne Basin with which this formation can be correlated.|16-MAY-23
74041|Milligans Road Formation|Defn author|G. Winston Pratt,  7-JUL-2010.|16-MAY-23
74041|Milligans Road Formation|References|Graham I., Sutherland L. & Zwingmann H. 2006. Mesozoic to Cenozoic magmatism, Lorne Basin, N.S.W. In: D. Denham ed. Australian Earth Sciences Convention: convention handbook 2006, Geological Society of Australia, Melbourne. **Pratt, G.W. 2010. A revised Triassic stratigraphy for the Lorne Basin, NSW. Quarterly Notes of the Geological Survey of New South Wales 126.|16-MAY-23
24381|Minnalong Sandstone|Name source|Minnalong homestead (GR 5209 9770, Narromine 1:250 000).|16-MAY-23
24381|Minnalong Sandstone|Type section locality|Quartz sandstone, conglomerate and shale; GR 5209 9770. Portion of unit unknown.|16-MAY-23
24381|Minnalong Sandstone|Extent|The unit extends north-south for 33 km from GR 5200 9848 north of 'Minnalong' to GR 52709486 in the south.|16-MAY-23
24381|Minnalong Sandstone|Thickness range|Unknown. Probably in the order of tens of metres.|16-MAY-23
24381|Minnalong Sandstone|Lithology|Quartz sandstone, conglomerate and shale.|16-MAY-23
24381|Minnalong Sandstone|Relationships and boundaries|Overlies the Early-Middle Devonian Yarra-Yarra Creek Group. Considered to be part of the Surat Basin.|16-MAY-23
24381|Minnalong Sandstone|Age reasons|Late Jurassic to earliest Cretaceous in age, from plant fossils in drill holes.|16-MAY-23
24381|Minnalong Sandstone|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982|16-MAY-23
24381|Minnalong Sandstone|Proposed publication|A metallogenic study of Narromine 1:250 0000 sheet.|16-MAY-23
24381|Minnalong Sandstone|Defn Reference|86/25274  Defined p.327.|16-MAY-23
24381|Minnalong Sandstone|Proposer|Bowman H.N., Richardson S.R., Dolanski J.|16-MAY-23
24381|Minnalong Sandstone|Reserved? Yes/No|Yes|16-MAY-23
24384|Monkellan Granodiorite|Name source|Parish of Monkellan, Co. Murray.|16-MAY-23
24384|Monkellan Granodiorite|Unit history|Previously regarded as part of the Michelago Granite.|16-MAY-23
24384|Monkellan Granodiorite|Type section locality|Southeast of Tea Tree Creek homestead at GR 002463, Michelago 1:100 000 Geological Series.|16-MAY-23
24384|Monkellan Granodiorite|Description at type locality|Contains both hornblende and biotite generally associated in clots, ranging between 5-10 mm in size. The clots approximate to a hornblende biotite quartz diorite while the host rock is a biotite granodiorite. The rock is therefore a hybrid biotite and hornblende granodiorite.|16-MAY-23
24384|Monkellan Granodiorite|Extent|Occupies the northern part of the Michelago Igneous Complex, north of the Tinderry Road and to the northeast of Michelago.  Size: 3.2 km2.|16-MAY-23
24384|Monkellan Granodiorite|Relationships and boundaries|Intrudes Late Ordovician Foxlow Beds. Its southern contact is with the Micaligo Adamellite.|16-MAY-23
24384|Monkellan Granodiorite|Age reasons|End of Silurian Period.|16-MAY-23
24384|Monkellan Granodiorite|Proposed publication|Geological Survey of NSW 1:100 000 Notes Series|16-MAY-23
22365|Montagu Dacite Member|Name source|Parish of Montagu, Cooma 1:100 000 sheet.|16-MAY-23
22365|Montagu Dacite Member|Unit history|Not previously differentiated as a seperate named unit.|16-MAY-23
22365|Montagu Dacite Member|Type section locality|15km east-southeast of Cooma, Cooma 1:100 000 sheet 8725, from GR059830 (base) to GR048825 (top). Representative outcrops along Carlaminda road about 14km east of Cooma.|16-MAY-23
22365|Montagu Dacite Member|Extent|Extends from 14km east to 20km southeast of Cooma.|16-MAY-23
22365|Montagu Dacite Member|Thickness range|Ranges to 800m.|16-MAY-23
22365|Montagu Dacite Member|Lithology|Coarsely porphyritic dacite; phenocrysts include distinctive euhedral black hornblende.|16-MAY-23
22365|Montagu Dacite Member|Relationships and boundaries|Overlies shale and overlain by assorted volcanics-dacite, tuff- of Rothlyn Formation; member of Rothlyn Formation.|16-MAY-23
22365|Montagu Dacite Member|Age reasons|Late Silurian from fossils enclosing the Rothlyn Formation.|16-MAY-23
22365|Montagu Dacite Member|Defn author|G.A.M. Henderson ?1989.|16-MAY-23
22365|Montagu Dacite Member|Comments|Although this appears to be an adequate unit definition, no evidence is available to show that this definition went through the Stratigraphy Commission approval process. The original card was supplied  to ASUD manager C. Brown by R. S. Abell, on his departure from BMR, after the publication of BMR Bulletin 233 Geology of the Canberra 1:100 000 sheet.|16-MAY-23
22365|Montagu Dacite Member|References|Henderson, G.A.M., 1987. Late Silurian geology of the Michelago-Cooma area: 1:100 000 preliminary edn map. Bur. Miner. Resour. Aust.|16-MAY-23
79335|Mooki Coal Member|Name source|Mooki River in northern New South Wales. This river overlies the parent unit Maules Creek Formation in the Gunnedah Basin.|16-MAY-23
79335|Mooki Coal Member|Unit history|Upper Maules Creek seam or Rutley seam used informally in well completion reports submitted to government departments by Force energy, Eastern Star Gas and Santos.|16-MAY-23
79335|Mooki Coal Member|Geomorphic expression|Concealed beneath 700-1000m of Permian-Cretaceous cover (Gunnedah and Surat Basins).|16-MAY-23
79335|Mooki Coal Member|Type section locality|Coal Seam Gas Exploration Drillhole Dewhurst 11 (Eastern Star Gas). 149.725147°E / 30.50355°S (GDA94) depth (899.93-903.43m).|16-MAY-23
79335|Mooki Coal Member|Extent|Restricted to three drillholes in the Pilliga East state forest area south of Narrabri over approximately 200 square kilometres.|16-MAY-23
79335|Mooki Coal Member|Thickness range|3.50 m in type section. Only recorded from three exploration drillholes in the Pilliga East and Jacks Creek State Forests. Thickness ranges from 1.5 to 3.5m.|16-MAY-23
79335|Mooki Coal Member|Lithology|Coal, dull with bright bands, pyrite blebs towards the top. Minor stone bands of siltstone may occur sporadically throughout the seam. Occurs as a single seam.|16-MAY-23
79335|Mooki Coal Member|Depositional environment|Coal Swamp (marginal marine).|16-MAY-23
79335|Mooki Coal Member|Fossils|Coal.|16-MAY-23
79335|Mooki Coal Member|Diastems or hiatuses|Nil.|16-MAY-23
79335|Mooki Coal Member|Relationships and boundaries|Uppermost seam (where developed) in the Maules Creek Formation. Above the Tullamullen Coal Member.|16-MAY-23
79335|Mooki Coal Member|Identifying features|Not described.|16-MAY-23
79335|Mooki Coal Member|Structure and Metamorphism|Dips at <5 degrees, probable early normal faulting is expected to be developed as observed in mining of the Maules Creek Formation in the Maules Creek Sub-basin to the east. Vitrinite reflectance values of between 0.65 and 0.85 RoMax where not heat affected by igneous intrusions.|16-MAY-23
79335|Mooki Coal Member|Age reasons|Permian - Cisuralian (Kungurian) part of Gunnedah Basin Bellata Group, contains Glossopteris and Gengamoptris (Cisuralian). Palynological Age of APP33 inferred from samples below this interval and samples of APP41 in samples above this seam in the Porcupine Formation.|16-MAY-23
79335|Mooki Coal Member|Correlations|Probable equivalent to the Narrawolga Coal Member at Werris Ck, Hilltop Coal Member at Muswellbrook Anticline North and South, Herndale seam at Maules Creek Sub-Basin.|16-MAY-23
79335|Mooki Coal Member|Alteration and Mineralisation|Coal - Bituminous in rank.|16-MAY-23
79335|Mooki Coal Member|Geophysical Expression|Possible seismic reflector, low downhole gamma (<50) and density (<1.50g/cc) geophysical response.|16-MAY-23
79335|Mooki Coal Member|Defn author|Mark Dawson, 10-FEB-2016.|16-MAY-23
24616|Moolarben Coal Member|Name source|Parish Moolarben, County Phillip; near Ulan.|16-MAY-23
24616|Moolarben Coal Member|Unit history|New name (C.S. Bembrick). First used in unpublished J.C.B. borelog from Ulan area (1975).|16-MAY-23
24616|Moolarben Coal Member|Type section locality|(1) Location - J.D.P. Ulan DDH 18 (377403 m E 1427419 m M, Gulgong 1:50 000, 8833-II and III).  (2) Repository - Dept of Mineral Resources Core Library, Londonderry.|16-MAY-23
24616|Moolarben Coal Member|Extent|Western Coalfield; Lithgow and Bungleboori 1:50 000 sheets. Also Ulan area.|16-MAY-23
24616|Moolarben Coal Member|General description|A thin, but relatively persistent coal or carbonaceous claystone horizon. Well developed in the Ulan area, and also the Wolgan area.|16-MAY-23
24616|Moolarben Coal Member|Thickness range|(1) Type section - from 84.03 m to 87.20 m; thickness, 3.17 m.  (2) Maximum recorded - 3.56 m (Ulan area).|16-MAY-23
24616|Moolarben Coal Member|Lithology|Coal, minor claystone.|16-MAY-23
24616|Moolarben Coal Member|Relationships and boundaries|Underlain conformably by the Angus place Sandstone. Occurs within the State Mine Creek Formation, at or very close to its base.|16-MAY-23
24616|Moolarben Coal Member|Proposed publication|Australian Coal Geology|16-MAY-23
24616|Moolarben Coal Member|Proposer|Bembrick C.S., Robertson Research (Australia) Pty Ltd|16-MAY-23
12292|Moorna Formation|Name source|Moorna Station|16-MAY-23
12292|Moorna Formation|Unit history|Not previously named.|16-MAY-23
12292|Moorna Formation|Type section locality|Type area: Fishermen's Cliff, along side "The Selection" Moorna Station, W of Anabranch, N bank of River Murray.  Location of Type Section:  Longitude 141o40'E, Latitude 34o6'S.|16-MAY-23
12292|Moorna Formation|Extent|From Salt Creek on Kulcurna Station for about 100 km to the east.|16-MAY-23
12292|Moorna Formation|Thickness range|a) At type seaction:                                b) Maximum known:|16-MAY-23
12292|Moorna Formation|Lithology|Silt to gravel|16-MAY-23
12292|Moorna Formation|Fossils|Paper by Larry Marshall in Mem. 34 gives complete fauna.|16-MAY-23
12292|Moorna Formation|Relationships and boundaries|Lens between Chowilla Sand and underlying Parilla Sand Boundaries defined as seen in cliff outcrops along the Murray River. Measured sections are being published in the Memoir.|16-MAY-23
12292|Moorna Formation|Age reasons|Late Pliocene - palaeontological similarity to Lchinchilla Sand. In Qld.|16-MAY-23
12292|Moorna Formation|Proposed publication|Memoir 34, National Museum Victoria|16-MAY-23
12292|Moorna Formation|Defn approved by|Copied from xerox sent by NSW Stratigraphic Nomenclature Sub-Committee|16-MAY-23
12292|Moorna Formation|Name first published by|Gill E.D., 1973|16-MAY-23
12292|Moorna Formation|Reserved? Yes/No|Gill E.D.|16-MAY-23
38897|Mossgiel Granite|Name source|Named after the location of the site of drillhole DM Mossgiel DDH1, located about 15 kilometres south of Mossgiel on the Cobb Highway between Hay to Ivanhoe.|16-MAY-23
38897|Mossgiel Granite|Geomorphic expression|All subsurface.|16-MAY-23
38897|Mossgiel Granite|Type section locality|33o22'41.9"S, 144o39'21.23"E; GDA94 datum.|16-MAY-23
38897|Mossgiel Granite|Extent|Barron (2000) suggests intrusion could be <2000m across.|16-MAY-23
38897|Mossgiel Granite|Thickness range|Intersected the granite at 1735.6 m in DM Mossgiel DDH1, base not recovered.|16-MAY-23
38897|Mossgiel Granite|Lithology|The granite has been described by Dr L.M. Barron (Barron; Geological Survey of NSW Petrological Report; 2000/006 (or GS2001/227)) as being a medium to coarse grained, high-level emplaced, quartz-megacrystic garnet-?cordierite-biotite-An25 feldspar-micrographic granite. The granite is relatively melanocratic and S type granite with low quartz and is completely undeformed.|16-MAY-23
38897|Mossgiel Granite|Depositional environment|None.|16-MAY-23
38897|Mossgiel Granite|Relationships and boundaries|Unconformably overlain by ?Early Devonian Darling Basin sediments (yet to be correlated).|16-MAY-23
38897|Mossgiel Granite|Age reasons|Simon Wilde (Curtin Uni. of Tech; Geological Survey Report GS2001/207) SHRIMP dated the granite at 427+/-7 Ma to 423+/-9 Ma (206Pb/238U).|16-MAY-23
38897|Mossgiel Granite|Correlations|Barron suggests there may be a close association with the newly named Wilkurra and Nambucurra Granites, the other S type granites in the region.|16-MAY-23
38897|Mossgiel Granite|References|Barron, L.M. 2000. Granitoids in DM Mossgiel DDH1. Geological Survey of New South Wales Petrological Report GS2000/006 (unpublished). **Moffitt, R. S. 2001. DM Mossgiel DDH1 well completion report. Geological Survey of New South Wales Report GS2001/399 (unpublished). **Wilde, S.A. 2000. SHRIMP U-Pb dating of four ?granite? samples from the Wilkurra No 1 and Mossgiel No 1 boreholes, NSW. Isotope Studies Group, Curtin University of Technology. Perth, Western Australia, Geological Survey of New South Wales, Report GS2001/207 (unpublished).|16-MAY-23
40756|Mount Byar Ignimbrite Member|Name source|From Mount Byar (0240000E 6624020N Plagan 1:25 000 sheet).|16-MAY-23
40756|Mount Byar Ignimbrite Member|Type section locality|At locality 439-4 30029?03?S,150019?04?E (0242513E 6624480N Plagan 1:25 000 sheet),1.6 km east-northeast of Mount Byar.|16-MAY-23
40756|Mount Byar Ignimbrite Member|Extent|Distribution between the crest of Mount Byar in the north and Mallee, 1 km north of Dripping Rock Creek in the south.|16-MAY-23
40756|Mount Byar Ignimbrite Member|Thickness range|Ranges from 7 m at Mount Byar to 40 m at Mallee (0237350E 6613560N Berrioye 1:25 000).|16-MAY-23
40756|Mount Byar Ignimbrite Member|Lithology|Varies from fine, purple, welded, rhyolitic ignimbrite (sample 433-5 Table 2 Appendix 3) with small phenocrysts of feldspars, mainly plagioclase, and pumice fragments at Mount Byar to coarser, purple to red, unwelded to poorly welded, ignimbrite farther south; the latter contains quartz, plagioclase, K-feldspar, opaque minerals and pumice fragments. Groundmass of both the fine and coarse ignimbrites spherulitic to micropoikilitic; basal part of coarse variety glassy at 0238701E 6621397N (Berrioye 1:25 000).|16-MAY-23
40756|Mount Byar Ignimbrite Member|Age reasons|?Late Namurian.|16-MAY-23
12623|Mount Daubeny Formation|Name source|Mt Daubeny, GR 5758 1428 on Willandra Property on 1:250 000 sheet area, Wilcannia.|16-MAY-23
12623|Mount Daubeny Formation|Unit history|The formation has previously been called the Wertago-Cootawundy Series (Kenny, 1930), and the Cootawundy Beds (Scheibner, 1978).|16-MAY-23
12623|Mount Daubeny Formation|Type section locality|Gnalta Creek from GR 5661 1512 to GR 5773 1500 on 1:250 000 sheet Wilcannia.|16-MAY-23
12623|Mount Daubeny Formation|Extent|The unit is exposed for 230 km2 on 250 000 sheets Wilcannia (northeastern corner) and Whitecliffs (southwestern corner).|16-MAY-23
12623|Mount Daubeny Formation|Thickness range|7 km in the south-central part of the outcrop area.|16-MAY-23
12623|Mount Daubeny Formation|Lithology|Coarse pale red (5R6/2) arenite in west which fines eastwards where brown, grey and green coloured beds are common. Beds are planar bedded; commonly with streaming lineations and minor crossbeds. Siltstone and conglomerate are present locally. Six metre-thick quartzite beds are present in the upper part of the formation.|16-MAY-23
12623|Mount Daubeny Formation|Relationships and boundaries|Overlies the Wonaminta Beds unconformably. In the south the base is marked by a quartzite (Koonburra Creek Quartzite Member). The formation is overlain by the Ravendale Formation in the west and possibly the Snake Cave Sandstone at Gnalta Peak (south of Gnalta Creek).|16-MAY-23
12623|Mount Daubeny Formation|Age reasons|Elements of the Baragwanathia Flora including Sporongonites sp., sp., Psilophyton sp., Zosterophyllum sp., and Hostimella sp. (pers. Comm. Mary White). These species are considered to represent a Gedinnian age (Early Devonian) (on basis of the width of the standard axes of Zosterophyllum, D. Edwards, pers. comm., 1983).|16-MAY-23
12623|Mount Daubeny Formation|Defn author|Neef et al.|16-MAY-23
12623|Mount Daubeny Formation|Proposed publication|Journal of the Royal Society of NSW|16-MAY-23
12623|Mount Daubeny Formation|Comments|Notes: The formation is largely composed of "humid" sand-rich, alluvial fans.|16-MAY-23
12623|Mount Daubeny Formation|References|01/31631; 79/19631|16-MAY-23
12623|Mount Daubeny Formation|Defn Reference|91/27221, 91/27287|16-MAY-23
12623|Mount Daubeny Formation|First Reference|90/27043 Formation|16-MAY-23
12623|Mount Daubeny Formation|Proposer|Neef G., Holzberger I., Kelly R., Edwards A.C.E., Vaughan J., Bottrill R.S., Hatty J.|16-MAY-23
12623|Mount Daubeny Formation|Reserved? Yes/No|Yes|16-MAY-23
26052|Mount Fairy Group|Name source|Mount Fairy, GR 376036, Braidwood 1:100 000 sheet.|16-MAY-23
26052|Mount Fairy Group|Unit history|The term "Mount Fairy Series" was used by Garretty (1936) to describe Silurian rocks in the vicinity of Mount Fairy. In 1953, the name Mount Fairy Group was used to describe an undifferentiated sequence of shale, greywacke, sandstone, tuff and limestone on the Canberra 1:250 000 geological sheet 1st edn (Jooplin et al. 1953). The same sequence is termed "Mount Fairy Beds" on the 2nd edition (Best et al. 1964) and includes rocks now known to be Ordovician and Devonian in age.|16-MAY-23
26052|Mount Fairy Group|Constituents|Covan Creek Formation, Currawang Basalt, Woodlawn Volcanics, De Drack Formation, Palerang Formation, Bombay Volcanics, Long Flat Volcanics.|16-MAY-23
26052|Mount Fairy Group|Extent|The Mount Fairy Group occurs over an area of about 1000 km2 in the northeastern part of the Canberra 1:250 000 sheet and the southeastern part of the Goulburn 1:250 000 sheet.|16-MAY-23
26052|Mount Fairy Group|Relationships and boundaries|The Mount Fairy Group is commonly faulted against Ordovician rocks. It unconformably overlies the Ordovician Birkenburn Beds (Felton and Huleatt, 1975) and is unconformably overlain by the late Early Devonian Tarago Conglomerate (Felton and Huleatt, op. cit.). It is intruded by the Early Devonian Boro Granite.|16-MAY-23
26052|Mount Fairy Group|Age reasons|Monograptus (?) bohemicus has abeen identified from the De Drack Formation by Strusz and Nicoll (1973), giving a maximum age of Late Silurian. Possible plant fragments of earliest Devonian affinity have been described by Sherwin (1973) from the Covan Creek Formation. An age range of Late Silurian to earliest Devonian is indicated for the Mount Fairy Group.|16-MAY-23
26052|Mount Fairy Group|Proposed publication|Felton E.A., and Huleatt M.B., 1975. Geology of the Braidwood 1:100 000 Sheet. Geological Survey NSW, Sydney.|16-MAY-23
26052|Mount Fairy Group|Status|1|16-MAY-23
12795|Mount Hercules Sandstone Member|Name source|The best occurrences of the unit are near Mount Hercules homestead (GR 641825 Camden 1:50 000 sheet).|16-MAY-23
12795|Mount Hercules Sandstone Member|Unit history|Previously called the Mount Hercules Sandstone (Dyer 1966).|16-MAY-23
12795|Mount Hercules Sandstone Member|Type section locality|18.4 m of medium to fine grained sandstone exposed along the southern climb of old Razorback road from GR 661814 to GR 662824 (Camden 1:50 000). The base and top of the section are marked by poorly outcropping laminite, siltstone and interbedded sandstone.|16-MAY-23
12795|Mount Hercules Sandstone Member|Extent|The unit occurs within the uppermost part of the Bringelly Shale (as defined by Herbert 1973, in prep.) and forms a prominent bench level in the Razorback Range area, Wollongong-Port Hacking 1:100 000 sheet area.|16-MAY-23
12795|Mount Hercules Sandstone Member|Thickness range|From less than 1 m to a maximum of 44 m.|16-MAY-23
12795|Mount Hercules Sandstone Member|Lithology|Sandstone, fine to medium grained, light grey, lithic, cross bedding is common in places, dipping to the southeast. Minor siltstone interbeds are present towards the top.|16-MAY-23
12795|Mount Hercules Sandstone Member|Relationships and boundaries|Occurs within the uppermost parts of the Bringelly Shale in the Razorback Range area. In places it appears to be a channel sand, with channel configurations and a basal breccia but it never completely lenses out, but does coalesce with other channel sands.|16-MAY-23
12795|Mount Hercules Sandstone Member|Age reasons|The same age as for the Bringelly Shale-Middle Triassic.|16-MAY-23
12795|Mount Hercules Sandstone Member|Proposed publication|Wollongong-Port Hacking 1:100 000 sheet and notes. NSW Dept Mines|16-MAY-23
37913|Mount Hook Rhyolite Member|Name source|Named after Mt Hook, 992 m, GR323579 Coryah 1:25,000 sheet.|16-MAY-23
37913|Mount Hook Rhyolite Member|Unit history|Mount Hook Rhyolite (Opdyke et al. 2000).|16-MAY-23
37913|Mount Hook Rhyolite Member|Type section locality|1 km east of Pound Creek at the northern boundary of Darthula, GR295608 to 292608 Coryah 1:25,000 sheet.|16-MAY-23
37913|Mount Hook Rhyolite Member|Extent|On the eastern and western limbs of the Berrygil Anticline south of Rocky Creek and on the western limb of the anticline at Lochiel Downs (GR281651 Grattai 1:25,000 sheet).|16-MAY-23
37913|Mount Hook Rhyolite Member|Thickness range|45 m|16-MAY-23
37913|Mount Hook Rhyolite Member|Lithology|The Mount Hook Rhyolite is normally characterised by two lithologies. The basal unit, up to 20 m thick, is a red, unwelded ignimbrite with fresh feldspars, rare quartz, minor opaque minerals, rare grey volcanic rock fragments and pebble-size pumices. The groundmass is vitric. The immediately succeeding upper part, up to 25 m thick, is celadonitised and pale green near the base, the remainder being beige to purple. It is moderately welded and contains sericitised feldpars, minor quartz, opaque minerals, rare volcanic rock fragments and pumice fiamme. The groundmass is micropoikilitic.|16-MAY-23
37913|Mount Hook Rhyolite Member|Depositional environment|Ignimbrite.|16-MAY-23
37913|Mount Hook Rhyolite Member|Relationships and boundaries|Overlies the Hazelvale Rhyodacite in the lower part of the Rocky Creek Conglomerate within the Darthula block.|16-MAY-23
37913|Mount Hook Rhyolite Member|Age reasons|Carboniferous (Namurian).|16-MAY-23
37913|Mount Hook Rhyolite Member|References|OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
12887|Mount Lewin Limestone Member|Unit history|The Mount Lewin Limestone Member was previously named informally as the 'grey' unit (Percival 1976; Osborne 1978). It is the upper of the two constituent members of the Vandon Limestone.  The locality now known as Malongulli Sugarloaf is shown as 'Mount Lewin' on a copy of an early nineteenth century sketch map of the area reproduced in Carne & Jones (1919, p.7).|16-MAY-23
12887|Mount Lewin Limestone Member|Type section locality|The type section is situated in the upper reaches of Copper Mine Creek (GR 725797*), 550 m ESE of Malongulli Sugarloaf (Mount Lewin). (*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978)|16-MAY-23
12887|Mount Lewin Limestone Member|Description at type locality|The type section has been measured across the southern slopes of the creek in steeply dipping, massive grey burrow-mottled lime mudstones and wackestones.|16-MAY-23
12887|Mount Lewin Limestone Member|General description|The type section has been measured across the southern slopes of the creek in steeply dipping, massive grey burrow-mottled lime mudstones and wackestones. These beds are some 25.5 m thick, and overlain by an upper unit of thinly bedded fawn-grey wackestones, 3.5 m thick. These latter are the uppermost beds of the Vandon Limestone (and Cliefden Caves Limestone Group). They are succeeded, comparatively abruptly by 0.05-0.2 m thick beds of dark grey, laminated calcareous siltstones of the basal Malongulli Formation. The Mount Lewin Limestone Member has been mapped as an independent unit throughout the Cliefden Caves area and at Licking Hole Creek (Percival 1976).|16-MAY-23
12887|Mount Lewin Limestone Member|Thickness range|29 m thick at the type section.|16-MAY-23
12887|Mount Lewin Limestone Member|Proposed publication|Stratigraphy of Cliefden Caves Limestone Group (Upper Ordovician) central NSW. J. geol. Soc. Aust.|16-MAY-23
12893|Mount Lidgbird Basalt|Name source|Mount Lidgbird, altitude 777 m, located at 159o05.24'E longitude, 31o33.52' S latitude on map of Lord Howe Island (Department of Lands, Sydney, 1966, 1:15 840).|16-MAY-23
12893|Mount Lidgbird Basalt|Unit history|Standard (1963) called these lavas the Mount Lidgbird volcanics, whereas Game (1970) referred to them as the Gower-Lidgbird lavas.|16-MAY-23
12893|Mount Lidgbird Basalt|Type section locality|No type section designated, although virtually the whole of Mounts Lidgbird and Gower are typical. Much of the sequence inaccessible (precipitous cliffs), but typical accessible exposures on ridge running southwest from Mount Lidgbird, in the lower part of Erskine Valley, and on ridge leading from the Saddle to the summit of Mount Gower. Lavas essentially flat lying.|16-MAY-23
12893|Mount Lidgbird Basalt|Extent|Exposed over about 8 km2 in southern one-third of Lord Howe Island forming much of Mount Lidgbird and all of Mount Gower (875 m).|16-MAY-23
12893|Mount Lidgbird Basalt|Thickness range|875 m +.|16-MAY-23
12893|Mount Lidgbird Basalt|Lithology|Tabular basaltic lavas, ranging from ~2 m to 30 m thick, often with well developed columnar jointing. Oxidation of lava tops common. Lavas markedly porphyritic (olivine, plagioclase, clinopyroxene) to aphyric, and are dominantly mildly alkaline basalts.|16-MAY-23
12893|Mount Lidgbird Basalt|Relationships and boundaries|Lavas are younger than Rocky Point Breccia and the dykes and sheets that intrude Rocky Point Breccia.|16-MAY-23
12893|Mount Lidgbird Basalt|Age reasons|Four samples yield concordant K-Ar ages at 6.4 +/- 0.1 Ma, regarded as good estimate for age of eruption of these lavas in Late Miocene.|16-MAY-23
12893|Mount Lidgbird Basalt|Proposed publication|Submitted to J. Geol. Soc. Australia|16-MAY-23
12893|Mount Lidgbird Basalt|Comments|Notes: The Mount Lidgbird Basalt is a sequence of lavas that were ponded in a caldera that formed in the summit region of the shield volcano of which Lord Howe Island is an erosional remnant. These lava have normal magnetic polarity.|16-MAY-23
12893|Mount Lidgbird Basalt|Defn approved by|See letter 1/7/82 from T. Russell on NSW file.|16-MAY-23
13247|Mount Wright Volcanics|Name source|Mt Wright, northeastern Broken Hill 1:250 000 sheet area.|16-MAY-23
13247|Mount Wright Volcanics|Type section locality|31o17'S 142o25'E to 31o12'S 142o24'E. The unit is thought to young progressively from south to north within the type area.|16-MAY-23
13247|Mount Wright Volcanics|Extent|North eastern Broken Hill 1:250 000 sheet area, on eastern side of valley drained by Mount Wright Creek.|16-MAY-23
13247|Mount Wright Volcanics|Thickness range|2440 m (Warris 1967, unpubl.).|16-MAY-23
13247|Mount Wright Volcanics|Lithology|Quartz keratophyres near base, spilitic and amygdaloidal basalts in middle, basalts and andesites toward top.|16-MAY-23
13247|Mount Wright Volcanics|Relationships and boundaries|Contacts not exposed. Presumed to rest unconformably on pre-Phanerozoic Wonominta Beds. Faualted relation with overlying Cymbric Vale Formation.|16-MAY-23
13247|Mount Wright Volcanics|Identifying features|Mount Wright Volcanics (Rose 1968 following Warris 1967, unpubl.)|16-MAY-23
13247|Mount Wright Volcanics|Age reasons|Archaeocyatha in upper part of unit at localities L96 and L97 indicate an Early Cambrian (later Atdabanian) age.|16-MAY-23
13247|Mount Wright Volcanics|Proposed publication|Palaeontographica A177 p.129-212.|16-MAY-23
13247|Mount Wright Volcanics|Defn approved by|Approved by NSW Sub-Committee (see file 82/86, folios 209 and 195)|16-MAY-23
26060|Mowbray Formation|Name source|Mowbray homestead (Paterson 4613 9755).|16-MAY-23
26060|Mowbray Formation|Unit history|Subdivision of the Gilmore Volcanic Group (Rattigan).|16-MAY-23
26060|Mowbray Formation|Type section locality|Two kilometres north of Paterson.  Location of Type Section: Paterson (4623 9764 to 4617 9753) from the Hilldale-Vacy Reg.-North Coast Railway intersection southwest to the Paterson River.|16-MAY-23
26060|Mowbray Formation|Extent|The unit is recognised in the Vacy, Gresford, Lamb's Valley, Mt Tyraman, Mirannie, Stanhope and Myall Creek areas.|16-MAY-23
26060|Mowbray Formation|Thickness range|a) At type section:  198 m.  b) Maximum known:|16-MAY-23
26060|Mowbray Formation|Lithology|Basal grey and red andesitic ignimbrite overlain by a sequence of purplish lithic sandstone, conglomerate, white and brownish ignimbrites and lithic tuff. The uppermost bed is a white and purple ignimbrite of dellenitic composition.|16-MAY-23
26060|Mowbray Formation|Relationships and boundaries|The unit overlies the purple lithic sandstones of the Newtown Formation; the contact is marked by the base of the Breckin Ignimbrite Member. The unit is overlain by the Mt Johnstone Formation; the upper contact is marked by the top of the Lamb's Valley Ignimbrite Member.|16-MAY-23
26060|Mowbray Formation|Age reasons|Lower Wesphalian, Correlation from Radiometric dating of Paterson Volcanics, Martins Creek Ignimbrite; and from faunal correlations by Campbell and McKelvey.|16-MAY-23
26060|Mowbray Formation|Defn author|Hamilton G., Hall G.C., Roberts J., 1974.|16-MAY-23
26060|Mowbray Formation|Proposed publication|Journal Roy. Soc NSW|16-MAY-23
26060|Mowbray Formation|Defn approved by|From xerox copy sent by NSW Sub-Committee.|16-MAY-23
26060|Mowbray Formation|Proposer|Hamilton G., Hall G.|16-MAY-23
26060|Mowbray Formation|Reserved? Yes/No|Hamilton G.|16-MAY-23
13338|Mugincoble Chert|Name source|Village of Mugincoble, southeast of Parkes on Forbes 1:250 000 Geological Sheet.|16-MAY-23
13338|Mugincoble Chert|Unit history|Previously published as the Mugincoble Beds (R.L. Brunker, 1972). On the Narromine 1:250 000 Geological Slheet, the Mugincoble Cherts are called the Hawkes Creek Beds.|16-MAY-23
13338|Mugincoble Chert|Type section locality|Near Mugincoble village (Forbes 1:250 000) ridges of chert outcrop.|16-MAY-23
13338|Mugincoble Chert|Extent|Unit extends from Daroobalgie (GR 615879, Forbes 1:250 000 Sheet) northwarads for 120 km to Narromine at GR 637009, Narromine 1:250 000 Sheet.  Size: Estimated maximum thickness of 3 km. However, undetected or unmapped folding may have excessively exaggerated this thickness.|16-MAY-23
13338|Mugincoble Chert|Lithology|Chert with minor phyllite beds.|16-MAY-23
13338|Mugincoble Chert|Relationships and boundaries|Conformably overlies the Tomingley Siltstone of E-M Ordovician age. Unconformably overlain by the Late Devonian Hervey Group.|16-MAY-23
13338|Mugincoble Chert|Age reasons|Middle Ordovician.|16-MAY-23
13338|Mugincoble Chert|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982|16-MAY-23
13338|Mugincoble Chert|Proposed publication|A Metallogenic Study of the Narromine 1:250 000 Sheet|16-MAY-23
13338|Mugincoble Chert|Defn Reference|86/25274|16-MAY-23
13338|Mugincoble Chert|Reserved? Yes/No|As Mugincoble Beds|16-MAY-23
29225|Mulculca Formation|Name source|Named after Mulculca homestead (GR 6185 4426 Redan 1:25 000 Sheet).|16-MAY-23
29225|Mulculca Formation|Unit history|Shown as undifferentiated Thackaringa Group, and Cues formation by Willis et al. (1983). Part of "Redan gneiss" of Rayner (1949). Partly equivalent to "Mulculca rock unit association" of Corbett (1981).|16-MAY-23
