Stratno | Stratigraphic Name | Category | Contents | Last update 
27074|Aldinga Member|Unit history|Aldinga Limestone, Crespin, 1954, p.9-10, excluding those beds at and above the first appearance of chert nodules.  "Aldingan Unit" Lindsay, 1970, p.7.|16-MAY-23
27074|Aldinga Member|Type section locality|Coastal cliffs along Aldinga Bay from Chinaman Gully, south across mouth of Aldinga Ck to near old jetty, specifically between 119-66 and 136-66 inclusive of Lindsay, 1967 (Figs 1 & 2).|16-MAY-23
27074|Aldinga Member|Extent|From subsurface data, the unit occurs in the Willunga Embayment, west of McLaren Vale. It also occurs in other regions of the St Vincent Basin - in the Noarlunga Embayment and in the subsurface of the Adelaide Plains.|16-MAY-23
27074|Aldinga Member|Thickness range|Range 0-20 m|16-MAY-23
27074|Aldinga Member|Lithology|The unit consists of variable shelly and bryozoal clays, silts and sands, and limestones, which are fawn, yellow-brown and grey in colour. Quartz is the predominant detrital mineral although carbonate in the form of bioclastic material is also an important constituent.|16-MAY-23
27074|Aldinga Member|Relationships and boundaries|The unit can be readily distinguished from the underlying Chinaman Gully Formation by its carbonate content. The top of the Aldinga Member is clearly defined in outcrop sections by the first appearance of chert nodules characteristic of the Ruwarung Member.|16-MAY-23
27074|Aldinga Member|Age reasons|Latest Eocene in age after Lindsay (1969). Lindsay studied the foraminifera and recognised two zones within the type section, the top Eocene (Subbotina linaperta Zone) and the top part of the underlying Turborotalia aculeata Zone).|16-MAY-23
27074|Aldinga Member|Comments|The Aldinga Member as considered here is clearly a modification of the original usage of Crespin (1954). The boundaries are here rigidly defined whereas Crespin's original proposal was vague and she was probably referring to the entire Port Willunga Formation as outcropping at the type section.|16-MAY-23
24153|Alinerta Gravel|Name source|Mount Alinerta; grid reference 576115, Dalhousie 1:250 000 Sheet area.|16-MAY-23
24153|Alinerta Gravel|Unit history|Part of "Gypsite land surface" on Oodnadatta 1:250 000 geological map area (Freytag et al., 1967); Warrina surface (Wopfner, 1978, p.122).|16-MAY-23
24153|Alinerta Gravel|Type section locality|Four metres gypcreted gravel at grid reference point 573104 (Air photo point Alinerta/2/080/5) exposed in a bluff. Reference section at 543057 (Air photo point Hamilton/1/0126/17) in dissected land surface.|16-MAY-23
24153|Alinerta Gravel|Extent|The unit occurs in the breached anticlines on Dalhousie 1:250 000 Sheet area (SG53-11), covering an area of some 400 km2.|16-MAY-23
24153|Alinerta Gravel|Thickness range|Usually 2-5 m.|16-MAY-23
24153|Alinerta Gravel|Lithology|Gypcreted, conglomeratic, silty sand; clasts of silcrete pebbles, cobbles and boulders, and of bleached and porcellanitized Mesozoic shale; gypsum finely to coarsely crystalline and imparts a very pale buff to pink hue to the unit.|16-MAY-23
24153|Alinerta Gravel|Relationships and boundaries|Overlies Marree Subgroup with erosional disconformity and mild angular unconformity. Lower boundary usually obscured but in places can be observed channelling into Marree Subgroup. Upper boundary almost invariably ground surface.|16-MAY-23
24153|Alinerta Gravel|Age reasons|No fossils have been recovered. Age indirectly estimated as Early Pleistocene from the tectonic development of Dalhousie Anticline.|16-MAY-23
24153|Alinerta Gravel|Comments|Alinerta Gravel is interpreted as the gypcreted debris derived from the break-up of anticlinal crests. Levelling out of debris during reworking, and fixing by groundwater gypsum impregnation, formed extensive, low-relief Pleistocene land surfaces which were dissected following tectonic uplift. Photo-interpretation indicates multiple surfaces representing intermittent tectonic uplift.|16-MAY-23
540|Arburee Rhyolite|Name source|From Arburee paddock on Lake Everard Station. Arburee paddock is adjacent to extensive outcrops of Arburee Rhyolite. The centre of this paddock is located at 31o48.5' lat. And 134o43' longitude.|16-MAY-23
540|Arburee Rhyolite|Type section locality|Defined as a north-south section through the range of hills immediately to the north of Lake Everard homestead. The section goes from the basal contact to the brecciated upper contact. Lake Everard homestead is at lat. 31o44.5' and long. 135o10.5'.|16-MAY-23
540|Arburee Rhyolite|Extent|Forms a long narrow dyke-like outcrop crossing from the south-western portion of the Gairdner 1:250 000 Sheet area onto the south-eastern portion of the Childara 1:250 000 Sheet area, occupying outcrop area of roughly 110 km2.|16-MAY-23
540|Arburee Rhyolite|Lithology|In weathered outcrop the unit has a distinct orange colour, but in fresh hand specimen the colour is a purplish-grey. In hand specimen the rock consists of coarse grained phenocrysts of alkali feldspar and medium-grained rounded phenocrysts of quartz sitting in an aphanitic groundmass - i.e., a rhyolite porphyry.  Well developed, contorted flow-banding is often developed on macro and micro scale. In thin section the rock consists of euhedral, corroded and altered phenocrysts of alkali feldspar of medium to coarse grainsize and anhedral medium grainsize phenocrysts of quartz. Plagioclase phenocrysts are very rare and ferromagnesian minerals and their alteration products are totally absent. Alkali feldspar phenocrysts:quartz phenocrysts roughly 4:1 with the phenocrysts making up 33% of the rock. Groundmass exhibits a snowflake devitrification texture and consists of a finely crystalline mosaic of quartz and feldspar. Red limenite is scattered throughout the groundmass. The complete devitrification has completely obliterated any original textures.|16-MAY-23
540|Arburee Rhyolite|Relationships and boundaries|In the west on the Childara 1:250 000 Sheet area the Arburee Rhyolite is clearly intrusive into the Mangaroongah Dacite. In the east in the vicinity of Lake Everard homestead, the Arburee Rhyolite conformably overlies the Mangaroongah Dacite. The upper contact of the Arburee Rhyolite is marked by a zone of autobrecciation (mainly flow brecciation) with angular blocks up to several metres across. These features indicate that the Arburee Rhyolite is a lava dome - i.e., a thick localised pile of highly viscous lava, with its feeder conduit (or roots) exposed in the west - as evidenced by its intrusive nature here. This unit has been previously correlated with the Wheepool Rhyolite (Blissett) by Blissett. Detailed mapping has led the proposer to believe this correlation is in error and that the Arburee Rhyolite is a distinct unit, as defined. Thickness not estimable.|16-MAY-23
540|Arburee Rhyolite|Age reasons|Co-magmatic with the rest of the volcanics in the Glyde Hill Complex (Blissett) as is conformably overlain by the Bunburn Dacite. Therefore age is roughly 1550 my - or mid-Carpentarian from geochronology.|16-MAY-23
24164|Arcoeillinna Sandstone|Name source|Arcoeillinna Soak, NW Mt Johns Range, Everard 1:250 000 grid reference (65606211).|16-MAY-23
24164|Arcoeillinna Sandstone|Unit history|Formerly the lower part of the Trainor Hill Sandstone of Krieg (1973).|16-MAY-23
24164|Arcoeillinna Sandstone|Type section locality|Located on the eastern margin of the Mount Johns Range (Section 8). Grid reference 34649877-34699880.|16-MAY-23
24164|Arcoeillinna Sandstone|Extent|Northern and eastern margin of the Mount Johns Range, part of the Officer Basin as sporadic outcrops around the Observatory Hill area.|16-MAY-23
24164|Arcoeillinna Sandstone|Thickness range|98 m in the Type area, 55 m in Byilkaoora-1 to 60 m on the northern part of the Mount Johns Range.|16-MAY-23
24164|Arcoeillinna Sandstone|Lithology|Red-brown arkosic and lithic sandstone and minor interbedded siltstone and claystone. Vary in being friable and porous to siliceous and indurated. Large to medium scale cross bedding, tangential to tabular.|16-MAY-23
24164|Arcoeillinna Sandstone|Relationships and boundaries|Sharply overlies (erosionally) the Observatory Hill on the northern margin of the Mount Johns Range. On the eastern margin of the range, there is an intertonguing and transitional lower boundary with the Observatory Hill Beds. Shale overlain by the Mount Johns Conglomerate.|16-MAY-23
24164|Arcoeillinna Sandstone|Age reasons|No fossil or radiometric age. Overlies the Early-?Middle Cambrian Observatory Hill Beds and underlies the ?Ordovician Mount Chandler Sandstone.|16-MAY-23
82223|Aristarchus Metaperidotite|Name source|Aristarchus Rise, TARCOOLA, SH5310, 1:250,000 map sheet (Daly and Fanning 1993). Located at GDA2020, MGA53, 367500 mE, 6634473 mN.|16-MAY-23
82223|Aristarchus Metaperidotite|Unit history|Previously known as the Aristarchus Peridotite. Previous definition also included the Burden Metagabbro (new name).|16-MAY-23
82223|Aristarchus Metaperidotite|Type section locality|Type Drillhole: Aristarchus 1 (3239), interval 99.5-106.1 m. Drilled by the South Australia Department of Mines and Energy, SADME, in 1991. Located at GDA2020, MGA53, 367200 mE, 6633919 mN. Reference Drillhole: DMDD-002 (234168), interval 307.44-307.89 m. Drilled by Dominion Mining in 2007. Located at GDA2020, MGA53, 367793 mE, 6634851 mN. Core available at the SA Drill Core Reference Library, Tonsley.|16-MAY-23
82223|Aristarchus Metaperidotite|Extent|Occurs in drillholes near Aristarchus Paddock in the southern Christie Domain.|16-MAY-23
82223|Aristarchus Metaperidotite|Thickness range|Up to 7 m, but typically 0.2-0.4 m thick in type drillhole.|16-MAY-23
82223|Aristarchus Metaperidotite|Lithology|In the type drillhole, the Aristarchus Metaperidotite comprises pargasite-tremolite-serpentine-olivine amphibolite interpreted as metaperidotite (lherzolite; Daly and van der Stelt 1992). Tremolite and pargasite are interpreted to replace pyroxene oikocrysts, with a fine-grained cumulus groundmass of olivine, tremolite, serpentine, magnetite, chromite and sulfide. Hornblende-biotite schist with minor plagioclase also occurs, interpreted as a metapyroxenite (Daly and van der Stelt 1992). Samples in the type drillhole are typically heavily weathered to bright green clay, whereas samples from the reference drillhole are fresher. In the reference drillhole, the Aristarchus Metaperidotite comprises granular hornblende-biotite metapyroxenite with sparse plagioclase, carbonate, ilmenite and titanite, and up to 8% disseminated sulfides including pyrrhotite, pentlandite, pyrite and lesser chalcopyrite (McKinnon-Matthews 2007).|16-MAY-23
82223|Aristarchus Metaperidotite|Relationships and boundaries|Intrudes the Aurora Tank Suite and Burden Metagabbro with sharp, irregular contacts. Occurs as narrow dykes.|16-MAY-23
82223|Aristarchus Metaperidotite|Identifying features|Weakly foliated, low proportion of plagioclase, pyroxene pervasively altered to amphiboles. Sharp intrusive contacts with surrounding lithologies.|16-MAY-23
82223|Aristarchus Metaperidotite|Structure and Metamorphism|Variable, generally weak foliation. Locally mylonitic. Pervasive replacement of pyroxene by amphiboles.|16-MAY-23
82223|Aristarchus Metaperidotite|Age reasons|Undated; maximum magmatic age c. 2474 Ma constrained by granite gneiss of the Aurora Tank Suite (DMDD-002; Jagodzinski et al. 2009).|16-MAY-23
82223|Aristarchus Metaperidotite|Correlations|Potential correlative of the c. 2460 Ma Skuse Hill Metapyroxenite.	|16-MAY-23
82223|Aristarchus Metaperidotite|Alteration and Mineralisation|Hosts disseminated pentlandite ore and has elevated nickel contents (McKinnon-Matthews et al., 2007).|16-MAY-23
82223|Aristarchus Metaperidotite|Geochemistry|Compositions range from tholeiitic to calc-alkaline, high MgO contents and juvenile Nd signatures. Aluminium-depleted komatiitic source (Daly and Fanning, 1993; Wade, 2012).|16-MAY-23
82223|Aristarchus Metaperidotite|Defn author|Willims, M.A., 9-JUN-2021.|16-MAY-23
82223|Aristarchus Metaperidotite|Comments|Replaces "Aristarchus Peridotite".|16-MAY-23
82223|Aristarchus Metaperidotite|References|Daly, S.J., Fanning, C.M., 1993. Archean, in: Drexel, J.F., Preiss, W.V., Parker, A.J. (Eds.), The geology of South Australia. Volume 1 - The Precambrian. Geological Survey of South Australia,Bulletin, 54, pp. 32-49.  **Daly, S.J., van der Stelt, B.J., 1992. Archaean metabasic diamond drilling project. Department of Mines and Energy. Open file Envelope 08541, 1531-1902.  **Jagodzinski, E.A., Reid, A.J., Fraser, G.L., 2009. Compilation of SHRIMP U-Pb geochronological data for the Mulgathing Complex, Gawler Craton, South Australia, 2007-09. Primary Industries and Resources South Australia. Report Book 2009/00016.  **Kennecott Explorations (Australia) Pty. Ltd., 1971. SML 491 - Final Report. South Australia. Department of Mines. Open file Envelope 01510, 304-347.  **McKinnon-Matthews, J., Purvis, A.C., Tomkins, A.G., 2007. Unlocking South Australia's Mineral and Energy Potential - A Plan for Accelerating Exploration. Theme 2 (drilling partnerships with PIRSA and industry) : Year 4 partnership no. DPY4-09, Dominion JV area magmatic nickel-copper-PGE mineral prospects. Project final report. Primary Industries and Resources South Australia. Open file Envelope 11447.  **Reid, A.J., Daly, S.J., 2009. The Mulgathing and Sleaford complexes of the Gawler Craton: a historical perspective of the geology and mineral potential. Primary Industries and Resources South Australia. MESA Journal 52, 4-12.  **Reid, A.J., Jagodzinski, E.A., Fraser, G.L., Pawley, M.J., 2014. SHRIMP U-Pb zircon age constraints on the tectonics of the Neoarchean to early Paleoproterozoic transition within the Mulgathing Complex, Gawler Craton, South Australia. Precambrian Research 250, 27-49.  **Wade, C.E., 2012. Geochemistry of pre-1570 Ma mafic magmatism within southern Australia: implications for possible tectonic settings and timing of major mineralisation events in South Australia. Government of South Australia. Department for Manufacturing, Innovation, Trade, Resources and Energy. Report Book 2012/00019.  **Williams, M.A., Reid, A.J., 2021. Linking lithostratigraphy to mineral potential for the Archean to earliest Paleoproterozoic Mulgathing Complex, central Gawler Craton. South Australia. Department for Energy and Mining. MESA Journal 94, 04-18.|16-MAY-23
82225|Aurora Tank Suite|Name source|Aurora Tank, COOBER PEDY, SH5306, 1:250,000 map sheet. Located at GDA2020, MGA53, 404643 mE, 6715420 mN.|16-MAY-23
82225|Aurora Tank Suite|Unit history|Previously informally attributed to the Kenella Gneiss, Glenloth Granite or undifferentiated Mulgathing Complex.|16-MAY-23
82225|Aurora Tank Suite|Type section locality|Four kilometres west of Aurora Tank. Located at GDA2020, MGA53, 400471 mE, 6715483 mN. Reference Drillhole: DMDD-002 (234168), interval 196-307 m. Drilled by Dominion Mining NL in 2007. Located at GDA2020, MGA53, 367793 mE, 6634851 mN. Core available at the SA Drill Core Reference Library, Tonsley.|16-MAY-23
82225|Aurora Tank Suite|Extent|The Aurora Tank Suite outcrops in the northern Gawler Craton near Aurora Tank and Commonwealth Hill Outstation and occurs in drillholes in the Aristarchus prospect.|16-MAY-23
82225|Aurora Tank Suite|Thickness range|Intersection of 313 m of Aurora Tank Suite interlayered with Burden Metagabbro in the reference drillhole (base not intersected), with individual granitoid layers 0.1 to 15 m thick.|16-MAY-23
82225|Aurora Tank Suite|Lithology|Metamorphosed granitoids including tabular K-feldspar granite, hematite-stained syenogranite gneiss and granoblastic granitic gneiss. At the type locality, the Aurora Tank Suite comprises porphyritic, feldspar-rich granite with elongate K-feldspar phenocrysts (Reid et al. 2014). At the reference locality, the Aurora Tank Suite comprises potassic-altered, granoblastic granitic gneiss. The granitic gneiss has variably assimilated older mafic material, and locally grades to granodiorite. The reference Aurora Tank Suite granitoid is typically orange-red. Locally, unaltered grey gneiss contains red alteration veins.|16-MAY-23
82225|Aurora Tank Suite|Relationships and boundaries|Intrudes Christie Gneiss and Burden Metagabbro. Variable assimilation of the Burden Metagabbro with generally diffuse contacts in reference drillhole. Intruded by and occurs as enclaves within Aristarchus Metaperidotite.|16-MAY-23
82225|Aurora Tank Suite|Identifying features|Magmatic ages c. 2475-2470 Ma. Foliated granites, intruded during early stages of regional (Sleafordian) metamorphism. Typically K-feldspar-rich (Jagodzinski and Reid, 2017; Jagodzinski et al., 2009; Reid et al., 2014).|16-MAY-23
82225|Aurora Tank Suite|Structure and Metamorphism|Recrystallisation and grain alignment resulting in foliation. Intensity and orientation variable between granites in the suite.|16-MAY-23
82225|Aurora Tank Suite|Age reasons|Paleoproterozoic; magmatic ages c. 2475-2470 Ma (SHRIMP U-Pb zircon; Jagodzinski and Reid 2017; Jagodzinski et al. 2009; Reid et al. 2014).|16-MAY-23
82225|Aurora Tank Suite|Correlations|Tentatively correlated to other granitoid lithologies of unknown age in the Aristarchus prospect which intrude the Christie Gneiss. Likely temporal correlative of Kiana Granite (Dutton Suite, Sleaford Complex).|16-MAY-23
82225|Aurora Tank Suite|Defn author|Williams, M.A., 9-JUN-2021.|16-MAY-23
82225|Aurora Tank Suite|References|Benbow, M.C., 1993. TALLARINGA, South Australia. Sheet SH/53-05. South Australia. Department of Mines and Energy. 1:250 000 Geological Series - Explanatory Notes.  **Fanning, C.M., Reid, A.J., Teale, G.S., 2007. A geochronological framework for the Gawler Craton, South Australia. Primary Industries and Resources South Australia. Bulletin 55.  **Halpin, J.A., Reid, A.J., 2016. Earliest Paleoproterozoic high-grade metamorphism and orogenesis in the Gawler Craton, South Australia: The southern cousin in the Rae family? Precambrian Research 276, 123-144.  **Hill, R.J., Hungerford, N., 2000. Mount Christie. Annual reports to licence expiry/renewal, for the period 24/2/1995 to 23/2/2000. Primary Industries and Resources. South Australia. Open file Envelope 09538.  **Jagodzinski, E.A., Reid, A.J., 2017. PACE Geochronology: Results of collaborative geochronology projects, 2013-2015. South Australia. Department of the Premier and Cabinet. Report Book 2015/00003.  **Jagodzinski, E.A., Reid, A.J., Fraser, G.L., 2009. Compilation of SHRIMP U-Pb geochronological data for the Mulgathing Complex, Gawler Craton, South Australia, 2007-09. Primary Industries and Resources South Australia. Report Book 2009/00016.  **McKinnon-Matthews, J., Purvis, A.C., Tomkins, A.G., 2007. Unlocking South Australia's Mineral and Energy Potential - A Plan for Accelerating Exploration. Theme 2 (drilling partnerships with PIRSA and industry) : Year 4 partnership no. DPY4-09, Dominion JV area magmatic nickel-copper-PGE mineral prospects. Project final report. Primary Industries and Resources South Australia. Open file Envelope 11447.  **Reid, A.J., Jagodzinski, E.A., Fraser, G.L., Pawley, M.J., 2014. SHRIMP U?Pb zircon age constraints on the tectonics of the Neoarchean to early Paleoproterozoic transition within the Mulgathing Complex, Gawler Craton, South Australia. Precambrian Research 250, 27-49.  **Wade, C.E., 2012. Geochemistry of pre-1570 Ma mafic magmatism within southern Australia: implications for possible tectonic settings and timing of major mineralisation events in South Australia. South Australia. Department for Manufacturing, Innovation, Trade, Resources and Energy. Report Book 2012/00019.  **Williams, M.A., Reid, A.J., 2021. Linking lithostratigraphy to mineral potential for the Archean to earliest Paleoproterozoic Mulgathing Complex, central Gawler Craton. South Australia. Department for Energy and Mining. MESA Journal 94, 04-18.|16-MAY-23
947|Baldry Rhyolite|Name source|From Baldry dam and paddock on Lake Everard station. Baldry paddock contains most of the exposed outcrop of Baldry Rhyolite. Baldry dam is located at 31o41 1/4' lat. And 135o04 1/2' longitude.  Origin: The Baldry Rhyolite is extremely variable, with no two outcrops exhibiting the same textural features. As the Baldry Rhyolite forms only low subdued outcrops few good sections are observable. However, on the basis of the variability and type of rocks forming the Baldry Rhyolite and the rapid thinning of this unit at its margins it is considered that the Baldry Rhyolite is a lava dome made up of highly viscous rhyolitic lavas and explosive ashflows (of low energy) that have been extruded onto a slope, hence explaining the flowage during welding. The source is not obvious, but undoubtedly would have been located within the confines of the present outcrop of the Baldry Rhyolite.|16-MAY-23
947|Baldry Rhyolite|Type section locality|Due to the variable nature of this unit it is not possible to propose a type section.|16-MAY-23
947|Baldry Rhyolite|Extent|Confined almost entirely to the far south west of the Gairdner 1:250 000 Sheet area. A few outcrops extend over onto the Childara 1:250 000 Sheet area. The outcrop covers a roughly circular area of diameter 12 km.|16-MAY-23
947|Baldry Rhyolite|Lithology|A white to buff coloured rock, invariably containing quartz phenocrysts, but showing a wide variety of textures. At one extreme flow banding is pervasively developed on all scales, often being extremely contorted, indicating an origin as a highly viscous lava. On the other extreme the unit appears to be a poorly welded lapilli-tuff of ashflow origin. The lapilli size lithic fragments and crystals of quartz and alkali feldspar are set in a vitroclastic groundmass, consisting of slightly deformed glass shards and pumice fragments, now entirely devitrified, but with outlines clearly visible. The most common rock type making up the Baldry Rhyolite lies between these two extremes and is a strongly welded lithic-vitric-crystal tuff of ashflow origin, exhibiting a well developed eutaxitic texture formed by the flattened lithic and pumice fragments. The glass shards in the groundmass are markedly flattened and wrapped around the crystals and lithic fragments. Often a semi-continuous flow banding is developed, indicating a certain degree of flowage during welding - thus the term rheoignimbrite would be applicable to these rocks. Rheoignimbrites are the major rock type making up the Baldry Rhyolite.|16-MAY-23
947|Baldry Rhyolite|Relationships and boundaries|The Baldry Rhyolite is considered to be younger than the Bunburn Dacite although the contact between the two is never seen. The Baldry Rhyolite is unconformably overlain by the Yantea Rhyodacite. The Baldry Rhyolite is very localised and is probably at least 60 m thick in the central regions of its outcrop, however at its margins it thins rapidly. The Baldry Rhyolite is almost certainly a lava dome formed of a series of highly viscous lava flows and ash flows, hence explaining its localised nature.|16-MAY-23
947|Baldry Rhyolite|Age reasons|Belongs to the Glyde Hill Complex as defined by Blissett. The complex is of mid-Carpentarian age, roughly 1550 ma upon the basis of geochronology.|16-MAY-23
1011|Balta Granite|Name source|Balta Baltana Creek which drains northwards into Lake Cadibarrawirracanna.|16-MAY-23
1011|Balta Granite|Type section locality|Type area 8.5 km north northwest of Hat View, bounded by latitudes 29o28' and 29o29'S, longitudes 135o11' and 135o13'E.|16-MAY-23
1011|Balta Granite|Extent|The unit is exposed over 200 km2 in the northwestern portion of the Billa Kalina 1:250 000 sheet area (SH53-7), in the headwaters of Engenina and Balta Baltana Creek|16-MAY-23
1011|Balta Granite|Lithology|Red, microcline-rich granites; porphyritic granites with feldspar phenocrysts ranging in size up to 15 mm; hornblende-biotite-scapolite-rich hybrid granites. Not foliated.|16-MAY-23
1011|Balta Granite|Relationships and boundaries|Intrudes unnamed metamorphics of assumed Archaean to Early Proterozoic age. Overlain by Cretaceous sediments of the Mount Anna Sandstone.|16-MAY-23
1011|Balta Granite|Age reasons|Approximate age from Rb/Sr geochronology of 1450-1550 Ma (Webb, 1977).|16-MAY-23
24172|Baltucoodna Quartzite|Name source|Baltucoodna is an Aboriginal name for a waterhole on the Peake Creek east of the Peake and Denison Ranges, 4.3 km north of the ruins of the Peake overland telegraph station. Warrina 1:100 000 sheet area, Warrina 1:250 000 sheet area, metric reference 6898300, 589350.|16-MAY-23
24172|Baltucoodna Quartzite|Type section locality|4 500 metres of white quartzites and basalts from 6888100, 592200 (base) through Mount Denison 6886100, 594100 to 6883600, 592150 (top of section).|16-MAY-23
24172|Baltucoodna Quartzite|Extent|Peake and Denison Ranges: the unit is exposed over 25 km2 south and southeast of "Peake" ruins and within ?Early Proterozoic basement rocks in the southern portion of the ranges.|16-MAY-23
24172|Baltucoodna Quartzite|Thickness range|Minimum of 4 500 metres.|16-MAY-23
24172|Baltucoodna Quartzite|Lithology|In the type section, greyish white quartzites, porphyritic and amygdaloidal basalts, minor quartz+muscovite schists, and grey phyllites. Elsewhere, also sillimanite gneisses, quartz+feldspar+biotite gneisses and schists, plagioclase+hornblende+epidote calc-silicates, calcite marbles.|16-MAY-23
24172|Baltucoodna Quartzite|Relationships and boundaries|In the type section, the base is sheared, elsewhere the unit conformably overlies unnamed schists of the Peake Metamorphics. Top of the unit is not exposed.|16-MAY-23
24172|Baltucoodna Quartzite|Age reasons|?Early Proterozoic: the intrusive Wirricurrie Granite has been radiometrically dated at 1648+/-21 Ma providing a minimum age.|16-MAY-23
81797|Bendieuta Member|Name source|Bendieuta Creek, east of Mt. Frome.|16-MAY-23
81797|Bendieuta Member|Unit history|Previously published as 'Bendieuta Formation' (Lafuste et al., 1991).|16-MAY-23
81797|Bendieuta Member|Geomorphic expression|Forms basal exposures of broad folds, or anticlinal cores.|16-MAY-23
81797|Bendieuta Member|Type section locality|Section M, 130 to 510 ft.(39.6 to 155.4 m) 31deg 0'50.17"S, 139deg14'44.83"E to 31deg 0'46.91"S, 139deg14'38.70"E|16-MAY-23
81797|Bendieuta Member|Extent|Exposed low on hill slopes in the area from Mt. Chambers Gorge to Mt. Chambers Mine, Mt. Daily, and south towards Mt. Frome.|16-MAY-23
81797|Bendieuta Member|Thickness range|116 m (381 ft) in type section on Section M. Lenticular across region.|16-MAY-23
81797|Bendieuta Member|Lithology|Massive to thick bedded, part mottled, buff to light grey or pink, part oolitic to fenestral, peloid limestones with interbeds of broadly cross-bedded, rippled, silty to sandy quartz granule-rich limestones, and small, buff, silty dolostone intraclasts. Sparse fauna, with rare transported archaeocyaths, and small brachiopods.|16-MAY-23
81797|Bendieuta Member|Depositional environment|Carbonate platform as backreef shelf or channel margin shoals at sites of high tidal energy, adjacent to abundant clastic carbonate (archaeocyath meadows) and siliciclastic (emergent salt dome) sources.|16-MAY-23
81797|Bendieuta Member|Relationships and boundaries|Member of the Mernmerna Formation, as a lenticular interbed. Passage zone from dark grey flaggy limestones of the basal Mernmerna Formation below. Abrupt contact (disconformity?) at top with the dark grey flaggy limestones of a younger unit of the Mernmerna Formation.|16-MAY-23
81797|Bendieuta Member|Structure and Metamorphism|Massive beds of moderate dip on broad fold limbs and cores.|16-MAY-23
81797|Bendieuta Member|Age reasons|Lower Cambrian, Stage 3 to 4, within the Dailyatia odyssei SSF zone and the Paraia tatei and P. bunyerooensis Zones (Betts et al., 2017b; Figure 2 of Jago et al., this volume).|16-MAY-23
81797|Bendieuta Member|Correlations|See Figure 2 of Jago et al., this volume.|16-MAY-23
81797|Bendieuta Member|Defn author|T. J. Mount, 8-JAN-2019, after Mount (1970).|16-MAY-23
81797|Bendieuta Member|Comments|Member status confirmed by local mapping.|16-MAY-23
81797|Bendieuta Member|References|Jago, J. B., Gehling, J. G., Betts, M. J., Brock, G. A., Dalgarno, C. R., Garcia-Bellido, D. C., ... Paterson, J. R. (2019). The Cambrian System in the Arrowie Basin, Flinders Ranges, South Australia. Australian Journal of Earth Sciences. doi:10.1080/08120099.2018.1525431  **Lafuste, J., Debrenne, F., Gandin, A., & Gravestock, D. I. (1991). The oldest tabulate corals and the associated Archaeocyatha, Lower Cambrian, Flinders Ranges, South Australia. Geobios, 24(6), 697-718. doi:10.1016/S0016-6995(06)80298-6  **Mount, T. J. (1970). Geology of the Mt. Chambers Gorge region (BSc. (Honours) thesis, unpublished).Adelaide, SA: University of Adelaide. http:hdl.handle.net/2440/67162.  **T. J. Mount, J. B. Jago, N. R. Langsford & C. R. Dalgarno (2019): Geological setting of the Moorowie Formation, lower Cambrian Hawker Group, Mt Chambers Gorge, eastern Flinders Ranges, South Australia, Australian Journal of Earth Sciences, DOI: 10.1080/08120099.2019.1586771.|16-MAY-23
24179|Benitos Clay|Name source|Benitos Folly Opal Field on Coober Pedy 1:63 360 map sheet, Coober Pedy 1:250 000.|16-MAY-23
24179|Benitos Clay|Type section locality|Type locality Benitos Folly and Black Flag opal fields. Section 2.62 km south of Coober Pedy township, 50 m on west side of Stuart Highway.|16-MAY-23
24179|Benitos Clay|Extent|Stuart Range and Uplands and flanking areas to the north and east.|16-MAY-23
24179|Benitos Clay|Thickness range|1-2 metre, average 1 metre.|16-MAY-23
24179|Benitos Clay|Lithology|Red brown clay and silt, prismtic structured silcrete gibber mantled.|16-MAY-23
24179|Benitos Clay|Relationships and boundaries|Sits sharply on Giddinna Formation. Holocene brown and greyish unnamed clays and silts, gibber covered, sit sharply on top.  No fossils that are diagnostic; considered to be latest Pleistocene.  Part of Firman's (1969) Pooraka Formation.|16-MAY-23
24185|Black Knob Marble|Name source|Black Knob Hill, 27 km SE of 'Callanna'.|16-MAY-23
24185|Black Knob Marble|Unit history|Black Knob Marble' of Murrell (1977).|16-MAY-23
24185|Black Knob Marble|Type section locality|Black Knob Hill, lat. 29o52', long. 137o41'.|16-MAY-23
24185|Black Knob Marble|Extent|Willouran Ranges.|16-MAY-23
24185|Black Knob Marble|Thickness range|25 m at type section, up to 100 m elsewhere.|16-MAY-23
24185|Black Knob Marble|Lithology|Black carbonaceous calcitic marbles with phlogopite, smoky quartz and potash feldspar restricted to certain beds, chalcedonic nodules in some bedding planes.|16-MAY-23
24185|Black Knob Marble|Relationships and boundaries|Occurs within megabreccia. Intruded by dolerite and thus may be older than Noranda Volcanics.|16-MAY-23
24185|Black Knob Marble|Identifying features|Large blocks or dismembered beds of dark grey to white calcitic marble within megabreccia.  |16-MAY-23
24185|Black Knob Marble|Age reasons|Early Willouran. Possibly equivalent to Wywyana Formation (Arkaroola Subgroup) and Coominaree Dolomite.|16-MAY-23
1901|Blanche Point Formation|Name source|From "Blanche Point" a conspicuous promontory on the east coast of Gulf St. Vincent seperating Maslin and Aldinga Bays.|16-MAY-23
1901|Blanche Point Formation|Type section locality|Coastal cliffs of Maslin and Aldinga Bays from Tortachilla Trig. South to Aldinga Ck.|16-MAY-23
1901|Blanche Point Formation|Extent|Eastern side of Cainozoic St. Vincent Basin including Willunga and Noarlunga Embayments as well as Adelaide Plains.|16-MAY-23
1901|Blanche Point Formation|Thickness range|Range 25-60 m|16-MAY-23
1901|Blanche Point Formation|Lithology|Siliceous, calcareous, glauconitic limestones, silts, and clays.  Beds containing abundant horizons of chert are separated off as the Gulf Rock Member.|16-MAY-23
1901|Blanche Point Formation|Relationships and boundaries|Unconformably overlies Tortachilla Limestone. Disconformably overlain by Chinaman Gully Formation. Lateral equivalent to Rogue Formation.|16-MAY-23
1901|Blanche Point Formation|Age reasons|Late Eocene. The occurrence of the planktic foraminifer Hantkenina primitiva near the base of the formation is diagnostic of this age.|16-MAY-23
1901|Blanche Point Formation|Proposed publication|Rep. Inv. Geol. Surv. S. Aust. 50|16-MAY-23
1901|Blanche Point Formation|Comments|The term 'Noarlunga' Limestone has also been used for this unit. Reynolds and several subsequent workers have called the formation a marl.|16-MAY-23
25795|Blue Mine Conglomerate|Type section locality|Approximately half a mile northeast of Arkaroola Homestead, north side of Kingsmill Creek, lat. 30degrees 19'19" long. 139degrees 22'16" to lat. 30degrees 19'32" long.139degrees 22'01 [assumed AGD 66]|16-MAY-23
25795|Blue Mine Conglomerate|Defn author|R.P. Coats, SA Dept of Mines, 1971.|16-MAY-23
27311|Boorloo Siltstone|Name source|Boorloo Creek, 8 km E. of The Dome.|16-MAY-23
27311|Boorloo Siltstone|Unit history|Boorloo Siltstone of Murrell (1977). Probably BS3 to BS5 and WU3 to WU5 units of Rowlands et al. (1980, p.62)|16-MAY-23
27311|Boorloo Siltstone|Type section locality|Hilly country west of Boorloo workings and immediately west of a megabreccia mass; lat. 29o45', long. 137o58'.|16-MAY-23
27311|Boorloo Siltstone|Extent|Willouran Ranges.|16-MAY-23
27311|Boorloo Siltstone|Thickness range|519 m in the type section.|16-MAY-23
27311|Boorloo Siltstone|Lithology|Top: 153 m alternating carbonate and grey, green-grey siltstone, minor sandstone; dolomite and limestone units up to 18 m thick, medium grey, dark brown to orange weathering, sandy laminae, flaggy to medium bedded, ?tepee structure.  106 m siltstone, light to dark grey, brownish and greenish grey, thin bedded.  45 m quartzite, fine grained, partly laminated, beds up to 20 cm.  170 m siltstone, partly calcitic, very dark grey, platy to flaggy.  10 m dolomite and silty dolomite, grey, thin bedded.  Base: 35 m siltstone, partly carbonate rich, dark grey, mud cracks, ripple marks, ?gypsum impressions.  Overall sand:shale:carbonate percentages 9:74:17.  Rowlands et al. (1980) observed tepee structures and cauliflower chert nodules.|16-MAY-23
27311|Boorloo Siltstone|Relationships and boundaries|Lies conformably on Cooranna Formation; upper contact against megabreccia.|16-MAY-23
27311|Boorloo Siltstone|Identifying features|A distinctively layered dark siltstone and dolomite sequence at the top of the less disturbed beds of the Callanna Group|16-MAY-23
27311|Boorloo Siltstone|Age reasons|Possibly late Willouran. May be partly equivalent to Duff Creek Beds of the Peake and Denison region (Ambrose et al., 1981), and perhaps to part of the sequence from Arkaba Hill Beds to Worumba Dolomite Beds of the Worumba Anticline.|16-MAY-23
2291|Boorthanna Formation|Name source|Boorthanna 1 well where the unit is best reepresented. Lat. 28o56'4"S, Long. 135o45'18"E on the Billakalinna 1:250 000 sheet.|16-MAY-23
2291|Boorthanna Formation|Unit history|Crown Point Formation (Wells 1966) of the Pedirka Basin. Merrimelia Formation Martin (1967) of the Cooper Basin.|16-MAY-23
2291|Boorthanna Formation|Type section locality|(Subsurface) Boorthanna 1 well between 739.1 m and 1158.2 m on the gamma ray and neutron logs.|16-MAY-23
2291|Boorthanna Formation|Extent|Covers most of the Arckaringa Basin except the structural highs. The lower part of the unit is restricted to the deeper grabens only. Minor tillites occur along the western side of the Peake and Denison Ranges but are not suitable as a type section. Present in Cootanoorina 1 and Weedina 1 wells in the Boorthanna Trough.|16-MAY-23
2291|Boorthanna Formation|Thickness range|419.1 m|16-MAY-23
2291|Boorthanna Formation|Lithology|The upper part consists of varicoloured conglomerates and sandstones depending on the colour of underlying basement and the lower part consists of sand to pebble clays generally grey (diamictites).|16-MAY-23
2291|Boorthanna Formation|Relationships and boundaries|Unconformably overlies crystalline basement on lower Palaeozoic rocks (Townsend 1973/1975). Conformably overlain by Stuart Range Formation (Townsend and Ludbrook 1975).|16-MAY-23
2291|Boorthanna Formation|Age reasons|Early Sakmarian. Ludbrook (1967).|16-MAY-23
2291|Boorthanna Formation|References|01/31594; R088; 01/31595; 79/04361.|16-MAY-23
24194|Bosanquet Formation|Name source|Mount Bosanquet, a prominent hill 10 km east of the type section, on the Kimba 1:100 000 sheet (No. 6131) of the Kimba 1:250 000 sheet.|16-MAY-23
24194|Bosanquet Formation|Type section locality|(Fig. 3) Broad View DDH 1 (Latitude 33o24'53"S, Longitude 136o19'8"E) over the interval 26.2 to 407.8 m. The drillhole did not intersect the eastern limit (possibly the top) of the formation.|16-MAY-23
24194|Bosanquet Formation|Extent|A 1 km-wide zone of outcrop and subcrop, with a strike length of 6 km, approximately 5 km east of Carappee Hill (Flint and Rankin, in prep.). Cainozoic sediments totally veneer basement lithologies to the west, but the Bosanquet Formation may be repeated by tight F2 folding of the Kimban Orogeny.|16-MAY-23
24194|Bosanquet Formation|Thickness range|In the incomplete type section it is 381.6 m but is inferred to have a minimum thickness of approximately 1000 m.|16-MAY-23
24194|Bosanquet Formation|Lithology|The Bosanquet Formation consists of megacrystic, recrystallised and deformed rhyodacite containing relic phenocrysts of coarse-grained microcline and medium-grained, subequant, bluish quartz, with a recrystallised matrix of fine-grained quartz + feldspar + biotite (+/- muscovite, sphene and zircon). The rhyodacite varies from weakly-foliated (with abundant megacrysts and minor embayed quartz) to proto- or blastomylonitic (with attenuation and dynamic recrystallisation of megacrysts producing an intense foliation). The degree of deformation decreases down the drillhole.  Banded grey-green, medium to coarse grained, granoblastic to granoblastic-elongate calcsilicate gneisses are interlayered with the rhyodacites in bands varying from 20 cm to 20 m thick. Rhyodacite clasts also occur within the calcsilicate gneisses, which contain diopside + quartz + microcline + plagioclase + actinolite hornblende + biotite + calcite, and have a weak to intense foliation. Diopside within the gneisses has been partially replaced by hornblende. Coarse grained, diopside-rich calcsilicate gneisses are exposed 500 m north of the drillhole. They contain elongate clasts of rhyolite-rhyodacite, dolomitic marble, granite and quartzite.|16-MAY-23
24194|Bosanquet Formation|Depositional environment|The association of porphyritic acid volcanics and carbonate-matrix conglomerateas (containing volcanic fragments) suggests volcanism contemporaneous with either marine or lacustrine sedimentation.|16-MAY-23
24194|Bosanquet Formation|Relationships and boundaries|The surface contact of the Bosanquet Formation with the Hutchison Group metasediments is concealed by a veneer of Cainozoic sediments, and is only known from drillcore. Within Broad View DDH 1, the boundary between the two units occurs at a depth of 407.8 m, and is marked by a zone of broken core and significant water loss during drilling. The boundary is lithologically sharp between iron-rich and calcium-rich lithologies of the Upper Middleback Jaspilite and acid volcanics of the Bosanquet Formation. There is a slight angular discordancy of 8o for the pervasive metamorphic foliations either side of the contact. It is unclear whether the contact represents either a contemporaneous change from sedimentation to volcanics, or an unconformity with an hiatus in sedimentation prior to eruption of the rhyodacites, or a fault. Stratigraphic facing for the formation is not known, but is assumed to be easterly, consistent with the dip of the foliation.|16-MAY-23
24194|Bosanquet Formation|Age reasons|Rb-Sr geochronology had previously been undertaken on specimen 6131RS45 from exposed volcanics west of the drillhole. The volcanics are highly deformed with ovoid phenocrysts and well-developed biotite and muscovite foliations. The Rb-Sr biotite total rock age was 1626 Ma with an initial 87Sr/86/Sr ratio of 0.7127. Due to low enrichment of radiogenic Sr in the total rock analysis, the age is strongly influenced by the biotite analysis and was thus interpreted to reflect a deformational episode rather than the age of primary crystallisation (Webb and Fanning, 1984).  U-Pb zircon geochronology was carried out on a sample of deformed rhyodacite (6131RS136) collected between 402.6-407.5 m in Broad View DDH 1. Procedures for dissolution, extraction and U-Pb isotopic analysis of the zircons were essentially identical to those reported in Fanning et al. (in press).  Zircon characteristics: The ziracons are characteristically clear, euhedral crystals which have a very pale gold colour. Crystals commonly have one pyramidal termination or are fractured fragments of euhedral crystals. Growth zoning is seen in some grains. Many contain opaque inclusions and colourless, oval and acicular inclusions or voids. There are significant numbers of clear, doubly-terminated cyrstals (Fig. 4).  U-Pb zircon results: The isotopic data are given in Table 1 and plotted on Fig. 5. The five conventional analyses are all discordant and the zircons have apparently lost between 17 and 63 percent of their radiogenic lead if one assumes a simple lead loss model. There is excess scatter about a discordia line fitted to these conventional analyses, MSWD = 13, with an upper concordia intercept of 1848+/-10 Ma and lower intercept of 16+/-30 Ma. These analyses show a strong positive correlation between degree of discordance and U content which suggests a cogenetic suite of zircons. Two crystals from the -160+92 nmO fraction were analysed by the small-sample technique. These grains were pale gold in colour, but glassy clear. They were very elongate grains each having one fractured and one pyramidal termination. The small-sample anslysis is marginally more concordant than the conventional analysis from the -72+53 nmO fraction (16 percent lead loss compared to 17 percent). A discordia line fitted to all siz analyses has a slightly higher MSWD of 15 but the intercepts of 1845+/-9 and 10+/-30 Ma are statistically indistinguishable from the conventional discordia. The apparent simple euhedral morphology of the zircons suggests that they are nof igneous origin and unaffected by metamorphism/deformation. The upper concordia intercept of 1845+/-9 Ma is therefore considered to record the crystallisation age of these zircons and the rhyodacite.|16-MAY-23
24194|Bosanquet Formation|Correlations|Both the boundary relationships with the Upper Middleback Jaspilite and petrographic evidence of intense folding and mylonitisation of the rhyodacites suggest that the Bosanquet Formation was deposited prior to the later stages of the Kimban Orogeny (Rankin and Flint, 1987). The U-Pb zircon age of 1845+/-9 Ma indicates that the Bosanquet Formation is appreciably older than other known Early Proterozoic silicic volcanics of the Gawler Craton, namely the Myola Volcanics (1791+/-4 Ma) and the McGregor Volcanics (1740 Ma) (Fanning et al., in press). This is consistent with geochemical dissimilarities between these three volcanic units (Rankin and Flint, 1987). The age is very similar to the 1850 Ma emplacement age of the Donington Granitoid Suite of southern Eyre Peninsula (Mortimer et al., 1986), which is interpreted to be coincident with the earliest deformational phase of the Kimban Orogeny. The Bosanquet Formation has no other known regional correlatives within South Australia. Volcanics of similar age occur in northern Australia (Wyborn et al., in prep,) including the Leichhardt Volcanics of the Mount Isa area (Blake, 1987) and the El Sherana and Edith River Group of the Pine Creek Inlier (Needham and Stuart-Smith, 1985). Calcsilicate bands in the Bosanquet Formation are lithologically identical to calcsilicates interbanded with Hutchison Group iron formation below 408 m in Broad View DDH 1. This suggests that the Bosanquet Formation may be a previously-unrecognised volcanic unit of the Hutchison Group although deposition of the Hutchison Group has been considered to precede the 1850 Ma Donington Granitoid Suite. The Bosanquet Formation is therefore interpreted to have been deposited within a restricted area of the central Gawler Craton either synchronous or immediately following regional deposition of the Hutchison Group.|16-MAY-23
2364|Boucaut Volcanics|Name source|After Boucauts West Dam, 62 km S of Olary.|16-MAY-23
2364|Boucaut Volcanics|Type section locality|Outcrop width 760 m of grey, pink-grey and greenish amygdaloidal grey rhyolite, dacite, andesite and schist, steeply dipping, 1.5 km SW of Division Dam, Anabama. (Isolated exposure: no top or base identifiable).|16-MAY-23
2364|Boucaut Volcanics|Extent|Central Anabama and NE Oakvale 1:100 000 areas.|16-MAY-23
2364|Boucaut Volcanics|Thickness range|Uncertain; possibly 300-800 m.|16-MAY-23
2364|Boucaut Volcanics|Relationships and boundaries|Possibly related to the Anabama lineament and Anabama granite. A.W. Webb (Amdel, 1976) dated (Rb-Sr) three samples Cambrian (507-569 m.y. approx.).|16-MAY-23
76217|Brillig Catch Member|Name source|Brillig Catch Creek, ~700 m northwest of Moorowie Mine.|16-MAY-23
76217|Brillig Catch Member|Geomorphic expression|Narrow, prominent, blocky ridges of up-ended strata.|16-MAY-23
76217|Brillig Catch Member|Type section locality|Section H, 687 to 792 ft. (209.4 to 241.4 m) 30deg59'56.00"S, 139deg15'58.90"E to 30deg59'56.33"S, 139deg15'59.89"E. Reference section: Section J, 136 ft (basal contact) to 268 ft (upper contact) (41.4 to 81.7 m) 30?58'54.06"S, 139?16'25.50"E to 30?58'57.87"S, 139?16'25.60"E.|16-MAY-23
76217|Brillig Catch Member|Extent|Exposed as a prominent ridge at the eastern margin of foothills from Mt. Chambers Gorge, to the south of Moorowie Mine.|16-MAY-23
76217|Brillig Catch Member|Thickness range|69 m (226 ft) in type section on Section H. Average 41 m (135 ft).|16-MAY-23
76217|Brillig Catch Member|Lithology|Massive cliff forming, homogeneous, pale grey, finely laminated to flaggy or medium bedded, microcrystalline microbial limestone with thin clay partings. Textures after anhydrite. No obvious macrofossils.|16-MAY-23
76217|Brillig Catch Member|Depositional environment|Intertidal to supratidal sabkhas and shallow penesaline lagoons.|16-MAY-23
76217|Brillig Catch Member|Relationships and boundaries|Uppermost unit of the Moorowie Formation, terminating the Hawker Group. Conformable, with passage zones from the purple micaceous siltstones of the Pack Creek Member below, and from an upper contact at the top of a marker bed of finely laminated to flaggy microcrystalline microbial limestone to the red-brown to green shales of the overlying Billy Creek Formation.|16-MAY-23
76217|Brillig Catch Member|Structure and Metamorphism|Ridge forming beds of moderate dip trace the eastern limb of a low-plunge anticline. Part faulted.|16-MAY-23
76217|Brillig Catch Member|Age reasons|Lower Cambrian, Stage 4, within the Pararaia janeae trilobite Zone (Figure 2 of Jago et al., this volume).|16-MAY-23
76217|Brillig Catch Member|Correlations|Probable equivalent of the Edeowie Limestone Member.|16-MAY-23
76217|Brillig Catch Member|Defn author|T. J. Mount,  8-JAN-2019, after Mount (1970).|16-MAY-23
76217|Brillig Catch Member|References|Jago, J. B., Gehling, J. G., Betts, M. J., Brock, G. A., Dalgarno, C. R., Garcia-Bellido, D. C., .., Paterson, J. R. (2019). The Cambrian System in the Arrowie Basin, Flinders Ranges, South Australia. Australian Journal of Earth Sciences. doi:10.1080/08120099.2018.1525431   **Mount, T. J. (1970). Geology of the Mt. Chambers Gorge region (BSc. (Honours) thesis, unpublished).Adelaide, SA: University of Adelaide. http:hdl.handle.net/2440/67162.  **T. J. Mount, J. B. Jago, N. R. Langsford & C. R. Dalgarno (2019): Geological setting of the Moorowie Formation, lower Cambrian Hawker Group, Mt Chambers Gorge, eastern Flinders Ranges, South Australia, Australian Journal of Earth Sciences, DOI: 10.1080/08120099.2019.1586771.|16-MAY-23
2585|British Empire Granite|Name source|British Empire Mine, situated at southern tip of granite. Previously called part of Mudnanatana Granite (Coats and Blissett, 1971).|16-MAY-23
2585|British Empire Granite|Type section locality|Occupies central section of Mount Painter Block, in what is known as Freeling Heights Wilderness area. The term British Empire Granite is a new name for the previously termed Mudnanatana Granite of the Mount Painter Block only.  Grid reference of sample analysed: 139o28'E and 30o05'S.|16-MAY-23
2585|British Empire Granite|Extent|Intrusive into Radium Creek Metamorphics of Coats (1971).|16-MAY-23
2585|British Empire Granite|Lithology|Contains quartz, microcline, albite/oligoclase, biotite, muscovite with minor MN. Rich garnet, apatite and magnetite.|16-MAY-23
2585|British Empire Granite|Identifying features|High Si02 and Rb (413 ppm) and low Ti02, MgO, Zr.  Low K/Rb (82). Composition is as follows:  SiO2 = 75.42; Al2O3 = 13.95; Fe2O3 = 0.90; MnO = 0.04; MgO = <0.01; CaO - 0.61; Na2O = 4.08; K2O = 4.07; TiO2 = 0.06; P2O5 + 0.12; L.O.1 = 0.60; Total = 99.84.|16-MAY-23
25818|Bunburn Dacite|Name source|From Bunburn paddock on Lake Everard station. Bunburn paddock is adjacent to extensive outcrops of Bunburn Dacite. Centre of paddock is at 31o49' latitude and 134o51' longitude. A strongly welded vitric tuff of ashflow origin with only a very minor crystal component. Complete devitrifiction has obscured original textures.|16-MAY-23
25818|Bunburn Dacite|Type section locality|Seen in a north-south section which starts at a point 3 km due north of Lake Everard homestead and runs north for 3/4 km. Lake Everard homestead is located at 31o44 1/2' latitude and 135o10 1/2' longitude|16-MAY-23
25818|Bunburn Dacite|Extent|Forms a long narrow outcrop crossing from the south-western portion of the Gairdner 1:250 000 Sheet area onto the south-eastern portion of the Childara 1:250 000 Sheet area, covering an area of roughly 80 km2.|16-MAY-23
25818|Bunburn Dacite|Thickness range|Thickness appears to be variable ranging from 30 m to at least 100 m in places.|16-MAY-23
25818|Bunburn Dacite|Relationships and boundaries|Upon the basis of field relationships seen, Bunburn Dacide conformably overlies the Arburee Rhyolite.|16-MAY-23
25818|Bunburn Dacite|Age reasons|This unit forms part of the Glyde Hill Complex as previously defined by Blissett and has a mid-Carpentarian age of roughly 1550 Ma as determined by geochronology.|16-MAY-23
25686|Bungadillina Monzonite|Name source|Bungadillina is an Aboriginal name for a waterhole and creek near Warrina railway siding. Warrina 1:100 000 sheet area, Warrina 1:250 000 sheet area, metric reference 6874650, 580950.|16-MAY-23
25686|Bungadillina Monzonite|Type section locality|Porphyritic monzonites, syenites and diorites from 6853100, 602250 to 6852700, 600000. Reference section of porphyritic monzonitic and syenitic sills from 6861400, 597050 to 6858500, 593400.|16-MAY-23
25686|Bungadillina Monzonite|Extent|Occurs as sills, dykes, stock and irregularly shaped intrusives around the headwaters of Bulldog, Levi and Bungadillina Creeks. Boorthanna and Anna Creek 1:100 000 sheet areas.|16-MAY-23
25686|Bungadillina Monzonite|Lithology|Porphyritic monzonites and syenites, porphyritic diorites, porphyritic albitites, minor granites, adamellites and granodiorites.|16-MAY-23
25686|Bungadillina Monzonite|Age reasons|Ordovician: radiometrically dated by K-Ar method. Youngest unit intruded is the Torrensian Skillogalee Dolomite.|16-MAY-23
25819|Bungaree Quartzite|Name source|Bungaree Hill lat. 33o46', long. 138o33'. Burra 1:250 000.|16-MAY-23
25819|Bungaree Quartzite|Type section locality|500 m quartzite, siltstone, carbonate along R. Broughton 7 km WSW of Spalding lat. 33o31', long. 138o32'. Underlain by Benbournie Dolomite, overlain by Skillogalee Dolomite.|16-MAY-23
25819|Bungaree Quartzite|Extent|W. Burra and NNW Adelaide 1:250 000 between Gladstone and Hamley Bridge.|16-MAY-23
25819|Bungaree Quartzite|Thickness range|About 500 m.|16-MAY-23
25819|Bungaree Quartzite|Lithology|Fine- to coarse-grained feldspathic quartzite or arkose, siltstone, minor dolomite; mainly light-coloured. Ripple marks, cross bedding.|16-MAY-23
25819|Bungaree Quartzite|Relationships and boundaries|As in type section: distinguished from Benbournie and Skillogalee by predominance of quartzite. Probably equivalent to upper parts of Aldgate Sandstone and Emeroo Quartzite and to Yednalve Quartzite.|16-MAY-23
25819|Bungaree Quartzite|Age reasons|Adelaidean, Torrensian (upper Precambrian); part of Burra Group. Possibly approx. 800 Ma.|16-MAY-23
25819|Bungaree Quartzite|Comments|Previously correlated with Yednalve Quartzite. Shown on Burra 1:250 000 geological map as part of Rhynic Sandstone. New name completes type formations of Burra Group in its type region. Name approved in letter 74/251, 6.12.76.|16-MAY-23
82226|Burden Metagabbro|Name source|Burden Tank, TARCOOLA, SH5310, 1:250,000 map sheet. Located at GDA2020, MGA53, 366804 mE, 6642670 mN.|16-MAY-23
82226|Burden Metagabbro|Unit history|Previously an unnamed lithology within the Aristarchus Peridotite (now Aristarchus Metaperidotite).|16-MAY-23
82226|Burden Metagabbro|Type section locality|DMDD-002 (234168), interval 96-318 m (total depth). Drilled by Dominion Mining in 2007. Located at GDA2020, MGA53, 367793 mE, 6634851 mN. Core available at the SA Drill Core Reference Library, Tonsley.|16-MAY-23
82226|Burden Metagabbro|Extent|Occurs in drillholes near Aristarchus Paddock in the southern Christie Domain.|16-MAY-23
82226|Burden Metagabbro|Thickness range|Occurs over >220 m in type drillhole, with individual layers 0.05 to >2 m thick.|16-MAY-23
82226|Burden Metagabbro|Lithology|Gabbroic gneiss with plagioclase, hornblende and opaques. Hornblende is poikiloblastic and contains abundant plagioclase, likely representing metamorphosed pyroxene (Reid et al. 2014).|16-MAY-23
82226|Burden Metagabbro|Relationships and boundaries|Intruded by the Aurora Tank Suite with partially diffuse contacts.|16-MAY-23
82226|Burden Metagabbro|Identifying features|Magmatic age c. 2488 Ma. Metamorphosed to amphibolite facies assemblages, pyroxene replaced by amphiboles.|16-MAY-23
82226|Burden Metagabbro|Structure and Metamorphism|Metamorphosed to amphibolite facies with primary pyroxene completely replaced by amphiboles. Locally foliated (Daly and van Der Stelt, 1992; Reid et al., 2014).|16-MAY-23
82226|Burden Metagabbro|Age reasons|Paleoproterozoic; magmatic crystallisation at c. 2488 Ma (SHIMP U-Pb zircon; Reid et al. 2014).|16-MAY-23
82226|Burden Metagabbro|Correlations|Temporal correlative of the Mobella Tonalite (Mulgathing Complex).|16-MAY-23
82226|Burden Metagabbro|Geophysical Expression|Coincident with northwest-trending band of moderate magnetic intensity. Moderate gravity response.|16-MAY-23
82226|Burden Metagabbro|Geochemistry|Calc-alkaline to shoshonitic compositions with variable LILE (Cs, Ba and Rb) and U and Th abundances. moderately to strongly negative Nb anomalies (Wade, 2012).|16-MAY-23
82226|Burden Metagabbro|Defn author|Williams, M.A., 9-JUN-2021.|16-MAY-23
82226|Burden Metagabbro|References|Daly, S.J., van der Stelt, B.J., 1992. Archaean metabasic diamond drilling project. South Australia. Department of Mines and Energy. Open file Envelope 08541, 1531-1902.  **Reid, A.J., Jagodzinski, E.A., Fraser, G.L., Pawley, M.J., 2014. SHRIMP U?Pb zircon age constraints on the tectonics of the Neoarchean to early Paleoproterozoic transition within the Mulgathing Complex, Gawler Craton, South Australia. Precambrian Research 250, 27-49.  **Wade, C.E., 2012. Geochemistry of pre-1570 Ma mafic magmatism within southern Australia: implications for possible tectonic settings and timing of major mineralisation events in South Australia. South Australia. Department for Manufacturing, Innovation, Trade, Resources and Energy. Report Book 2012/00019.  **Williams, M.A., Reid, A.J., 2021. Linking lithostratigraphy to mineral potential for the Archean to earliest Paleoproterozoic Mulgathing Complex, central Gawler Craton. South Australia. Department for Energy and Mining. MESA Journal 94, 04-18.|16-MAY-23
27124|Burnham Limestone|Name source|Burnham Road at Kingston Park on the coast of the Gulf St Vincent about 16 km southeast of Adelaide.|16-MAY-23
27124|Burnham Limestone|Type section locality|The Burnham Limestone is exposed in a cliff at the rear of No. 25 Burnham Road, 200 m south of the intersection of that road with the entrance to Kingston Caravan Park. Supplementary Section:  County Adelaide, Hundred of Willunga, Section 286. The supplementary section is exposed at the top of the boat ramp near the Pt. Willunga kiosk. This site has been selected because the section is representative of sequences within the Pleistocene basins where the unit is associated with sandy clays.|16-MAY-23
27124|Burnham Limestone|Extent|The Burnham Limestone and the underlying Hallett Cove Sandstone crop out near the top of marine cliffs cut into the basement rocks of the Eden Block.|16-MAY-23
27124|Burnham Limestone|Thickness range|About 0.5 m in the type section.|16-MAY-23
27124|Burnham Limestone|Lithology|Pale grey micritic limestone with manganese coatings on irregular surfaces. The limestone contains clasts derived from the underlying Hallett Cove Sandstone.|16-MAY-23
27124|Burnham Limestone|Relationships and boundaries|At the type section, the Burnham Limestone is overlain by at least 4 m of gravelly Pooraka Formation. The limestone contains clasts of the underlying Hallett Cove Sandstone and penetrates eroded joints in the older unit.  The Hallett Cove Sandstone is about 0.5 m thick and overlies about 2 m of red and yellow weathered steeply dipping Proterozoic siltstone.|16-MAY-23
27124|Burnham Limestone|Age reasons|Dr N.H. Ludbrook "..who has examined samples collected in Maslin Bay by Brian Daily, reports that the fauna is indicative of an estuarine or lagoonal environment and is probably of Pleistocene age". (Twidale, Daily and Firman, 1967, p.239). "The paleontological work suggests a correlation of the Maslin Bay unit with sands at Lockleys (in the Adelaide Plains Basin), which were also deposited in a lagoonal environment according to Ludbrook (1963), who assigned the unit to the Pleistocene Calabrian Stage". (Twidale et al., (op. cit.)).|16-MAY-23
27124|Burnham Limestone|References|79/05041; 79/05157; 01/31596|16-MAY-23
26296|Cadlareena Volcanics|Name source|Cadlareena 1:63 360 Sheet area, Warrina 1:250 000 Sheet area.|16-MAY-23
26296|Cadlareena Volcanics|Type section locality|The basal part of the type section is on Warrina where a basal contact with the Younghusband Conglomerate is preserved (metric ref is - base 6890725, 587625 - top 6890725, 587625). The upper part of the section occurs about 5 km east of Douglas Well on Anna Creek (metric ref: base 6823210, 622333 - top 6823210, 622333).|16-MAY-23
26296|Cadlareena Volcanics|Extent|Peake and Denison Ranges; the unit is exposed over about 6 km2 1-2 km east of Douglas Well (metric ref: 6822020, 616750). A number of small outcrops occur on the eastern side of the Ranges about a 5-10 km south-east of Nilpinna H.S. and 1.5 km northeast of Coominaree Mine. On Warrina about 3.5 km southwest of 'Peake' ruins, the volcanics outcrop along a total strike length of 7 km.|16-MAY-23
26296|Cadlareena Volcanics|Thickness range|Maximum true thickness is uncertain. Maximum observed thicknesses are variable up to 750 m measured near Douglas Well.|16-MAY-23
26296|Cadlareena Volcanics|Lithology|Vesicular basalts and altered dolerites; minor andesites, dacites and rhyolites; tuffs lapilli tuffs; minor lenticular reddish mudstone and quartzite with red shale interbeds near base and top.|16-MAY-23
26296|Cadlareena Volcanics|Relationships and boundaries|Disconformably overlies the Younghusband Conglomerate (Ambrose and Flint, in prep.) in the type section. Conformably overlies Coominaree Dolomite on the eastern side of the Peake and Denison Ranges (Ambrose and Flint, in prep.). Throughout the Ranges diapirism occurs above the Volcanics and consequently the upper limit of the unit is unknown.|16-MAY-23
26296|Cadlareena Volcanics|Age reasons|Lower Adelaidean-Callanna Beds (Willouran); the Cadlareena Volcanics are the uppermost member of the Callanna Beds recognised in the Peake and Denison Ranges. In the Mount Painter Province the Wooltana Volcanics (Coats, 1971) are considered equivalent. The Roopena Volcanics (Fander, 1963) from the Whyalla 1:250 000 sheet area are probable equivalents.|16-MAY-23
26296|Cadlareena Volcanics|Proposed publication|Rep. Invest., geol. Surv. S. Aust.|16-MAY-23
26296|Cadlareena Volcanics|References|79/00849; 01/31597.|16-MAY-23
24206|Calthorinna Tillite|Name source|Calthorinna Creek which is a tributary of Anna Creek and joins the main stream 1 km south of Anna Creek R.S. on the Central Australia Railway; Boorthanna 1:100 000 sheet area; Warrina 1:250 000 sheet area; metric reference 6812550, 607475.|16-MAY-23
24206|Calthorinna Tillite|Type section locality|650 metres of sediments outcropping on the northern limb of the Box Creek Syncline, 5.5 km northwest of Box Creek R.S. The top of the un;it is not exposed. Metric reference: Base 6825850, 591950 - Top 6824710, 591550.|16-MAY-23
24206|Calthorinna Tillite|Extent|The unit is restricted in outcrop to a syncline 1 km northeast of Box Creek R.S. (Box Creek Syncline) in the southern part of the Peake and Denison Ranges (Margaret Inlier). A smaller outcrop occurs as a rafted block in a diapir 6 km south of Mt Anna.|16-MAY-23
24206|Calthorinna Tillite|Thickness range|Maximum thickness of the unit observed (650 m) is in the type section. True maximum thickness of the unit is uncertain since the top of the unit is not exposed in the type section.|16-MAY-23
24206|Calthorinna Tillite|Lithology|Mixtite, conglomeratic dolomite, laminated green shale, gritty sandstone; arkose and quartzite; cross-bedding, ripple marks and graded bedding are common. The unit was first described by Reyner (1955).|16-MAY-23
24206|Calthorinna Tillite|Relationships and boundaries|The unit is underlain disconformably by Upper Burra Group sediments-Kalachalpa Formation (Ambrose and Flint, in prep.) It is overlain by and interfingers with an unnamed sandstone.|16-MAY-23
24206|Calthorinna Tillite|Age reasons|Adelaidean-Umberatana Group (Sturtian). Believed to represent the second of the two Sturtian, glaciations - main evidence is the presence of gritty quartzite clasts assumed to have been reworked from the Pandurra Formation (Coats and Forbes, 1977).|16-MAY-23
24206|Calthorinna Tillite|Proposed publication|Rep. Invest., geol. Surv. S. Aust.|16-MAY-23
24206|Calthorinna Tillite|References|79/00850; 01/31598.|16-MAY-23
24213|Carnot Gneisses|Name source|Cape Carnot, approximately 35 km southwest of Port Lincoln.|16-MAY-23
24213|Carnot Gneisses|Unit history|Sleaford Gneisses: Tilley, 1921. Part of Hutchison Group: Johns, 1961. Included in Sleaford Complex: Thomson, 1980.|16-MAY-23
24213|Carnot Gneisses|Type section locality|The coastal outcrop at Cape Carnot (refer to fig 1,p9 in QGN 80 ).|16-MAY-23
24213|Carnot Gneisses|Extent|Exposed over at least 25 km2 in southernmost Eyre Peninsula. From west side of Sleaford Bay, along the southern coast to at least Shoal Point. Occurs in cuttings and quarries along B.H.P. Coffin Bay tramline, at Cobler Hill, and Strawberry Hill.|16-MAY-23
24213|Carnot Gneisses|Lithology|Thinly layered (1-3 cm) garnetiferous quartzofeldspathic gneiss, in parts with layers (thin) of leucogneiss, biotite garnet gneiss, hypersthene gneiss and basic granulite. Less abundantly: augen gneiss, plagioclase gneiss and cordierite garnet gneiss. Within the sequence as minor layers, coarse to medium grained garnetiferous granitic gneiss.|16-MAY-23
24213|Carnot Gneisses|Relationships and boundaries|The Carnot Gneisses are part of the Sleaford Complex. The relationship with other units of the Sleaford Complex has not been observed. At Sleaford Bay the eastern boundary of the unit is structurally concordant with the Hutchison Group, but the nature of the contact is unknown|16-MAY-23
24213|Carnot Gneisses|Age reasons|Whole rock Rb-Sr age of 2412+/-72 Ma (IR = 0.7060+/-0.0008) for a cordierite garnet gneiss at Cape Carnot (87Rb=1.42 x 10-11y-1), this may refer to the petrographically defined granulite facies event. Augen gneiss samples from Cape Carnot yield an imperfect fit age of 2586+/-131 Ma (IR = 0.7012+/-0.0043), believed to be a relict age partially recording an earlier geological process. A Late Archaean/Early Proterozoic Age is assigned to the Carnot Gneisses.|16-MAY-23
24213|Carnot Gneisses|Defn author|Fanning, C.M., Oliver, R.L. & Cooper, J.A. 1981.|16-MAY-23
27309|Chandabooka Dacite|Name source|Chandabooka Well, 18 km east of Kokatha H.S. and 5 km west of Lake Gairdner. Lt. 31o16'30"S; Long. 125o24'30"E. (Gairdner 1:250 000 sheet (SH53-15)).|16-MAY-23
27309|Chandabooka Dacite|Type section locality|East of the Kokatha-Kingoonya road, 3.5 km east of Kokatha H.S. Forms an irregular saucer-shaped structure 14 km wide (west-east) and 10 km long.|16-MAY-23
27309|Chandabooka Dacite|Extent|Between Kokatha H.S. and Lake Gairdner. South of Kultanaby siding on the Transcontinental railway line.|16-MAY-23
27309|Chandabooka Dacite|Thickness range|About 200 m.|16-MAY-23
27309|Chandabooka Dacite|Lithology|Porphyritic dacite grading to rhyodacite, with cream coloured phenocrysts of plagioclase partly replaced by chlorite and epidote. The matrix is generally reddish brown to purplish red; dark greenish-grey to black in lower part. Base is marked by persistent band of fine-grained banded welded tuff.|16-MAY-23
27309|Chandabooka Dacite|Relationships and boundaries|This is the uppermost layered unit in the Gawler Range Volcanics in the Kokatha area, but is intruded by porphyritic rhyolite dykes of unknown age.  Rests unconformably upon the Lake Gairdner Rhyolite north of Chandanooka Well; and upon the Chitanilga Volcanic Complex east of the Kokatha-Kingoonya road|16-MAY-23
27309|Chandabooka Dacite|Age reasons|Carpentarian.|16-MAY-23
27309|Chandabooka Dacite|Comments|The Chandabooka Dacite might be equivalent in age to the Yardea Dacite, though probably ejected from different volcanic vents. The plagioclase phenocrysts are generally smaller (about 2-5 mm long) than in the Yardea Dacite.|16-MAY-23
3975|Childera Dacite|Name source|From Childera outstation, an outstation on Lake Everard station. Located on Childara 1:250 000 Sheet area. Lat 31o41' Long. 134o49'. A strongly welded crystal+vitric tuff of ashflow origin.|16-MAY-23
3975|Childera Dacite|Type section locality|At least 200 m of dark green to dark grey dacite exposed on Sketching Pile hill and on adjacent hills. Sketching Pile hilll is located on the Childara 1:250 000 Sheet area. Lat. 31o38'. Long. 134o51'. Base not exposed as is lowest unit in Glyde Hill Complex (Blissett). Top marked by a fine grained, white, airfall tuff.|16-MAY-23
3975|Childera Dacite|Extent|Unit is exposed over an area of 60 km2 in the central eastern portion of the Childara 1:250 000 Sheet area and over an area of 20 km2 in the extreme south-western portion of the Gairdner 1:250 000 Sheet area, near Taff's tank.|16-MAY-23
3975|Childera Dacite|Thickness range|At least 200 m.|16-MAY-23
3975|Childera Dacite|Lithology|In hand specimen is a dark green to dark grey aphanitic rock with rare scattered phenocrysts of plagioclase feldspar. The rare, medium grained phenocrysts are well oriented. In thin section is quite variable, but the altered, corroded, euhedral plagioclase feldspar phenocrysts sitting in an aphanitic groundmass is characteristic. Clinopyroxene (augite) occurring as numerous very fine grained euhedral phenocrysts is common, with occasional phenocrysts reaching 2 mm in diameter. White quartz phenocrysts are absent. Groundmass is variable, but most commonly it consists of an aphanitic devitrified mosaic with variable amounts of magnetite and chlorite, imparting a dark grey to dark green colour to the rock respectively. When the magnetite is oxidised to limonite a brownish tinge is imparted to the rock. Sometimes the groundmass consists of strongly oriented plagioclase laths of very fine grainsize interlocking with chlorite, magnetite and K feldspar. The proportion of plagioclase and clinopyroxene phenocrysts is roughly equal, the total phenocryst component making up from 2-10% of the rock.|16-MAY-23
3975|Childera Dacite|Relationships and boundaries|Oldest unit of Glyde Hill Complex (Blissett). Conformably overlain by Mangaroongah Dacite, but separated from this unit by a white airfall tuff bed and a zone of fused tuff.|16-MAY-23
3975|Childera Dacite|Age reasons|Roughly 1550 Ma - i.e. Carpentarian-based on geochronology and stratigraphic relationships.|16-MAY-23
3975|Childera Dacite|Defn author|Chris Giles 1977.|16-MAY-23
3975|Childera Dacite|References|Blissett, A.H., 1975. Rock units in Gawler Range Volcanics, South Australia. SA Dept Mines Quarterly Geological Notes 55|16-MAY-23
25843|Chinaman Gully Formation|Name source|From Chinaman Gully, a small cleft in the coastal cliffs of Gulf St. Vincent immediately north of the mouth of Aldinga Creek.|16-MAY-23
25843|Chinaman Gully Formation|Type section locality|In and around Chinaman Gully, along coast of Gulf St. Vincent.|16-MAY-23
25843|Chinaman Gully Formation|Extent|Eastern side of Cainozoic St. Vincent Basin, especially Willunga and Noarlunga Embayments. Also recognised in subsurface of Adelaide Plains.|16-MAY-23
25843|Chinaman Gully Formation|Thickness range|Up to 7 m thick in Willunga and Noarlunga Embayments. May be 12-13 m thick under the Adelaide City area.|16-MAY-23
25843|Chinaman Gully Formation|Lithology|Quartz and micaceous sands, silts, and clays, carbonaceous and pyritic in subsurface.|16-MAY-23
25843|Chinaman Gully Formation|Relationships and boundaries|Disconformably separated from Port Willunga Formation above and from Blanche Point Formation below. Lateral equivalent of Rogue Formation.|16-MAY-23
25843|Chinaman Gully Formation|Age reasons|Late Eocene|16-MAY-23
25843|Chinaman Gully Formation|Comments|The unit was originally called the Chinaman's Gully Beds by Reynolds. Redefinition was provided by Cooper (1979). Lindsay and Harris (1979) recognise a Tandanya Sand Member within the unit.|16-MAY-23
4023|Chitanilga Volcanic Complex|Name source|Chitanilga Hill, 2 km northwest of Kokatha H.S. (Gairdner 1:250 000 sheet (SH53-15)). Lat. 31o14'53"S; Long. 135o13'34"E.|16-MAY-23
4023|Chitanilga Volcanic Complex|Constituents|Pag5 Rhyodacite and rhyolite, Pac4 Andesite, Pac3 Basalt. ? Lake Gairdner Rhyolite equivalent (defined in this note) (Unconformity.) Pac1 basalt.|16-MAY-23
4023|Chitanilga Volcanic Complex|Type section locality|Unit Pac5. (Top) Reddish brown, purplish red, dark grey and pale greenish grey rhyodacite and rhyolite with small scattered potash feldspar phenocrysts. Some bands of dark grey to black obsidian with magnetite. Contorted flow- or compaction-banding. Probably includes lava flows and welded tuff. In the lower part is a flow of dark greenish grey andesite 20 m thick, (Pac4) exposed on the ridge 2 km east of Kokatha over a distance of 4 km north-south. Basalt about 15 m thick near the base of the unit is poorly exposed over a distance of 1.5 km on the lower slope of the ridge (Pac3). Total estimated thickness: 200 m.  ?Lake Gairdner Rhyolite equivalent (b) red and black rhyolite and rhyodacite lava flows, welded ash flow tuffs and agglomerates. Some beds of obsidian and air fall tuff. Estimated thickness 200 m. (a) Grey to black porphyritic welded ash flow tuff with fine-grained banded tuff at base. Estimated thickness 20 m (Unconformity).  Unit Pac2. Predominantly reddish brown and dark grey rhyodacitic welded ash flow tuff with small scattered potash feldspar phenocrysts, grading to rhyolite. Contorted flow- or compaction-banding. About 13 km northeast of Kokatha H.S. this unit is overlain by basalt exposed only over a few metres at the edge of an arm of Lake Harris. Estimated thickness: 250 m.  Unit Pac1: Dark bluish-grey and greenish-grey basalt in a succession of lava flows, the tops of which are vesicular. Several bands of rhyodacitic, dacitic and andesitic welded ash flows and air fall tuff (base not exposed). Estimated thickness: 350 m. |16-MAY-23
4023|Chitanilga Volcanic Complex|Extent|Kokatha area.|16-MAY-23
4023|Chitanilga Volcanic Complex|Relationships and boundaries|The upper rhyodacitic unit (Pac5) is overlain unconformably by the Chandabooka Dacite. The base of the Chitanilga Volcanic Complex is not exposed. Calc-silicate hornfels assigned to the Cleve Metamorphics crops out 500 m west of the outcrop of basalt (Pac1) in the lower part of the Gawler Range Volcanics so that the basalt probably rests unconformably upon the Cleve Metamorphics at Kokatha. Units Pac1 and Pac2 are intruded by the Hiltaba Granite (c.1500 m.y. BP.).|16-MAY-23
4023|Chitanilga Volcanic Complex|Age reasons|Carpentarian.|16-MAY-23
4023|Chitanilga Volcanic Complex|Comments|These rocks appear to be confined to the Kokatha district. Much of the area to the north, west and south is obscured by Quaternary deposits.|16-MAY-23
27375|Coober Pedy Paleosol|Name source|Coober Pedy township and/or Coober Pedy 1:250 000 map sheet.|16-MAY-23
27375|Coober Pedy Paleosol|Type section locality|Type locality - Black Flag Opal Field. 2.62 km south of Coober Pedy, 50 m to the west of the Stuart Highway.|16-MAY-23
27375|Coober Pedy Paleosol|Extent|Stuart Range and Uplands.|16-MAY-23
27375|Coober Pedy Paleosol|Thickness range|1-2 m, average 1 metre.|16-MAY-23
27375|Coober Pedy Paleosol|Lithology|A reddened indurated hard pan developed in the Giddinna Formation. A weak sheet calcrete is associated with it.|16-MAY-23
27375|Coober Pedy Paleosol|Relationships and boundaries|Developed in the upper part of the Giddinna Formation. Overlain sharply by the Benitos Clay (Benbow in prep.)|16-MAY-23
27375|Coober Pedy Paleosol|Age reasons|Late Pleistocene approx.|16-MAY-23
24225|Coolardie Formation|Name source|From Coolardie Park Homestead, about 8 km southeast of Lock, Tooligie 1:100 000 sheet, Eyre Peninsula, South Australia.|16-MAY-23
24225|Coolardie Formation|Type section locality|Typical Coolardie Formation occurs from 188 m to 369 m in SADME stratigraphic borehole Lock No. 1 (State No. 557000901) located on Kimba 1:250 000 sheet, Tooligie 1:100 000 sheet 57795E 6280085N, County Musgrave, Hundred Palkagee, adjacent Section 9. Eyre Peninsula, South Australia.|16-MAY-23
24225|Coolardie Formation|Thickness range|The thickest recorded sections of the Coolardie Formation are in Lock No. 1 and Polda No. 8 where thicknesses of 181 m and 108 m have been recognised respectively. Seismic refraction results from the Lock No. 1 site imply Precambrian basement at a depth of 650 m and a thickness of Late Palaeozoic sediments in the range of 480 m.|16-MAY-23
24225|Coolardie Formation|Lithology|The Coolardie Formation is composed principally of glacial and glacially-derived sediments. A thick succession of brown, grey, green and white coloured mudstones, siltstones and sandstones is most characteristic of the unit. Most horizons also contain assorted cobbles, pebble sand and smaller fragments of igneous, metamorphic and sedimentary origins.|16-MAY-23
24225|Coolardie Formation|Relationships and boundaries|It is presumed that the Coolardie Formation unconformably overlies either the ?mid-Proterozoic coarse-grained feldspathic sands, grits and conglomerates of the Blue Range Beds that are found at nearby Mt Wedge and Talia Caves (Flint and Parker 1981) or ?Precambrian granite similar to that described from the Bramfield area (Harris and Foster 1974). However the base of the formation has not yet been penetrated by SADME drilling. The Coolardie Formation is unconformably overlain by the Late Jurassic Polda Formation, a unit of sand, silt and lignite.|16-MAY-23
24225|Coolardie Formation|Age reasons|The Coolardie Formation contains microfloras, which may be compared with the Stage 2 assemblage of Evans (1969) and Kemp et al. (1977). Unpublished work by Norvik quoted in Kemp et al. (1977, p.189) suggests that this assemblage is correlated with his Upper Stage 2 due to the occurrence of the trilete spores Microbaculispora tentula, Apiculatisporis cornutus (Balme and Hennelly) Hoeg and Bose and Punctatisporites gretensis. The absence of Verrucosisporites pseudoreticulatus Balme and Hennelly mitigates against correlation with Stage 3. This microfloral assemb lage enables the Coolardie Formation to be correlated with the lower Tamarian stage in the Permo-Carboniferous (Rekunian) succession of Tasmania (Clark and Farmer 1976; Truswell, 1978). On current knowledge this interval is best correlated with latest Carboniferous on the international scale (Balme, 1980). Locally the Coolardie Formation is correlated with the Cape Jervis Beds in the Troubridge Basin and the Boorthanna and basal Stuart Range Formations in the Arckaringa Basin (Cooper, 1981).|16-MAY-23
26491|Coomb Spring Formation|Name source|Coomb Spring on Lake Tarkarooloo, north of Coomb Bore on Curnamona 1:250 000 Map Sheet, Benagerie 1:100 000 Sheet 6935. First used in Callen et al. (1983).|16-MAY-23
26491|Coomb Spring Formation|Type section locality|SW shore of Lake Millyera at Lat. 31o02'59", Long. 139o56'36". Section 5 of Callen & Tedford (1976) and Callen et al. (1983 in press). See Fig. 2.|16-MAY-23
26491|Coomb Spring Formation|Extent|Lake Millyera, Northern L. Tarkarooloo.|16-MAY-23
26491|Coomb Spring Formation|Thickness range|6-7 m.|16-MAY-23
26491|Coomb Spring Formation|Lithology|Interbedded gypseous greenish, laminated clay, greenish yellow fine sand, with non-marine gastropods, ostracods, eggshell, charophytes and fish bones. Intertongues with fine red sands containing calcareous palaeosol horizons (not present at type section). These overlie with sharp contact, greenish sands with rippled 'sedimentary' gypsum laminae, and sandy clay grading down to gravel.|16-MAY-23
26491|Coomb Spring Formation|Relationships and boundaries|Formerly part of the Millyera Formation. At type section - top is eroded and marked by a well-developed soil profile containing gypsum nodules, in green clay. Usually unconformably overlain by Eurinilla Formation or Coonarbine Formation. Overlies Millyera Formation or is unconformable upon Namba Formation. See comments on redefinition of Millyera Fm.|16-MAY-23
26491|Coomb Spring Formation|Age reasons|From relationships to Namba Fm. and Eurinilla Formation, age could range over all or any part of Late Miocene to Middle Pleistocene. The Millyera Formation has normal magnetic polarity, and is thought to be Bruhne. Dates on shell in the Coomb Spring Fm are given in Callen et al and shown above. They suggest an age beyond the limit of radiocarbon dating. Estimates by Callen et al suggest the age of the unit is likely to be at least 95 000 years old|16-MAY-23
26491|Coomb Spring Formation|Name first published by|Callen R.A., Tedford R.H. 79/00723|16-MAY-23
24226|Coominaree Dolomite|Name source|Coominaree Mine situated 7 km northwest of Nilpinna H.S. in the Peake and Denison Ranges; Warrina 1:100 000 sheet area, Warrina 1:250 000 sheet area; metric reference is 6852300, 596080.|16-MAY-23
24226|Coominaree Dolomite|Type section locality|Occurs in a lower Adelaidean succession on the northern margin of the Coominaree Mine Block (Lower Proterozoic); totals 77 metres in thickness; metric reference is 6853300, 596600. The unit was first described by Thomson (1966).|16-MAY-23
24226|Coominaree Dolomite|Extent|Small outcrops occur 3 km south of War Loan Mine and 1.2 km north of Coominaree Mine on the eastern margin of Margaret Inlier in the Peake and Denison Ranges.|16-MAY-23
24226|Coominaree Dolomite|Thickness range|Variable up to 77 metres.|16-MAY-23
24226|Coominaree Dolomite|Lithology|The lower part of the unit consists of interbedded buff and pale brown dolomites with minor sandstones and pebbly layers; low angle crossbedding is common. The upper part of the unit consists of a non stromatolitic dolomite, oolitic at the base, and an overlying stromatolitic unit.|16-MAY-23
24226|Coominaree Dolomite|Relationships and boundaries|A lenticular unit conformably overlying the Younghusband Conglomerate and in turn, conformably overlain by the Cadlareena Volcanics (Ambrose and Flint, in prep.).|16-MAY-23
24226|Coominaree Dolomite|Age reasons|Lower Adelaidian-Callanna Beds (Willouran); contains stromatolite types Acaciella c.f. australica and Gymnosolen c.f. ramsayi (Preiss, 1973). In the Mount Painter Province the Wywyana Formation (Lower Callanna Beds) is a carbonate rich unit considered equivalent to the Coominaree Dolomite (Coats, 1971).|16-MAY-23
24226|Coominaree Dolomite|Proposed publication|Rep. Invest., geol. Surv. S. Aust.|16-MAY-23
24226|Coominaree Dolomite|References|01/31599; 79/00849;|16-MAY-23
24227|Cooranna Formation|Name source| Cooranna Bore, 24 km NW of 'Callanna'.|16-MAY-23
24227|Cooranna Formation|Unit history|Cooranna Formation' of Murrell (1977). Probably BS1 and BS2 units of Rowlands et al. (1980, p.61).|16-MAY-23
24227|Cooranna Formation|Type section locality|Rounded hills 2 km WSW of the Boorloo workings; lat. 29o45', long. 137o58'.|16-MAY-23
24227|Cooranna Formation|Extent|Willouran Ranges.|16-MAY-23
24227|Cooranna Formation|Thickness range|781 m in the type section.|16-MAY-23
24227|Cooranna Formation|Lithology|Top: 94 m fine-grained sandstone and siltstone, partly dolomitic, grey-green, brownish, thin bedded, fine cross-bedding, lenticular bedding, halite and ?gypsum casts.  135 m interbedded fine sandstone, siltstone and dolomite-sandstone, pale grey, pale brownish, light greenish grey, thin bedded, lenticular bedding, halite, shortite and gypsum casts, mud cracks; siltstone, partly dolomitic, light brown-grey, pale blue-grey, olive-grey; dolomite, partly sandy, cherty, light brown-grey, weathering yellowish orange, medium bedded.  96 m interbedded calcitic carbonates, siltstone, fine sandstone, similar to the above; shortite pseudomorphs.  68 m sandstone and siltstone, greyish, weathering brownish, greenish grey, flaggy, mud cracks, halite casts.  41 m siltstone, greyish.  202 m interbedded calcitic and dolomitic carbonates, siltstone and sandstoane, grey, green-=grey, light brown, light yellowish, thin to medium bedded, some wavy, slump and convolute bedding, fine cross-lamination, mud cracks, halite and gypsum casts, micaceous porphyroblasts and shortite pseudomorphs.  95 m limestone and dolomite, partly cherty, yellow-brown; sandstoane, light brownish, greenish grey, fine grained, flaggy, mud cracks, ripple marks, halite and ?gypsum casts. 47 m sandstone and quartzite, light grey, brown or greenish, partly calcitic, fine grained with lenses of medium-grained sandstone; halite casts in darker weathering lower part.  Base: 4 m quartzite, beds up to 13 cm, mud cracks, ripple marks. Overall sand:shale:carbonate percentages 43:36:21. Rowlands et al. (1980) report shortite pseudomorphs and cauliflower chert in this sequence.|16-MAY-23
24227|Cooranna Formation|Relationships and boundaries|Lies conformably between Hogan Dolomite and Boorloo Siltstone.|16-MAY-23
24227|Cooranna Formation|Identifying features|A thick sequence of mixed lithology lying between the more distinctive Hogan Dolomite and Boorloo Siltstone.|16-MAY-23
24227|Cooranna Formation|Age reasons|Possibly late Willouran.  May be partly equivalent to Duff Creek Beds of the Peake and Denison region (Ambrose et al., 1981), and perhaps to part of the Arkaba Hill Beds (Mount, 1980) of the Arkaba Diapir and Worumba Anticline.|16-MAY-23
4658|Cootanoorina Formation|Name source|Cootanoorina 1 well. Lat. 28o00.5'S Long. 135o20'E where it was first intersected.|16-MAY-23
4658|Cootanoorina Formation|Unit history|Possibly correlates with unnamed Devonian sediments in the Officer Basin.|16-MAY-23
4658|Cootanoorina Formation|Type section locality|Weedina 1 well at Lat. 28o28'31"S Long. 135o59'20"E between 726.3 and 1624.3 metres.|16-MAY-23
4658|Cootanoorina Formation|Extent|Central part of Boorthanna Trough and possibly the Wintinna anomaly first intersected in Mt Willoughby 1 (Townsend 1973/75)|16-MAY-23
4658|Cootanoorina Formation|Thickness range|898 m in Weedina 1 is the thickest intersection.|16-MAY-23
4658|Cootanoorina Formation|Lithology|The unit consists of grey dolomite and anhydrite (pink) interbedded with massive dolomitic sandstones. It is more sandy in the upper part and more dolomitic in the lower.|16-MAY-23
4658|Cootanoorina Formation|Relationships and boundaries|The Cootanoorina Formation unconformably overlies crystalline basement or ?Ordovician unnamed quartzites and is unconformably overlain by the Boorthanna Formation (Townsend & Ludbrook 1975).|16-MAY-23
4658|Cootanoorina Formation|Age reasons|Harris (in Allchurch et al 1973) tentatively dated the Cootanoorina Formation as (?) Devonian.|16-MAY-23
28474|Cooyerdoo Granite|Name source|Cooyerdoo Homestead.  Grid reference 695200 mE, 6362750 mN, GDA94. Nearest town: Iron Knob.|16-MAY-23
28474|Cooyerdoo Granite|Unit history|The previous use of the name Cooyerdoo Granite [Strat ID 28474] is in Flint, R.B. , Parker, A.J. , Fanning, C.M. 1985 'Geology', in Twidale C.R., Tyler M.J., Davies M.(eds) - Natural history of Eyre Peninsula. Royal Society of South Australia 1v p 34, where the Cooyerdoo Granite is described as a member of the Moody Suite.  I believe the authors are referring to the same rock but do not describe it in any detail. the name has also been published informally as Cooyerdoo granite in:  Anthony J Reid, Stacey O McAvaney, and Geoff L Fraser, 2008. Nature of the Kimban Orogeny across northern Eyre Peninsula. MESA Journal 51: 25-34|16-MAY-23
28474|Cooyerdoo Granite|Type section locality|Type locality: a 100m-diameter circle centred on 701050mE 6363550mN GDA94 Zone 53, ~4.5 km ESE of Cooyerdoo Hill near the boundary between Cooyerdoo and Katunga Stations, PORT AUGUSTA 1:250 000 sheet, Roopena 6332 1:100 000 sheet.|16-MAY-23
28474|Cooyerdoo Granite|Extent|Outcrop exposure over ~ 120 km2 east of the northern Middleback Ranges, NE Eyre Peninsula, Roopena 1:100 000 map sheet.  The granite defines a magnetic and gravity low which is interpreted to extend ~ 30 km further south beneath the southern Middleback Range on the Middleback 1:100 000 map sheet|16-MAY-23
28474|Cooyerdoo Granite|Lithology|The Cooyerdoo Granite is a medium grained granite composed of potassium feldspar, plagioclase, quartz, biotite and minor opaques.  It contains a sporadically developed weak lineation and foliation defined by quartz ribbons wrapping feldspar augen.  It contains feldspar and quartz rich leucocratic bands and biotite rich schlieren often elongate parallel to the fabric.  It also contains granodioritic compositional banding which is shallowly dipping.|16-MAY-23
28474|Cooyerdoo Granite|Relationships and boundaries|The relationship between the Cooyerdoo and adjacent rocks is unclear, as contacts are very rarely exposed.  A deformed granite believed to be Cooyerdoo Granite is in sheared contact with an amphibolite and Hutchison Group sediments on the eastern side of the Iron Baron Mine.  The granite is crosscut by undeformed aplite and pegmatite dykes of unknown age.  The granite contains foliated dolerite bodies which are orientated parallel to the foliation.|16-MAY-23
28474|Cooyerdoo Granite|Age reasons|Mesoarchaean.  Crystallisation age ~3157±2 Ma [Fraser, G; McAvaney, S.; Neumann, N.; Szpunar, M. and Reid, A. (in press 2010) Early Mesoarchean crust in the eastern Gawler Craton, South Australia, Precambrian Research.|16-MAY-23
28474|Cooyerdoo Granite|Defn author|McAveney, Stacey (PIRSA), January 2010|16-MAY-23
28474|Cooyerdoo Granite|Proposed publication|Fraser, G; McAvaney, S.; Neumann, N.; Szpunar, M. and Reid, A. (in press) Early Mesoarchean crust in the eastern Gawler Craton, South Australia, Precambrian Research|16-MAY-23
28474|Cooyerdoo Granite|References|Flint, R.B. , Parker, A.J. , Fanning, C.M. 1985 'Geology', in Twidale C.R., Tyler M.J., Davies M.(eds) - Natural history of Eyre Peninsula. Royal Society of South Australia 1v p 34Anthony J Reid, Stacey O McAvaney, and Geoff L Fraser, 2008. Nature of the Kimban Orogeny across northern Eyre Peninsula. MESA Journal 51: 25-34|16-MAY-23
24236|Curdimurka Subgroup|Name source|Curdimurka railway siding (disused).|16-MAY-23
24236|Curdimurka Subgroup|Type section locality|From a point 6 km SSE of 'Callanna' northeasterly to a point 1 km W of Boorloo workings; lat. 29o46', long. 137o56' to lat. 29o45', long. 137o58'.|16-MAY-23
24236|Curdimurka Subgroup|Thickness range|4700 m in the reference section.|16-MAY-23
24236|Curdimurka Subgroup|Identifying features|This is proposed to refer to the upper part of the Callanna Group in the Curdimurka region, a little-disturbed, partly evaporitic sequence from Dome Sandstone to Boorloo Siltstone.  |16-MAY-23
25688|Dalhousie Formation|Name source|Dalhousie Springs; grid reference 548072 approx; Dalhousie 1:250 000 Sheet area, AGM.|16-MAY-23
25688|Dalhousie Formation|Type section locality|Approx. 4 m dolomitic limestone in cliff section beside track at grid reference 546074.|16-MAY-23
25688|Dalhousie Formation|Extent|The unit occurs over approx. 70 km2 immediately around the Dalhousie Springs area in the west-central part of Dalhousie 1:250 000 Sheet area.|16-MAY-23
25688|Dalhousie Formation|Thickness range|Up to 8 metres.|16-MAY-23
25688|Dalhousie Formation|Lithology|Hard, dense, pale grey or cream dolomitic limestone overlying drab grey-green unstructured clay with scattered grey silcrete granules locally in basal beds.|16-MAY-23
25688|Dalhousie Formation|Relationships and boundaries|Upper boundary is ground surface. Lower boundary - unit overlies Bulldog Shale and Oodnadatta Formation with very low angular unconformity perceived from map unit distribution and not locally observable.|16-MAY-23
25688|Dalhousie Formation|Age reasons|No fossils have been recovered. Age indirectly estimated as Pleistocene from tectonic development of Dalhousie Anticline.|16-MAY-23
25688|Dalhousie Formation|Comments|Unit is interpreted as a lake deposit, the lake having formed by the pooling of local spring discharge.|16-MAY-23
24241|Delisser Formation|Name source|Delisser 1:63 360 map sheet of Tallaringa 1:250 000.|16-MAY-23
24241|Delisser Formation|Type section locality|Western-most Wilkinson Lakes, Tallaringa 1:250 000 map sheet. Lat. 29o41'49"S  Long. 132o24'00"E.|16-MAY-23
24241|Delisser Formation|Extent|Eastern Great Victoria Desert and margins.|16-MAY-23
24241|Delisser Formation|Thickness range|Average approximately 2 metre.|16-MAY-23
24241|Delisser Formation|Lithology|Sandstone, red brown. May be clayey in part, moderately well sorted. Little in the way of sedimentary structure preserved. Moderately indurated.|16-MAY-23
24241|Delisser Formation|Relationships and boundaries|Overlain by the Wintrena Formation (Benbow, in prep.). Underlain by the Garford Formation (Benbow and Pitt 1978) and red prismatic clays (Benbow, in prep.).|16-MAY-23
24241|Delisser Formation|Age reasons|Equivalent to Willawortina Formation on FROME (Callen and Tedford 1976). Considered to be approximately Lower Pleistocene.|16-MAY-23
24241|Delisser Formation|Proposed publication|Explanatory Notes Tallaringa 1:250 000 map sheet. Geol. Surv. S. Aust.|16-MAY-23
24247|Dome Sandstone|Name source|The Dome (Dome Hill), 3 km SSE of 'Callanna' station.|16-MAY-23
24247|Dome Sandstone|Type section locality|NE-dipping sandstone sequence forming low ridges 3 km SW of 'Callanna'.  From lat. 29o44', long. 137o52' to lat. 29o43', long. 137o52' (Fig. 1A).|16-MAY-23
24247|Dome Sandstone|Extent|Willouran Ranges.|16-MAY-23
24247|Dome Sandstone|Thickness range|At least 1480 m in type section. Thinner to the SE.|16-MAY-23
24247|Dome Sandstone|Lithology|Top: 79 m quartzite, very light grey, medium grained, minor black lamination, poorly exposed on low ridge.  390 m (partly covered intervals) similar quartzite and sandstone, fine to coarse grained, medium to thin bedded, with some cross-bedding, shale clasts (halite casts reported nearby by Murrell, 1977).  584 m sandstone and quartzite, mainly white weathering and coarse grained with channel cross-beds and pebbly and black hematitic layers (Whitehead, 1980; Collins, 1980).  Base: at least 300-450 m siltstone and shale, grey and light greenish; sandstone, partly calcitic or dolomitic, fine to coarse grained, thin to medium bedded with some black lamination, current bedding, mud cracks, ripple marks. Overall sand:shale:carbonate percentages - 87:12:1.|16-MAY-23
24247|Dome Sandstone|Relationships and boundaries|In type section and generally elsewhere - lower boundary faulted against megabreccia, upper boundary conformable against Rook Tuff.|16-MAY-23
24247|Dome Sandstone|Identifying features|Prominent basal sandstone-siltstone sequence of the Curdimurka Subgroup.  |16-MAY-23
24247|Dome Sandstone|Age reasons|Possibly late Willouran.|16-MAY-23
24247|Dome Sandstone|Proposed publication|Q. Geol. Notes, Geol. Surv. S. Aust. 79: 7-16.|16-MAY-23
24255|Dullingari Group|Name source|Dullingari Waterhose: Lat. 28o0'00"S, Long. 140o35'30"E.|16-MAY-23
24255|Dullingari Group|Type section locality|A single type section is not possible, but the most typical section occurs in Dullingari-1 over the interval 2758 m to 3532 m. Probable equivalents of this unit can be found in Nappacoongee-1, Moomba-2, Poolawanna-1, Mudrangie-1, Putamurdie-1, Pandieburra-1 and many others. Dullingari-1 location 28o07'55.6"S, 140o52'30"E.|16-MAY-23
24255|Dullingari Group|Extent|This subsurface unit or its equivalent occurs throughout the Warburton Basin in many drillholes.|16-MAY-23
24255|Dullingari Group|Thickness range|Unknown, in the type section it is at least 774 m (drilled) thick.|16-MAY-23
24255|Dullingari Group|Lithology|The type section is dominantly a shale section, with minor siltstone; pyrite is a major accessory mineral with dolomite and calcite. At Daralingie-1 sandstone containing glauconite? and lithic grains was intersected and at Daralingie-2 shale with interbedded sandstone occurs. All lithologies are characterised by a high degree of induration, most probably to the zeolite facies of metamorphism. Cleavage and fractures occur as two sets, one at about 70o and perpendicular to each other, and one at about 15o.|16-MAY-23
24255|Dullingari Group|Relationships and boundaries|Overlies the Kalladeina Fmn with possible conformity at Coongie-1 and is overlain by Permo-Carboniferous rocks of the Cooper Basin with unconformity. At Coongie-1 the sandstone is partly silicified and is underlain by oosparite of Late Cambrian age.|16-MAY-23
24255|Dullingari Group|Age reasons|At Dullingari-1 diplograptid graptolites in core 26 indicate a Middle to early Late Ordovician age, uniserial graptolites in cores 30 and 31 indicate an Early Ordovician age (Opik and Jones, 1962). Pandieburra-1 core 9 contains "graptolite remains which indicate Lower to Middle Ordovician age" (Daily, 1963). At Coongie-1 Core 4 contains as asaphid tribolite (Daily, 1970) which may range from Late Cambrian to Late Ordovician.|16-MAY-23
24255|Dullingari Group|Proposed publication|Q. geol Notes, Geol. Surv. S. Aust 86; March 1983|16-MAY-23
25887|Dunns Mine Limestone|Name source|Dunns Mine, 6 km SE of The Dome.|16-MAY-23
25887|Dunns Mine Limestone|Unit history|Dunns Mine Formation' of Murrell (1977). Probably unit R3.2-4 of Rowlands et al. (1980, p.62)|16-MAY-23
25887|Dunns Mine Limestone|Type section locality|Ridges forming main divide 3 km SSE of The Dome; lat 29o46', long. 137o56'.|16-MAY-23
25887|Dunns Mine Limestone|Extent|Willouran Ranges.|16-MAY-23
25887|Dunns Mine Limestone|Thickness range|334 m in type section, but less than 50 m to SE.|16-MAY-23
25887|Dunns Mine Limestone|Lithology|Lithological sequence in type section: Top: 26 m limestone, partly sandy, cherty, medium grey, beds up to 15 cm (Collins, 1980). 86 m limestone with sandstone and quartzite interbeds; light to dark grey, with scapolite-like, chlorite porphyroblasts; thin to medium bedded.  101 m sandstone (partly carbonate rich) and carbonate (partly sandy) with minor sedimentary carbonate breccia, thin to medium bedded; limestone with shortite pseudomorphs and chlorite.  16 m shale, light and medium grey, thin bedded.  68 m limestone, partly sandy and quartzite, mainly thin bedded.  Base: 37 m quartzite, carbonate rich, light brownish; thin to medium bedded; some platy, light medium grey carbonate. Rowlands et al. (1980) reported shortite (Na2Ca2(CO3) moulds and cauliflower chert (after evaporitic anhydrite nodules). Overall sand: shale: carbonate percentages - 36:5:59.|16-MAY-23
25887|Dunns Mine Limestone|Relationships and boundaries|Lies conformably between Rook Tuff and Recovery Formation, with intervention of megabreccia between top and base of Recovery.|16-MAY-23
25887|Dunns Mine Limestone|Identifying features|Prominent, ridge-forming sandy carbonate sequence below the more silty Recovery Formation.  |16-MAY-23