29225|Mulculca Formation|Type section locality|There is no exposed section sufficiently complete to be nominated as a type section. A type area is nominated in grid squares 7652 and 7553 Kinalung 1:25 000 Sheet. A reference area is nominated in grid squares 6443, 6444, 6544 and 6445 Redan 1:25 000 sheet.|16-MAY-23
29225|Mulculca Formation|Description at type locality|The formation is characterised by a greater abundance of metasediments and/or metasedimentary composite gneisses than the underlying and overlying formations. The abundant albite-quartz (+/- magnetite) rocks in Mulculca Formation are similar to those in adjacent formations. Quartz-magnetite "lode" rocks are common near the top of Mulculca Formation, and are also known near the base. Other minor components of the formation include amphibolite/basic granulite, albite-quartz-amphibole rocks, and albite-quartz-magnetite gneiss.|16-MAY-23
29225|Mulculca Formation|Extent|The formation crops out poorly, but is inferred to extend across the northern part of the Redan 1:25 000 sheet and across a substantial area of the Kinalung 1:25 000 sheet.|16-MAY-23
29225|Mulculca Formation|Thickness range|Estimated at 1.5 km, but very approximate.|16-MAY-23
29225|Mulculca Formation|Relationships and boundaries|The base is defined by an increase in the abundance of metasediments or metasedimentary composite gneiss, in comparison with the underlying Ednas Gneiss. This corresponds with a decrease in the abundance of albite-quartz-magnetite gneiss. The top is defined as where the metasediment (or metasedimentary composite gneiss) bearing association gives way to the albite-quartz rock/leucocratic gneiss/basic gneiss association of Lady Brassey Formation.|16-MAY-23
29225|Mulculca Formation|Age reasons|Part of Proterozoic Willyama Supergroup - similarity of rock types, no observed unconformity.|16-MAY-23
29225|Mulculca Formation|Proposed publication|Australian Journal of Earth Sciences|16-MAY-23
26064|Mulwaree Group|Name source|Mulwaree River, which flows north through the township of Tarago (GR 420159) and Lake Bathurst (GR 417217; Braidwood 1:100 000 sheet), and near which the unit crops out.|16-MAY-23
26064|Mulwaree Group|Constituents|descending order: Bongalaby Formation (Felton & Huleatt, 1975), Lake Bathurst Limestone Member (Felton & Huleatt, 1975), Tarago Conglomerate (Pogson, 1972; defined Felton & Huleatt, 1975).\|16-MAY-23
26064|Mulwaree Group|Extent|The unit crops out mainly in the north-trending synclinal belt west of Tarago and Lake Bathurst. Isolated outcrops occur further south (see definition of Tarago Conglomerate). The Mulwaree Group as defined here occurs only on the Braidwood 1:100 000 sheet.|16-MAY-23
26064|Mulwaree Group|Thickness range|About 500 m (est).|16-MAY-23
26064|Mulwaree Group|Lithology|Thin-bedded fossiliferous calcareous sandstone and siltstone, occasionally tuffaceous, and minor flow-banded rhyolite (Bongalaby Formation); limestone (Lake Bathurst Limestone Member); purple boulder and cobble conglomerate, coarse gritty sandstone and red siltstone (Tarago Conglomerate).|16-MAY-23
26064|Mulwaree Group|Relationships and boundaries|Unconformably overlies Silurian-early Early Devonian Mount Fairy Group; unconformably overlies Ordovician Birkenburn Bedsand Early Devonian Boro Granite. Top eroded.|16-MAY-23
26064|Mulwaree Group|Age reasons|The Lake Bathurst Limetone Member contains Gephuropora duni Etheridge, Chalcidophyllum sp., Polygnathus linguiformis foreolata Philip & Jackson; Neoprioniodus Bicurvatus (Brahnson & Mehl); Ozarkodina cf. Jaegeri Walliser (Philip, 1966); Spathognathodus linearis (Philip). Receptaculites sp. and Plasmophyllum sp. occur within the Bongalaby Formation. See Philip and Pewdder, 1968; Strusz and Nicoll, 1973. An Emsian age is indicated.|16-MAY-23
26064|Mulwaree Group|Proposed publication|Felton E.A. and Huleatt M.B., 1975. Geology of the Braidwood 1:100 000 Sheet. Geological Survey NSW, Sydney.|16-MAY-23
13477|Munmorah Conglomerate|Name source|Formerly defined by Hanlon et al. (1954) in Alisons Wyong Bore DDH2, from depths 83.6 m to 240 m. As correlation with other bores in the area shows that the lower 32.2 m of this section could be included in the Dooralong Shale, a new type section for the Munmorah Conglomerate is now defined. The core of Alisons Wyong Bore DDH2 no longer exists.|16-MAY-23
13477|Munmorah Conglomerate|Type section locality|DM Dooralong DDH1 (same locality as for Dooralong Shale), depths 218.63 m to 334.80 m (GR 355979 Morisset 1:63 360). Core at NSW Mines dept, Londonderry.|16-MAY-23
13477|Munmorah Conglomerate|Extent|The unit crops out around the southern shores of Lake Macquarie, to Martinsville and Morisset in the west. The formation is also exposed in coastal cliffs from Wybung Head in the north to Norah Head in the south. The outcrop area covers the northeastern part of the Gosford-Lake Macquarie 1:100 000 sheet area. The formation can be recognised in boreholes from the Lake Macquarie area to DM Murrays Run DDH1 in the west, and to Windeyers Hawkesbury River Bore in the south.|16-MAY-23
13477|Munmorah Conglomerate|Thickness range|Over 140 m thick just south of Lake Macquarie, near Lake Munmorah; thins to about 80 m in Gosford-Wyong-Jilliby area in the south and west.|16-MAY-23
13477|Munmorah Conglomerate|Lithology|Pebbly sandstone, conglomerate, smaller amounts of grey and garey-green siltstone and claystone. Unit is dominantly conglomeratic in outcrop area, and becomes less pebbly to the south and west.|16-MAY-23
13477|Munmorah Conglomerate|Relationships and boundaries|Laterally equivalent in part to, and overlies Dooralong Shale. Overlain by the dominantly sandy Tuggerah Formation. Top of Munmorah Conglomerate is defined at top of dominantly pebbly sequence.|16-MAY-23
13477|Munmorah Conglomerate|Age reasons|?Late Permian-Early Triassic, contains Lunatisporites pellucidus microfloral assemblage zone of Helby (1973), Morgan (1976, 1977).|16-MAY-23
13477|Munmorah Conglomerate|Defn author|Standing Committee on Coalfield Geology of New South Wales, 1975.|16-MAY-23
13477|Munmorah Conglomerate|Proposed publication|The Geology of the Gosford and Lake Macquarie 1:100 000 Sheets.|16-MAY-23
13477|Munmorah Conglomerate|Status|1|16-MAY-23
13560|Murrumbateman Creek Formation|Name source|Named after Murrumbateman Creek, a tributary of the Yass River, NSW|16-MAY-23
13560|Murrumbateman Creek Formation|Unit history|None|16-MAY-23
13560|Murrumbateman Creek Formation|Type section locality|Low hills and creeks east of Murrumbateman Creek and along Gundaroo - Murrumbateman road (Canberra 1:100 000 sheet 8727). Laminated mudstone and siltstone pass gradationally up into thick beds of sandstone.  The sequence is upward facing and deformed into tight southwest-trending folds.|16-MAY-23
13560|Murrumbateman Creek Formation|Extent|Broad north-northeast-trending triangular belt extending about 1km north of Gunderoo-Murrumbateman road and south to 'Wantagong' homestead (GR 934/152).|16-MAY-23
13560|Murrumbateman Creek Formation|Thickness range|Estimated as 900m by Smith (1964).|16-MAY-23
13560|Murrumbateman Creek Formation|Lithology|Buff coloured laminated shale with sandstone interbeds which become thicker and more frequent to the top.|16-MAY-23
13560|Murrumbateman Creek Formation|Depositional environment|Marine-series of turbidite units deposited towards the distal edge of a submarine fan complex.|16-MAY-23
13560|Murrumbateman Creek Formation|Relationships and boundaries|Base unconformable on the Late Ordovician Pittman Formation. Upper boundary not exposed but Henderson (1978) mapped basal sandstone of the Canberra Formation (Camp Hill Sandstone Member) in apparent unconformity with the Murrumbateman Creek Formation. Contacts otherwise faulted.|16-MAY-23
13560|Murrumbateman Creek Formation|Age reasons|Early Silurian based on its stratigraphic position above the Pittman Formation and below the Canberra Formation.  Presence of laminated shale lithologically similar to Early Silurian State Circle Shale and similarly sandstone near the top typical of the Black Mountain Sandstone (Henderson 1978).|16-MAY-23
24413|Murrumbogie Intrusive Complex|Name source|Parish Murrumbogie, County Cunningham.|16-MAY-23
24413|Murrumbogie Intrusive Complex|Type section locality|GR 5385 9270, Narromine 1:250 000|16-MAY-23
24413|Murrumbogie Intrusive Complex|Extent|1 km north of Derriwong trig. Station.|16-MAY-23
24413|Murrumbogie Intrusive Complex|Thickness range|Approximately 1 km in diameter.|16-MAY-23
24413|Murrumbogie Intrusive Complex|Lithology|Hornblende melasyenite and hornblende meladiorite.|16-MAY-23
24413|Murrumbogie Intrusive Complex|Relationships and boundaries|Intrudes Cambro-Ordovician Girilambone Group.|16-MAY-23
24413|Murrumbogie Intrusive Complex|Age reasons|Early Devonian, because of similarity to Tout Complex.|16-MAY-23
24413|Murrumbogie Intrusive Complex|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982|16-MAY-23
24413|Murrumbogie Intrusive Complex|Proposed publication|A metallogenic study of Narromine 1:250 000 sheet.|16-MAY-23
24413|Murrumbogie Intrusive Complex|Defn Reference|86/25274 Defined P.328.|16-MAY-23
24413|Murrumbogie Intrusive Complex|Proposer|Bowman H.N., Richardson S.J., Dolanski J.|16-MAY-23
24413|Murrumbogie Intrusive Complex|Reserved? Yes/No|Yes|16-MAY-23
26071|Nangahrah Formation|Name source|The name is derived from Nangahrah Creek (Cobbadah 1:100 000 topographic map sheet 9037 GR 864246) where the unit is well exposed.|16-MAY-23
26071|Nangahrah Formation|Unit history|Woolomin Series, Benson 1911; Woolomin Group, Voisey 1959; Woolomin beds (Crook 1961) in part; Nangahrah beds (unpublished thesis name of Cuddy 1978).|16-MAY-23
26071|Nangahrah Formation|Type section locality|Stratotype: a type area is nominated as Nangahrah Creek (Cobbadah 1:100 0000 topographic map sheet 9037 GR 864246 to GR 891246).|16-MAY-23
26071|Nangahrah Formation|Extent|Similar rocks can be traced along strike from north of Bingara to as far south as Tamworth.|16-MAY-23
26071|Nangahrah Formation|Thickness range|Indeterminate due to deformation and poor exposure.|16-MAY-23
26071|Nangahrah Formation|Lithology|In places highly deformed. Local basalt overlain by ribbon-bedded, red chert up to 100 m thick. Above this argillite occurs interstratified with ?olistostromal deposits containing angular clasts, blocks and slabs of ribbon-bedded, red radiolarian chert, pillow basalt, and scarce limestone in a fine-grained matrix of basaltic rock fragments, chert and rather abundant angular quartz.|16-MAY-23
26071|Nangahrah Formation|Relationships and boundaries|Thrust contacts, structurally overlying Bobs Creek Formation and structurally overlain by Woodsreef Ophiolitic Melange.|16-MAY-23
26071|Nangahrah Formation|Age reasons|Radiolaria indicate a possible age range from Middle Devonian to Early Carboniferous.|16-MAY-23
26071|Nangahrah Formation|Correlations|Wisemans Arm Formation (introduced without definition by Leitch and Cawood 1980 without definition) is a possible correlative and the presence of similar lithologies in the type area of Woolomin Group has been noted by Leitch and Cawood (1980). However, the relationship of the Wisemans Arm Formation to the rest of the Woolomin Group is not clear (Ishiga et al. 1988).|16-MAY-23
26071|Nangahrah Formation|Proposed publication|Quarterly Notes Geological Survey NSW|16-MAY-23
26071|Nangahrah Formation|Comments|Metamorphism: Prehnite-pumpellyite facies.|16-MAY-23
26071|Nangahrah Formation|Category|2|16-MAY-23
26071|Nangahrah Formation|Reserved? Yes/No|Yes|16-MAY-23
13911|Narrow Plain Formation|Name source|Narrow Plain Property; 2.8 km west of DM Oaklands RDH 3 (GR DA 215587) where the formation was first observed.|16-MAY-23
13911|Narrow Plain Formation|Type section locality|34.37 m of sandstone, claystone and siltstone interbedded as found in bore DM Oaklands RDH 3; a few thin coal bands occur in middle of sequence. The top is identified by a thick coal seam, the Lanes Shaft Coal Member and the base is identified by a conglomerate overlying Permian marine sediments; from 93.04 m to 127.41 m.|16-MAY-23
13911|Narrow Plain Formation|Extent|The formation occurs in the subsurface only. Its subcrop extends for at least 500 km2 in the central portion of Jerilderie 1:250 000 sheet and probably further north.|16-MAY-23
13911|Narrow Plain Formation|Thickness range|Range 15 m to 35 m; lenses out towards the Eastern margin of the basin.|16-MAY-23
13911|Narrow Plain Formation|Lithology|Coarse sediments such as conglomerate and sandstones, loosely cemented, consisting mainly of milky white or clear quartz and grey quartzite, occur mainly towards the middle and the base of the sequence. Finer sediments such as claystones and siltstones, brown or grey, micaceous, with coaly lamellae, occur especially towards the lower half of the formation, associated with the lower coal bearing sequence. In this sequence, coal occurs generally in two or more bands, up to 0.30 m thick, separated by claystones, carbonaceous and possibly tuffaceous. A thick coal band, the Lane's Shaft Coal Member, occurs at the top of the formation.|16-MAY-23
13911|Narrow Plain Formation|Relationships and boundaries|Overlies the Permian Marine sediments; its basal conglomerate suggests unconformity. It is unconformably overlain by the Loughmore Formation (Palese and Morgan, in prep.). It includes the Lanes Shaft Coal Member (Palese and Morgan, in prep.) at top.|16-MAY-23
13911|Narrow Plain Formation|Age reasons|Impressions of Glossopteris, Vertebraria and Noeggerathiopsis can be observed on bedding planes. The microflora is dominated by Luekisporites and Parasaccites. Diagnostic elements include Didecitriletes ericianus, Marsupipollenites sinuosus, Dulhunryispora dulhuntyi and occasional Quadrisporites horridus. They identify the Lower Stage 5 microflora of Late Permian age (? Roadian).|16-MAY-23
13911|Narrow Plain Formation|Proposed publication|Records of the Geological Survey of NSW|16-MAY-23
13911|Narrow Plain Formation|Comments|Core of the mentioned bores is preserved in the NSW Dept of Mines Core Library in Londonderry, near Penrith. The major coal seam was destroyed for sampling purposes and the resulting analyses are available in the bore logs (GS 1974/090).|16-MAY-23
13911|Narrow Plain Formation|First Reference|79/20208|16-MAY-23
24423|Narwonah Rhyolite|Name source|Narwonah railway siding (GR 6258 0030, Narromine 1:250 000).|16-MAY-23
24423|Narwonah Rhyolite|Type section locality|At GR 6185 0000, Narromine 1:250 000 (most of section).|16-MAY-23
24423|Narwonah Rhyolite|Extent|The unit outcrops southwest of Narromine to the west of the Narwonah railway siding, over a distance of 2 km.|16-MAY-23
24423|Narwonah Rhyolite|Thickness range|200 m.|16-MAY-23
24423|Narwonah Rhyolite|Lithology|Rhyolite, tuff and chert.|16-MAY-23
24423|Narwonah Rhyolite|Relationships and boundaries|Has a facies relationship with the Trundle Group.|16-MAY-23
24423|Narwonah Rhyolite|Age reasons|Early Devonian from stratigraphic position.|16-MAY-23
24423|Narwonah Rhyolite|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982.|16-MAY-23
24423|Narwonah Rhyolite|Proposed publication|A metallogenic study of Narromine 1:250 000 sheet.|16-MAY-23
24423|Narwonah Rhyolite|Defn Reference|86/25274 Defined P.328.|16-MAY-23
24423|Narwonah Rhyolite|Proposer|Bowman H.N., Richardson S., Dolanski J.|16-MAY-23
24423|Narwonah Rhyolite|Reserved? Yes/No|Yes|16-MAY-23
24618|Newnes Formation|Name source|Village of Newnes, Wolgan Valley|16-MAY-23
24618|Newnes Formation|Unit history|New name (C S Bembrick)|16-MAY-23
24618|Newnes Formation|Type section locality|(1) Location: Placer Wolgan DDH 2 (231121 m E 1319262 m N Bungleboori 1:50 000 sheet, 8931-11); (2) Repository - NSW Dept of Mineral Resources Core Library, Londonderry.*  (*Reference Section: Browns Gap, GR 158600, Hampton 8930 - IV).|16-MAY-23
24618|Newnes Formation|Extent|Western Coalfield; Lithgow and Bungleboori 1:50 000 sheets. Also on parts of Glen Davis and Glen Alice sheets.|16-MAY-23
24618|Newnes Formation|General description|A most persistant unit, recognisable over virtually all of the Western Coalfield. The top most sandstone fines downward. Commonly bioturbated. Contains the "Ivanhoe Sandstone" of Branagan (1960) in limited areas near the basin margin. The top of the unit is recognised by the sharp transition from sandstone to coal, argillaceous and carbonaceous sediments of the Glen Davis Formation.|16-MAY-23
24618|Newnes Formation|Thickness range|(1) Type section - from 372.68 m to 380.78 m; thickness 8.10 m.  (2) Maximum recorded - 14.5 m.|16-MAY-23
24618|Newnes Formation|Lithology|Fine grained quartz-lithic sandstone and interbedded and laminated mudstone, siltstone and claystone.|16-MAY-23
24618|Newnes Formation|Relationships and boundaries|Conformably overlain by Glen Davis Formation and underlain by the Irondale Coal. Part of Charbon Sub-Group.|16-MAY-23
24618|Newnes Formation|Proposed publication|Australian Coal Geology|16-MAY-23
24618|Newnes Formation|Proposer|Bembrick C.S. - Robertson Research (Australia) Pty Limited|16-MAY-23
25341|Newton Boyd Granodiorite|Name source|Newton Boyd' School; GR 537304, Grafton 1:250 000 Sheet area (SH 56-6).|16-MAY-23
25341|Newton Boyd Granodiorite|Unit history|Previously considered to be part of the Mt Mitchell Adamellite (Brunker et al. 1976) occurring to the west of the Demon Fault. Partial chemical analyses by Archer (1975) suggest that these are two separate plutons.|16-MAY-23
25341|Newton Boyd Granodiorite|Type section locality|In the Boyd River to the east of Broadmeddows Homestead at GR 539303 (Grafton 1:250 000).|16-MAY-23
25341|Newton Boyd Granodiorite|Extent|This pluton is exposed over 25 km2 east of the Demon Fault in the vicinity of Newton Boyd School.|16-MAY-23
25341|Newton Boyd Granodiorite|Lithology|Medium-grained biotite granodiorite, mainly of equigranular texture but becoming slightly porphyritic near its margins.|16-MAY-23
25341|Newton Boyd Granodiorite|Relationships and boundaries|The pluton intrudes the Brooklana Beds producing a narrow albite-epidote hornfels zone. The western margin of the pluton has been truncated by the Demon Fault.|16-MAY-23
25341|Newton Boyd Granodiorite|Age reasons|Unknown, but it intrudes the Brooklana Beds which are postulated to be Late Palaeozoic.|16-MAY-23
25341|Newton Boyd Granodiorite|Defn author|Korsch R.J., Archer N.R., McConachy G.W., 1978|16-MAY-23
25341|Newton Boyd Granodiorite|Proposed publication|Journal and Proceedings of Royal Society of NSW|16-MAY-23
26078|Newtown Formation|Name source|"Newtown" homestead (Paterson 4602 9797).|16-MAY-23
26078|Newtown Formation|Unit history|Subdivision of the Gilmore Group (Rattigan 1966). Includes Martins Creek Andesite (Roberts).|16-MAY-23
26078|Newtown Formation|Type section locality|Two kilometers east of the Vacy Township.  Location of Type Section: Paterson 4613 9804 to 4584 9798. From Mt Breckin east to a prominent ridge 1 km east of the Paterson River.|16-MAY-23
26078|Newtown Formation|Extent|Found in the vicinity of Paterson (NE) Vacy, Martins Creek, Gresford, Lambs Valley, Myall Creek & Mirannie.|16-MAY-23
26078|Newtown Formation|Thickness range|a) At type section: 565 m.  B) Maximum known:|16-MAY-23
26078|Newtown Formation|Lithology|Basal Martins Creek Ignimbrite Member overlain by purplish lithic sandstone and conglomerate. The unit includes 490 ft below the top, the Vacy Ignimbrite Member.|16-MAY-23
26078|Newtown Formation|Relationships and boundaries|The unit overlies the Wallaringa Formation, the base of the Martins Creek Ignimbrite Member marks the base of the unit. The unit is overlain by the Mowbray Formation, the contact marked by the base of the Breckin Ignimbrite Member.|16-MAY-23
26078|Newtown Formation|Age reasons|Range from Upper Visean to Lower Westphalian. Dating of Martin's Creek Andesite indicates Upper-Visean and correlations by ANZAAS indicates the upper boundary.|16-MAY-23
26078|Newtown Formation|Defn author|Hamilton G., Hall G.C., Roberts J., 1974.|16-MAY-23
26078|Newtown Formation|Proposed publication|Journal of the Royal Soc. NSW|16-MAY-23
26078|Newtown Formation|Defn approved by|From xerox copy sent by NSW Stratigraphic Nomenclature Sub-Committee.|16-MAY-23
26078|Newtown Formation|Proposer|Hamilton G., Hall G.|16-MAY-23
26078|Newtown Formation|Reserved? Yes/No|G. Hamilton|16-MAY-23
14148|Nimbin Rhyolite|Name source|Nimbin' village; GR 217366, Nimbin 1:50 000 sheet 9540-IV.|16-MAY-23
14148|Nimbin Rhyolite|Type section locality|500 m of rhyolite flows and minor pyroclastics from the base on the eastern side of Terania Creek (284400) to the summit of Mt Matheson (294428). |16-MAY-23
14148|Nimbin Rhyolite|Extent|The unit is exposed over 400 km2 of mainly elevated, heavily vegetated areas north-east and east of Nimbin, mainly within the northern half of the Rosebank 1:50 000 sheet 9540-I area.|16-MAY-23
14148|Nimbin Rhyolite|Thickness range|Range 50-500 m. Highly variable over short distances.|16-MAY-23
14148|Nimbin Rhyolite|Lithology|Two feldspar rhyolites, including aphyric and porphyritic flows and pyroclastics (tuffs and breccias). A glassy selvage up to 10 m thick is preserved at the base of many flows. Very minor rhyodacite. A few basaltic flows intercalated with the rhyolites in the Whian Whian State Forest area.|16-MAY-23
14148|Nimbin Rhyolite|Relationships and boundaries|Conformably overlies the Lismore Basalt and is overlain by the Blue Knob Basalt (McElroy 1962). The base is marked by an abrupt change from the subalkaline basaltic rocks of the Lismore Basalt to rhyolitic flows and pyroclastics; the top by an equally abrupt change back to subalkaline basalts comprising the Blue Knob Basalt. Belongs to Lamington Volcanics (Gp).|16-MAY-23
14148|Nimbin Rhyolite|Age reasons|No rhyolites from the southern portion of the Tweed Shield Volcano have been dated. Rhyolites from the Binna Burra Rhyolite in the northern portion have been dated at about 21 m.y. and the volcanic sequence as a whole at 23-20 m.y. by K-Ar methods (Wellman and McDougall, 1974).|16-MAY-23
14148|Nimbin Rhyolite|Defn author|Duggan M.B., Mason D.R., 1978|16-MAY-23
14148|Nimbin Rhyolite|Proposed publication|Journal of the Geological Society of Australia|16-MAY-23
14148|Nimbin Rhyolite|Comments|The name 'Nimbin Rhyolite' was originally proposed by McElroy (1962). It is here redefined to exclude the rhyolites west and south of Nimbin, remnants of a single flow and now thought to be stratigraphically lower than the Nimbin Rhyolite.|16-MAY-23
72992|Nobbys Beach Lamprophyre|Name source|Nobbys Beach, Port Macquarie.|16-MAY-23
72992|Nobbys Beach Lamprophyre|Type section locality|The type area of the unit is the headland at the northern end of Nobbys Beach (31o26'42"S 152o55'45"E).|16-MAY-23
72992|Nobbys Beach Lamprophyre|Description at type locality|Nobbys Beach Lamprophyre dykes are composed of fine-grained dark green to almost black rocks that show dark chilled margins rarely exceeding 30 mm wide. Some dykes have an internal zoning resulting from variations in the abundance of small (<4 mm)spherical ocelli and a few show subtle flow layering. Small phenocrysts of mafic minerals are present but rarely prominent. The dykes range from 0.05 to 1 m wide although most are less than 0.3 m and are on average notably less wide than those of either the Karikeree Metadolerite or the Sea Acres Dolerite.|16-MAY-23
72992|Nobbys Beach Lamprophyre|Extent|Narrow lamprophyre dykes, first recognised by Barron et al. (1976) that are a widespread although minor component of the Port Macquarie Block.|16-MAY-23
72992|Nobbys Beach Lamprophyre|Lithology|...as above...|16-MAY-23
72992|Nobbys Beach Lamprophyre|Relationships and boundaries|Intrusive into the Watonga Formation, Port Macquarie Serpentinite, Tacking Point Gabbro and Karikeree Metadolerite.|16-MAY-23
72992|Nobbys Beach Lamprophyre|Age reasons|(?) Permian based on geochemical affinity with the 290 - 250 Ma Clarence River Supersuite (Och 2007; Och and Leitch, in prep).|16-MAY-23
72992|Nobbys Beach Lamprophyre|References|BARRON, B. J., SCHEIBNER, E. and SLANSKY, E. 1976. A dismembered ophiolite suite at Port Macquarie, New South Wales. Records of the Geological Survey of New South Wales 18, 69-102.OCH, D. J. 2007. Eclogite, serpentinite, mélange and mafic intrusive rocks: manifestation of long-lived Palaeozoic convergent margin activity, Port Macquarie, eastern Australia. Unpublished PhD thesis, University of Technology, Sydney.OCH, D. J. and LEITCH, E. C. (in prep) New and revised lithostratigraphic units from the Port Macquarie Block, northeastern New South Wales. Quarterly Notes ¿ Geological Survey of New South Wales.|16-MAY-23
14280|North Ridge Basalt|Name source|North Ridge is a locally used name for east-west trending ridge adjacent to north coast of Lord Howe Island, rising to 209 m at Malabar. Not named on map of Lord Howe Island (Department of Lands, Sydney, 1966, 1:15840). Term coined by Standard (1963) as North Ridge volcanics.|16-MAY-23
14280|North Ridge Basalt|Unit history|Standard (1963) called these rocks the North Ridge volcanics, and Game (1970) referred to them as the "horizontal altered series".|16-MAY-23
14280|North Ridge Basalt|Type section locality|In North Ridge, with typical exposures along north coast of Lord Howe Island over 2 km. Accessible at Old Gulch.|16-MAY-23
14280|North Ridge Basalt|Extent|Underlies much of northern one-third of Lord Howe Island, cropping out in North Ridge, extending from Neds Beach to the west coast, in Transit Hill and on Mutton Bird Island, over an area of about 4 km2.|16-MAY-23
14280|North Ridge Basalt|Thickness range|200 m +|16-MAY-23
14280|North Ridge Basalt|Lithology|Sequence of basalt (tholeiitic) lava flows dipping gently to the northwest in North Ridge. Flows 1 to 10 m thick, averaging 2 to 5 m thick. Fragmental, often oxidized tops and bottoms of flows, with more massive interiors.|16-MAY-23
14280|North Ridge Basalt|Relationships and boundaries|Overlies with erosional disconformity the Malabar Tuff Complex. Overlain by much younger Neds Beach Calcarenite and alluvial deposits.|16-MAY-23
14280|North Ridge Basalt|Age reasons|K-Ar ages on five samples range from 6.6 +/- 0.2 Ma to 7.2 +/- 0.1 averaging 6.9 +/- 0.2 Ma, and therefore probably Late Miocene. Normal magnetic polarity.|16-MAY-23
14280|North Ridge Basalt|Proposed publication|Submitted to J. Geol. Soc. Australia|16-MAY-23
14280|North Ridge Basalt|Comments|Notes: This unit is interpreted as the main shield building phase for the large basaltic volcano, of which Lord Howe Island is an erosional remnant.|16-MAY-23
14280|North Ridge Basalt|Defn approved by|See letter 1/7/82 on NSW file from T. Russell.|16-MAY-23
26082|Nowranie Creek Formation|Name source|Nowranie Creek; situated 2 km E of bore DM Oaklands RDH 17, GR DA 162748, Urana 1:100 000 Sheet.|16-MAY-23
26082|Nowranie Creek Formation|Type section locality|3.87 m of laminated claystone as found in bore DM Oaklands RDH 17 (GR DA 162748), Urana 1:100 000 sheet, from 175.56 m to 179.43 m. Sharp top and gradational base. Its top is identified by a coarse sandstone and its base grades into carbonaceous material and/or coal.|16-MAY-23
26082|Nowranie Creek Formation|Extent|The formation occurs only in the subsurface. Its subcrop extends over about 500 km2 in the central portion of Jerilderie 1:250 000 sheet (SI 55-14) and probably further north.|16-MAY-23
26082|Nowranie Creek Formation|Thickness range|Range from a few centimetres to over 7 metres.|16-MAY-23
26082|Nowranie Creek Formation|Lithology|Claystone dark grey, carbonaceous and claystone light grey to buff; laminated; minor slumping in upper half; abundant coaly partings; claystone dark grey is predominant. Claystone laminated is generally weathered and iron stained at top. In Oaklands-Coorabin area the formation is represented mainly by a pink clay band underlain by sandstone and/or conglomerate.|16-MAY-23
26082|Nowranie Creek Formation|Relationships and boundaries|It unconformably overlies the Loughmore Formation (Palese and Morgan, in prep.). It is unconformably overlain by Tertiary sediments of the Renmark Beds (Harris, 1966) to the south and by Triassic sediments to the north. The nature of the contact is not known.|16-MAY-23
26082|Nowranie Creek Formation|Age reasons|Plant remains are very scarse and poorly preserved. Microflora is dominated by bisaccate grains. Diagnostic for this unit are Tigrisporites playfordi and Falcisporites australis. Common Peltacystia spp. and Quadrisporites horridus.|16-MAY-23
26082|Nowranie Creek Formation|Proposed publication|Records of the Geological Survey of NSW|16-MAY-23
26082|Nowranie Creek Formation|Comments|a) Core of the mentioned bores is preserved in the NSW Dept of Mines Core Library in Londonderry, near Penrich.  b) Microflora from samples of bore A.O.G. Jerilderie RDH 1 shows the existence of Triassic sediments that, however, have not as yet been lithologically identified.|16-MAY-23
26082|Nowranie Creek Formation|First Reference|79/20208|16-MAY-23
26082|Nowranie Creek Formation|Proposer|Palese G.W.|16-MAY-23
24434|Noyeau Hollow Andesite|Name source|Noyeau Hollow Creek which runs east-west through Woodstock.|16-MAY-23
24434|Noyeau Hollow Andesite|Type section locality|GR 1808 8390|16-MAY-23
24434|Noyeau Hollow Andesite|Extent|The formation crops out in a belt over 100 km2 to the northwest and west of the Rothery Tuff, extending west of Walli, south of Cowra.|16-MAY-23
24434|Noyeau Hollow Andesite|Thickness range|1500 to 3000 m.|16-MAY-23
24434|Noyeau Hollow Andesite|Lithology|The formation consists mainly of aphanitic and porphyritic lavas, both equally abundant. They vary from light to dark grey to greenish grey in colour, weathering to purplish brown. Plagioclase phenocrysts (20-50%) (1-4 mm) are most common in the porphyritic types. Pyroxene phenocrysts also present. Vesicles are present mainly in the aphanitic types. The groundmass for both types consists of opaques and altered microlaths of plagioclase and chlorite.|16-MAY-23
24434|Noyeau Hollow Andesite|Relationships and boundaries|The Noyeau Hollow Andesite with the underlying Rothery Tuff comprise the Walli Sub Group. The Cliefden Caves Limestone of Middle to Late Ordovician age conformably overlies the Noyeau Hollow Andesite.|16-MAY-23
24434|Noyeau Hollow Andesite|Age reasons|The Noyeau Hollow Andesite is believed to be of Early Ordovician age although no fossil evidence exists for this.|16-MAY-23
24434|Noyeau Hollow Andesite|Proposed publication|Geological Survey of NSW Record|16-MAY-23
24434|Noyeau Hollow Andesite|Proposer|Richardson S, Bowman H|16-MAY-23
24434|Noyeau Hollow Andesite|Reserved? Yes/No|Yes|16-MAY-23
25356|Nundooka Sandstone|Name source|Nundooka Station|16-MAY-23
25356|Nundooka Sandstone|Type section locality|The type section is made ENE from ~620 m east of Sandstone Dam. (GR 4714 1708 (base) to 4775 1414) 1:250 000 map, Cobham Lake.|16-MAY-23