25887|Dunns Mine Limestone|Age reasons|Possibly late Willouran; may be equivalent to Rockwater Beds of the Peake and Denison Ranges (Ambrose et al., 1981, p.31)  and possibly to the Wirrawilka Beds of the Worumba Anticline (Preiss, 1980).|16-MAY-23
25887|Dunns Mine Limestone|Proposed publication|Q. Geol. Note, Geol. Surv. S. Aust. 79: 7-16.|16-MAY-23
25895|Emeroo Subgroup|Name source|Emeroo Range, southwest Flinders Ranges.|16-MAY-23
25895|Emeroo Subgroup|Type section locality|East of 'Emeroo' H.S., Emeroo Range.|16-MAY-23
25895|Emeroo Subgroup|Thickness range|1300 m|16-MAY-23
25895|Emeroo Subgroup|Identifying features|Emeroo Subgroup (upgraded from Emeroo Quartzite) is proposed for the basal arenaceous sequence of the Burra Group, and corresponds to Mawson's (1947) 'Emeroo Range basal rudaceous and arenaceous sediments'. |16-MAY-23
25895|Emeroo Subgroup|References|01/31600|16-MAY-23
27149|Eregunda Sandstone Member|Name source|Eregunda Creek' which dissects the sequence at Lat. 31o07'05"S, Long. 138o52'37"E.|16-MAY-23
27149|Eregunda Sandstone Member|Type section locality|107 m of red sandstone with minor shale and siltstone interbeds, exposed in an area of undulatory topography 2.5 km north of Ten Mile Creek, from Lat. 31o15'42"S, Long. 138o50'07"E (bottom) to Lat. 31o15'42"S, Long. 138o50'12"E (top).|16-MAY-23
27149|Eregunda Sandstone Member|Extent|The unit is exposed over approximately 20 km2 in the central Flinders Ranges (along the Heysen Range, between Wirrealpa and the Ten Mile Creek and near Mount Frome), on the Parachilna 1:250 000 Geological Sheet (SH54-13). It also outcrops over approximately 6 km2 in the Mount Scott Range, on the western portion of the Copley 1:250 000 Geological Sheet (SH54-9).|16-MAY-23
27149|Eregunda Sandstone Member|Thickness range|Range 40-165 metres|16-MAY-23
27149|Eregunda Sandstone Member|Lithology|Fine-grained red micaceous arkose, with minor shale and siltstone interbeds. Poorly bedded to horizontally laminated, with minor tabular and rare trough cross-stratification.|16-MAY-23
27149|Eregunda Sandstone Member|Relationships and boundaries|Upper member of the Billy Creek Formation in the central Flinders Ranges and at Mount Scott. Red micaceous sandstones of the Eregunda Sandstone Member rest sharply but conformably on shales and siltstones of the Nildottie Siltstone Member. The unit is overlain conformably by the Wirrealpa Limestone in the central Flinders Ranges, and by the Wirrealpa Limestone at Mount Scortt (Youngs, 1977).|16-MAY-23
27149|Eregunda Sandstone Member|Age reasons|The Lower-Middle Cambrian boundary occurs at an undefined position in the upper portion of the Billy Creek Formation (Daily, 1956). It is likely therefore that the Eregunda Sandstone Member is largely, if not entirely, early Middle Cambrian in age.|16-MAY-23
24637|Fulham Sand|Name source|Following Firman (1966), unit named after Adelaide suburb of Fulham; Grid reference 613172727, Adelaide 6628-III, 1:50 000 Sheet, Zone 54.|16-MAY-23
24637|Fulham Sand|Unit history|Fulham Sand has been informally referred to as the "Older Sand Dunes" by Fenner (1927) and Miles (1952), and the "Osborne Association" by Aitchison et al. (1954).|16-MAY-23
24637|Fulham Sand|Type section locality|None readily accessible; none described by Firman (1966). Reference section: 2.95 metres of fine, very well sorted quartz sand, colour 5YR 4/8 (yellowish red); intersected in cored hole GH36 (SADME Core Library number 662800301060) by Metro-Adelaide Soil Investigations. Site: small reserve off Telford St, Findon, Section 428, Hundred of Yatala, (grid ref. 73883460, Sheet 6628-41, 1:10 000 Series, SA Lands Department).|16-MAY-23
24637|Fulham Sand|Extent|The unit is exposed as irregular dunes on the southern Adelaide Plains between Somerton Park (south) and Port Adelaide (north), and from 1 to 4 km inland from the present coast line. The areal extent is about 60 square kilometres.|16-MAY-23
24637|Fulham Sand|Thickness range|Range 0-15 metres.|16-MAY-23
24637|Fulham Sand|Lithology|Sand, quartzose, fine well-sorted, mean size range 250-177 micron (2.00-2.50 phi units, standard deviation 0.50 and 0.7 phi). Grain size distribution is slightly negatively to slightly positively skewed, kurtosis (k = 0.6 to 2.0) ranging from mesokurtic to leptokurtic. Sand upper portions generally affected by pedogenic process. Mineralogy: 98% quartz, minor lithics (feldspars, ferro-magnesians, garnet, silimanite) after Cornelius & Stevens (1945) and Aitchison et al. (1954). Sand grains moderately well rounded, frosted and irregularly coated with clay and iron oxides.|16-MAY-23
24637|Fulham Sand|Depositional environment|Aeolian, based on granulometric character, unit-morphology, distribution, topography, stratigraphy. Sub-coastal location and morphology suggest dunes are a reworked pre Holocene coastal sand barrier. Sand source probably Adelaide Plains ephemeral streams.|16-MAY-23
24637|Fulham Sand|Relationships and boundaries|Overlies Glanville Fm (Firman, 1966, Cann, 1978) and Pooraka Fm (Daily et al., 1976) and various "Quaternary alluvium" deposits. It is unconfined except where overlain by various anthropogenic deposits.|16-MAY-23
24637|Fulham Sand|Age reasons|Late Pleistocene. Fulham sand is unfossiliferous, it overlies the Glanville Fm (last Interglacial in Age, 110 KA, Belperio et al., 1984), it also overlies Pooraka Fm (35 KA, Williams, 1969; 20-30 KA Belperio & Bateman, 1986). It is stratigraphically overlain by St Kilda Fm., Holocene (7 KA, Bowman & Harvey, 1986). Probable Age 16-20 KA, Fulham Sand dunes were likely initiated during aeolian landscape instability during last Glacial - recognised by Belperio et al. (1983, 84).|16-MAY-23
24637|Fulham Sand|Proposed publication|Quarterly Geological Notes. Geol. Surv. S. Aust., 106; 7-15|16-MAY-23
24637|Fulham Sand|Comments|Fulham Sand does not overly the St Kilda Formation as originally described by Firman (1966) and later by Daily et al. (1976). Landscaping, Sand mining, market gardening, residential and Industrial development, have combined to alter the thickness and extent of Fulham Sand.|16-MAY-23
24637|Fulham Sand|References|01/31603; 79/00747; 86/25056; 01/31602; 86/25351; 01/31601; 01/31604|16-MAY-23
24637|Fulham Sand|Resdate|06-SEP-1988|16-MAY-23
24637|Fulham Sand|Reserved? Yes/No|Yes|16-MAY-23
25918|Garford Formation|Name source|The name is taken from 'Garford' Outstation, on the Commonwealth Hill pastoral lease. 'Garford' is situated on the northern flanks of the Garford Palaeochannel, within which the formation is best developed.|16-MAY-23
25918|Garford Formation|Type section locality|In the absence of suitable exposures, a composite type section is used to define the Garford Formation combining drillhole TPS4 (lat. 29o38'50"S, long. 133o32'25"E) with nearby exposed section, 400 m to the north (Figs. 1 and 5). Both top and bottom boundaries, and the dominant lithologies of the formation, may be observed in this composite section. Drillhole TPS 12 (lat. 29o35'40"S, long. 133o42'30"E) intersected a range of lithologies most typical of the Garford Formation and is taken as the principal reference section (Figs. 1 and 5).  Composite Type Section:  Base of Section - Padinga Formation Clayey, olive to greyish-green or dull yellow, fine to very fine-grained, subangular to subrounded, quartz sand with occaisonal quartz granules. Garford Formation. Unit 1 yellow-grey clay containing rounded granule-sized clasts of lighter coloured clay. Unit 2 White, weakly calcareous to dolomitic clay with scattered coarse subangular to angular quartz grains, manganese staining and worm burrows and minor interbedded light green pearly-lustred clay. Unit 3 As above, with a few percent of fine to very fine-grained quartz grains. Unit 4 Grey sandy limestone to calcareous sandstone, with subangular medium to very coarse-sized gains. Wintrena Beds Gypseous sand and silts, with carbonate nodules.Top of section.  PRINCIPAL REFERENCE SECTION: Base of section: Pidinga Formation medium to fine-grained sands with subangular to angular quartz and 1-2 percent granule-sized subrounded quartz grains. Sharp contact with overlying clays. Garford Formation   Unit 1 Compact green and grey clay with 1-4 percent subangular to rounded quartz sand; yellow to red alternation colours.  Unit 2 White calcareous clay occasional subrounded coarse-grained quartz grains.  Unit 3 Green, pearly-lustred clays.  Unit 4 Green sandy clays with quartz up to very coarse-grained.  Unit 5 White calcaraeous clays, with manganese staining, worm tubes and 1-2 percent of fine to medium-grained quartz grains.   Wintrena Beds Red, calcareous, clayey, medium-grained poorly-sorted sands with nodular calcrete developed at places. Basal part contains dolomite clasts from underlying unit. Holocene sands Modern aeolian sand spreads.  Top of Section|16-MAY-23
25918|Garford Formation|Extent|The Garford Formation essentially occupies the Tallaringa Palaeodrainage System and portions of a topographic depression southwest of Coober Pedy, centred on Lake Phillipson (Fig. 4). Specifically, the green and white clays have been recorded in the Tallaringa Palaeochannel between WL 5 and Tallaringa Well (represented by outcrops of high-grade sepiolite clay in 'R.S. Lake'). Both north and south of this zone, the unit has been removed by post-Miocene erosion; south of WL 5, the Pidinga Formation subcrops beneath dune sands. In the Garford Palaeochannel, clays infilling the channel, overlie Pidinga Formation, from TPS14 to TPS3 (Fig. 4). Continuity is interrupted by 'bars' of weathered and/or fresh crystalline basement, exposed by post-Garford erosion. Limestone (and interbedded clays) in the upper part of the preserved Garford Formation are exposed on the southern margin of the channel near TPS5 and 4 southwest of Wallira 2, and near Wallira 1, Lake Phillipson and Mickey's Swamp.|16-MAY-23
25918|Garford Formation|Lithology|The dominant lithologies of exposures, seen in many of the claypans of the Garford Palaeochannel, consist of white, generally calcareous clays (dolomitic in part), with lesser green pearly-lustred palygorskitic, or rarely sepiolitic clays. The white clays are dense, and when dry, break with a splintery fracture. The green clays, usually non-calcareous, often contain 1-2 mm sized, well-rounded to angular grains of blue to milky quartz, and rare 1-5 mm sized, well-rounded clasts of cream-coloured silcrete. Both types of clay may be sandy, particulalry at the top and bottom of the unit, and thin sand lenses may be present. A thin, but relatively widespread dolomitic limestone (Fig. 4) forms the top of the formation.|16-MAY-23
25918|Garford Formation|Relationships and boundaries|The Garford Formation is underlain by sands and lignites of the Eocene Pidinga Formation. Intersections in TPS4 and TPS6, shown in figure 2, suggest this contact is unconformable. Despite this, the contact is generally not sharp, probably owing to the lack of lithifaction and consequent ease of reworking of the underlying unit. In the Lake Phillipson area, the Garford Formation overlies still older units. Its upper contact is likewise erosional and gradational with the overlying Wintrena Beds of late Tertiary to Quaternary age. An intertonguing relationship between Garford Formation and interpreted Mount Sarah Sandstone has been described above. On the basis of the distinctive lithology and dolomite-palygorskite-sepiolite clay mineralogy that the Garford Formation has in common with the Etadunna and Namba Formations of the Lake Eyre and Tarkarooloo Basins (Callen and Tedford, 1976), it is considered to be a  time and rock-correlative thereof.  The unit is, however, given a new name as its sediments were deposited in a basin distinct from those in which the Etadunna and Namba Formations were deposited.  The observation of units and lithologies identical to the Mount Sarah Sandstone, Mirackina Conglomerate and Garford Formation, interlayered within Etadunna Formation limestone and clays at Billa Kalina (G.J. Ambrose, SADME, pers. comm.) supports the suggestion of stratigraphic equivalence and essential contemporaneity of all four units.|16-MAY-23
25918|Garford Formation|Age reasons|An early to mid-Miocene age has been established for sediments within the Namba Formation (Callen and Tedford, 1976). Preliminary searches for vertebrate fossils in the Garford Formation and for microfossils within drill core have been unsuccessful. Despite this, correlations with the Namba and Etadunna Formations are considered strong enough to suggest a Miocene or, at least, mid-Tertiary, age for the Garford Formation.|16-MAY-23
7059|Gawler Range Volcanics|Name source|Gawler Ranges, northern Eyre Peninsula, South Australia.|16-MAY-23
7059|Gawler Range Volcanics|Constituents|Yardea Dacite, Chandabooka Dacite, Lake Gardner Rhyolite, Chitanilga Volcanic Complex, Glyde Hill Volcanic Complex, Wheepool Rhyolite, Yandoolka Rhyolite.|16-MAY-23
7059|Gawler Range Volcanics|Extent|The volcanics extend over at least 25 000 km2 in the region covered by the Gairdner (SH53-15), Childara (SH53-14), Yardea (SI53-3) and Port Augusta (SI53-4) 1:250 000 sheets. Scattered masses in the Tarcoola (SH53-10) and Streaky Bay (SI53-2) 1:250 000 sheet areas may be erosional remnants of the Gawler Range Volcanics.|16-MAY-23
7059|Gawler Range Volcanics|Thickness range|Up to at least 1500 m|16-MAY-23
7059|Gawler Range Volcanics|Lithology|Predominantly a calc-alkaline dacite-rhyodacite-rhyolite assemblage, with less abundant andesites and basalts.|16-MAY-23
7059|Gawler Range Volcanics|Relationships and boundaries|Overlain unconformably by Adelaidean formations east of Lake Gairdner and in the northern portion of the area covered by the Port Augusta 1:250 000 sheet. Intruded by the Hiltaba Granite (c. 1500 m.y. B.P.)  Rests unconformably on the Cleve Metamorphics and "Older granites" (Lower Proterozoic to early Carpentarian).|16-MAY-23
7059|Gawler Range Volcanics|Age reasons|Carpentarian (c. 1535 m.y. B.P.)|16-MAY-23
7059|Gawler Range Volcanics|Comments|This name supersedes the names: Gawler Range Porphyry (Miles, 1955 p.35). Gawler Ranges Volcanic Complex (Crawford, 1963, pp.2-4; Turner, in press).|16-MAY-23
7059|Gawler Range Volcanics|Apprdate|MAR-APR 1975|16-MAY-23
7059|Gawler Range Volcanics|Category|1  Defined below|16-MAY-23
82227|George Hill Iron Member|Name source|George Hill, TARCOOLA, SH5310, 1:250,000 map sheet. Located at GDA2020, MGA53, 360010 mE, 6643684 mN.|16-MAY-23
82227|George Hill Iron Member|Unit history|Informally known as 'Christie Gneiss unit 2' (Rankin et al. 1996).|16-MAY-23
82227|George Hill Iron Member|Geomorphic expression|Outcrops as prominent, discontinuous bands interlayered with metasedimentary gneisses and mafic lithologies (Daly and van der Stelt, 1992).|16-MAY-23
82227|George Hill Iron Member|Type section locality|Mount Christie (Rankin et al. 1996). Located at MGA53, 357389 mE, 6646645 mN. Reference Drillhole: GWL023 (266872), interval 24?138 m (total depth). Drilled by Dominion Gold Operations Pty Ltd in 2010 at the Boomer prospect. Located at GDA2020, MGA53, 350902 mE, 6645938 mN. Core available at the SA Drill Core Reference Library, Tonsley.|16-MAY-23
82227|George Hill Iron Member|Extent|Outcrops extensively in the southern Christie Domain, particularly near Mount Christie. Outcrops and drillhole intersections predominantly occur in a northeast-southwest-trending band, closely associated with distinct strong magnetic highs.|16-MAY-23
82227|George Hill Iron Member|Thickness range|Typically 10-50 m thick, although significantly thicker zones are present in areas of structural thickening by isoclinal folding (Daly and Fanning 1993; Iron Road 2012).|16-MAY-23
82227|George Hill Iron Member|Lithology|Iron-rich, quartz magnetite gneiss. The predominant lithology is a medium- to coarse-grained, quartz-magnetite-diopside-hypersthene-amphibole gneiss, with magnetite, partly altered to martite, and trace sulfides. The lithology is strikingly banded green and black on a millimetre scale with local massive sections. The lithology displays complex folding with abundant open to right dextral-vergence folds (Rankin et al. 1996). The magnetite-rich gneiss contains thin interlayers and laminae of carbonate with accessory garnet, clinopyroxene and olivine and quartzofeldspathic gneiss (Daly and Fanning 1993; Rankin et al. 1996). Outcrops are weathered to goethite and have a distinctive shiny black appearance (Rankin et al. 1996).|16-MAY-23
82227|George Hill Iron Member|Depositional environment|Genesis: Protolith either sedimentary banded iron formation or iron-rich clastic rock (Davies, 2000; Reid et al., 2014). Restricted marine environment suggested by interlayered carbonates (Jagodzinski et al., 2009).|16-MAY-23
82227|George Hill Iron Member|Relationships and boundaries|Commonly associated with olivine-bearing metacarbonate and interlayered with quartzofeldspathic gneiss (Christie Gneiss) and metamafic lithologies (Skuse Hill Metapyroxenite; Daly and Fanning 1993).|16-MAY-23
82227|George Hill Iron Member|Identifying features|Coarse grained magnetite-quartz gneiss. Association with the Christie Gneiss.|16-MAY-23
82227|George Hill Iron Member|Structure and Metamorphism|Isoclinal folds refolded by right-dextral-vergence open to tight folds. Granulite facies metamorphism indicated by presence of both clino- and ortho-pyroxene (Rankin, 1996).|16-MAY-23
82227|George Hill Iron Member|Age reasons|Paleoproterozoic; maximum depositional age c. 2480 Ma; metamorphosed at c. 2460-2415 Ma with ages derived from adjacent quartz-feldspar-biotite gneiss (Jagodzinski et al. 2009).|16-MAY-23
82227|George Hill Iron Member|Correlations|Iron-rich lithologies also occur within the Harris Greenstone Domain, within the Kenella Gneiss. Sedimentary lithologies in the Harris Greenstone Domain may be slightly older than the George Hill Iron Member, but the ages of both lithologies are not well constrained.|16-MAY-23
82227|George Hill Iron Member|Alteration and Mineralisation|Hosts several iron (magnetite) prospects, typically with large grains of magnetite.|16-MAY-23
82227|George Hill Iron Member|Geophysical Expression|Characteristically strong and distinct magnetic highs, surrounded by lithologies with low magnetic response (metasediments). Associated with regional band of high gravity response. High thorium radiometric response, no characteristic potassium or uranium radiometric response.|16-MAY-23
82227|George Hill Iron Member|Geochemistry|Iron rich, up to 45% Fe (Iron Road Ltd., 2014).|16-MAY-23
82227|George Hill Iron Member|Defn author|Williams, M.A., 9-JUN-2021.|16-MAY-23
82227|George Hill Iron Member|References|Crawford, A.R., 1957. Iron Ore near Mount Christie. South Australia. Department of Mines. Mining Review 104, 6-15.  **Daly, S.J., Fanning, C.M., 1993. Archean, in: Drexel, J.F., Preiss, W.V., Parker, A.J. (Eds.), The Geology of South Australia. Volume 1 - The Precambrian. Geological Survey of South Australia, Bulletin, 54, pp. 32-49.  **Daly, S.J., van der Stelt, B.J., 1992. Archaean metabasic diamond drilling project. South Australia. Department of Mines and Energy. Open file Envelope 08541, 1531-1902.  **Daly, S.J., Webb, A.W., Whitehead, S.G., 1978. Archaean to Early Proterozoic banded iron formations in the Tarcoola Region, South Australia. Transactions of the Royal Society of South Australia 102, 141-149.  **Davies, M.B., 2000. Iron ore in South Australia 2000 Commodity Review. Primary Industries and Resources South Australia. ComRev 008.  **Iron Road Ltd., 2010. Combined Annual Technical Report for the period 1/7/2009 to 30/6/2010. EL 3435, 3554, 4014, 4468, 4532 (Mulgathing). Primary Industries and Resources. South Australia. Open file Envelope 12107, 2-94.  **Iron Road Ltd., 2012. Unlocking South Australia's Mineral and Energy Potential - A Plan for Accelerating Exploration. Theme 2 (drilling partnerships with PIRSA and industry) : Year 6 partnership no. DPY6-63 - Gawler Iron Project, Mount Christie district - Archaean BIF hosted stratabound iron ore prospects. Drilling project final report. South Australia. Department for Manufacturing, Innovation, Trade, Resources and Energy. Open file Envelope 12245.  **Iron Road Ltd., 2014. Data release - as updated [made at SA Director of Mines' discretion] : Blowout, Campfire Bore, Mulgathing, Jumbuck, Mobella and Sandstone (the Gawler Project Central Tenements Area). Joint venture operators' separate joint annual reports for the period 1/7/2010 to 30/6/2014. South Australia. Department for Energy and Mining. Open file Envelope 12204   **Jagodzinski, E.A., Reid, A.J., Fraser, G.L., 2009. Compilation of SHRIMP U-Pb geochronological data for the Mulgathing Complex, Gawler Craton, South Australia, 2007-09. Primary Industries and Resources South Australia. Report Book 2009/00016.  **Morris, B.J., Hill, P.W., Ferris, G.M., 1994. Barton bedrock drilling project, 1993. South Australia. Department of Mines and Energy. Report Book 94/00019.  **Rankin, L.R., Benbow, M.C., Fairclough, M.C., Daly, S.J., 1996. BARTON, South Australia, 1:250 000 geological series - explanatory notes. Geological Survey of South Australia. Department of Mines and Energy.  **Reid, A.J., Birt, T., Fraser, G.L., Daly, S.J., 2007. The geology of the Mulgathing Complex: from eastern Tallaringa to Glenloth Goldfield. Primary Industries and Resources South Australia. Report Book 2007/00017.  **Reid, A.J., Jagodzinski, E.A., Fraser, G.L., Pawley, M.J., 2014. SHRIMP U-Pb zircon age constraints on the tectonics of the Neoarchean to early Paleoproterozoic transition within the Mulgathing Complex, Gawler Craton, South Australia. Precambrian Research 250, 27-49.  **Robinson, H.A., 1972. Quarterly report, SML 638 and 639, 29/1/72, for Otter Exploration NL. South Australia. Department of Mines and Energy. Open file Envelope 01857.  **Whitehead, S.G., 1977. Description of Mt. Christie banded iron formation and associated rocks. The Australian Mineral Development Laboratories. AMDEL Report MP 1816/77.  **Whitehead, S.G., 1978. Comparison of some Archean and Proterozoic iron-formations in South Australia. Progress Report no. 2. South Australia. Department of Mines and Energy. Open file Envelope 03220, 29-173.  **Whitten, G.F., 1965. The investigation of iron formations in the Mulgathing district (Tarcoola 4 mile sheet). South Australia. Department of Mines. Report Book 60/00042.  **Williams, M.A., Reid, A.J., 2021. Linking lithostratigraphy to mineral potential for the Archean to earliest Paleoproterozoic Mulgathing Complex, central Gawler Craton. South Australia. Department for Energy and Mining. MESA Journal 94, 04-18.|16-MAY-23
24285|Giddinna Formation|Name source|Giddinna 1:63 360 map sheet, on S.E. Murloocoppie 1:250 000 map sheet.|16-MAY-23
24285|Giddinna Formation|Unit history|Correlated with the Pooraka Formation (Firman 1969, Williams 1973).|16-MAY-23
24285|Giddinna Formation|Type section locality|Type locality - Black Flag Opal Field, Coober Pedy. Section 2.62 km south of Coober Pedy township, 50 m west of the Stuart Highway.|16-MAY-23
24285|Giddinna Formation|Extent|Over the Stuart Range and Uplands and on the northeastern flanks.|16-MAY-23
24285|Giddinna Formation|Thickness range|1-4 metres, average 1.5 m|16-MAY-23
24285|Giddinna Formation|Lithology|Silty gravels, red clays and silts, indurated moderately.|16-MAY-23
24285|Giddinna Formation|Relationships and boundaries|Overlies massive calcreted and gypcreted colluvial and alluvial sediments. Often overlain by red brown prismatic clay (Benitos Clay).|16-MAY-23
24285|Giddinna Formation|Age reasons|No fossils, probably late Pleistocene.|16-MAY-23
24285|Giddinna Formation|Proposed publication|Coober Pedy 1:250 000 Explanatory Notes Geol. Surv. S. Aust.|16-MAY-23
24285|Giddinna Formation|First Reference|83/23476|16-MAY-23
7458|Glyde Hill Volcanic Complex|Name source|Glyde Hill outstation, 13 km north of Lake Everard H.S. Lat. 31o37'30"S; Long. 135o09'30"E (Gairdner 1:250 000 sheet (SH53-15)).|16-MAY-23
7458|Glyde Hill Volcanic Complex|Constituents|Pag3 Dacite, Pag2 Rhyodacite, Wheepool Rhyolite (defined below) Pag1 Rhyolite, Yandoolka Rhyolite (defined below). The unit Pag3 consists of porphyritic dacite grading into rhyodacite and may be equivalent in age to the Yardea Dacite, though probably erupted from a separate centre. The unit either overlies or is a facies variant of unit Pag2. It rests upon the Wheepool Rhyolite 7 km north-northwest of Wheepool wells, the base being marked by a weathered layer of tuff. The unit Pag2 is mainly reddish brown porphyritic rhyodacite with scattered phenocrysts of pink potash feldspar up to 1 cm long, locally grading into dacite. The lower part is fine grained with rare small feldspar phenocrysts. The rhyodacite overlies the Wheepool Rhyolite north of Lake Everard H.S. and southeast of Dingo Hill; and also the basal (Pag1) west of Glyde Hill outstation. East of the outstation, the unit either rests upon or passes into the Wheepool Rhyolite. Southeast of Dingo Hill and eastwards into Lake Gairdner, the rhyodacite either passes into, or is overlain by the Yardea Dacite. The unit Pag1 includes fine grained pale yellowish and cream coloured banded rhyolite and rhyolitic welded ash flow tuff, cropping out in the area west of Glyde Hill outstation for aboaut 25 km westwarads. The rhyolite is overlain by the rhyodacite unit Pag2. The base is not exposed, but the unit is probably at least 20 m thick. The rhyolite may be equivalent to pale reddish brown banded rhyolite underlying Yardea Dacite on the western shore of Lake Acraman, about 45 km to the southeast.|16-MAY-23
7458|Glyde Hill Volcanic Complex|Extent|Lake Everard area, centred about Glyde Hill outstation and eastward to Lake Gairdner.|16-MAY-23
7458|Glyde Hill Volcanic Complex|Defn author|Blissett A.H., 1975|16-MAY-23
7458|Glyde Hill Volcanic Complex|Proposed publication|Quarterly Note|16-MAY-23
7458|Glyde Hill Volcanic Complex|Apprdate|MAR-APR 1975|16-MAY-23
7596|Gordon Springs Granodiorite|Name source|From Gordon Springs Creek, one of the main streams draining from the southern Mount Painter Block.|16-MAY-23
7596|Gordon Springs Granodiorite|Type section locality|Occurs as small stocks and dykes throughout southern sections of Mount Painter Block 139o19'E, 30o14'S. Upper reaches of Radium Creek.|16-MAY-23
7596|Gordon Springs Granodiorite|Extent|Radium Creek Metamorphics and Mt Neil Granite Porphyry|16-MAY-23
7596|Gordon Springs Granodiorite|Lithology|Consists of quartz, sodic andesine, microcline, biotite with accessory magnetite, zircon and monazite. Muscovite occurs in the more corondum normative variants. Hornblende is rare and occurs in only one small stock in Radium Creek.|16-MAY-23
7596|Gordon Springs Granodiorite|Identifying features|High Ba, Sr, and TiO2. More Zr rich and SiO2 deficient than other palaeozoic intrusives. Chemical composition: SiO2 = 68.70; Al2O3 = 16.21; Fe2O3 = 2.35; MnO = 0.01; MgO = 1.27; CaO = 2.85; Na2O = 4.38; K2O = 2.73; TiO2 = 0.42; P2O5 = 0.11; L.O.1. = 0.77;  TOTAL = 99.79. (Ba = 1480 ppm; Sr = 845 ppm).|16-MAY-23
7596|Gordon Springs Granodiorite|Age reasons|Palaeozoic|16-MAY-23
7596|Gordon Springs Granodiorite|Proposed publication|Trans. Roy. Soc. S. Aust.|16-MAY-23
7861|Gull Rock Member|Name source|From Gull Rock, a small rock stack adjacent to Blanche Point on the east coast of Gulf St. Vincent. Grid Reference 268960967, Noarlunga 1:50 000.|16-MAY-23
7861|Gull Rock Member|Unit history|Blanche Point Banded Marls. Reynolds, 1953, p.125-127.|16-MAY-23
7861|Gull Rock Member|Type section locality|Coastal outcrop along Aldinga and Maslin Bays, about Blanche Point specifically between samples A2 and A106A inclusive of Reynolds (1953, fig. 1).|16-MAY-23
7861|Gull Rock Member|Extent|Wide distribution in Willunga and Noarlunga Embayments and in the subsurface of the Adelaide Plains.|16-MAY-23
7861|Gull Rock Member|Thickness range|Range 10-26 m in the Willunga Embayment.|16-MAY-23
7861|Gull Rock Member|Lithology|Unit characterised by alternating bands of tough, dark grey chert and friable clays, silts and calcareous clays.|16-MAY-23
7861|Gull Rock Member|Relationships and boundaries|This unit is conformable with the rest of the Blanche Point Formation. Its boundaries are defined by the first and last occurrence of chert bands in any section.|16-MAY-23
7861|Gull Rock Member|Age reasons|Late Eocene. The important foraminiferal zone of Hantkenina primitiva can be discerned immediately below this unit. Important planktic foraminifera occurring within the unit include Turburotalia aculeata, Chiloyuembelina cubensis and Subbotina linaperta.|16-MAY-23
7861|Gull Rock Member|Proposed publication|Q. geol. Notes, geol. Surv. S. Aust. 64: 2-5 (1977)|16-MAY-23
7861|Gull Rock Member|References|01/31605|16-MAY-23
24309|Heysen Supergroup|Name source|The Heysen Supergroup combines the Umberatana and Wilpena Groups of the Adelaide Geosyncline.  The Heysen Range of the central Flinders Ranges, itself named after the artist Sir Hans Heysen.|16-MAY-23
24309|Heysen Supergroup|Type section locality|Umberatana Group: north Flinders Ranges.  Wilpena Group: central Flinders Ranges.|16-MAY-23
24309|Heysen Supergroup|Extent|Thickest in Adelaide Geosyncline but deposition spread on to adjacent platforms.|16-MAY-23
24309|Heysen Supergroup|Lithology|Glaciogenic sediments at base and top of Umberatana Group, with interglacial siltstones and carbonates. Post-glacial Wilpena Group red and green siltstones, carbonates and quartzites.|16-MAY-23
24309|Heysen Supergroup|Relationships and boundaries|Umberatana Group disconformable to unconformable on Burra Group or older rocks. Wilpena Group mostly conformable on Umberatana Group.|16-MAY-23
24309|Heysen Supergroup|Age reasons|Late Adelaidean (late Proterozoic).|16-MAY-23
24309|Heysen Supergroup|Proposed publication|Trans. R. Soc. S. Aust. (Brief communication)|16-MAY-23
24309|Heysen Supergroup|Proposer|Preiss W.V.|16-MAY-23
8381|Hindmarsh Clay|Name source|'Hindmarsh' a suburb of Adelaide where the unit crops out in the River Torrens banks, after Firman (1966).|16-MAY-23
8381|Hindmarsh Clay|Unit history|Tate (1878, 82) referred to this unit as "pipe clay" and "drift". Tate (1890) renamed this unit "Mammaliferous drift". Howchin (1888) referred to this unit as "argillaceous sands" and later (1896) "tenaceous blue to brown clays". Howchin (1918) renamed this unit "alluvial mottled clays". Allchurch (1965) called this unit "Mottled Clay". Selby & Lindsay (1982) cite "Adelaide Clay" and "Pleistocene  Clay" as common usage terms.|16-MAY-23
8381|Hindmarsh Clay|Type section locality|No complete section available. Suburb of Hindmarsh, Adelaide, Grid reference 27876134, Adelaide 1:50 000 Sheet, 6628-III, Zone 54.|16-MAY-23
8381|Hindmarsh Clay|Extent|Extensive within the St Vincent Basin.|16-MAY-23
8381|Hindmarsh Clay|Lithology|Clay with silt, sand, gravel-lenses strings and layers, micaceous. Two main lithologies occur: 1) west of Para Fault; clay with rapid facies changes lateral and vertical - clay - sand - silt - gravel are common, mica is conspicuous; 2) east of Para Fault; clay with less sand and rare mica. Clay matrix consistency - stiff to very stiff, sub-plastic to plastic within a light to heavy clay texture. Colours - gleyed (greyish to greenish) with layers, patches and mottles exhibiting reds, yellows and brown. The upper 1-3 m of the unit displays relict soil horizonation and pedogenic alteration west of the Para Fault.|16-MAY-23
8381|Hindmarsh Clay|Depositional environment|(Upper 10 m of unit only) Alluvial fan-piedmont slope deposit.|16-MAY-23
8381|Hindmarsh Clay|Relationships and boundaries|A disconformable upper boundary with overlying strata, representing an erosional surface, is recognised. This boundary is sharp in the Adelaide Plains Sub-Basin and diffuse or "gradational" in the Adelaide/Golden Grove Embayment. The Hindmarsh Clay "Sand Member" of Selby & Lindsay (1982) has been included (for convenience) in the Hindmarsh Clay. Overlying strata include the Marine Glanville Fm and St Kilda Fm; and the terrestrial Keswick Clay, Pooraka Fm and various later alluvial/colluvial deposits. Hindmarsh Clay no longer includes Keswick Clay within its upper boundary.|16-MAY-23
8381|Hindmarsh Clay|Identifying features|The Hindmarsh Clay is calcrete capped in places west of the Para Fault but subsequent erosion and surficial processes have rendered this an unreliable marker horizon.|16-MAY-23
8381|Hindmarsh Clay|Age reasons|Early Pleistocene, Firman (1967), Lindsay (1969), based on palaeontology and stratigraphic position. Hindmarsh Clay is overlain by Glanville Fm (Late Pleistocene), Ludbrook (1984), (110 KA) - Belperio et al. (1984).|16-MAY-23
8381|Hindmarsh Clay|Proposed publication|Quarterly Geological Notes, geol. Surv. S. Aust., 103, 9-16.|16-MAY-23
8381|Hindmarsh Clay|Comments|Roy. Soc. of SA Transac. 93 (1969)|16-MAY-23
8381|Hindmarsh Clay|References|01/31607; ?01/31604; 01/31608; 01/31606; 79/05157; 82/22968;|16-MAY-23
26307|Hogan Dolomite|Name source|Hogan's Well (shown as 10 km ESE of The Dome on Pastoral Plan 12N). Map symbol Pkh.|16-MAY-23
26307|Hogan Dolomite|Unit history|Hogan Dolomite' of Murrell (1977). Probably R5 unit of Rowlands et al. (1980, p. 61).|16-MAY-23
26307|Hogan Dolomite|Type section locality|Plain with marginal ridges 6 km ESE of The Dome; lat. 29o46', long. 137o58'.|16-MAY-23
26307|Hogan Dolomite|Extent|Willouran Ranges.|16-MAY-23
26307|Hogan Dolomite|Thickness range|645 m in type section.|16-MAY-23
26307|Hogan Dolomite|Lithology|in type section. Top: 2 m dolomite, partly sandy, light yellowish; prominent low ridge.  10 m poorly outcropping sandstone, calcitic and dolomitic; sandy carbonate, green, yellow, brownish.  600 m poorly outcropping dolomite forming plain; partly sandy, calcitic, light brownish grey, pinkish brown, yellowish, thin to medium bedded, rippled sandy lenses and layers, stromatolitic domes, wavy laminations, pale chert layers; possible interbedded shale, siltstone not exposed.  31 m dolomite, grey to dark grey, flaggy, dark chert layers, cauliflower chert nodules, and shortite pseudomorphs.  Base: 2 m dolomite, very pale brown grey, medium bedded, light grey chert, wavy ?stromatolitic bedding; prominent low ridge. Overall sand:shale:carbonate percentages - 3:3:94.|16-MAY-23
26307|Hogan Dolomite|Relationships and boundaries|Lies conformably between Recovery Formation and Cooranna Formation.|16-MAY-23
26307|Hogan Dolomite|Identifying features|Characterised by poorly ourcropping dolomite beds forming a plain between prominent narrow ridges of the lowermost and uppermost dolomite members.|16-MAY-23
26307|Hogan Dolomite|Age reasons|Possibly late Willouran.  No certain correlatives outside the Willouran Ranges.|16-MAY-23
24326|Kalachalpa Formation|Name source|Kalachalpa is the Aboriginal synonym for Anna Creek which is a creek on the southern margin of the Peake and Denison Ranges. Anna Creek also gives its name to a cattle station encompassing most of the Ranges and a railway siding on the Central Australia Railway; Boorthanna 1:100 000 sheet area; Warrina 1:250 000 sheet area.|16-MAY-23
24326|Kalachalpa Formation|Type section locality|The type section occurs in an area first described in detail by Fairchild (1975). The type section outcrops 6 km north of Box Creek R.S., metric ref. Base 6826575, 595450 - top 6824900, 594275; thickness is 900 metres.|16-MAY-23
24326|Kalachalpa Formation|Extent|Outcrops in a southwesterly facing sequence, 6 km north of Box Creek R.S. on the Central Australia Railway. A faulted sequence of the formation outcrops 1 km northeast of Box Creek R.S. Smaller outcrops occur 8 km northwest and 11 km north of Anna Creek H.S.|16-MAY-23
24326|Kalachalpa Formation|Thickness range|Maximum total thickness of the formation is 900 metres in the type section.|16-MAY-23
24326|Kalachalpa Formation|Lithology|Grey-green and brown siltstone and shale, gritty sandstone and quartzite, conglomeratic dolomite, stromatolitic dolomite, oolitic sediments, black chert, quartzites and shales at the top; abundant sedimentary features throughout the sequence include ripple marks, crossbedding graded bedding, clay galls and mudcracks.|16-MAY-23
24326|Kalachalpa Formation|Relationships and boundaries|Grades downwards into a unnamed tranational unit which in turn overlies the Skillogalee Dolomite. The formation is disconformably overlain by Calthorinna Tillite (Ambrose and Flint, in prep.).|16-MAY-23
24326|Kalachalpa Formation|Age reasons|Adelaidean-Uppermost Burra Group (Torrensian); correlates with the Myrtle Springs Formation (Coats, 1973).|16-MAY-23
24326|Kalachalpa Formation|Proposed publication|Rep. Invest., geol. Surv. S. Aust.|16-MAY-23
24326|Kalachalpa Formation|Resdate|29-NOV-1979|16-MAY-23
24329|Kalladeina Formation|Name source|Kalladeina-1 Well at 27o39'29"S, 139o24'00"E.|16-MAY-23
24329|Kalladeina Formation|Type section locality|Kalladeina-1 well from 1957 m to 3615 m.|16-MAY-23
24329|Kalladeina Formation|Extent|In subsurface only, it occurs in Coongie-1, Gidgealpa-1, -3, -5 and -7, and Cuttapirrie-1? ie between the Birdsville Track Ridge and the Gidgealpa-Merrimelia-Innamincka Trend.|16-MAY-23
24329|Kalladeina Formation|Thickness range|In the type section it is 1658 m thick, but is known to vary; 129 m (G-5), 28.3 m (G-3), and in Coongie-1 it is 1196 m thick.|16-MAY-23
24329|Kalladeina Formation|Lithology|Limestone, dolomite, shale, siltstone, and sandstone, with minor tuffaceous intervals.|16-MAY-23
24329|Kalladeina Formation|Relationships and boundaries|It overlies the Mooracoochie Volcanics in Kalladeina-1, Gidgealpa-1, and also probably in Coongie-1, Gidgealpa-3, -5 and 7. The base is an unconformity. The unit is unconformably overlain by the Dullingari Group of Ordovician? age.|16-MAY-23
24329|Kalladeina Formation|Age reasons|The age of the unit ranges from early Middle Cambrian to late Late Cambrian. Numerous agnostid and polymerid trilobites, eg. Nepea, Pagetia cf. Significans, Ptychagnostus gibbus, Blackwelderia, Leiopyge laevigata armata, and many others (see summary in Appendix 1, Gatehouse, 1982).|16-MAY-23
24329|Kalladeina Formation|Defn approved by|South Australia Sub-Committee|16-MAY-23
76223|Kandramooka Member|Name source|Kandramooka Creek, ~450 m west of Moorowie Mine.|16-MAY-23
76223|Kandramooka Member|Geomorphic expression|Exposed as wide prominent ridges tracing major folds.|16-MAY-23
76223|Kandramooka Member|Type section locality|Section G, 127 ft (basal contact) to 457 ft. (38.7 to 139.3 m) 30deg9'33.82"S, 139deg16'1.59"E to 30deg59'35.91"S, 139deg16'11.60"E (includes minor faults). Reference section: Section H, 367 ft (basal contact; faulted?) to 467 ft (upper contact) (118.9 to 142.3 m) 30deg59'51.77"S, 139deg15'49.28"E to 30deg9'54.84"S, 139deg15'56.89"E),  Section X, -22 ft (basal contact) to 120 ft (faulted?) (-6.7 to 36.6 m)  30deg59'1.65"S, 139deg16'14.12"E to 30deg59'5.78"S, 139deg16'18.58"E), Section Y, 8 (fault) to 368 ft (2.4 to 112.2 m) (30deg58'39.81"S, 139deg16'47.11"E to 30deg58'44.19"S, 139deg16'40.80"E.|16-MAY-23
76223|Kandramooka Member|Extent|Exposed in low hills from Mt. Chambers Gorge, south, past Moorowie Mine, to east of Mt. Daily.|16-MAY-23
76223|Kandramooka Member|Thickness range|Apparent maximum of 101 m (330 ft) in the type section (base faulted) on Section G. Estimated average 81 m (266 ft: megabreccia, 49 m; upper beds 32 m) from other partly faulted sections measured across lenticular beds.|16-MAY-23
76223|Kandramooka Member|Lithology|At base: megabreccia: massive, poorly bedded, buff or grey to red, angular to sub-rounded cobbles to boulders of (i) clean light grey archaeocyath limestone and (ii) dark brown silty to quartz granule-rich (arkosic) limestones, reworked from the breccia matrix. Upper beds: massive, buff, light to dark grey or ferric red, richly fossiliferous, peloidal to part oolitic archaeocyath limestones, with siliciclastic silt to grit stringers, silty dolostone intraclasts, and conglomerates of grey limestone boulders to 3 m in a quartz-granule rich, red to buff, silty carbonate matrix.|16-MAY-23
76223|Kandramooka Member|Depositional environment|High-energy intertidal carbonate platform margin to backreef shelf bioherms and ooid-peloid shoals, with reef bypass tidal channels. Adjacent siliciclastic sources from emergent salt domes and dune fields.|16-MAY-23
76223|Kandramooka Member|Relationships and boundaries|Third unit from the base of the Moorowie Formation. Conformable, with passage zones from the red-brown to green micaceous siltstones of the Wookata Shale Member below, to the purple micaceous siltstones of the Pack Creek Member above.|16-MAY-23
76223|Kandramooka Member|Structure and Metamorphism|Massive beds of moderate dip defining limbs and core of a low-plunge anticline.|16-MAY-23
76223|Kandramooka Member|Age reasons|Lower Cambrian, Stage 4, within the Pararaia janeae trilobite Zone (Lafuste et al., 1991).|16-MAY-23
76223|Kandramooka Member|Correlations|Not confirmed outside Moorowie area; possible equivalents in the Bunkers Graben. Broadly related to the upper Wilkawillina Limestone (Figure 2 of Jago et al., this volume).|16-MAY-23
76223|Kandramooka Member|Defn author|T. J. Mount, 8-JAN-2019, after Mount (1970).|16-MAY-23
76223|Kandramooka Member|References|Jago, J. B., Gehling, J. G., Betts, M. J., Brock, G. A., Dalgarno, C. R., Garcia-Bellido, D. C.,.., Paterson, J. R. (2019). The Cambrian System in the Arrowie Basin, Flinders Ranges, South Australia.Australian Journal of Earth Sciences. doi:10.1080/08120099.2018.1525431  **Lafuste, J., Debrenne, F., Gandin, A., & Gravestock, D. I. (1991). The oldest tabulate corals and the associated Archaeocyatha, Lower Cambrian, Flinders Ranges, South Australia. Geobios, 24(6), 697-718. doi:10.1016/S0016-6995(06)80298-6   **Mount, T. J. (1970). Geology of the Mt. Chambers Gorge region (BSc. (Honours) thesis, unpublished).Adelaide, SA: University of Adelaide. http:hdl.handle.net/2440/67162.  **T. J. Mount, J. B. Jago, N. R. Langsford & C. R. Dalgarno (2019): Geological setting of the Moorowie Formation, lower Cambrian Hawker Group, Mt Chambers Gorge, eastern Flinders Ranges, South Australia, Australian Journal of Earth Sciences, DOI: 10.1080/08120099.2019.1586771.|16-MAY-23
29269|Karkulta Rhyolite|Name source|From Karkulta dam, a dam on Moonarie station, which adjoins Lake Everard station. Locality of Karkulta dam is: 31o45' latitude and 135o30' longitude.  Origin: This unit is considered to be a lava dome, built up by a series of viscous lava flows and minor ashflows (now strongly welded crystal tuffs).B25|16-MAY-23
29269|Karkulta Rhyolite|Type section locality|It is not possible to propose a type section for this unit, however the basal members are well exposed at 31o40.5' lat. and 134o52.25' longitude. The upper contact is well exposed at 31o40.25' latitude and 134o54.5' longitude.|16-MAY-23
29269|Karkulta Rhyolite|Extent|Confined entirely to the eastern portion of the Childara 1:250 000 Sheet area.|16-MAY-23
29269|Karkulta Rhyolite|Lithology|A light grey to buff coloured rock containing white alkali feldspar and plagioclase phenocrysts and green biotite sitting in an aphanitic matrix. In thin section the glomeroporphyritic aggregates of euhedral, fine to medium grainsize feldspar phenocrysts and plates of green biotite are characteristic. Single, euhedral, medium grained phenocrysts of plagioclase and alkali feldspar also occur as do numerous corroded very fine grained alkali feldspar phenocrysts scattered throughout the groundmass. Rounded anhedral quartz phenocrysts are present. Plagioclase dominant. Total feldspar:quarta:green biotite phenocrysts roughly 10:2:3. Phenocrysts make up 5% of rock. Groundmass consists of a microgranular textured devitrified mosaic. The basal part of this unit is completely and pervasively autobrecciated probably cuased by flowage - i.e., flow breccia. The upper contact with the Yantea Rhyodacite is marked by a distinctive banded airfall tuff.|16-MAY-23
29269|Karkulta Rhyolite|Relationships and boundaries|The Karkulta Rhyolite conformaly overlies the Mangaroongah Dacite and underlies the Yantea Rhyodacite. It is at the same stratigraphic level as the Arburee Rhyolite, but is not regarded as the equivalent of this unit, upon the basis of field, petrological and geochemical evidence. It forms a localised lava dome with maximum thickness probably not exceeding 40 m.|16-MAY-23
29269|Karkulta Rhyolite|Age reasons|mid-Carpentarian -1550 Ma, upon geochronological evidence. This unit forms part of the Glyde Hill Complex as previously defined by Blissett.|16-MAY-23
29269|Karkulta Rhyolite|Defn author|Giles C.W., 1977|16-MAY-23
29269|Karkulta Rhyolite|Proposed publication|SA Department of Mines, Quarterly Notes: 61.|16-MAY-23
9477|Keswick Clay|Name source|Keswick' Railway Yards, western edge of the West Park Lands, Adelaide: grid reference 2792061313, Adelaide 1:50 000 Sheet, 6628-III, Zone 54.|16-MAY-23
9477|Keswick Clay|Unit history|Allchurch (1965) referred to this unit as 'Mottled Clay'. Ward (1966) equated this unit with the Ngaltinga Clay (Noarlunga & Willunga Embayments). Firman (1966), Allchurch (1967) includes this unit with Hindmarsh Clay. Selby & Lindsay (1982) referred to this unit as the 'Upper Member' of Hindmarsh Clay and also cite 'Cadelaide Clay' as a common usage informal name.|16-MAY-23
9477|Keswick Clay|Type section locality|Keswick Railway Yards cutting, 4-5 m of green-grey stiff plastic clay, variously mottled with reddish ferruginous colours is exposed over a 1.8 km distance (Ward, 1966). The base rests disconformably on Hindmarsh Clay (brownish) and is overlain by solonised brown soil - carbonate rich. Type drill hole: 5.2 metres of greenish-grey (5GY 6/1) to light olive-grey (5Y 6/1) stiff plastic clay; intersected in cored hole GH03 (SADME Core Library no. 662800301773), Metro-Adelaide Soil Investigations (Colour Names - Kelly & Judd, 1976; Colour notation - Munsell, 1975). The drill site is 180 m east of the Type Section and 450 m north of Greenhill Road, Wayville, in the South West Park Lands, Hundred of Adelaide.|16-MAY-23
9477|Keswick Clay|Extent|The unit covers an area of 150 km2 on the eastern margin of the St Vincent Basin. It is extensively developed in the Adelaide/Golden Grove Embayment, onlaps the Para Block and is more restricted on the Edan Block (Ward, 1966); Firman 1969a; Daily et al., 1976|16-MAY-23
9477|Keswick Clay|Thickness range|Range 0.5 to 6.8 metres.|16-MAY-23
9477|Keswick Clay|Lithology|Clay; silty to gritty (quartz sand), texture range - light to heavy, often with waxy lustre. Generally ;massive, poorly bedded, with steep and shallow angle slicken sided fissures often apparent. Gligai structures are common in the upper parts of the unit. jSand lenses and silty zones proximal to ephemeral creek lines are common. Colour range yellow-greys to green-greys, mottles - reddish to yellowish. X-ray diffraction studies indicate predominant Smectite mineralogy, less dominant Illite and randomly interstratified clays.|16-MAY-23
9477|Keswick Clay|Depositional environment|aeolian' (Ward, 1966), "terrestrial alluvial fan deposit" Firman (1969a). Present investigations imply two origins: terrestrial alluvial fan overbank sedimentation (Adelaide/Golden Grove Embayment); in situ bedrock weathering and minimal transport (Para and Eden Blocks). Mineralogy and morphology suggest clay derived by deep weathering during period of tectonic stability, subsequent clay erosion on reactivation of teactonic movement and a probable climate change. No evidence for aeolian origin is revealed by micromorphological studies.|16-MAY-23
9477|Keswick Clay|Relationships and boundaries|Stratigraphically it overlies Hindmarsh Clay (Firman, 1966; Taylor et al., 1974), its basal contact is disconformable (Selby & Lindsay, 1982) and ranges from sharp to diffuse. The upper contact is sharp when overlain by calcareous Red-Brown Earths/Brown Solonised soils but gradational with overlying Black Earth soils. Its western limit is marked by the Para Fault escarpment. South and east the limits are less well defined due to interfingering with other gleyed alluvial/colluvial deposits associated with the Eden-Burnside Fault escarpment. Isolated irregular remnants occur in bedrock depressions on the upthrown Eden & Para Blocks, Sheard & Bowman (1987).|16-MAY-23
9477|Keswick Clay|Age reasons|Middle Pleistocene; unit is unfossiliferous, it overlies Hindmarsh Clay ;(Early Pleistocene) and underlies Pooraka Formation (Late Pleistocene), Firman (1969a,b), Daily et al. (1976).|16-MAY-23