25356|Nundooka Sandstone|Extent|The formation which trends north-south is bounded by the Nundooka Creek Fault (in the west) and the Western boundary Fault in the east, has an outcrop area of ~50 km2.|16-MAY-23
25356|Nundooka Sandstone|Thickness range|The formation is ~1425 m thick at the type section.|16-MAY-23
25356|Nundooka Sandstone|Lithology|The formation is composed of fine and very fine arenite. Six stratigraphic units (1. Basal friable arenite; 2. Lower light grey arenite; 3. Quartzose arenite; 4. Central light grey fine arenite; 5. "Marker Bed" arenite; and 6. Upper light-grey arenite) are recognised.|16-MAY-23
25356|Nundooka Sandstone|Relationships and boundaries|The formation is the fault contact at its base (Nundooka Creek Fault) and its top (Western Boundary Fault). It may overlie the Coco Range Sandstone subsurface.|16-MAY-23
25356|Nundooka Sandstone|Age reasons|Late Devonian based on Famennian fossils found in the "Marker Bed" arenite and upper light-grey arenite.|16-MAY-23
25356|Nundooka Sandstone|Proposed publication|Australian Journal of Earth Sciences|16-MAY-23
25356|Nundooka Sandstone|Comments|(no type section was designated by Ward et al. 1969).|16-MAY-23
25356|Nundooka Sandstone|Reserved? Yes/No|Yes|16-MAY-23
25356|Nundooka Sandstone|Status|1|16-MAY-23
24437|Ondyong Point Formation|Name source|Ondyong Point, a small spur at the end of Lake George (GR 206/205).|16-MAY-23
24437|Ondyong Point Formation|Unit history|None.|16-MAY-23
24437|Ondyong Point Formation|Type section locality|A fully cored type section is unavailable as recovery from the unit was poor.  Representative sections are designated from the best recovered intervals of core from the BMR drillholes C251 (36.0-48.2m), C352 (42.5-48.0m), C353 (58.0-71.0m) and C358 (40.0-59.0m). Over other intervals partially weathered sand, silt and clay have been cored with recovery levels mostly in excess of 90%.|16-MAY-23
24437|Ondyong Point Formation|Extent|Lake George drainage basin (Canberra 1:100 000 sheet 8727).  The formation is only known in the subsurface. It may extent laterally beneath alluvial plains marginal to the lake.|16-MAY-23
24437|Ondyong Point Formation|Thickness range|A maximum known thickness of 53m in BMR drillhope C354 and minimum of 10m on C360.|16-MAY-23
24437|Ondyong Point Formation|Lithology|Horizontally bedded sand, silt and clay. Sandy units near the base maybe coarse-grained and graded.  Towards the top of the unit it is dominated by mottled and laminated clay. Reddish-brown ferrigineous weathering profiles occur intermittently throughout the unit. Gamma and neutron logs record lithological constraints (Abell, 1985a). The relative distribution of clay and non-clay minerals is given in Abell (1985b).|16-MAY-23
24437|Ondyong Point Formation|Depositional environment|Transitional fluvio-lacustrine sequence.|16-MAY-23
24437|Ondyong Point Formation|Relationships and boundaries|The base of formation is arbitrarily placed at the top of the deep weathering profile in the Gearys Gap Formation - this boundary may represent a disconformity.  The formation is conformably overlain by the Bungendore Formation: the upper boundary is taken at the highest and most persistent sand bed at the top of the formation which is readily picked from gamma and neutron logs.  The unit grades laterally into alluvial sediments at the northen, eastern and southern margins of the Lake George basin. It is truncated by the Lake George Fault.|16-MAY-23
24437|Ondyong Point Formation|Age reasons|A pollen assemblage in carboneous clays gives a preliminary age of Late Miocene (Truswell, 1984).|16-MAY-23
24437|Ondyong Point Formation|Correlations|Based on pollens the formation may at least be the same age as the Triporopollenites bellus zone of the Gippsland Basin and perhaps rainforest-dominated intervals in the Lachlan River valley (Truswell, 1984).|16-MAY-23
24440|Onslow Granodiorite|Name source|Parish of Onslow,  Co. Beresford|16-MAY-23
24440|Onslow Granodiorite|Unit history|Previously regarded as part of the Michelago Granite.|16-MAY-23
24440|Onslow Granodiorite|Type section locality|Well represented at GR 014323|16-MAY-23
24440|Onslow Granodiorite|Description at type locality|Medium-grained mafic rich (20%) granodiorite with bluish-coloured quartz crystals, the latter a result of the mild granulation the rock appears to have undrgone in its last phases of crystallisation. Thin section analysis reveals plagioclase (andesine), quartz, biaotite, hornblende and alkali feldspar with minor magnetite and rare zircon and apatite. Xenoliths with a higher mafic content are present.|16-MAY-23
24440|Onslow Granodiorite|Extent|Crops out along the eastern margin of the northern body of the Michelago Igneous Complex, to the south of the headwaters of Cockatoo Creek, between GR 029348 and GR 015311, Michelago 1:100 000 Geological Sheet.  Size: 2.2 km2.|16-MAY-23
24440|Onslow Granodiorite|Relationships and boundaries|Bounded to the west by the Micaligo Adamellite, a larger phase of the Michelago Igneous Complex. The Onslow Granodiorite intrudes Late Ordovician Foxlow Beds.|16-MAY-23
24440|Onslow Granodiorite|Age reasons|K-Ar analyses of biotite by AMDEL indicate an age of 395 +/- 8 m.y. This indicates intrusion at the close of the Silurian Period.|16-MAY-23
24440|Onslow Granodiorite|Proposed publication|Geological Survey of NSW 1:100 000 Notes Series|16-MAY-23
39261|Ourimperee Ignimbrite Member|Name source|After the property Ourimperee (0252580E 6577900N Gunnedah 1:25,000 sheet; Geeve 1995).|16-MAY-23
39261|Ourimperee Ignimbrite Member|Unit history|Ourimperee Ignimbrite Member (Geeve 1995).|16-MAY-23
39261|Ourimperee Ignimbrite Member|Type section locality|Type section taken from 30o54'29"S 150o24'00"E to 30o54'30"S 150o23'52"E (0251502E 6577686N to 0251310E 6577642N Gunnedah 1:25,000 sheet) from the base of section 509, 1 km west-southwest of Ourimperee.|16-MAY-23
39261|Ourimperee Ignimbrite Member|Extent|Crops out discontinuously over about 3 km on eastern margin of Gunnan Ridge in the vicinity of Ourimperee; tentatively identified on the southeastern edge of the ridge.|16-MAY-23
39261|Ourimperee Ignimbrite Member|Thickness range|115 m in the type section.|16-MAY-23
39261|Ourimperee Ignimbrite Member|Lithology|Pink, red or beige, unwelded to moderately welded rhyolitic ignimbrite with quartz, plagioclase, K-feldspar, biotite, opaque minerals and pumices; groundmass micropoikilitic. An XRF analysis (Geeve 1995 MU55237) indicates a rhyolitic composition.|16-MAY-23
39261|Ourimperee Ignimbrite Member|Relationships and boundaries|Underlain by an unnamed andesite in section 109.|16-MAY-23
39261|Ourimperee Ignimbrite Member|Age reasons|Early Namurian.|16-MAY-23
24448|Owendale Intrusive Complex|Name source|Owendale homestead GR 5511 9584, Narromine 1:250 000 sheet.|16-MAY-23
24448|Owendale Intrusive Complex|Unit history|Yates 1966 (unpubl.) called it the Kelvin Grove intrusion. Stroud 1973 (unpubl.) included it within his description of the Tout Complex.|16-MAY-23
24448|Owendale Intrusive Complex|Type section locality|No surface outcrop. The intrusion is defined by diamond and auger drilling. A variety of compositions have been detected.|16-MAY-23
24448|Owendale Intrusive Complex|Extent|This intrusion lies 11 km north of Fifield.  Size: The complex is thought to be circular in shape with 6 km diameter.|16-MAY-23
24448|Owendale Intrusive Complex|Lithology|Composition: Auger holes in the northwest area intersected hornblende meladiorite, hornblende diorite, biotite diorite. Diamond drill holes in the southern part intersected biotite pyroxenite, lmeladiorite, hornblende serpentinite.|16-MAY-23
24448|Owendale Intrusive Complex|Relationships and boundaries|Intrudes Cambro-Ordovician Girilambone Beds.|16-MAY-23
24448|Owendale Intrusive Complex|Age reasons|Thought to be Early-Middle Devonian through similarity with Tout Complex.|16-MAY-23
24448|Owendale Intrusive Complex|Defn author|Bowman H., Richardson S., Dolanski J., 1982|16-MAY-23
24448|Owendale Intrusive Complex|Proposed publication|A metallogenic study of the Narromine 1:250 000 sheet.|16-MAY-23
24448|Owendale Intrusive Complex|Defn Reference|86/25274 Defined 329.|16-MAY-23
24448|Owendale Intrusive Complex|Proposer|Bowman H., Richardson S., Dolanski J.|16-MAY-23
24448|Owendale Intrusive Complex|Reserved? Yes/No|Yes|16-MAY-23
14788|Palerang Formation|Name source|Palerang trig. Station, GR 358762 Braidwood 1:100 0000 sheet.|16-MAY-23
14788|Palerang Formation|Unit history|On the Canberra 1:250 000 geological sheet 2nd edn. (Best et al., 1964), the Palerang Formation is shown partly as Bombay Volcanics and partly as Mount Fairy Beds.|16-MAY-23
14788|Palerang Formation|Type section locality|Type section at GR 359776, Braidwood 1:100 000 sheet (cuttings and other outcrops in fire trail north of Braidwood - Hoskingtown road).|16-MAY-23
14788|Palerang Formation|Extent|The unit is exposed over about 50 km2 in high country about 15 km west of Braidwood.|16-MAY-23
14788|Palerang Formation|Thickness range|Exposed thickness 920 m (minimum).|16-MAY-23
14788|Palerang Formation|Lithology|Massive, occasionally graded, grey to fawn quartz and quartz-lithic arenite; brown siltstone, occasionally cross-bedded on small scale; micaceous shale.|16-MAY-23
14788|Palerang Formation|Relationships and boundaries|Conformably overlies the Late Silurian Bombay Volcanics with which its contact is gradational. The base of the Palerang Formation is defined as the top of the uppermost volcanic unit (crystal tuff, ignimbrite or rhyolite) in the Bombay Volcanics. The Palerang Formation is unconformably overlain by the late Early Devonian Tarago Conglomerate and is intruded by the Early Devonian Boro Granite. The unit is faulted against Ordovician metasediments, the Boro Granite and the Late Silurian De Drack Formation.|16-MAY-23
14788|Palerang Formation|Age reasons|Late Silurian to Early Devonian. Evidence as above. No fossils are known from the unit.|16-MAY-23
14788|Palerang Formation|Proposed publication|Felton E.A. and Huleatt M.B., 1975. Geology of the Braidwood 1:100 000 Sheet. Geological Survey NSW, Sydney.|16-MAY-23
14788|Palerang Formation|Defn Reference|79/20208|16-MAY-23
39262|Penryn Rhyolite Member|Name source|After the property Penryn (0240400E 6599600N Willuri 1:25,000 sheet).|16-MAY-23
39262|Penryn Rhyolite Member|Type section locality|Type section taken at the northeastern crest of Tulcumba Ridge between 30o43'21"S 150o20'13"E (0245000E 6598112N) and 30o43'25"S 150o20'12"E (0244972E 6597978N Willuri 1:25,000 sheet).|16-MAY-23
39262|Penryn Rhyolite Member|Extent|In the core and flanks of a syncline on the northeastern part of Tulcumba Ridge. A rhyolite flow (Liang 1989, XRF MU47961) identified as the lower part of this unit is present in a quarry at 0243500E 6501400N near the Gunnedah-Boggabri-Manilla road junction. Other XRF analyses (Liang 1989 MU47971, MU47976) of lavas near the base and top of the unit indicate a rhyolitic and dacitic composition, respectively.|16-MAY-23
39262|Penryn Rhyolite Member|Thickness range|Ranges from 50 m in the type section to 10 m.|16-MAY-23
39262|Penryn Rhyolite Member|Lithology|Basal flow followed by thicker ignimbrite containing at least one thin bed of obsidian. Flow beige to orange, fine to very fine grained, with small oriented plagioclase, K-feldspar, biotite and minor opaque minerals and elongate stringers of chalcedony and zeolite. Overlying ignimbrite  beige to rarely purple, moderately welded, with plagioclase, K-feldspar, opaque minerals and pumice fragments; groundmass spherulitic to micropoikilitic.|16-MAY-23
39262|Penryn Rhyolite Member|Age reasons|Namurian|16-MAY-23
23904|Pigeon Square Gabbro|Name source|Pigeon Square Creek, GR 380650 Tantangara 1:100 000 Sheet area.|16-MAY-23
23904|Pigeon Square Gabbro|Type section locality|On Peppercorn Trail from GR 408620 to 394630. This gives a section through the layered intrusion, with olivine gabbro at the base (west) through leucogabbro and into hornblende gabbro and dolerite at the top (east).|16-MAY-23
23904|Pigeon Square Gabbro|Extent|A gabbro stock about 2 km across at the headwaters of Pigeon Square Creek and Feints Creek.|16-MAY-23
23904|Pigeon Square Gabbro|Lithology|Two pyroxene bearing leucogabbro, hornblende gabbro, dolerite, olivine gabbro, gabbro pegmatite.|16-MAY-23
23904|Pigeon Square Gabbro|Relationships and boundaries|The gabbro intrudes the Middle Silurian Goobarragandra Beds and the Kennedy Range Granite. It is chemically related to the Micalong Swamp Basic Igneous Complex.|16-MAY-23
23904|Pigeon Square Gabbro|Age reasons|Unknown, but probably Late Silurian as the Micalong Swamp Basic Igneous Complex has been dated by K/Ar method at 430 +/- 9 m.y.|16-MAY-23
23904|Pigeon Square Gabbro|Proposed publication|Bureau of Mineral Resources Bulletin.|16-MAY-23
23904|Pigeon Square Gabbro|Proposer|Owen M., Wyborn D.|16-MAY-23
37909|Pine Cliffs Rhyolite Member|Name source|Named after the property `Pine Cliffs' GR369655 Eulowrie I:25,000 sheet.|16-MAY-23
37909|Pine Cliffs Rhyolite Member|Unit history|Pine Cliffs Rhyolite (Opdyke et al. 2000).  Named informally by Hocking (1973).|16-MAY-23
37909|Pine Cliffs Rhyolite Member|Geomorphic expression|Ridge forming.|16-MAY-23
37909|Pine Cliffs Rhyolite Member|Type section locality|In a cutting on the Back Creek-Narrabri road at GR366662 Eulowrie 1:25,000 sheet.|16-MAY-23
37909|Pine Cliffs Rhyolite Member|Extent|Extends along a ridge line 2.5 km long between the properties `Pine Cliffs' and `Bexley' Eulowrie 1:25,000 sheet.|16-MAY-23
37909|Pine Cliffs Rhyolite Member|Thickness range|>25 m|16-MAY-23
37909|Pine Cliffs Rhyolite Member|Lithology|Pink to beige, unwelded ignimbrite containing scattered quartz, feldspar, minor opaque minerals, fragments of pumice and rare ferruginised volcanic rock fragments. The groundmass is micropoikilitic.|16-MAY-23
37909|Pine Cliffs Rhyolite Member|Depositional environment|Ignimbrite.|16-MAY-23
37909|Pine Cliffs Rhyolite Member|Relationships and boundaries|Stratigraphically above the Bexley Rhyolite Member within the southern part of the Kathrose block.|16-MAY-23
37909|Pine Cliffs Rhyolite Member|Age reasons|Carboniferous (Namurian)|16-MAY-23
37909|Pine Cliffs Rhyolite Member|References|HOCKING R.M. 1973. The Carboniferous Back Creek-Pound Creek sequence, southwest of Caroda, New South Wales. BSc (Hons) thesis, University of new England, Armidale (unpubl.).OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
40758|Piney Range Member|Name source|From Piney Range homestead (0243600E 6603400N Willuri 1:25 000).|16-MAY-23
40758|Piney Range Member|Type section locality|The type section is taken from ignimbrite bed a at locality 430-19 30o38'12"S, 150o19'30"?E (0243611E 6607595N Willuri 1:25 000 sheet), projected 100 m laterally into section 297, to the top of ignimbrite bed c at locality 297-12. The initial part of the section along Mihi Creek was measured to locality 297-6 at 30o38'13"S 150o19'13"E (0243174E 6607545N Willuri 1:25 000 sheet). Because of lack of further outcrop, the section was linked southwards with locality 297-12 at 30o38'57"?S,150o18'59"E (ignimbrite bed c, 02428160E 6606196N Willuri 1:25 000 sheet) by traverse; cliffs prevent ready access to ignimbrite bed b east of Haystack Rock (0243340E 6604800N Willuri 1:25 000 sheet).|16-MAY-23
40758|Piney Range Member|Extent|The Piney Range Member contains three beds of purple ignimbrite, a, b and c. The base of the member is taken at the base of ignimbrite bed a and the top either at the upper surface of ignimbrite bed c or, where that bed is absent, the top of ignimbrite bed b. The member crops out adjacent to the Plagyan Thrust and extends from the southern part of Nioka to 2 km west of Arizona. It extends westwards into the region adjacent to Dripping Rock and Mallee. Beds a and possibly b crop out on the northeastern margin of Tulcumba Ridge; ?bed b extends southwards to a tributary of Rangira Creek. Additional outcrops tentatively referred to bed a may be present at Connors Creek beneath the Bideroi Ignimbrite Member. Beds a and b are present throughout the greater part of the member. Bed c is restricted to the eastern margin of an amphitheatre south of Mihi Creek and to a small area south and southwest of Dripping Rock.|16-MAY-23
40758|Piney Range Member|Thickness range|The member ranges in thickness from a maximum of about 400 m in section 297, in which all three ignimbrite beds are present, to about 230 m in section 406 at Mallee south. The range of thickness of the ignimbrite beds is: a 10-20 m; b 20-35 m; and c 12 m.|16-MAY-23
40758|Piney Range Member|Lithology|Ignimbrite beds a-c are purple to grey, slightly welded to unwelded, with scattered phenocrysts of plagioclase, minor K-feldspar, quartz, ? biotite and opaque minerals. Pumice fragments are rare. Shards are oriented, thick and accompanied by slightly distorted bubbles. Groundmass is micropoikilitic or spherulitic. In the region between Mallee and Dripping rock, ignimbrite bed b is more strongly welded and has more abundant quartz. XRF analyses of ignimbrite bed b indicate a rhyolitic or rhyodacitic composition (sample G1 Table 1 and sample 437-1 Table 2, Appendix 3; Liang (1989 MU47952,3), respectively. Conglomerate, volcanolithic sandstone and ash-rich siltstone are Intercalated within the Piney Range Member (Figure 5).|16-MAY-23
40758|Piney Range Member|Age reasons|SHRIMP AS3 ages for ignimbrite bed b on Piney Range and Tulcumba Ridge are 317.7?2.4 (sample 512-1A, Figure 10b) and 317.0?3.5 Ma (sample 437-1, Figure 10c), respectively. Namurian.|16-MAY-23
27221|Pitt Town Sand|Name source|Village of Pitt Town (GR 855503, Windsor 1:63 360).|16-MAY-23
27221|Pitt Town Sand|Unit history|Included in Windsor Formation of Bell (1966).|16-MAY-23
27221|Pitt Town Sand|Type section locality|5 m of medium to coarse grained, clayey quartz sand exposed in a sand pit of Farley and Lewers Ltd (GR 863508, Windsor 1:63 360).|16-MAY-23
27221|Pitt Town Sand|Extent|Formation exposed over approximately 4 km2 north of the village of Pitt Town.|16-MAY-23
27221|Pitt Town Sand|Thickness range|Range 1-8 m.|16-MAY-23
27221|Pitt Town Sand|Lithology|Indistinctly mottled, medium-grained, clayey quartz sand with scattered feldspar and chert grains. Grains are angular to sub-rounded in shape and poorly sorted. Clay content increases with depth. Isolated igneous? pebbles and iron cemented sand aggregates scattered throughout.|16-MAY-23
27221|Pitt Town Sand|Relationships and boundaries|Probably disconformable on the underlying Londonderry Clay. Erosional upper surface.|16-MAY-23
27221|Pitt Town Sand|Age reasons|No floral or faunal assemblages available for dating. Pitt Town Sand overlies the Londonderry Clay, the latter affected by late Miocene or Early Pliocene Lataeritisation (Gobert in press). Unit occurs on a higher river terrace than the Lowlands Formation which is thought to be Pleistocene age. Pitt Town Sand is thus thought to be Pliocene.|16-MAY-23
27221|Pitt Town Sand|Defn author|Gobert V., 1978.|16-MAY-23
27221|Pitt Town Sand|Proposed publication|Gobert Val, _______. Cumberland Basin Stratigraphy in The geology of the Penrith 1:100 000 sheet by C. Herbert Geol. Survey NSW, Sydney (in press).|16-MAY-23
37911|Plagyan Ignimbrite Member|Name source|After Mt Plagyan, GR394254 Plagyan 1:25,000 sheet|16-MAY-23
37911|Plagyan Ignimbrite Member|Unit history|Plagyan Rhyolite Member (White 1965) Plagyan Rhyodacite Tuff Member (Brown et al. 1990)|16-MAY-23
37911|Plagyan Ignimbrite Member|Geomorphic expression|Strong rib- to cliff-forming.|16-MAY-23
37911|Plagyan Ignimbrite Member|Type section locality|No type locality has been designated. More detailed mapping of individual flow units in the region south of the Nandewar Range is required before a definitive section is designated.|16-MAY-23
37911|Plagyan Ignimbrite Member|Extent|Major outcrops occur west of the Plagyan Fault on the southern slopes of the Nandewar Range, particularly in headwaters of Maules Creek, Plagyan State Forest, and between Middle and Horsearm Creeks in Rusden State Forest. Erosional remnants are present in axial regions of the Rocky Creek Syncline south of `Myola' (GR487264 Plagyan 1:25,000 sheet) and on Tareela Creek. From Tareela Creek the member extends northwards on both limbs of the syncline, a thin dacite flow extending slightly north of Boomi Creek.|16-MAY-23
37911|Plagyan Ignimbrite Member|Thickness range|Up to ~300 m|16-MAY-23
37911|Plagyan Ignimbrite Member|Lithology|East of the Plagyan Fault, the bulk of the Plagyan Ignimbrite consists of a crystal-rich, moderately welded, red-brown to grey, rhyolitic ignimbrite containing embayed quartz, plagioclase (frequently zoned), biotite and/or hornblende, opaque minerals and rare pumices. West of the Plagyan Fault, rhyolites in the southern Nandewar region have the same mineral assemblage as in those in the east but differ in being more strongly welded. Dark grey to black, hornblende-rich dacitic ignimbrite is also widely distributed within the Plagyan Ignimbrite. Dacite constitutes the major part of the member in the vicinity of Boomi Creek and is also present on Myola at GR478269 (Plagyan 1:25,000 sheet), on the flanks of Old Man Ridge, 4.5 km southeast of Round Mountain GR426656 Horton 1:25,000 sheet), and in the Nandewar Range at Stony Creek (GR363280 Plagyan 1:25,000 sheet).|16-MAY-23
37911|Plagyan Ignimbrite Member|Depositional environment|Ignimbrite.|16-MAY-23
37911|Plagyan Ignimbrite Member|Relationships and boundaries|Usually the oldest ignimbrite member within the Rocky Creek Conglomerate.|16-MAY-23
37911|Plagyan Ignimbrite Member|Age reasons|Carboniferous (Namurian).|16-MAY-23
37911|Plagyan Ignimbrite Member|Comments|The change in name reflects the presence of more than one lithology and the depositional nature of the unit.|16-MAY-23
37911|Plagyan Ignimbrite Member|References|BROWN R.E., KRYNEN J.P. & BROWNLOW J.W. 1990. Manilla - Narrabri  1:250 000 Metallogenic Map. Geological Survey of New South Wales, Sydney.WHITE A.H. 1965. Geological Map of New England 1:100,000 Tareela Sheet (No. 300), with marginal text. The University of New England, Armidale, New South Wales, Australia.|16-MAY-23
15452|Porcupine Formation|Name source|Porcupine Lookout, Gunnedah, NSW|16-MAY-23
15452|Porcupine Formation|Unit history|Approved. Copies from xerox sent by NSW Stratigraphic Nomenclature Sub-Committee.|16-MAY-23
15452|Porcupine Formation|Type section locality|Alliance, Quirindi No. 1 Well west of Willow Tree.  Location of type section: Here designated from 3682 ft to 4043 ft 6 inches (Packham, 1970) in Alliance Quirindi Nol 1 well. (Core is stored in Department of Mines Core Library, Londonderry).|16-MAY-23
15452|Porcupine Formation|Extent|West of Willow Tree|16-MAY-23
15452|Porcupine Formation|Thickness range|a) At Type Section: 361ft 6 in.,  b) Maximum known:  600 ft at Gunnedah;  c) Representative Section 716839 to 715838 westerly bearing = 183 ft (Quirindi A-D 1:31 680 topographic sheet).|16-MAY-23
15452|Porcupine Formation|Lithology|Grey and white pebbly sandstones with minor shale units.|16-MAY-23
15452|Porcupine Formation|Fossils|Fauna IV assemblage.|16-MAY-23
15452|Porcupine Formation|Relationships and boundaries|The Porcupine Formation disconformably overlies the Willow Tree Formation (Runnegar, 1970). The Gladstone Formation conformably overlies the Porcupine Formation.|16-MAY-23
15452|Porcupine Formation|Age reasons|An early Late Permian age is suggested by the presence of a Fauna IV assemblage (Runnegar, 1969).|16-MAY-23
15452|Porcupine Formation|Proposed publication|Jour. & Proc. Roy. Soc. NSW|16-MAY-23
15452|Porcupine Formation|Proposer|Lowe S.P.|16-MAY-23
15452|Porcupine Formation|Status|1|16-MAY-23
73111|Port Macquarie Serpentinite|Name source|Port Macquarie township.|16-MAY-23
73111|Port Macquarie Serpentinite|Constituents|Includes the serpentinite masses informally referred to by Leitch (1980) as the "Burrawan serpentinite" and the "Lake Innes mass". Also includes other small occurrences known from outcrop and drilling in the Port Macquarie Block.|16-MAY-23
73111|Port Macquarie Serpentinite|Type section locality|Extensive exposures of serpentinite between Town Beach and Rocky Beach (31o25'59"S 152o55'27"E) constitute the type area for the unit.|16-MAY-23
73111|Port Macquarie Serpentinite|Description at type locality|The unit here comprises serpentinite melange with a matrix of schistose serpentinite, native phacoids of massive serpentinite, phacoids of highly altered mafic rock (rodingite) that may originally have been dykes in the serpentinite protolith, rare exotic phacoids of high-pressure metamorphic rocks, and rocks derived from the adjacent Watonga Formation.|16-MAY-23
73111|Port Macquarie Serpentinite|Extent|Applied to the bodies of serpentinite exposed in the Port Macquarie Block.|16-MAY-23
73111|Port Macquarie Serpentinite|Lithology|Serpentinite (massive and schistose), rodingite|16-MAY-23
73111|Port Macquarie Serpentinite|Relationships and boundaries|Surrounded by Watonga Formation and intruded by Town Beach Diorite, Karikeree Metadolerite, Nobbys Beach Lamprophyre and Sea Acres Dolerite|16-MAY-23
73111|Port Macquarie Serpentinite|Age reasons|At Port Macquarie older than the probable Permian Town Beach Diorite, that intrudes the unit at Town Beach. Ultramafic protolith probably earliest Cambrian based on correlation with comparable rocks from elsewhere in the southern New England Fold Belt (Aitchison and Ireland 1995). Age of serpentinisation uncertain but probably pre-Permian based on unconformable contacts between serpentinite and overlying Early Permian strata in the Curricabark area (Sharp 1995)|16-MAY-23
73111|Port Macquarie Serpentinite|Correlations|Serpentinite bodies within the southern New England Fold Belt|16-MAY-23
73111|Port Macquarie Serpentinite|References|AITCHISON, J. C. & IRELAND, T. R. 1995. Age profile of ophiolitic rocks across the Late Palaeozoic New England Orogen, New South Wales: implications for tectonic models. Australian Journal of Earth Sciences  42, 11-23.LEITCH, E. C. 1980a. Rock units, structure and metamorphism of the Port Macquarie Block, eastern New England Fold Belt. Proceedings of the Linnean Society of New South Wales 104, 273-292.SHARP, T. 1995. The Manning Group of the Curricabark district: stratigraphy, sedimentology and tectonics Unpublished MSc thesis, University of Technology, Sydney, Sydney.|16-MAY-23
37915|Pound Rock Rhyodacite Member|Name source|The name is taken from a prominent hill on the property Darthula at GR289593 Coryah 1:25,000 sheet.|16-MAY-23
37915|Pound Rock Rhyodacite Member|Unit history|Pound Rock Rhyodacite (Opdyke et al. 2000).  Originally informally named by Hocking (1973).|16-MAY-23
37915|Pound Rock Rhyodacite Member|Geomorphic expression|Ridge to cliff-forming.|16-MAY-23
37915|Pound Rock Rhyodacite Member|Type section locality|On the ridge 2 km south-southwest of Darthula homestead at GR281566, Coryah 1:25,000 sheet.|16-MAY-23
37915|Pound Rock Rhyodacite Member|Extent|Extends for approximately 3 km along a ridge south and west of Darthula homestead.|16-MAY-23
37915|Pound Rock Rhyodacite Member|Thickness range|45 m|16-MAY-23
37915|Pound Rock Rhyodacite Member|Lithology|Poorly to non-welded, grey to purple ignimbrite containing quartz, zoned plagioclase, ferrugenised biotite, opaque minerals and small pumice fragments. Groundmass spherulitic; shards and bubble walls coarse and unoriented.|16-MAY-23
37915|Pound Rock Rhyodacite Member|Depositional environment|Ignimbrite.|16-MAY-23
37915|Pound Rock Rhyodacite Member|Relationships and boundaries|The uppermost ignimbrite within the Rocky Creek Conglomerate in the Darthula block. Overlies the Darthula Rhyodacite.|16-MAY-23
37915|Pound Rock Rhyodacite Member|Age reasons|Carboniferous (Namurian).|16-MAY-23
37915|Pound Rock Rhyodacite Member|References|HOCKING R.M. 1973. The Carboniferous Back Creek-Pound Creek sequence, southwest of Caroda, New South Wales. BSc (Hons) thesis, University of new England, Armidale (unpubl.).OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
15797|Raggatt Volcanics|Name source|Named after Raggatt Hill GR 578935, Narromine 1:250 000.|16-MAY-23
15797|Raggatt Volcanics|Type section locality|Northeast of Trundle, at GR 578935, basal to central section.|16-MAY-23
15797|Raggatt Volcanics|Extent|Crops out east of Trundle in a belt approximately 17 km north-south on the Narromine 1:250 000 and a small belt east of Tullamore at GR 5650 9665.|16-MAY-23
15797|Raggatt Volcanics|Thickness range|50 to 600 m.|16-MAY-23
15797|Raggatt Volcanics|Lithology|Andesitic lavas and tuffs, rhyolite and sediments.|16-MAY-23
15797|Raggatt Volcanics|Relationships and boundaries|Underlies or is interbedded with the Derriwong Group and unconformably overlies the Cambro-Ordovician Girilambone Group.|16-MAY-23
15797|Raggatt Volcanics|Age reasons|Late Silurian-Early Devonian.|16-MAY-23
15797|Raggatt Volcanics|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982|16-MAY-23
15797|Raggatt Volcanics|Proposed publication|Metallogenic study of the Narromine 1:250 000 sheet.|16-MAY-23
15797|Raggatt Volcanics|Reserved? Yes/No|Yes|16-MAY-23
70120|Rasp Ridge Granite Gneiss|Unit history|After Laing et al. (1978) correlated the previously named 'upper' and 'lower' granite gneisses, Stevens et al. (1983) defined the Rasp Ridge Gneiss to include both of these and many other granite gneiss bodies throughout the Broken Hill district. The name is here modified to Rasp Ridge Granite Gneiss and confined to the bodies on either side of the Broken Hill Line of Lode, correlated across the Broken Hill Antiform by Laing et al. (1978). Some of the other bodies previously classed as Rasp Ridge Gneiss are not of the same age (see earlier discussion).|16-MAY-23
70120|Rasp Ridge Granite Gneiss|Extent|One mass crops out discontinuously from near Kelly's Creek, passing west of White Leeds mine to the closure of the Hanging Wall Synform at Block 10 Hill in Broken Hill City. The other main mass crops out in the hinge of the Broken Hill Synform, extending along the western limb through Rasp Ridge and south of Broken Hill City. In the eastern limb, it terminates abruptly.|16-MAY-23
70120|Rasp Ridge Granite Gneiss|Defn Reference|Stevens B.P.J., Page R.W. and Crooks A. 2008, 'Geochronology of Willyama Supergroup metavolcanics, metasediments and contemporaneous intrusions, Broken Hill, Australia' , Australian Journal of Earth Sciences, vol. 55(3) p329.|16-MAY-23
15968|Redan Gneiss|Name source|Used informally by Rayner (1949). Redan Homestead occurs about 1 km east of the area occupied by the Redan Gneiss.|16-MAY-23
15968|Redan Gneiss|Unit history|Rayner (1949) used the term "Redan gneiss" to encompass a very large area of rock in the southeastern part of the Broken Hill Block, but did not formally define the term. His Redan Gneiss is more or less equivalent to Redan Gneiss, Ednas Gneiss and Mulculca Formation as defined here. Corbett's (1981) "Redan rock unit association" incorporates Redan Gneiss as defined here, but also includes much of Ednas Gneiss and some of Mulculca Formation.|16-MAY-23
15968|Redan Gneiss|Type section locality|The type area extends from 1 to 7 km west of Redan Homestead (grid squares 5836, 6036 and 6236, Redan 1:25 000 sheet). A type section is nominated in this area, from GR 6150 3600 to GR 6240 3900 (top). The base of the Redan Gneiss is not exposed. A reference section is nominated between GR 5700 3300 and GR 5100 3300 (Redan 1:25 000 sheet), to provide additional lithological information.|16-MAY-23
15968|Redan Gneiss|Description at type locality|The Redan Gneiss consist essentially of two types of mapped rock unit. The more distinctive type of unit consists mainly of albite-quartz-hornblende-magnetite (+/- K-feldspar, clinopyroxene) rock (afm) (Fig. 4). The afm rocks (described by Corbett 1981, and Stroud et al. 1983 p.248-252) are typically medium grained and have well-defined lamination consisting of thin (1-4 mm) hornblende-rich and quartz+feldspar layers (5-20 mm). The rocks consist of albite and quartz with various proportions of hornblende, clinopyroxene, K-feldspar, and iron/titanium oxides. Epidote occurs replacing clinopyroxene, and minor scapolite, apatite and zircon have been identified. These rocks have chemical and textural similarities to the sodic plagioclase-quartz rocks abundant elsewhere in the Broken Hill Block (Brown et al. 1983). The other abundant type of rock unit in the Redan Gneiss consists mostly of albite-quartz-magnetite rock (P1 (Fig. 5). The rock is medium to fine grained and commonly exhibits layering defined by variation in magnetite content. These rocks consist mostly of albite and quartz, with sporadic K-feldspar and about 2-7% magnetite (Corbett 1981). They are a magnetite bearing variety of the sodic plagioclase-quartz rocks abundant elsewhere. The Redan Gneiss contains very few outcrops of amphibolite, and no quartz-magnetite rocks have been observed. There are also no ourcrops of sillimanite bearing or micaceous metasediments, although the large areas of non-outcrop could contain some of these.|16-MAY-23
15968|Redan Gneiss|Extent|The Redan Gneiss is confined to the Redan 1:25 000 sheet, and extends southwestwards for about 15 km from Redan Creek, near the Redan Homestead. It occupies the core of the Redan Antiform.|16-MAY-23
15968|Redan Gneiss|Thickness range|Difficult to determine due to lack of information on internal folding, but estimated at 1.5 km (base no exposed).|16-MAY-23
15968|Redan Gneiss|Relationships and boundaries|The base is not exposed. The upper boundary with Ednas Gneiss is taken where the abundant afm rocks of the Redan Gneiss give way to abundant sodic plagioclase-quartz-magnetite gneiss (BT) of Ednas Gneiss. The northwestern boundary corresponds with the margin of a strong linear magnetic anomaly in the basal part of Ednas Gneiss.|16-MAY-23
15968|Redan Gneiss|Proposed publication|AJES|16-MAY-23
24470|Reevesdale Basalt|Name source|Reevesdale' property GR 706351, Kooringaroo 1:25 000 Topographic Sheet (8828-II-S).|16-MAY-23
24470|Reevesdale Basalt|Unit history|The Reevesdale Basalt is the northernmost flow of the Nerriga Province (Wellman & McDougall, 1974).|16-MAY-23
24470|Reevesdale Basalt|Type section locality|2 km SE of Reevesdale homestead GR 720336 - Kooringaroo 1:25 000 Topographic Sheet (8828-II-S).|16-MAY-23
24470|Reevesdale Basalt|Extent|The unit extends over 10 km2 as an arcuate series of outliers from 4 km SW of Bungonia to 6 km SE of Bungonia. The largest outlier is in the Reevesdale area.|16-MAY-23
24470|Reevesdale Basalt|Thickness range|0-8+ m.|16-MAY-23
24470|Reevesdale Basalt|Lithology|Alkali olivine basalt.|16-MAY-23
24470|Reevesdale Basalt|Relationships and boundaries|Unconformably overlies Ordovician to Devonian sedimentary and intrusive rocks.|16-MAY-23
24470|Reevesdale Basalt|Age reasons|Late Eocene (Wellman & McDougall, 1974).|16-MAY-23
24470|Reevesdale Basalt|Proposed publication|Proceedings of the Linnean Society of New South Wales |16-MAY-23
24470|Reevesdale Basalt|Proposer|Carr P.F., Jones B.G., Kantsler A.J., Moore P.S., Cook A.C.|16-MAY-23
16079|Rickabys Creek Gravel|Name source|From Rickabys Creek, a tributary of the Hawkesbury River which flows northeast from near Castlereagh to the Hawkesbury River at Windsor. Rickabys Creek Gravel is exposed on banks of the creek (GR 776441, Windsor 1:63 360).|16-MAY-23
16079|Rickabys Creek Gravel|Unit history|Described by Bell (1966) in his Windsor Formation. Walker and Hawkins (1957) included Rickabys Creek Gravel in their Londonderry Formation.|16-MAY-23
16079|Rickabys Creek Gravel|Type section locality|10 m of poorly sorted polymictic gravel exposed in a railway cutting on the Great Western Railway Line west of Emu Plains (GR 641304, Windsor 1:63 360). Clasts consist of quartz, quartzite, silcrete, chert, and weathered porphyry, minor granite, hornfels, and sandstone set in a sandy-clay matrix. Variably cemented by iron. Horizontally bedded..|16-MAY-23
16079|Rickabys Creek Gravel|Extent|Occurs as a subsurface gravel sheet between Cranebrook and Windsor, exposed where dissected by Rickabys Creek. Also as outliers on the Blue Mountains Plateau.|16-MAY-23
16079|Rickabys Creek Gravel|Thickness range|Range 2-12 m.|16-MAY-23
16079|Rickabys Creek Gravel|Lithology|Polymictic gravel, sporadic crossbedded sand lenses. High matrix content of unconsolidated silt, sand and clay.|16-MAY-23
16079|Rickabys Creek Gravel|Relationships and boundaries|Erosional into and hence disconformable on both the Wianamatta Group in the Cumberland Basin, and on the Hawkesbury Sandstone on the Blue Mountains Plateau. Gradually fines up into the overlying Londonderry Clay.|16-MAY-23
16079|Rickabys Creek Gravel|Age reasons|No floral or faunal assemblages are available for dating. Silcrete boulders found within the gravel suggest that the formation was deposited subsequent to a period of duricrust formation. Londonderry Clay Overlying the Rickabys Creek Gravel has been lateritised suggesting that the gravel was deposited between two periods of duricrust formation. It is suggested (Gobert in press) that the widespread lateritisation of the Londonderry Clay is of latest Miocene or early Pliocene age while the formation of silcrete took place during or prior to the mid Oligocene. On this evidence a Miocene age for the deposition of Rickabys Creek Gravel is suggested.|16-MAY-23
16079|Rickabys Creek Gravel|Defn author|Wallace I., 1976|16-MAY-23
16079|Rickabys Creek Gravel|Proposed publication|Gobert Val, _____, Cumberland Basin Strataigraphy in The geology of the Penrith 1:100 000 sheet, by C. Herbert. Geological Survey of NSW, Sydney (in press).|16-MAY-23
16079|Rickabys Creek Gravel|References|01/31632|16-MAY-23
24473|Roach Island Tuff|Name source|Roach Island, largest of Admiralty Islands, immediately north of Lord Howe Island at 159o04.3' longitude, 31o29.9'S latitude on map of Lord Howe Island (Department of Lands, Sydney, 1966, 1: 15 840). Origin: Eruptions from local volcanic centre.|16-MAY-23
24473|Roach Island Tuff|Type section locality|About 60 m of this formation is exposed in the point under Malabar, a hill adjacent to the north coast of Lord Howe Island. No base is exposed. Overlain with erosional disconformity by North Ridge Basalt.|16-MAY-23
24473|Roach Island Tuff|Extent|The unit is exposed on the point extending northeast under Malabar, and on the Admiralty Islands which lie just north of Lord Howe Island.|16-MAY-23
24473|Roach Island Tuff|Thickness range|60 m +.|16-MAY-23
24473|Roach Island Tuff|Lithology|Interbedded tuff, thin rubbly basaltic lavas, beds of coarser fragmental material, including breccia sheets (talus or lahar?). Cut by younger dykes.|16-MAY-23
24473|Roach Island Tuff|Relationships and boundaries|No base exposed, overlain by North Ridge Basalt.|16-MAY-23
24473|Roach Island Tuff|Age reasons|North Ridge Basalt is dated by ;K-Ar age measurements as 6.9 +/- 0.2 Ma, Malabar Tuff Complex regarded as only a little older. Probably Late Miocene|16-MAY-23
24473|Roach Island Tuff|Proposed publication|Submitted to J. Geol. Soc. Australia|16-MAY-23
24473|Roach Island Tuff|References|Not previously described.|16-MAY-23
24473|Roach Island Tuff|Defn approved by|Approved - see letter on file 79/665 11/12/80.|16-MAY-23
24473|Roach Island Tuff|Proposer|McDougall I., Embleton B.J.J., Stone D.B.|16-MAY-23
24473|Roach Island Tuff|Status|1|16-MAY-23
72991|Rocky Beach Metamorphic Melange|Name source|Rocky Beach - Port Macquarie|16-MAY-23
72991|Rocky Beach Metamorphic Melange|Geomorphic expression|Knocker topography surrounded by beach sand|16-MAY-23
72991|Rocky Beach Metamorphic Melange|Type section locality|The type area of the unit is at the northern end of Rocky Beach (31o26'14"S 152o55'32"E) where exposure varies according to the amount of surficial sand along the beach.|16-MAY-23
72991|Rocky Beach Metamorphic Melange|Description at type locality|Rounded phacoids of high-P metamorphic rocks and Watonga Formation lithologies embedded in a chlorite-actinolite schist matrix.|16-MAY-23
72991|Rocky Beach Metamorphic Melange|Extent|Two lenses of metamorphic mélange apparently surrounded by serpentinite at the north end of Rocky Beach.|16-MAY-23
72991|Rocky Beach Metamorphic Melange|Lithology|Eclogite, blueschist, omphacitite, tremolite marble and chlorite-actinolite schist|16-MAY-23
72991|Rocky Beach Metamorphic Melange|Relationships and boundaries|Surrounded by Port Macquarie Serpentinite.|16-MAY-23
72991|Rocky Beach Metamorphic Melange|Age reasons|Collectively the phacoids show a complex metamorphic history involving both prograde and retrograde blueschist facies metamorphism separated by an episode of static eclogitic metamorphism at a pressures in excess of 1.8 GPa (>54 km burial) and a temperature of about 560OC. K-Ar dating of white mica suggests that retrograde blueschist metamorphism probably occurred around 469 Ma (Middle Ordovician).|16-MAY-23
72991|Rocky Beach Metamorphic Melange|Correlations|Attunga eclogite, and eclogitic and blueschist phacoids in serpentinite bodies within the southern New England Fold Belt (e.g. Allan and Leitch 1992; Offler 1999; Watanabe et al 1998)|16-MAY-23
72991|Rocky Beach Metamorphic Melange|References|OCH, D. J., LEITCH, E. C., CAPRARELLI, G. and WATANABE, T. 2003. Blueschist and eclogite in tectonic melange, Port Macquarie, New South Wales, Australia. Mineralogical Magazine 67, 609-624.OCH, D. J., LEITCH, E. C., GRAHAM, I. T. and CAPRARELLI, G. 2005. A Field guide to the palaeosubduction complex of Port Macquarie, NSW, Specialist Group in Geochemistry, Mineralogy and Petrology Field Guide, Geological Society of Australia, Sydney. 33 p.OFFLER, R. 1999. Origin and significance of blueschist "knockers", Glenrock Station, NSW. In: Flood, P. G. (ed).NEO 99, pp.35-44. Earth Sciences, The University of New England, Armidale.ALLAN, A. D. & LEITCH, E. C. 1992. The nature and origin of eclogite blocks in serpentinite from the TamworthBelt, New England Fold Belt, eastern Australia. Australian Journal of Earth Sciences  39, 29-35.WATANABE, T., FANNING, C. M. & LEITCH, E. C. 1998. Neoproterozoic Attunga Eclogite in the New England Fold Belt. Geological Society of Australia, Abstracts  49, 458.|16-MAY-23
33761|Rocky Tank Conglomerate Member|Name source|ROCKY TANK lies 200 m west of the south-flowing Ramparts Creek on Waterbag Station.|16-MAY-23
33761|Rocky Tank Conglomerate Member|Unit history|Unit A (sandy conglomerate) Neef & Bottrill 1996. Journal & Proceedings Roy. Soc. NSW 129, 105-122. Waverly Creek beds Neef & Bottrill in press AJES.|16-MAY-23
33761|Rocky Tank Conglomerate Member|Constituents|None|16-MAY-23
33761|Rocky Tank Conglomerate Member|Geomorphic expression|Forms the lower part of a narrow valley.|16-MAY-23
33761|Rocky Tank Conglomerate Member|Type section locality|In an east-flow tributary of Ramparts Creek 1.5km south of Rocky Tank South (Lat. 31o 24' Long. 142o 22.5').|16-MAY-23
33761|Rocky Tank Conglomerate Member|Extent|Forms a narrow belt between Ramparts Creek in the southeast and the southern boundary of the Mootwingee National Park in the North.|16-MAY-23
33761|Rocky Tank Conglomerate Member|Thickness range|50 m|16-MAY-23
33761|Rocky Tank Conglomerate Member|Lithology|Boulders (max. clast size 34 cm) of grey quartzose sandstone and quartzite. Fines upwards to beds of coarse sandstone and conglomerate lenses.|16-MAY-23
33761|Rocky Tank Conglomerate Member|Depositional environment|Fluvial deposited. Shallow gravel braided river system (Scott type, Miall 1996).|16-MAY-23
33761|Rocky Tank Conglomerate Member|Relationships and boundaries|Is unconformable on Units 1-7 of the Snake Cave Sandstone and is conformably overlain by the Ramparts Creek Sandstone.|16-MAY-23
33761|Rocky Tank Conglomerate Member|Age reasons|? Late Eifelian - ? early Givetian (Neef in prep.).|16-MAY-23
33761|Rocky Tank Conglomerate Member|Correlations|Unit A  Neef, G. & Bottrill, R.S. 1996.|16-MAY-23
33387|Rosemeath Formation|Name source|The unit is named for the property of Rosemeath which is located 3 km south of Bombala. The name was first applied by Istadi (1985) in an unpublished BAppSci report on the geology of the area south of Bombala.|16-MAY-23
33387|Rosemeath Formation|Unit history|Rocks comprising part of this unit and outcropping near Bombala were referred to by McRoberts (1948) as the 'Bombala Beds'. Unfortunately this name has since been used to refer to the Ordovician metasedimentary rocks in the Bombala area (Hall et al., 1967) and also more recently to the Bombala Tonalite (Lewis et al ., 1994). On the recent compilation of the Bega-Mallacoota 1:250 000 geological sheet (Lewis et al., 1994) the fluvial 'red bed' rocks in the Bombala area have been included in the Merrimbula Group, defined and mapped on the south coast of New South Wales, 50km to the east. The Merrimbula group contains predominantly fluvial 'red bed' sediments with a minor but significant shallow marine component. Based on fossil evidence the Merrimbula Group is considered to be Late Devonian and to range in age from Frasnian to Famennian. Recent zircon dating of the Rosemeath Formation at Bombala indicates that it extends into the Early Carboniferous (Sircombe and McQueen, in press). These results imply either that the South Coast correlation is not valid for the upper sequences, or that the Merrimbula Formation seqeunces also extend upward into the Carboniferous.|16-MAY-23
33387|Rosemeath Formation|Geomorphic expression|The coarser grained sandstones and conglomerates in the Rosemeath Formation form prominent outcrops with gentle dip slopes and small joint-controlled scarps. Shale dominated units crop out poorly and generally form smooth areas of low relief between the more resistant sandstones and grits.|16-MAY-23
33387|Rosemeath Formation|Type section locality|The type locality is a section extending NW to SE along Caveat Street in Bombala up to the Endeavour Lookout. Supplementary exposures occur and near the Wellington Street Quarry in the township of Bombala and along the Rosemeath and Bucky Springs roads south of Bombala.  The type section begins at lat. 36o 55' 12"S, long. 149o 14' 35" E and ends at Lat 36o 55' 42" S, long. 149o 15' 8" E.|16-MAY-23
33387|Rosemeath Formation|Extent|Rocks of the Rosemeath Formation occur as small fault-bounded remnants which extend over an area from just north of Bibbenluke to 20km south of Bombala. The total area covered is approximately 60km^2.|16-MAY-23
33387|Rosemeath Formation|Thickness range|In the type area the Rosemeath Formation is approximately 420m thick.|16-MAY-23
33387|Rosemeath Formation|Lithology|In the type section the Rosemeath Formation can be subdivided into three components. A lower section (about 50m thick) consists mainly of quartz-rich grits and siliceous gritty conglomerates with interbedded red sandstones and mudstones. This is overlain by a section (about 70m thick) of red mudstones with some coarses sandstones and minor conglomerates. Sandstone beds are typically less than 2m thick. The upper part of the formation (about 300m thick) consists of more resistant purplish siliceous grits and sandstones with narrow less resistant bands of interbedded red shales. Beds are generally 3-5m thick. West of Bibbenluke, the base of the sequence is well defined by a pebble-cobble conglomerate. This unit is overlain by coarse grits and sandstones with less prominent, red and drab-coloured shale and siltstone units. The sequence here is at least 250m thick. Conglomerates in the Rosemeath Formation are moderately sorted, generally with a bimodal distribution of clast size in the pebble and coarse sand sizes. Basal conglomerates are highly siliceous with clasts up to 10cm. Many clasts are subangular with low sphericity but some of the larger pebbles are highl spherical and subrounded. Lithic fragments make up 50% or more of the rock and most are of sedimentary origin. They include quartz-rich sandstones, micaceous sandstones, abundant siltstone and chert clasts, lesser amounts of schist, phyllite and vein quartz and rare, highly weathered fragments that appear to be of volcanic origin. The matrix consists of coarse-grained, anuglar to subrounded quartz and finer rock fragments. The quartz includes predominant microcrystalline and lesser polycrystalline varieties. Other detrital minerals include small amounts of muscovite, zircon and pleochroic green to deep brown tourmaline. Sandstones and grits are composed of angular to subrounded quartz clasts with some feldspar and a weakly ferruginous siliceous cement. many of the sandstone are pebbly with sub-rounded to rounded pebbles of quartz and siltstone. intraformational clasts of red siltstone/mudstone are a feature of some of the sandstones. Mudstones in the lower part of the Rosemeath Formation are generally red to maroon, with green reduction spots. They are composed of rounded to subrounded quartz grains in a highly ferruginised cement. Interbedded with these mudstones are purple. feldspathic sandstones and yellow to red, fine-grained sandstones.|16-MAY-23
33387|Rosemeath Formation|Depositional environment|Based on lithology and sedimentary structures (including sorting, channel structures, fining upward sequences and current cross bedding) the unit is considered to be entirely fluvial. Possible worm burrows have been found in some of the mudstones. Current directions determined from currrent cross-bedded sandstones at Bibbenluke, the Endeavour Lookout SE of Bombala and also to the south of Bombala indicate palaeocurrent directions predominantly to the southeast and east-southeast, at least for the sandstones in the upper portion of the unit.|16-MAY-23
33387|Rosemeath Formation|Relationships and boundaries|Just east of Bombala, the Rosemeath Formation directly overlies Ordovician metasedimentary rocks of the Adaminaby Group, the Coolumbooka Granodiorite, of early Devonian age, and ignimbrites of the Hospital Porphyry. An irregular, unconformable contact between the Rosemeath Formation and ignimbrites can be seen in the Wellington Street Quarry in Bombala. At this locality, the immediately overlying sediments contain porphyry-derived quartz grains. Near Bibbenluke the Rosemeath Formation overlies hornfelsed Adaminaby Group rocks and is overlain by Eocene basalts of the Monaro Volcanics.|16-MAY-23
33387|Rosemeath Formation|Age reasons|No definitive fossils have been found in the Rosemeath Formation and previously these rocks have been assigned a Late Devonian age on the basis of lithological similarity to Late Devonian 'red beds' on the south coast of New South Wales. Recent SHRIMP dating of detrital zircons from the base and near the top of the formation indicates an age extending into the Early Carboniferous (347 Ma, Sircombe and McQueen, in press). Zircon dating of the ignimbrites which are unconformably overlain by the Rosemeath Formation indicates a maximum possible age for the unit of 366 Ma (i.e. Late Devonian).|16-MAY-23
33387|Rosemeath Formation|Correlations|The lower part of the Rosemeath Formation can possibly be correlated to similar rocks with Late Devonian fossil ages in the lower parts of the Merrimbula Group along the south coast (Fergusson et al., 1979). The upper part of the formation may correlate with the youngest units in the Merrimbula Group (e.g. Ben Boyd Formation) although these are not known to extend into the Early Carboniferous.|16-MAY-23
33387|Rosemeath Formation|Defn author|K.G. McQueen 1999.|16-MAY-23
33387|Rosemeath Formation|Comments|The Rosemeath Formation appears to be a condensed sequence. The presence of Early Carboniferous detrital zircons raises interesting questions about the provenance for the sediments.|16-MAY-23
33387|Rosemeath Formation|References|Fergusson, C.L., Car, R.A.F., Collins, W.J., Craig, G.Y., Crook, K.A.W., Powell, CMcA., Scott, P.A. and Young, G.C., 1979. The Upper Devonian Boyd Volcanic Complex, Eden, New South Wales, Journal of the Geological Society of Australia, 26, 87-105. **Hall, L.R., Rose, G.R. and Pogson, D.J., 1967. Bega 1:250 000 Geological Sheet SJ/55-4. Geological Survey of N.S.W., Sydney. **Istadi, B.P. 1985. Geological investigation of the Saucy Creek area south of Bombala N.S.W. Unpublished BAppSci thesis, Canberra College of Advanced Education 49 pp. **Lewis P.C., Glen, R.A., Pratt, G.W. and Clarke, I., 1994. Bega-Mallacoota 1:250 000 Geological Sheet SJ/55-4, SJ.55-8: Explanatory Notes, 148 pp, 8 pls. Geological Survey of New South Wales, Sydney. **McRoberts, H.M., 1948. The general geology of the Bombala Disctrict, N.S.W. Journal and Proceedings of the Royal Society of N.S.W., 81, 248-266. **Sircombe, K.N. and McQueen, K.G. 1999. Zircon dating of Devonian-Carboniferous rocks from the Bombala area New South Wales. Australian Journal of Earth Sciences in press.|16-MAY-23
24477|Rossi Granodiorite|Name source|From the town of Rossi, GR 274730, Braidwood 1:100 000 sheet area.|16-MAY-23
24477|Rossi Granodiorite|Type section locality|As most of the Granodiorite probably crops out in Braidwood 1:100 0000 where it is not well defined, no type locality is recommended at this stage. In Araluen 1:100 0000 sheet area it is best exposed as tors up to 2 m high at GR 270684.|16-MAY-23
24477|Rossi Granodiorite|Extent|Northwest corner of Araluen 1:100 000 sheet, overlapping into Braidwood, Canberra and Michelago 1:100 000 sheet areas. Not accurately defined in Braidwood where it probably has its greatest development.|16-MAY-23
24477|Rossi Granodiorite|Lithology|In Araluen it is a strongly foliated quartz rich granodiorite containing recrystallized green biotite, hornblende, epidote, sphene, opaques and allanite. Hornblende is present mainly around GR 268670.|16-MAY-23
24477|Rossi Granodiorite|Age reasons|Early Devonian, contains late Devonian dolerite dykes, which together with the granodiorite have been deformed in the Carboniferous.|16-MAY-23
24477|Rossi Granodiorite|Defn author|Wyborn D., Owen M., 1986.|16-MAY-23
24477|Rossi Granodiorite|Proposed publication|BMR map commentary: Araluen 1:100 000 Sheet.|16-MAY-23
24477|Rossi Granodiorite|Proposer|Wyborn D.|16-MAY-23
24477|Rossi Granodiorite|Resdate|26-MAY-1982|16-MAY-23
24477|Rossi Granodiorite|Reserved? Yes/No|Yes|16-MAY-23
24478|Rothery Tuff|Name source|Rothery Trig. Station. Parish Waugoola, County Bathurst.|16-MAY-23
24478|Rothery Tuff|Type section locality|GR 18408390-GR 18698398, Bathurst 1:250 000 sheet.|16-MAY-23
24478|Rothery Tuff|Extent|The formation crops out in a 200 km2 area extending from east of Cowra to just north of Walli.|16-MAY-23
24478|Rothery Tuff|Thickness range|6000 m|16-MAY-23
24478|Rothery Tuff|Lithology|Tuff, minor lavas and interbedded sediments. The tuffs are predominantly lithic tuffs although welded tuffs, lithic crystal tuffs and crystal tuffs are also present. Lithic tuffs and welded tuffs are mid grey to greenish grey to purplish grey in colour. Crystal tuffs are generally lighter in colour. They range in grainsize from fine tuffs to agglomerates. The sediments are mainly grey to chocolate shales with lesser yellow-grey sandstones.|16-MAY-23
24478|Rothery Tuff|Relationships and boundaries|The basal formation of the Walli Sub Group (formerly Walli Andesite). The Rothery Tuff is overlain conformably by the Noyeau Hollow Andesite. The Rothery Tuff conformably overlies the Abercrombie Beds.|16-MAY-23
24478|Rothery Tuff|Age reasons|The Rothery Tuff is considered to be of Early Ordovician age. This is based mainly on the faunal evidence from the Cliefden Caves Limestone which conformably (?) overlies the Walli Sub Group.|16-MAY-23
24478|Rothery Tuff|Proposed publication|Geological Survey NSW Record Por 19|16-MAY-23
24478|Rothery Tuff|Proposer|Richardson S., Bowman H.|16-MAY-23
24478|Rothery Tuff|Reserved? Yes/No|Yes|16-MAY-23
24479|Rothlyn Formation|Name source|'Rothlyn' property; GR965072, Cooma 1:100 000 Sheet.|16-MAY-23
24479|Rothlyn Formation|Unit history|Main southern part previously unnamed; formation includes some rocks in Bredbo area and west of Michelago previously mapped as Colinton Volcanics and Bransby Beds (Richardson, 1979).|16-MAY-23
24479|Rothlyn Formation|Type section locality|11km southeast of Bredbo, Cooma 1:100 000 sheet 8725, from GR983086 (base) to GR963085 (top); rock types exposed along section include from the base going west - 0-550m shale; 550-900m hornblende dacititc crystal tuff (Billilingra Dacite Member); 900-1350m shale; 1350-1500m basalt; 1500-1800m siltstone and shale; 1800-1950m sandstone.|16-MAY-23
24479|Rothlyn Formation|Extent|Mainly in area extending from southeast of Bredbo to southeast of Cooma; also a narrow belt extending south from Bredbo along Murrumbidgee River nearly to Williamsdale.|16-MAY-23
24479|Rothlyn Formation|Thickness range|About 1900m+ along type section; probably thicker to south.|16-MAY-23
24479|Rothlyn Formation|Lithology|Sedimentary rocks, mainly shale and siltstone with some sandstone and limestone, interbedded with flows of hornblende dacite and dacitic crystal tuff, tuff, and minor basalt and rhyolite.|16-MAY-23
24479|Rothlyn Formation|Relationships and boundaries|Conformably overlies Colinton Volcanics, top not preserved; base is first major sedimentary unit above Colinton volcanics or Billilingra Dacite Member.|16-MAY-23
24479|Rothlyn Formation|Age reasons|Late Silurian from fossils; K/Ar isotopic age determination of Billilingra Dacite Member of 407 +/- 7 Ma indicates possible early Devonian.|16-MAY-23
24479|Rothlyn Formation|Defn author|G.A.M. Henderson ?1990.|16-MAY-23
24479|Rothlyn Formation|Comments|Although this appears to be an adequate unit definition, no evidence is available to show that this definition went through the Stratigraphy Commission approval process. The origina card was supplied  to ASUD manager C. Brown by R. S. Abell, on his departure from BMR, after the publication of BMR Bulletin 233 Geology of the Canberra 1:100 000 sheet.|16-MAY-23
24479|Rothlyn Formation|References|G.A.M., 1987. Late Silurian geology of the Michelago-Cooma area: 1:100 000 preliminary edn map. Bur. Miner. Resour. Aust. **Richardson, S.J., 1979. Geology of the Michelago 1:100 000 Sheet 8726. Geol. Surv. NSW. Sydney.|16-MAY-23
26323|Roxburgh Formation|Name source|County of Roxburgh.|16-MAY-23
26323|Roxburgh Formation|Type section locality|550 m of quartz arenite, lutite, conglomerate, and sublitharenite along Oakey Creek between GR 765700 6363950 and GR 764000 6363800.|16-MAY-23
26323|Roxburgh Formation|Extent|The unit is exposed over 15 km2 on the southeastern part of the Mudgee 1:100 000 sheet from the Cudgegong-Rylstone road to Aarons Pass.|16-MAY-23
26323|Roxburgh Formation|Thickness range|500 to 1000 m.|16-MAY-23
26323|Roxburgh Formation|Lithology|Quartz arenite, grey-white to red, cross-bedded, ripple marks, common lutite interbeds, fossiliferous; lutite, cream, unfossiliferous; conglomerate, well rounded and sorted rhyolitic pebbles; sublitharenite, fine-grained, grey, well bedded.|16-MAY-23
26323|Roxburgh Formation|Relationships and boundaries|Base unknown - folded in south-plunging anticline and syncline, latter faulted out by Cudgegong Fault (Game, 1935) overlain by the Riversdale Volcanics (Offenberg et al., 1971).|16-MAY-23
26323|Roxburgh Formation|Age reasons|Fauna include Iridistrophia sp., Howellella sp., Delthris sp., Gypidula sp. Indicating an Early Devonian age.|16-MAY-23
26323|Roxburgh Formation|Proposed publication|Journal and Proceedings of the Royal Society of NSW|16-MAY-23
26323|Roxburgh Formation|References|01/31633; 97/28471; 79/03255|16-MAY-23
26323|Roxburgh Formation|Proposer|Pemberton J.W.|16-MAY-23
26323|Roxburgh Formation|Reserved? Yes/No|Yes|16-MAY-23
16491|Ryrie Formation|Name source|Ryrie Trig. Station (958 m); GR 969382, Michelago 1:100 000 Sheet area.|16-MAY-23
16491|Ryrie Formation|Unit history|Previously unnamed.|16-MAY-23
16491|Ryrie Formation|Type section locality|Best represented on the eastwest ridge of Colinton Hill, the base of the formation at GR 988285 (Michelago 1:100 000) being marked by the Gungoandra Siltstone Member and the top around GR 972284 (Michelago 1:100 000) by massive quartz arenite lithologies with minor siltstone/shale interbeds.|16-MAY-23
16491|Ryrie Formation|Extent|The formation has two main areas of outcrop separated by the Collingwood Fault. The northern, more restricted locality lies to the west of Ryrie Trig. Station while the southern area extends from Colinton Trig. Station (GR 980283) south to a westward flowing tributary of Cappanana Creek at GR 977246.|16-MAY-23
16491|Ryrie Formation|Thickness range|1600 m in type section.|16-MAY-23
16491|Ryrie Formation|Lithology|The Gungoandra Siltstone Member which is the basal unit of the formation is overlain by quartz arenite interbedded with minor brown shale and coarse grey sandy siltstones. The massive quartzites become progressively dominant towards the top of the sequence. Jointing is prominant but there appear to be no sedimentary structures.|16-MAY-23
16491|Ryrie Formation|Relationships and boundaries|Angular unconformity with underlying Late Ordovician Foxlow Beds, and angular unconformity with overlying Late Silurian Cappanana Formation.|16-MAY-23
16491|Ryrie Formation|Age reasons|Late Llandoverian age graptolites have been collected from both northern and southern areas of outcrop.|16-MAY-23
16491|Ryrie Formation|Defn author|Richardson, 1979.|16-MAY-23
16491|Ryrie Formation|Proposed publication|Geological Survey of NSW 1:100 000 Note Series|16-MAY-23
26130|Saint Marys Formation|Name source|Original name proposed by Walker and Hawkins (1957) from St Marys, a village in the western suburbs of Sydney, where the type section is exposed (GR 773286, Liverpool 1:63 360).|16-MAY-23
26130|Saint Marys Formation|Unit history|First called St Marys Formation by Walker and Hawkins (1957). Bell (1966) included this formation in his Windsor Formation.|16-MAY-23
26130|Saint Marys Formation|Type section locality|9.6 m of colluvial/alluvial sediment exposed in a channel eroded into shales of the Wianamatta Group in a railway cutting 200 m east of St Marys Railway Station on the Great Western Line (GR 778285, Liverpool 1:63 360).|16-MAY-23