9477|Keswick Clay|Proposed publication|Quarterly Geological Notes, geol. Surv. S. Aust., 103, 4-9.|16-MAY-23
9477|Keswick Clay|Comments|Geomechanical Properties: Liquid limit range 40 to 130%; Plastic Limit range 17 to 30%; field moisture approximates Plastic limit below 4 m from ground surface; unconfined 'pocket penetrometer' strengths range 100 to 400 kPa.    Roy. Soc. SA Transac. 93 (1969)|16-MAY-23
9477|Keswick Clay|References|01/31607; 01/31609; 86/25351; 01/31604; 79/05042;79/05041; 82/22968;88/26038; 79/04256; 98/29165.|16-MAY-23
9477|Keswick Clay|Name first published by|79/05042 Firman J.B.|16-MAY-23
9477|Keswick Clay|Reserved? Yes/No|Yes|16-MAY-23
24335|Kilburn Sand|Name source|Unit named after the Adelaide suburb of Kilburn; Grid reference 795390, Adelaide 6628-III, 1:50 000 sheet, Zone 54.|16-MAY-23
24335|Kilburn Sand|Unit history|Kilburn Sand has been informally referred to as "older dune sands near Gepps Cross" by Bowman and Sheard (1988).|16-MAY-23
24335|Kilburn Sand|Type section locality|1.0 m of reddish brown well sorted quartz sand exposed in a cutting within Irish Harp Reserve, off Regency Road, Prospect, (section 367, Hundred of Yatala, Grid reference: 793381, Adelaide 6628-III). The Kilburn sand dune ridge is approximately 90 m wide at this location and rises to about 2 m above the level of the surrounding plain. Reference Section:  1.13 m of non calcareous, unfossiliferous, well sorted quartz sand with a sandy clay soil B horizon between 230 and 440 mm depth. Colour - uniform dark brown (7.5 YR 3/4 to 7.5 YR 3.5/4, moist), soil B horizon is reddish brown (5 YR 4/3, moist). Proposed reference section is cored hole GH 91 from the Metro-Adelaide Soils Investigations; SADME Core Library number 662840002062. This hole is located in the Irish Harp Reserve adjacent to the Type Section.|16-MAY-23
24335|Kilburn Sand|Extent|The unit is exposed as a composite linear dune ridge, 200 to 300 m west of the Para Fault escarpment, running from Dudley Park (south) to Gepps Cross west of the Para Fault escarpment, running from Dudley Park (south) to Gepps Cross (north). The areal extent is approximately 4 square km.|16-MAY-23
24335|Kilburn Sand|Thickness range|range <0.30 to 1.80 m.|16-MAY-23
24335|Kilburn Sand|Lithology|Kilburn Sand has been extensively affected by soil development. Sand mineralogy consists of about 91% subrounded quartz grains; 5% feldspar grains and minor lithics, heavy minerals; and a trace of muscovite. Lithic grains are more abundant than for the Fulham Sand (Bowman and Sheard, 1988). Kilburn sand grains are moderately well rounded, few are frosted and iron oxides/clay fill grain depressions and/or form grain coatings. The sand is fine well sorted, with a significant clay-silt fraction (25 to 50%); mean size range from 31.2 micron sediment = 2.78 phi (146 microns) with standard deviation of 0.97 phi. Skewness of distribution = -0.11 to +0.17. Kurtosis (peakedness) of the Kilburn Sand is mesokurtic (-0.70 to +0.29) - distinctively different from the Fulham Sand as redefined by Bowman and Sheard (1988).|16-MAY-23
24335|Kilburn Sand|Depositional environment|Aeolian, based on granulometric character, unit morphology, distribution, topography and stratigraphy. Sediment sources are possibly the River Torrens alluvial fan, Dry Creek alluvial fan, or reworked Pooraka Formation. High lithic-silt/clay content reflects a terrigenous source and lack of marine reworking.|16-MAY-23
24335|Kilburn Sand|Relationships and boundaries|Kilburn Sand overlies Quaternary alluvium, carbonate silt deposits and forms part of the Enfield Soil Association of Aitchison et al (1954). The upper boundary is unconfined except where overlain by anthropogenic deposits.|16-MAY-23
24335|Kilburn Sand|Age reasons|Kilburn Sand is unfossiliferous. It stratigraphically overlies Quaternary alluvium and the Pookaka Fm (dated at 35 K A: Williams, 1969). On pedologic grounds Kilburn Sand is probably older than Fulham Sand (about 16-20kA; Bowman and Sheard, 1988). Probable age 20 to 30 kA; poor soil development in surrounding drift sand indicates more recent reworking of sediment.|16-MAY-23
24335|Kilburn Sand|Category|2|16-MAY-23
24335|Kilburn Sand|Resdate|01-FEB-1988|16-MAY-23
24335|Kilburn Sand|Reserved? Yes/No|Yes|16-MAY-23
24336|Kingscote Limestone|Name source|The richly fossiliferous yellow to buff limestones exposed at Kingscote between the jetty at Beare Point and Brownlow Beach (Figs 2, 3) have never been formally designated as a stratigraphic unit distinct from the more continuous but partly time-correlative units exposed in Aldinga and Maslin Bays.|16-MAY-23
24336|Kingscote Limestone|Type section locality|Typical Kingscote Limestone is exposed in the coastal cliffs and associated shore platforms at Kingscote, sections 406 and 407 hundred of Menzies; a measured type section is designated 150 m southwest of the swimming pool. Another important section occurs at the base of cliffs at "Table Rock" near Point Reynolds, section H hundred of Haines, but it is difficult to access except at low tide. Important subsurface sections of Kingscote Limestone were penetrated by the E. & W.S. Dept Pumphouse bore (Fig. 4), drilled in 1962 6 km southwest of Kingscote (section 46 hundred of Menzies); and by the Engineer-in-Chief's Kingscote bore, drilled in 1909-10 1 km north of Beare Point (section J1 hundred of Menzies).|16-MAY-23
24336|Kingscote Limestone|Extent|On Kangaroo Island at Kingscote, Cygnet River, Freestone Creek and Point Reynolds. In addition, a succession comparable with the Eocene part of the Kingscote Limestone has been recognised in Beach Petroleum Troubridge Shoal No. 1 borehole between 229 m and 259 m (Ludbrook 1963; Stuart 1970). The Kingscote section comprises three lithologically distinguishable units: the lowest consisting of echinoid-rich limestones capped by a rubbly mollusc-rich conglomerate of Late Eocene age; an intermediate bioclastic limestone of latest Eocene to Middle Oligocene age; and an upper unit of well-bedded to flaggy and cross-bedded bioclastic limestones of Late Oligocene age. For practical purposes all are best included for the time being in the Kingscote Limestone. However, they have lithological and chronological counterparts in the Port Willunga Formation on the eastern side of Gulf St Vincent. The lowest unit of the Kingscote Limestone, of Late Eocene age, is on faunal evidence, a correlative of the Tortachilla Limestone and at least part of the  Blanche Point Formation in the eastern St Vincent Basin; while in terms of units on eastern Yorke Peninsula (Stuart 1970) it correlates faunally with Muloowurtie Formation, Throoka Silts, and perhaps the basal part of Rogue Formation. A summary of contributions to correlations within the St Vincent Basin was provided by Cooper (1979).|16-MAY-23
24336|Kingscote Limestone|Thickness range|In the coastal exposures in the type section, 4.5 m; in the Kingscote bore, 25-30 m; in the Pumphouse bore, approximately 50 m.|16-MAY-23
24336|Kingscote Limestone|Lithology|Bioclastic limestone, with a thin basal bed of pebbly quartzose greensand (not exposed but penetrated in the Pumphouse bore).|16-MAY-23
24336|Kingscote Limestone|Age reasons|Late Eocene to Late Oligocene.|16-MAY-23
24336|Kingscote Limestone|Proposed publication|Trans. Roy. Soc. S. Aust. 1983 107: 1-35.|16-MAY-23
27065|Kirwan Siltstone|Name source|The Kirwan Mine (copper) occurs within this unit.  Map Symbol: -Pci.|16-MAY-23
27065|Kirwan Siltstone|Unit history|The Kirwan Siltstone was referred to informally as Unit E by Preiss (1978).|16-MAY-23
27065|Kirwan Siltstone|Type section locality|A structurally uncomplicated section is chosen along the north bank of the major unnamed stream north of Morgan Creek, commencing at 276180-6461850 and finishing at 275930-6461700.|16-MAY-23
27065|Kirwan Siltstone|Extent|In the Worumba Anticline, the Kirwan Siltstone occurs over a strike length of about 8 km. It has not been identified with certainty elsewhere.|16-MAY-23
27065|Kirwan Siltstone|Thickness range|160 m in type section.|16-MAY-23
27065|Kirwan Siltstone|Lithology|Top:  60 m siltstone, dark blue-grey, well laminated, poorly outcropping in upper part; some beds micaceous. 44 m siltstone, dark grey, blocky, very thinly laminated; one bed with limy nodules with differential compaction around them. 10 m dolomite, buff weathered, laminated, with irregular black chert lenses; laminated pale grey crystalline dolomite. 26 m siltstone, finely laminated, weathered brown to white. 4 m limestone, pale grey, flaggy, well laminated, broadly wavy, with small irregular cumulate stromatolites.  Base: 16 m siltstone, dark grey, weathering brown, very finely laminated.|16-MAY-23
27065|Kirwan Siltstone|Relationships and boundaries|The Kirwan Siltstone conformably and gradationally overlies correlatives of the Arkaba Hill Beds (Mount, 1980) and is conformably overlain by the Waraco Limestone.|16-MAY-23
27065|Kirwan Siltstone|Identifying features|A mappable marker of laminated carbonaceous siltstones, lying conformably between the Arkaba Hill Beds (below) and Waraco Limestone (above), in the core complex of the Worumba Anticline.|16-MAY-23
27065|Kirwan Siltstone|Age reasons|Inferred to be Willouran.|16-MAY-23
27065|Kirwan Siltstone|Correlations|The Kirwan Siltstone is similar in lithology to dark-coloured carbonaceous siltstones in many diapirs, and also to the lower units of the River Broughton Beds type section in the Spalding Inlier (Preiss, 1974). However, the Kirwan Siltstone cannot be easily distinguished from other siltstone units (e.g. lower Arkaba Hill Beds, Wirrawilka Beds, Worumba Dolomite Beds), on lithololgy alone, when out of stratigraphic context.|16-MAY-23
27065|Kirwan Siltstone|Proposed publication|Q. geol. Notes, geol. Surv. S. Aust., 76: 12-23.|16-MAY-23
27065|Kirwan Siltstone|Resdate|03-JUL-1979|16-MAY-23
25985|Lake Gairdner Rhyolite|Name source|Lake Gairdner, South Australia (Gairdner (SH-53-15); and Yardea (SI53-3), 1:250 000 sheets)|16-MAY-23
25985|Lake Gairdner Rhyolite|Type section locality|Northwestern shore of Lake Gairdner.|16-MAY-23
25985|Lake Gairdner Rhyolite|Extent|Northern part of Lake Gairdner; Lake Harris; 20 km east of Kingoonya, on road to Pimba.|16-MAY-23
25985|Lake Gairdner Rhyolite|Thickness range|Up to at least 25 m.|16-MAY-23
25985|Lake Gairdner Rhyolite|Lithology|Predominantly reddish-brown, cream and pale greenish rhyolites and rhyolitic welded ash flow tuffs with many rounded phenocrysts of quartz. Grades into rhyodacite with rare or no quartz phyenocrysts. Much contorted flow - or compaction-banding. Some layers of nodualr and spherulitic rhyolite.|16-MAY-23
25985|Lake Gairdner Rhyolite|Relationships and boundaries|Base not exposed. May be at or near the base of the Gawler Range Volcanics 15 km north-northeast of Kokatha; in the Glenloth district, and east of Kingoonya. Overlain by Chandabooka Dacite near Chandabooka Well west of Lake Gairdner, and south of Kultanaby Siding on the Transcontinental railway line.|16-MAY-23
25985|Lake Gairdner Rhyolite|Apprdate|MAR-APR-1975|16-MAY-23
10273|Le Hunte Formation|Name source|Port Le Hunte near Lake Macdonnell south of Penong.|16-MAY-23
10273|Le Hunte Formation|Type section locality|Lake Macdonnell Bore A.A.IOW, and other bores described in Dickinson and King (1949 and 1950).|16-MAY-23
10273|Le Hunte Formation|Extent|Lake Macdonnell and elsewhere in lagoons and coastal swamps on the coastal margin of southern Australia, where similar materials occur in the same position in sequence and continuity can be demonstrated by association with St Kilda Formation or equivalent.|16-MAY-23
10273|Le Hunte Formation|Thickness range|Up to 10 m|16-MAY-23
10273|Le Hunte Formation|Lithology|"Pale grey marl and gypsum" and "off-white to pale grey crystalline gypsum" (Lindsay, 1967 p.5). Shelly in part and containing a fauna including Katelysia and Zeacumantus commonly found in shallow marine-estuarine-littoral St Kilda Formation.|16-MAY-23
10273|Le Hunte Formation|Relationships and boundaries|Overlies Glanville Formation containing Anadara and older units elsewhere. Le Hunte Formation in Lake Macdonnell, is a lagoonal equivalent of non-marine Yamba Formation found in southern Australia in inland lakes and swamps (Firman, 1966b, 1972 and 1973, Lindsay 1967, Lindsay and Harris, 1973). Dark grey silt, yellowish brown gypsum sand and off-white gypsum silt at the top of the unit are not differentiated.|16-MAY-23
10273|Le Hunte Formation|Age reasons|Upper Pleistocene - Recent.|16-MAY-23
10273|Le Hunte Formation|References|01/31610; 01/31611; 79/01461|16-MAY-23
10273|Le Hunte Formation|Defn approved by|Approved by Sub-Committee see 72/1371 letter 4/12/1974 from Strat. Index.|16-MAY-23
24359|Linns Springs Member|Name source|After Linns Springs, Wirrealpa 1:50 000 topographic map sheet, GR 943496.|16-MAY-23
24359|Linns Springs Member|Type section locality|361 metres of interbedded black limestone and siltstone exposed in east-west creeks in the Bunkers Range: The Bunkers GR 991392-997391. As amended.|16-MAY-23
24359|Linns Springs Member|Extent|The unit is particularly well developed in the Bunkers Graben, but also occurs further north along the eastern margin of the Flinders Ranges along the Bunkers Range and near Eregunda Creek.|16-MAY-23
24359|Linns Springs Member|Thickness range|361-43 m.|16-MAY-23
24359|Linns Springs Member|Lithology|Interbedded turbiditic couplets of black wackestone-lime mudstone and calcareous siltstone 5-10 cm thick. Some thicker debris flows of intraclast floatstones, grain flows of intraclast-pelloidal packstone and erratic blocks also occur. Some slump folding and sedimentary boudinage. Trace fossils are rare.|16-MAY-23
24359|Linns Springs Member|Relationships and boundaries|The unit is conformably underlain by the Six Mile Bore Member and conformably overlain by the Third Plain Creek Member. The unit is very thin (100 metres) outside the graben to the north, where its deposition was controlled by fault bounded grabens and half grabens. The Linns Springs Member pinches out to the southeast within platform and platform edge facies. It can be distinguished from the Third Plain Creek and Six Mile Bore Members by its more uniform outcrop and from the Six Mile Bore Member by its yellow-grey weathered appearance, as opposed to the Six Mile Bore Member's reddish-brown-grey weathered colour.|16-MAY-23
24359|Linns Springs Member|Age reasons|The unit contains brachiopods and trilobites of Daily's (1956) Faunal Assemblages 4 and 5. It is therefore middle Early Cambrian in age (?Botomian).|16-MAY-23
24359|Linns Springs Member|References|01/31612|16-MAY-23
24359|Linns Springs Member|Resdate|25-OCT-1985|16-MAY-23
11173|Mangaroongah Dacite|Name source|From Mangaroongah paddock on Lake Everard station. Mangaroongah Dacite is the only volcanic rock type occurring in Mangaroongah paddock. The centre of the paddock is at 31o51' latitude, 135o06' longitude.|16-MAY-23
11173|Mangaroongah Dacite|Type section locality|It is not possible to propose a type section that adequately reveals the Mangaroongah Dacite from base to top. However the type area is Palthrobie Hill located at 31o47' lat. And 135o12.5' longitude. The upper contact is well exposed immediately to the north of Lake Everard homestead.|16-MAY-23
11173|Mangaroongah Dacite|Extent|Exposed over an area of 170 km2 in the central eastern portion of the Childara 1:250 000 sheet area and in the extreme south-western portion of the Gairdner 1:250 000 sheet area.|16-MAY-23
11173|Mangaroongah Dacite|Lithology|In hand specimen a dark brown-red porphyry, containing medium to fine grained phenocrysts of plagioclase, K feldspar and patches of green chlorite after clinopyroxene, sitting in an aphanitic groundmass. In thin section the feldspar phenocrysts are largely altered to sericite and have been corroded during devitrification. Fine grained clinopyroxene (augite) is scattered throughout and in places has been altered to chlorite and serpentine. Plagioclase phenocrysts are dominant, while quartz phenocrysts are absent. Phenocrysts make up to 20% of the rock. The groundmass texture is microlitic, with randomly oriented microlites of alkali feldspar interlocking with magnetite, chlorite and aphanitic material that is stained red with limonite, hence giving the rock its red-brown colour. Total feldspar phenocrysts exceed those of augite by 4:1. Locally more acid variants occur with modal quartz as do more basic variants which have a dark green colour and contain a higher % of augite. The upper zone of this unit is highly vesicular, containing flattened vesicles filled with vapour phase minerals such as actinolite, chlorite, epidote, quartz, calcite. Origin: A strongly welded crystal-vitric tuff of ashflow origin. Complete devitrification has obscured original textures.|16-MAY-23
11173|Mangaroongah Dacite|Relationships and boundaries|Conformably overlies the Childera Dacite, often separated by a white airfall tuff bed from this unit. Contact with younger Aburee Rhyolite is complex, but upper zones of Mangaroongah Dacite are invariably highly vesicular, with the development of vapour phase minerals. Thickness at least 200 m.|16-MAY-23
11173|Mangaroongah Dacite|Comments|This unit forms part of the Glyde Hill Complex as previously defined by Blissett.|16-MAY-23
11173|Mangaroongah Dacite|References|79/00495|16-MAY-23
11173|Mangaroongah Dacite|Proposer|Giles C.|16-MAY-23
27190|Maslin Sands|Name source|From "Maslin Beach" a coastal town south of Adelaide.|16-MAY-23
27190|Maslin Sands|Type section locality|The coastal cliffs along Gulf St Vincent between Blanche Point and Ochre Point at Maslin Beach.|16-MAY-23
27190|Maslin Sands|Extent|Eastern side of Cainozoic St Vincent Basin, best developed in Willunga Embayment.|16-MAY-23
27190|Maslin Sands|Thickness range|Range 0-80 m in the Noarlunga and Willunga Embayment.|16-MAY-23
27190|Maslin Sands|Lithology|Friable quartz sands with minor lignites clays and coarse grits. Glauconite is an important constituent in the topmost beds.|16-MAY-23
27190|Maslin Sands|Relationships and boundaries|Unconformably overlies Precambrian/Cambrian succession of Adelaide Fold Belt or disconformably lies on Permian Cape Jervis Beds. In part, a lateral equivalent of the Clinton Formation (Harris, 1966). Overlain by Tortachilla Limestone or Blanche Point Formation.|16-MAY-23
27190|Maslin Sands|Age reasons|Middle to Late Eocene. Spore/Pollen dating in McGowran, Harris & Lindsay (1970).|16-MAY-23
27190|Maslin Sands|Proposed publication|Rep. Inv. Geol. Surv. S. Aust. 50|16-MAY-23
27190|Maslin Sands|Comments|The unit is typically subdivided into two members, North Maslin Sand and South Maslin Sand Members. Cooper (1979) provides the most recent description of unit.|16-MAY-23
27190|Maslin Sands|References|79/20399; 01/31613; 79/02878.|16-MAY-23
27190|Maslin Sands|Status|1|16-MAY-23
26734|Merinjina Tillite|Name source|Merinjina Well (latitude 30o25'40", longitude 139o24'21", Wooltana 1:100 000, Copley 1:250 000 (pub).|16-MAY-23
26734|Merinjina Tillite|Unit history|Corresponds both in total or in part [??] with the unnamed unit labelled Py1 on Copley 1:250k geol. sheet, 1973 - 79/00848.|16-MAY-23
26734|Merinjina Tillite|Type section locality|In two parts 30o20'46", 139o24'23" to 30o20'29", 139o25'44" and 30o19'55", 139o26'06" to 30o19'53" 139o26'06". Balance Rock Creek to Arkaroola Creek to base of conglomeratic quartzite thence 1.2 km to NNE from base of conglomeratic quartzite to top of Blue Mine Conglomerate (Torrension).|16-MAY-23
26734|Merinjina Tillite|Extent|The unit is explored over an area of 8000 km2.|16-MAY-23
26734|Merinjina Tillite|Thickness range|Upper member - 150 m; Middle member - range 240-1500 m; Lower member - 260 m.  Total thickness Merinjina Tillite 650-1500 m.|16-MAY-23
26734|Merinjina Tillite|Lithology|Upper unnamed member - poorly bedded pebble-boulder, greenish shale matrix, tillite, pale green shale at base.  Middle unnamed member - sandy reddish cobble tillite, 2 x 1 m beds of medium quartzite, pebbly quartzite.  Lower unnamed member - dark grey dolomitic pebble-boulder tillite inc[luding?]. 25 m pink quartzite and boulder quartz.|16-MAY-23
26734|Merinjina Tillite|Relationships and boundaries|Underlies Tindelpina Shale Member, of Tapley Hill Formation, with sharply conformable (or disconformable) contact. Overlies Burra Group or Callanna Beds with moderately strong unconformity in type section.|16-MAY-23
26734|Merinjina Tillite|Age reasons|The Merinjina Tillite is overlain by the following stromatolite assemblages from the middle and upper Umberatana Group (Preiss, 1977) Jurusaria burrensis, Inzeria c/f I, tjomusi, Linella Ukka Kulparia Kulparensis, Tungussia etina, Katavia costata, I. conjuncta I. multiplex, Boxonia melrosa, Acaciella augusta and Onachteria utschurica. Baicalia burra is widepsread in the unconformably underlying Burra Group. A geochronometric age of about 790 Ma BP for the Merinjina Tillite is projected from a date of 750+/-53 Ma for the upper? Tapley Hill Formation.|16-MAY-23
26734|Merinjina Tillite|Proposed publication|Bull. Geol. Surv. S. Aust.|16-MAY-23
26734|Merinjina Tillite|References|79/19655; 82/22790; 79/00850; 88/26325; +|16-MAY-23
26734|Merinjina Tillite|Name first published by|Coats R.P., Forbes B.G., 1977|16-MAY-23
11872|Millyera Formation|Name source|See original definition|16-MAY-23
11872|Millyera Formation|Type section locality|See original definition and new reference section.|16-MAY-23
11872|Millyera Formation|Extent|Lake Millyera|16-MAY-23
11872|Millyera Formation|Thickness range|2-3 m.|16-MAY-23
11872|Millyera Formation|Lithology|Redefined to exclude Section 5 of Callen & Tedford (1976), Units 5-7 in Section 4 and "Millyera Formation" of sections 6 and 7.|16-MAY-23
11872|Millyera Formation|Relationships and boundaries|Overlain by Eurinilla Formation, unconformably overlies Namba Formation (erosional contact). Relationship with Coomb Spring Formation uncertain, but probably younger.|16-MAY-23
11872|Millyera Formation|Age reasons|See Relationships and boundaries. Palaeomagnetic results: Normal magnetism (J.M.Bowler, personal comment, 1982, Dept Biogeogr./Geomorph. R.S. Pac. S., ANU) - probably Late Pleistocene at type section. Older than, or intertongues with, Eurinilla Formation, older than Coonarbine Formation.|16-MAY-23
11872|Millyera Formation|References|85/24691; 79/00723; 83/23555|16-MAY-23
34768|Mimili Formation|Name source|The formation is named after the Mimili Aboriginal settlement.|16-MAY-23
34768|Mimili Formation|Type section locality|Surface to 1018 m in Munyarai 1.|16-MAY-23
34768|Mimili Formation|Extent|Seismic data suggest that the Mimili Formation is restricted to the Munyarai Trough area.|16-MAY-23
34768|Mimili Formation|Thickness range|The Mimili Formation is over 1018 m thick in Munyarai 1, with the top eroded; from seismic data it may be up to 2000 m thick.|16-MAY-23
34768|Mimili Formation|Lithology|Tucker (1994) recognised three units in the type section. The lowermost consists of fine to medium-grained micaceous and occasionally calcareous clean arkosic sandstone. The middle unit is fossil-bearing and composed of interbedded greenish grey micaceous, calcareous mudstone with minor siltstone and fine to medium-grained sandstone. The uppermost unit is generally ferruginised, muddy brown arkosic sandstone.|16-MAY-23
34768|Mimili Formation|Depositional environment|Planar and ripple laminations are present in the basal part of the sequence, but the vertebrate faunas are found elsewhere in Australia in both marine and freshwater palaeoenvironments (Long et al., 1988). From a regional perspective, a non-marine palaeoenvironment is favoured (Tucker, 1994).|16-MAY-23
34768|Mimili Formation|Relationships and boundaries|The upper contact is not known, but is presumed to be unconformably overlain by Permian, Cretaceous or younger sediments. The basal contact with the Blue Hills Sandstone is disconformable, but has not been cored. The formation may correlate with the Pertnjara Group and possibly the Mereenie Sandstone of the Amadeus Basin.|16-MAY-23
34768|Mimili Formation|Age reasons|Late Devonian, Frasnian (375-360 Ma). A vertebrate fish fauna indicates an Early to Middle Devonian (Eifelian) age, and palynology indicates a Late Devonian (Frasnian) age - the latter is considered more reliable. The upper and lower parts of the sequence are barren, and thus the age spanned by the Mimili Formation is wider than indicated by fossils.|16-MAY-23
34768|Mimili Formation|Defn author|J.G.G.Morton,  (1997). Chapter 6 IN: The petroleum geology of South Australia. Volume 3: Officer Basin.South Australia. Department of Mines and Energy Resources. Report Book 1997/19, p83-84.|16-MAY-23
34768|Mimili Formation|Comments|This name is introduced here for the youngest sandstone unit in the Officer Basin.|16-MAY-23
34768|Mimili Formation|References|Long, J.A., Turner, S. and Young, G.C., 1988. A Devonian fish fauna from subsurface sediments in the eastern Officer Basin, South Australia. Alcheringa, 12:61-78.  **Tucker, L.R., 1994. Devonian geology of the Munyarai Trough. South Australia. Department of Mines and Energy. Report Book, 94/10.|16-MAY-23
11952|Mirackina Conglomerate|Name source|Mirackina 1:63 360 sheet area on which the type section is situated.|16-MAY-23
11952|Mirackina Conglomerate|Unit history|May be equivalent to the Mt Alice Conglomerate and the unnamed channel conglomerates on Torrens.|16-MAY-23
11952|Mirackina Conglomerate|Type section locality|Latitude 28o14'5"S and longitude 134o41'24"E. The southern end of an elongate mesa, 19.5 km on a bearing of 268oT from Mt Barry H.S.|16-MAY-23
11952|Mirackina Conglomerate|Extent|Confined to the Mirackina Palaeochannel and its tributaries - a palaeodrainage feature in the Stuart Range area.|16-MAY-23
11952|Mirackina Conglomerate|Thickness range|11 m in Type Section. Ranging from 2 to 15 m.|16-MAY-23
11952|Mirackina Conglomerate|Lithology|The Mirackina Conglomerate comprises conglomerates with silcrete, quartz and bleached shale clasts, massive and cross-bedded medium to coarse grained quartz sandstones and minor siltstones and shales. It is variably cemented by silica and iron oxides, and generally strongly silicified to a massive quartzose silcrete in the uper part.|16-MAY-23
11952|Mirackina Conglomerate|Relationships and boundaries|Unconformably overlies bleached Lower Cretaceous Bulldog Shale and Oodnadatta Formation. Overlain disconformably by Mt Willoughby Limestone.|16-MAY-23
11952|Mirackina Conglomerate|Age reasons|Tertiary, probably Neogene.|16-MAY-23
11952|Mirackina Conglomerate|Defn author|Barnes L.C., Pitt G.M., 1976|16-MAY-23
11952|Mirackina Conglomerate|Proposed publication|Quart. Geol. Notes Geol. Surv. S. Aust. 59|16-MAY-23
11952|Mirackina Conglomerate|Name first published by|Barnes L.C., Pitt G.M., 1976|16-MAY-23
24617|Moolawatana Suite|Name source|Moolawatana Station 9 km E of Mount Babbage, on the Moolawatana 1:100 000 sheet of the Callabonna 1:250 000 map.|16-MAY-23
24617|Moolawatana Suite|Unit history|Moolawatana was first used by David (1926) as Moolawatana Glacial beds, a term no longer used and now superseded.|16-MAY-23
24617|Moolawatana Suite|Type section locality|The best section exhibitiing all five phases can be seen between Petermorra Springs to White Well Bore to Wattleowie Hut ruins to Birthday Well.|16-MAY-23
24617|Moolawatana Suite|Extent|The three main phases of granite emplacement (Yerila Granite, Wattleowie Granite and Terrapinna Granite) occur widely in both the Mount Babbage and Mount Painter Inliers, the Terrapinna Granite predominating. The minor phases (Prospect Hill Granite and White Well Granite) are restricted to the Mount Babbage Inlier. Granitoids of the Moolawatana Suite are believed to be extensive in the subsurface north and east of the two inliers (Callen et al., 1990; Sheard and Cockshell, 1992).|16-MAY-23
24617|Moolawatana Suite|Lithology|The Moolawatana Suite consists of complex of coeval felsic intrusive rock types. Three main and two minor rock type phases are evident in the well exposed Mount Babbage Inlier. Primary textures and composition vary within the three major lithotypes, which have been further modified with the development of a pervasive mica foliation during the Delamerian Orogeny.  The five phases are: 1. Yerila Granite: lineated tabular feldspar granite, usually melanocratic, and composed of microcline laths, albite, quartz, biotite and muscovite, with accessory apatite, zircon and tourmaline. Shown as map symbol pCy on the Mount Painter Province 1:125 000 geological map (Coats and Blissett, 1971).  2. Wattleowie Granite: weakly gneissic, coarse-grained white granite and adamellite, and composed of microcline, quartz, oligoclase, albite, and biotite, with accessory zircon, apatite and opaque grains. Shown as map symbol pCw on the Mount Painter Province 1:125 000 geological map (Coats and Blissett, 1971).  3. Terrapinna Granite: massive pink-weathering grey to white very coarse-grained rapakivi granite to adamellite, and composed of ovoid microcline and round quartz phenocrysts set in a coarse-grained mosaic of K-feldspar, quartz, biotite, muscovite, and albite, with accessory tourmaline, opaques, apatite and zircon. Shown as map unit symbol pCt on the Mount Painter Province 1:125 000 geological map (Coats and Blissett, 1971).  4. Prospect Hill Granite: as defined (M.J. Sheard, C.M. Fanning and R.B. Flint 1992, South Australia).  5. White Well Granite: as defined (Geological Survey Quarterly Geological Notes, 123: 18-31).|16-MAY-23
24617|Moolawatana Suite|Relationships and boundaries|Within the Mount Babbage Inlier intrusives of the suite form a series of east-west elongate bodies - a distribution pattern in part due to effects of the Delamerian Orogeny. Yerila Granite is considered the oldest granitoid, it is intruded by Terrapinna Granite, with xenoliths of Yerila Granite in both the Wattleowie and Terrapinna Granites. Xenoliths of Wattleowie Granite also occur in Terrapinna Granite (Coats and Bliissett, 1971; Sheard and Callen (in prep.). Xenoliths are usually restricted to within 1-10 m of an intrusive contact. In most cases contacts between the various phases are sharp, however, contacts between Wattleowie and Terrapinna Granites range from sharp to diffuse. All intrusive phases are cross-cut by related coarse-grained pegmatite dykes which are usually moderately deformed. Younger pegmatite dykes, which are only weakly deformed are related to the Cambrian-Ordovician Mudnawatana Tonalite (Teale, 1979).  Both the Prospect Hill and White Well Granites intrude the Petermorra Volcanics, and their characteristics are consistent with intrusion at high levels within the crust. Their relationship to each other and the three other phases is not known. The Yerila, Wattleowie and Terrapinna Granites probably represent deeper level intrusions. Their contacts with older (?Palaeoproterozoic) basement metasediments are also intrusive, with numerous rafts of metasediments.|16-MAY-23
24617|Moolawatana Suite|Age reasons|More robust U-Pb zircon analyses are given in Johnson (1980), Thornton (1980), sites 1 and 2 respectively on Figure 2, and Cooper et al. (1982). The Yerila Granite has an upper concordia intercept of 1556+/-10 Ma (Johnson, 1980, and as modified by Cooper et al., 1982), whilst a melanocratic phase, we consider to be equivalent to the Terrapinna Granite, has an upper intercept of 1556+/-4 Ma (Thornton, 1980). The lower concordia intercepts of 344+/-23 Ma and 77+/-11 Ma respectively may reflect younger Pb loss events as discussed by Cooper et al. (1982). It must be noted that bulk zircon fractions containing many millions of grains were analysed and so the ages may be biased by the inclusion of grains not formed in total at the time of primary igneous crystallisation. Never the less, the ages of 1556+/-10 Ma and 1556+/-4 Ma provide the best estimates for the crystallisation ages of the Yerila and Terrapinna Granites.  Terrapinna Granite in Skelton 2: A homogeneous population of zircons was separated from sample 6938 RS 25, Terrapinna Granite in Skeleton 2. The zircons are in general structureless clear grains, a deep hyacinth in colour and with pyramidal terminations, or are fractured parts of such grains. The zircons are interpreted to have a simple igneous origin.  It is consluded from the data at hand that Palaeozoic event(s) have influenced the loss of radiogenic Pb for some of the more discordant zircon analyses from sample 6938 RS 25. The best estimate for the crystallisation age of the zircons is given by those that have suffered little or no loss of radiogenic Pb, or Pb loss near the present day. The upper intercept of 1557+/-6 Ma for the regression line fitted to five of the six analyses with essentially a zero lower intercept (Fig. 4d) is interpreted as the crystallisation age for the zircons and enclosing Terrapinna Granite in Skeleton 2.  The Mount Babbage and Mount Painter Inliers, represent a former northwesterly extension of the Curnamona Craton. Volcanics within the inliers have a broadly similar stratigraphic position and geochemistry to those of the Curnamona Craton and Gawler Craton (Giles and Teale, 1979, 1981). However, from recent U-Pb zircon isotopic studies (as presented here) a much more complicated Mesoproterozoic succession can be inferred with probably several volcano-sedimentary sequences (Fig. 5). A succession in the Mount Painter Inlier, including the Pepegoona Porphyry, parts of the Mount Neill Granite Porphyry, Freeling Heights Quartzite and Yagdlin Phyllite of Coats and Blissett (1971) has an age of ~1575 Ma.|16-MAY-23
24617|Moolawatana Suite|Correlations|Outcrops of porphyritic rhyolite from Harts Creek and dacitic tuff near the Gunsight Prospect have U-Pb zircon crystallisation ages of 1576+/-2 and 1575+/-14 Ma (Teale, in prep. b). This is significantly younger than the extrusive age of ~1592 Ma for the Gawler Range Volcanics of the Gawler Craton and ?volcanism of the Curnamona Craton. The Petermorra Volcanics of the northern Mount Babbage Inlier represent yet another, younger, volcano-sedimentary sequence with an age of 1560+/-2 Ma. High-level plutons of the Prospect Hill Granite and White Well Granite intrude the sequence. Neither has been dated, but are assumed to be of similar age to other, deeper-level granitoids in the region that have statistically identical U-Pb zircon ages of 1556+/-4, 1556+/-10 and 1557+/-6 Ma; the Terrapinna Granite, Yerila Granite and adamellite in Skeleton 2 respectively. Along with the Wattleowie Granite, the Terrapinna Granite, Yerila Granite, Prospect Hill Granite and White Well Granite collectively define the cogenetic, anorogenic Moolawatana Suite.  The Petermorra Volcanics and marginally younger widespread intrusives of the Moolawatana Suite thus form a major episode of volcano-plutonic activity at 1560-1555 Ma in the Mount Babbage and Mount Painter Inliers and also probably in the northern Curnamona Craton. This activity is significantly younger than both the ~1575 Ma and 1590 Ma igneous episodes.|16-MAY-23
24617|Moolawatana Suite|Proposed publication|South Australia. Geological Survey Quarterly Geological Notes, 123: 18-31.|16-MAY-23
24617|Moolawatana Suite|Category|2|16-MAY-23
24617|Moolawatana Suite|Proposer|Sheard M.J., Fanning C.M., Flint R.B.,|16-MAY-23
24617|Moolawatana Suite|Resdate|15-JAN-1992|16-MAY-23
24617|Moolawatana Suite|Reserved? Yes/No|Yes|16-MAY-23
27294|Mooracoochie Volcanics|Name source|Mooracoochie Hill, latitude 27o48'S, longitude 139o41'E on the Pastoral Plan 15.|16-MAY-23
27294|Mooracoochie Volcanics|Type section locality|Gidgealpa-3 from 2373 m to 3333 m.|16-MAY-23
27294|Mooracoochie Volcanics|Extent|Subsurface on Gidgealpa-1, -14, Spencer-1, Kalladeina-1. Possibly also Cuttapirrie-1, Coongie-1, Paning-1, and Pinna-1 where the volcanics should be regarded as Mooracoochie Volcanics equivalent. Andesites intersected at Murteree A-1 which are lithologically different from the Mooracoochie Volcanics may be equivalent.|16-MAY-23
27294|Mooracoochie Volcanics|Thickness range|In the type section it is 960 m (3149 ft) thick. The range is unknown as the base has not been penetrated.|16-MAY-23
27294|Mooracoochie Volcanics|Lithology|Gidgealpa-3 contains tuff, lapillituff, trachyte, crystal tuff, sodic trachyte, and rhyolite. Conglomerate, and shale also occur within the section. Sericitisation, and chloritisation, with dolomite and calcite veins, are common. Spherulitic agglomerate blocks occur in Gidgealpa-1, obsidian and vitric rock fragments are also common.|16-MAY-23
27294|Mooracoochie Volcanics|Relationships and boundaries|The base has not been penetrated, the top is erosional, though in the type section there are interbeds of dolomite and limestone.|16-MAY-23
27294|Mooracoochie Volcanics|Age reasons|The volcanics are overlain by early Middle Cambrian carbonates of the Kalladeina Beds, the oldest of which are dated as Templetonian. The volcanics are therefore no younger than Templetonian, they are thought to be Early Cambrian but may be older.|16-MAY-23
27294|Mooracoochie Volcanics|Proposed publication|Quarterly geol Notes, Geological Survey of SA, No. 86, March 1983|16-MAY-23
27294|Mooracoochie Volcanics|Proposer|Gatehouse C.G.|16-MAY-23
26042|Moornaba Sand|Name source|After Moornaba Rockhole which is within the main area of occurrence of the unit on the Fowler 1:250 000 map area.|16-MAY-23
26042|Moornaba Sand|Type section locality|Dune crest near junction of Koonibba-Inila Rock Waters track with Vermin Proof Fence, and at intersection of north-south road and Vermin Proof Fence 11 km northeast of Charoba Tank.|16-MAY-23
26042|Moornaba Sand|Extent|Western Eyre Peninsula marginal to the Gawler Ranges and extending northwest beyond Lake Tallacootra.|16-MAY-23
26042|Moornaba Sand|Thickness range|A thin veneer on Wiabuna Formation on the margins of the large dune fields. Up to 10 metres within the dune fields proper.|16-MAY-23
26042|Moornaba Sand|Lithology|Aeolian off-white and pale yellowish brown quartz sand overlying darker yellow and orange coloured quartz sand with soft carbonate pipes in some places.|16-MAY-23
26042|Moornaba Sand|Relationships and boundaries|Overlies Wiabuna Formation inland. The upper pale yellowish brown quartz sand occupies a similar position in sequence to Semaphore Sand on the coastal margin as described in Firman, 1966a, and 1969.|16-MAY-23
26042|Moornaba Sand|Age reasons|Recent.|16-MAY-23
26042|Moornaba Sand|Defn author|Firman J.B., 1974|16-MAY-23
26042|Moornaba Sand|Proposed publication|Quarterly Geological Notes of the Geological Survey of SA: No. 52|16-MAY-23
26042|Moornaba Sand|Defn approved by|Gatehouse C.G. (approved by Sub-Committee letter 4/12/74 from Strat. Index - see 72/1371).|16-MAY-23
12300|Moorowie Formation|Name source|Moorowie Spring at eastern entrance to Mt. Chambers Gorge.|16-MAY-23
12300|Moorowie Formation|Unit history|A unit at the top of the Hawker Group, the Moorowie Formation, was introduced without definition by Mount (1970) and was first published by Forbes (1971) before use on the Copley 1:250,000 geological map sheet by Coats (1973). The name has since been widely used. The formation is here defined, together with five named constituent members.|16-MAY-23
12300|Moorowie Formation|Geomorphic expression|Low hills and ridges, dissected by ephemeral streams and narrow ravines.|16-MAY-23
12300|Moorowie Formation|Type section locality|Composite section comprising 190 to 320 ft (57.9 to 97.5 m) (30°59'58.14"S, 139°15'30.88"E to 30°59'53.86"S, 139°15'28.44"E) in Section Q for the basal beds, as partly repeated and extended by Section H, 0 to 792 ft. (0 to 241.4 m) 30°59'47.36"S, 139°15'43.04"E to 30°59'56.33"S, 139°15'59.89"E, and Section G, 0 to 476 ft (0 to 145.1 m) (incomplete; part faulted at top). 30°59'33.14"S, 139°15'57.49"E to 30°59'37.98"S, 139°16'11.93"E. Reference sections: Section X, -22 to 120 ft (faulted?) (-6.7 to 36.6 m) 30°59'1.65"S, 139°16'14.12"E to 30°59'5.78"S, 139°16'18.58"E), Section Y, 8 (fault) to 368 ft (2.4 to 112.2 m) (30°58'39.81"S, 139°16'47.11"E to 30°58'44.19"S, 139°16'40.80"E, Section I, 70 to 222 ft. (21.3 to 67.7 m) 30°59'2.12"S, 139°16'10.24"E to 30°59'3.12"S, 139°16'12.72"E.|16-MAY-23
12300|Moorowie Formation|Extent|Along the crest of the low range from Mt. Chambers Gorge southward towards Mt. Frome.|16-MAY-23
12300|Moorowie Formation|Thickness range|Composite thickness, possibly faulted, from Sections H, Q is 334 m (1096 ft; a probable maximum). Estimated average ~237 m (778 ft) from 17 other variably faulted sections measured across partly lenticular beds.|16-MAY-23
12300|Moorowie Formation|Lithology|Massive to thick bedded, cliff forming, peloid limestones at base; buff, pink to light grey, part silty to quartz granule-rich, part oolitic, with cross-bedded arkosic sands, ripple marks, buff silty dolostone intraclasts, and abundant archaeocyaths. Interbed above of ferric red to khaki green, finely micaceous siltstones with thin limestone interbeds at base, abundant ripple marks, mud cracks, and rare trilobite tracks. Overlain by a megabreccia of massive, poorly bedded, buff or grey to red, angular to sub-rounded cobbles to boulders of (i) clean, light grey archaeocyath limestone and (ii) dark brown silty to quartz granule-rich (arkosic) limestones, reworked from the breccia matrix. Superseded by massive, buff, light to dark grey or ferric red, richly fossiliferous, peloidal to part oolitic archaeocyath limestones, with siliciclastic silt to grit stringers, silty dolostone intraclasts, and conglomerates of grey limestone boulders to 3 m in a quartz-granule rich, red to buff, silty carbonate matrix. Purple-red micaceous siltstones above with thin grey limestone laminations at base. Local thin polymict conglomerate lenses with light grey limestone cobbles and quartz granule-rich limestone pebbles in a silty lime matrix. Formation capped by a massive, cliff forming, homogeneous, pale grey, finely laminated to flaggy or medium bedded, microcrystalline microbial limestone with thin clay partings. No obvious macrofossils.|16-MAY-23
12300|Moorowie Formation|Depositional environment|High-energy intertidal carbonate platform margin or reef barrier set between a shallow restricted marine ramp, and landward to backreef shelf bioherms and ooid-peloid shoals, channelised tidal flats with penesaline lagoons, passing to supratidal sabkhas and alluvial fans. Local extrusive salt domes.|16-MAY-23
12300|Moorowie Formation|Relationships and boundaries|Terminal unit of the Hawker Group, as a conformable passage between Mernmerna Formation below and Billy Creek Formation above. Basal contact at transition from dark grey flaggy limestones and slump talus beds of the Mernmerna Formation, into massive light grey peloid limestones. Upper contact at the top of a maker bed of finely laminated to flaggy microcrystalline microbial limestone, below red-brown to green shales of the overlying Billy Creek Formation.|16-MAY-23
12300|Moorowie Formation|Structure and Metamorphism|Moderately dipping, thick beds defining broad fold limbs and cores; partly faulted.|16-MAY-23
12300|Moorowie Formation|Age reasons|Lower Cambrian, Stage 4, within the Pararaia janeae trilobite Zone (Figure 2 of Jago et al., this volume).|16-MAY-23
12300|Moorowie Formation|Correlations|Related to the upper Wilkawillina Limestone. Possible equivalent deposits in Bunkers Graben and at Reaphook Hill.|16-MAY-23
12300|Moorowie Formation|Defn author|T. J. Mount,  8-JAN-2019, after Mount (1970).|16-MAY-23
12300|Moorowie Formation|Comments|The name Moorowie Formation has been widely used since it was introduced without definition by Mount (1970).|16-MAY-23
12300|Moorowie Formation|References|Coats, R. P. (1973). Copley map sheet. Adelaide, SA: Geological Survey of South Australia, Geological Atlas 1:250 000 Series. Sheet SH54-9.  **Forbes, B. G. (1971). A table of Adelaidean and Cambrian stratigraphic names. Geological Survey of South Australia, Quarterly Geological Notes, 38 (1-2), 5-6.  ** Jago, J. B., Gehling, J. G., Betts, M. J., Brock, G. A., Dalgarno, C. R., Garcia-Bellido, D. C., .., Paterson, J. R. (2019). The Cambrian System in the Arrowie Basin, Flinders Ranges, South Australia. Australian Journal of Earth Sciences. doi:10.1080/08120099.2018.1525431   **Mount, T. J. (1970). Geology of the Mt. Chambers Gorge region (BSc. (Honours) thesis, unpublished).Adelaide, SA: University of Adelaide. http:hdl.handle.net/2440/67162.  **T. J. Mount, J. B. Jago, N. R. Langsford & C. R. Dalgarno (2019): Geological setting of the Moorowie Formation, lower Cambrian Hawker Group, Mt Chambers Gorge, eastern Flinders Ranges, South Australia, Australian Journal of Earth Sciences, DOI: 10.1080/08120099.2019.1586771.|16-MAY-23
26314|Moralana Supergroup|Name source|The Moralana Supergroup includes all Cambrian rocks deposited in the Adelaide Geosyncline. From "Moralana" Station in the central Flinders Ranges.|16-MAY-23
26314|Moralana Supergroup|Type section locality|Hawker Group/Lake Frome Group/Billy Creek Formation/Wirrealpa Limestone - central Flinders Ranges. Normanville Group/Kanmantoo Group - Fleurieu Peninsula.|16-MAY-23
26314|Moralana Supergroup|Extent|Thickest in Adelaide Geosycline; thinner on adjacent platforms (Hawker to Lake Frome Groups). Kanmantoo Group known only in south-east portion of Adelaide Geosyncline.|16-MAY-23
26314|Moralana Supergroup|Lithology|Shelf and basin carbonates dominate in Hawker and Normanville Groups. Redbeds and sandstones dominate in Lake Frome Group. Very thick metamorphosed sandstone/siltstone sequence in Kanmantoo Group.|16-MAY-23
26314|Moralana Supergroup|Relationships and boundaries|Regionally disconformable on Wilpena Group.|16-MAY-23
26314|Moralana Supergroup|Age reasons|Early to Middle Cambrian.|16-MAY-23
26314|Moralana Supergroup|Proposed publication|Trans. R. Soc. SA (Brief Communication)|16-MAY-23
26314|Moralana Supergroup|Proposer|Preiss W.V.|16-MAY-23
27201|Mordinyabee Rhyodacite|Name source|Origin: As a strongly welded vitric-crystal ashflow tuff. The original textures have been largely obscured by devitrification. Derivation: From Mordinyabee dam and hill on Lake Everard station. These two features occur within the main outcrops of the Mordinyabee Rhyodacite. Mordinyabee hill is located at 31o33.25' latitude and 135o19.5' longitude.|16-MAY-23
27201|Mordinyabee Rhyodacite|Type section locality|Typical Mordinyabee Rhyodacite can be seen outcropping in the hills 0.5 km south of Mordinyabee dam which is located at 31o33' latitude and 135o18.25' longitude.|16-MAY-23
27201|Mordinyabee Rhyodacite|Extent|Covers an area of 53 km2 on the central west of the Gairdner 1:250 000 Sheet area. The outcrop is mainly confined to Mordinyabee peninsular but does extend westwardsas a loing linear outcrop.|16-MAY-23
27201|Mordinyabee Rhyodacite|Lithology|A red-brown porphyry sometimes with a greenish-grey tinge containing medium to fine grained phenocrysts of alkali feldspar, plagioclase and green patches of chlorite after clinopyroxene sitting in a featureless aphanitic groundmass. In thin section the alkali feldspar and plagioclase occurs as distinct medium grained euhedral crystals and as glomeroporphyritic aggregates. The alkali feldspar is extensively sericitised and corroded. Plagioclase phenocrysts are dominant. Chlorite is commonly seen, replacing clinopyroxene. The devitrified groundmass exhibits a microgranular texture and the feldspar component of this groundmass is stained red with limonite. Phenocrysts make up approximately 7% of rock.|16-MAY-23
27201|Mordinyabee Rhyodacite|Relationships and boundaries|Underlies the Yantea Rhyodacite and is separated from this unit by a 4 m ashflow lithic lapilli tuff. Relationships with older units are not seen but this unit undoubtedly overlies the Wheepool Rhyolite (Blissett) and has been subject to erosion prior to the outpouring of the Yantea Rhyodacite. The thickness is uncertain but reaches at least 100 m in places.|16-MAY-23
27201|Mordinyabee Rhyodacite|Age reasons|This unit forms part of the Glyde Hill Complex as defined by Blissett. Age upon geochronological grounds is mid-Carpentarian, roughly 1550 Ma.|16-MAY-23
27201|Mordinyabee Rhyodacite|Defn author|Giles C.W., 1977|16-MAY-23
27201|Mordinyabee Rhyodacite|Proposed publication|SA Department of Mines, Quarterly Notes: No. 61|16-MAY-23
79616|Mount Friday Formation|Name source|The name is derived from Mount Friday, which is within the Hiltaba Nature Reserve at GDA94, zone 53, 513820 mE, 6435988 mN.|16-MAY-23