26130|Saint Marys Formation|Extent|Small isolated outcrops occur in the Cumberland Basin within the valleys of the South Creek system and Mulgoa Creek.|16-MAY-23
26130|Saint Marys Formation|Thickness range|Range 2-9.6 m.|16-MAY-23
26130|Saint Marys Formation|Lithology|Silcrete, siliceous sandstone, shale, and transported ironstone clasts, all variable cemented by limonite within a sandy, mottled clay. Interbeds of mottled red-grey plastic clay throughout.|16-MAY-23
26130|Saint Marys Formation|Relationships and boundaries|Occurs in small isolated channels eroded into shales of the Wianamatta Group, hence disconformable on the Wianamatta Group. Erosional upper surface.|16-MAY-23
26130|Saint Marys Formation|Age reasons|No floral or faunal assemblages are available for dating. Silcrete and laterite pebbles found in the formation suggest that the formation was deposited after a period of duricrusting of probable mid-Oligocene age. The formation also appears to have undergone lateritisation, probably during the Late Miocene/Early Pliocene. A Late Oligocene-Early Miocene age is hence suggested (Gobert in press).|16-MAY-23
26130|Saint Marys Formation|Proposed publication|Gobert Val, ______. Cumberland Basin Stratigraphy in The geology of the Penrith 1:100 0000 sheet, by C. Herbert. Geological Surv NSW, Sydney (in press).|16-MAY-23
26130|Saint Marys Formation|Status|1|16-MAY-23
24487|Salisbury Sandstone|Name source|Salisbury is a small hamlet situated on the Williams River approximately 31 km north of Dungog. GR 45770161 (Newcastle 1:250 000).|16-MAY-23
24487|Salisbury Sandstone|Type section locality|Approximately 2.5 km NE of Salisbury.  Type Section: Down the steep scarp on the western side of the Chichester Range (46010177 to 46080179).|16-MAY-23
24487|Salisbury Sandstone|Extent|From Upper Chichester in the north to approximately 3 km south of Brownmore in the south. From approximately 2 km west of Upper Chichester in the west to Chichester in the east.|16-MAY-23
24487|Salisbury Sandstone|Thickness range|(a) 655 m (2150 ft).|16-MAY-23
24487|Salisbury Sandstone|Lithology|Predominantly lithic sandstone with conglomerate, conglomeratic sandstone and mudstone.|16-MAY-23
24487|Salisbury Sandstone|Fossils|Rare occurrences of plant fragments - Archaeocalamites scrobiculatus Schlotheim.|16-MAY-23
24487|Salisbury Sandstone|Relationships and boundaries|Conformably overlies the Chichester Formation and is overlain by the Booral Fm. Can possibly be correlated to the Karuah Formation near Booral (Packham 1969) and the Buckets Gap Formation near Barrington (Campbell and McKelvey 1972).|16-MAY-23
24487|Salisbury Sandstone|Age reasons|Late Visean-Namurian. (Marginirugus barringtonensis) Zone. Based on fossils in underlying and overlying units.|16-MAY-23
24487|Salisbury Sandstone|Defn approved by|Copied from xerox from NSW Sub-Committee|16-MAY-23
24487|Salisbury Sandstone|Proposer|Roberts J.|16-MAY-23
24487|Salisbury Sandstone|Reserved? Yes/No|J. Roberts|16-MAY-23
16597|Sandhills Creek Limestone Member|Name source|Sandhills Creek (centred on GR 364019, Braidwood 1:100 0000 sheet).|16-MAY-23
16597|Sandhills Creek Limestone Member|Unit history|Carne and Jones (1919) referred collectively to the limestones at Mount Fairy as the "Fairy Meadow Limestones". The Fairy Meadow Limestone Member is redefined in Felton and Huleatt (1975).|16-MAY-23
16597|Sandhills Creek Limestone Member|Type section locality|Within and adjacent to Fairy Meadow Creek between GR 377028 (bottom) and GR 376027 (top) (Braidwood 1:100 000 sheet). 100 m of section are exposed.|16-MAY-23
16597|Sandhills Creek Limestone Member|Extent|The unit occurs at Mount Fairy, cropping out adjacent to Fairy Meadow Creek between GR 373026 and GR 377024 and along Sandhills Creek between GR 366022 and GR 368028. A further small outcrop occurs in Fairy Meadow Creek centred on GR 367038 (all GR's refer to Braidwood 1:100 000 sheet).|16-MAY-23
16597|Sandhills Creek Limestone Member|Thickness range|Variable; about 200 m maximum.|16-MAY-23
16597|Sandhills Creek Limestone Member|Lithology|Massive and bedded fossiliferous biomicrite; microcrystalline dolomite; occasional calcarenite and calcareous shale.|16-MAY-23
16597|Sandhills Creek Limestone Member|Relationships and boundaries|The base of the unit is marked by thinly interbedded biomicrite and calcareous shale about 30 m thick. The base of the first thin limestone bed is defined as the base of the unit. At the top of the unit there is a sharp boundary between limestone and grey shale. The unit passes laterally into De Drack Formation siltstone and shale. Boundaries are sharp. The Sandhills Creek Limestone Member is partly faulted against De Drack Formation sediments and against the Ordovician Birkenburn Beds.|16-MAY-23
16597|Sandhills Creek Limestone Member|Age reasons|The following assemblage is recorded by Felton (1969) from the unit: Tryplasma sp. Indet.; Zenophila walli; Circophyllum sp. Indet.; Phaulactis sp. Indet.; Favosites spp. (probably including F. gothlandicus); Heliolites(?) daintreei; Thamnopora sp. Indet.; Conchidium (?) knight; (?)Atrypa sp. indet.; (?)Clathrodictyon sp. indet.; (?)Spathognathodus sp. indet. Although most of these genera are non-diagnostic, a Middle Late Silurian age is indicated.|16-MAY-23
16597|Sandhills Creek Limestone Member|Proposed publication|Felton E.A. and Huleatt M.B. 1975. Geology of the Braidwood 1:100 000 sheet. Geological Surv. NSW, Sydney.|16-MAY-23
16597|Sandhills Creek Limestone Member|References|01/31634|16-MAY-23
16597|Sandhills Creek Limestone Member|Parent|De Drack Formation (Felton and Huleatt, 1975)|16-MAY-23
26134|Sapling Flat Igneous Complex|Name source|After Sapling Flat Creek which trends along the north-northwest extremity of the mass.|16-MAY-23
26134|Sapling Flat Igneous Complex|Unit history|Joplin et al. (1953) introduced the name Sapling Flat Granite and this usage was continued by subsequent workers.|16-MAY-23
26134|Sapling Flat Igneous Complex|Type section locality|The complex has been divided into two main phases. These are the Wangrah Adamellite and the Danswell Creek Granodiorite. Type areas are defined under these latter names.|16-MAY-23
26134|Sapling Flat Igneous Complex|Description at type locality|Refer Wangrah Adamellite and Danswell Creek Granodiorite.  Size: 26.7 km2. The complex is a meridionally elongate mass of irregular width, developing from 0.3 km wide near the Bredbo-Jerangle Road to a maximum width of 3.8 km near Jerangle and decreasing northwards to 0.8 km.|16-MAY-23
26134|Sapling Flat Igneous Complex|Extent|The Complex lies in the southeast portion of the Michelago 1:100 000 Geological Sheet area, to the west of Jerangle and parallel to the Bredbo-Jerangle Road.|16-MAY-23
26134|Sapling Flat Igneous Complex|Relationships and boundaries|Intrudes Late Ordovician metasediments (Foxlow Beds. The Narongo Fault along the eastern boundary of the complex separates it from Late Silurian sediments and volcanics (the Kohinoor Volcanics). Contact metamorphism is best developed along the northern and northeast margins.|16-MAY-23
26134|Sapling Flat Igneous Complex|Age reasons|Late Silurian to Earliest Devonian (refer Wangrah Adamellite and Danswell Creek Granodiorite).|16-MAY-23
26134|Sapling Flat Igneous Complex|Proposed publication|Geological Slurvey of NSW 1:100 000 Note Series|16-MAY-23
26134|Sapling Flat Igneous Complex|Status|1|16-MAY-23
26134|Sapling Flat Igneous Complex|Unit name|Sapling Flat Igneous Complex (nov. after Joplin et al. 1953)|16-MAY-23
73110|Sea Acres Dolerite|Name source|Sea Acres Nature Reserve, Port Macquarie|16-MAY-23
73110|Sea Acres Dolerite|Type section locality|The type area of the unit is located at southern end of Shelly Beach, Sea Acres National Park (31o27'33"S 152o56'06"E) where 10 m wide of feldspar phyric dolerite has intruded both the Port Macquarie Serpentinite and Watonga Formation.|16-MAY-23
73110|Sea Acres Dolerite|Description at type locality|Fine-medium grained dark green plagioclase-phyric rocks, undeformed and with alteration confined to narrow quartz epidote veins except locally where it intrudes Port Macquarie Serpentinite and Watonga Formation, minor epidote development close to joints. The dykes, which have chilled margins up to several centimetres wide range in width from 0.15 m to 10 m, are moderately to steeply dipping.|16-MAY-23
73110|Sea Acres Dolerite|Extent|Dolerite dykes included in the Karikeree Metadolerite by Leitch (1980a) but distinguished from bodies typical of this unit by their comparative lack of alteration and a distinctive geochemistry, notably elevated abundances of Fe, TiO2 and Zr are here grouped in a new unit, the Sea Acres Dolerite, the name coming from the proximity to the Sea Acres National Park at GR 93841913 where the rocks are typically exposed at Shelly Beach.|16-MAY-23
73110|Sea Acres Dolerite|Thickness range|...as above...|16-MAY-23
73110|Sea Acres Dolerite|Lithology|...as above...|16-MAY-23
73110|Sea Acres Dolerite|Relationships and boundaries|Intrusive into the Watonga Formation, Port Macquarie Serpentinite, Tacking Point Gabbro, Karikeree Metadolerite, Nobbys Beach Lamprophyre and felsic dykes, the last younger than 240Ma (Aitchison & Ireland, 1995).|16-MAY-23
73110|Sea Acres Dolerite|Age reasons|Late Triassic as they cut a felsic dyke that is possibly 240 Ma (Aitchison and Ireland 1995)|16-MAY-23
73110|Sea Acres Dolerite|References|AITCHISON, J. C. & IRELAND, T. R. 1995. Age profile of ophiolitic rocks across the Late Palaeozoic New England Orogen, New South Wales: implications for tectonic models. Australian Journal of Earth Sciences  42, 11-23.LEITCH, E. C. 1980a. Rock units, structure and metamorphism of the Port Macquarie Block, eastern New England Fold Belt. Proceedings of the Linnean Society of New South Wales 104, 273-292.|16-MAY-23
70121|Silver City Suite|Name source|After the Silver City Highway which passes close to, or over several of the metagranites.|16-MAY-23
70121|Silver City Suite|Unit history|Willis et al. (1983) observed that a number of granitic gneiss bodies approximately occupy two stratigraphic positions and interpreted them as metamorphosed acid volcanic rocks, part of the Thackaringa Group. More recent evidence, especially geochronology, has shown that these gneisses are metamorphosed and deformed granites (see text). Therefore, they are excluded from the Thackaringa Group. The Silver City Suite is erected to accommodate these metagranites.|16-MAY-23
70121|Silver City Suite|Constituents|Alma Granite Gneiss, Georges Bore Granite Gneiss, Stephens Creek Granite Gneiss, Wondervale Well Granite Gneiss, Rasp Ridge Granite Gneiss and other unnamed granite gneiss bodies.|16-MAY-23
70121|Silver City Suite|Type section locality|The large Stephens Creek Granite Gneiss body is nominated as the type metagranite body.|16-MAY-23
70121|Silver City Suite|Extent|Mainly concentrated in a belt extending northeastwards from near Oakdale homestead, through Broken Hill to Stephens Creek and in the Euriowie Inlier near Paringa homestead. Other metagranite bodies include those north of Thackaringa, south of Silverton, at Mundi Mundi Creek and in the eastern part of the Darling Range.|16-MAY-23
70121|Silver City Suite|General description|The granite gneiss bodies tend to be elongate parallel to the enclosing stratigraphy, except where they occupy fold closures. The largest body is the Stephens Creek Granite Gneiss, a mass 18 km   5 km occupying a fold hinge, while some of the smaller bodies are 50 - 300 m across and a few kilometres in length.|16-MAY-23
70121|Silver City Suite|Lithology|The Silver City Suite of metagranites are quartz - feldspar - biotite gneisses with or without garnet, sillimanite and/or retrograde muscovite. The gneisses include evenly medium- to fine-grained varieties and megacrystic varieties. Leucocratic variants occur in some bodies. Partial melting during the ca 1600 Ma Olarian Orogeny produced granitic to pegmatitic leucosome veins and patches, constituting up to 20% of the volume of the granite gneisses.Wyborn et al. (1997) classed the 'Potosi Supersuite', including the proposed Silver City Suite, as S-type, restite-rich and showing no evidence of fractionation.|16-MAY-23
70121|Silver City Suite|Relationships and boundaries|All of the granite gneiss bodies of the Silver City Suite are intrusive into the Thackaringa Group and/or into lower Broken Hill Group. The Alma Granite Gneiss intrudes at the lowest stratigraphic level, into the Alders Tank Formation or the lowest part of the Cues Formation. The Rasp Ridge Granite Gneiss and the Wondervale Well Granite Gneiss were emplaced at the top of the Thackaringa Group. Zircon U - Pb dating (see text) indicates that granite emplacement took place no more than ~10 million years after deposition of the host sedimentary rocks.|16-MAY-23
70121|Silver City Suite|Age reasons|Ranges from 1704 ± 3 Ma to 1683 ± 3 Ma. SHRIMP U - Pb zircon dating: Page et al. 2005a and this paper.|16-MAY-23
70121|Silver City Suite|Defn Reference|Stevens B.P.J., Page R.W. and Crooks A. 2008, 'Geochronology of Willyama Supergroup metavolcanics, metasediments and contemporaneous intrusions, Broken Hill, Australia' , Australian Journal of Earth Sciences, vol. 55(3) p328-329.|16-MAY-23
25478|Sinclair Conglomerate Member|Name source|Named after Sinclair Trig. Station (859 m) on the Michelago 1:100 000 sheet area (Richardson 1979).|16-MAY-23
25478|Sinclair Conglomerate Member|Unit history|None.|16-MAY-23
25478|Sinclair Conglomerate Member|Type section locality|Beds of lithic tuff with locally rounded boulders of slate, quartzite and dacitic porphyry crop out in a drainage line at GR 229/298 on the Michelago 1:100 000 sheet 8726.  The 'conglomerate facies' with limited strike length is a local development in the unit. Top and bottom are not exposed.|16-MAY-23
25478|Sinclair Conglomerate Member|Extent|The unit forms two narrow outcrops belts (probably as limbs of an overturned syncline) separated by argillaceous sediments in the southeast corner of the Canberra 1:100 000 sheet area. The unit is absent along the western edge of the Captains Flat Graben.|16-MAY-23
25478|Sinclair Conglomerate Member|Thickness range|Estimated as 130m by Oldershaw (1965).|16-MAY-23
25478|Sinclair Conglomerate Member|Lithology|Lithic tuff with minor conglomerate interbedded with shale.|16-MAY-23
25478|Sinclair Conglomerate Member|Depositional environment|Shallow marine.|16-MAY-23
25478|Sinclair Conglomerate Member|Relationships and boundaries|A member within the Captains Flat Formation.|16-MAY-23
25478|Sinclair Conglomerate Member|Age reasons|Late Silurian based on its conformable position within the Captains Flat Formation.|16-MAY-23
25478|Sinclair Conglomerate Member|Correlations|Local derivation without a known correlative outside the Captains Flat Block.|16-MAY-23
25699|State Mine Creek Formation|Name source|State Mine Creek, Lithgow Valley|16-MAY-23
25699|State Mine Creek Formation|Unit history|New name (C.S. Bembrick)|16-MAY-23
25699|State Mine Creek Formation|Type section locality|(1) Location: Elecom Lithgow-Newnes DDH31 (221925mE, 1310965mN, Lithgow 1:50 000 sheet, 8931-111).  (2) Repository - Elecom core store, Lithgow.  Reference Section: Brickworks Quarry, GR 376921 Lithgow 8931-111.|16-MAY-23
25699|State Mine Creek Formation|Extent|Western Coalfield. Lithgow and Bungleboori 1:50 000 sheets. Equivalent lithologies known in Ulan area. Also occurs on parts of the Hampton, Katoomba, Glen Davis and Glen Alice sheets.|16-MAY-23
25699|State Mine Creek Formation|General description|Locally completely or partially eroded by The Gap Sandstone. Commonly contains the Moolarben Coal Member at or near base. The top and base of this unit marked by a transition from argillaceous and/or coaly and carbonaceous sediments to sandstone.|16-MAY-23
25699|State Mine Creek Formation|Thickness range|(1) Type Section - from 228.86 m to 239.22 m. Thickness 10.36 m.  (2) Maximum recorded 31.5 m.|16-MAY-23
25699|State Mine Creek Formation|Lithology|Claystone, mudstone, siltstone, often interbedded; minor sandstone and coal.|16-MAY-23
25699|State Mine Creek Formation|Relationships and boundaries|Conformably overlain by the Gap Sandstone and underlain by the Angus Place Sandstone. Part of Charbon Sub-Group.|16-MAY-23
25699|State Mine Creek Formation|Proposed publication|Australian Coal Geology|16-MAY-23
25699|State Mine Creek Formation|Proposer|Bembrick C.S., Robertson Research (Australia) Pty Limited|16-MAY-23
70114|Stephens Creek Granite Gneiss|Name source|Stephens Creek flows (very occasionally) across the southern, poorly outcropping part of this granite gneiss.|16-MAY-23
70114|Stephens Creek Granite Gneiss|Type section locality|Between GR 529230E 6456700N and GR 529475E 6456270N (Zone 54 AGD 1966). This is a double thickness type section across the width of the Stephens Creek Fold (Stroud 1989b). The grid references above are both on the stratigraphic top of the Stephens Creek Gneiss. The mid-point of the line is close to the probable base of the body.|16-MAY-23
70114|Stephens Creek Granite Gneiss|Extent|Occupies the core of the Stephens Creek Fold, 18 km long and 5 km across the folded width. Thickness before folding was probably about 2 km.|16-MAY-23
70114|Stephens Creek Granite Gneiss|Lithology|The Stephens Creek Granite Gneiss comprises three main varieties of granite gneiss (Stroud 1978a, 1989b) (simplified in Figure 11), zoned as follows: (i) the lowest zone consists of medium- to coarse-grained quartz - feldspar - biotite gneiss with sillimanite aggregates; (ii) the middle zone consists of medium- to coarse-grained gneiss with abundant K-feldspar megacrysts; and (iii) the relatively thin upper zone consists of medium- to coarse-grained quartz - feldspar - biotite gneiss with few megacrysts. Amphibolite/basic granulite sills and dykes are abundant in the upper half of the Stephens Creek Granite Gneiss.|16-MAY-23
70114|Stephens Creek Granite Gneiss|Relationships and boundaries|On both limbs of the Stephens Creek Fold, the Stephens Creek Granite Gneiss is stratigraphically overlain by Broken Hill Group, specifically the Allendale Metasediments or the Parnell Formation. In the core of the fold, there is an area of psammitic to psammopelitic metasediments lacking any diagnostic features for stratigraphic classification. Some of these metasediments contain disseminated magnetite.|16-MAY-23
70114|Stephens Creek Granite Gneiss|Age reasons|Ranges from 1689 ± 5 to 1686 ± 4 Ma. SHRIMP U - Pb zircon dating, this paper.|16-MAY-23
70114|Stephens Creek Granite Gneiss|Defn Reference|Stevens B.P.J., Page R.W. and Crooks A. 2008, 'Geochronology of Willyama Supergroup metavolcanics, metasediments and contemporaneous intrusions, Broken Hill, Australia' , Australian Journal of Earth Sciences, vol. 55(3) p329-330.|16-MAY-23
24505|Stockinbingal Formation|Name source|Stockinbingal (GR 73725889, Cootamundra 1:250 000).|16-MAY-23
24505|Stockinbingal Formation|Type section locality|A number of local sections are nominated GR 58567436 to GR 58457435, GR 59107352 to GR 59037351, GR 59387320 to GR 59347312, and GR 59327310 to GR 59207319, Cootamundra 1:250 000 sheet.|16-MAY-23
24505|Stockinbingal Formation|Extent|The unit is exposed in a narrow (less than 4 km wide) belt extending about 7 km south and north from Stockinbingal.|16-MAY-23
24505|Stockinbingal Formation|Thickness range|500-1000 m(?)|16-MAY-23
24505|Stockinbingal Formation|Lithology|Tuffs, dacitic and lithic with minor garnet and magnetite-bearing lavas. Tuffs are dominantly airfall, some ash flow tuffs near base; minor chert, conglomerate, and pyritic siltstones.|16-MAY-23
24505|Stockinbingal Formation|Relationships and boundaries|Overlies Frampton Volcanics with local unconformities. Overlain by undifferentiated sequence of siltstone, conglomerate, and sandstone.|16-MAY-23
24505|Stockinbingal Formation|Age reasons|Equivalent to Bethungra Formation where a brachiopod fauna (schizophorid, strophoedontid, and rynchonellid species) was identified as Early Devonian by K.S.W. Campbell of Australian National University (Schmidt 1972).|16-MAY-23
24505|Stockinbingal Formation|Proposed publication|Cootamundra 1:250 000 Metallogenic Map SI 55-11, Mine Data sheets and Metallogenic Study.|16-MAY-23
24505|Stockinbingal Formation|Proposer|Fitzpatrick K, after B.L. Schmidt|16-MAY-23
26154|Sutton Granodiorite|Name source|The village of Sutton, NSW at GR 051/063.|16-MAY-23
26154|Sutton Granodiorite|Unit history|Sutton Granite and Greenwood Granite (Joplin and others, 1953, Moore, 1957 and Stauffer and others, 1964); Bywong Granite (Moore, 1957)  and Sutton Group (Strusz, 1971).|16-MAY-23
26154|Sutton Granodiorite|Type section locality|Slopes west of Bywong Hill where the unit is represented by tors and pavements of mildly deformed coarse biotite-rich granodiorite (Canberra 1:100 000 sheet 8727).|16-MAY-23
26154|Sutton Granodiorite|Extent|As elongated stocks roughly parallel to meridional trending Ordovician sediments.  The northerly intrusion (10km2) form the western half of a small range culminating in Bywong Hill (GR 079/083).  To the southwest a smaller intrusion of 4km2 is poorly exposed in elevated wooded terrain west of Greenwood Hill (GR 040/989).  The subsurface extent maybe inferred from hornfelsed and spotted sediments in a surrounding contact metamorphic aureole.|16-MAY-23
26154|Sutton Granodiorite|General description|Pale grey granodiorite with small and sparsely distributed hornblende-rich xenoliths. The intrusions are cut by quartz reefs and occasional aplite veins. Specimens typically contain quartz, zoned plagioclase, perthitic potash feldspar, biotite, accessory zircon, apatite and allanite. Two magnetic anomalies (BMR 1978) indicate these intrusions are relatively rich in magnetite. Poorly exposed outcrops of leucocratic adamellite and felsic porphyry maybe a fractionated sequence cogenetic with the granodiorite.|16-MAY-23
26154|Sutton Granodiorite|Age reasons|Intrudes and hornfelses Late Ordovician Pittman Formation. Upper age limit constrained by an East-West trending dolerite dyke of presumed Early Devonian age which cuts a marginal intrusion south of Oakdale Homestead (GR 093/109). A latest Silurian age is indicated by a Rb-Sr date of 410+/-4Ma.  Presence of allanite and hornblende-rich xenoliths suggest the Sutton Granodiorite is probably an I-type intrusion and probably the same age as similar I-type intrusions south of Queanbeyan, eg., Barracks Creek Adamellite and Googong Adamellite.|16-MAY-23
72990|Tacking Point Gabbro|Name source|Tacking Point Gabbro 6 km south southeast of Port Macquarie township.|16-MAY-23
72990|Tacking Point Gabbro|Type section locality|The type area comprises rocky outcrops immediately south of the headland of Watonga Formation at the south end of Miners Beach  about 250 m north of Tacking Point lighthouse (31o28'20"S 152o56'16"E).|16-MAY-23
72990|Tacking Point Gabbro|Description at type locality|Gabbroic body ranging from pyroxene-rich melanocratic gabbro to plagioclase dominated leucocratic gabbro, gabbroic pegmatite and uncommon aplite, all highly altered.|16-MAY-23
72990|Tacking Point Gabbro|Extent|A pluton exposed in the inter-tidal and on rock platforms zone 200 m north of the Tacking Point Lighthouse intruding the Watonga Formation.|16-MAY-23
72990|Tacking Point Gabbro|Lithology|Gabbroic body ranging from pyroxene-rich melanocratic gabbro to plagioclase dominated leucocratic gabbro, gabbroic pegmatite and uncommon aplite, all highly altered.|16-MAY-23
72990|Tacking Point Gabbro|Relationships and boundaries|Intrusive into the Watonga Formation.|16-MAY-23
72990|Tacking Point Gabbro|Age reasons|(?) Permian based on geochemical affinity with the 290 - 250 Ma Clarence River Supersuite (Och 2007; Och and Leitch, in prep).|16-MAY-23
72990|Tacking Point Gabbro|Correlations|Town Beach Diorite|16-MAY-23
72990|Tacking Point Gabbro|References|OCH, D. J. 2007. Eclogite, serpentinite, melange and mafic intrusive rocks: manifestation of long-lived Palaeozoic convergent margin activity, Port Macquarie, eastern Australia. Unpublished PhD thesis, University of Technology, Sydney.   OCH, D. J. and LEITCH, E. C. (in prep) New and revised lithostratigraphic units from the Port Macquarie Block, northeastern New South Wales. Quarterly Notes - Geological Survey of New South Wales.|16-MAY-23
24511|Tallaganda Granodiorite|Name source|Tallaganda State Forest which is partly underlain by the granodiorite.|16-MAY-23
24511|Tallaganda Granodiorite|Type section locality|Bluffs about 3 m high on the SW side of the Hilltop-Rossi road at GR 293680.|16-MAY-23
24511|Tallaganda Granodiorite|Extent|North west corner of Araluen 1:100 0000 sheet area where it occupies about 8.5 km2. Occupies about 10 km2 in adjacent Michelago 1:100 000 sheet area and probably less than 2 km2 in adjacent Braidwood 1:100 000 sheet area.|16-MAY-23
24511|Tallaganda Granodiorite|Lithology|Foliated, quartz-rich granodiorite with about 10% mafic minerals (recrystallised biotite, epidote, allanite, sphene and opaques).|16-MAY-23
24511|Tallaganda Granodiorite|Age reasons|Probably early Devonian as it is intruded by dolerite dykes similar to late Devonian dolerites further east, however both the granodiorite and dolerites have been deformed in the Carboniferous Kanimblan Fold episode.|16-MAY-23
24511|Tallaganda Granodiorite|Defn author|Wyborn D., Owen M., 1986|16-MAY-23
24511|Tallaganda Granodiorite|Proposed publication|BMR map commentary: Araluen 1:100 000 Sheet|16-MAY-23
24511|Tallaganda Granodiorite|Proposer|Wyborn D.|16-MAY-23
24511|Tallaganda Granodiorite|Resdate|26-MAY-1982|16-MAY-23
24511|Tallaganda Granodiorite|Reserved? Yes/No|Yes|16-MAY-23
26327|Taplow Limestone Member|Name source|The name derives from Taplow Flat (GR 738815), 1.2 km west of the type locality. (*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978).|16-MAY-23
26327|Taplow Limestone Member|Unit history|Informally named the 'upper coral' unit (Webby 1969).|16-MAY-23
26327|Taplow Limestone Member|Type section locality|Type section on Dunhill Bluff (GR 753814*) immediately to the north-east of Fossil Hill. (*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978).|16-MAY-23
26327|Taplow Limestone Member|Thickness range|It is 10 m thick in type section.|16-MAY-23
26327|Taplow Limestone Member|Identifying features|the Taplow Limestone Member of the Fossil Hill Limestone has its type section on Dunhill Bluff (GR 753814*) immediately to the north-east of Fossil Hill. A 1 m-thick unit of grey, massive-bedded skeletal wackestones and packstones with large colonies of Tetradium cribriforme defines the base of the Taplow Limestone Member on Dunhill Bluff.  The directly underlying beds are thin, nodular, skeletal wackestones and calcareous siltstones of the Wyoming Limestone Member. A similar sharp contact with the underlying Wyoming Limestone Member exists in the Fossil Hill section. Massively bedded skeletal packstones and grainstones form the lower part, and thinner bedded skeletal wackestones, lime mudstones and minor interbedded shales the upper part of the Taplow Limestone Member. The transition into the overlying Dunhill bluff limestone Member is gradational with the boundary placed on the top of the last 0.12 m thick 'platy' limestone bed. Succeeeding beds of the Dunhill Bluff Limestone Member are thinner, more prominently nodular, and have more conspicuous shaly partings. The Taplow Limestone Member has been mapped as a persistent and recognizable unit throughout the Cliefden Caves area. (*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978).|16-MAY-23
26327|Taplow Limestone Member|Proposed publication|Stratigraphy of Cliefden Caves Limestone Group (Upper Ordovician) central NSW. J. geol. Soc. Aust.|16-MAY-23
26327|Taplow Limestone Member|Defn Reference|82/23085 |16-MAY-23
26327|Taplow Limestone Member|Proposer|Webby B.D., Packham G.H.|16-MAY-23
26327|Taplow Limestone Member|Resdate|12-MAY-1981|16-MAY-23
26327|Taplow Limestone Member|Reserved? Yes/No|Central Register, BMR Canberra (Ref. 80/1569)|16-MAY-23
25516|Tarago Conglomerate|Unit history|Red Bed Stage (Garretty, 1936). This name was applied to "a thick series of boulder beds and tuffs [actually arenites containing some tuffaceous material] outcropping as a horeshoe-shaped exposure to the south of Tarago", this sequence being equivalent to the Tarago Conglomerate as now defined.|16-MAY-23
25516|Tarago Conglomerate|Type section locality|In Merigan Creek, adjacent to the railway line, 3 km southwest of Tarago (GR 420159 Braidwood 1:100 000 sheet).|16-MAY-23
25516|Tarago Conglomerate|Extent|The unit crops out extensively around the northern flanks of the Woolowalar Ridge, (GR 393099, Braidwood 1:100 000 sheet) about 3 km southwest of Tarago. It continues to the north as far as Lake Bathurst township (GR 417217 Braidwood 1:100 000 sheet). Isolated but fairly extensive outcrops occur to the south, at GR 358762, and GR 388047. Isolated but fairly extensive outcrops occur to the south at GR 358762, and GR 388047. The unit does not occur outside the Braidwood 1:100 000 sheet area.|16-MAY-23
25516|Tarago Conglomerate|Thickness range|Variable; maximum probably of the order of 300 m.|16-MAY-23
25516|Tarago Conglomerate|Lithology|Boulder and pebble conglomerate, purple in colour; coarse red arenite, red siltstone.|16-MAY-23
25516|Tarago Conglomerate|Relationships and boundaries|Unconformably overlies Silurian-early Early Devonian Mount Fairy Group; overlain, possibly disconformably, by the late Early Devonian Bongalaby Formation; unconformably overlies Ordovician Birkenburn Beds and Early Devonian Boro Granite. Base of unit contains boulders of igneous rock up to 1 m diameter; top of unit always poorly exposed but consists mainly of arenite and siltstone with occasional pebbles.|16-MAY-23
25516|Tarago Conglomerate|Age reasons|Middle to Late Early Devonian (Siegenian-Emsian); Lake Bathurst Limestone (Siegenian-Emsian); Lake Bathurst Limestone Member of the Bongalaby Formation is dated as Emsian (Philip & Pedder, 1968) and the underlying Covan Creek Formation is dated as Early Devonian (Sherwin, 1973).|16-MAY-23
25516|Tarago Conglomerate|Proposed publication|Felton E.A. and Huleatt M.B., 1975.  Geology of the Braidwood 1:100 000 Sheet. Geol. Surv. NSW, Sydney.|16-MAY-23
17938|Temi Formation|Name source|Parish of Temi, County of Buckland.|16-MAY-23
17938|Temi Formation|Unit history|The original Temi Group/Formation (Hanlon, in Hill, 1954) has been subdivided into two new units - an older unit named the Kerona Formation, while the name Temi Formation has been retained for the thicker, more characteristic unit.|16-MAY-23
17938|Temi Formation|Type section locality|Willow Tree, NSW.   Location of Type Section: Here designated from 824905 to 823893 along Brees Gully (Quirindi A-D 1:31 680 topographic sheets).|16-MAY-23
17938|Temi Formation|Extent|Exposed in the Temi Syncline and Back Creek Anticline.|16-MAY-23