79616|Mount Friday Formation|Unit history|First described as an unnamed subunit of the Paney Rhyolite Member in Werner et al. (2016a). Subsequently described for the first time as Mount Friday Formation in Werner et al. (2016b). Used as a stratigraphic unit on the Peltabinna 1:75 000 map sheets (Pawley et al., 2017; Werner et al., 2017a) and formally defined and described in detail in Werner et al. (2017b).|16-MAY-23
79616|Mount Friday Formation|Geomorphic expression|The volcaniclastic-sedimentary deposits of the Mount Friday Formation typically form subdued, rubbly to bouldery outcrops and colluvium-covered subcrops in the low-lying areas between the hill-forming volcanic rocks of the underlying Eucarro Rhyolite and the overlying Yardea Dacite.|16-MAY-23
79616|Mount Friday Formation|Type section locality|The type area of the Mount Friday Formation is defined as the ~3.5 km long and up to 120 m wide southeast-trending outcrop strip east of Mount Friday extending from GDA94, zone 53, 516115 mE, 6436048 mN to 518349 mE, 6433576 mN. The type area is in the immediate vicinity of the Hiltaba - Yardea road. Access on foot or by vehicle should be arranged by the Nature Foundation SA who manages Hiltaba Nature Reserve. The Mount Friday Formation intersected in drillhole MSDP07 (drillhole 288773; GDA94 zone 53 527372 mE 6420351 mN; interval 143.7-231.6 m) is proposed as a reference section. Drillcore viewing can be arranged at the South Australia Drill Core Reference Library.|16-MAY-23
79616|Mount Friday Formation|Description at type locality|Bouldery to rubbly discontinuous outcrops of mainly coarse-grained volcaniclastic-sedimentary rocks. Continuous diamond drillcore from MSDP05 and MSDP07.|16-MAY-23
79616|Mount Friday Formation|Extent|The Mount Friday Formation is exposed as a discontinuous, narrow, ~3.5 km long and up to 120 m wide, southeast-trending outcrop belt near Mount Friday. It was also intersected in drillholes YRT 19, MSDP07 and MSDP05, increasing the known lateral extent of the Mount Friday Formation along strike to about 30 km. Together with the stratigraphically equivalent Mount Double Ignimbrite and unnamed volcaniclastic-sedimentary rocks in the Nonning ¿ Mount Ive area, these volcaniclastic deposits form a lithologically distinct and regionally extensive marker horizon that can be traced for at least 150 km along the southern margin of the Gawler Range Volcanic Province.|16-MAY-23
79616|Mount Friday Formation|General description|More occurrences of fluvially reworked volcaniclastic and volcanogenic sedimentary deposits (Mount Friday Formation), and primary pyroclastic deposits (Mount Double Ignimbrite), are likely to be discovered and recognised between the Eucarro Rhyolite and the Yardea Dacite in future outcrop mapping and drilling across the Gawler Range Volcanic Province.|16-MAY-23
79616|Mount Friday Formation|Thickness range|The Mount Friday Formation crops out in its type area as an erosional remnant and has a maximum preserved thickness of about 10-20 m. In drillhole MSDP07 the Mount Friday Formation forms a ~90 m thick succession of volcaniclastic-sedimentary rocks between the Yannabie Rhyolite Member and the Pondanna Dacite Member.  In drillhole MSDP05 volcaniclastic-sedimentary rocks of the Mount Friday Formation occur in the interval 125.10¿220.95 m, where they are intercalated with coherent and autoclastic volcanics of the Yannabie Rhyolite Member. Within this ~96 m thick interval volcaniclastic facies makes up about 35 m of the total thickness.|16-MAY-23
79616|Mount Friday Formation|Lithology|The Mount Friday Formation consists at the outcrop type locality predominantly of massive, very poorly sorted, matrix-supported, diamictic volcanic lithic breccias grading locally into massive, clast-bearing volcanic mudstones (debris and mud flow deposits). It locally contains intercalations of better sorted, clast-supported volcanic conglomerates, thin intervals of fine- to coarse-grained, massive or thinly bedded to laminated volcanic sandstones, and rare laminated volcanic siltstones. Lithic clasts are almost entirely composed of massive or flow-banded, quartz- and feldspar-phyric, originally glassy rhyolite (reworked Paney Rhyolite Member). The matrix of the volcaniclastic deposits is mainly composed of fine-grained, originally glassy, now devitrified and/or recrystallised rhyolite detritus. Some samples contain bubble wall and bubble junction shards and represent a minor pyroclastic component within these volcaniclastic deposits.  The Mount Friday Formation intersected in drillholes MSDP07 (reference drillhole) and MSDP05 also consists predominantly of massive, very poorly sorted, matrix-supported, diamictic volcanic breccias and intercalated massive to laminated mudstones. It also contains volcanic sandstones and conglomerates. The lithic clasts within volcanic breccias are mainly derived from the Paney Rhyolite Member or the Yannabie Rhyolite Member. Intraformational rip-up clasts of massive or laminated mudstones are very common. In drillhole MSDP05, volcanogenic sedimentary material also forms clastic dykes at the top of fractured coherent rhyolite and the peperitic matrix of autoclastic rhyolite. Some of the mudstones show soft-sediment deformation and mobilisation structures such as injection into overlying deposits due to density loading and reverse density stratification. Some tuffaceous deposits contain glass shards and pumice fragments as minor pyroclastic components.|16-MAY-23
79616|Mount Friday Formation|Depositional environment|Soft sediment deformation features such as injection of mud into overlying sandy material, downward sinking of sand into underlying muddy deposits, and disintegration of sedimentary structures due to liquefaction, show that the Mount Friday Formation is mainly composed of water-lain deposits. Parts of these deposits behaved plastically due to their high water content and were mobilised during ongoing deposition as a result of reverse density stratification and dewatering. The majority of the deposits can be interpreted as resedimented autoclastic volcanic material. The poorly sorted, matrix supported volcanic breccias to mudstones were probably deposited by debris and mud flows. Better sorted massive volcanic conglomerates and sandstones probably represent hyperconcentrated flow deposits. Traction current structures such as cross-bedding or ripple cross-lamination were not observed in the Mount Friday Formation, implying that more dilute fluvial stream flow systems were probably not widely established during deposition. Rare horizontally-bedded sandstones probably reflect deposition under upper flow regime conditions in hyperconcentrated flows. Between these episodes of high-energy mass-flow deposition, laminated fine-grained sandstones, siltstones and mudstones were probably deposited in short-lived, pool- or pond-sized water bodies. Some of the small, normally graded sandy laminae within these muddy deposits probably represent microturbidites. These fine-grained deposits were commonly reworked during subsequent high-energy flow events as evidenced in the occurrence of numerous intraformational mud rip-up clasts. Rock relationships such as interbedding and mingling of volcanogenic sedimentary deposits with coherent and autoclastic volcanics (drillhole MSDP05) show that locally alluvial-fluvial sedimentation was contemporaneous with subaerial extrusion of lava, leading to the formation of peperite-like rocks. Parts of the Mount Friday Formation contain variable amounts of bubble wall shards and pumice clasts. These pyroclastic components indicate that explosive volcanism was contemporaneous with sedimentation and extrusion of rhyolitic lavas during deposition of the Mount Friday Formation. These observations suggest that the deposits of the Mount Friday Formation record deposition in a continental subaerial fluvio-lacustrine setting within a volcanically active environment. Episodic rainfall probably triggered reworking of autoclastic volcanic deposits on top of the Eucarro Rhyolite lava flow, leading to deposition of mainly poorly sorted and coarse-grained material from high-concentration sediment gravity flows. Input of pyroclastic material from explosive volcanic activity intermittent throughout the dominantly effusive volcanism appears to have been rather sporadic and only a subordinate detrital source for the bulk of the Mount Friday Formation, but was more significant at times.|16-MAY-23
79616|Mount Friday Formation|Relationships and boundaries|In outcrop near Mount Friday the Mount Friday Formation overlies coherent and autobrecciated facies of the Paney Rhyolite Member. The contact is erosional and probably slightly disconformable. The present erosion surface forms the preserved top of the outcropping Mount Friday Formation and its original upper contact to the overlying Pondanna Dacite Member is not preserved. The outcropping part of the Mount Friday Formation is in fault contact (Eurilla Fault) with the Pondanna Dacite Member.  In drillhole MSDP07 the Mount Friday Formation overlies with an erosional contact coherent volcanic facies of the Yannabie Rhyolite Member. The contact with the overlying basal welded autobreccia of the Pondanna Dacite Member appears to be conformable. In drillhole MSDP05 volcaniclastic-sedimentary rocks of the Mount Friday Formation are intercalated and partly mingled (peperites) with coherent and autoclastic facies of the Yannabie Rhyolite Member, demonstrating local interfingering relationships between these two stratigraphic units.|16-MAY-23
79616|Mount Friday Formation|Identifying features|The Mount Friday Formation consists of volcanogenic sedimentary and resedimented volcaniclastic deposits which are underlain and overlain by coherent and autoclastic volcanic rocks.|16-MAY-23
79616|Mount Friday Formation|Structure and Metamorphism|The rocks of the Mount Friday Formation were not subjected to ductile deformation and are unmetamorphosed.|16-MAY-23
79616|Mount Friday Formation|Age reasons|The age of the Mount Friday Formation is constrained by CA-TIMS U-Pb age dates for the underlying Eucarro Rhyolite (1587.5 ± 0.6 Ma) and the overlying Yardea Dacite (1587.2 ± 0.5 Ma) (Jagodzinski et al., 2016).|16-MAY-23
79616|Mount Friday Formation|Correlations|The Mount Friday Formation is correlated with the Mount Double Ignimbrite near Paney (Allen et al., 2003 and 2008) and unnamed volcaniclastic-sedimentary rocks in the Nonning ¿ Mount Ive area (Crooks, 1996; Crooks et al., 1996; Allen et al., 2008) based on their comparable stratigraphic position between the Eucarro Rhyolite and the Yardea Dacite.|16-MAY-23
79616|Mount Friday Formation|Alteration and Mineralisation|Parts of the Mount Friday Formation are variably silicified, hematised and/or overprinted by sericite and chlorite alteration, especially in the vicinity of faults. Epithermal alteration and quartz-pyrite veining in the Mount Friday Formation in drillhole MSDP05 is documented in Fabris et al. (2017).|16-MAY-23
79616|Mount Friday Formation|Geophysical Expression|The Mount Friday Formation and stratigraphic equivalents typically form together with the underlying Paney and Yannabie rhyolite members a zone of low magnetic intensities between the stronger magnetic rocks of the Eucarro Rhyolite and the Yardea Dacite.|16-MAY-23
79616|Mount Friday Formation|Geochemistry|Whole rock geochemical data exist for a number of samples of the Mount Friday Formation from drillholes MSDP05 and MSDP07. The objective of these analyses was to test the rocks for geochemical anomalies indicating epithermal alteration and mineralisation. Geochemical data can be accessed via the South Australian Resource Information Gateway (SARIG; https://map.sarig.sa.gov.au/). No significant geochemical anomalies are associated with the Mount Friday Formation in drillhole MSDP07. The volcaniclastic rocks of the Mount Friday Formation are in this drillhole more silica-rich and contain lower concentrations of Al2O3, Fe2O3, Na2O, TiO2 and P2O5 in contrast to the underlying Eucarro Rhyolite and the overlying Pondanna Dacite Member. In drillhole MSDP05 the volcaniclastics-rich interval of intercalated Mount Friday Formation and Yannabie Rhyolite Member contains zones with anomalous values of Ag, Pb, Cu, Mo, S, As, Bi, and Sb.|16-MAY-23
79616|Mount Friday Formation|Defn author|Mario Werner, GSSA, 12-SEP-2017.|16-MAY-23
79616|Mount Friday Formation|References|Allen SR, Simpson CJ, McPhie J and Daly SJ 2003. Stratigraphy, distribution and geochemistry of widespread felsic volcanic units in the Mesoproterozoic Gawler Range Volcanics, South Australia. Australian Journal of Earth Sciences 50(1):97¿112. **Allen SR, McPhie J, Ferris G and Simpson C 2008. Evolution and architecture of a large felsic Igneous Province in western Laurentia: The 1.6 Ga Gawler Range Volcanics, South Australia. Journal of Volcanology and Geothermal Research 172(1¿2):132¿147. **Crooks A 1996. New exploration targets ¿ vent breccias in the southern Gawler Ranges. MESA Journal 2:9¿17. Department of Mines and Energy South Australia, Adelaide. **Crooks AF, Hill PW, Polito P, Abbot PJ, Crettenden PP, Gray N and Major RB 1996. Gawler Ranges Drilling Report 1994, Report Book 1996/24. Department of Primary Industries and Resources South Australia, Adelaide. **Fabris AJ, Tylkowski L, Brennan J, Flint RB, Ogilvie A, McAvaney S, Werner M, Pawley M, Krapf C, Burtt AC, Rowe R, Henschke C, Chalmers NC, Rechner S, Hardwick I and Keeling J 2017. Mineral Systems Drilling Program in the southern Gawler Ranges, South Australia, Report Book 2016/00030. Department of the Premier and Cabinet, South Australia, Adelaide. **Jagodzinski E, Reid A, Crowley J, McAvaney S and Wade C 2016. New CA-TIMS dates for the Gawler Range Volcanism: Implications for the duration of volcanism. In A Reid comp, Geological Survey of South Australia Discovery Day 2016: presentation abstracts and posters, Report Book 2016/00032. Department of State Development, South Australia, Adelaide, pp. 17-18. **Pawley MJ, Werner M, McAvaney SO and Krapf CBE 2017. Interpreted Proterozoic solid geology of Peltabinna. Mineral Systems Drilling Program Special Map Series, 1:75 000 scale, DIGIMAP 00091. Geological Survey of South Australia, Adelaide. **Werner M, Krapf C, McAvaney S and Fabris A 2016a. Newly discovered occurrences of the Paney Rhyolite and associated volcaniclastic deposits, Narlaby Well area, Gawler Range Volcanic Province. Australian Earth Science Convention 2016, Abstracts 118. Geological Society of Australia, Adelaide, p. 462.  **Werner M, Krapf CBE, McAvaney SO, Nicolson B and Pawley MJ 2016b. New discoveries from the Gawler Ranges: greisen-style mineralisation in Hiltaba Suite granite and a regional stratigraphic marker in the upper Gawler Range Volcanics (GRV). In A Reid comp, Geological Survey of South Australia Discovery Day 2016: presentation abstracts and posters, Report Book 2016/00032. Department of State Development, South Australia, Adelaide, pp. 13¿16. **Werner M, Krapf CBE, McAvaney SO and Pawley MJ 2017a. Surface geology of Peltabinna. Mineral Systems Drilling Program Special Map Series, 1:75 000 scale, DIGIMAP 00090. Geological Survey of South Australia, Adelaide. **Werner M, McAvaney SO, Krapf CBE, Pawley MJ and Fabris AJ 2017b. Geology of the Peltabinna 1:75 000 Map Sheet, Mineral Systems Drilling Program Special Map Series, Report Book 2016/00025. Department of the Premier and Cabinet, South Australia, Adelaide.|16-MAY-23
26054|Mount Margaret Quartzite|Name source|Mount Margaret, on the eastern margin of the Margaret Inlier, in the Peake and Denison Ranges, 15.5 km east of Nilpinna H.S., Umbum 1:100 000 sheet area, Warrina 1:250 000 sheet area - metric reference 6848490, 605010.|16-MAY-23
26054|Mount Margaret Quartzite|Unit history|Mount Margaret Quartzites (Reyner, 1955), Mount Margaret Formation (Thomson and Coats, 1964).|16-MAY-23
26054|Mount Margaret Quartzite|Type section locality|Outcrops 5.5 km north-northwest of Mt Fox from the base of the section (metric ref: 6853810, 598120) to the top (metric ref: 6850175, 600675) measures 2500 m.|16-MAY-23
26054|Mount Margaret Quartzite|Extent|The formation is restricted to the southern part of the Peake and Denison Ranges (i.e. the Margaret Inlier) and outcrops at Mount Margaret and also constitutes the Mount Margaret Plateau.|16-MAY-23
26054|Mount Margaret Quartzite|Thickness range|Maximum total thickness of the formation is 2500 m in the type section.|16-MAY-23
26054|Mount Margaret Quartzite|Lithology|White orthoquartzite, slaty quartzitic sandstone, dark grey sandy siltstone, green-grey silty shale, minor dolomitic siltstone near the base; thick orthoquartzite at the top; clay galls, ripplemarks and cross-bedding.|16-MAY-23
26054|Mount Margaret Quartzite|Relationships and boundaries|The lower contact with the Fountain Springs Beds is gradational. A high silt-shale: quartzite ratio marks the transition down into the Fountain Spring beds (Ambrose and Flint, in prep.). The Mount Margaret Quartzite is conformably overlain by a sandy facies of the Skillogalee Dolomite (Ambrose and Flint, in prep.).|16-MAY-23
26054|Mount Margaret Quartzite|Age reasons|Adelaidean-Burra Group (Torrensian).|16-MAY-23
26054|Mount Margaret Quartzite|Proposed publication|Rept Invest., Geological Survey SA|16-MAY-23
26054|Mount Margaret Quartzite|Status|1|16-MAY-23
13151|Mount Toondina Formation|Name source|Mt Toondina; grid reference 331534 latitude 27o56'42"S, longitude 135o21'41"E Oodnadatta 1:250 000 Sheet area.|16-MAY-23
13151|Mount Toondina Formation|Unit history|Purni Formation of the Pedirka Basin. (Youngs 1975) and part of Patchawarra Formation of the Cooper Basin. Gatehouse (1972).|16-MAY-23
13151|Mount Toondina Formation|Type section locality|As defined by Freytag (1965) at Mt Toondina which is 45 km S 10oW of Oodnadatta township. Standard subsurface section: Cootanoorina 1 well 8 km south of Mt Toondina at latitude 28o00.5'S and longitude 135o20'E between 187.5 m and 516.6 m.|16-MAY-23
13151|Mount Toondina Formation|Extent|Only at Mt Toondina - an assumed piercement structure. In the subsurface the unit is present over most of the Arckaringa Basin.|16-MAY-23
13151|Mount Toondina Formation|Thickness range|180 m at surface 329.1 m in Cootanoorina 1.|16-MAY-23
13151|Mount Toondina Formation|Lithology|The upper part of the unit consists of interbedded coal, carbonaceous shale and grey siltstone and the lower part is less carbonaceous and contains interbeds of sandstone, siltstone and shale.|16-MAY-23
13151|Mount Toondina Formation|Relationships and boundaries|Overlies the Stuart Range Formation (Townsend and Ludbrook 1975) conformably and is unconformably overlain by the Late Jurassic Algebuckina Sandstone.|16-MAY-23
13151|Mount Toondina Formation|Age reasons|Dated in various papers by Balme (1964) Ludbrook (1967) Harris & McGowran (1973). Age is Artinskian, Early Permian.|16-MAY-23
13151|Mount Toondina Formation|Defn author|Townsend I.J., Ludbrook N.H., 1975|16-MAY-23
13151|Mount Toondina Formation|Proposed publication|Quarterly geol. Notes Geological Survey SA, 53|16-MAY-23
13151|Mount Toondina Formation|Status|1|16-MAY-23
13323|Mudnawatana Tonalite|Name source|Reclassification of part of Mudnawatana Tonalite Granite of Bowes (1953), Coats (1971).  (The Mudnawatana tonalite is a reclassification of the name Mudnawatana Granite, for the Palaeozoic intrusive of the Mount Babbage Block ONLY).|16-MAY-23
13323|Mudnawatana Tonalite|Type section locality|Mudnawatana Creek, which is located in the Mount Babbage Block. Only found in Mount Babbage Block. Grid ref. Of type locality 139o35'E and 29o53'S.|16-MAY-23
13323|Mudnawatana Tonalite|Identifying features|Has highest K/Rb ratio of any Palaeozoic intrusives (275). Characterised by low Rb (58 ppm) and Nb (8 ppm) and high Na2O (5.33%). Initial Sr87/Sr86 ratio is lower than other Palaeozoic intrusives (its I.R. = .7045+/-.00118). Chem. Comp. Is as follows: SiO2 = 71.93; Al203 = 15.64; Fe203 = 1.27; MnO = 0.04; Na2O = 5.33, K2O = 1.92; TiO2 = 0.15; P2O5 = 0.04; L.O.I. = 0.63; Total = 99.74|16-MAY-23
13323|Mudnawatana Tonalite|Age reasons|Palaeozoic and pre-Delamerian (Teale and Mortimer, in prep.).|16-MAY-23
13323|Mudnawatana Tonalite|Correlations|Intrudes Terrapinna and Yerila Granites.|16-MAY-23
13323|Mudnawatana Tonalite|Proposed publication|Trans. Roy. Soc. South Australia|16-MAY-23
24409|Mundallio Subgroup|Name source|"Mundallio" Station, latitude 31o28'S, longitude 137o53'E, Port Augusta, 1:250 000 Sheet area (SI 53-4).|16-MAY-23
24409|Mundallio Subgroup|Constituents|Woolshed Flat Shale/Yadlamalka Formation/Mirra Formation|16-MAY-23
24409|Mundallio Subgroup|Extent|Occurs within Burra Group (Thomson et al. 1964) outcrops in the Mt Lofty and Flinders Ranges on the following 1:250 000 sheet areas - Adelaide (SI 54-9) Burra (SI 54-5), Orroroo (SI 54-1), Port Augusta (SI 53-4), Parachilna (SH-54.13), Copley SH 54-9), Andamooka (SH 53.12), Curdimurka (SH 53-8) Marree (SH 54-5).|16-MAY-23
24409|Mundallio Subgroup|Age reasons|Torrensian because of its position within the Burra Group, which is considered as Torrensian (Thomson et al. 1964). New names to be proposed in same publication: Mawson D. and Sprigg R.C. (1950) Subdivision of the Adelaide System. Aust., J. Science 13. 69-72). Murrell B. (1977). Stratigraphy and tectonics across the Torrens Hinge Zone between Andamooka and Marree. Unpubl. Ph.D thesis, Univ of Adelaide.  Wilson A.F. (1952) The Adelaide System as developed in the Riverton-Clare Region, northern Mount Lofty Ranges, South Australia. Trans. R. Soc. S. Aust. 75: 131-149.|16-MAY-23
24409|Mundallio Subgroup|Proposed publication|Transactions of the Royal Society of South Australia|16-MAY-23
24409|Mundallio Subgroup|Proposer|Uppill R.K.|16-MAY-23
24409|Mundallio Subgroup|Resdate|26-SEP-1977|16-MAY-23
26316|Murnaroo Formation|Name source|Murnaroo 1:100 000 Sheet, number 5339 of the Tallaringa 1:250 000 Sheet area.|16-MAY-23
26316|Murnaroo Formation|Type section locality|Murnaroo-1 drillhole (latitude 29o01'25"S, longitude 132o01'35"E) over the interval 316.8 m to total depth 627.5 m. The hole failed to reach the base of the unit.|16-MAY-23
26316|Murnaroo Formation|Description at type locality|Reference section: Lake Maurice East (or SMD 5002) is located at latitude 29o37'S, longitude 131o28'E. There, a probable complete section occupies the interval 117.3 m to 691.3 m (thickness 574 m) and its base unconformably overlies crystalline basement.|16-MAY-23
26316|Murnaroo Formation|Extent|Within the southeastern Officer Basin mainly in the subsurface.|16-MAY-23
26316|Murnaroo Formation|Thickness range|In the type section which is incomplete it is at least 311 m but at the reference section the probably complete sequence is 574 m.|16-MAY-23
26316|Murnaroo Formation|Lithology|Sandstone, coloured pale grey-green to pale green when fresh but most has been altered to dark brown and dark red-brown by iron oxide in groundwater. Generally poorly sorted with occasional very well-rounded, in part bimodal, fine to coarse-grained and minor granule quartz sand, rarely conglomeratic; lithic grains and clay clasts variably rare to common. Feldspar and heavy minerals are present, the latter often as concentrations on bedding planes; biotite and muscovite are similarly concentrated. Shale interbeds are more common near the top but are scattered randomly throughout the section. Cement most commonly is silica with carbonate to a lesser extent. Accessory minerals include feldspar, rare gypsum, and ?glauconite.|16-MAY-23
26316|Murnaroo Formation|Relationships and boundaries|The Murnaroo Formation conformably underlies the shale/sandstone/carbonate sequence of the Observatory Hill beds in Murnaroo-1. In the reference section the unit is unconformably underlain by unnamed steeply-dipping gneiss, of the Gawler Craton. However, its contact with overlying Observatory Hill beds is not seen because the contact was not cored.|16-MAY-23
26316|Murnaroo Formation|Identifying features|Definition: The Murnaroo Formation is a thick sequence of fine to coarse-grained quartz-rich clastic sediments, mainly sandstone, conformably beneath the ?Cambrian Observatory hill beds and was first intersected in SADME Murnaroo-1 drilled in 1978 (Gatehouse, 1979). Recent drilling near Lake Dey-Dey (Aquitaine SMD 5001, SADME Lake Maurice West, SADME 1982a), and northwest of Maralinga (Aquitaine SMD5002, SADME Lake Maurice East, SADME 1982b) (Major, in prep.) and elsewhere (Fig. 1) indicates that it is widespread. This sandstone body is thick and having been recognised in a number of drillholes, sufficient information is now available for the unit to be defined. Figure 1 shows the distribution and Figure 2 the correlation and relationships to known overlying and underlying units. The name 'Murnaroo Formation' was reserved in the Central Register of Stratigraphic Names, Canberra and is being used on the Tallaringa 1:250 000 geological map (Benbow, in prep).  Map symbol: Cmm|16-MAY-23
26316|Murnaroo Formation|Age reasons|No direct evidence is available to suggest age. A fossil recorded close to the type section of the Observatory Hill beds suggests a late Early to early Middle Cambrian age (Gatehouse, 1976). On this basis the conformably underlying Murnaroo Formation is taken to be Early Cambrian or older. Rb-Sr whole rock dating of siltstone near the base of the Observatory Hill beds in Murnaroo-1 gave a poorly controlled age of 715+/-210 Ma (Webb in Gatehouse, 1979).|16-MAY-23
26316|Murnaroo Formation|Correlations|The Murnaroo Formation in the reference section may eventually be correlated with the Wallatinna Formation which was described by Benbow in 1982 on Everard in the Mount Johns area of the northeast Officer Basin. This formation intertongues with and conformably underlies chert-bearing carbonates which themselves are correlated with the Observatory Hill beds (see Krieg, 1973; p.17). Based on lithology and the identification of quartz type (magmatic versus metamorphic) broad correlations may eventually be pssible (Farrand and Gatehouse, 1985).|16-MAY-23
26316|Murnaroo Formation|Defn author|Gatehouse C.G., Benbow M.C., Major R.B.|16-MAY-23
26316|Murnaroo Formation|Proposed publication|Quarterly Geol. Notes, Geological Survey SA, 1986, 97, 17-20|16-MAY-23
26316|Murnaroo Formation|Name first published by|Gatehouse C.G. et al. 86/25341|16-MAY-23
26316|Murnaroo Formation|Proposer|Gatehouse C.G., Benbow M.C.|16-MAY-23
24419|Napoleon Megabreccia Member|Name source|After the Napoleon Mine situated 600 m west of Mount Craig.  |16-MAY-23
24419|Napoleon Megabreccia Member|Type section locality|A well-exposed section along a creek bed, commencing at 276450-6471170 and finishing at 276080-6471470 is chosen as type section, but reference sections 1 km to the north and 1.5 km to the south along strike, provide good exposure of the northern basal sandy facies and the southern upper siltstone facies respectively.|16-MAY-23
24419|Napoleon Megabreccia Member|Extent|Known only on the west  limb of the Worumba Anticline.|16-MAY-23
24419|Napoleon Megabreccia Member|Thickness range|Approximately 500 m exposed in the type section, but may reach 900 m, 1.5 km to the south.|16-MAY-23
24419|Napoleon Megabreccia Member|Lithology|Lithological Sequence: For lithological details, see Preiss (1979).|16-MAY-23
24419|Napoleon Megabreccia Member|Relationships and boundaries|Overlies the lower part of the Skillogalee Dolomite with erosional contact; intertongues with the upper part of the Skillogalee Dolomite at southern termination of the megabreccia.|16-MAY-23
24419|Napoleon Megabreccia Member|Identifying features|Definition: A thick lens of sedimentary megabreccia intertonguing with the Skillogalee Dolomite on the west limb of the Worumba Anticline (Preiss, 1979). Map symbol Pbk1.|16-MAY-23
24419|Napoleon Megabreccia Member|Age reasons|mid-Torrensian.|16-MAY-23
24419|Napoleon Megabreccia Member|Correlations|The Napoleon Megabreccia Member is contemporaneous with part of the Skillogalee Dolomite.|16-MAY-23
24419|Napoleon Megabreccia Member|Proposed publication|Quarterly Geological Notes, Geological Survey of South Australia, 76: 12-23|16-MAY-23
24419|Napoleon Megabreccia Member|Proposer|Preiss W.V.|16-MAY-23
28251|Nildottie Siltstone Member|Name source|"Nildottie Spring"; latitude 31o02'50"S, longitude 138o47'29"E.|16-MAY-23
28251|Nildottie Siltstone Member|Type section locality|460 metres of red siltstone, with minor red shale and sandstone, exposed in an area of undulatory topography 2.5 km north of Ten Mile Creek, from latitude 31o15'47"S, longitude 138o49'43"E (bottom) to latitude 31o15'43"S, longitude 138o50'07"E (top).|16-MAY-23
28251|Nildottie Siltstone Member|Extent|The unit is exposed over approximately 50 km2 in the central Flinders Ranges (along the Heysen Range, at Mernmerna, between Wirrealpa and the Ten Mile Creek, near Mount Frome and adjacent to Chambers Gorge), on the Parachiulna 1:250 000 Geological Sheet (SH 54-13).  It also outcrops over approximately 15 km2 in the Mount Scott Range, on the western portion of the Copley 1:250 000 Geological Sheet (SH 54-9).|16-MAY-23
28251|Nildottie Siltstone Member|Thickness range|150-470 m|16-MAY-23
28251|Nildottie Siltstone Member|Lithology|Red siltstone, with minor shale and fine sandstone. Evenly lamiantaed to ripple laminated. Contains abundant desiccation cracks and halite casts.|16-MAY-23
28251|Nildottie Siltstone Member|Relationships and boundaries|The Nildottie Siltstone Member is the middle member of the Billy Creek Formation in the central Flinders Ranges and at Mount Scott. Generally, it rests conformably on the Warragee Member of the Billy Creek Formation. However, in the southern portion of the Wirrealpa Basin south of the Ten Mile Creek graben, the Warragee Member is absent and the Nildottie Siltstone Member rests directly and with possible disconformity on Wilkawillina Limestone. In all outcrops, the Nildottie Siltstone Member is sharply but conformably overlain by red sandstone of the Ereguna Sandstone Member.|16-MAY-23
28251|Nildottie Siltstone Member|Age reasons|The Billy Creek Formation is Lower to Middle Cambarian in ae (Daily, 1956), however the position of the Lower-Middle Cambrian boundary occurs at an undefined position in the upper portion of the formation. It is likely therefore that the Nildottie Siltstone Member is largely, if not entirely, late Lower Cambarian in age.|16-MAY-23
28251|Nildottie Siltstone Member|Proposed publication|Transactions of the Royal Society of South Australia|16-MAY-23
26318|Noranda Volcanics|Name source|Site of Noranda Aust. Pty Ltd exploration camp near Boorloo workings 10 km SE of 'Callanna' (Fig. 1B).|16-MAY-23
26318|Noranda Volcanics|Unit history|Noranda Volcanics' of Murrell (1977).|16-MAY-23
26318|Noranda Volcanics|Type section locality|Noranda campsite; latitude 29o45', longitude 137o59'.|16-MAY-23
26318|Noranda Volcanics|Extent|Willouran Ranges.|16-MAY-23
26318|Noranda Volcanics|Thickness range|Possibly 80 m NE of Chintapanna Dam.|16-MAY-23
26318|Noranda Volcanics|Lithology|Amygdaloidal basaltic rock.  Pillow structure near Chintapanna Dam (Radke, 1980).|16-MAY-23
26318|Noranda Volcanics|Relationships and boundaries|Faulted contacts. Occurs within megabreccia or adjacent to Dome Sandstone.|16-MAY-23
26318|Noranda Volcanics|Identifying features|Basaltic volcanics low in the Callanna Group. Map symbol Pan.|16-MAY-23
26318|Noranda Volcanics|Age reasons|Early Willouran, probably below Dome Sandstone.|16-MAY-23
26318|Noranda Volcanics|Correlations|Correlated with the Wooltana Volcanics (Arkaroola Subgroup) and Cadlareena Volcanics.|16-MAY-23
26318|Noranda Volcanics|Proposed publication|Quarterly geological Notes, Geological Survey SA 79: 7-16|16-MAY-23
26318|Noranda Volcanics|Proposer|Murrell B.|16-MAY-23
26083|Nuckulla Basalt|Name source|From Nuckulla Hill, located 6 km west of the main basalt outcrop. Nuckulla well is located adjacent to the main basalt outcrop. Nuckulla Hill is at 31o43.5' latitude and 134o51.25' longitude. Origin: As a series of lava flows of limited areal extent.|16-MAY-23
26083|Nuckulla Basalt|Type section locality|A north-south section running for a distance of 1.25 km, 2 km west of Nuckulla well. Nuckulla well is at 31o43.75' latitude and 134o56.5' longitude.|16-MAY-23
26083|Nuckulla Basalt|Extent|A small localised outcrop in the far east of the Childara 1:250 000 Sheet area. Area covered is roughly 2.5 km2.|16-MAY-23
26083|Nuckulla Basalt|Lithology|A green, non variable aphanitic rock. In thin section the rock is composed of strongly oriented plagioclase laths interlocking with unresolvable, altered groundmass material which appears devitrified. The plagioclase is altered, untwinned and makes up 60% of the rock. Scattered throughout are minute, euhedral clinopyroxene crystals - these are not interlocking with the plagioclase, but appear to have grown later. Chlorite and hornblende has replaced much of the clinopyroxene, which makes up a total of 25% of the rock. Scattered euhedral opaques (probably magnetite) make up 5% of the rock. Unresolvable matrix forms the remaining 10% of the rock. The unit becomes notably vesicular in its upper zones. The vesicularity increases until a 6 m band of poorly welded lithic-vitric ashflow tuff (with a variety of lithic fragments of lapilli size) is reached. This unit is definitely the lateral equivalent of the Waurea Pyroclastics.|16-MAY-23
26083|Nuckulla Basalt|Relationships and boundaries|Conformably overlies the Bunburn Dacite and is separated from this unit by a 10 m thickness of airfall tuff and strongly welded ashflow tuff which may be the lateral equivalent of the Waurea Pyroclastics. Maximum thickness 80m, although the unit thins rapidly to the east and west.|16-MAY-23
26083|Nuckulla Basalt|Age reasons|Forms part of the mid-Carpentarian Glyde Hill Complex as defined by Blissett.|16-MAY-23
26083|Nuckulla Basalt|Defn author|Giles C.W., 1977|16-MAY-23
26083|Nuckulla Basalt|Proposed publication|SA Department of Mines, Quarterly Notes No. 61|16-MAY-23
26083|Nuckulla Basalt|Comments|The Nuckulla Basalt is underlain and overlain by presumed equivalents of the Waurea Pyroclastics, therefore its eruption occurred contemporaneous with but occupying a shorter time span than the eruption of the Waurea Pyroclastics.|16-MAY-23
14485|Observatory Hill Formation|Name source|From Observatory Hill (latitude 28o58'06"S, longitude 132o03'42"E) on the Giles 1:250 000 topographic map.|16-MAY-23
14485|Observatory Hill Formation|Unit history|This unit was named by Wopfner (1969) as 'Observatory Hill Beds'. Krieg (1973) extended Wopfner's description to include outcrop in the Mount Johns Range, 250 km to the northeast. The unit is now recognised in many drillholes over a wide area (Fig. 4), demonstrating lateral continuity and consistency of lithology, and allowing formation status to be applied.  Two members and a marker horizon are recognised within the Observatory Hill Formation. These are the Oolarinna Member (Benbow, 1982) the Moyles Chert Marker, and the Parakeelya Alkali Member (described herein).|16-MAY-23
14485|Observatory Hill Formation|Type section locality|Twenty metres of outcrop at latitude 28o58.2'S, longitude 131o57.7'E as described by Wopfner (1969) and the interval 0 to 155.25 m in Observatory Hill-1 which was spudded just above the base of Wopfner's section (Gatehouse and Hibburt, 1987).|16-MAY-23
14485|Observatory Hill Formation|Description at type locality|Reference Section:  Byilkaoora-1 (latitude 27o16'47.8"S, longitude 133o24.1"E), 155.8 to 379.4 m.|16-MAY-23
14485|Observatory Hill Formation|Extent|The Observatory Hill Formation crops out at scattered localities in a northeast-southwest trending belt running from the Mount Johns Range to Observatory Hill and Lake Maurice (Benbow, 1982, 1986; Krieg, 1973; Wopfner, 1968; Pitt, 1983). Drillhole intersections extend the distribution of the formation to the south and north of the outcrop belt (Fig. 4).|16-MAY-23
14485|Observatory Hill Formation|Thickness range|Ranges from 178 m to in excess of 494 m in the Marla area and from 178 m to more than 294 m in the Emu area.|16-MAY-23
14485|Observatory Hill Formation|Lithology|The Observatory Hill Formation consists of multicoloured micaceous siltstone and claystone, calcareous and dolomitic in part, with minor light yellow brown very fine-grained sandstone and light grey to dark grey limestone and dolomite. The siltstone and claystone are dominantly red brown to brown in colour but range through purple and greenish grey to dark grey, especially where they are interbedded with the carbonates. The carbonates are concentrated at three levels within the formation and make up the Moyles Chert Marker, the Parakeelya Alkali Member and an unnamed unit found near the base of the Observatory Hill Fm in the Emu area. With the exception of the Oolarinna Member (Benbow, 1982), the fine-grained red-bed clastaics of the Observatory Hill Formation have not been subdivided into members. Moyles Chert Marker Bed: A unit of greenish grey to dark grey limestone, dolomite and siltstone, ranging from 8 to 20 m thick and containing abundant chert nodules, lenses, and fragments occurs near the top of the Observatory Hill Fm. This Bed forms a distinctive horizon which has been recognised in outcrop in the vicinity of the Mount Johns Range and Wallatinna Homestead (Benbow, 1982), and in most drillholes in the Marla and Emu areas. Its name is derived from Moyles Dam, Wantapella 1:100 000 sheet, latitude 27o28'30"s, longitude 133o20'15"E. It is not present in the type section where the top of the Observatory Hill Fm has been eroded but can be seen from 200.00 to 213.1 m in the Byilkaoora-1 reference section. Parakeelya Akali Member: A second, thicker, carbonate-rich section which is encountered 30 to 40 m below the Moyles Chert Marker. The name has been derived from Parakeelya Bore, Marla 1:100 000 sheet, latitude 27o24'36", longitude 133o33'06" (Fig. 5). It consists of a distinctive sequence of laminated to thinly bedded, dominantly light brownish grey and greenish grey to dark grey, limestone, dolomite, siltstone and claystone, characterised by the presence of: i) abundant desiccation features; ii) chert lenses, nodules and fragments; iii) calcite and dolomite crusts.  The Parakeelya Alkali Member type section can be seen from 240.0 to 334.5 m in Byilkaoora-1 in the Marla area where calcite pseudomorphs after alkali evaportite minerals (Pitt et al. 1979; White and Youngs, 1980) occur. The Parakeelya Alkali Member is thinner and less well developed in the Emu area but is still clearly recognisable. It contains a higher proportion of clastics than in the Marla area and calcite pseudomorphs of alkali evaporite minerals are less common. Intersections indicate that the Parakeelya Alkali Member maintains a fairly constant thickness over wide areas (80-100 m in the Marla area, 60-70 m in the Emu area) but can lens out abruptly (as seen in exposure in the Mount Johns Range). The 22.7 m of outcrop at the Observatory Hill Fm type section lies within the Parakeelya Alkali Member; an additional 39.3 m was intersected in Observatory Hill-1, a total of 62 m.|16-MAY-23
14485|Observatory Hill Formation|Depositional environment|The carbonate-rich sections preserve features indicative of deposits from shallow water subject to exposure, desiccation and local brine overprints. The presence of alkali evaporite pseudomorphs is key evidence of a continenntal playa system. The red-beds surrounding the pllaya sediments are not so clearly indicative of environments but probably represents arid terrestrial deposits. The extension of the terrestrial red-beds into a marginal sabkha setting is evidenced by interbedding with shallow marine carbonates of the underlying Ouldburra Formation in the Marla-Manya area.|16-MAY-23
14485|Observatory Hill Formation|Relationships and boundaries|The Observatory Hill Formation in the Mount Johns area is conformably overlain by the Arcoeillinna Sandstone (Benbow, 1982). The upper boundary is placed at the base of the first major sandstone which overlies red-brown claystone and siltstone of the Oolarinna Member. In the Marla-Manya area the Observatory Hill Formation lies conformably to locally disconformably on the Ouldburra Formation. A lateral intertonguing relationship with the Wallatinna Formation is observed in exposures in the Mount Johns Range (Benbow, 1982).  In the Emu area the Observatory Hill Formation conformably to disconformably overlies the Relief Sandastone and unconformably overlies the Adelaidean Rodda beds.|16-MAY-23
14485|Observatory Hill Formation|Age reasons|Uncertain, but stratigraphically younger than the Ouldburra Formation (Early Cambrian) and overlain by an extensive development of shallow marine-fluvial clastics, dominated by sandstone, interpreted as Late Cambrian-Devonian (Krieg, 1973).|16-MAY-23
14485|Observatory Hill Formation|Defn author|Brewer A.M. et al. 82/25860|16-MAY-23
14485|Observatory Hill Formation|Proposed publication|Quarterly geological Notes, Geological Survey SA, No. 102|16-MAY-23
14485|Observatory Hill Formation|Comments|First published as Observatory Hill Beds (Wopfner 1969) R.Soc. SA Trans. 93: 169-81|16-MAY-23
14485|Observatory Hill Formation|Name first published by|Brewer A.M., Dunster J.N., Gatehouse C.G. |16-MAY-23
14485|Observatory Hill Formation|Status|1|16-MAY-23
24441|Oolarinna Member|Name source|Oolarinna Hill, Everard 1:250 000 grid reference (6100572522).|16-MAY-23
24441|Oolarinna Member|Type section locality|Located on the northern margin of the Mount Johns Range (Section 6). Grid reference 34389974-34379973.|16-MAY-23
24441|Oolarinna Member|Extent|Outcrops poorly around the northern and eastern margin of the Mount Johns Range. Thought to equate with the Type Observatory Hill Beds near Observatory Hill 250 km to the SW.|16-MAY-23
24441|Oolarinna Member|Thickness range|35 m at the type section, 45 m in Byilkaoora-1 to 23 m adjacent to the type section (section 6).|16-MAY-23
24441|Oolarinna Member|Lithology|Dirty red-brown to red-brown, thin to very thin bedded calcareous to non calcareous (dominantly) siltstone to claystone with interbedded pebble conglomerate and sandstone at the base.|16-MAY-23
24441|Oolarinna Member|Relationships and boundaries|Represents the uppermost part of the Observatory hill Beds. Overlies the chert marker horizon and both sharply and transitionally underlies (in the north and south respectively) the Arooeillinna Sandstone.|16-MAY-23
24441|Oolarinna Member|Age reasons|No direct fossil age. A radiometric age of 617+/-138 Ma (IR87Sr/86Sr of  0.7146 + 0.018) max. age 524+/-68 Ma (IR87Sr/86Sr of 0.7244+/-0.0097) min. age (Webb, 1979). Thought to be Early to Middle Cambrian.|16-MAY-23
24441|Oolarinna Member|Proposed publication|Trans. Roy. Soc. SA|16-MAY-23
24441|Oolarinna Member|Proposer|Benbow M.|16-MAY-23
27068|Oolgelima Gravel|Name source|Oolgelima Creek on SE Murloocoppie 1:250 000 map sheet.|16-MAY-23
27068|Oolgelima Gravel|Type section locality|Type locality in Oolgelima Creek. Section located 9.3 km north of Coober Pedy.  Latitude 28o56'22", longitude 134o46'42".|16-MAY-23
27068|Oolgelima Gravel|Extent|On the northern and eastern flanks of the Stuart Range, especially in drainage lines.|16-MAY-23
27068|Oolgelima Gravel|Thickness range|1-3 m average 1.5 m|16-MAY-23
27068|Oolgelima Gravel|Lithology|Medium to weakly consolidated gravel, red-brown clayey lenses. Gravel (to sand) sized clasts of bleached (and silicified in part) claystone and siltstone.|16-MAY-23
27068|Oolgelima Gravel|Relationships and boundaries|Intertongues with the Benitos Clay (Benbow, in prep.). Sits sharply on the Giddlinna Formation.|16-MAY-23
27068|Oolgelima Gravel|Age reasons|Considered to be Late Pleistocene, no fossils however. Considered to equate with the upper part of the Pooraka Formation (Firman, 1969).|16-MAY-23
27068|Oolgelima Gravel|Defn Reference|83/23476|16-MAY-23
27068|Oolgelima Gravel|Proposer|Benbow M|16-MAY-23
26319|Ouldburra Formation|Name source|From Ouldburra Hill (latitude 27o31'00"S, longitude 133o55'00"E approximately) on the Wintinna 1:250 000 topographic map.|16-MAY-23
26319|Ouldburra Formation|Unit history|Originally correlated with the Observatory Hill beds (Pitt et al., 1980; Benbow, 1982) as described by Wopfner (1969).|16-MAY-23
26319|Ouldburra Formation|Type section locality|Manya-6, (latitude 27o40'08"S, longitude 133o42'59.7"E), 571.4 to 1685.6 m.|16-MAY-23
26319|Ouldburra Formation|Extent|The Ouldburra Formation is not known to crop out, however it has been intersected in numerous drillholes in the Marla-Manya area (Figure 6). Marine carbonates intersected in SADME drillholes Marla-1A, 1B, Mount Willoughby-1, and Manya-1 were previously correlated with the Observatory Hill beds (Pitt et al., 1980) but are now assigned to the Ouldburra Formation. Similar carbonates and evaporites intersected in the drillhole Wilkinson-1, to the southwest, are probable correlatives of the Ouldburra Formation.|16-MAY-23
26319|Ouldburra Formation|Thickness range|Maximum known thickness is in the type section of 1114.2 m, but considerable variation is observed. Drillhole Marla-3 penetrated a complete basin margin section of only 142.6 m. Figure 6 shows the present known distribution and thickness of the unit from drillhole intersections.|16-MAY-23
26319|Ouldburra Formation|Lithology|The Ouldburra Formation consists of mixed carbonates/siliciclastics, marine carbonates and evaporites. In the type section, the basal unit is typified by halite and sandstone grading up to stacked sand/silt/mudstone sets which become increasingly calcareous. These units are overlain by a thick sequence of calcareous and dolomitic carbonates with sporadic clastics and gypsum/anhydrite interbeds. The carbonate lithofacies are dominated by laminated and silty carbonate mudstone but include wackestone, packstone, minor grainstone, stromatolitic and thrombolitic algal bindstone, and archaeocyath bafflestone/framestone. The top of the formation is typically an interdigitation of laminated carbonate mudstones and red-bed siltstones with abundant nodular sulphate evaporite and bedded 'chicken-wire' anhydrite.|16-MAY-23
26319|Ouldburra Formation|Depositional environment|In the Manya area, deposition began with the precipitation of bottom-nucleated halite in small isolated salinas on a peri-emergent sand flat. This was followed by a series of widespread transgressions and regressions of restricted shallow marine waters over a flanking carbonate sabkha. Ooid shoals, algal/carbonate mud mounds and archaeocyath/algal bioherms were developed offshore. The flanking sabkha was characterised by near-surface dolomitisation, the growth of displacive 'chicken-wire' anhydrite within the emergent sediment profile and, ultimately, the deposition of red-bed sediments.|16-MAY-23
26319|Ouldburra Formation|Relationships and boundaries|The Ouldburra Formation conformably overlies the Relief Sandstone. The contact is defined as the bottom of the lowermost carbonate unit, siltstone or halite bed. The upper boundary is taken as the top of the uppermost carbonate unit underlying the gypsiferous red-beds of the lower portion of the Observatory Hill Formation.|16-MAY-23
26319|Ouldburra Formation|Age reasons|Regular and irregular archaeocyaths enable an Early Cambrian (?Botoman) age to be inferred.|16-MAY-23
26319|Ouldburra Formation|Defn author|Brewer A.M., Dunster J.N., Gatehouse C.G., Henry R.L., Weste G.  GSSA Quarterly Geol. Notes 102|16-MAY-23
26319|Ouldburra Formation|Proposed publication|Quarterly Geological Notes, Geological Survey SA, 102|16-MAY-23
26319|Ouldburra Formation|Proposer|Brewer A.M., Dunster J.N., Gatehouse C.G., Henry R.L., Weste G.|16-MAY-23
76222|Pack Creek Member|Name source|Pack Creek, ~1100 m southeast of South Moorowie Mine.|16-MAY-23
76222|Pack Creek Member|Geomorphic expression|Part scree covered narrow beds, at basal slope concavities.|16-MAY-23
76222|Pack Creek Member|Type section locality|Section H, 467 ft (basal contact) to 687 ft (upper contact) (142.3 to 209.4 m) 30°59'54.84"S, 139°15'56.89"E to 30°59'56.00"S, 139°15'58.90"E.|16-MAY-23
76222|Pack Creek Member|Extent|Exposed at eastern margin of foothills, south of Moorowie Mine.|16-MAY-23
76222|Pack Creek Member|Thickness range|67 m (220 ft) in type section on Section H. Average 46 m (151 ft), measured across other possibly faulted sections.|16-MAY-23
76222|Pack Creek Member|Lithology|Purple-red micaceous siltstones with thin grey limestone laminations at base. Local thin polymict channel conglomerate lenses with light grey limestone cobbles and quartz granule-rich limestone pebbles in a silty lime matrix.|16-MAY-23
76222|Pack Creek Member|Depositional environment|Intertidal flats landward of the backreef, with extensive tidal channels and shallow lagoons.  Adjacent to fine siliciclastics winnowed from emergent salt domes, basement uplifts, alluvial fans, or dune field sources.|16-MAY-23
76222|Pack Creek Member|Relationships and boundaries|Fourth unit from the base of the Moorowie Formation. Conformable, with passage zones from the massive archaeocyathan limestones of the Kandramooka Member below, and to the microcrystalline microbial limestones of the Brillig Catch Member above.|16-MAY-23
76222|Pack Creek Member|Structure and Metamorphism|Soft beds of moderate dip follow the eastern limb of a low-plunge anticline. Partly faulted.|16-MAY-23
76222|Pack Creek Member|Age reasons|Lower Cambrian, Stage 4, within the Pararaia janeae trilobite Zone (Figure 2 of Jago et al., this volume).|16-MAY-23
76222|Pack Creek Member|Correlations|A possible eastern extension of the Oraparinna Shale, together with the Wookata Shale Member of the Moorowie Formation.|16-MAY-23
76222|Pack Creek Member|Defn author|T. J. Mount, 8-JAN-2019, after Mount (1970).|16-MAY-23
76222|Pack Creek Member|References|Jago, J. B., Gehling, J. G., Betts, M. J., Brock, G. A., Dalgarno, C. R., Garcia-Bellido, D. C., .., Paterson, J. R. (2019). The Cambrian System in the Arrowie Basin, Flinders Ranges, South Australia. Australian Journal of Earth Sciences. doi:10.1080/08120099.2018.1525431   **Mount, T. J. (1970). Geology of the Mt. Chambers Gorge region (BSc. (Honours) thesis, unpublished).Adelaide, SA: University of Adelaide. http:hdl.handle.net/2440/67162.  **T. J. Mount, J. B. Jago, N. R. Langsford & C. R. Dalgarno (2019): Geological setting of the Moorowie Formation, lower Cambrian Hawker Group, Mt Chambers Gorge, eastern Flinders Ranges, South Australia, Australian Journal of Earth Sciences, DOI: 10.1080/08120099.2019.1586771.|16-MAY-23
28186|Palthrubie Granophyre|Name source|From Palthrubie hill, 6.5 km southeast of Lake Everard homestead on Gairdner 1:250 000 Sheet area. Palthrubie hill is located at 31o47' latitude and 135o12.5' longitude. Origin: This unit is intrusive into the Mangaroongah Dacite, as evidenced by its outcrop pattern (circular and plug-like) and chilled margins. The well developed granophyric texture indicates that this unit is a shallow intrusive.|16-MAY-23
28186|Palthrubie Granophyre|Type section locality|The centre of the intrusive plug is located at 31o46' latitude and 135o12' longitude.|16-MAY-23
28186|Palthrubie Granophyre|Extent|Small circular outcrop 2 km in diameter, the centre of which is 3 km southeast of Lake Everard homestead.|16-MAY-23
28186|Palthrubie Granophyre|Lithology|An orange weathering rock of medium grainsize, containing only quartz and K feldspar. This unit outcrops as reounded tors, typical of granite. In thin section a granophyric intergrowth of quartz and K feldspar is the most characteristic feature. The quartz occurs as euhedral, fine grained blebs within the K feldspar. These blebs are arranged in an ordered pattern, aligned along crystallographic directions in the K feldspar. Elsewhere K feldspar and quartz grains form a granular aggregate, showing no intergrowth. The K feldspar is strongly stained with limonite, giving the rock its characteristic reddish-orange colour in fresh specimen. The K feldspar has been extensively sericitized.|16-MAY-23
28186|Palthrubie Granophyre|Relationships and boundaries|An intrusive plug. Intrusive into the Mangaroongah Dacite. This unit is petrographically distinct from the intrusive Yandoolka Rhyolite (as defined by Blissett) which outcrops nearby.|16-MAY-23
28186|Palthrubie Granophyre|Age reasons|Co-magmatic with the Glyde Hill Complex volcanics. Undoubtedly the same age as the other intrusive plugs and dykes that intrude the complex. Probably the same age as the co-magmatic Hiltaba Granite (Blissett) and may be a local phase of this granite - to which it has a great geochemical resemblance.  Age mid-Carpentarian, slightly less than 1550 Ma.|16-MAY-23
28186|Palthrubie Granophyre|Defn author|Giles C.W., 1977|16-MAY-23
28186|Palthrubie Granophyre|Proposed publication|Quarterly Notes No. 61, SA Department of Mines|16-MAY-23
22621|Pando Formation|Name source|Delhi-Santos Pando No. 1 well (latitude 28o24'56"S, longitude 139o48'20"E), Diamond Bog 1:100 000 sheet area.|16-MAY-23
22621|Pando Formation|Unit history|Gatehouse (1983, 1986) included the sandstone lithotype (eg in Daralingie-1) in the Dullingari Group. The Moolalla-1 occurrence was referred questionably to the Dullingari Group (Taylor et al., 1991).|16-MAY-23
22621|Pando Formation|Type section locality|Pando No. 1 well (1736-1933 m, logger's depth) represented in part by Cores 4, 5 and 6. The top is identified on the gamma ray log by rapid increase to 300API units and by grey-buff glauconitic sandstone in the basal 1.5 m of Core 4. The base has not been penetrated in the type section.|16-MAY-23
22621|Pando Formation|Extent|Subsurface only. Distribution uncertain but ranges northeast from the Boxwood Depression to the Moomba Ridge; the formation has been intersected most often in the Daralingie 1:100 000 sheet area (6941).|16-MAY-23
22621|Pando Formation|Thickness range|246+ m of section (55o dip) were drilled in Moolalla No. 1 well but maximum thickness is unknown.|16-MAY-23
22621|Pando Formation|Lithology|Sandstone, grey-buff-pale green, fine- to coarse-grained with abundant glauconite and detrital zircon. The sandstone is bioturbated with penetrative burrows resembling Chondrites. Interbeds of grey-buff slightly pyritic siltstone occur. Shale intersected in other drillholes (eg Boxwood-1) is also included in the Pando Formation. Shale is olive-green to grey with disseminated glauconite and patchy carbonate cement. Interbeds of ripple laminated ?tuffaceous fine grained sandstone are common. The shale is weakly bioturbated.|16-MAY-23
22621|Pando Formation|Relationships and boundaries|Underlain by steeply dipping quartzite of unknown age in Daralingie-1. Overlain conformably by or interbedded with Mooracoochie Volcanics (Gatehouse, 1983) in Boxweed-1. Overlain unconformably by Permian sediments in most wells (e.g. Pando-1, Pando North-1, Daralingie-1, Moolalla-1).|16-MAY-23
22621|Pando Formation|Age reasons|Pando Formation is the oldest known unit in the Warburton Basin. It underlies and is interbedded with Mooracoochie Volcanics of Early Cambrian (pre-Templetonian) age. Penetrative burrows indicate that the Pando Formation is also Early Cambrian.|16-MAY-23
22621|Pando Formation|Proposed publication|Strzelecki, South Australia - Explanatory Notes - 1:250 000 Geological Series Sheet SH/54-2|16-MAY-23
22621|Pando Formation|Proposer|Gravestock D.I.|16-MAY-23
14844|Pantoulbie Formation|Name source|"Pantoulbie" homestead; grid reference 300673, Ripon 1:50 000 Sheet 5732-II.|16-MAY-23
14844|Pantoulbie Formation|Unit history|No specific name has been used but earlier writers referred to this unit as 'late Tertiary sandstone' - (Segnit and Dridan, 1938).|16-MAY-23
14844|Pantoulbie Formation|Type section locality|Between 8 and 22.5 in Department of Mines & Energy observation well FOR4 situated 4.5 km southeast of 'Pantoulbie' homestead in Sec. 57, Hd.Forrest. Samples are stored in the Departmental Core Library at Glenside, SA.|16-MAY-23
14844|Pantoulbie Formation|Extent|The unit is intersected in sub-surface by Department of Mines & Energy (For 10) observation wells and private water wells in the Robinson Basin. This basin covers an area of approximately 500 km2 to the south and east of Streaky Bay.|16-MAY-23
14844|Pantoulbie Formation|Thickness range|About 40 m maximum known thickness.|16-MAY-23
14844|Pantoulbie Formation|Lithology|Interbedded orange-brown clayey sands, quartz sands and sandy clays with occasional beds of lateritic gravel.|16-MAY-23
14844|Pantoulbie Formation|Relationships and boundaries|Unconformably overlies granites. Top of unit defined by orange brown mottled sandy clay. Disconformably overlain by the Bridgewater Formation (Boutakoff, 1963)|16-MAY-23
14844|Pantoulbie Formation|Age reasons|There are no fossils evident in these sediments but stratigraphic evidence suggests a late Tertiary age.|16-MAY-23
14844|Pantoulbie Formation|Defn author|Barnett S., 1978|16-MAY-23
14844|Pantoulbie Formation|Proposed publication|Quarterly Geological Notes, Geol Surv. S. Aust. No. 67|16-MAY-23
25694|Parakeelya Alkali Member|Name source|Parakeelya Bore, Latitude 27o24'36"S, on Marla 1:100 000 sheet.|16-MAY-23
25694|Parakeelya Alkali Member|Unit history|A member of the Observatory Hill Formation.|16-MAY-23
25694|Parakeelya Alkali Member|Type section locality|Byilkaoora 1, Latitude 27o16'47.8"S, Longitude 133o31'24.1"E from 240.0 m to 334.5 m.|16-MAY-23
25694|Parakeelya Alkali Member|Extent|Marla and Emu areas of the Officer Basin.|16-MAY-23
25694|Parakeelya Alkali Member|Thickness range|94.5 m at the type-section, it ranges up to 100 m in the Marla area and 70 m in the Emu area. It occupies all of the outcrop type-section at Observatory Hill.|16-MAY-23
25694|Parakeelya Alkali Member|Lithology|Limestone, dolomite, siltstone and claystone, brown grey to dark grey with chert nodules, lenses and fragments. Desiccation cracks, pseudomorphs of alkali evaporite minerals are characteristic.|16-MAY-23
25694|Parakeelya Alkali Member|Relationships and boundaries|Conformably overlain and underlain by unnamed red-bed siltstones of the Observatory Hill Formation, it occurs 30-40 m below the Moyles Chert Marker.|16-MAY-23
25694|Parakeelya Alkali Member|Age reasons|The unit lies within the Observatory Hill Formation, it is younger than Early Cambrian Ouldburra Formation, and older than Late Cambrian-Devonian (Krieg, 1973).|16-MAY-23
25694|Parakeelya Alkali Member|Proposed publication|Quarterley geological Notes, Geological Survey SA, 102|16-MAY-23
25694|Parakeelya Alkali Member|Defn approved by|Photocopy sent by N F Alley Conv. SA Sub-Committee. No signature for approval.|16-MAY-23
25694|Parakeelya Alkali Member|Proposer|Brewer et al.|16-MAY-23
24453|Pedirka Formation|Name source|Pedirka Railway Siding (disused); grid reference 521051, Dalhousie 1:250 000 sheet area.|16-MAY-23
24453|Pedirka Formation|Unit history|Part of "Gypsite land surface" on Oodnadatta 1:250 000 geological map (Freytag, et al., 1967).|16-MAY-23
24453|Pedirka Formation|Type section locality|Three metres red-brown clayey sand exposed in gully 200 m north of Hamilton Creek beside old railway line. Grid reference 523051.|16-MAY-23
24453|Pedirka Formation|Extent|The unit covers the flanks of all the surface anticlines and the broad, upland synclines of the Stevenson-Hamilton area on Dalhousie, an area of at least 2500 km2.|16-MAY-23
24453|Pedirka Formation|Thickness range|Up to 3 metres.|16-MAY-23
24453|Pedirka Formation|Lithology|Two metres dark red-brown, very fine to medium, poorly sorted, stiff clayey sand passing up to 1 m red-brown fine sand with minor red clay, moderately sorted, somewhat friable and becoming a dark red-brown clayey sand at top. The middle one metre of the lower unit is strongly infused with finely crystalline gypsum making a relatively tough, somewhat resistant interval and at the top of this lower interval is a weak carbonate palaeosol. Above the gypseous layer, the unit develops a somewhat prismatic structure. |16-MAY-23
24453|Pedirka Formation|Relationships and boundaries|Rests on Cordillo Silcrete/apparently conformably and either forms ground surface or is overlain by Woodgate Gravel probably disconformably.|16-MAY-23
24453|Pedirka Formation|Age reasons|No fossils have been recovered from the unit. Age indirectly estimated as ?Plio-Pleistocene from tenuous regional correlation and from the tectonic development of Dalhousie Anticline.|16-MAY-23
24453|Pedirka Formation|Proposed publication|Dalhousie, South Australia. Explanatory Notes, 1:250 000 geological series. Sheet SG/53-11.|16-MAY-23
24453|Pedirka Formation|Comments|The origin of the unit is obscure, and the interpretation and age quite unclear. The age given is the oldest reasonable estimate based on local observation.|16-MAY-23
24453|Pedirka Formation|Proposer|Krieg G.|16-MAY-23
24620|Petermorra Volcanics|Name source|From Petermorra Spring, 1.2 km northeast of Prospect Hill trig, northern Flinders Ranges, Moolawatana 1:100 000 and Callabonna 1:250 000 map sheets (TSAGG, 1986). Prospect Hill is the highest of a series of low hills rising ~100 m above the surrounding plains. Fringing the hills are a number of springs, including Petermorra Spring, which discharge from the Great Artesian Basin aquifer.|16-MAY-23
24620|Petermorra Volcanics|Type section locality|Along a north-south line 500 m west of Prospect Hill trig and between Petermorra Creek and the Dog Proof Fence.|16-MAY-23
24620|Petermorra Volcanics|Extent|Outcrop is restricted to a series of low east-west trending ridges in the Prospect Hill area.|16-MAY-23
24620|Petermorra Volcanics|Thickness range|The true thickness is indeterminate due to the lack of primary layering, the presence of superimposed strong foliation, and folding of unknown magnitude.|16-MAY-23
24620|Petermorra Volcanics|Lithology|The dominant rock type is porphyritic rhyolitic volcanics. Also present are volcaniclastic, epiclastic volcanic sandstone and sericitic sandstone. The volcanics have abundant ovoid phenocrysts (2-5 mm) of grey K-feldspar, mostly microcline and orthoclase, but also have some microperthite, sanidine, and plagioclase. Quartz phenocrysts (2-4 mm) occur in varying amounts and range from translucent grey to bluish in colour. The groundmass is fine grained, grey to dark yellowish grey, displaying a foliated granoblastic texture. It consists of quartz, K-feldspar, plagioclase and biotite with accessory apatite, zircon, monazite, allanite and tourmaline. The porphyritic lithotypes range in composition from ?dacite to rhyodacite through to rhyolite. Primary volcanic layering is poorly displayed, though broad compositional variations may reflect primary igneous layering. The porphyries have been deformed; recrystallisation of some feldspars and micas has resulted in a well developed muscovite-sericite foliation which is subvertical and trending 75o-105o magnetic. This unit is anomalously high in boron, with values ranging from 20-100 ppm. Pegmatite and quartz+tourmaline veins and dykes are both parallel to and cross-cut the foliation. The porphyry conformably overlies an unnamed sericitic sandstone member. This sandstone is a medium grained, pale greenish grey to pale grey, poorly bedded quartz-dominant unit with occasional pebbly zones (rounded clasts 3-5 mm diameter) with variable amounts of K-feldspar and sericite-muscovite, which together form less than 35% of the whole rock.|16-MAY-23
24620|Petermorra Volcanics|Relationships and boundaries|The volcanics conformably overlie an unnamed sericitic metasandstone member with a sharp contact that is exposed in a small creek northwest of Prospect Hill trig. The volcanics are intruded by White Well Granite and Prospect Hill Granite. Contacts with other igneous and metasedimentary rocks at Prospect Hill are either faulted or concealed. Unconformably overlying the Petermorra Volcanics is the Adelaidean Shanahan Conglomerate Member of the Paralana Quartzite.|16-MAY-23
24620|Petermorra Volcanics|Age reasons|The zircons from samples 6838 RS 675 and 678 form a relatively homogeneous population of deep hyacinth-coloured elongate grains with pyramidal terminations or fractured parts thereof. The grains are interpreted, on morphological grounds, to have formed from a single igneous crystallisation event. From a combined plot of the analyses of 6838 RS 675 together with those for 6838 RS 678. A regression line fitted to all twelve analyses has no excess scatter (MSWD of 1.1) with intercepts at 1560+/-2 Ma and 74+/-37 Ma. These two felsic volcanics therefore are considered to be coeval.|16-MAY-23
24620|Petermorra Volcanics|Correlations|Highly deformed felsic volcanics at the northern end of the Mount Painter Inlier between Moolawatana Homestead and Mount Fitton may be of similar age to the Petermorra Volcanics. Other felsic volcanics in the Mount Painter Inlier, including those near the Gunsight Prospect, Mount Neill, Harts Creek and west of Freeling Heights represent an older succession (Teale, in prep. b). No correlatives of the Petermorra Volcanics are known in SA outside of the Mount Babbage Inlier. However, it is reasonable to assume that they may occur on the concealed northern margin of the Curnamona Craton east of the Mount Babbage and Mount Painter Inliers.|16-MAY-23
24620|Petermorra Volcanics|Proposed publication|South Australia. Geological Survey Quarterly Geological Notes, 123: 18-31|16-MAY-23
24620|Petermorra Volcanics|Category|2|16-MAY-23
24620|Petermorra Volcanics|Proposer|Sheard M.J., Fanning C.M., Flint R.B.|16-MAY-23
24620|Petermorra Volcanics|Resdate|24-OCT-1991|16-MAY-23
24620|Petermorra Volcanics|Reserved? Yes/No|Yes|16-MAY-23
76225|Pinyatta Member|Name source|Pinyatta Creek, ~1300 m east of Mt. Daily.|16-MAY-23
76225|Pinyatta Member|Geomorphic expression|Mid level exposures on dissected hills, in ravines, and in anticlinal cores.|16-MAY-23
76225|Pinyatta Member|Type section locality|Composite section comprising Section H, 0 to 348 ft. (0 to 106.1 m) 30°59'47.36"S, 139°15'43.04"E to 30°59'51.77"S, 139°15'49.28"E, with faulted-out top beds and upper contact represented by Section G, 0 to 61 ft (0 to 18.6 m) 30°59'34.58"S, 139°16'0.24"E. Reference section: Basal beds of Section H repeated in Section Q, 190 to 320 ft (57.9 to 97.5 m) 30°59'58.14"S, 139°15'30.88"E to 30°59'53.86"S, 139°15'28.44"E, extending down to lower contact with Mernmerna Formation.|16-MAY-23
76225|Pinyatta Member|Extent|Exposed in low hills from South Moorowie Mine to Mt. Chambers Mine, Mt. Daily, and south towards Mt. Frome.|16-MAY-23
76225|Pinyatta Member|Thickness range|Composite maximum thickness, possibly faulted, from Sections H, Q is 277 m (489 ft). Estimated average ~46 m (151 ft) measured in other partly faulted sections across highly lenticular beds.|16-MAY-23
76225|Pinyatta Member|Lithology|Massive to thick bedded, cliff forming, peloid limestones at base; buff, pink to light grey, part silty to quartz granule-rich, part oolitic, with cross bedded arkosic sands, ripple marks, buff silty dolostone intraclasts, and abundant archaeocyaths.|16-MAY-23
76225|Pinyatta Member|Depositional environment|Carbonate platform as backreef shelf shoals at sites of high tidal energy, adjacent to abundant clastic carbonate (archaeocyath meadows) and moderate siliciclastic (emergent salt dome) sources.|16-MAY-23
76225|Pinyatta Member|Relationships and boundaries|Basal unit of the Moorowie Formation. Passage zones into massive light grey peloid limestones from the dark grey flaggy limestones and slump talus of the Mernmerna Formation below, and from the limestones into the overlying green and red micaceous siltstones of the Wookata Shale Member.|16-MAY-23
76225|Pinyatta Member|Structure and Metamorphism|Massive beds of low dip as ridge caps on broad fold limbs, to moderate dips in anticlinal cores.|16-MAY-23
76225|Pinyatta Member|Age reasons|Lower Cambrian, Stage 4, within the Pararaia janeae trilobite Zone (Figure 2 of Jago et al., this volume).|16-MAY-23
76225|Pinyatta Member|Correlations|Not confirmed outside Moorowie area; possible equivalents in Bunkers Graben. Broadly related to the upper Wilkawillina Limestone (Figure 2 of Jago et al., this volume).|16-MAY-23
76225|Pinyatta Member|Defn author|Mount, T.J. 08-JAN-2019, after Mount (1970).|16-MAY-23
76225|Pinyatta Member|References|Jago, J. B., Gehling, J. G., Betts, M. J., Brock, G. A., Dalgarno, C. R., Garcia-Bellido, D. C., .., Paterson, J. R. (2019). The Cambrian System in the Arrowie Basin, Flinders Ranges, South Australia. Australian Journal of Earth Sciences. doi:10.1080/08120099.2018.1525431   **Mount, T. J. (1970). Geology of the Mt. Chambers Gorge region (BSc. (Honours) thesis, unpublished).Adelaide, SA: University of Adelaide. http:hdl.handle.net/2440/67162.  **T. J. Mount, J. B. Jago, N. R. Langsford & C. R. Dalgarno (2019): Geological setting of the Moorowie Formation, lower Cambrian Hawker Group, Mt Chambers Gorge, eastern Flinders Ranges, South Australia, Australian Journal of Earth Sciences, DOI: 10.1080/08120099.2019.1586771.|16-MAY-23
15294|Pirramimma Sand Member|Name source|Pirramimma Vineyards and Winery, grid reference 275761988 Noarlunga 1:50 000 Sheet area.|16-MAY-23
15294|Pirramimma Sand Member|Type section locality|Above 51.5 m in S. Australian Department of Mines Stratigraphic Borehole WLG 42 (State No. 697017402), adjacent section 174, Hundred Willunga. Noarlunga 1:50 000 sheet area, grid reference 275360982. No outcrop positively recognised. Soil cover prevents outcrop of the unit.|16-MAY-23
15294|Pirramimma Sand Member|Extent|From subsurface data, the unit occurs in the central area of the Willunga Embayment from Willunga and McLaren Vale in the east towards Aldinga in the west. Lithologically similar sand in the subsurface of the Adelaide Plains may also be referred to this unit.|16-MAY-23
15294|Pirramimma Sand Member|Thickness range|Range 0-115 m.|16-MAY-23
15294|Pirramimma Sand Member|Lithology|Weakly cemented, homogenous, fine grained sand. Quartz is the predominant mineral constituent. Localised calcareous and ferruginous cementation occurs. Yellow/buff colour.|16-MAY-23
15294|Pirramimma Sand Member|Relationships and boundaries|Pirramimma Sand is distinguished from other members of the Port Willunga Formation by its non-calcareous nature. A sharp boundary between calcareous Aldinga or Ruwarung Members and Pirramimma Sand is generally recognised. Pirramimma Sand passes laterally into calcareous units of the Port Willunga Formation towards the centre of the St Vincent Basin. Pirramimma Sand is unconformably overlain by Quaternary silts, sands and gravels in many sections.|16-MAY-23
15294|Pirramimma Sand Member|Age reasons|Fossils are scarce in most sections of Pirramimma Sand but rare foraminifera support a late Eocene to early Miocene age. This is supported by the age of units underlying and laterally equivalent to Pirramimma Sand.|16-MAY-23
15294|Pirramimma Sand Member|Proposed publication|Quarterly Geol Notes, Geological Survey SA 64:2-5 (1977)|16-MAY-23
24460|Point Ellen Formation|Unit history|Point Ellen Formation New stratigraphic unit.|16-MAY-23
24460|Point Ellen Formation|Type section locality|The type section is exposed in the sea-cliffs at Point Ellen at the southwestern entrance to Vivonne Bay, in the Marine Board Reserve adjacent to section 106 hundred of Newland.|16-MAY-23
24460|Point Ellen Formation|Extent|Limited to a small area at point Ellen, overlying Late Pliocene sediments in the "Table Rock" cliff section, a small outcrop at Cape Willoughby and a thin remnant overlying the Cape Jervis Beds at Cape Jervis.|16-MAY-23
24460|Point Ellen Formation|Thickness range|Variable, but up to 2 m.|16-MAY-23
24460|Point Ellen Formation|Lithology|Richly fossiliferous limestone and coquinite composed predominantly of fossil gastropods.|16-MAY-23
24460|Point Ellen Formation|Age reasons|Early Pleistocene.  On the ocean coastline of Point Ellen, just south of the car park, the bedrock Kanmantoo Group metasediments are overlain with marked unconformity by richly fossiliferous coquinite (Fig. 21). These sediments infill a highly irregular surface eroded in the bedrock, and clearly represent deposition in a restricted bay or inlet on a rocky coast. Abundant cobbles and boulders of bedrock metasediments occur within the fossiliferous sediments. In some places, there are beds crowded with gastropods including a new species of Nerita (Fig. 22). The section is of highly variable thickness to a maximum of 2 m because of the irregular topography of the bedrock unconformity, and is capped by a complex calcrete profile. Towards the eastern end of the outcrop, conspicuous large solution pipes extend through the calcrete capping and the fossiliferous sandstones, and bottom on bedrock at the unconformity. The rich molluscan fauna can be directly correlated with that of the Roe Calcarenite in the Eucla Basin described by Ludbrook (1978). Its most important constituent is the pelagic janthinid gastaropod Hartungia dennanti chavani which is conspicuous among the mass of Nerita shells in the cliff face. This molluscan fauna, so far unrecognised in South Australia, is reported in a separate paper (Ludbrook 1983) which includes a description of the new species of Nerita and a new lucinid. Specimens first collected from this locality in 1914 by Arthur Wade were identified by F. Chapman. Most of Wade's material is in the Palaeontological Collection of the Geological Survey of South Australia, but some was retained in the National Museum of Victoria, including the holotype of Glycymeris australia var. gigantea Chapman, which is a specimen of Anodontia sphericula (Basedow), common in both the Hallett Cove Sandstone and the Roe Calcarenite, and having a range of Middle Miocene to Early Pleistocene. Chapman correctly determined the fossils from Point Ellen as "equivalent to the Werrikooian of Victoria or Upper Pliocene". The Werrikoo Limestone in Victoria is now considered to straddle the Pliocene-Pleistocene boundary, the foraminifera indicating that only the lower part including the basal shell bed is of probable Late Pliocene age, the rest being Early Pleistocene (Singleton et al. 1976).|16-MAY-23
24460|Point Ellen Formation|Correlations| Problems of making direct faunal correlation between the Point Ellen Formation and the Werrikoo Limestone are twofold: first, no modern descriptions or differentiated lists of Werrikooian molluscs from the Glenelg River sequence are published and, secondly, depositional environments were sufficiently different to be reflected in the assemblages. The western side of the Point Ellen outcrop was illustrated by Daily et al. (1979), who considered the presence of Anodontia to indicate a possible Pliocene age. This is not supported by the stratigraphical range of Anodontia sphericula. Other Roe Calcarenite species occurring in the Point Ellen Formation include Timoclea (Veremolpa) kendricki Monilea euclensis and Hartungia dennam chavani. Foraminifera are poorly represented but include Ammonia beccarii, Elphidium rotatum and Epistomaroides polystomelloides all of which are species still living.|16-MAY-23
24460|Point Ellen Formation|Proposed publication|Trans. Roy. Soc. S. Australia 107: 1-35 (1983)|16-MAY-23
24460|Point Ellen Formation|Proposer|Cooper B.J.|16-MAY-23
15393|Polda Formation|Name source|Polda Pumping Station: grid reference 531400 m E, 292100 m N of Zone 53, Kimba 1:250 000 Sheet area.|16-MAY-23
15393|Polda Formation|Unit history|"Polda formation" (Harris and Foster 1974).|16-MAY-23
15393|Polda Formation|Type section locality|Polda Stratigraphic Hole No. 1 from 68 m to 154 m below ground level. The top is poorly identified as it occurs within a sandstone. The base is identified by a change from carbonaceous sand and gravel to grey-green silt bearing pebbles of gneiss and other metamorphic rocks. Located at 530080 m E 6290070 m N of Zone 53.|16-MAY-23
15393|Polda Formation|Extent|Subsurface only. From 25 km east of Lock to at least 40 km west of Lock with a known width of 10 km. Known only on the Kimba 1:250 000 Sheet area.|16-MAY-23
15393|Polda Formation|Thickness range|In the type section, 86 m, in reference section P17 it is 57 m and in P84 it is 55.9 m thick. The thickest knowns ection is 96 m at P70 (558998.7 m E, 6287543.4 m N).|16-MAY-23
15393|Polda Formation|Lithology|a) Upper sandstone: dark brown, grye, medium to coarse grained, angular to sub-angular, quartz, pyritic, with clay matrix; 31 m thick.  b) middle carbonaceous claystone, lignite, siltstone, and fine-grained sandstone, all pyritic, 18 m thick; lower sandstone and claystone: sandstone is grey, silty, with clay matrix; of subangular quartz; claystone very dark grey, with coarse, subangular quartz grains.  Reference sections: The type section is supplemented by two reference sections: Drillhole P17 (AMG coordinates 559103.9 m E, 624863.7 m N) from 51.0 m to 108 m and drillhole P84 (552993.6 m E, 628636.7 m N) from 44.1 m to 104.0 m.|16-MAY-23
15393|Polda Formation|Relationships and boundaries|In the type section the Polda Formation overlies presumed Permian glacigene sediments, elsewhere in the Polda Basin it overlies proven Permian or, in its absence Proterozoic metamorphic rocks. The formation top is an unconformity, it may be recognised by Tertiary sandstone or Jurassic claystone or sandstone, the latter is very difficult to recognise on any grounds other than palynological.|16-MAY-23
15393|Polda Formation|Age reasons|Palynological age dating everywhere indicates Late Jurassic (Harris and Foster, 1974, Harris in Gatehouse, 1980). Genera and species are described in Harris and Foster (1974).|16-MAY-23
15393|Polda Formation|Proposed publication|Quarterly Geological Notes, SA Geological Survey|16-MAY-23
26109|Port Willunga Formation|Name source|From town of Port Willunga on eastern shore of Gulf St Vincent.|16-MAY-23
26109|Port Willunga Formation|Type section locality|Coastal cliffs of Gulf St Vincent from Snapper Point to Chinaman Gully.|16-MAY-23
26109|Port Willunga Formation|Extent|Wide occurrence throughout St Vincent Basin.|16-MAY-23
26109|Port Willunga Formation|Thickness range|Extremely variable due to erosional removal 0-150 m ranges known.|16-MAY-23
26109|Port Willunga Formation|Lithology|Coarse grained bioclastic limestone with variable amounts of clay. Nodular chert is characteristic of the Ruwarung Member. Quartz sand predominant in the Pirramimma Sand Member.|16-MAY-23
26109|Port Willunga Formation|Relationships and boundaries|Disconformably overlies Chinaman Gully Formation. Unconformably overlain by Pliocene or younger sediments. Lateral equivalent to much of Rogue Formation.|16-MAY-23
26109|Port Willunga Formation|Age reasons|Late Eocene to Middle Miocene.|16-MAY-23
26109|Port Willunga Formation|Proposed publication|Rep. Inv. Geological Survey SA, 50|16-MAY-23
26109|Port Willunga Formation|Comments|Aldinga Limestone and Oaklands Limestone (Crespin, 1954) are identical with the Port Willunga Formation.|16-MAY-23
26109|Port Willunga Formation|Status|1|16-MAY-23
24622|Prospect Hill Granite|Name source|Adapted from Prospect Hill, 16.6km northwest of Mount Babbage at the northern end of the Flinders Ranges, Moolawatana 1:100 000 and Callabonna 1:250 000 map sheets. Initially used informally by Teale et al. (1989).|16-MAY-23
24622|Prospect Hill Granite|Type section locality|West of Petermorra Springs and north of Prospect Hill trig point (Fig. 3).|16-MAY-23
24622|Prospect Hill Granite|Extent|A narrow exposure at the northern end of the Prospect Hill area about 2.8 km long and only 100-200 m wide. It is the northernmost exposure of the Mount Babbage Inlier.|16-MAY-23
24622|Prospect Hill Granite|Lithology|The dominant rock type consists of a distinctive porphyritic granitic rock, grey in colour with fine to medium-grained groundmass. Sparsely scattered throughout are anhedral to round off-white phenocrysts (10-15 mm) of microperthitic microcline. The groundmass consists of subequal amountsof orthoclase, plagioclase, bluish quartz and approximately 10% biotite. Accessory minerals include tourmaline, fluorite, monazite and allanite. The bulk mineralogy is consistent with an adamellite. Wispy biotite-rich xenoliths are common in some zones at the eastern end of the outcrop within a more equigranular variety of the adamellite. Characteristic of the Prospect Hill Granite are clots of tourmaline (30-100 mm across) which are concentrated along the southern contact with the Petermorra Volcanics. Boron is anomalously high with values ranging from 90-550 ppm. Post emplacement deformation has imparted a weak foliation with a subvertical dip and strike of ~85o-95o magnetic.|16-MAY-23
24622|Prospect Hill Granite|Relationships and boundaries|A broadly concordant but intrusive southern contact with Petermorra Volcanics. Adjacent volcaniclastic sandstone (including the unnamed sericitic sandstone member of Petermorra Volcanics) near the contact contains abundant clots and aggregates with tourmaline and quartz, formed by fluids which emanated from the Prospect Hill Granite.|16-MAY-23
24622|Prospect Hill Granite|Age reasons|High-level plutons of the Prospect Hill Granite and White Well Granite intrude the sequence. Neither has been dated, but are assumed to be of similar age to other, deeper-level granitoids in the region that have statistically identical U-Pb zircon ages of 1556+/-4, 1556+/-10 and 1557+/-6 Ma.|16-MAY-23
24622|Prospect Hill Granite|Correlations|A similar porphyritic adamellite occurs as pods and narrow lenticular bodies within the Terrapinna Granite south of White Well Bore. No other direct correlative is known.|16-MAY-23
24622|Prospect Hill Granite|Proposed publication|South Australia. Geological Slurvey Quarterly Geological Notes, 123: 18-31.|16-MAY-23
24622|Prospect Hill Granite|Category|2|16-MAY-23
24622|Prospect Hill Granite|Proposer|Sheard M.J., Fanning C.M., Flint R.B.|16-MAY-23
24622|Prospect Hill Granite|Resdate|24-OCT-1991|16-MAY-23
24622|Prospect Hill Granite|Reserved? Yes/No|Yes|16-MAY-23
27223|Pualco Tillite|Name source|Pualco Range latitude 32o58'03", longitude 139o36'57" Olary 1:250 000 sheet area.|16-MAY-23
27223|Pualco Tillite|Type section locality|3300 m tillite and quartzite, Pualco Range. Base latitude 32o58'45"S, longitude 139o38'28"E; top latitude 32o57'15", 139o36'45". Top is ridge-forming tillite with greenish-grey sandy calcitic matrix (18 m). Base is valley-forming tillite with dark grey matrix, sparse pebbles (18 m).|16-MAY-23
27223|Pualco Tillite|Extent|Olary 1:250 000 sheet area; part of Orroroo 1:250 000 sheet area.|16-MAY-23
27223|Pualco Tillite|Thickness range|Usually less than in type section; very variable, 0-3300 m.|16-MAY-23
27223|Pualco Tillite|Lithology|Greyish tillite with sandy, carbonate-bearing matrix, contains pebbles and cobbles of igneous and metasedimentary lithology. Also feldspathic quartzite, siltstone and minor martite-rich rocks (toward top of formation).|16-MAY-23
27223|Pualco Tillite|Relationships and boundaries|Unconformably overlies Burra Group; conformably overlain by Benda Siltstone.|16-MAY-23
27223|Pualco Tillite|Age reasons|Precambrian, Adelaidean, Sturtian-earliest glacial phase. Probably equivalent to Bolla Bollana Formation, at least in part. Previoulsly referred to as 'Appila Tillite', but Coats has demonstrated this to be unlikely.|16-MAY-23
27223|Pualco Tillite|Defn author|Forbes B.G., Cooper R.S., 1976|16-MAY-23
27223|Pualco Tillite|Proposed publication|Quarterly Geological Notes, Geological Survey SA|16-MAY-23
15684|Purni Formation|Name source|French Petroleum Co. (Australia) Ltd. Purni No. 1 well. Dalhousie 1:250 000 sheeet area. Grid Ref. 412736.|16-MAY-23
15684|Purni Formation|Type section locality|F.P.C.(A) Purni No. 1 well between 1417 m and 1698 m.|16-MAY-23
15684|Purni Formation|Extent|The formation is not known in outcrop. Its subcrop is believed to extend over the thicker parts of the Pedirka Basin (Youngs, in press)*.|16-MAY-23
15684|Purni Formation|Thickness range|3-350 m.|16-MAY-23
15684|Purni Formation|Lithology|Beds of white kaolinitic sandstone; occasional thin conglomerates; thinly bedded grey shales, frequently carbonaceous; siltstones; thin coals and very carbonaceous shales.|16-MAY-23
15684|Purni Formation|Relationships and boundaries|It disconformably overlies the Crown Point Formation (except in Amerada Hale River No. 1) and is unconformably overlain by Mesozoic strata. The base is defined by a conglomeratic, silty, grey to black shale with minor coal lenses. The top of the formation at the type section, is marked by beds of black coal, interbedded with thin silty shales.|16-MAY-23
15684|Purni Formation|Age reasons|Early Permian. Palynological evidence suggests it is restricted to Stage 3, but it could extend down to Stage 2 (Harris, 1972).|16-MAY-23
15684|Purni Formation|Defn author|Youngs B.C., 1975|16-MAY-23
15684|Purni Formation|Proposed publication|Quarterly Geological Notes, Geological Survey SA|16-MAY-23
15684|Purni Formation|Comments|The Purni Formation is divisable into three members, these are defined briefly below: Upper Member - F.P.C.(A).  Purni No. 1 well between 1417 and 1536 m. Fine, white, kaolinitic sandstones; silts; grey shales; carbonaceous shales.  Middle Member - F.P.C.(A) Purni No. 1 well between 1536 and 1603 m. Fine to medium, grey-brown, well sorted, kaolinitic sandstone. Occasional thin interbeds of silts and carbonaceous shales.  Lower Member - F.P.C.(A). Purni No. 1 well between 1603 and 1698 m. Thinly bedded, grey shales with lenses of fine to medium, grey, kaolinitic sandstones and occasional conglomerates. Rare coal bands.  *The Purni Formation is also known from Mokari No. 1, McDills No. 1 and Hale River No. 1.|16-MAY-23
15684|Purni Formation|Defn approved by|Stuart W.J., Gatehouse C.G.|16-MAY-23
15684|Purni Formation|State(s)|SA & NT|16-MAY-23
24469|Recovery Formation|Name source|Recovery Creek, 5 km E. of 'Callanna'.  Map Symbol Pkr.|16-MAY-23
24469|Recovery Formation|Unit history|Recovery Formation' of Murrell (1977). Probably R4 unit of Rowlands et al. (1980, p.61).|16-MAY-23
24469|Recovery Formation|Type section locality|Plains and low hills 3 km SE of The Dome; from latitude 29o46', longitude 137o56' to latitude 29o45', longitude 137o57'.|16-MAY-23
24469|Recovery Formation|Extent|Willouran Ranges.|16-MAY-23
24469|Recovery Formation|Thickness range|2217 m in the type section; thins to the south.|16-MAY-23
24469|Recovery Formation|Lithology|Lithological sequence in type section: Top: 60 m quartzite, medium grey, greenish grey, very fine grained, laminated, mud cracks. 374 m fine-grained sandstone and siltstone; grey, greenish grey, brownish, thin to medium bedded, lenticular bedding, mud cracks, ripple marks, shale clasts, halite and gypsum casts. 240 m similar sandstone and siltstone to that above with interbedded limestone and dolomite, yellowish, grey brownish; shortite pseudomorphs and micaceous porphyroblasts. 908 m siltstone, sandstone and quartzite, fine to coarse grained; grey, greenish grey, brownish, ripple marks, shale clasts, mud cracks, cross-bedding, lenticular bedding, load casts, halite and shortite casts. 529 m siltstone and carbonate (calcitic and dolomitic) with minor fine-grained sandstone; carbonate, grey, yellowish, brownish, thin and medium bedded, with shortite pseudomorphs and micaceous mineral; some covered intervals.  Base: 142 m poorly exposed sandstone and quartzite, grey, platy to flaggy, mud cracks, ripple marks, halite casts. Overall sand:shale:carbonate percentages - 38:45:17.|16-MAY-23
24469|Recovery Formation|Relationships and boundaries|Base is faulted against megabreccia and top conformably overlain by Hogan Dolomite.|16-MAY-23
24469|Recovery Formation|Identifying features|A thick silty to sandy sequence between Dunns Mine Limestone and Hogan Dolomite.|16-MAY-23
24469|Recovery Formation|Age reasons|Possibly late Willouran.  Some resemblance to Nilpinna Beds or adjacent units in the Peake and Denison Ranges (Ambrose et al., 1981). May be equivalent to the lithologically similar Niggly Gap Beds of the Worumba Anticline (Preiss, 1980).|16-MAY-23
24469|Recovery Formation|Proposed publication|Quarterly Geological Notes, Geological Survey SA, 79: 7-16|16-MAY-23
24469|Recovery Formation|Proposer|Murrell B.|16-MAY-23
26322|Relief Sandstone|Name source|From Relief Bore (Latitude 27o50'11"S, Longitude 133o50'52"E) on the Wintinna 1:250 000 topographic map.|16-MAY-23
26322|Relief Sandstone|Type section locality|Meramangye-1 (Latitude 28o22'10"S, Longitude 132o16'28"E) 357.6 to 447.2 m.|16-MAY-23
26322|Relief Sandstone|Extent|The Relief Sandstone is not known to crop out, but has been intersected in numerous drillholes in the Emu and Marla-Manya areas (Fig. 7). It may also occur at the bottom of Wilkinson-1 below the Ouldburra Formation.|16-MAY-23
26322|Relief Sandstone|Thickness range|In the type section the Relief Sandstone is approximately 90 m thick, it is 117 m at Giles-1 while in the Marla-Manya area it exceeds 300 m. Figure 7 shows the distribution of thickness in drillhole intersections.|16-MAY-23
26322|Relief Sandstone|Lithology|The Relief Sandstone is a mottled medium to pale brown moderately well consolidated silica cemented, very fine to very coarse grained sandstone. In the type section and other nearby drillholes the lower portion is medium to fine grained, moderately to poorly sorted with subrounded to rounded terrigenous and metamorphic quartz clastic grains. The cement is commonly siliceous but minor calcite, dolomite, and gypsum occur locally and iron staining is evident in part. Small and medium scale cross-bedding is present. The upper unit contains numerous pale to olive-grey siltstone and minor claystone interbeds up to, and occasionally exceeding, half a metre thick. In the Marla-Manya area the sandstone ranges from pale red to olive-grey and medium brown. The formation top is characterised by planar laminae delineated by very fine to very coarse variations of grainsize. Sorting is moderate to poor; anhydrite nodules, and fragments and patches of sulphate  evaporite cement are rare. Small and medium-scale cross-bedding is common. The composition of the lower portion of the formation reflects proximity to the underlying rock units with an overall increase in grainsize and abundance of pebble to cobble sized gneiss clasts.|16-MAY-23
26322|Relief Sandstone|Depositional environment|There is no unequivocal evidence for the environment of deposition. The lower portion of the formation (up to 80 m thick) in the Emu area is moderately to locally well-=sorted with small to medium low-angle cross bedding and carbonate and evaporite cement in parts. This widespread unit of monotonous clean sandstone is thought to be a marine deposit. The basal few metres of the type section, and at Observatory Hill-1, appear to be reworked. This possibly suggests deposition and subsequent reworking during transgression. Alternating siltstone and sandstone in the upper portion of the type section and in Giles-1 suggest a possible fluvial environment, and may indicate local regression. In the Marla-Manya area the relationship between the Relief Sandstone and the overlying Ouldburra Formation indicates that the upper portion of the Relief Sandstone was deposited in shallow marine conditions.|16-MAY-23
26322|Relief Sandstone|Relationships and boundaries|In the Emu area the Relief Sandstone disconformably overlies the Rodda beds. In the Marla-Manya area however the unit unconformably overlies either ?Adelaidean volcanics, crystalline basement, or rests disconformably on older sediments.|16-MAY-23
26322|Relief Sandstone|Age reasons|The Relief Sandstone is stratigraphically older than the Early Cambrian Ouldburra Formation and younger than the ?Adelaidean Rodda beds.|16-MAY-23
26322|Relief Sandstone|Defn author|Brewer A.M., Dunster J.N., Gatehouse C.G., Henry R.L., Weste G.|16-MAY-23
26322|Relief Sandstone|Proposed publication|Quarterly Geological Notes, Geological Survey SA, 102|16-MAY-23
26322|Relief Sandstone|Proposer|Brewer A.M., Dunster J.N., Gatehouse C.G., Henry R.L., Weste G.|16-MAY-23
24623|Rockleigh Formation|Name source|Rockleigh, grid reference 6130500N, 325150E, Tepko 1:50 000 Sheet area, Adelaide 1:250 000 Sheet area.|16-MAY-23
24623|Rockleigh Formation|Type section locality|130 m downstream from Loxtons Creek on north bank of Gorge Creek. Supplementary section 300 m up Gorge Creek from Loxtons Creek in east bank.|16-MAY-23
24623|Rockleigh Formation|Extent|1 km in the valley of Gorge Creek and its tributary Loxtons Creek on the eastern slopes of the South Mount Lofty Ranges.|16-MAY-23
24623|Rockleigh Formation|Thickness range|Maximum 9 m but variable|16-MAY-23
24623|Rockleigh Formation|Lithology|The basal unit (unit A) comprises light to dark grey sandy clay, about 2 m thick. Overlain by unit B a bioturbated pale grey-brown porous laterally persistent locally calcified unit. Overlain by unit C which is a sandy clay with persistent carbonaceous laminae and local peat beds. At the supplementary type section unit C is a soft sand with peat beds to 10 cm thick. Unit D is a calcareous sand with some clay matrix and calcrete horizons and overlies the entire area.|16-MAY-23
24623|Rockleigh Formation|Relationships and boundaries|Overlies Backstairs Passage of the Kanmantoo Group with unconformity. The Rockleigh Formation extends laterally up small secondary valleys of Gorge and Loxtons Creeks.|16-MAY-23
24623|Rockleigh Formation|Age reasons|The Formation contains freshwater gastropods (Austrosuccinea australis (Ferussac)) (Ludbrook, 1984), spore and pollen (Grubb, 1978), ?Macropus bone fragments (Pledge, pers. Comm., 1984). Radiocarbon age dating on two samples gave 6600+/-100 yrs B.P. on the lower sample and 8000 yrs B.P. (Grubb, 1978) on the upper. Amins acid racemization suggest a late Pleistocene age for the gastropods. Ludbrook suggests that the gastropods are of Holocene age.|16-MAY-23
24623|Rockleigh Formation|Defn author|First defined: Gatehouse C.G., Murray-Wallace C.V|16-MAY-23
24623|Rockleigh Formation|Comments|GSSA Q.N. 92|16-MAY-23
24623|Rockleigh Formation|First Reference|85/2487|16-MAY-23
24623|Rockleigh Formation|Proposer|Gatehouse C.G., Murray-Wallace C.|16-MAY-23
24623|Rockleigh Formation|Resdate|12-FEB-1988|16-MAY-23
27299|Rook Tuff|Name source|West Rook workings, NNW of Willouran Hill. Map symbol: Pkk.|16-MAY-23
27299|Rook Tuff|Unit history|Rook Tuff' of Murrell (1977), probably R3.1 unit of Rowlands et al. (1980, p.62).|16-MAY-23
27299|Rook Tuff|Type section locality|Dark, fine-grained rocks on SW side of ridge, 3 km SSE of The Dome; latitude 29o46', longitude 137o56'.|16-MAY-23
27299|Rook Tuff|Extent|Willouran Ranges.|16-MAY-23
27299|Rook Tuff|Thickness range|42 m in type section; 15-60 m elsewhere.|16-MAY-23
27299|Rook Tuff|Lithology|In type section, very dark-weathering, medium dark grey or light brownish flagstones, partly laminated. Near Rook workings, contains partly tuffaceous grey shale and siltstone with thin reddish porphyritic tuff, possibly an ignimbrite (Whitehead, 1980).|16-MAY-23
27299|Rook Tuff|Relationships and boundaries|Lies conformably between Dome Sandstone and Dunns Mine Limestone.|16-MAY-23
27299|Rook Tuff|Identifying features|Dark flaggy, fine-grained rocks, partly volcanic, between Dome Sandstone and Dunns Mine Limestone.|16-MAY-23
27299|Rook Tuff|Age reasons|Possibly late Willouran. No certain equivalents known from outside the Willouran Ranges.|16-MAY-23
27299|Rook Tuff|Proposed publication|Quarterly Geological Notes, Geological Survey SA, 79:7-16.|16-MAY-23
16480|Ruwarung Member|Name source|An aboriginal place name meaning brackish water place. Ruwarung refers to springs originating in the Port Willunga Formation along Aldinga Bay between Aldinga Ck and Snapper Point.|16-MAY-23
16480|Ruwarung Member|Unit history|"Interval with cherty nodules". Lindsay, 1967, p.95-97. Port Willunga Beds "siliceous unit". Lindsay, 1969, p.35|16-MAY-23
16480|Ruwarung Member|Type section locality|Coastal cliffs along Aldinga Bay between Aldinga Creek and Snapper Point, specifically between samples 138-66 and 9-67 inclusive of Lindsay (1967, Figs 1 and 2).|16-MAY-23
16480|Ruwarung Member|Extent|Near the coast of Aldinga Bay in the Willunga Embayment, Noarlunga Embayment and in the subsurface of the Adelaide Plains.|16-MAY-23
16480|Ruwarung Member|Thickness range|Type Section = 16 m. Noarlunga Embayment coastal section = 22 m.|16-MAY-23
16480|Ruwarung Member|Lithology|Hard, grey spicular nodules of chert characterise this unit. These are interbedded with fawn/grey fossiliferous, calcareous sands, silts and clays.|16-MAY-23
16480|Ruwarung Member|Relationships and boundaries|This unit is distinguished solely on the occurrence of nodular silicification. It overlies the Aldinga Member and passes laterally into the Pirramimma Sand Member.|16-MAY-23
16480|Ruwarung Member|Age reasons|Oligocene in age after Lindsay (1967). Lindsay studied the foraminifera and recognised the Chiloguembelina cubensis zone in this unit.|16-MAY-23