17938|Temi Formation|Thickness range|a) At type section:  600 ft;  b) Maximum known:  600 ft.|16-MAY-23
17938|Temi Formation|Relationships and boundaries|The Temi Formation conformably overlies the Kerona Formation on the western limb of the Back Creek Anticline. Elsewhere it unconformably overlies the Willawarra Dacite or Inglewood Mudstone. The Werrie Formation conformably overlies the Temi Formation.|16-MAY-23
17938|Temi Formation|Age reasons|Early Permian - glossopterid remains.|16-MAY-23
17938|Temi Formation|Proposed publication|Journal & Proc. Royal Soc. Of NSW|16-MAY-23
17938|Temi Formation|Defn approved by|Approved. Copied from xerox sent by NSW Stratigraphic Nomenclature Sub-Committee.|16-MAY-23
40755|The Calpe Ignimbrite Member|Name source|From the property named The Calpe (0242000E 6620900N Berrioye 1: 25 000 sheet).|16-MAY-23
40755|The Calpe Ignimbrite Member|Type section locality|Locality 440-2 on The Calpe 30o30'49"S, 150o18'43"E (0242055E 6621200N Berrioye 1: 25 000 sheet).|16-MAY-23
40755|The Calpe Ignimbrite Member|Extent|Extends from Mount Byar in the north to hills between Maules and Connors Creek Creeks in the south.|16-MAY-23
40755|The Calpe Ignimbrite Member|Thickness range|~10-20 m, but possibly thicker in the south.|16-MAY-23
40755|The Calpe Ignimbrite Member|Lithology|In the type area adjacent to Maules Creek, unwelded, pink to purple ignimbrite with phenocrysts of quartz, plagioclase, minor K-feldspar and biotite; groundmass shard-rich, partly micropoikilitic, vitric at the base. At Mount Byar, moderately welded, orange, ignimbrite with plagioclase, minor K-feldspar, opaque minerals, minor pumice fragments and a spherulitic groundmass.|16-MAY-23
40755|The Calpe Ignimbrite Member|Age reasons|?Late Namurian.|16-MAY-23
24518|The Secrets Andesite|Name source|The Secrets Prospect, Parkes GR 61799103 Forbes 1:250 000.|16-MAY-23
24518|The Secrets Andesite|Type section locality|Prospect area. Basal boundary not defined as it does not crop out. Traverse from top of unit in road material quarry to west.|16-MAY-23
24518|The Secrets Andesite|Extent|Core of anticline west of Parkes. Mapped over 5 km of strike.|16-MAY-23
24518|The Secrets Andesite|Thickness range|Over 1000 m at type section. Range uncertain.|16-MAY-23
24518|The Secrets Andesite|Lithology|Includes all the flow andesites of the Goonumbla Volcanics.|16-MAY-23
24518|The Secrets Andesite|Relationships and boundaries|Underlies Black Ridge Tuff together with which it forms the constituent formations of the Goonumbla Volcanics (Group) (Andrews, 1910).|16-MAY-23
24518|The Secrets Andesite|Age reasons|Possible Latae Ordovician from stratigraphic evidence.|16-MAY-23
24518|The Secrets Andesite|Proposed publication|Records Geol. Surv. NSW|16-MAY-23
24518|The Secrets Andesite|Proposer|Bowman H.N.|16-MAY-23
24518|The Secrets Andesite|Resdate|18-JUN-1975|16-MAY-23
37917|The Tops Rhyolite Member|Name source|From the property The Tops GR356970 Terry Hie Hie 1:50 000 sheet.|16-MAY-23
37917|The Tops Rhyolite Member|Geomorphic expression|Ridge-forming.|16-MAY-23
37917|The Tops Rhyolite Member|Type section locality|Roadside exposures on The Tops road (GR345977 Terry Hie Hie 1:50 000 sheet).|16-MAY-23
37917|The Tops Rhyolite Member|Extent|Crops out over approximately 10 km on both limbs in the northern part of the Rocky Creek Syncline (P.G. Flood unpublished data); on the western limb from GR350951 in the south to GR371054 in the north; on the eastern limb from GR374967 in the south to GR393050 in the north (all from the Terry Hie Hie 1:50 000 sheet.|16-MAY-23
37917|The Tops Rhyolite Member|Thickness range|12m.|16-MAY-23
37917|The Tops Rhyolite Member|Lithology|Unwelded grey-green to red ignimbrite. The grey-greeen beds contain abundant coarse feldspars, predominantly plagioclase including zoned crystals, sparse quartz and biotite. The groundmass is pumiceous and has well preserved flow features, but shards and bubble walls are rarely preserved; original pumice has been replaced by a fine mosaic of chlorite and zeolite. The red ignimbrite  is finer grained, contains the same mineral assemblage but with more abundant quartz, and has tube pumices. The groundmass is largely vitric.|16-MAY-23
37917|The Tops Rhyolite Member|Depositional environment|Ignimbrite.|16-MAY-23
37917|The Tops Rhyolite Member|Relationships and boundaries|The youngest ignimbrite within the Rocky Creek succession.|16-MAY-23
37917|The Tops Rhyolite Member|Age reasons|Carboniferous (Namurian or Westphalian).|16-MAY-23
34356|The Valley Tank Arenite Member|Name source|The Valley Tank - which lies 4.25 km northwest of Nundooka Station.|16-MAY-23
34356|The Valley Tank Arenite Member|Type section locality|The type section is made ~2.5 km south of The Valley Tank from 4700 1786 (base) to 4716 1799, Cobham Lake 1:250 000 Sheet.|16-MAY-23
34356|The Valley Tank Arenite Member|Extent|The member extends 24 km northwards from Sandstone Tank to northeast of The Veldt. It is also recognised south of the Silver City Highway and also in Bancannia South No. 1 well (between 2845 m to 2867 m).|16-MAY-23
34356|The Valley Tank Arenite Member|Thickness range|The member is ~150 m thick at the type section.|16-MAY-23
34356|The Valley Tank Arenite Member|Lithology|The member is composed of subangular and subrounded coarse and very coarse grained pebbly arenite.|16-MAY-23
34356|The Valley Tank Arenite Member|Relationships and boundaries|The member is conformable with the lower fine arenite (below) and the central fine arenite (above). It lies within the Coco Range Sandstone.|16-MAY-23
34356|The Valley Tank Arenite Member|Age reasons|The member is considered to Emsian-Eifelian in age (from the fish fragments at the base of the lower fine arenite).|16-MAY-23
34356|The Valley Tank Arenite Member|Proposed publication|Australian Journal of Earth Sciences.|16-MAY-23
34356|The Valley Tank Arenite Member|Category|2|16-MAY-23
34356|The Valley Tank Arenite Member|Reserved? Yes/No|Yes|16-MAY-23
24527|Toggannoggra Rhyolite Member|Name source|Toggannoggra homestead, GR 360524.|16-MAY-23
24527|Toggannoggra Rhyolite Member|Unit history|The name is probably synonymous with the whole of the Long Flat Volcanics as used in the Braidwood 1:100 000 sheet area.|16-MAY-23
24527|Toggannoggra Rhyolite Member|Type section locality|The bed of the Shoalhaven River at GR 361526|16-MAY-23
24527|Toggannoggra Rhyolite Member|Extent|Occupies a large area of the Shoalhaven River valley north of Wyanbene and extends onto the Braidwood 1:100 000 sheet area.|16-MAY-23
24527|Toggannoggra Rhyolite Member|Lithology|Porphyritic pale cream, buff or grey rhyolite with about 30-35% phenocrysts up to 3 mm. Phenocrysts include plagioclase (mostly An25-30 but some grains have cores of An50-60), quartz, alkali feldspar and chloritised biotite (2%). Accessories include allanite opaques, apatite and zircon. The groundmass commonly shows well developed eutaxitic layering indicative of ignimbritic deposition.|16-MAY-23
24527|Toggannoggra Rhyolite Member|Age reasons|Overlies the Late Silurian De Drack Formation and is intruded by the Early Devonian Jinden Adamellite and Braidwood Granodiorite after the rhyolite had been folded. Hence it is Late Silurian or possibly Early Devonian in age.|16-MAY-23
24527|Toggannoggra Rhyolite Member|Proposed publication|BMR map commentary: Araluen 1:100 000 Sheet|16-MAY-23
24527|Toggannoggra Rhyolite Member|Defn Reference|Wyborn D., Owen M., 1986|16-MAY-23
24527|Toggannoggra Rhyolite Member|First Reference|86/25183|16-MAY-23
24527|Toggannoggra Rhyolite Member|Resdate|21-JUN-1982|16-MAY-23
26175|Tomboye Basalt|Name source|"Tomboye" property, GR 707946, Braidwood 1:100 000 sheet.|16-MAY-23
26175|Tomboye Basalt|Type section locality|At "Tomboye" Trig. Station, GR 674963, Braidwood, 1:100 000 sheet.|16-MAY-23
26175|Tomboye Basalt|Extent|Occurs in the eastern part of the Braidwood 1:100 000 sheet, where all outcrops lie within a few kilometres of the Braidwood-Nowra road in the vicinity of "Tomboye".|16-MAY-23
26175|Tomboye Basalt|Thickness range|Variable; estimated thickness at type section 40 metres.|16-MAY-23
26175|Tomboye Basalt|Lithology|Olivine basalt.|16-MAY-23
26175|Tomboye Basalt|Relationships and boundaries|Overlies weathered Early Palaeozoic metasediments and thin deposits of Tertiary ferricrete and is overlain by weakly consolidated quartz sand and gravel.|16-MAY-23
26175|Tomboye Basalt|Age reasons|Carr (1966) records tawo dates for the basalt : 43.60 x 106 and 40.46 x 106 years (+/- 3 percent). The difference in ages may be due to sampling from different flows. These ages place the basalt in the Late Eocene.|16-MAY-23
26175|Tomboye Basalt|Proposed publication|Felton E.A., Huleatt M.B., 1975. Geology of the Braidwood 1:100 000 Sheet. Geological Surv. NSW, Sydney.|16-MAY-23
26175|Tomboye Basalt|Name first published by|Felton E.A., Huleatt M.B., 1977|16-MAY-23
18317|Tomingley Siltstone|Name source|Village of Tomingley, GR 628971, Narromine 1:250 000 Sheet.|16-MAY-23
18317|Tomingley Siltstone|Unit history|Previously published as the Towingley Beds (R.L. Brunker, 1967).|16-MAY-23
18317|Tomingley Siltstone|Type section locality|To south of Tomingley village.|16-MAY-23
18317|Tomingley Siltstone|Extent|Extends from Narromine (Narromine 1:250 000 Sheet) south for 80 km. Further south, it probably extends for another 100 km but has not been differentiated from andesites and limestones in mapping.  Size: Estimated maximum thickness of 7.5 km. However, undetected/unmapped folding may have excessively exaggerated this thickness.|16-MAY-23
18317|Tomingley Siltstone|Lithology|Slate, silicified siltstone, fine sandstone, shale.|16-MAY-23
18317|Tomingley Siltstone|Relationships and boundaries|Underlies the Mugincoble Chert (M. Ordovician). Unconformably overlain by the Early Devonian Narwonah Rhyolite.|16-MAY-23
18317|Tomingley Siltstone|Age reasons|E-M Ordovician.|16-MAY-23
18317|Tomingley Siltstone|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982|16-MAY-23
18317|Tomingley Siltstone|Proposed publication|A Metallogenic Study of the Narromine 1:250 000 Sheet|16-MAY-23
18317|Tomingley Siltstone|Reserved? Yes/No|As Tomingley Beds|16-MAY-23
18490|Tout Intrusive Complex|Name source|Derived from Parish named "TOUT" in which the complex is found.|16-MAY-23
18490|Tout Intrusive Complex|Unit history|Previously referred to by Raggott (1937, Ann Dip Dip Mines, p.93) as "Fifield hornblende rock". No other published references.|16-MAY-23
18490|Tout Intrusive Complex|Type section locality|To the south of the road at GR 542950. Type Section: Drill core, drilled by Anaconda Australia Inc. FKDZ, 978 ft Narromine 1:250 000 SE-55/3 GR 5484095290.|16-MAY-23
18490|Tout Intrusive Complex|Thickness range|(a) Elyptical in shape, 18 km by 6 km (at type section).|16-MAY-23
18490|Tout Intrusive Complex|Lithology|The bulk of the intrusive is intermediate to basic in composition. It ranges from augite/pyroxenite, biotite pyroxenite, hornblendite, hornblend/pyroxenite, hornblende rich diorite, syenite, quartz-hornblende monzonite to hornblende adamellite.|16-MAY-23
18490|Tout Intrusive Complex|Relationships and boundaries|The boundaries are discordant and the body is intrusive into the ameta sediments of the Cambro-Ordovician Girilambone Beds and the Fifield Serpentinite.|16-MAY-23
18490|Tout Intrusive Complex|Age reasons|397 +/- 16 m.y. b.p. K-Ar dating Early Devonian.|16-MAY-23
18490|Tout Intrusive Complex|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982|16-MAY-23
18490|Tout Intrusive Complex|Proposed publication|Notes to accompany Narromine 1:250 000 Metallogenic Map.|16-MAY-23
18490|Tout Intrusive Complex|Defn approved by|Copied from xerox sent by NSW Sub-Committee|16-MAY-23
18490|Tout Intrusive Complex|Name first published by|Thomson J., 1975|16-MAY-23
18490|Tout Intrusive Complex|Reserved? Yes/No|J. Stroud|16-MAY-23
72989|Town Beach Diorite|Name source|Town Beach,  Port Macquarie|16-MAY-23
72989|Town Beach Diorite|Type section locality|Town Beach (31o25'47"S 152o55'19"E) where exposure varies according to the amount of surficial sand that mantles the low shore platform.|16-MAY-23
72989|Town Beach Diorite|Description at type locality|Compositionally heterogenous body composed mainly of altered and veined hornblende diorite but including irregular dykes and segregations of gabbro, dolerite, hornblende pegmatite and tonalite aplite.|16-MAY-23
72989|Town Beach Diorite|Extent|A small pluton in the inter-tidal zone at the eastern end of Town Beach, Port Macquarie.|16-MAY-23
72989|Town Beach Diorite|Lithology|...as above...|16-MAY-23
72989|Town Beach Diorite|Relationships and boundaries|Intrusive into the Port Macquarie Serpentinite.|16-MAY-23
72989|Town Beach Diorite|Age reasons|(?) Permian based on geochemical affinity with the 290 ¿ 250 Ma Clarence River Supersuite (Och 2007; Och and Leitch, in prep).|16-MAY-23
72989|Town Beach Diorite|Correlations|A probable correlative of the Tacking Point Gabbro.|16-MAY-23
72989|Town Beach Diorite|References|OCH, D. J. 2007. Eclogite, serpentinite, mélange and mafic intrusive rocks: manifestation of long-lived Palaeozoic convergent margin activity, Port Macquarie, eastern Australia. Unpublished PhD thesis, University of Technology, Sydney.OCH, D. J. and LEITCH, E. C. (in prep) New and revised lithostratigraphic units from the Port Macquarie Block, northeastern New South Wales. Quarterly Notes ¿ Geological Survey of New South Wales.|16-MAY-23
39263|Tranquille Dacite Member|Name source|After the property Tranquille (0250500E 6581100N Gunnedah 1:25,000 sheet) east of Gunnan Ridge.|16-MAY-23
39263|Tranquille Dacite Member|Unit history|Ambrose Dacite Ignimbrite Member (Geeve 1995).|16-MAY-23
39263|Tranquille Dacite Member|Type section locality|Eastern slope of Gunnan Ridge from 30o54'33"S 150o23'48"E to 30o55'41"S 150o23' 36"E (0251200E 6577540N to 0250930E 6575452N Gunnedah 1:25,000 sheet), 1.5 km west-southwest of Ourimperee (part of section 509).|16-MAY-23
39263|Tranquille Dacite Member|Extent|Central eastern and southeastern edges of Gunnan Ridge; southeastern margin of Tulcumba Ridge south from about 3 km north of the junction of Tydd and Mountain Forest Roads, Kelvin State Forest.|16-MAY-23
39263|Tranquille Dacite Member|Thickness range|130 m in the type section, but thinner elsewhere; 20 m in section 523 near the southern end of the Gunnan Ridge; more than 40 m on the southeastern margin of Tulcumba Ridge.|16-MAY-23
39263|Tranquille Dacite Member|Lithology|Grey to brown dacitic ignimbrite with plagioclase, hornblende, biotite, rare quartz, opaque minerals and pumices; groundmass largely chloritic. XRF analyses (Geeve 1995 MU55238, MU55245) indicate a dacitic composition; MU55245 is almost andesitic.|16-MAY-23
39263|Tranquille Dacite Member|Age reasons|?Early Namurian.|16-MAY-23
27303|Transmission Limestone Member|Name source|The name derives from Transmission Flat (GR 762823*) 1.2 km north-east of the type locality.  (*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978)).|16-MAY-23
27303|Transmission Limestone Member|Unit history|Previously an 'upper big shell' unit and an overlying 'lithic' unit were differentiated (Webby 1969). However, it seems preferable to include the 2-3 m thick lithic sandstone, which outcrops very discontinuously throughout the area as the topmost part of the Transmission Limestone Member.|16-MAY-23
27303|Transmission Limestone Member|Type section locality|The type section is taken at the top of the ridge on Dunhill Bluff (GR 753814*) not on the west facing slope of the bluff where the succession is cut by a fault. . [Reference section:] The lithic sandstone is perhaps best exposed at the west side of Davys Creek (GR 744811)(*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978))|16-MAY-23
27303|Transmission Limestone Member|General description|All the beds except the topmost lithic sandstone appear to be exposed in the type section. They are some 21 m thick. The lithic sandstone is perhaps best exposed at the west side of Davys Creek (GR 744811). A 5 m thick sequence of massive  bedded, dark grey lime mudstones, wackestones and fine grainstones define the base of the member. The next 7 m of succession is more thin bedded - with fawn brown skeletal wackestones and including a 3 m thick Eodinobolus shell bank. A 1 m-thick nautiloid-rich bed of skeletal packstone and grainstone forms the base of the next, massively bedded 9 m-thick sequence, the upper part of which is more predominantly lime mudstone and wackestone. The nature of contact with the overlying lithic sandstone is not exposed in the type section, but is elsewhere, for example on west side of Davys Creek. The Transmission Limestone Member has been mapped as an independent and persistent unit throughout the Cliefden Caves area.|16-MAY-23
27303|Transmission Limestone Member|Thickness range|21 m thick in type section.|16-MAY-23
27303|Transmission Limestone Member|Relationships and boundaries|The Transmission Limestone Member represents the topmost of the six constituent members of the Fossil Hill Limestone.|16-MAY-23
27303|Transmission Limestone Member|Proposed publication|Stratigraphy of the Cliefden Caves Limestone Group (Upper Ordovician) central New South Wales. J. geol. Soc. Aust.|16-MAY-23
27303|Transmission Limestone Member|Proposer|Webby B.D., Packham G.H.|16-MAY-23
27303|Transmission Limestone Member|Resdate|12-MAY-1981|16-MAY-23
27303|Transmission Limestone Member|Reserved? Yes/No|Central Register, BMR Canberra (Ref 80/1569)|16-MAY-23
24537|Trilobite Hill Limestone Member|Unit history|The Trilobite Hill Limestone Member was previously known informally as the 'Island' unit (Webby 1969)|16-MAY-23
24537|Trilobite Hill Limestone Member|Type section locality|the unit derives its name from Trilobite Hill (GR 737809*), the type section. (*Canowindra 1:50 000 sheet 8362 I & IV, edit 1 (1978)).|16-MAY-23
24537|Trilobite Hill Limestone Member|Description at type locality|The lower limit of the Trilobite Hill Limestone Member in the type section is defined at the change to more thinly-bedded lime mudstones and skeletal wackestone beds less than 0.1 m thick. Of the 22 m total thickness, the lower 5.5 m comprises grey, thin bedded wackestones and lime mudstones, the middle 10.5 m, fawn brown skeletal wackestones and packstones with shaly interbeds and abundant fossils, and the upper 6 m, well bedded wackestones. The top is defined by the appearance of the massive, grey lime mudstones of the Mount Lewin Limestone Member, in the Trilobite Hill section only 1.5 m thick.|16-MAY-23
24537|Trilobite Hill Limestone Member|General description|The Trilobite Hill Limestone Member has been mapped as an independent unit throughout the Cliefden Caves area and at Licking Hole Creek (Percival 1976).|16-MAY-23
24537|Trilobite Hill Limestone Member|Thickness range|22 m total thickness in type section.|16-MAY-23
24537|Trilobite Hill Limestone Member|Relationships and boundaries|It is the lower of the two constituent members of the Vandon Limestone.|16-MAY-23
24537|Trilobite Hill Limestone Member|Proposed publication|Stratigraphy of Cliefden Caves Limestone Group (Upper Ordovician) central NSW. J. geol. Soc. Aust.|16-MAY-23
24537|Trilobite Hill Limestone Member|Proposer|Webby B.D., Packham G.H.|16-MAY-23
24537|Trilobite Hill Limestone Member|Resdate|12-MAY-1981.  Ref. 80/1589|16-MAY-23
24537|Trilobite Hill Limestone Member|Reserved? Yes/No|Central Register, BMR Canberra|16-MAY-23
24539|Tullamore Intrusive Complex|Name source|Township of Tullamore GR 5605 9645, Narromine 1:250 000 Geological Sheet.|16-MAY-23
24539|Tullamore Intrusive Complex|Type section locality|At GR 5682 9660.|16-MAY-23
24539|Tullamore Intrusive Complex|Extent|7 km east of Tullamore.  Size: Less than 0.5 km in diameter.|16-MAY-23
24539|Tullamore Intrusive Complex|Lithology|Composition:  Pyroxene monzonite.|16-MAY-23
24539|Tullamore Intrusive Complex|Relationships and boundaries|Intrudes the Late Silurian Talingaboolba Formation.|16-MAY-23
24539|Tullamore Intrusive Complex|Age reasons|Early-Middle Devonian became of similarity with Tout Complex.|16-MAY-23
24539|Tullamore Intrusive Complex|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982|16-MAY-23
24539|Tullamore Intrusive Complex|Proposed publication|A metallogenic study of the Narromine 1:250 000 sheet.|16-MAY-23
24539|Tullamore Intrusive Complex|Proposer|Bowman H., Richardson S., Dolanski J.|16-MAY-23
24539|Tullamore Intrusive Complex|Reserved? Yes/No|Yes|16-MAY-23
79334|Tullamullen Coal Member|Name source|Tulla Mullen Creek in northern New South Wales. This creek overlies the parent unit Maules Creek Formation in the Gunnedah Basin. Spelt Tullamullen on all local signs in the area and is the name of the DRE's stratigraphic hole Tullamullen 1.|16-MAY-23
79334|Tullamullen Coal Member|Unit history|Upper Maules Creek seam or Rutley seam used informally in well completion reports submitted to government departments by Force energy, Eastern Star Gas and Santos.|16-MAY-23
79334|Tullamullen Coal Member|Geomorphic expression|Concealed beneath 400-1000m of Permian-Cretaceous cover (Gunnedah and Surat Basins).|16-MAY-23
79334|Tullamullen Coal Member|Type section locality|Coal Seam Gas Exploration Drillhole Dewhurst 11 (Eastern Star Gas). 149.725147°E / 30.50355°S (GDA94) depth (905.80-909.08m).|16-MAY-23
79334|Tullamullen Coal Member|Extent|Restricted to the Pilliga East and Jacks Creek State Forest area south of Narrabri over approximately 700 square kilometres.|16-MAY-23
79334|Tullamullen Coal Member|Thickness range|4.28 m in type section. Range: 1.5 to 4.5m.|16-MAY-23
79334|Tullamullen Coal Member|Lithology|Coal, dull with bright bands. Comprises two splits in type section. Three stone bands of carbonaceous mudstone and sandstone occur within the seam. Generally, occurs as a single seam with a sandstone/mudstone parting 10-30cm thick, 80cm above the base of the seam.|16-MAY-23
79334|Tullamullen Coal Member|Depositional environment|Coal swamp (wet terrestrial to marginal marine).|16-MAY-23
79334|Tullamullen Coal Member|Fossils|Coal.|16-MAY-23
79334|Tullamullen Coal Member|Diastems or hiatuses|Nil.|16-MAY-23
79334|Tullamullen Coal Member|Relationships and boundaries|Above the Coxs Coal Member and below the Mooki Coal Member (if developed) in the Maules Creek Formation.|16-MAY-23
79334|Tullamullen Coal Member|Identifying features|Nil given.|16-MAY-23
79334|Tullamullen Coal Member|Structure and Metamorphism|Dips at <5 degrees, probable early normal faulting is expected to be developed as observed in mining of the Maules Creek Formation in the Maules Creek Sub-basin to the east. Vitrinite reflectance values of between 0.65 and 0.85 RoMax where not heat affected by igneous intrusions.|16-MAY-23
79334|Tullamullen Coal Member|Age reasons|Permian - Cisuralian (Kungurian) part of Gunnedah Basin Bellata Group, contains Glossopteris and Gengamoptris (Cisuralian). Palynological Age of APP33 inferred from samples below this interval and samples of APP41 in samples above this seam in the Porcupine Formation.|16-MAY-23
79334|Tullamullen Coal Member|Correlations|Possible equivalent to the Aberglen Coal Member at Werris Ck, Flemming Coal Member at Muswellbrook Anticline north, Brougham Coal Member at Muswellbrook Anticline south, Onavale seam at Maules Creek Sub-Basin.|16-MAY-23
79334|Tullamullen Coal Member|Alteration and Mineralisation|Coal - Bituminous in rank.|16-MAY-23
79334|Tullamullen Coal Member|Geophysical Expression|Possible seismic reflector, low downhole gamma (<50) and density (<1.50g/cc) geophysical response. Stone band 80cm above floor of seam can be used as a guide to correlate this seam in places.|16-MAY-23
79334|Tullamullen Coal Member|Defn author|Mark Dawson, 10-FEB-2016.|16-MAY-23
18747|Tyagong Serpentinite|Name source|Town of Tyagong 148o15'E 34o5'S.|16-MAY-23
18747|Tyagong Serpentinite|Type section locality|On southern bank of Tyagong Creek 2 km east of its junction with Emu Creek.|16-MAY-23
18747|Tyagong Serpentinite|Extent|In a narrow (0.25 km wide) belt with a northeasterly trend 0.5 km long, 5 km west of Tyagong.|16-MAY-23
18747|Tyagong Serpentinite|Lithology|Serpentinite|16-MAY-23
18747|Tyagong Serpentinite|Relationships and boundaries|Intrusive into Late Ordovician sediments.|16-MAY-23
18747|Tyagong Serpentinite|Age reasons|Early Silurian (?), emplaced into the present position in the Early Devonian (?) by analogy with the Coolac Serpentinite to the south.|16-MAY-23
18747|Tyagong Serpentinite|Defn author|Bowman H.N., 1977|16-MAY-23
18747|Tyagong Serpentinite|Proposed publication|Forbes 1:250 000 Metallogenic Map.|16-MAY-23
18747|Tyagong Serpentinite|Name first published by|Bowman H.N., 1977|16-MAY-23
37916|Tycannah Rhyodacite Member|Name source|After Tycannah Creek  4 km southwest of The Tops road Terry Hie Hie 1:50,000 sheet.|16-MAY-23
37916|Tycannah Rhyodacite Member|Geomorphic expression|Low ridge.|16-MAY-23
37916|Tycannah Rhyodacite Member|Type section locality|Roadside exposures on The Tops road (GR336975 Terry Hie Hie 1:50,000 sheet)|16-MAY-23
37916|Tycannah Rhyodacite Member|Extent|A single exposure extending 5.5 km north-northeast from The Tops Road (GR336975 to 359025 Terry Hie Hie 1:50,000 sheet) adjacent to Cap and Bonnet Mountain.|16-MAY-23
37916|Tycannah Rhyodacite Member|Thickness range|~ 5 m|16-MAY-23
37916|Tycannah Rhyodacite Member|Lithology|An unwelded rhyodacitic ignimbrite containing feldspar, quartz, hornblende, biotite and opaque minerals, fragments of felsic ignimbrites and abundant tube pumices. The groundmass consists largely of broken fragments of pumice which are either zeolitised or remain vitric.|16-MAY-23
37916|Tycannah Rhyodacite Member|Depositional environment|Ignimbrite|16-MAY-23
37916|Tycannah Rhyodacite Member|Age reasons|Carboniferous (?Westphalian)|16-MAY-23
37916|Tycannah Rhyodacite Member|References|Distribution data from Professor P.G. Flood, University of new England, Armidale.|16-MAY-23
18770|Ugalong Dacite|Name source|Ugalong Trig Station.|16-MAY-23
18770|Ugalong Dacite|Type section locality|Burcher-Ungarrie road, 17 km west of Burcher. 510859 (top) to ? westwards.  Forbes 1:250 000.|16-MAY-23
18770|Ugalong Dacite|Extent|About 30 km2, 20 km west of Burcher.|16-MAY-23
18770|Ugalong Dacite|Thickness range|About 5000 m??|16-MAY-23
18770|Ugalong Dacite|Lithology|The Dacite consists of a massive, grey, medium grained, slightly foliated volcanic rock with small quartz and plagioclase phenocrysts in a quartz-feldspar mosaic groundmass.|16-MAY-23
18770|Ugalong Dacite|Relationships and boundaries|The upper contact of the Ugalong Dacite is covered by soil and alluvium to the west. Laterally along strike it is intruded by granite in the south and covered by soil to the north. It is possible that the unit is intrusive.|16-MAY-23
18770|Ugalong Dacite|Age reasons|Lower Devonian, from regional considerations.|16-MAY-23
18770|Ugalong Dacite|Proposed publication|Bulletin Australian Society of Exploration Geophysicists (v.7 No. 1)|16-MAY-23
18976|Urana Formation|Name source|A.P.E. Urana-1 (latitude 35o16'33", longitude 146o00'10").|16-MAY-23
18976|Urana Formation|Type section locality|A.O.G. Jerilderie No. 1, 425 m to 1312 m (latitude 35o15'S, longitude 145o58'E).|16-MAY-23
18976|Urana Formation|Extent|Infrabasins beneath the Murray Basin (Figure 1, O'Brien, in press). Full list of bores intersecting the unit in Brown & Stephenson (in press). Does not crop out.|16-MAY-23
18976|Urana Formation|Thickness range|Maximum penetrated so far 887 m in Jerilderie No. 1. Varies from O m on edges of infrabasins to several metres in the infrabasin axes.|16-MAY-23
18976|Urana Formation|Lithology|Dark grey sandy mudstones with scattered pebbles, dark grey silty diamictites, thin white to grey coarse to fine sandstone beds. Lithofacies interbedded on a scale of a few centimeters to several metres. In the type section, diamictites predominate in the lower half where as mudstone and sandstone predominate in the upper half (O'Brien, 1981 & O'Brien in press, conain lithological logs of petroleum wells that intersect the Urana Formation).|16-MAY-23
18976|Urana Formation|Depositional environment|Glaciomarine.|16-MAY-23
18976|Urana Formation|Fossils|Arenaceous and calcareous foraminifera (Terpstra, 1963; Ludbrook, 1962, 1963, 1967), and unidentified ostracods (Terystra, 1963). Palynomorphs (see Evans, 1962; Morgan, 1975a, b; Morgan, 1976a, b; Morgan, 1977a, b; McLeod, 1977, 1978, 1979; McMinn, 1981; Price, 1976.|16-MAY-23
18976|Urana Formation|Relationships and boundaries|Rests unconformably on metasediments of the Willyama Complex, the Kanmantoo fold belt, Palaeozoic metasediments of the Lachlan fold belt, Mulga Downs and Amphitheatre Groups of the Darling Basin (see Brown & Stephenson, in press) in various parts of the Murray Basin area. The Urana Formation is overlain by the late Permian Coorabin Coal Measures, Triassic Jerilderie Formation, Early Tertiary Renmark Group and unnamed Cretaceous sediments. Each of these units overlies the Urana Formation unconformably in different parts of the Murray Basin area.|16-MAY-23
18976|Urana Formation|Identifying features|Dark grey pebbly and sandy mudstones and diamictites with Permo-Carboniferous microflora.|16-MAY-23
18976|Urana Formation|Structure and Metamorphism|Flat lying.|16-MAY-23
18976|Urana Formation|Age reasons|Contains Stage 2 and Stage 3 microfloras of Kemp & others (1977) and therefore is Late Carboniferous to Early Permian in age.|16-MAY-23
18976|Urana Formation|Correlations|Correlates with other glacial sediments in south-eastern Australia because it has similar lithologies and microfloras (O'Brien, in press). Correlates with Cape Jervis beds of the Troubridge Basin, the Merrimelia Formation in the Cooper Basin and the lower part of the Parmeener Supergroup in Tasmania (O'Brien, in press).|16-MAY-23
18976|Urana Formation|Proposed publication|The Stratigraphy and sedimentology of Late Palaeozoic Glaciomarine sediments beneath the Murray Basin. BMR Journal of Australian Geology & Geophysics, 10(1).|16-MAY-23
18976|Urana Formation|Category|2|16-MAY-23
18976|Urana Formation|Proposer|O'Brien P.E.|16-MAY-23
18976|Urana Formation|State(s)|NSW/SA/VIC|16-MAY-23
27247|Urialla Granite|Name source|Mt Urialla at GR 043606, Michelago 1:100 000 Geological Sheet.|16-MAY-23
27247|Urialla Granite|Type section locality|No type area has been previously defined but the granite is well represented in the vicinity of Urialla Trig. Station where both porphyritic and fine-grained varieties appear.|16-MAY-23
27247|Urialla Granite|Description at type locality|Fine to medium-grained biotite is the main phase developed with coarse porphyritic variaties developed particularly along the western margin. Xenoliths up to 22 cm long are found along the margins of the body in the porphyry and reveal varying stages of absorption by the porphyry. The biotite granite typically contains microcline, quartz, oligoclase and biotite. A minor granodioritic phase contains plagioclase (oligoclase-andesine) quartz, biotite and opaques ranging in grain size between 0.5 and 3 mm, in a dominantly feldspar groundmass. The bulk of the granite appears to have no foliation developed and it is only in the marginal porphyritic phases that a groundmass foliation is developed.|16-MAY-23