16480|Ruwarung Member|Proposed publication|Quarterly Geological Notes, Geological Survey SA 64: 2-5 (1977)|16-MAY-23
16480|Ruwarung Member|References|01/31615; 79/05157|16-MAY-23
24484|Saint Francis Granite|Name source|St Francis Is, Nuyts Archipelago, located ~55 km SW of Ceduna.|16-MAY-23
24484|Saint Francis Granite|Type section locality|Reference sections: Outcrops containing representative lithologies occur widely on eastern St Francis Is, western West Is and at Point Peter.|16-MAY-23
24484|Saint Francis Granite|Extent|Isolated exposures on St Francis, West, Masillon, Fenelon, Smooth and Egg Islands, plus Point Peter and Cape Beaufort.|16-MAY-23
24484|Saint Francis Granite|Lithology|Three similar leucogranite to leucoporphyry varieties occur. Exposed on eastern St Francis, Fenelon, Masillon, Smooth and Egg Islands is a distinctive grey granite which varies from equigranular, medium-grained to porphyritic with both K-feldspar and quartz phenocrysts. The mafic content is low (<2%) and is chiefly aegerine-augite, hornblende and magnetite. Graphic intergrowths of quartz and K-feldspar form >90% of the rock. White to pale grey leucogranite, exposed on West Is, and intruding Nuyts Volcanics on St Francis Is, also have low mafic content. Amphibole, sphene and magnetite are the main mafic constituents. The felsic component varies greatly in nature from coarse-grained fragments of perthitic K-feldspar to a recrystallised granular mosaic of quartz and feldspar within microshear bands. White leucoporphyry at Point Peter has similar lithological characteristics being very felsic and containing only very minor quantities of biotite and magnetite. Microcline and quartz are the dominent constituents, with the perthitic microcline forming coarse crystals, partly corroded, in a graphic quartz and K-feldspar matrix.|16-MAY-23
24484|Saint Francis Granite|Relationships and boundaries|3 suites of felsic volcanic dykes and dolerite dykes intrude the grey granite on St Francis Is. The felsic dykes are correlated with the Nuyts Volcanics. Leucogranite intrudes and truncates dykes of pink rhyolite (Pa3-Nuyts Volcanics) which are within mylonitic augen gneiss on West Is, and leucogranite also form a small intrusive plug within the Nuyts Volcanics on western St Francis Is. These relationships suggest more than one phase of plutonism.|16-MAY-23
24484|Saint Francis Granite|Age reasons|Rb-Sr geochronology summarised in Webb et al (1986), 8 samples of grey granite from St Francis Is have high Rb/Sr ratios, and regression of 6 samples produced an isochron of 1478+/-15 Ma, IR = 0.70114+/-0.0032. A similar result was obtained for the leucogranite from West Is's regression of 4 samples gave an age of 1466+/-79 Ma, IR = 0.7142+/0.0196. Similar ages in the range 1470-1490 Ma were obtained for the Nuyts Volcanics, but are significantly younger than ages derived from U-Pb studies. Extrusive age of Nuyts Volcanics are 1631+/-3 Ma for St Francis Is, and 1627+/-2 Ma for St Peter Is. Rb-Sr ages are considered unreliable; field relationships infer intrusion of St Francis Granite is broadly synchronous with the Nuyts Volcanics.|16-MAY-23
24484|Saint Francis Granite|Correlations|Stratigraphic correlations: U-Pb isotopic ages for Nuyts Volcanics indicate the Nuyts Volcanics and St Francis Granite are older than, and not related to, the Gawler Range Volcanics and Hiltaba Suite granite. St Francis Granite and Nuyts Volcanics represent a discrete phase of felsic magmatism during the latter part of the Palaeoproterozoic. Correlatives of the St Francis Granite are not known elsewhere in South Australia.|16-MAY-23
24484|Saint Francis Granite|Proposed publication|Quarterly Geological Notes, Geological Survey of SA|16-MAY-23
24484|Saint Francis Granite|Comments|Published as Saint Francis Island Acid Volcanics 86/25148 Table 1 M.|16-MAY-23
24484|Saint Francis Granite|Category|2|16-MAY-23
24491|Second Plain Creek Member|Name source|Named after Second Plain Creek, near Wilkawillina Gorge, The Bunkers 1:50 000 Topographic Map, GR 930930.|16-MAY-23
24491|Second Plain Creek Member|Type section locality|The type section of the member is composed of 73.5 m of predominantly grey limestone exposed in an east-west running creek and on adjacent ridges at GR 986378 (the Bunkers topographic map sheet). This section is 760 m south of the type section of the Wilkawillina Limestone (Daily 1956) and the reference section of the Hawker Group (Dalgarno, 1964). The new member does outcrop in the above type/reference sections, but the new locality was chosen as the type section of the new member because in this locality the unit is both thicker and better developed.|16-MAY-23
24491|Second Plain Creek Member|Extent|The unit occurs discontinuously along the eastern margin of the Flinders Ranges, particularly in the Bunkers Range. The member is best developed near Wilkawillina Gorge within the Bunkers Graben.|16-MAY-23
24491|Second Plain Creek Member|Thickness range|Where measured the unit reaches a maximum thickness of 76 m. There is no reason to suspect that this is the minimum thickness of the unit. It is thickest in the centre of the Bunkers Graben, and thins markedly towards the margins of the structure, where it is at times absent.|16-MAY-23
24491|Second Plain Creek Member|Lithology|The unit is lithologically variable and includes lime mudstones, wackestones, packstones and grainstones, with intraclastic rudstones and floatstones. In the type section the member passes from a sparry red nodular limestone at the base into mottled limes, mudstones and wackestones which grade upward into interbedded wackestones, packstones and grainstones. The top of the sequence is often marked by intraclastic rudstones and floatstones. Fossils are common in the unit but are normally preserved as fragments.|16-MAY-23
24491|Second Plain Creek Member|Relationships and boundaries|The member disconformably overlies the Winnitinny Creek Member of the Wilkawillina Limestone (Clarke 1986a) along a karstic and locally calcreted surface. The member can be distinguished from the underlying unit by its darker colour and more micritic composition. The base of the Second Plain Creek Member locally contains clasts and pisoliths reworked from the underlying unit and its calcrete cap. The disconformity surface is irregular on a scale range from millimetres to tens of metres. The unit is conformably overlain by the Six Mile Bore Member of the Parara Limestone (Clarke 1986b). The member can be distinguished from the Parara Limestone by the Parara Limestone's much darker colour (grey to black when fresh), brown to yellow colour on weathered surfaces and abundant shale interbeds. The Parara Limestone is also nodular to flaggy in outcrop, while the Second Plain Creek Member tends well bedded to massive.|16-MAY-23
24491|Second Plain Creek Member|Age reasons|The underlying Winnitinny Creek Member contains Faunal Assemblage (FA) 2 of Daily (1956) while the Six ;Mile Bore Member of the Parara Limestone (overlying the Second Plain Creek Member) contains FA 3. The type section for the new member lies in the upper part of Gravestock's (1984) Section 'I' from which a new assemblage (as yet undesribed) was found to  contain archaeocyaths, Lapworthellids and brachipods. Gravestock (1984) correlated FA2 with the Early Cambarian Kameshky Horizon of the Altai-Sayan region of the USSR. The truncation of the top of FA in the Wilkawillina Gorge region makes determination of its duration difficult, but the absence of the subaerial disconformity at the top of FA 2 in the Mt Scott Range area, and its replacement by a rapid faunal turnover between FA 2 and 3 therefore suggests that this hiatus was of relatively brief biostratigraphic duration.|16-MAY-23
24491|Second Plain Creek Member|Proposed publication|Quarterly Notes of the Geological Survey of South Australia|16-MAY-23
24491|Second Plain Creek Member|Proposer|Clarke J.D.A.|16-MAY-23
24491|Second Plain Creek Member|Resdate|27-FEB-1986|16-MAY-23
24491|Second Plain Creek Member|Unit name|Second Plain Creek Member of the Wilkawillina Limestone|16-MAY-23
24496|Six Mile Bore Member|Name source|After Six Mile Bore, Wirrealpa 1:50 000 topographic map GR 080444.|16-MAY-23
24496|Six Mile Bore Member|Type section locality|207 metres of interbedded limestone and siltstone exposed in creek sections running east-west through the Bunkers  Range, The Bunkers, 1:50 000 topographic map GR 990392-991392. This is part of the type section as amended.|16-MAY-23
24496|Six Mile Bore Member|Extent|Within the Graben, and at various localities to the north along the Bunkers Range.|16-MAY-23
24496|Six Mile Bore Member|Thickness range|207-17 m|16-MAY-23
24496|Six Mile Bore Member|Lithology|Interbedded turbiditic limestone black calcareous siltstone, skeletal-pelloidal-sandy packstones and wackestones. Intraclastic mudstone and floatstone beds are also present. Mega blocks and large lithoclasts of older sediments (e.g. Wilkawillina Limestone) also occur. Slump folds, graded beds and sedimentary boudinage are common. Cross beds, ripple cross laminations and trace fossils are rare.|16-MAY-23
24496|Six Mile Bore Member|Relationships and boundaries|The unit is conformably overlain by Linns Springs Member and disconformably overlies the Wilkawillina Limestone. The unit interfingers with shallow water platform and platform edge facies to the southeast and becomes thin and discontinuous outside the graben to the north.|16-MAY-23
24496|Six Mile Bore Member|Age reasons|The unit contains trilobites of Faunal Assemblage III (Daily, 1956). It can therefore be assigned to the middle Early Cambrian (?Botomian).|16-MAY-23
24496|Six Mile Bore Member|Proposed publication|Quarterly Notes Geological Survey SA|16-MAY-23
24496|Six Mile Bore Member|Resdate|25-OCT-1985|16-MAY-23
82222|Skuse Hill Metapyroxenite|Name source|Skuse Hill, TARCOOLA, SH5310, 1:250,000 map sheet. Located at GDA2020, MGA53, 360175 mE, 6645030 mN.|16-MAY-23
82222|Skuse Hill Metapyroxenite|Unit history|Formerly known as 'Blackfellow Hill Pyroxenite' (Daly and Fanning 1993).|16-MAY-23
82222|Skuse Hill Metapyroxenite|Geomorphic expression|Weathers to bright green clay and chalcedony. Fresh lithology does not crop out (Daly and van der Stelt, 1992).|16-MAY-23
82222|Skuse Hill Metapyroxenite|Type section locality|Drillhole Blackfellow Hill 1 (3243), interval 86-170 m (total depth). Drilled by SADME, in 1991. Located at GDA2020, MGA53, 359420 mE, 6643868 mN. Reference Drillhole: Skuse Hill 2 (3242), interval 18-76 m. Drilled by SADME in 1991. Located at GDA2020, MGA53, 360686 mE, 6644988 mN. Core available at the SA Drill Core Reference Library, Tonsley.|16-MAY-23
82222|Skuse Hill Metapyroxenite|Extent|Occurs in drillholes near Skuse Hill in the southern Christie Domain.|16-MAY-23
82222|Skuse Hill Metapyroxenite|Thickness range|Intersections of the Skuse Hill Metapyroxenite are up to 58 m thick in the reference drillhole, but are significantly less in other drillholes (Daly and van der Stelt 1992). Individual intervals sometimes very thin (~10 cm; Daly and van der Stelt, 1992).|16-MAY-23
82222|Skuse Hill Metapyroxenite|Lithology|The Skuse Hill Metapyroxenite comprises metapyroxenite and metagabbro-norite. Metapyroxenite occurs as pale green tremolite-phlogopite schist with some actinolite +/- hornblende, variable plagioclase, minor chlorite and trace oxides and apatite. Tremolite may preserve textures of primary pyroxene. In some zones, original orthopyroxene (bronzite) is preserved forming a distinctive crescumulate texture and in others, sericitised plagioclase up to 8 mm occurs (Daly and van der Stelt 1992).The metagabbro-norite comprises amphibole, plagioclase, quartz and biotite with minor oxides and trace zircon and apatite. Recrystallised amphibole aggregates replaced pyroxene. Biotite and zircons in this lithology are interpreted to indicate some crustal contamination. Locally, augen of plagioclase up to 1 mm occur and elsewhere garnet occurs in layers with biotite (Daly and van der Stelt 1992).|16-MAY-23
82222|Skuse Hill Metapyroxenite|Relationships and boundaries|The pyroxenite lithology of the Skuse Hill Metapyroxenite occurs structurally below the discontinuous George Hill Iron Member, also associated with olivine-bearing metacarbonate (Christie Gneiss; Daly and van der Stelt 1992).|16-MAY-23
82222|Skuse Hill Metapyroxenite|Identifying features|Magmatic age c. 2460 Ma. Characteristic association with iron formation and carbonate rocks. Weakly magnetic.|16-MAY-23
82222|Skuse Hill Metapyroxenite|Structure and Metamorphism|Metamorphic texture varies from schistose to gneissic. Faint foliation related to retrogression at angle to main metamorphic fabric. Locally deformed to mylonite (Daly and van der Stelt, 1992).|16-MAY-23
82222|Skuse Hill Metapyroxenite|Age reasons|Early Paleoproterozoic; magmatic crystallisation at c. 2460 Ma (SHRIMP U?Pb zircon; Fanning et al. 2007)|16-MAY-23
82222|Skuse Hill Metapyroxenite|Correlations|Potential correlative of the Aristarchus Metaperidotite.|16-MAY-23
82222|Skuse Hill Metapyroxenite|Alteration and Mineralisation|Host accessory sulphide and has elevated nickel and chromium contents (Daly and van der Stelt, 1992; Kennecott Explorations (Australia) Pty. Ltd., 1971b).|16-MAY-23
82222|Skuse Hill Metapyroxenite|Geochemistry|Primitive Nd signature, low MgO and high Al2O3, Fe2O3T and CaO contents, which suggest mixing or modification of a depleted mantle source with fertile material possibly similar to primitive mantle or asthenospheric mantle (Wade, 2012).|16-MAY-23
82222|Skuse Hill Metapyroxenite|Defn author|williams, M.A., 9-JUN-2021.|16-MAY-23
82222|Skuse Hill Metapyroxenite|References|Claoue-Long, J.C., Hoatson, D.M., 2009. Guide to using the Map of Australian Proterozoic Large Igneous Provinces. Geoscience Australia. Record 2009/55, 37.  **Daly, S.J., Fanning, C.M., 1993. Archean, in: Drexel, J.F., Preiss, W.V., Parker, A.J. (Eds.), The Geology of South Australia. Volume 1 - The Precambrian. Geological Survey of South Australia,Bulletin, 54, pp. 32-49.  **Daly, S.J., van der Stelt, B.J., 1992. Archaean metabasic diamond drilling project. South Australia. Department of Mines and Energy. Open file Envelope 08541, 1531-1902.  **Fanning, C.M., Reid, A.J., Teale, G.S., 2007. A geochronological framework for the Gawler Craton, South Australia. Primary Industries and Resources South Australia. Bulletin 55.  **Kennecott Explorations (Australia) Pty. Ltd., 1971a. SML 491 - Final Report. South Australia. Department of Mines. Open file Envelope 01510, 304-347.  **Kennecott Explorations (Australia) Pty. Ltd., 1971b. SML 491 - Progress Report - July 1971. South Australia. Department of Mines. Open file Envelope 01510, 66-303.  **Lewis, P., 1983. Eighth quarterly and final report on Lake Barry EL 930, LEPA EL 931, and Mt. Christie EL 932, South Australia, for the period ending 15th November, 1983. South Australia. Department of Mines and Energy. Open file Envelope 04613, 150-222.  **Reid, A.J., Birt, T., Fraser, G.L., Daly, S.J., 2007. The geology of the Mulgathing Complex: from eastern Tallaringa to Glenloth Goldfield. Primary Industries and Resources South Australia. Report Book 2007/00017.  **Reid, A.J., Jagodzinski, E.A., Fraser, G.L., Pawley, M.J., 2014. SHRIMP U-Pb zircon age constraints on the tectonics of the Neoarchean to early Paleoproterozoic transition within the Mulgathing Complex, Gawler Craton, South Australia. Precambrian Research 250, 27-49.  **Wade, C.E., 2012. Geochemistry of pre-1570 Ma mafic magmatism within southern Australia: implications for possible tectonic settings and timing of major mineralisation events in South Australia. South Australia. Department for Manufacturing, Innovation, Trade, Resources and Energy. Report Book 2012/00019.  **Williams, M.A., Reid, A.J., 2021. Linking lithostratigraphy to mineral potential for the Archean to earliest Paleoproterozoic Mulgathing Complex, central Gawler Craton. South Australia. Department for Energy and Mining. MESA Journal 94, 04-18.|16-MAY-23
82224|Sloan Hill Tonalite|Name source|Sloan Hill, BILLA KALINA, SH5307, 1:250,000 map sheet. Located at GDA2020, MGA53, 565570 mE, 6681525 mN.|16-MAY-23
82224|Sloan Hill Tonalite|Unit history|Informally known as 'hematite-stained tonalite' (Jagodzinski and Reid 2017) and 'Mulgathing Complex unit 8'.|16-MAY-23
82224|Sloan Hill Tonalite|Geomorphic expression|Does not crop out.|16-MAY-23
82224|Sloan Hill Tonalite|Type section locality|Type Drillhole: (DDH) SH 7C (SA Geodata drillhole 237530), interval 1,427-1,467.5 m. Drilled by Uranium Exploration Australia Ltd in 2009. Located at GDA2020, MGA53, 569219 mE, 6682981 mN. Core available at the SA Drill Core Reference Library, Tonsley.|16-MAY-23
82224|Sloan Hill Tonalite|Extent|Intersected in drillholes in the eastern Mulgathing Complex near Sloan Hill. No known outcrop.|16-MAY-23
82224|Sloan Hill Tonalite|Thickness range|The minimum thickness of the Sloan Hill Tonalite is 40.5 m, as intersected in the type drillhole (base of lithology not intersected).|16-MAY-23
82224|Sloan Hill Tonalite|Lithology|Massive biotite-bearing tonalite, with abundant plagioclase, minor K-feldspar occurring as rims on plagioclase and minor muscovite. Granite with equigranular quartz, K-feldspar and lesser plagioclase also occurs. Variably hematite altered with zones of sericite-chlorite alteration (Jagodzinski and Reid 2017; Reid et al. 2017).|16-MAY-23
82224|Sloan Hill Tonalite|Relationships and boundaries|Unconformably overlain by Pandurra Formation. Relationship with other Mulgathing Complex units unknown.|16-MAY-23
82224|Sloan Hill Tonalite|Identifying features|Magmatic age c. 2530 Ma.|16-MAY-23
82224|Sloan Hill Tonalite|Structure and Metamorphism|Quartz shows undulose extinction, indicating minor deformation but lithology lacks solid-state deformation. Greenschist-facies metamorphism is inferred.|16-MAY-23
82224|Sloan Hill Tonalite|Age reasons|Neoarchean; magmatic age c. 2530 Ma (SHRIMP U-Pb zircon; Jagodzinski and Reid 2017).|16-MAY-23
82224|Sloan Hill Tonalite|Correlations|The Sloan Hill Tonalite may be a corelative of a c. 2526 Ma granite gneiss intersected in GOMA 4 DDH (Jagodzinski et al. 2013).	|16-MAY-23
82224|Sloan Hill Tonalite|Alteration and Mineralisation|Variable hematite and sericite-chlorite alteration. No mineralisation.|16-MAY-23
82224|Sloan Hill Tonalite|Defn author|Williams, M.A., 9-JUN-2021.|16-MAY-23
82224|Sloan Hill Tonalite|References|Cherry, J., 2009. Prominent Hill South. Annual & Final Report on Exploration Licence EL 3429 for the period 20 October 2007 to 19 October 2008. Primary Industries and Resources. South Australia. Open file Envelope 11345, 196-229.  **Jagodzinski, E.A., Reid, A.J., 2017. PACE Geochronology: Results of collaborative geochronology projects, 2013?2015. South Australia. Department of the Premier and Cabinet. Report Book 2015/00003.  **Jagodzinski, E.A., Reid, A.J., Dutch, R.A., 2013. Zircon and monazite geochronology via SHRIMP and LA-ICPMS for the northern Gawler Craton, from 2009 GOMA Drilling. South Australia. Department for Manufacturing, Innovation, Trade, Resources and Energy. Report Book 2013/00013.  **Raetz, M., Gilbert, D.J., 1993. CR 7837. Exploration Licence EL 1603. Reedy Lagoon Joint Venture. . South Australia. Department of Mines and Energy. Open file Envelope 08211, 292-362.  **Reid, A.J., Jourdan, F., Jagodzinski, E.A., 2017. Mesoproterozoic fluid events affecting Archean crust in the northern Olympic Cu-Au Province, Gawler Craton: insights from 40Ar/39Ar thermochronology. Australian Journal of Earth Sciences 64, 103-119.  **Williams, M.A., Reid, A.J., 2021. Linking lithostratigraphy to mineral potential for the Archean to earliest Paleoproterozoic Mulgathing Complex, central Gawler Craton. South Australia. Department for Energy and Mining. MESA Journal 94, 04-18.|16-MAY-23
24502|St Peter Suite|Defn author|Flint, Rankin and Fanning April 1990 (Issued in 1991) 91/27214|16-MAY-23
24502|St Peter Suite|Proposed publication|Geological Survey of SA Quarterly Geological Notes, 114.|16-MAY-23
24502|St Peter Suite|Category|2|16-MAY-23
24502|St Peter Suite|Name first published by|Flint, Rankin and Fanning April 1990 (Issued in 1991)|16-MAY-23
24502|St Peter Suite|Reserved? Yes/No|Yes|16-MAY-23
17451|Stuart Range Formation|Name source|A range of hills near Coober Pedy at Latitude 29o00 and Longitude 134o50' on the Coober Pedy 1:250 000 sheet. First discovered in Stuart Range No. 3 bore at Coober Pedy.|16-MAY-23
17451|Stuart Range Formation|Unit history|There is no marine shale unit in either the Cooper or the Pedirka Basins.|16-MAY-23
17451|Stuart Range Formation|Type section locality|(Subsurface) Cootanoorina 1 well Latitude 28o00.5'S and Longitude 135o20'E between 516.6 m and 777.2 m.|16-MAY-23
17451|Stuart Range Formation|Extent|No outcrop. In the subsurface, it covers most of the Arckaringa Basin with the exception of major structural highs (Townsend 1973/1975).|16-MAY-23
17451|Stuart Range Formation|Thickness range|260.6 m in Cootanoorina 1.|16-MAY-23
17451|Stuart Range Formation|Lithology|Shale or claystone dark greenish grey (wet), pale grey (dry). Occasional silt to fine sand grains but generally a uniform marine shale.|16-MAY-23
17451|Stuart Range Formation|Relationships and boundaries|Overlain conformably by the Mt Toondina Formation (Townsend & Ludbrook 1975) and conformably overlies the Boorthanna Formation (Townsend & Ludbrook 1975). Sharp boundaries at base and top on gamma ray and neutron logs.|16-MAY-23
17451|Stuart Range Formation|Age reasons|Sakmarian to Artinskian Balme (1957) Ludbrook (1967).|16-MAY-23
17451|Stuart Range Formation|Defn author|Townsend I.J., Ludrook N.H., 1975|16-MAY-23
17451|Stuart Range Formation|Proposed publication|Quarterly geological notes Geological Survey SA, 53|16-MAY-23
17451|Stuart Range Formation|References|01/31616; ?79/04361; 01/31594..|16-MAY-23
17451|Stuart Range Formation|Status|1|16-MAY-23
79386|Sugarloaf Dam Sandstone|Name source|The name is derived from Sugarloaf Dam, which is located about 7 km east of Cariewerloo Woolshed in the Port Augusta area at GDA94, zone 53, 741180 mE, 6409777 mN (LAT -32.423035° LONG 137.564857°).|16-MAY-23
79386|Sugarloaf Dam Sandstone|Unit history|Originally described and defined in McAvaney et al. (2016): Geology of the Six Mile Hill 1:75 000 Map Sheet, Mineral Systems Drilling Program Special Map Series. Report Book 2016/00014. Department of State Development South Australia (description pp. 137-141; brief definition Appendix 4, p. 229).  Used for the first time as a stratigraphic unit on Krapf et al. (2016): Surface geology of Six Mile Hill - Mineral Systems Drilling Program Special Map Series, 1:75 000 scale. DIGIMAP00088. Department of State Development South Australia.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Geomorphic expression|Due to the friable character of the Sugarloaf Dam Sandstone it is mainly exposed at small hills below low-lying silcrete surfaces or along the side walls of incised creeks.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Type section locality|The type locality of the Sugarloaf Dam Sandstone is a small hill located about 450 m northeast of Sugarloaf Dam at GDA94, zone 53, 741540 mE, 6410005 mN (LAT -32.420902° LONG 137.568624°).  A reference locality is at GDA94, zone 53, 734334.2 mE, 6412125.6 mN (LAT -32.4033284° LONG 137.4915326°), representing the hilly terrain between Sugarloaf Hill and South Tent Hill, from where a detrital zircon geochronology sample was collected.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Description at type locality|Outcrops of white, friable, kaolinitic sandstone.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Extent|Outcrops of the Sugarloaf Dam Sandstone are mainly located along the foothills of the mesas in the vicinity of Cariewerloo Woolshed and along creek exposures between drill site MSDP02 and Martin Catch Dam. It was deposited in an intermontane basin and is today distributed over an area with an extent of about 12 km in W-E direction and about 10 km in N-S direction.|16-MAY-23
79386|Sugarloaf Dam Sandstone|General description|The Sugarloaf Dam Sandstone locally contains rare, isolated, floating clasts of the Tregolana Shale Member or the Simmens Quartzite Member. The predominantly sandy facies of the Sugarloaf Dam Sandstone locally grades laterally into an earthy, clay-rich material, which when silcretised forms a porous porcellanitic rock composed of a mildly silcretised kaolinitic clay matrix with scattered quartz grains.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Thickness range|About 2-3 m in type area. Typical outcrop thicknesses range between one and two metres. Maximum preserved thickness is about 5 m.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Lithology|The Sugarloaf Dam Sandstone is at the type locality a white to cream coloured, friable, moderately sorted, fine- to medium-grained sandstone composed of angular quartz grains enclosed in a kaolinitic clay matrix. It is massive to vaguely planar bedded and silcretised at its top.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Depositional environment|The Sugarloaf Dam Sandstone was deposited in an intermontane basin or sheltered embayment mainly by sheet-like mass flows under high-energy conditions in an alluvial-fluvial environment.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Fossils|The sandstone contains evidence of plant bioturbation in form of scattered rhizoliths.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Relationships and boundaries|The Sugarloaf Dam Sandstone unconformably overlies weathered Neoproterozoic shales and sandstones of the Tregolana Shale Member (Tent Hill Formation, Wilpena Group). At the type locality it is overlain by Cenozoic landslide deposits composed of blocks of the Neoproterozoic Simmens Quartzite Member (Tent Hill Formation, Wilpena Group). At other localities, it is unconformably overlain by Quaternary fluvial conglomerates or gravels. The top parts of the Sugarloaf Dam Sandstone were affected by silcretisation processes associated with the formation of the Corraberra palaeosurface.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Identifying features|The Cenozoic Sugarloaf Dam Sandstone contains rhizoliths and root casts, which distinguishes it from the surrounding weathered Neoproterozoic sedimentary rocks.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Structure and Metamorphism|The Sugarloaf Dam Sandstone is unmetamorphosed and undeformed.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Age reasons|The Sugarloaf Dam Sandstone has a Cenozoic age based on rhizoliths and other forms of plant bioturbation. Deposition of the Sugarloaf Dam Sandstone occurred between the formation of two regional silicified palaeosurfaces, the higher and older Tent Hill Surface and the lower and younger Corraberra Surface. The Tent Hill Surface is tentatively correlated with the Cordillo Surface of Late Eocene to Early Oligocene age, whereas the Corraberra Surface probably formed in the mid to late Neogene. Consequently, an Oligocene to Miocene depositional age is inferred for the Sugarloaf Dam Sandstone based on its topographic position between these palaeosurfaces.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Correlations|The Sugarloaf Dam Sandstone was deposited in an intermontane basin, possibly at a time when the fluvio-lacustrine Miocene Neuroodla Formation was deposited in the adjacent Torrens Basin and the marine Miocene Melton Limestone in the nearby Pirie Basin.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Alteration and Mineralisation|The Sugarloaf Dam Sandstone is variably silcretised.|16-MAY-23
79386|Sugarloaf Dam Sandstone|Defn author|C. Krapf & M. Werner (GSSA) 12-DEC-2019.|16-MAY-23
79386|Sugarloaf Dam Sandstone|References|Krapf CBE, Werner M, Pawley MJ and McAvaney SO 2016. Surface geology of Six Mile Hill - Mineral Systems Drilling Program Special Map Series, 1:75 000 scale. DIGIMAP00088. Department of State Development South Australia, Adelaide.  **McAvaney SO, Werner M, Pawley MJ, Krapf CBE and Nicolson BE 2016. Geology of the Six Mile Hill 1:75 000 Map Sheet, Mineral Systems Drilling Program Special Map Series. Report Book 2016/00014. Department of State Development South Australia, Adelaide.   **Werner M, Krapf C and Reid A 2019. The Sugarloaf Dam Sandstone: a new Cenozoic sandstone unit in the northern Eyre Peninsula. MESA Journal, 91, pp. 4-25.|16-MAY-23
26161|Tandanya Sand Member|Name source|'Tandanya' is the aboriginal place name for the 'site of Adelaide south of the Torrens' (Black, 1920, p.84). This corresponds closely with the known distribution of the sand. The name has been approved by the Central Register of Stratigraphic Nomenclature, Canberra.|16-MAY-23
26161|Tandanya Sand Member|Type section locality|The type section is at a depth of 39.9-43.o m (131-141 feet) in foundation test bore 4. State Administration Building, eastern siute of Victoria Square, central City of Adelaide (Lindsay, 1964); Selby and Lindsay, 1973),Borehole Unit No. 662841 MEW00276, Town Acre 270, hundred Adelaide. Tube-core samples are stored in the Departmental Core Library at Glenside. |16-MAY-23
26161|Tandanya Sand Member|Extent|The Member is known only subsurface from more than 30 boreholes in the Adelaide City area south of the River Torrens, including the East, South, and West Parklands (Fig. 1). It has apparently been removed by erosion north of the Torrens. The sand was probably penetrated by a water bore in the Collegiate School of St Peter, Hackney, a little to the east of the city area and by boreholes in the Mile End Block west of the city. All localities are in the Adelaide Plains Sub-basin of the St Vincent Basin.|16-MAY-23
26161|Tandanya Sand Member|Thickness range|The thickness varies between 1.3 and at least 5.3 m. The type section is 3.1 m.|16-MAY-23
26161|Tandanya Sand Member|Lithology|The unit is a quartz sand, which is glauconitic (ovoid pellets common), pyritic and carbonaceous. It varies from poorly-sorted, pebbly, muddy, to clean medium-coarse sand, to soft silty fine sand. The colour is generally dark to pale grey and brownish, but yellowish-grey where oxidised. Animal fossils include sparse and sporadic foraminifera (including a few planktonic forms), sponge spicules (mostly pyritised), fragments and minute internal casts of molluscs, occasional bryozoal and echinoid fragments. Plant fossils include spores, pollen and organic-walled micro-plankton. Pyritised tube-casts (?burrows) also occur.|16-MAY-23
26161|Tandanya Sand Member|Relationships and boundaries|The sand grades upwards into laminated fine sand and soft mudstone, overlain by mudstone and silt. This interval, 5.5 to 7.5 m thick, between the Tandanya Sand Member and the basal Aldinga Member of Port Willunga Formation, is identified as undifferentiated Chinaman Gully Formation. The Tandanya Sand is stratigraphically distinct from the basal sand of the Aldinga Member. Beneath the Tandanya Sand, the chert-banded Gull Rock Member of Blanche Point Formation is separated from the sand either by a sharp disconformity, or by a metre or so of laminated clayey silt (predominant) and very fine sand, also regarded as undifferentiated Chinaman Gully Formation. Upper Blanche Point Formation ('Soft Marls') appears to be not present in the City area. The upper and lower boundaries of the Tandanya Sand Member are defined by the predominance of sand-sized grains over other constituents.|16-MAY-23
26161|Tandanya Sand Member|Identifying features|This Note names and describes the sand which occurs beneath the City of Adelaide, in the St Vincent Basin, near the base of beds correlated lithologically and palynologically with Chinaman Gully Formation (Reynolds, 1953; Cooper, 1977). The sand unit was distinguished  (JML) as a marker bed in 'equivalents of Blanche Point Soft Marl' or upper Blanche Point Formation, in geological cross-sections through the City area (in Selby and Lindsay, 1975, 1978).|16-MAY-23
26161|Tandanya Sand Member|Structure and Metamorphism|Structural contours of the top of the Tandanya Sand Member have been constructed from intersections in 34 boreholes (Fig. 1). The contours show that, like the other mid-Tertiary formations, the surface dips evenly at little more than 1o towards the south to southeast.|16-MAY-23
26161|Tandanya Sand Member|Correlations|The member is stratigraphically below the Aldinga Member of Port Willunga Formation and above the lower units of Blanche Point Formation. Since all these are well dated Late Eocene, the Tandanya Sand Member is also Late Eocene, probably Zone P. 16. Lithological units interposed between Gull Rock member and Aldinga Member in the Adelaide Plains Sub-basin (Lindsay, 1968; 1969, p.34) were identified broadly as ' Blanche Point Soft Marls Member' of Reynolds (1953) and included 'in its upper part...time-equivalents of Chinaman's Gully Beds'. Recent evidence from dinoflagellate assemblages (WKH) indicates a more precise correlation of at least part of this interval with Chinaman Gully Formation, now recognised as a very widespread unit in the St Vincent Basin, thickening northwards. Beyond Adelaide, the basal unit of the Chinaman Gully Formation (correlative of the Tandanya Sand Member in the Adelaide City area) is strongly progradational, very marginal-marine, and may be a lignite. In terms of palynological zones, the unit lies within the spore/pollen zone of Sparganiaceaepollenites barungensis. Similar assemblages have been recorded from the Chinaman Gully Formation in the Willunga Embayment.|16-MAY-23
26161|Tandanya Sand Member|Proposed publication|Quarterly Geological Notes, Geological Survey SA, 70:2-4).|16-MAY-23
26161|Tandanya Sand Member|Comments|Groundwater:  Where the sand is not too muddy, it comprises Aquifer 3, with pressure water, in the Adelaide City area (Selby and Lindsay, 1978).|16-MAY-23
26161|Tandanya Sand Member|References|79/00926; 01/31617; 79/05157; 79/03867|16-MAY-23
17992|Terrapinna Granite|Type section locality|Hamilton Creek, 0.3 miles south of Terrapinna Waterhole [probably Terrapinna Springs], lat. 29degrees 54'55" S long. 139degrees 40'08"E. [location mistakenly given as 25 degress 54'55" S]|16-MAY-23
17992|Terrapinna Granite|Defn author|R.P.Coats, SA Dept Mines, 1971.|16-MAY-23
24519|Third Plain Creek Member|Name source|After Third Plain Creek The Bunkers 1:50 000 topographic map, GR 974403|16-MAY-23
24519|Third Plain Creek Member|Type section locality|234 metres of interbedded limestone and calcareous siltstone, exposed in the east-west creek in the Bunkers Range The Bunders 1:50 000 topographic map GR 997391-999390. This is close to Dalgarno's (1964) reference section of the Hawker Group.|16-MAY-23
24519|Third Plain Creek Member|Extent|Confined to the Bunkers Graben (Dalgarno 1983).|16-MAY-23
24519|Third Plain Creek Member|Thickness range|0-376 m|16-MAY-23
24519|Third Plain Creek Member|Lithology|Interbedded black turbiditic wackestone-packstone and calcaraeous siltstone, with each couplet 7-20 cm thick. Graded and parallel-laminated beds, and fill-structures, slump-folds, sedimentary boudinage disrupted laminae, intraclast floatstone beds are common. Rare dislodged blocks also occur.|16-MAY-23
24519|Third Plain Creek Member|Relationships and boundaries|Conformably overlies Linns Springs Member of the Parara Limestone Base often marked by series of slump rolls. Differentiated from Linns Springs member by more frequent intraclast floatstones and rudstones, and more extensive slump features. Unit coarsens upwards and may contain quartz sand stringers at top. Disconformably overlain by the Bunkers Sandstone. Unit wedges out to the northwest and is not known to occur outside the graben. To the southeast the unit interfingers with a tongue of platform-derived oolitic-pelloidal-intraclastic limestone, mapped as Wilkawillina Limestone.|16-MAY-23
24519|Third Plain Creek Member|Age reasons|The member is sparsely fossiliferous, with brachiopods, fragmentary archaeocyaths and trilobites. The presence of Pararia sp (Kobayashi) (P. Jell, pers. comm.) places it in Daily's (1956) Faunal Assemblages 4 and 5. This suggests a middle Early Cambrian age (?Botomian).|16-MAY-23
24519|Third Plain Creek Member|Defn author|Clarke J.D.A. 1986 86/25584. Briefly described p5.|16-MAY-23
24519|Third Plain Creek Member|Proposed publication|Quarterly Notes Geological Survey SA|16-MAY-23
24519|Third Plain Creek Member|Resdate|25-OCT-1985|16-MAY-23
24520|Thora Dolomite|Name source|Thora Soakage, 2 km northeast of Peake H.S. in the Peake and Denison Ranges; Warrina 1:100 000 sheet area, Warrina 1:250 000 Sheet area; metric reference 6877620, 589800.|16-MAY-23
24520|Thora Dolomite|Type section locality|30-40 metres of sediments on the southern limb of the Creek Syncline 5 km northeast of Box Creek R.S., metric reference 6820525, 601350; section occurs where a tributary of Wilyalallina Ccreek cuts through the units.|16-MAY-23
24520|Thora Dolomite|Extent|Sole outcrop is on the southern limb of a syncline (Box Creek Syncline) 5 km northeast of Box Creek R.S. on the Central Australia Railway; Boorthanna 1:100 000 sheet area, Warrina 1:250 000 sheet area.|16-MAY-23
24520|Thora Dolomite|Thickness range|Range  30-40 m|16-MAY-23
24520|Thora Dolomite|Lithology|Grey-green and brown dolomite, minor siltstone; weathers a light brown buff colour; large festoon surfaces and algal bedding.|16-MAY-23
24520|Thora Dolomite|Relationships and boundaries|Conformably overlies the Tapley Hill Formation (Coats, 1971). Conformably underlies an unnamed siltstone of the Willochra Subgroup (Ambrose and Flint, in prep.).|16-MAY-23
24520|Thora Dolomite|Age reasons|Adelaidean-Umberatana Group (Sturtian).|16-MAY-23
24520|Thora Dolomite|Proposed publication|Rep. Invest., Geological Survey SA|16-MAY-23
24520|Thora Dolomite|Proposer|Ambrose G., Coats R.P.|16-MAY-23
24520|Thora Dolomite|Resdate|29-NOV-1979|16-MAY-23
24522|Tidnamurkuna Volcanics|Name source|Tidnamurkuna is an Aboriginal name for a waterhole on the Peake Creek just west of the Peake and Denison Ranges, 9.5 km northwest of the ruins of the Peake overland telegraph station. Warrina 1:100 000 sheet area, Warrina 1:250 000 sheet area, metric reference 6898050, 580000.|16-MAY-23
24522|Tidnamurkuna Volcanics|Type section locality|500 metres of amygdaloidal basalts and porphyritic rhyolites exposed in the creek banks from 6888940, 590850 (bottom) to 6888300, 590750 (top of section). The base is not exposed and the top is identified by a cream-weathering porphyritic rhyolite.|16-MAY-23
24522|Tidnamurkuna Volcanics|Extent|The unit outcrops along a strike length of 10 km to the west of "Peake" ruins and 3 km north of Mount Denison on the Warrina 1:250 000 sheet araea.|16-MAY-23
24522|Tidnamurkuna Volcanics|Thickness range|Minimum thickness of 600 m.|16-MAY-23
24522|Tidnamurkuna Volcanics|Lithology|Flow-banded porphyritic rhyolites, amygdaloidal basalts, minor epidosites and phyllites.|16-MAY-23
24522|Tidnamurkuna Volcanics|Age reasons|?Early Proterozoic: the intrusive Wirriecurrie Granite has been radiometrically dated at 1648+/-21 Ma providing a minumum age.|16-MAY-23
24522|Tidnamurkuna Volcanics|Proposed publication|Bull. Geological Survey SA, 50.|16-MAY-23
24522|Tidnamurkuna Volcanics|Defn approved by|Definition published prior to receipt by SNC and as such cannot be modified - thus no approval.|16-MAY-23
24522|Tidnamurkuna Volcanics|Defn Reference|81/21524|16-MAY-23
24522|Tidnamurkuna Volcanics|Proposer|Flint R.B.|16-MAY-23
18357|Toolachee Formation|Type section locality|Toolachee 1 (Lat 28 deg25'58", Long 140deg 46' 54". Here redefined as the interval 5878 - 6223 ft (1792 - 1897 m), to exclude the Daralingie Formation not previously recognised in this well|16-MAY-23
18357|Toolachee Formation|Defn author|Morton, J.G.G., Gatehouse, C.G., 1985.|16-MAY-23
18357|Toolachee Formation|Proposed publication|Quarterly Geological Notes S.A., 94, pp8-15 (1985)|16-MAY-23
18473|Tortachilla Limestone|Name source|From Tortachilla Trig. Point, an elevated point along the coast immediately north of Blanche Point.|16-MAY-23
18473|Tortachilla Limestone|Type section locality|Coastal cliffs at the south end of Maslin Bay from immediately south of Tortachilla Trig. to Blanche Point, Gulf St Vincent.|16-MAY-23
18473|Tortachilla Limestone|Thickness range|0-6 m range|16-MAY-23
18473|Tortachilla Limestone|Lithology|Biodastic limestone with abundant glauconite and polished goethite pellets.|16-MAY-23
18473|Tortachilla Limestone|Relationships and boundaries|Overlies South Maslin Sands (Maslin Sands), unconformably overlain by Blanche Point Formation. Probably passes laterally into Maslin Sands.|16-MAY-23
18473|Tortachilla Limestone|Age reasons|Late Eocene|16-MAY-23
18473|Tortachilla Limestone|Proposed publication|Rep. Inv. Geological Survey SA, 50.|16-MAY-23
18473|Tortachilla Limestone|Defn Reference|79/20399 Redefined 83/23493|16-MAY-23
18532|Trainor Hill Sandstone|Name source|From Trainor Hill, Everard 1:250 000 map sheet, grid reference 6581 6036.|16-MAY-23
18532|Trainor Hill Sandstone|Unit history|Krieg's (1973) definition included the underlying sandstones of the Arceoillinna Sandstone (new name) and the Mount Johns Conglomerate (redefined).|16-MAY-23
18532|Trainor Hill Sandstone|Type section locality|Located on the SE margin of the Mount Johns Range, to the foot of Mount Byilkoora. Grid reference section 16 a 35249835-53209831; 16 b 35289824-35119823.|16-MAY-23
18532|Trainor Hill Sandstone|Extent|The north, east and southern part of the Mount Johns Range. White kaolinitic sandstone in the Officer Basin of South Australia, is correlated with this formation.|16-MAY-23
18532|Trainor Hill Sandstone|Thickness range|The type section is 370 m thick, and thins northwards to 0 m.|16-MAY-23
18532|Trainor Hill Sandstone|Lithology|A sequence of cross-bedded well sorted, medium to very fine sandstone with minor interbedded red siltstone and claystone and with minor pebbly horizons near the base. The sandstone becomes light red, feldspathic and calcareous near the top, with minor sandy dolomite.|16-MAY-23
18532|Trainor Hill Sandstone|Relationships and boundaries|Sharply overlies the Apamurra member of the Mount Johns Conglomerate in the south. In the north the boundary with the Mount Johns Conglomerate is a transitional one. The top is a sharp and unconformable one with the Byilkaoora Formation of the Munda Sequence.|16-MAY-23
18532|Trainor Hill Sandstone|Age reasons|No direct age. A Middle to Late Cambrian age is suggested as it occurs between the Early-?Middle Cambrian Observatory Hill Beds and the ?Early Ordovician Mount Chandler Sandstone.|16-MAY-23
18532|Trainor Hill Sandstone|Defn author|Benbow, 1982.|16-MAY-23
18532|Trainor Hill Sandstone|Proposed publication|Trans. Roy. Soc. S. Aust.|16-MAY-23
28298|Uley Formation|Name source|Uley' homestead; grid reference 508529, Lincoln 1:100 000 sheet 6028.|16-MAY-23
28298|Uley Formation|Unit history|No specific name has been used but earlier writers referred to this unit as "late Tertiary sediments" (Harris, 1966).|16-MAY-23
28298|Uley Formation|Type section locality|Between 14 and 38 m in Department of Mines and Energy observation well VB12, situated 14 km north of 'Uley' homestead in Sec. FA, Hd. Lake Wangary. Samples are stored in the Departmental Core Library at Glenside, SA.|16-MAY-23
28298|Uley Formation|Extent|The unit is intersected in sub-surface in several basins in southern Eyre Peninsula-Cummins Basin (Cummins School Drainage Well), Lincoln Basin (Observation Wells FLN42, 46), Uley South Basin (Observation Wells ULE 127, 139) and Coffin Bay Basin (Observation Wells VB12 and LKW31) plus ;many other wells.|16-MAY-23
28298|Uley Formation|Thickness range|About 40 m maximum known thickness.|16-MAY-23
28298|Uley Formation|Lithology|Sandy clays orange-brown quartz sands generally well sorted and rounded, with occasional ironstone nodules (lateritic gravel) and rounded gravel beds.|16-MAY-23
28298|Uley Formation|Relationships and boundaries|Disconformably overlies the Wanilla Formation (Harris, 1966) which consists of carbonaceous quartz sands, generally poorly sorted and subangular. Top of unit defined by an orange-brown mottled sandy clay. Disconformably overlain by the Bridgewater Formation (Boutakoff, 1963).|16-MAY-23
28298|Uley Formation|Age reasons|There are no fossils evident in these sediments but stratigraphic relationships suggest a late Tertiary age.|16-MAY-23
28298|Uley Formation|Defn author|Burnett S., 1978|16-MAY-23
28298|Uley Formation|Proposed publication|Quarterly Geological lNotes Geological Survey SA, No. 67|16-MAY-23
24560|Waraco Limestone|Name source|From Waraco Creek at the northern margin of the Worumba Anticline core complex.  Map Symbols: Pcq1, Pcq2, Pcq3.|16-MAY-23
24560|Waraco Limestone|Unit history|The dark limestone and pale dolomite members were referred to informally as Units F and G by Preiss (1978).|16-MAY-23
24560|Waraco Limestone|Type section locality|For reasons of outcrop constraints, two separate structurally uncomplicataed sections are chosen to represent the Waraco Limestone. The more northerly is along the bed of the major unnamed stream north of Morgan Creek, commencing at 275900-6461630 and finishing at 275680-6461690.  This section does not include the top of the dolomitic member and the overlying siltstone member. The southern section is nominated 1.5 km along strike to the south, commencing at 276120-6460280 and finishing at 275840-6460270, to represent the remainder.|16-MAY-23
24560|Waraco Limestone|Extent|Not yet recognised with certainty outside the Worumba Anticline, where it forms an easily mappable ;marker for a strike length of about 7 km.|16-MAY-23
24560|Waraco Limestone|Thickness range|277 m thick in the type section.|16-MAY-23
24560|Waraco Limestone|Lithology|Lithological Sequence in Southern Section: Top: Plq3, (siltstone member). 41 m siltstone, dark grey, very thinly laminated, platy, with possible synaeresis cracks.n 36m siltstone, green-grey, coarse grained, flaggy to blocky, poorly laminated, with ferruginous weathering rings. Pcq2 (dolomitic member).  25 m dolomite, pale buff-grey, blocky, with irregular quartzitic nodules, authigenic quartz blebs predating compaction and lithification, and some calcitic laminations. 20 m limestone, pale grey, weathering brown, blocky, coarsely crystalline, with intraclast bands (possibly disrupted algal mats); stylolites.  Base 30 m dolomite marble, pale cream, poorly bedded, coarsely crystalline, quartz blebs.  Continuation of Lithological Sequence in Northern Section: Top: Pcq2 (dolomitic member). 16 m limestone, dolomitic, white to pale pink, weathering brown, well laminated, in part with cumulate stromatolites and tepee structures.  8 m dolomite, pale brownish grey, very finely crystalline, with cumulate and reclined columnar stromatolites.  11 m dolomite, cream, recrystallised, flaggy, and fine-grained marble.  Pcq1 (limestone member).  32 m limestone, medium grey to blue-grey cryptalgal laminated, siliceous nodules, slight irregularities in the lamination, and very thin band of black chert.  11 m limestone, blue-grey, massive, part laminated, disrupted tepee structures and bands with large rounded intraclasts.  10 m limestone, blue-grey, massive to blocky, finely crystalline; stromatolitic, columns broken, slumped and commonly inverted; some dolomitic laminations.  13 m limestone, blue-grey, massive to blocky, finely crystalline, partly thinly banded, partly with mottled or poddy fabric and wavy lamination, cryptalgal lamination and possibly cumulate stromatolites; black chert concretions.  11 m limestone, blue-grey, massive, stromatolitic, with columns leaning to the north; irregular masses of speckled black and white chert. Fine-grained cryptalgal laminated dolomite at the base.  Base: 11 m limestone, dolomitic, flaggy, medium grey, weathering brown.|16-MAY-23
24560|Waraco Limestone|Relationships and boundaries|Conformably overlies Kirwan Siltstone. In one small area, it appears to be conformably overlain by the Worumba Dolomite Beds, but elsewhere upper boundary is faulted, or intrusive contact with carbonate breccia.|16-MAY-23
24560|Waraco Limestone|Identifying features|A distinctive marker consisting of three mappable members: a lower dark grey limestone, middle pale dolomite, and upper siltstone.|16-MAY-23
24560|Waraco Limestone|Age reasons|Age inferred to be Willouran.|16-MAY-23