27247|Urialla Granite|Extent|The granite lies to the east of Burra Road, extending south from the Queanbeyan River. The mass is elongated meridionally over a distance of some 11 km and lies roughly parallel to the Watch Box Granite to the east.  Size: 17 km2; 2.5 km wide by 11 km long.|16-MAY-23
27247|Urialla Granite|Relationships and boundaries|The southern and northern boundaries are indistinct and the present ground surface would seem to be coincident with the roof of the granite in these parts. Contact metamorphism is evident with sediments raised to the biotite zone on the western contact (a width of 1.5 km) and a metaquartzite developed on the eastern margin. Ordovidian sediments (Foxlow Beds) completely surround the granite, separating it from the Watch Box Granite to the east by a minimum distance of 180 m.|16-MAY-23
27247|Urialla Granite|Proposed publication|Geological Survey of NSW 1:100 0000 Note Series|16-MAY-23
27247|Urialla Granite|Status|1|16-MAY-23
27247|Urialla Granite|Unit name|Urialla Granite (Joplin et al. 1953)|16-MAY-23
26191|Vacy Ignimbrite Member|Name source|Vacy Township (Paterson).|16-MAY-23
26191|Vacy Ignimbrite Member|Unit history|Subdivision of the Gilmore Volcanic Group (Rattigan, 1966).|16-MAY-23
26191|Vacy Ignimbrite Member|Type section locality|North of Martin's Creek. Location of Type Section: Paterson 46309766 railway cutting, under a bridge at the intersection of the North Coast Railway and the Hilldale-Paterson Road.|16-MAY-23
26191|Vacy Ignimbrite Member|Extent|Forms a thin band in the area of Paterson, Vacy, Kealey's Bight, Gresford.|16-MAY-23
26191|Vacy Ignimbrite Member|Thickness range|a) At type section: 12 metres.  B) Maximum known: 16 metres.|16-MAY-23
26191|Vacy Ignimbrite Member|Lithology|Basal reddish, porphyritic, ash-flow tuff of rhyo-dacitic composition overlain by a white, micaceous, porphyritic, ash-flow tuff of dacitic composition.|16-MAY-23
26191|Vacy Ignimbrite Member|Relationships and boundaries|Forms a band up to 490' below the top of the Newtown Formation. Within the Newtown Formation.|16-MAY-23
26191|Vacy Ignimbrite Member|Age reasons|Upper Namurian. Correlations based on Campbell and McKelvey.|16-MAY-23
26191|Vacy Ignimbrite Member|Defn author|Hamilton G., Hall G.C., & Roberts J., 1974|16-MAY-23
26191|Vacy Ignimbrite Member|Proposed publication|Jour. Roy. Soc. NSW|16-MAY-23
26191|Vacy Ignimbrite Member|Defn approved by|From xerox copy sent by NSW Stratigraphic Nomenclature Sub-Committee|16-MAY-23
26191|Vacy Ignimbrite Member|Proposer|Hamilton G., Hall G.|16-MAY-23
26191|Vacy Ignimbrite Member|Reserved? Yes/No|G Hamilton|16-MAY-23
27304|Vandon Limestone|Name source|The name derives from the 'Vandon' property, on which the most complete sections of beds (on the slopes below Malongulli Sugarloaf) are found.|16-MAY-23
27304|Vandon Limestone|Unit history|The informal 'Upper Member' of Webby (1969) was named the Large Flat Limestone Member by Osborne (1978): this latter is now defined as a new formation, the Vandon Limestone. The name 'Large Flat' has been used previously to describe the upper part of the Lower Member of the Cliefden Caves Limestone (see Hill, 1957, p.100), i.e. as revised in the upper part of the Fossil Hill Limestone.|16-MAY-23
27304|Vandon Limestone|Type section locality|The type section was not designated by Osborne (1978). It will be designated in the forthcoming publication as composite, including the section on Trilobite Hill (GR 737809*) for the lower part, and the section on the upper reaches of Copper Mine Creek, 550 m east-south-east of Malongulli Sugarloaf (GR 725797*) for the upper part. (*Canowindra 1:50 000 sheet 8630 I & IV, edit 1 (1978)).|16-MAY-23
27304|Vandon Limestone|Thickness range|In the composite type section a total of 51 m of Vandon Limestone is recognised.|16-MAY-23
27304|Vandon Limestone|Relationships and boundaries|The Vandon Limestone is the upper of the three constituent formations of the Cliefden Caves Limestone Group.|16-MAY-23
27304|Vandon Limestone|Proposed publication|Stratigraphy of the Cliefden Caves Limestone Group (Upper Ordovician) - J. geol. Soc. Aust.|16-MAY-23
27304|Vandon Limestone|Proposer|Webby B.D., Packham G.H.|16-MAY-23
27304|Vandon Limestone|Status|1|16-MAY-23
19281|Wallerawang Subgroup|Name source|Town of Wallerawang, west of Lithgow.|16-MAY-23
19281|Wallerawang Subgroup|Unit history|The term Wallerawang Coal Measures was used by Stephens (1883).|16-MAY-23
19281|Wallerawang Subgroup|Type section locality|(1) Location: Elecom Lithgow-Newnes DDH 31. (221925E, 1310965N Lithgow 1:50 000 Sheet (8931-111))*.  (2) Repository: Elecom core store, Lithgow.  (*Reference Section: Brickworks Quarry, GR 376921, Lithgow 8931-111).|16-MAY-23
19281|Wallerawang Subgroup|Extent|Western Coalfield - Lithgow and Bungleboori 1:50 000 sheets; also parts of Hampton, Katoomba, Glen Davis and Glen Alice sheets.|16-MAY-23
19281|Wallerawang Subgroup|General description|Comprises two formations - Farmers Creek Formation at top and the Gap Sandstone at base.|16-MAY-23
19281|Wallerawang Subgroup|Thickness range|(1) Type section: From 202.23 m to 228.86 m - thickness 26.62 m.  (2) Maximum recorded: 58.5 m.|16-MAY-23
19281|Wallerawang Subgroup|Lithology|Claystone, mudstone, carbonaceous shale, coal, sandstone, siltstone, siliceous claystone, oil shale.|16-MAY-23
19281|Wallerawang Subgroup|Relationships and boundaries|Within and at top of the Illawarra Coal Measures in the Western Coalfield. Overlain with regional unconformity by Caley Formation (Narrabeen Group) sediments. Conformably overlies the Charbon Sub-Group.|16-MAY-23
19281|Wallerawang Subgroup|Proposed publication|Australian Coal Geology|16-MAY-23
19281|Wallerawang Subgroup|References|01/31636|16-MAY-23
26198|Wambidgee Serpentinite|Name source|Wambidgee Railway Station 123 917 (yds) Cootamundra 1:100 000 sheet SI/55-11. 8528.|16-MAY-23
26198|Wambidgee Serpentinite|Type section locality|Due west of Coolac.  Type Section: Due west of Coolac, 137845 (yds) Cootamundra 1:100 000 Sheet.|16-MAY-23
26198|Wambidgee Serpentinite|Extent|Comprises three bodies extending over a distance of 28.6 km between a point 7.5 km east of Brawlin in the north to 2 km west of Sandy Falls in the south (between 135094 and 166779, Cootamundra 1:100 000 Sheet).|16-MAY-23
26198|Wambidgee Serpentinite|Thickness range|(a) At type section: 1.9 km  (b) Maximum known: 1.9 km.|16-MAY-23
26198|Wambidgee Serpentinite|Lithology|Serpentinites (Antigorite Serpentinite, Antigorite-Carbonate Rock, Antigorite-Magnetite-Talc Rock, Opal-bearing Serpentinite).|16-MAY-23
26198|Wambidgee Serpentinite|Relationships and boundaries|Intrusive (cold emplacement) or possibly tectonic (fault) boundary with banded quartzite, amphibolites and volcanics of the Jindalee Beds.|16-MAY-23
26198|Wambidgee Serpentinite|Age reasons|Cambrian to Early Ordovician - Part of the Jindalee Beds which are assigned this age on analogy to Girilambone Beds, Scheibner - Tectonic Map of NSW.|16-MAY-23
26198|Wambidgee Serpentinite|Proposed publication|Geology of the Cootamundra 1:100 000 Sheet (Geological Survey of NSW - in prep.)|16-MAY-23
26198|Wambidgee Serpentinite|Defn approved by|Copied from xerox from NSW Sub-committee.|16-MAY-23
26198|Wambidgee Serpentinite|Name first published by|Clift D.S.L., 1976.|16-MAY-23
37906|Wanganui Andesite Member|Name source|The property `Wanganui' GR495163 Berrioye1:25,000 sheet.|16-MAY-23
37906|Wanganui Andesite Member|Unit history|Wanganui Andesite (Opdyke et al. 2000).  Named informally by Nott (1968).|16-MAY-23
37906|Wanganui Andesite Member|Type section locality|In a tributary of Oaky Creek at GR497192 Berrioye 1:25,000 sheet, 0.5 km south-southwest of `The Pinnacles'.|16-MAY-23
37906|Wanganui Andesite Member|Extent|Rocky Creek Syncline: on the western limb from the southern closure northwards towards the Barraba-Boggabri road, terminating about 2 km southeast of `Kashmir'; on the eastern limb between GR499202 Berrioye 1:25,000 sheet on `The Pinnacles' and Coxs Creek gorge, 3 km to the north. Maules Creek Anticline. In the Maules Creek Anticline the andesite is confined to the region between `Arizona' and a branch of Connors Creek (GR461130 to 456147 Berrioye 1:25,000 sheet).|16-MAY-23
37906|Wanganui Andesite Member|Thickness range|10 m|16-MAY-23
37906|Wanganui Andesite Member|Lithology|Dark grey to black ignimbritic andesite with angular and broken plagioclase, augite, biotite and opaque minerals. Some beds contain fragments of andesite lava. The groundmass is vitric. The basal unit is usually a red unwelded ignimbrite with the same mineralogy.|16-MAY-23
37906|Wanganui Andesite Member|Depositional environment|Ignimbrite|16-MAY-23
37906|Wanganui Andesite Member|Relationships and boundaries|Lowermost ignimbrite within the Clifden Formation|16-MAY-23
37906|Wanganui Andesite Member|Age reasons|Carboniferous (Namurian) The SHRIMP (SL13) age is 319.2 +/- 2.8 Ma (Opdyke et al. 2000).|16-MAY-23
37906|Wanganui Andesite Member|References|NOTT S.A. 1968. The Upper Devonian-Carboniferous sequence at Wean, west of Manilla, New South Wales. BSc (Hons) thesis, University of New England, Armidale (unpubl.).OPDYKE N.D., ROBERTS J., CLAOUE-LONG J., IRVING E. & JONES P.J. 2000. Base of the Kiaman: Its definition and global stratigraphic significance. Geological Society of America Bulletin 112, 1315-1341.|16-MAY-23
19559|Watch Box Granite|Name source|Watch Box Creek which joins the Queanbeyan River at GR 093635, Michelago 1:100 000 sheet area.|16-MAY-23
19559|Watch Box Granite|Unit history|Veevers (1951) was the first to map and describe the granite, calling it the 'Urialla Massive Microcline Granite'. Subsequent authors (Joplin et al., 1953, Best et al., 1964, and Strusz, 1971) referred to the Urialla Granite and the Watch Box Granite under the single name of the Urialla Granite.|16-MAY-23
19559|Watch Box Granite|Type section locality|Immediately south of the Burra-Urialla Road at GR 087611 Michelago 1:100 000 Sheet.|16-MAY-23
19559|Watch Box Granite|Description at type locality|Massive granite, fine to medium-grained hypidiomorphic granular texture. Contains biotite, quartz, microcline and plagioclase with minor apatite and opaques. Marginal microgranites are developed (contain muscovite). No.xenoliths.|16-MAY-23
19559|Watch Box Granite|Extent|East of Burra, intersecting the Burra-Urialla Road, near the northern end of the Michelago Sheet.  Size: 12 km2; average width of 1.2 km.|16-MAY-23
19559|Watch Box Granite|Relationships and boundaries|Surrounded by Late Ordovician Foxlow Beds; along its northern limit the igneous rocks show intimate mixing with the sediments but elsewhere contact metamorphism is barely evident. The northwest granite boundary is faulted.|16-MAY-23
19559|Watch Box Granite|Age reasons|As the granite is of similar composition to other masses in the area, the Watch Box Granite was probably formed at the close of the Silurian Period - early Devonian.|16-MAY-23
19559|Watch Box Granite|Proposed publication|Geological Survey of NSW 1:100 000 Note Series|16-MAY-23
19559|Watch Box Granite|References|79/03619; ?85/24687; ?01/31637|16-MAY-23
37905|West Lynne Rhyodacite Member|Name source|`West Lynne' homestead GR338021 Terry Hie Hie 1:50,000 sheet (McKelvey 1966).|16-MAY-23
37905|West Lynne Rhyodacite Member|Unit history|West Lynne Andesite Tuff (Stroud 1990).West Lynne Rhyodacite (Wang 1999).|16-MAY-23
37905|West Lynne Rhyodacite Member|Geomorphic expression|Low, discontinuous ridge.|16-MAY-23
37905|West Lynne Rhyodacite Member|Type section locality|Quarry on the eastern side of the Gravesend-Terry Hie Hie road, approximately 3 km north of `Yuendoo' (GR3430394 Terry Hie Hie 1:50,000 sheet)).|16-MAY-23
37905|West Lynne Rhyodacite Member|Extent|Discontinuous outcrops are present in three areas on the northwestern limb of Rocky Creek Syncline. Apart from the type locality (below) small outcrops occur 2 km north-northeast of `Brigalow Creek' GR344100, and between GR373216 and 365202 ( all Gravesend 1:50,000 sheet), 5 km southwest of Gravesend (Stroud 1990).|16-MAY-23
37905|West Lynne Rhyodacite Member|Thickness range|3 m (McKelvey 1966).|16-MAY-23
37905|West Lynne Rhyodacite Member|Lithology|A red, unwelded ignimbrite with plagioclase, biotite and fragments of pumice and volcanic rocks. Abundant shards and bubble walls are present in a glassy groundmass.|16-MAY-23
37905|West Lynne Rhyodacite Member|Depositional environment|Ignimbrite.|16-MAY-23
37905|West Lynne Rhyodacite Member|Relationships and boundaries|Overlies the Yuendoo Rhyolite Member and disconformably overlain by the Spion Kop Conglomerate.|16-MAY-23
37905|West Lynne Rhyodacite Member|Age reasons|Carboniferous (Visean).|16-MAY-23
37905|West Lynne Rhyodacite Member|Comments|Geochemical studies by Wang (1999) indicate that this unit is a rhyolite rather than an andesite.|16-MAY-23
37905|West Lynne Rhyodacite Member|References|MCKELVEY B.C. 1966. The stratigraphy and petrology of a Devonian and Carboniferous sequence in northeastern New South Wales. PhD thesis, University of New England, Armidale, NSW, Australia.STROUD J.L. 1990. Gravesend 1: 100,000 Geological Map Series 8938. Geological Survey of New South Wales, Sydney (unpubl.).WANG X. 1999. Carboniferous volcanic rocks of the Rocky Creek region, northern Tamworth Belt, Southern New England Orogen. PhD thesis, University of New South Wales, Sydney (unpubl.).|16-MAY-23
24570|Wheeo Basalt|Name source|Wheeo locality; GR 10507855 Goulburn 1:250 000 Sheet area (SI 55-12).|16-MAY-23
24570|Wheeo Basalt|Unit history|On field criteria, this basalt may have formerly been continuous with the Divide Basalt.|16-MAY-23
24570|Wheeo Basalt|Type section locality|This unit is very poorly exposed and generally very weathered. The type section is a 90 m section in a tributary gully to the Crookwell River, north of "Table Top" homestead from 02259720 (bottom) to 02059695 (top). The top is the sub-aerial upper surface of the basalt and the base is a weathered amygdaloidal grey hackly basalt overlying very weathered gneissic granite and grus.|16-MAY-23
24570|Wheeo Basalt|Extent|The unit occurs continuously from the vicinity of Grabben Gullen through Wheeo to the Crookwell River, in the central part of the Goulburn 1:250 000 sheet.|16-MAY-23
24570|Wheeo Basalt|Thickness range|Up to 110 m.|16-MAY-23
24570|Wheeo Basalt|Lithology|Olivine basalt; columnar in good exposures with colonnade columns overlain by entablature (e.g. 00959750).|16-MAY-23
24570|Wheeo Basalt|Relationships and boundaries|Disconformably overlies granitic rocks of the Palaeozoic Wyangala Batholith or undifferentiated Ordovician phyllites, or conformably overlies sporadically occurring quartzose to mixed quartzose and lithic sub-basaltic sand and gravels which are presumed to be essentially contemporaneous with the basalt. Upper boundary is the sub-aerial top of the basalt.|16-MAY-23
24570|Wheeo Basalt|Age reasons|Miocene on basis of four K-Ar age determinations by ;I. McDougall: range 14.4 to 19.4 m.y. Uncertainties about loss of radiogenic argon due to alteration of the basalt suggest that the true age may be closest to the oldest age determined (19.4 m.y. - I. McDougall, pers. comm.) and hence the basalt is essentially coeval with the Bevendale Basalt.|16-MAY-23
24570|Wheeo Basalt|Proposed publication|J & P Roy. Soc. NSW|16-MAY-23
24570|Wheeo Basalt|Proposer|Bishop P.|16-MAY-23
24570|Wheeo Basalt|Resdate|28-MAR-1984 (Reference 82/86)|16-MAY-23
19873|Whinstone Basalt|Name source|Whinstone trig. Station (1266 m) at GR 178213, Michelago 1:100 000 Geological Sheet|16-MAY-23
19873|Whinstone Basalt|Unit history|Baker (1915) notes that the basalt was locally referred to as the Whinstone Basalt. Joplin et al. (1953) first indicated its position on a map.|16-MAY-23
19873|Whinstone Basalt|Type section locality|[Presumabaly the same as  extent] to the southeast of Jerangle for approximately 7.5 km, from GR 143272 to GR 179210.[Note the Michelago notes, publ 1979, p124 give co-ords as 146274 to 182211].|16-MAY-23
19873|Whinstone Basalt|Description at type locality|Olivine phenocrysts are set in a dark, fine-grained groundmass of plagioclase, olivine, augite and magnetite. The olivine has brownish inclusions of ?spinel.|16-MAY-23
19873|Whinstone Basalt|Extent|It extends southeast of Jerangle for approximately 7.5 km, from GR 143272 to GR 179210. Size: The basalt covers some 7 km2.|16-MAY-23
19873|Whinstone Basalt|Relationships and boundaries|The basalt overlies the Jerangle Igneous Complex.|16-MAY-23
19873|Whinstone Basalt|Age reasons|Tertiary age.|16-MAY-23
19873|Whinstone Basalt|Defn author|Presumed to be Richardson S.J. 1975.|16-MAY-23
19873|Whinstone Basalt|Proposed publication|Geological Survey of NSW 1:100 000 Note Series|16-MAY-23
26212|Whitlow Formation|Name source|The name is derived from Upper Whitlow Road (Gum Flat 9038-11-N 1:25 000 topographic map sheet) where the unit is well exposed.|16-MAY-23
26212|Whitlow Formation|Unit history|Previously mapped as undifferentiated Palaeozoic (Chestnut et al. 1968, 1969).|16-MAY-23
26212|Whitlow Formation|Type section locality|Stratotype: Whitlow Formation is poorly exposed and therefore a type area is nominated. The type area is nominated along Upper Whitlow Road and Ironbark Creek Road from GR 827943 to GR 849964 (Gum Flat 9038-11-N 1:25 000 topographic map sheet).|16-MAY-23
26212|Whitlow Formation|Extent|The unit is well exposed over at least 50 km2 west of Copeton Dam between Gwydir River and Sheep Station Creek.|16-MAY-23
26212|Whitlow Formation|Thickness range|Indeterminate due to faulting and poor exposure.|16-MAY-23
26212|Whitlow Formation|Lithology|Whitlow Formation is dominated by thickly bedded, coarse grained, feldspathic volcarenites. Interbedded siltstone, fine sandstone, minor granule conglomerate, and rare olistostromal beds are subordinate. Oolites are occasionally present as detrital grains in volcarenites and some siltstones and sandstones are tuffaceous.|16-MAY-23
26212|Whitlow Formation|Relationships and boundaries|Both the base and top of Whitlow Formation are not well exposed. The formation is thought to unconformably overlie Cara Formation with the base nominated as the base of the lowermost volcarenites. Whitlow Formation is repeated by impricate thrust faulting and the top of the unit has not been observed.|16-MAY-23
26212|Whitlow Formation|Age reasons|?Early-Middle Carboniferous. Younger than underlying Cara Formation and older than Late Carboniferous Bundarra Suite granitoids which intrude the formation.|16-MAY-23
26212|Whitlow Formation|Proposed publication|Quarterly Notes Geol. Survey NSW|16-MAY-23
26212|Whitlow Formation|Comments|Metamorphism: Prehnite-pumpellyite facies.|16-MAY-23
26212|Whitlow Formation|Reserved? Yes/No|Yes|16-MAY-23
27615|Wilgaroon Granite|Name source|"Wilgaroon" property; GR 367180, Bourke 1:250 000 Sheet area.|16-MAY-23
27615|Wilgaroon Granite|Type section locality|Petrographic descriptions have been made of samples from the southern outcrop area. GR 373163, Cobar 1:250 000 sheet, by Fander, 1972.|16-MAY-23
27615|Wilgaroon Granite|Extent|Three small outcrop areas totalling about 2 km2 west of Yanda Creek in the southwest portion of the Bourke 1:250 000 sheet (SH 55-10) and northwest of the Cobar 1:250 000 sheet (SH 55-14).|16-MAY-23
27615|Wilgaroon Granite|Lithology|Granite, granodiorite; samples described as Porphyritic microgranite, greisenised granodiorite.|16-MAY-23
27615|Wilgaroon Granite|Relationships and boundaries|Intrudes Ballast Beds|16-MAY-23
27615|Wilgaroon Granite|Age reasons|Post Ballast Beds. An ostracode of probable Early Silurian age has been found in the Ballast Beds (Sherwin, 1974). The age is therefore post Early Silurian.|16-MAY-23
27615|Wilgaroon Granite|Proposed publication|Quarterly Notes of the Geological Survey of New South Wales|16-MAY-23
38898|Wilkurra Granite|Name source|Derived from the property name "Wilkurra" and the subsequent drillhole DM Wilkurra DDH1 located on that property. The property is located in the Karpa Kora area, north of Pooncarie and is about 23 km from the new "Wyoming" property residence which is approximately 41 km northeast along the Karpa Kora loop road from the Karpa Kora - Menindee road intersection, 17km north of Pooncarie.|16-MAY-23
38898|Wilkurra Granite|Geomorphic expression|None|16-MAY-23
38898|Wilkurra Granite|Type section locality|Intersected in drillhole DM Wilkurra DDH1. 33o04'25.7"lat, 142o54'29.8" long; GDA94 datum, GRS80 spheroid.|16-MAY-23
38898|Wilkurra Granite|Extent|Unknown (entirely subsurface).|16-MAY-23
38898|Wilkurra Granite|Thickness range|Intersected at 618.2 m in DM Wilkurra DDH1.|16-MAY-23
38898|Wilkurra Granite|Lithology|The granite has been described by Dr L.M. Barron (Barron 2000; Geological Survey of New South Wales Report; GS2000/585) as being a medium to coarse grained unfoliated, high-level, high-temperature, muscovite-biotite-cordierite sodic granite. Minor xenoliths indicate a melt source regime of high temperature ? low pressure metasedimentary granulite terrane (S type granite).|16-MAY-23
38898|Wilkurra Granite|Depositional environment|None.|16-MAY-23
38898|Wilkurra Granite|Relationships and boundaries|Unconformably overlain by Cainozoic Murray Basin sediments (Mid Miocene - Late Oligocene Geera Clay).|16-MAY-23
38898|Wilkurra Granite|Age reasons|Dated by Dr S Wilde (Wilde 2001;  Geological Survey of NSW Report GS2001/207) [SHRIMP U-Pb dating of four "granite" samples from the Wilkurra No.1 and Mossgiel No.1 boreholes, NSW.] Emplacement dates were determined at circa 425 Ma (Mid Silurian).|16-MAY-23
38898|Wilkurra Granite|Correlations| ?Nambucurra Granite and, yet to be formally named, Mossgiel Granite, intersected in a Departmental stratigraphic drillhole drilled between Booligal and Ivanhoe in early 2000.|16-MAY-23
38898|Wilkurra Granite|References|REFERENCES: Moffitt, R. S. 2001. DM Wilkurra DDH1 well completion report. Geological Survey of New South Wales Report GS2001/202 (unpublished). **Barron, L.M. 2000. Granitoids in DM DDH1 Wilkurra. Geological Survey of New South Wales Report GS2000/585 (unpublished). **Wilde, S.A. 2000. SHRIMP U-Pb dating of four ?granite? samples from the Wilkurra No 1 and Mossgiel No 1 boreholes, NSW. Isotope Studies Group, Curtin University of Technology. Perth, Western Australia, Geological Survey of New South Wales, Report GS2001/207 (unpublished).|16-MAY-23
20085|Williamsdale Dacite Member|Name source|Village of Williamsdale, GR 933613, Michelago 1:100 000 sheet.|16-MAY-23
20085|Williamsdale Dacite Member|Unit history|Conforms essentially with the Williamsdale Volcanics (Richardson, 1979) but slightly more restricted in lateral extent.|16-MAY-23
20085|Williamsdale Dacite Member|Type section locality|Along Burra-Williamsdale road Michelago 1:100 000 sheet 8726, from GR007628 (base) to GR958605 (top) excluding coarse porphyry intrusives at GR993620 and GR975603.|16-MAY-23
20085|Williamsdale Dacite Member|Extent|Extends from about 12km south of Queanbeyan (on Canberra 1:100 000 sheet) south to Michelago village.|16-MAY-23
20085|Williamsdale Dacite Member|Thickness range|At least 2000m and possibly as much as 4000m in area of type section.|16-MAY-23
20085|Williamsdale Dacite Member|Lithology|Massive dacitic crystal tuff, pale grey with fresh biotite towards base and darkening upwards; coarse-grained rock fragments up to 130mm long mainly recrystallised pumice containg feldspar aggregates; indistinct primary foliation and lignment of rock fragments in some places.|16-MAY-23
20085|Williamsdale Dacite Member|Relationships and boundaries|Overlies dark grey foliated and sheared dacitic crystal tuff to east; overlain to west by rhyolitic crystal tuff containing small pink K-feldspar-phenocrysts and lacking coarse rock fragments; member of Colinton Volcanics.|16-MAY-23
20085|Williamsdale Dacite Member|Age reasons|Late Silurian from relationship to fossiliferous sediments in Colinton Volcanics and from isotopic age determinations.|16-MAY-23
20085|Williamsdale Dacite Member|Defn author|G.A.M. Henderson ?1989.|16-MAY-23
20085|Williamsdale Dacite Member|Comments|Although this appears to be an adequate unit definition, no evidence is available to show that this definition went through the Stratigraphy Commission approval process. The original card was supplied  to ASUD manager C. Brown by R. S. Abell, on his departure from BMR, after the publication of BMR Bulletin 233 Geology of the Canberra 1:100 000 sheet.|16-MAY-23
20085|Williamsdale Dacite Member|References|G.A.M., 1987. Late Silurian geology of the Michelago-Cooma area: 1:100 000 preliminary edition map. Bur. Miner. Resour. Aust. **Richardson, S.J., 1979. Geology of the Michelago 1:100 000 sheet 8726. Geol. Surv. NSW Sydney.|16-MAY-23
20119|Willow Glen Formation|Name source|Willow Glen' property, GR 764700 6365800, Mudgee 1:100 000 sheet.|16-MAY-23
20119|Willow Glen Formation|Type section locality|600 m of litharenite, limestone, and rhyodacitic tuff between GR 764550 6364000 and GR 765000 63640000.|16-MAY-23
20119|Willow Glen Formation|Extent|The unit outcrops over at least 7 km long and up to 1.5 km wide between the Cudgeogong-Rylstone road and Aarons Pass.|16-MAY-23
20119|Willow Glen Formation|Thickness range|500 to 900 m.|16-MAY-23
20119|Willow Glen Formation|Lithology|Litharenite, grey, coarse-grained, massive; Lower Limestone Bed, grey to white biomicrite, sparsely fossiliferous, minor silty interbeds; Rhyodacitic Tuff, fine-grained, massive, common andy interbeds near top; Upper Limestone Bed, well bedded, fossiliferous, common chert pebbles.|16-MAY-23
20119|Willow Glen Formation|Relationships and boundaries|Conformably overlain by Toolamanang Volcanics (new name).|16-MAY-23
20119|Willow Glen Formation|Age reasons|Fauna in the Upper Limestone Bed dominated by Kirkidium sp. - Silurian.|16-MAY-23
20119|Willow Glen Formation|Proposed publication|Journal and Proceedings of the Royal Society of NSW|16-MAY-23
20119|Willow Glen Formation|Defn Reference|80/21035|16-MAY-23
20119|Willow Glen Formation|Reserved? Yes/No|Yes|16-MAY-23
20121|Willowie Creek beds|Name source|Willowie Creek, GR 4000 5900 Washpool 1:25 000 Topographic Sheet.|16-MAY-23
20121|Willowie Creek beds|Unit history|Fitzroy Series (Kenny, 1936), Fitzroy beds (McElroy, 1962).|16-MAY-23
20121|Willowie Creek beds|Type section locality|Representative Section: An excellent section is exposed along Washpool Creek from GR 3765 5410 to GR 4090 5870 (Washpool).|16-MAY-23
20121|Willowie Creek beds|Extent|The unit covers an area of about 900 km2 in the eastern part of the Grafton 1:250 000 Sheet area (SH 56-6) around the Mann-Clarence rivers junction area.|16-MAY-23
20121|Willowie Creek beds|Thickness range|Structural complication and the massive nature of most lithologies prevent any realistic assessment of true stratigraphic thickness.|16-MAY-23
20121|Willowie Creek beds|Lithology|Tuffaceous mudstones, fine-grained intermediate to mafic igneous rocks and less abundant greywackes, argillites, breccias, conglomerates, jaspers, cherts and deformed gabbroic and dioritic rock types.|16-MAY-23
20121|Willowie Creek beds|Relationships and boundaries|Unconformably overlain by the Mesozoic Clarence-Moreton Basin and intruded by a number of coarse-grained intermediate to silicic plutonic bodies. It is in fault contact with the Baryulgil Serpentinite, part of the Coombadjha Volcanic and Gundahl Complex.|16-MAY-23
20121|Willowie Creek beds|Age reasons|Corals poorly preserved in limestone to the northeast of Jackadgery were considered by Fletcher (in Whiting, 1954) to be Silurian but may be Devonian (Runnegar in Korsch, 1977). The age is probably Siluro-Devonian (see Korsch, 1977; Day et al., 1978).|16-MAY-23
20121|Willowie Creek beds|Proposed publication|Journal of the Geological Society of Australia|16-MAY-23
20121|Willowie Creek beds|References|79/19409; 79/02437; 97/28843 McElroy, C.T. 1962. The geology of the Clarence-Moreton Basin.Geological Survey of New South Wales. Memoir (Geology) 9, 172p. ; 01/31639|16-MAY-23
39257|Willuri Formation|Name source|After the Parish of Willuri (Willuri 1:25,000 sheet).|16-MAY-23
39257|Willuri Formation|Unit history|Clifden Formation, Rocky Creek Conglomerate and Lark Hill Formation White (1965); Rocky Creek Conglomerate, Lark Hill Formation, Currabubula Formation Brown et al. (1990)|16-MAY-23
39257|Willuri Formation|Geomorphic expression|Rugged ridges with cliff lines.|16-MAY-23
39257|Willuri Formation|Type section locality|Section 297 Mihi Creek-Piney Range measured along Mihi Creek from the Plagyan Thrust 30o37'58"S 150o19'50"E (0244153E 6608055N) to an amphitheatre; thence from Haystack Rock to the end of outcrop at 30o39'21"S 150o18'16"E (0241700E 6605429N Willuri 1:25,000 sheet). The upper part of the formation, absent from the type section because of lack of outcrop, is best displayed in section 405 from unnamed ignimbrite Cw7 at 0238934E 6608122N on Bunaleer to the end of outcrop at 0237489E 6608203N (Willuri 1:25,000 sheet) on Lyndhurst (Roberts et al. ms).|16-MAY-23
39257|Willuri Formation|Extent|Carroll-Nandewar block between Carroll and Cenozoic basalts of the southern Nandewar Range; possibly in the Clifton-Carroll block west of the Werrie Syncline.|16-MAY-23
39257|Willuri Formation|Thickness range|1565 m in the type section. Thicker sections adjacent to the type section are 298 Piney Range 1830 m, and 410-436 Bunaleer-Dripping Rock 1780 m; on Tulcumba Ridge 1920 m thick in section 578 Kelvin State Forest-Surrey (Roberts et al. ms). Thinner sections are present adjacent to the southern Nandewar Range and on Gunnan Ridge, the latter being incomplete because of faulting.|16-MAY-23
39257|Willuri Formation|Lithology|Coarse to medium grained, medium to very thickly bedded, rarely cross bedded, pink, beige, brown, orange, green or grey volcanolithic sandstone, and pebbly sandstone; conglomerate containing predominantly volcanic clasts ranging in size from granules to boulders, commonly pebbles to cobbles; thinly bedded, laminated to occasionally contorted grey, brown, beige, red or purple siltstone and tuffaceous siltstone;  fine to coarse purple to pink tuff with angular to rounded volcanic clasts; volcanic breccia; and interbedded ignimbrites, lavas and one, possibly two domes. The range of variation within the volcanic units is outlined in this paper. The composition of the volcanic rocks range from rare andesite through mafic dacite to felsic dacite and rhyolite.|16-MAY-23
39257|Willuri Formation|Depositional environment|Alluvial to fluvial environment on the flanks of or in close proximity to volcanic sources. Conglomerates and conglomeratic sandstones were largely derived from nearby volcanic sources; granitic clasts, presumably derived from the Lachlan Craton to the west, are also present. The conglomerates differ from those in the Werrie region in that they do not appear to infill large palaeovalleys, the erosion of which removed substantial proportions of the pyroclastic flows of that region (McPhie 1983; 1987). No evidence of glaciation was observed in the Willuri Formation in the Carroll-Nandewar block. Analysis of the interbedded and intertonguing packages of volcanics suggest that during an interval of more than 12 Ma in the Namurian to Westphalian there were at least two volcanic centres between the southern Nandewar Range and the region west of the Werrie Syncline.|16-MAY-23
39257|Willuri Formation|Relationships and boundaries|Indeterminable: both the lower and upper parts of the formation are bounded by faults.|16-MAY-23
39257|Willuri Formation|Age reasons|Late Carboniferous (Namurian to Westphalian), with possible extension into the Early Permian. Lavas which disconformably overlie the Carboniferous succession could either be part of the Willuri Formation or the Boggabri Volcanics.|16-MAY-23
39257|Willuri Formation|Correlations|Equivalent to the Currabubula Formation, Rocky Creek Conglomerate, Lark Hill Formation and possibly the upper part of the Clifden Formation in the Darthula block north of the Nandewar Range (Roberts et al. in press). Early Permian rhyodacite and dacite flows which appear to disconformably overlie the Carboniferous succession on Tulcumba Ridge could be partially equivalent to the Boggabri Volcanics.|16-MAY-23
25639|Wirrinya Granite|Name source|Wirrinya GR 583838, Forbves 1:250 000|16-MAY-23
25639|Wirrinya Granite|Unit history|Unnamed previously, this granite is distinct lithologically from other granites in the southern central portion of the Forbes 1:250 000 sheet and thus warrants a separate name.|16-MAY-23
25639|Wirrinya Granite|Type section locality|Outcrops at GR 578830 on hillside.|16-MAY-23
25639|Wirrinya Granite|Extent|Small outcrops over area of 2 km2 1 km west of Pullabooka.|16-MAY-23
25639|Wirrinya Granite|Lithology|Granite (quartz, oligoclase, opaques and biotite in graphic groundmass).|16-MAY-23
25639|Wirrinya Granite|Relationships and boundaries|Intrusive into Early Devonian sediments.|16-MAY-23
25639|Wirrinya Granite|Age reasons|Early Devonian (?) by analogy with the Grenfell Granite.|16-MAY-23
25639|Wirrinya Granite|Defn author|Bowman H.N., 1977|16-MAY-23
25639|Wirrinya Granite|Proposed publication|Forbes 1:250 000 Metallogenic Map|16-MAY-23
25639|Wirrinya Granite|Name first published by|Bowman H.N., 1977|16-MAY-23
25698|Wombiana Formation|Name source|Wombiana railway station(?) GR 2192 8595. Bathurst 1:250 000 Metallogenic Sheet.|16-MAY-23
25698|Wombiana Formation|Type section locality|Limestones and slates of the formation are well exposed in a small quarry north of Blayney of GR 2204 8562 Bathurst 1:250 000.|16-MAY-23
25698|Wombiana Formation|Extent|Extends for about 20 km in a north-northwest direction through Blayney.|16-MAY-23
25698|Wombiana Formation|Thickness range|No upper boundary, but estimated to be around 300 m thick.|16-MAY-23
25698|Wombiana Formation|Lithology|Buff to light-coloured shales, siltstone, limestones and fine-grained sandstones.|16-MAY-23
25698|Wombiana Formation|Relationships and boundaries|The Wombiana Formation overlies the Quigleys Hill Tuff (nov.) in part but the relationship between the two is unknown. The Wombiana Formation may be unconformable or may be fault bounded.|16-MAY-23
25698|Wombiana Formation|Age reasons|It is thought to be of Early Silurian age, but evidence for this is lacking.|16-MAY-23
25698|Wombiana Formation|Proposed publication|Geological Survey of NSW|16-MAY-23
25698|Wombiana Formation|Category|2|16-MAY-23
25698|Wombiana Formation|Proposer|Richardson S., Bowman H.N.|16-MAY-23
25698|Wombiana Formation|Reserved? Yes/No|Yes|16-MAY-23
24582|Wombin Volcanics|Name source|Parish Wombin, County Kennedy|16-MAY-23
24582|Wombin Volcanics|Type section locality|Middle exposed at GR 6043 9228.|16-MAY-23
24582|Wombin Volcanics|Extent|South and central area of Narromine 1:250 000 sheet, extending in a north-south belt from GR 5920 9730 Narromine 1:250 000 towards Parkes.|16-MAY-23
24582|Wombin Volcanics|Thickness range|Maximum thickness 700 m.|16-MAY-23
24582|Wombin Volcanics|Lithology|Dacite, andesite and rhyolite tuffs, lavas and intrusives, sediments and limestones.|16-MAY-23
24582|Wombin Volcanics|Relationships and boundaries|Unconformably overlain by the Early Devonian Trundle Group. Unconformably overlies the Late Ordovician Goonumbla Volcanics.|16-MAY-23
24582|Wombin Volcanics|Age reasons|Late Silurian from stratigraphic evidence.|16-MAY-23
24582|Wombin Volcanics|Defn author|Bowman H.N., Richardson S.J., Dolanski J., 1982.|16-MAY-23
24582|Wombin Volcanics|Proposed publication|A metallogenic study of the Narromine 1:250 000 sheet.|16-MAY-23
24582|Wombin Volcanics|Defn Reference|86/25274|16-MAY-23
24582|Wombin Volcanics|Proposer|Bowman H., Richardson S., Dolanski J.|16-MAY-23
24582|Wombin Volcanics|Reserved? Yes/No|Yes|16-MAY-23
26333|Wongabel Rhyodacite Member|Name source|Wongabel Homestead at GR 443568|16-MAY-23
26333|Wongabel Rhyodacite Member|Type section locality|Bouldery outcrops beside the road at GR 466588.|16-MAY-23
26333|Wongabel Rhyodacite Member|Extent|A belt about 3 km wide trending NNE between Wongabel and Majors Creek and extending north towards Exeter Farm. Another small area crops out near the headwaters of Back Creek.|16-MAY-23
26333|Wongabel Rhyodacite Member|Lithology|A dark blue-green crystal-rich ignimbrite with about 50% phenocrysts of plagioclase An60 to An30 with broad cores of An60-50 quartz, alkali feldspar, pyroxene pseudomorphs, altered biotite allanite and opaques.|16-MAY-23
26333|Wongabel Rhyodacite Member|Age reasons|The Wongabel Rhyodacite Member interdigitates within the Toggannoggra Rhyolite Member of the Long Flat Volcanics and is thus Late Silurian or possibly Early Devonian in age.|16-MAY-23
26333|Wongabel Rhyodacite Member|Defn author|Wyborn D., Owen M., 1986|16-MAY-23
26333|Wongabel Rhyodacite Member|Resdate|21-JUN-1982|16-MAY-23
20516|Woodlawn Volcanics|Name source|"Woodlawn" property, GR 331170, Braidwood 1:100 000 Sheet.|16-MAY-23
20516|Woodlawn Volcanics|Unit history|The Woodlawn Volcanics are shown partly as Ellenden Granite and partly as Mount Fairy Beds on the Canberra 1:250 000 geological sheet (Best et al., 1964).|16-MAY-23
20516|Woodlawn Volcanics|Type section locality|In a creek west of "Woodlawn", between GR 321169 (base) and GR 326168 (top) (Braidwood 1:100 000 Sheet) where 600 m of section, mainly lithic tuffs, are exposed.|16-MAY-23
20516|Woodlawn Volcanics|Extent|The unit crops out over about 10 km2 in the vicinity of "Woodlawn", with sporadic occurrences further south as far as the Queanbeyan-Braidwood road. As defined here, the unit is restricted to the Lake Bathurst 1:50 000 Sheet.|16-MAY-23
20516|Woodlawn Volcanics|Thickness range|Variable; estimatead maximum 1000 m.|16-MAY-23
20516|Woodlawn Volcanics|Lithology|Lithic tuff, acid flows, ignimbrite, agglomerate, chert and minor sediments.|16-MAY-23
20516|Woodlawn Volcanics|Relationships and boundaries|The Woodlawn Volcanics interfinger with and overlie the De Drack Formation and interfinger with and are overlain by the Currawang Basalt. The unit is disconformably overlain by the Covan Creek Formation.|16-MAY-23
20516|Woodlawn Volcanics|Age reasons|On structural and stratigraphic grounds the Woodlawn Volcanics are Late Silurian.|16-MAY-23
20516|Woodlawn Volcanics|Proposed publication|Felton E.A., Huleatt M.B., 1975. Geology of the Braidwood 1:100 0000 Sheet. Geol. Surv. NSW, Sydney|16-MAY-23
31412|Woodton Formation|Name source|Woodton Homestead 833883 (Quirindi A-D 1:31 680 topographic sheet).|16-MAY-23
31412|Woodton Formation|Unit history|Currabubula Formation, in part.|16-MAY-23
31412|Woodton Formation|Type section locality|Eastern Limb of the Temi Syncline, Willow Tree, NSW.  Location of Type Section: Along Sheep Station Creek 828896 to 827903 (Quirindi A-D 1:31 680 topographic sheets).|16-MAY-23
31412|Woodton Formation|Extent|Exposed in Temi Syncline and Back Creek Anticline.|16-MAY-23
31412|Woodton Formation|Thickness range|a) At type section:  819 ft  b) Maximum known: 819 ft.|16-MAY-23
31412|Woodton Formation|Lithology|Poorly sorted feldspathic and lithic sandstones and minor conglomerates high in the formation, also near the top of the formation are lensoidal sheets of finely laminataed sands, silts and volcanic ashes.|16-MAY-23
31412|Woodton Formation|Relationships and boundaries|The Woodton Formation is conformably overlain by the Chilcotts Mudstone and conformably overlies the Rockford Formation.|16-MAY-23
31412|Woodton Formation|Age reasons|Late Carboniferous - due to stratigraphic position.|16-MAY-23
31412|Woodton Formation|Proposed publication|J. Proc. R. Soc. NSW|16-MAY-23
31412|Woodton Formation|Category|2|16-MAY-23
31412|Woodton Formation|Defn approved by|Copied from xerox sent by NSW Stratigraphic Nomenclature Sub-Committee.|16-MAY-23
31412|Woodton Formation|Reserved? Yes/No|S.P. Lowe|16-MAY-23
27097|Woolomin Group|Name source|The name is derived from Woolomin township (Woolomin 1:25 000 topographic mapsheet 9135-111-N GR 238351).|16-MAY-23
27097|Woolomin Group|Unit history|Woolomin Series, Benson 1911; Woolomin Group, Spry 1953, Voisey 1959; Woolomin Beds, Crook 1961. Revision: Woolomin Beds (Crook 1961) are herein revised to Woolomin Group. Detailed mapping of the Woolomin beds has allowed the recognition of two constituent formations and it is therefore appropriate (ASNC notes 9 & 10, article 3H, Staines 1985) that this unit be formalised and assigned group status. Detailed mapping also allows for recognition of the previously undetermined eastern limit of the Woolomin Group where it is in thrust fault contact with Cara Formation (Blake and Murchey fig. 3, this issue).|16-MAY-23
27097|Woolomin Group|Constituents|Nangahrah Formation, Bobs Creek Formation, undifferentiated in other areas.|16-MAY-23
27097|Woolomin Group|Type section locality|Nundle to Woolomin road near Anderson Flat south of Tamworth (Crook 1961, Woolomin Beds). Reference areas are proposed along the Barraba to Bundarra road (Cobbadah 1:100 000 topographic map sheet 9037 GR 833360 to GR 880500) and in the type areas of the constituent formations.|16-MAY-23
27097|Woolomin Group|Extent|Outcrops in an elongate belt approximately 10 km wide and 300 km long immediately east of the Peel Fault System.|16-MAY-23
27097|Woolomin Group|Thickness range|Indeterminate due to deformation and poor exposure.|16-MAY-23
27097|Woolomin Group|Relationships and boundaries|Base and top of the group are both faulted; base is a thrust fault contact where Woolomin Group is thrust over Cara Formation; Woolomin Group in turn overthrust by Woodsreef Ophiolitic Melange.|16-MAY-23
27097|Woolomin Group|Age reasons|Radiolarian faunas indicate a ?Middle Devonian to Early Carboniferous age.|16-MAY-23
27097|Woolomin Group|Proposed publication|Quarterly Notes Geological Survey NSW|16-MAY-23
27097|Woolomin Group|Comments|Discussion: Benson (1911, 1913) introduced the term Woolomin Series to apply to "jaspers, altered spilitic rocks, schistose tuffs, slates, phyllites and hornstones" which crop out east of the Peel Fault. Notably he did not set an eastern limit to the series. Spry (1953), following recommendations of the then current code of stratigraphic nomenclature (Raggatt 1950) assigned the lithological term Group. Voisey (1959) subsequently used the name Woolomin Group for these rocks in the Manilla District. Crook (1961) revised the name to Woolomin Beds applying it to the rocks mapped as Woolomin Series by Benson (1911, 1913, 1914 and others) as far east as Bundarra Suite granitoids but did not feel that the name was appropriate further east (eg., Spry 1953) until stratigraphic continuity could be demonstrated. Leitch and Cawood (1980) subdivided Woolomin Group into two undefined units. They subdivided Woolomin Beds (sensu Crook 1961) introducing, but not defining Wisemans Arm Formation, as a new unit and applying the name Woolomin to an undefined but restricted formation. In a similar manner Cawood (1982) introduces, without definition, Cockburn Formation and, again without definition, uses the name Woolomin Formation for a more restricted formation. These new applications of the name Woolomin are clearly inappropriate for two reasons: the usage is undefined and ISSC (Hedberg 1976) and ASNC (Staines 1985) clearly state that "when a unit is divided into two or more units, the original name should not be employed for any of the subdivisions".  Metamorphism: Prehnite-pumpellyite facies.|16-MAY-23
20575|Woolooma Formation|Name source|Derived from Woolooma Gully, between 155368 and 131293, Woolooma 1:63 360 Sheet.|16-MAY-23
20575|Woolooma Formation|Type section locality|Back Creek-Upper Rouchel.  Location of Type Section: Measured westwards along Back Creek from 143293 to 117287, Woolooma 1:63 360 Sheet.|16-MAY-23
20575|Woolooma Formation|Extent|Outcrops over an area of aboaut 200 km2 between the village of Rouchel Brook and the Mt Royal Range.|16-MAY-23
20575|Woolooma Formation|Thickness range|a) At type section: 567 m.  B) Maximum known: 1100 m. Composite thickness from the Malumla-Scrumlo area.|16-MAY-23
20575|Woolooma Formation|Lithology|Blue-grey siltstone, brown mudstone, both of which are thinly bedded, thickly bedded green lithic sandstone and minor limestone.|16-MAY-23
20575|Woolooma Formation|Fossils|Brachiopods, corals, polyzoans, ammonoids, foraminifers, conodonts, algae.|16-MAY-23
20575|Woolooma Formation|Relationships and boundaries|In the eastern part of the Rouchel district the Woolooma Formation overlies the Waverley Formation. In the west it intertongues with the non-marine Isismurra Formation. The Woolooma Formation is overlain by the upper part of the Isismurra Formation. In the type section the base of the formation is taken at a transition from coarse-grained zeolitic lithic sandstone (Isismurra Formation) to fine grained lithic sandstone and fossiliferous siltstone. In the east, the boundary is taken at the transition from massive coarse-grained lithic sandstone (Waverley Formation) to thinly bedded sandstone, calcarenite and siltstone. The upper boundary is marked by a change to massive pink zeolitic sandstone and ignimbrites of the Isismurra Formation.|16-MAY-23
20575|Woolooma Formation|Age reasons|Lower Carboniferous (Visean). Contains brachiopods of the Orthotetes australis and lower part of the Delepinea aspinosa Zones.|16-MAY-23
20575|Woolooma Formation|Defn author|Roberts J., Oversby B.S., 1974.|16-MAY-23
20575|Woolooma Formation|Proposed publication|BMR Bulletin|16-MAY-23
20575|Woolooma Formation|Defn approved by|Approved. Copied from xerox sent by NSW Stratigraphic Nomenclature Sub-Committee.|16-MAY-23
20575|Woolooma Formation|Proposer|Roberts J., Oversby B.S.|16-MAY-23
20575|Woolooma Formation|Reserved? Yes/No|J Roberts|16-MAY-23
20693|Wyanbene Limestone Member|Name source|Probably after Wyanbene Cave, which is developed within the limestone lense.|16-MAY-23
20693|Wyanbene Limestone Member|Unit history|The name Wyanbene Limestone was introduced by Best et al. (1964, Canberra 1:250 000 Geological Map, 2nd edition). No formal definition has been published. Our mapping on the Araluen 1:100 000 sheet has demonstrated that it is best regarded as a limestone lens developed in the De Drack Formation (defined on the Braidwood sheet), and is of member status. A formal definition is given for the first time.|16-MAY-23
20693|Wyanbene Limestone Member|Type section locality|On a ridge between the headwaters of Curmulee Creek and Wyanbene Creek, from GR 428398 to 425346, Araluen sheet.|16-MAY-23
20693|Wyanbene Limestone Member|Extent|About 2 km2 in the headwaters of Wyanbene Creek.|16-MAY-23
20693|Wyanbene Limestone Member|Thickness range|Uncertain but not less than 150 m.|16-MAY-23
20693|Wyanbene Limestone Member|Lithology|Massive recrystallised sporite to biosporite, small areas of micrite, bedding not obvious.|16-MAY-23
20693|Wyanbene Limestone Member|Relationships and boundaries|A limestone lens surrounded by sediments of De Drack Formation. Also overlain unconformably by Late Devonian sediments.|16-MAY-23
20693|Wyanbene Limestone Member|Age reasons|Conodonts indicate a Late Silurian age.|16-MAY-23
20693|Wyanbene Limestone Member|Defn author|Wyborn D., Owen M., 1986|16-MAY-23
24589|Wylora Quartz Gabbro|Name source|'Wylora' property; GR 696406, Bungonia 1:25 000 Topographic Sheet (8828-II-N).|16-MAY-23
24589|Wylora Quartz Gabbro|Unit history|Synonymous in part with the Bungonia Granite (Garretty, 1937).|16-MAY-23
24589|Wylora Quartz Gabbro|Type section locality|1 km S of 'Wylora' homestead, GR 695394 - Bungonia 1:25 000 Topographic Sheet (8828-II-N).|16-MAY-23
24589|Wylora Quartz Gabbro|Extent|The unit extends over 2.5 km2 as a 0.2-0.75 km wide N-S belt through Bungonia.|16-MAY-23
24589|Wylora Quartz Gabbro|Lithology|Quartz gabbro.|16-MAY-23
24589|Wylora Quartz Gabbro|Relationships and boundaries|A pluton of the Marulan Batholith (Naylor, 1939). It intrudes the Tangerang volcanics and the Springponds Granodiorite and is intruded by the Lumley Adamellite. It is overlain in part by Tertiary surficial deposits.|16-MAY-23
24589|Wylora Quartz Gabbro|Age reasons|395 +/- 8 m.y., K-Ar age determination on a biotite separate (Carr, Jones and Wright, 1980).|16-MAY-23
24589|Wylora Quartz Gabbro|Proposed publication|Proceedings of the Linnean Society of New South Wales|16-MAY-23
24589|Wylora Quartz Gabbro|Proposer|Carr P.F., Jones B.G., Kantsler A.J., Moore P.S., Cook A.C.|16-MAY-23
26334|Wyoming Limestone Member|Name source|The name derives from the property of Wyoming (GR 774770*).  (*Canowindra 1:50 000 Sheet 8630 I & IV, edit 1 (1978)).|16-MAY-23
26334|Wyoming Limestone Member|Unit history|Previously known as the 'brachiopod' unit (Webby 1969).|16-MAY-23
26334|Wyoming Limestone Member|Type section locality|Type section on Fossil Hill (GR 751812*) (*Canowindra 1:50 000 Sheet 8630 I & IV, edit 1 (1978)).|16-MAY-23
26334|Wyoming Limestone Member|Description at type locality|The type section on Fossil Hill is well exposed and uncomplicated except for an interval between 5 and 6 m above the base which is intersected by small faults. No large repetition or loss of beds is however apparent. The base is defined at a marked lithological change - grey brown skeletal wackestones with abundant corals assigned to the top of Kalimna Limestone Member and succeeding greenish brown, volcaniclastic fine sandstones to the basal Wyoming Limestone Member. The Wyoming Limestone Member is characterised by its several volcaniclastic influxes and a rich and varied brachiopod fauna. The lithologies of the member include skeletal wackestones, packstones and volcaniclastic, calcareous sandstones. The upper part of the sequence in the type section includes a prominent 4 m thick Eodinobolus shell bank. The transition into the overlying Taplow Limestone Member - into more massively-bedded, grey, skeletal packstones and grainstones with colonies of Tetradium cribriforme - is relatively sharp.|16-MAY-23
26334|Wyoming Limestone Member|General description|The Wyoming Limestone Member has been mapped as an independent unit throughout the Cliefden Caves area.|16-MAY-23
26334|Wyoming Limestone Member|Thickness range|27 m thick in type section.|16-MAY-23
26334|Wyoming Limestone Member|Relationships and boundaries|Wyoming Limestone Member is part of the Fossil Hill Limestone.|16-MAY-23
26334|Wyoming Limestone Member|Proposed publication|Stratigraphy of Cliefden Caves Limestone Group (Upper Ordovician) central NSW. J. geol. Soc. Aust.|16-MAY-23
26334|Wyoming Limestone Member|Proposer|Webby B.D., Packham G.H.|16-MAY-23
26334|Wyoming Limestone Member|Resdate|12-MAY-1981|16-MAY-23
26334|Wyoming Limestone Member|Reserved? Yes/No|Central Register, BMR Canberra (Ref. 80/1569)|16-MAY-23
20864|Yarrabandai Formation|Name source|After the village of Yarrabandai, Forbes 1:250 000 GR 561 904.|16-MAY-23
20864|Yarrabandai Formation|Type section locality|Low hill on north east outskirts of Yarrabandai, Forbes 1:250 000 GR 562905.|16-MAY-23
20864|Yarrabandai Formation|Extent|Scattered outcrops between Yarrabandai and Bogan Hill (Forbes 1:250 000 GR 580914, and north west of Trundle between Watts Dan (Narromine 1:250 000 GR 5665 9415) and Kadungle (do., GR 566 949).|16-MAY-23
20864|Yarrabandai Formation|Thickness range|About 700 m.|16-MAY-23
20864|Yarrabandai Formation|Lithology|White to off-white iron stained medium-grained quartzose sandstone, well bedded and producing very flaggy outcrops.|16-MAY-23
20864|Yarrabandai Formation|Relationships and boundaries|Overlies the Byong Volcanics, or the Cookeys Plains Formation near Kadungle. Overlain by a fine conglomerate between Trundle and Bogan Gate, and by rhyolitic volcanics near Kadungle.|16-MAY-23
20864|Yarrabandai Formation|Age reasons|Early Devonian faunas dominated by brachiopods - Howellella sp., Nannothyris sp., ?Areostrophia sp., tentaculitids, and lamellibranchs - ?Goniophora sp.|16-MAY-23
20864|Yarrabandai Formation|Proposed publication|Quarterly Notes Geological Survey, NSW|16-MAY-23
20864|Yarrabandai Formation|Reserved? Yes/No|Yes|16-MAY-23
39264|Yarralumba Ignimbrite Member|Name source|From a property of the same name southwest of Gunnan Ridge (0249700E 6571520N Gunnedah 1:25,000 sheet).|16-MAY-23
39264|Yarralumba Ignimbrite Member|Unit history|Iventure Ignimbrite Member (Geeve 1995).|16-MAY-23
39264|Yarralumba Ignimbrite Member|Type section locality|Type section from 30o51'44"S 150o21'30"E to 30o51'50"S 150o21'23"E (0247417E 6582653N to 0247231E 6582489N Gunnedah 1:25,000 sheet) in section 510 on Gunnan Ridge, 1 km west of Glen Allyn (0248300E 6582660N).|16-MAY-23
39264|Yarralumba Ignimbrite Member|Extent|Gunnan Ridge: along eastern margin, extensive outcrops at closure of folds north of narrowest part of ridge south of Gunnan Trig. Tulcumba Ridge: from about 3 km north of the junction of Tydd and Mountain Forest Roads, Kelvin State Forest, to southeastern flank.|16-MAY-23
39264|Yarralumba Ignimbrite Member|Thickness range|>135 m in the type section, but base unexposed; elsewhere on Gunnan ridge between 100 and 175 m (sections 519 and 509); 30-110 m (sections 521 and 576) on Tulcumba Ridge. Section number are those of Roberts et al. ms).|16-MAY-23
39264|Yarralumba Ignimbrite Member|Lithology|Pink, red or purple, unwelded to welded ignimbrite with coarse grained quartz, plagioclase, K-feldspar, opaque minerals and pumice fragments; shards generally slender, moderately stratified, some thick and wavey; groundmass micropoikilitic, spherulitic or chloritic/zeolitic. Ash-rich parts of the unit contain scatted crystals of the above minerals in a fine, shard-rich matrix. Lapillae tuffs well developed on a number of horizons; a good example is exposed at 0248840E 6580263N (Gunnedah 1:25,000 sheet) near the base of section 519. XRF analyses (Geeve 1995 MU55246, MU55260, MU55263, MU55264, MU55240, MU55241) indicate a rhyolitic to rhyodacitic composition.|16-MAY-23
39264|Yarralumba Ignimbrite Member|Age reasons|Namurian.|16-MAY-23
40760|Yarrari Pyroclastic Member|Name source|From the property Yarrari, formerly Highview (0240600E 6594520N Kelvin 1:25 000 sheet).|16-MAY-23
40760|Yarrari Pyroclastic Member|Unit history|Unit F of Liang (1989).|16-MAY-23
40760|Yarrari Pyroclastic Member|Type section locality|Locality 403-1 at 30045?14?S,150018?12?E (0241863E 6594567N Kelvin 1:25 000 sheet) at the western margin of Tulcumba Ridge 1.2 km east-northeast of Yarrarai.|16-MAY-23
40760|Yarrari Pyroclastic Member|Extent|Extends along the western edge of the mid-part of Tulcumba Ridge. Discontinuous exposures at the western margins of outcrop between Lyndhurst and Bollol Creek (Figure 3).|16-MAY-23
40760|Yarrari Pyroclastic Member|Thickness range|50 m at the type locality. Varies between 20 m in section 578 (Figure 6), south of the type locality, to 60 m near the top of section 410 (Figure 5) south of Bunaleer.|16-MAY-23
40760|Yarrari Pyroclastic Member|Lithology|The basal unit is a coarse, red, crystal-rich pyroclastic with phenocrysts of quartz, plagioclase, K-feldspar, and biotite as well as rounded pebbles of ignimbrite, rhyolite lava, common pumice fragments, coarse shards and bubbles. The groundmass is glassy, chloritic or pumiceous. This portion of the member may be resedimented. The upper unit is a coarse, grey to beige, crystal-rich, pyroclastic, containing the same mineral constituents, smaller pumice fragments and ignimbrite and ferruginised perlite pebbles; the groundmass is shard-rich and spherulitic to micropoikilitic. XRF analyses by Liang (1989 MU47002) and from samples 492-5 and 492-6 (Table 2 Appendix 3) indicate a dacitic composition|16-MAY-23
40760|Yarrari Pyroclastic Member|Age reasons|Zircons from sample 403-1 (Figure 11b) dated by SHRIMP (AS3) group into two ages; 14 grains give an age of 306.8?3.7 Ma and 11 grains an age of 294.0?3.9 Ma. The older age is preferred because of radiogenic Pb loss. In sample 429-1 (Figure 11a) the probability density plot for the 30 analyses of zircons is not a simple bell shaped curve but appears to be formed by two closely spaced age peaks. The overall weighted mean 206Pb/238U age for 29 of the 30 analyses has an MSWD factor of 2.0, giving 307.8 ? 3.7 Ma. However, using the mixture modelling routine of Sambridge and Compston (as available in the ISOPLOT Excel Macro; Ludwig 2003), there appears to be a more dominant peak or grouping at 312.5 ? 3.6 Ma (17 analyses) and a younger subordinate group at 301.6 ? 3.7 Ma. The slightly older group may reflect a primary magmatic age, whilst the younger group may result from small amounts of radiogenic Pb loss. Since ignimbrite bed b of the Carramundra Member (309.6?4.3 Ma) underlies the Yarrarai Ignimbrite Member in the region adjacent to Bunaleer, the mean age of 307.8?3.7 Ma for sample 429-6 (Figure 11a) is preferred to that derived by mixture modelling. The age of both dated samples is taken as Late Westphalian.|16-MAY-23
38118|Yegi Conglomerate|Name source|From Yegi trigonometric station.|16-MAY-23
38118|Yegi Conglomerate|Geomorphic expression|Forms low ridges.|16-MAY-23
38118|Yegi Conglomerate|Type section locality|Pits 50m east of intersection of Blackers Lane and Thomas Lane, 8km northeast of of Naradhan, NSW.  Also, Yegi trigonometric station.|16-MAY-23
38118|Yegi Conglomerate|Description at type locality|Pebbly lithic quartz sandstone and polymictic cobble conglomerate exposed in scrapings.|16-MAY-23
38118|Yegi Conglomerate|Extent|Extends 10km SE from Begargo Hill towards the parish of Hannan.|16-MAY-23
38118|Yegi Conglomerate|Thickness range| 400m - estimate based on geomorphic expression.|16-MAY-23
38118|Yegi Conglomerate|Lithology|Pebbly lithic quartz sandstone and matrix-supported polymictic cobble conglomerate with dominant quartzite cobbles, minor white vein quartz pebbles.|16-MAY-23
38118|Yegi Conglomerate|Depositional environment|Alluvial fan/braid plain.|16-MAY-23
38118|Yegi Conglomerate|Relationships and boundaries|Not exposed.|16-MAY-23
38118|Yegi Conglomerate|Age reasons|Apparently conformably underlies Devonian Ural Volcanics.|16-MAY-23
38118|Yegi Conglomerate|Correlations|Square Head Formation?|16-MAY-23
38118|Yegi Conglomerate|Proposed publication|Explanatory Notes - Cargelligo 1:250 00 geological map.|16-MAY-23
38118|Yegi Conglomerate|References|Rankin Springs 1:100 000 geology map (in prep. 2003) by Cameron et al.|16-MAY-23
26246|Yeo Yeo Rhyodacite Member|Name source|Yeo Yeo Railway Station (GR 5967 7379 Cootamundra 1:250 000).|16-MAY-23
26246|Yeo Yeo Rhyodacite Member|Type section locality|GR 5990 7251 to GR 5980 7251, Cootamundra 1:250 000 Sheet.|16-MAY-23
26246|Yeo Yeo Rhyodacite Member|Extent|The unit extends from about 4 km west of Cootamundra to north of Yeo Yeo Railway Station.|16-MAY-23
26246|Yeo Yeo Rhyodacite Member|Thickness range|1000 m(?)|16-MAY-23
26246|Yeo Yeo Rhyodacite Member|Lithology|Rhyodacite ash flow with distinctive pink potash feldspar content; rare sediment lenses.|16-MAY-23
26246|Yeo Yeo Rhyodacite Member|Relationships and boundaries|Occurs within and either near or at the base of the Frampton Volcanics. Base obscured by unconformably overlying Cootamundra Group and Hervey Group.|16-MAY-23
26246|Yeo Yeo Rhyodacite Member|Age reasons|The age of the Frampton Volcanics is thought to be Middle to Late Silurian based on structural evidence only.|16-MAY-23
26246|Yeo Yeo Rhyodacite Member|Proposed publication|A Metallogenic study of the Cootamundra 1:250 000 sheet.|16-MAY-23
26246|Yeo Yeo Rhyodacite Member|First Reference|79/20317|16-MAY-23
26246|Yeo Yeo Rhyodacite Member|Name first published by|Basden H., Adrian J., Clift D.S.l., Winchester R.E., 1978|16-MAY-23
37904|Yuendoo Rhyolite Member|Name source|After `Yuendoo' homestead GR343039 Terry Hie Hie 1:50,000 sheet.|16-MAY-23
37904|Yuendoo Rhyolite Member|Unit history|Yuendoo Andesite Tuff (McKelvey 1968).Yuendoo Andesite Tuff (Chesnut et al.1971).|16-MAY-23
37904|Yuendoo Rhyolite Member|Geomorphic expression|Low ridge|16-MAY-23
37904|Yuendoo Rhyolite Member|Type section locality|1 km south of `Yuendoo' homestead (GR343039 Terry Hie Hie) 1:50,000 sheet).|16-MAY-23
37904|Yuendoo Rhyolite Member|Extent|Northwestern limb and area of northern closure of the Rocky Creek Syncline. Crops out over a distance of 12 km between a northwesterly fault (GR347115 Gravesend 1:50,000 sheet), and 1.5 km south-southwest of `West Lynne' (GR334008 Terry Hie Hie 1:50,000 sheet). In the area of closure of the syncline north-northeast of Slaughterhouse Pinnacle ( GR 390072) it crops out on either side of Lowes Creek and in a low ridge south-southwest of `Malvern' (GR380145 Gravesend 1:50,000 sheet; Stroud 1990).|16-MAY-23
37904|Yuendoo Rhyolite Member|Thickness range|Up to 20m.|16-MAY-23
37904|Yuendoo Rhyolite Member|Lithology|Pale grey, poorly to non-welded ignimbrite containing feldspar, and fine chloritised and ferruginised volcanic rock and pumice fragments.|16-MAY-23
37904|Yuendoo Rhyolite Member|Depositional environment|Ignimbrite.|16-MAY-23
37904|Yuendoo Rhyolite Member|Relationships and boundaries|Underlies the West Lynne Rhyodacite Member on northwestern limb of Rocky Creek Syncline.|16-MAY-23
37904|Yuendoo Rhyolite Member|Age reasons|Carboniferous (Visean).|16-MAY-23
37904|Yuendoo Rhyolite Member|Comments|Geochemical studies by Wang (1999) indicate that this unit is a rhyolite rather than an andesite.|16-MAY-23
37904|Yuendoo Rhyolite Member|References|CHESNUT W.S. 1971. Inverell 1:250,000 Geological Series Sheet SH 56-5. Geological Survey of NSW, Sydney.MCKELVEY B.C. 1968. Geological Map of New England 1:100,000, Bangheet Sheet (No. 280) with marginal text. The University of New England, Armidale, NSW, Australia.WANG X. 1999. Carboniferous volcanic rocks of the Rocky Creek region, northern Tamworth Belt, Southern New England Orogen. PhD thesis, University of New South Wales, Sydney (unpubl.).|16-MAY-23