24560|Waraco Limestone|Correlations|No correlatives of the Waraco Limestone yet described from outside the Worumba Anticline, but may occur in the Arkaba Diapir (T.J. Mount, 1980, pers. comm.).|16-MAY-23
24560|Waraco Limestone|Proposer|Preiss W.V.|16-MAY-23
24560|Waraco Limestone|Resdate|04-SEP-1979|16-MAY-23
27953|Warcowie Dolomite Member|Name source|After 'Warcowie' H.S., situated 25 km northeast of Hawker.  Map Symbol: Puw.|16-MAY-23
27953|Warcowie Dolomite Member|Type section locality|Although easily accessible and well-exposed sections of the Warcowie Dolomite Member are common, its base is mostly a tectonic contact with carbonate breccia. Only on the east limb of the Worumba Anticline is a sedimentary base (disconformaity to unconformity) preserved, and a less accessible type section is therefore chosen in this area, on a western spur of Mount Plantagenet, commencing at 279470-6470800 and finishing at 279630-6470750. Other good sections may be examined along Maraby Creek, Waraco Creek, and along the road 1.5 km west of 'Worumba' H.S.|16-MAY-23
27953|Warcowie Dolomite Member|Extent|The Member occurs at base of Wilyerpa Formation on both limbs of the Worumba Anticline, except where it laps out. Forbes (1970) recorded similar yellow-brown pebbly dolomite at the base of the Wilyerpa Formation in the Benda Range, Olary region.|16-MAY-23
27953|Warcowie Dolomite Member|Thickness range|In type section, 80 m, but elsewhere thinner (10-20 m). The Member laps out against a syndepositional high (a small block of Wirreanda Dolomite Beds) 3 km SSW of 'Worumba'.|16-MAY-23
27953|Warcowie Dolomite Member|Lithology|Lithological Sequence in Type Section: Top: 35 m conglomerate, massive, partly matrix supported, with poorly outcropping silty and sandy matrix. Clasts mostly well rounded, pebble to boulder size, including granites, pale grey and red quartzites. Elsewhere include also schist, gneiss, dolomite, chert, and altered dolerite. 20 m dolomite, pale grey to buff, pale brown weathering, massive, poorly bedded. Elsewhere contains scattered pebbles.  20 m dolomite, buff, brown weathering, sandy and gritty, well bedded. Base 5 m breccia, with dolomitic matrix, including angular fragments of micaceous siltstone and sandstone, derived from nearby unconformably underlying disrupted Niggle Gp Beds.|16-MAY-23
27953|Warcowie Dolomite Member|Relationships and boundaries|Overlies Holowilena Ironstone with low-angle unconformity in the type section, and overlaps eastwards on to disrupted Niggly Gap Beds. Elsewhere, base of the Member commonly tectonic contact with carbonate breccias, in part intrusive into the Member and overlying Sturtian formations. Upper boundary is a well defined by conformable contact with olive green siltstones and sandstones (upper part of the Wilyerpa Formation). |16-MAY-23
27953|Warcowie Dolomite Member|Identifying features|Distinctive basal dolomitic and conglomeratic sequence of the Wilyerpa Formation, Umberatana Group.|16-MAY-23
27953|Warcowie Dolomite Member|Structure and Metamorphism|The Member, together with remainder of Umberatana Group, outlines the structure of the Worumba Anticline, with a gently dipping east limb and steeply dipping to overturned west limb. Wilyerpa Formation is cut by  north west-trending cross faults, many of which were active during deposition.|16-MAY-23
27953|Warcowie Dolomite Member|Age reasons|The age is mid-Sturtian.|16-MAY-23
27953|Warcowie Dolomite Member|Correlations|The Wilyerpa Formation) is a basinal clastic variant of the Apila Tillite of the Mid North region, and probably also correlates with the Sturt Tillite (Adelaide region).|16-MAY-23
27953|Warcowie Dolomite Member|Defn author|Preiss W.V.  Fully described P.43 86/25202.|16-MAY-23
27953|Warcowie Dolomite Member|Proposed publication|Quarterly Geological Notes, Geological Survey SA, 76: 12-23.|16-MAY-23
27953|Warcowie Dolomite Member|Proposer|Preiss W.V.|16-MAY-23
29118|Warragee Member|Name source|Warragee Bore'; Latitude 31o00'57"S, Longitude 138o47'29"E.|16-MAY-23
29118|Warragee Member|Type section locality|350 metres of red and green shale, with minor calcareous and tuffaceous intervals, exposed over an area of undulatory topography 2.5 km north of Ten Mile Creek, from Latitude 31015'50"S, Longitude 138o49'24"E (bottom) to Latitude 31o15'47"S, Longitude 138o49'43"E (top).|16-MAY-23
29118|Warragee Member|Extent|The unit is exposed over approximately 35 km2 in the central Flinders Ranges (along the Heysen Range, at Mernmerna, between Wirrealpa and the Ten Mile Creek, near Mount Frome and adjacent to Chambers Gorge), on the Parachilna 1:250 000 Geological Sheet (SH54-13). It also outcrops over approximately 10 km2 in the Mount Scott Range, on the western portion of the Copley 1:250 000 Geological Sheet (SH54-9).|16-MAY-23
29118|Warragee Member|Thickness range|Range 0-360 m|16-MAY-23
29118|Warragee Member|Lithology|Red, green and grey shales and fine to medium siltstones. Minor interbeds of dolomite, dolomitic limestone, tuff and coarse siltstone. Generally evenly laminated. Minor ripple lamination.|16-MAY-23
29118|Warragee Member|Relationships and boundaries|Basal member of the Billy Creek Formation in central Flinders Ranges and at Mount Scott. Conformably overlies the Oraparinna Shale (Daily, 1956) where the latter unit is present. Rests conformably on the Wilkawillina Limestone east of the Wirrealpa Diapir. Rests sharply and probably disconformably on the Wilkawillina Limestone south of the Ten Mile Creek graben and near Mount Frome. Rests conformably on the Ajax Limestone in the Mount Scott Range (Moore, in press) and rests conformably on the Moorowie Formation south of the Chambers Gorge (Mount, 1970). Base of the unit is defined by red and minor green shales. Conformably overlain by the Nildottie Siltstone Member of the Billy Creek Formation.|16-MAY-23
29118|Warragee Member|Age reasons|The Warragee Member is underlain by the Oraparinna Shale and its equivalents, which are of middle Lower Cambrian age (Walter, 1967). It is overlain by up to 550 metres of unfossiliferous red-beds of the Billy Creek Formation, which are in turn overlain by the early Middle Cambrian Wirrealpa Limestone (Daily, 1956). The Warragee Member is therefore probably entirely late Lower Cambrian in age.|16-MAY-23
29118|Warragee Member|Proposed publication|Transactions of the Royal Society of South Australia|16-MAY-23
29118|Warragee Member|References|79/20092; 01/31619|16-MAY-23
24564|Warrina Supergroup|Name source|Warrina 1:250 000 Map Sheet, itself named after the disused railway siding in the Peake and Denison Ranges, SA.|16-MAY-23
24564|Warrina Supergroup|Type section locality|Burra Group: Auburn and Clare region. Callanna Group: Arkaroola area (Arkaroola Subgroup) Willouran Ranges (Curdimurka Subgroup).|16-MAY-23
24564|Warrina Supergroup|Extent|Restricted to Adelaide Geosyncline, deposited in fault-controlled basins.|16-MAY-23
24564|Warrina Supergroup|Lithology|Mixed clastic and carbonate cyclical sequences, with basic volcanics and evaporites in the Callanna Group, and with dolomite and magnesite in the Burra Group.|16-MAY-23
24564|Warrina Supergroup|Relationships and boundaries|Callanna Group unconformably overlies crystalline basement, Burra Group either transgressive on to crystalline basement, or in conformable to disconformable contact over Callanna Group.|16-MAY-23
24564|Warrina Supergroup|Identifying features|The Warrina Supergroup combines the Callanna and Burra Groups of the Adelaide Geosyncline|16-MAY-23
24564|Warrina Supergroup|Age reasons|Early Adelaidean (late Proterozoic).|16-MAY-23
24564|Warrina Supergroup|Proposed publication|Trans. R. Soc. S. Aust. (Brief Communication).|16-MAY-23
24564|Warrina Supergroup|References|79/03449|16-MAY-23
24564|Warrina Supergroup|Proposer|Preiss W.V.|16-MAY-23
26205|Waurea Pyroclastics|Name source|From Waurea hill on Moonarie station, adjacent to Lake Everard station. Waurea hill is located at 31o52' latitude and 135o26' longitude, within mapped area. Origin: The lateral continuity and uniformity and petrographic features of this unit indicates that it is a poorly welded to unwelded ashflow deposit. The tuff breccias, containing blocks up to 1 m across cannot be far from the original vent.|16-MAY-23
26205|Waurea Pyroclastics|Type section locality|Due to the isolated nature of outcrops and variability of this unit it is not possible to propose a type section. However, typical Waurea Pyroclastics may be seen 1.2 km due east of Glyde Hill outstation, which is located at latitude 31o37' and longitude 135o09.5'.|16-MAY-23
26205|Waurea Pyroclastics|Extent|Occurs as isolated outcrops extending from the southwest of the Gairdner 1:250 000 Sheet area onto the southeast of the Childara 1:250 000 Sheet area. Total outcrop area would not exceed 7 km2.|16-MAY-23
26205|Waurea Pyroclastics|Lithology|Invariably a white to buff coloured lapilli-tuff to tuff breccia of ashflow origin. Usually poorly welded, it weathers to a white, shaky-looking rock. The lapilli and blocks are composed of a variety of volcanic rock types, the most common being a strongly flow banded rhyolite and a fine grained, dense, strongly welded ashflow tuff. There is a complete lack of sorting and bedding among the lapilli and block size fragments. In the lapilli-tuffs, the lapilli size pumice and lithic fragments sit in a matrix of ash size fragments and undeformed glass shards (devit.). In the tuff breccias, the blocks of volcanic rock fragments are within a completely unsorted matrix of lapilli and ash size fragments. The tuff breccias are far less common than the lapilli tuffs and are localised in only two areas.|16-MAY-23
26205|Waurea Pyroclastics|Relationships and boundaries|The Waurea Pyroclastics conformably overly the Baldry Rhyolite and conformably underly the Wheepool Rhyolite (defined by Blissett). Thickness is variable, ranging from 3 m to 20 m. The thickness is unlikely to exceed 40 m.|16-MAY-23
26205|Waurea Pyroclastics|Age reasons|This unit forms part of the Glyde Hill Complex as defined by Blissett. Age is roughly 1550 Ma.|16-MAY-23
26205|Waurea Pyroclastics|Defn author|Giles C.W., 1977|16-MAY-23
26205|Waurea Pyroclastics|Proposed publication|SA Department of Mines, Quarterly Notes No. 61|16-MAY-23
19865|Wheepool Rhyolite|Name source|Wheepool Wells, 20 km northeast of Lake Everard H.S.  Latitude 31o39'S; longitude 135o21'30"E. (Gairdner 1:250 000 sheet (SH53-15)).|16-MAY-23
19865|Wheepool Rhyolite|Type section locality|Near Wheepool wells; north of Lake Everard H.S.|16-MAY-23
19865|Wheepool Rhyolite|Thickness range|About 300 m|16-MAY-23
19865|Wheepool Rhyolite|Lithology|Blocky-weathering reddish brown porphyritic rhyolite with phenocrysts of pink feldspar up to about 5 mm long, and rounded clear quartz. Weathers yellowish brown. For about 13 km east from Glyde Hill outstation, the rhyolite is underlain by a bed of coarse rhyolitic agglomerate and tuff about 5 m thick. containing blocks of rhyolite up to at least 30 cm long, and dipping northwards at 10-15o.|16-MAY-23
19865|Wheepool Rhyolite|Relationships and boundaries|Overlain by porphyritic dacite (unit Pag3) north of Wheepool Wells and at Dingo Hill. Cut by dacite dykes 1.5 km south-southeast of Wheepool Wells. Near Glyde Hill outstation, the rhyolite either passes westwards into or is overlain by the rhyodacite unit Pag2.|16-MAY-23
19865|Wheepool Rhyolite|Apprdate|March or April|16-MAY-23
19865|Wheepool Rhyolite|Defn approved by|South Australia Sub-Committee|16-MAY-23
24632|White Well Granite|Name source|Adapted from White Well Bore, 3 km south of Prospect Hill trig and 15 km northwest of Mount Babbage at the northern end of the Flinders Ranges, Moolawatana 1:100 000 and Callabonna 1:250 000 map sheets. This name was first used informally by Teale et al. (1989).|16-MAY-23
24632|White Well Granite|Type section locality|North of White Well Bore between the old Dog Proof Fence and the new electric Dog Proof Fence, with exposures of two medium-sized and one small stock occurring on a south-facing ridge flank.|16-MAY-23
24632|White Well Granite|Extent|Limited to an outcrop area of 2.2 x 1.3 km south of Prospect Hill and north of White Well bore.|16-MAY-23
24632|White Well Granite|Lithology|The dominant rock type consists of deformed, medium-grained biotite granite. Composition is essentially microcline, quartz, plagioclase, biotite and secondary muscovite. Accessory minerals include zircon, monazite and apatite. The rock has aligned K-feldspar and plagioclase prismatic phenocrysts and bluish to translucent grey quartz, and decussate biotite aggregates. The granitoid stocks are compositionally zoned; adamellite cores contain mostly grey quartz whereas the outer granitic zones contain bluish quartz. Xenoliths occur within the granite contact margins. Post-emplacement deformation has imposed a mica foliation, similar to that of the surrounding Petermorra Volcanics (i.e. trend of ~85o-95o magnetic and subvertical).|16-MAY-23
24632|White Well Granite|Relationships and boundaries|Three ovoid stocks of this granitoid intrude Petermorra Volcanics. Dimensions of these stocks are 400 x 1200 m. Most contacts with the host Petermorra Volcanics are intrusive, the granite also forming apophyses and dykes. Faulted contacts also occur, mostly on the southwest margins of each stock. The southern most stock is in fault contact with the Terrapinna Granite.|16-MAY-23
24632|White Well Granite|Age reasons|High-level plutons of the Prospect Hill Granite and White Well Granite intrude the sequence. Neither has been dated, but are assumed to be of similar age to other, deeper-level granitoids in the region that have statistically identical U-Pb zircon ages of 1556+/-4, 1556+/-10 and 1557+/-6 Ma.|16-MAY-23
24632|White Well Granite|Proposed publication|South Australia Geological Survey. Quarterly Geological Notes, 123:18-31.|16-MAY-23
24632|White Well Granite|Category|2|16-MAY-23
24632|White Well Granite|Proposer|Sheard M.J., Fanning C.M., Flint R.B.|16-MAY-23
24632|White Well Granite|Resdate|24-OCT-1991|16-MAY-23
24632|White Well Granite|Reserved? Yes/No|Yes|16-MAY-23
19949|Whyeela Dacite|Name source|From Whyeela dam on Lake Everard station. Whyeela dam is near extensive outcrops of Whyeela Dacite and is located at 31o38' latitude and 135o14.5' longitude. Origin:  A strongly welded crystal-vitric ashflow tuff. Devitrification has obscured primary texture. The more basic variants probably represent different ashflows within the composite sheet.|16-MAY-23
19949|Whyeela Dacite|Type section locality|Top of unit is not seen, however a good basal section may be seen adjacent to the Lake Everard station - Kokatha station track at 31o41' latitude and 135o15.25' longitude.|16-MAY-23
19949|Whyeela Dacite|Extent|Forming a semi-circular outcrop, covering an area of roughly 12 km2 in the central west of the Gairdner 1:250 000 Sheet area.|16-MAY-23
19949|Whyeela Dacite|Thickness range|At least 100 m.|16-MAY-23
19949|Whyeela Dacite|Lithology|A red-brown porphyry containing medium grained phenocrysts of alkali feldspar, plagioclase sitting in an aphanitic groundmass. Dark green, more basic variants occur, these containing visible phenocrysts of clinopyroxene, sometimes altered to chlorite. In thin section, medium grained euhedral phenocrysts of alkali feldspar, plagioclase and fine grained phenocrysts of clinopyroxene (augite) are scattered through a devitrified, microlitic textured groundmass. Fine grained phenocrysts of plagioclase are present, commonly occurring as glomoroporphyritic aggregates. Odd fine grained, euhedral phenocrysts of orthopyroxene (hypersthene) are scattered throughout but are far less common than augite phenocrysts. Limonite stains the groundmass red giving the rock its characteristic red-brown colour. In the rocks containing a higher percentage of pyroxene, chlorite and magnetite are scattered throughout the groundmass, giving the rock a dark green colouration. Minute fractured, crustal chips are common. Phenocrysts make up roughly 15% of the rock, with plagioclase, alkali feldspar and augite predominating.|16-MAY-23
19949|Whyeela Dacite|Relationships and boundaries|Overlies the Yantea Rhyodacite and is separated from this unit in places by a thin (>2 m thick) ashflow tuff. Top of this unit is not seen as it is the youngest volcanic unit exposed in the Glyde Hill Complex (Blissett).  |16-MAY-23
19949|Whyeela Dacite|Age reasons|Forms part of the Glyde Hill Complex as defined by Blissett. Age mid-Carpentarian, roughly 1550 Ma. Is the youngest volcanic unit in the Glyde Hill Complex.|16-MAY-23
19949|Whyeela Dacite|Proposed publication|SA Department of Mines, Quarterly Notes No. 61|16-MAY-23
19949|Whyeela Dacite|Defn Reference|Giles C.W., 1977|16-MAY-23
19958|Wiabuna Formation|Name source|Wiabuna Railway Station 50 km east of Penong on the Port Lincoln, Minnipa, Thevenard, Penong Line, (now abandoned).|16-MAY-23
19958|Wiabuna Formation|Type section locality|On the Eyre Highway 19 km east of Penong, and at other road cuttings through dune crests between Penong and Koonibba where the unit overlies Upper Member Bridgewater Formation. Good exposures in interdunal areas occur 5 km west of Woolshed Flat.|16-MAY-23
19958|Wiabuna Formation|Extent|Western Eyre Peninsula including the Quondong Plains.|16-MAY-23
19958|Wiabuna Formation|Thickness range|Up to 2 m. The unit is thin on dune crests and thick in the interdune swales.|16-MAY-23
19958|Wiabuna Formation|Lithology|Pale brown quartz or shell sand with carbonate silt. Upper part contains carbonates of the Loveday Soil in most places. Sand-size material is usually derived from adjacent source material. Mainly aeolian, but the dune form is derived in part from earlier forms as old as Lower Member Bridgewater Formation.|16-MAY-23
19958|Wiabuna Formation|Relationships and boundaries|Overlain by Recent aeolian sands, including Semaphore Sand on the coastal margin and Moornaba Sand inland. Thin sandy overlays not differentiated. Overlies Bridgewater Formation - as defined in Firman, 1967 and 1969 - and re-worked ?aeolian - colluvial material possibly occupying the same position in sequence as the Pooraka Formation (see Firman, 1966a for description). Stratigraphically equivalent to Woorinen Formation of the Murray Basin (Firman, 1972 and 1973).|16-MAY-23
19958|Wiabuna Formation|Age reasons|Upper Pleistocene.|16-MAY-23
19958|Wiabuna Formation|Defn author|Firman J.B., 1974|16-MAY-23
19958|Wiabuna Formation|Proposed publication|Quarterly Geological Notes of the Geological Survey of South Australia, No. 52.|16-MAY-23
19958|Wiabuna Formation|Defn approved by|Gatehouse C.G.   Approved by Sub-Committee - see 72/371 letter of 4/12/74 from Strat. Index|16-MAY-23
24574|Willawalpa Formation|Name source|Willawalpa Creek, 10 km ENE of Kingston Dam, near Mt Nor'West outstation. Map symbol Po1.|16-MAY-23
24574|Willawalpa Formation|Type section locality|Near Wattle Creek, upsteam from Upper Wattle Well, from latitude 29o55', longitude 137o58' to latitude 29o55', longitude 137o59'.|16-MAY-23
24574|Willawalpa Formation|Extent|Willouran Range. Probably also SW of Cadnia Hill, about 34 km W. of 'Callanna'.|16-MAY-23
24574|Willawalpa Formation|Thickness range|2 242 in type section.|16-MAY-23
24574|Willawalpa Formation|Lithology|Lithological sequence in the type section. Top: 96 m sandy siltstone and sandstone, thin-bedded to flaggy; mud cracks. 68 m quartzite, very pale brownish, thin to medium bedded, cross-bedding, ripple marks, shale clasts. 677 m partly coarse-grained quartzite with sandstone, siltstone, and minor dolomite and limestone; siltstone and carbonates medium and dark grey; thin to medium bedded, wavy lamination, ripple marks, shale clasts, mud cracks, current lineations, lenticular bedding. 133 m quartzite, medium to coarse grained, thin to medium bedded, cross-bedding, ripple marks. 71 m sandy siltstone and fine sandstone, platy to flaggy, lenticular bedding. 130 m sandstone partly coarse grained, partly dolomitic and sandy siltstone; flaggy, shale flakes, mud cracks, ripple marks. 969 m partly coarse sandstone with quartzite, siltstone, shale, limestone and dolomite; dolomite partly stromatolitic, dark; siltstone partly black, thin to medium bedded, lenticular bedding, slump structure, cross-bedding, ripple marks, mud cracks, wavy bedding, shale clasts. 75 m partly coarse sandstone with dark dolomite and sandy shale; platy to flaggy, lenticular bedding. 15 m sandstone, pale weathering, coarse grained, rounded grains, medium bedded, ripple marks, cross-bedding.  Base: 28 m sandstone, silty and fine sandstone, lenticular bedding, wavy lamination. Overall sand:shale:carbonate percentages 65:28:7.|16-MAY-23
24574|Willawalpa Formation|Relationships and boundaries|Lies conformably between top Mount Sandstone Beds and Witchelina Quartzite.|16-MAY-23
24574|Willawalpa Formation|Age reasons|Probably early Torrensian. May be equivalent to River Wakefield Subgroup, Fountain Spring Beds and Opaminda Formation.|16-MAY-23
24574|Willawalpa Formation|Comments|Definition: Quartzite and siltstone sequence below the Wichelina Quartzite.|16-MAY-23
24574|Willawalpa Formation|Proposer|Murrell B.|16-MAY-23
27008|Wintrena Formation|Name source|Wintrena 1:63 360 map sheet, Coober Pedy 1:250 000 map sheet, SA.|16-MAY-23
27008|Wintrena Formation|Unit history|Upper part of the Wintrena Beds (Benbow and Pitt 1978). The lower part being defined as Delisser Formation (Benbow in prep.).|16-MAY-23
27008|Wintrena Formation|Type section locality|Western most Wilkinson Lakes, Tallaringa 1:250 000 latitude 29o41'49"S, longitude 132o24'00"E.|16-MAY-23
27008|Wintrena Formation|Extent|Eastern Great Victoria Desert and margins.|16-MAY-23
27008|Wintrena Formation|Thickness range|Average approximately 4 m.|16-MAY-23
27008|Wintrena Formation|Lithology|Sandstone, clayey to silty, orange brown to red. Little sedimentary structure preserved. Only moderately to weakly consolidated. Moderately to poorly sorted.|16-MAY-23
27008|Wintrena Formation|Relationships and boundaries|Overlain by unconsolidated to weakly consolidated red to light orange or white calcareous aeolian sands. Underlain by Delisser Formation (Benbow, in prep) a deep reddened calcrete cemented sandstone.|16-MAY-23
27008|Wintrena Formation|Proposed publication|Explanatory Notes Coober Pedy 1:250 000 and Tallaringa 1:250 000. Geological Survey SA.|16-MAY-23
27008|Wintrena Formation|Name first published by|Benbow M.C., Pitt G.M., 1978|16-MAY-23
20297|Wirrapowie Limestone|Name source|Wirrapowie Creek adjacent to the Type Section. A major creek draining eastward from the Flinders Ranges to Lake Frome.|16-MAY-23
20297|Wirrapowie Limestone|Type section locality|In a small tributary of the Wirrapowie Creek at 31o00' latitude; 139o00' longitude. The tributary drains NE from Woodendinna Bore which is most easily reached by 4-WD some 15 km from a point midway between Point Well and Narrina on the road to Pinda Spring.|16-MAY-23
20297|Wirrapowie Limestone|Extent|Mainly developed in the NE Flinders, thinning sharply southward and gradually to the west. Also occurs in the southern Flinders Ranges near Mernmerna but is absent from the Central Flinders.|16-MAY-23
20297|Wirrapowie Limestone|Thickness range|216 m in the Type Section. Variable elsewhere.|16-MAY-23
20297|Wirrapowie Limestone|Lithology|Flaggy green-grey calcareous siltstones and impure lime mudstones. Intraformational conglomerates and stromatolites are common interbeds. Rare ooid grainstones are also present, as are infrequent desiccation mud-cracks. The unit is very poorly fossiliferous. The base is taken at the top of the topmost dolomite of the Woodendinna Dolomite which it conformably overlies. The top is chosen at the uppermost algal stromatolite bed beneath the fossiliferous black limestones of the Parara L/S.|16-MAY-23
20297|Wirrapowie Limestone|Age reasons|Lower Cambrian. Well above the Diplocraterion beds of the basal Cambrian Parachilna Formation and below Faunal assemblage 2 of Daily (1956).|16-MAY-23
20297|Wirrapowie Limestone|Proposed publication|Trans. R. Soc. S. Aust. 99(4), 211-219, 30/11/75|16-MAY-23
20297|Wirrapowie Limestone|Comments|Additional notes: This unit has been mapped on published map sheets (Copley and Parachilna 1:250 000) as Wilkawillina L/S as that unit occurs in its type section in Ten Mile Creek. In fact the two abovementioned units laterally interfinger with one another, the Wirrapowie L/S outcropping in the NE and South, whilst the Wilkawillina L/S occurs in the Western and Central Flinders Ranges.|16-MAY-23
20297|Wirrapowie Limestone|Name first published by|Thomson B.P., Daily B., Coats R.P., Forbes B.G., 1976|16-MAY-23
26332|Wirriecurrie Granite|Name source|Wirriecurrie is the aboriginal word for Peake Creek, which cuts the ranges north of the ruins of the Peake overland telegraph station. Warrina 1:100 000 sheet area, Warrina 1:250 000 sheet area.|16-MAY-23
26332|Wirriecurrie Granite|Type section locality|3 km northwest of "Peake" ruins, area bounded by metric references 6896600, 6894700 and 585800, 587800.|16-MAY-23
26332|Wirriecurrie Granite|Extent|The granite outcrops in an area of 15 km2 to the west and northwest of Peake ruins and 4 km north of Mount Denison on the Warrina 1:250 000 sheet area.|16-MAY-23
26332|Wirriecurrie Granite|Lithology|Coarse-grained porphyritic granites, augen granites, adamellites, granodiorites, minor aplitic dykes.|16-MAY-23
26332|Wirriecurrie Granite|Age reasons|Middle Proterozoic, radiometrically dated by K-Ar method on biotite yielding an age of 1050 Ma and by Rb-Sr method on total rock giving an age of 1648+/- 21 Ma. Intrudes the Tidnamurkuna Volcanics and unnamed metamorphics north of Peake Creek.|16-MAY-23
26332|Wirriecurrie Granite|Proposed publication|Bull. Geological Survey SA, 50.|16-MAY-23
26332|Wirriecurrie Granite|Defn approved by|Definitions published prior to receipt by SNC and as such cannot be modified - thus no approval|16-MAY-23
26332|Wirriecurrie Granite|Proposer|Flint R.B.|16-MAY-23
24581|Wisanger Basalt|Name source|From small agricultural area between Smith Bay and Rettie Bluff on the northern side of Kangaroo Island. Two homesteads, Wisanger Park and Wisanger Hills are the major settlements in the region, Vivonne 1:100 000 Sheet area.|16-MAY-23
24581|Wisanger Basalt|Unit history|Forbes (1969) refers to the 'basalt at Kingscote'. Other workers have mentioned the 'basalt on Kangaroo Island'.|16-MAY-23
24581|Wisanger Basalt|Type section locality|The Bluff Quarry (Sections 397, 398, Hundred of Menzies) and other quarries on the northern outskirts of Kingscote.|16-MAY-23
24581|Wisanger Basalt|Extent|Exposed as conspicuous flat topped hills (the Gap Hills) at Wisanger, as a small basalt knoll 3.5 km south of Rettie Bluff, at The Bluff near Kingscote and at Alex Lookout east of Penneshaw. The unit is only known on Kangaroo Island.|16-MAY-23
24581|Wisanger Basalt|Thickness range|Range 20-30 metres|16-MAY-23
24581|Wisanger Basalt|Lithology|Basalt composed principally of plagioclase, clinopyroxene and enstatite.|16-MAY-23
24581|Wisanger Basalt|Relationships and boundaries|Disconformably overlies fluvial sediments of Late Palaeozoic or Early Mesozoic age at Wisanger and Kingscote. Ferruginous gravels and sands thinly cover the basalt near the eastern end of the Gap Hills.|16-MAY-23
24581|Wisanger Basalt|Age reasons|Middle Jurassic, based on radiometric determintions by McDougall & Wellman (1976) and accompanying the definition.|16-MAY-23
24581|Wisanger Basalt|Proposed publication|Transactions Royal Society of South Australia 106:1-13.|16-MAY-23
24581|Wisanger Basalt|Proposer|Cooper B.J.|16-MAY-23
20313|Witchelina Quartzite|Name source|Witchelina Station.  Map symbol Pow|16-MAY-23
20313|Witchelina Quartzite|Unit history|Witchelina quartzite' (Sprigg, 1950), 'Witchelina Quartzite' (Forbes and Coats, 1963), 'Copley Quartzite' (Murrell, 1977).|16-MAY-23
20313|Witchelina Quartzite|Type section locality|Old Norwest Gorge, Willawalpa Creek, 12 km SSE of Willouran Hill, latitude 29o52', longitude 138o2'.|16-MAY-23
20313|Witchelina Quartzite|Extent|Willouran Ranges|16-MAY-23
20313|Witchelina Quartzite|Thickness range|1200 m at type section; thins to NW.|16-MAY-23
20313|Witchelina Quartzite|Lithology|Feldspathic (plagioclase, microcline) quartzite and sandstone (64%), very light grey, and black or dark grey shales (36%). Sandstone well sorted, fine grained, with ripple marks, clay galls; mud cracks more common close to base. Shales silty or sandy toward base but black, finely laminated, more pyritic toward top. Idiomorphic authigenic pyrite in both shale and sandstone. Early-formed shortite sand crystals in some sandstones. Four sandstone units exceed 30 m thickness and together aggregate nearly 500 m. Remainder of sequence dominated by shales in ratio 3:2.|16-MAY-23
20313|Witchelina Quartzite|Relationships and boundaries|Transitionally overlies Willawalpa Formation and overlain by black shale of Skillogalee Dolomite.|16-MAY-23
20313|Witchelina Quartzite|Age reasons|Early Torrensian. Lithologically equivalent to upper Copley Quartzite (Parkin and King, 1952), Wortupa Quartzite, Yednalue Quartzite and Bungaree Quartzite.|16-MAY-23
20313|Witchelina Quartzite|Comments|Definition: Ridge-forming quartzite-shale sequence below the Skillogalee Dolomite.|16-MAY-23
20313|Witchelina Quartzite|References|01/31620|16-MAY-23
27954|Woodgate Gravel|Name source|Woodgate Swamp; grid reference 547050 Dalhousie 1:250 000 sheet area.|16-MAY-23
27954|Woodgate Gravel|Type section locality|Three metres of pebbly sandstone exposed in shallowly-sloping south bank of Hamilton Creek 1.5 km west of old railway line; grid reference 521050 Dalhousie 1:250 000 sheet area. Reference localities at Woodgate Swamp and 2.5-5 km east of "Hamilton" homestead on north bank of Hamilton Creek, grid reference 511046.|16-MAY-23
27954|Woodgate Gravel|Extent|Along trunk streams of the large synclines and in the low areas around Woodgate Swamp.|16-MAY-23
27954|Woodgate Gravel|Thickness range|Up to 3 m observed.|16-MAY-23
27954|Woodgate Gravel|Lithology|Light to medium red-brown, consolidated polymict gravel (or pebbly sand) with clasts that include reworked chalcedony from Mt Willoughby Limestone; small to medium scale, low-angle, planar cross-bedding; minor carbonate veining in base of unit.|16-MAY-23
27954|Woodgate Gravel|Relationships and boundaries|Rests disconformably on Pedirka Formation and is overlain with gradational contact by Simpson Sand (Firman, 1970).|16-MAY-23
27954|Woodgate Gravel|Age reasons|No fossils have been recovered from the unit. It may be Late Pleistocene, being the youngest consolidated channel deposit prior to modern stream bed-load.|16-MAY-23
27954|Woodgate Gravel|Proposed publication|Dalhousie, South Australia. Explanatory Notes, 1:250 000 geological series. Sheet SG/53-11.|16-MAY-23
27954|Woodgate Gravel|Proposer|Krieg G.|16-MAY-23
76224|Wookata Shale Member|Name source|Wookata Creek, ~550 m southeast of South Moorowie Mine.|16-MAY-23
76224|Wookata Shale Member|Geomorphic expression|Exposed in eroded anticlinal cores south of Moorowie Mine, to ridge caps near Mt. Daily.|16-MAY-23
76224|Wookata Shale Member|Type section locality|Section I, 70 ft (basal contact?) to 222 ft (upper contact) (21.3 to 67.7 m) 30°59'2.12"S, 139°16'10.24"E to 30°59'3.12"S, 139°16'12.72"E.  Reference section: Section U, 0 to 186ft. (0 to 56.7 m) 30°58'55.57"S, 139°16'7.84"E to 30°58'57.36"S, 139°16'11.18"E.|16-MAY-23
76224|Wookata Shale Member|Extent|Exposed in low hills from Mt. Chambers Gorge, to west of Moorowie Mine, to Mt. Daily.|16-MAY-23
76224|Wookata Shale Member|Thickness range|116 m (152 ft) in type section on Section I. Estimated average ~23 m (76 ft) from other sheared or faulted sections, measured across partly lenticular beds.|16-MAY-23
76224|Wookata Shale Member|Lithology|Ferric red-brown to khaki green, finely micaceous siltstones with thin limestone interbeds at base. Abundant ripple marks, mud cracks, and rare trilobite tracks.|16-MAY-23
76224|Wookata Shale Member|Depositional environment|A restricted shallow marine ramp and flats seaward of a carbonate platform margin, as a depocentre for fine siliciclastics winnowed from tidal channels.|16-MAY-23
76224|Wookata Shale Member|Relationships and boundaries|Second unit from the base of the Moorowie Formation. Conformable, with passage zones from the massive peloid limestones of the Pinyatta Member below and into the megabreccias and archaeocyathan limestones of the Kandramooka Member above.|16-MAY-23
76224|Wookata Shale Member|Structure and Metamorphism|Thin beds of low dip on ridges across broad fold limbs, to layers in tighter folds in anticlinal cores.|16-MAY-23
76224|Wookata Shale Member|Age reasons|Lower Cambrian, Stage 4, within the Pararaia janeae trilobite Zone (Figure 2 of Jago et al, this volume).|16-MAY-23
76224|Wookata Shale Member|Correlations|A probable eastern extension of the Oraparinna Shale, together with the Pack Creek Member of the Moorowie Formation.|16-MAY-23
76224|Wookata Shale Member|Defn author|T. J. Mount,  8-JAN-2019, after Mount (1970).|16-MAY-23
76224|Wookata Shale Member|References|Jago, J. B., Gehling, J. G., Betts, M. J., Brock, G. A., Dalgarno, C. R., Garcia-Bellido, D. C., .., Paterson, J. R. (2019). The Cambrian System in the Arrowie Basin, Flinders Ranges, South Australia. Australian Journal of Earth Sciences. doi:10.1080/08120099.2018.1525431   **Mount, T. J. (1970). Geology of the Mt. Chambers Gorge region (BSc. (Honours) thesis, unpublished).Adelaide, SA: University of Adelaide. http:hdl.handle.net/2440/67162.  **T. J. Mount, J. B. Jago, N. R. Langsford & C. R. Dalgarno (2019): Geological setting of the Moorowie Formation, lower Cambrian Hawker Group, Mt Chambers Gorge, eastern Flinders Ranges, South Australia, Australian Journal of Earth Sciences, DOI: 10.1080/08120099.2019.1586771.|16-MAY-23
20817|Yandoolka Rhyolite|Name source|Yandoolka Well, 7 km east of Lake Everard H.S.  Latitude 31o45'S, longitude 135o14'30"E (Gairdner 1:250 000 sheet (SH 53-15)).|16-MAY-23
20817|Yandoolka Rhyolite|Type section locality|Hill on east side of road to Hiltaba, 1.5 km south of Lake Everard H.S.|16-MAY-23
20817|Yandoolka Rhyolite|Extent|Low scattered outcrops extend over 20 km2, 2 km southeast of Yandoolka Well, and over an isolated area of about 5 km2, 1.5 km southeast of Lake Everard H.S.|16-MAY-23
20817|Yandoolka Rhyolite|Lithology|Highly porphyritic rhyolite or porphyritic microgranite with many phenocrysts of potash feldspar and quartz up to 5 mm long, in a reddish brown finely granular matrix. Accessory biotite and amphibolite has been altered to chlorite and epidote. The rock contains microphenocrysts of sphene. If extrusive the rhyolite must have been a crystal rich lava. It may have been intruded as a plug of crystal rich magma which cooled rapidly after emplacement.|16-MAY-23
20817|Yandoolka Rhyolite|Relationships and boundaries|The base is not exposed, and boundaries are obscured by Quaternary deposits. The unit apparently lies below the porphyritic rhyodacite and dacite units -Pag2 and -Pag3. However, it may be an intrusive neck or plug related to the system of vents from which the volcanic breccia and agglomerate in the lower part of the Wheepool Rhyolite was ejected.|16-MAY-23
20817|Yandoolka Rhyolite|Comments|Outcrops tend to form low yellowish brown weathered rounded masses and tors, similar to granite.|16-MAY-23
20817|Yandoolka Rhyolite|Apprdate|MAR/APR-1975|16-MAY-23
20817|Yandoolka Rhyolite|Defn approved by|South Australia Sub-Committee|16-MAY-23
79744|Yannabie Rhyolite Member|Name source|Yannabie Rhyolite Member. Derived from East Yannabie Dam, 14 km northwest of Nonning Homestead, GDA94, 626570 mE, 6403400 mN, zone 53.|16-MAY-23
79744|Yannabie Rhyolite Member|Unit history|Blissett (1986) defined the Yannabie Rhyodacite as a distinct lava occurring between the Eucarro Rhyolite (at that time named the Eucarro Dacite) and the Paney Rhyolite Member (at that time named the Paney Rhyolite) in the southern Gawler Ranges, which he mapped on the YARDEA 1:250 000 Map Sheet (Blissett et al., 1988). Allen et al. (2003) reinterpreted the stratigraphy of the upper GRV, and recognised that the Yannabie Rhyodacite represented the vesicular flow top of the underlying Eucarro Rhyolite. In their stratigraphic scheme, Allen et al. (2003) did not retain the name Yannabie Rhyodacite as a member within the Eucarro Rhyolite for this vesicular facies. However, given that this facies is a mappable unit and of stratigraphic significance, the term Yannabie Rhyolite Member has been formally reinstated for the use on the Peltabinna 1:75 000 Map Sheet (Werner et al., 2017).|16-MAY-23
79744|Yannabie Rhyolite Member|Type section locality|The use of the type locality defined by Blissett (1986) is here proposed, which is a low ridge 5 km northeast of Paney (GDA94 561850 mE, 6390300 mN, zone 53). In the outcrop belt extending ~4 km to the east and ~7 km to the west the Yannabie Rhyolite Member can be observed intermingled with the Paney Rhyolite Member (Morrow and McPhie, 2000).|16-MAY-23
79744|Yannabie Rhyolite Member|Extent|The Yannabie Rhyolite Member occurs from east to west in three main areas, all of which are along the northern margin of the Eucarro Rhyolite: (1) a ~25 km long, east-northeast-trending belt on Nonning and Siam stations, between Telegraph Dam and Separation Camp, (2) a ~20 km long, east-northeast-trending belt to the south of the Iron Knob ¿ Yardea Road, between Buller Dam in the east and Yannabie Rockhole in the west, on Kolendo and Nonning stations, and (3) an arcuate, east- to southeast-trending belt in the southern part of the Gawler Ranges National Park extending for ~30 km from Mount Double in the east to Paney Arm in the northwest. Occurrence of the Yannabie Rhyolite Member near Mount Friday (described in this report) increases the known extent of this stratigraphic unit about 45 km to the northwest.|16-MAY-23
79744|Yannabie Rhyolite Member|Thickness range|Blissett (1986) estimates the thickness of the Yannabie Rhyolite Member to be up to 100 m.|16-MAY-23
79744|Yannabie Rhyolite Member|Lithology|The Yannabie Rhyolite Member is a reddish-brown, vesicular, porphyritic rhyolite containing phenocrysts of plagioclase, alkali-feldspar, ferromagnesian phases and quartz in a fine grained groundmass (Morrow and McPhie, 2000). Vesicles are (partly) filled with quartz, chlorite, calcite and/or fluorite. The size of these amygdales ranges from microscopically small (~100 micro m) up to several centimetres in width, but mostly in the range of 1-10 mm. Vesicles up to 30 cm are recorded around Nonning Station (Allen et al., 2003). Feldspar phenocrysts are typically subhedral to euhedral and between 1 and 4 mm in length. The groundmass of the rhyolite varies from perlitic, microspherulitic, micropoikilitic to granophyric (Morrow and McPhie, 2000). At Mount Friday the Yannabie Rhyolite Member contains locally accumulations of coarser feldspar crystals ranging in size from 5-10 mm, which probably represent crystals liberated from disintegrated and partially molten granitoid clasts.|16-MAY-23
79744|Yannabie Rhyolite Member|Relationships and boundaries|The Yannabie Rhyolite Member represents the vesicular flow top of the Eucarro Rhyolite (Allen et al., 2003). In outcrop it has gradational to interfingering contacts with the underlying middle part of the Eucarro Rhyolite and the overlying Paney Rhyolite Member (Morrow and McPhie, 2000). In drillhole MSDP07 the Yannabie Rhyolite Member is overlain with an erosional contact by volcaniclastic-sedimentary rocks of the Mount Friday Formation. In drillhole MSDP05 coherent and autoclastic facies of the Yannabie Rhyolite Member are intercalated with volcaniclastic-sedimentary rocks of the Mount Friday Formation, demonstrating locally interfingering relationships between these two stratigraphic units.|16-MAY-23
79744|Yannabie Rhyolite Member|Age reasons|The age of the Yannabie Rhyolite Member can be inferred from a CA-TIMS date of the Eucarro Rhyolite, which yielded a magmatic age of 1587.5 +/- 0.6 Ma (Jagodzinski et al., 2016).|16-MAY-23
79744|Yannabie Rhyolite Member|Defn author|Definition copied from Appendix 3: Werner M, McAvaney SO, Krapf CBE, Pawley MJ and Fabris AJ 2017. Geology of the Peltabinna 1:75 000 Map Sheet, Mineral Systems Drilling Program Special Map Series, Report Book 2016/00025. Department of the Premier and Cabinet, South Australia, Adelaide.|16-MAY-23
79744|Yannabie Rhyolite Member|References|Allen SR, Simpson CJ, McPhie J and Daly SJ 2003. Stratigraphy, distribution and geochemistry of widespread felsic volcanic units in the Mesoproterozoic Gawler Range Volcanics, South Australia.Australian Journal of Earth Sciences 50(1):97-112. **Blissett AH 1986. Subdivision of the Gawler Range Volcanics in the Gawler Ranges. Quarterly Geological Notes 97:2-11. Geological Survey of South Australia, Adelaide. **Blissett AH, Parker AJ and Crooks AF 1988. YARDEA, South Australia, 1:250 000 Geological Atlas Series Map, sheet SI53-03. Geological Survey of South Australia, Adelaide. **Jagodzinski E, Reid A, Crowley J, McAvaney S and Wade C 2016. New CA-TIMS dates for the Gawler Range Volcanism: Implications for the duration of volcanism. In A Reid comp, Geological Survey of South Australia Discovery Day 2016: presentation abstracts and posters, Report Book 2016/00032. Department of State Development, South Australia, Adelaide, pp. 17-18. **Morrow N and McPhie J 2000. Mingled silicic lavas in the Mesoproterozoic Gawler Range Volcanics, South Australia. Journal of Volcanology and Geothermal Research 96(1-2):1-13. **Werner M, McAvaney SO, Krapf CBE, Pawley MJ and Fabris AJ 2017. Geology of the Peltabinna 1:75 000 Map Sheet, Mineral Systems Drilling Program Special Map Series, Report Book 2016/00025. Department of the Premier and Cabinet, South Australia, Adelaide.|16-MAY-23
20845|Yardea Dacite|Name source|Yardea H.S.  Latitude 32o23'S, longitude 135o32'E (Yardea 1:250 000 sheet (SI 53-3)).|16-MAY-23
20845|Yardea Dacite|Type section locality|Yardea area; Mt Nott; area 10 km north of Waurea Hill.|16-MAY-23
20845|Yardea Dacite|Extent|The dacite crops out over several thousand km2 in the area around Yardea, including islands in the southern two-thirds of Lake Gairdner.|16-MAY-23
20845|Yardea Dacite|Thickness range|At least 250 m (Mt Nott).|16-MAY-23
20845|Yardea Dacite|Lithology|Little variation over a wide area. The dacite is highly porphyritic with many phenocrysts of cream plagioclase up to about 1 cm long. Some phenocrysts of hornblende. The matrix is reddish or purplish red to purplish brown. Grades to rhyodacite locally.|16-MAY-23
20845|Yardea Dacite|Relationships and boundaries|Uppermost layered member of the Gawler Range Volcanics in the Gawler Ranges proper. Overlies rhyolite on the western shore of Lake Acraman and the Wheepool Rhyolite south of Dingo Hill. Intruded by the Hiltaba Granite (c. 1500 Ma B.P.) in the Hiltaba district, and by dykes or plugs of banded rhyolite whose age is unknown, near Paney outstation and also 13 km southwest of Mt Nott.|16-MAY-23
20845|Yardea Dacite|Age reasons|Carpentarian|16-MAY-23
20845|Yardea Dacite|Comments|The enormous volume of material erupted indicates that the Yardea Dacite may be composed of welded ash flow tuffs rather than lava flows. However, no positive evidence of welding has been found to date.|16-MAY-23
20845|Yardea Dacite|Apprdate|MAR/APR-1975|16-MAY-23
20845|Yardea Dacite|Defn approved by|South Australia Sub-Committee|16-MAY-23
26243|Yarle Sandstone|Name source|Yarle Lakes ison the northern margin of the Nullarbor Plain, between Watson and Maralinga (Fig. 1).|16-MAY-23
26243|Yarle Sandstone|Unit history|The previously published names for conceptually equivalent rocks on the northwestern and northern part of the platform, the Colville Sandstone (Lowry, 1970) and Plumridge Beds (Lowry et al, 1972; Jackson and van de Graaff, 1981) are not used (Benbow, in prep.).  Examination of the type and reference sections of the former unit indicate that the limestone is best included within the Nullarbor Limestone and that the bulk (at least) of the terrigenous sediments are likely to be Cretaceous, if not Permian, in age.  At one of the reference sections, basal and capping limestone units were described as being separated by about 20m of shale, sandstone and conglomerate, however it appears that there is only one limestone unit.  An unconformable relationship can be demonstrated between it and the underlying sandstone.  There is a transgressive lag beneath this limestone, not described by Lowry (1970), as occurs around the east margin of the Eucla Platform. The term Plumridge Beds is not used since a relationship with Nullarbor Limestone cannot be demonstrated and the lithological variation of this unit is much greater that that known for the Yarle Sandstone.  Furthermore, estimated thicknesses of 20-100m (Playford et al, 1975; Jackson and van de Graaff, 1981) far exceed that known for the Yarle Sandstone.|16-MAY-23
26243|Yarle Sandstone|Type section locality|This is located at Yarle Lakes; a type section has not been chosen because of minimal section exposure and uncertainty of recognition in drillholes that are commonly inadequately sampled.|16-MAY-23
26243|Yarle Sandstone|Extent|The Yarle Sandstone occurs along the northeast margin of the Nullarbor Plain, between Yarle Lakes and Seven Miles Swamps, adjacent to the Ooldea Range (Fig. 1; Benbow and Lindsay, 1988). It apparently formsa narrow belt, generally less than 10km wide, along the inner margin of the Miocene platform,  at the limit of the Nullarbor Limestone.  There are exposures, now silicified and ferruginised, in the floors and around margins of the playa lakes, and also along the adjacent interdune corridors on the margin of the Great Victoria Desert between Yarle Lakes and Ooldea.|16-MAY-23
26243|Yarle Sandstone|Thickness range|Up to 5m of section is exposed, but generally less than 2m is evident. maximum thickness could be about 20m, if the sand, intersected in the nearby Maralinga 14 to 17 wells is assigned to the formation (Benbow, 1990, Fig. 7).|16-MAY-23
26243|Yarle Sandstone|Lithology|The formation is composed predominantly of quartz-rich sand, with a local bioclastic component that includes abraded fragments of foraminifers, echinoids, algae and molluscs. In the Yarle Lakes -Ooldea area the sand is mostly very fine and medium-grained. the finer sand is commonly bimodal, with a sunsidiary mode of coarse to very coarse-grained, well rounded quartz. Here there are also rare deformed, irregularly shaped clasts of yellow-brown limestone similar to those which make up the Nullarbor limestone.  Minor terrigenous mud also occurs. At Yarle Lakes there is cross0bedding that dips shorewards to the northeast; this is partly destroyed by bioturbation.|16-MAY-23
26243|Yarle Sandstone|Relationships and boundaries|The formation unconformably overlies weathered Precambrian basement of the gawler Craton and sedimentary rocks of the Neoproterozoic-Palaeozoic Officer Basin. At Seven Mile Swamps in Australian Mining Corporation (AMC) 316-5 Drillhole where the unit is ~10m thick and silcrete capped, the formation to conformably overlie very thin limestone that is at present included in the Nullarbor Limestone (Benbow and Lindsay, 1988).  Here the basal sand is calcareous. In the type area, Yarle sandstone is overlain sharply but apparently conformably, by faminiferal packstone of the Nullarbor Limestone.  Silicification and ferruginisation has obscured the nature of the boundary.  The absence of a basal transgressive lag, seen elsewhere at the base of the nullarbor Limestone, and the occurrence of limestone clasts, supports a conformably relationship.  Conspicuous intertonguing of Yarle Sandstone and Nullarbor Limestone has not been observed and any intertonguing that may have existed is considered to have been largely removed by post-depositional erosion.  Also in the Yarle Lakes region, the formation is unconformably overlain Quaternary aoeolian sand of the Great Victoria Desert.  Where Yarle sandstone is not duricrust capped, the position of the upper boundary is difficult to judge because of reworking and Quaternary weathering.|16-MAY-23
26243|Yarle Sandstone|Age reasons|The presence of the large benthonic foraminifer Austrotrillina howchini and Marginopora vertbralis (the latter has been observed in the limestone clasts), indicates an age no older than earliest Miocene (Adams 1984).  An Early to early Middle Miocene age may be deduced from the age of the Nullarbor Limestone (Benbow and Lindsay, 188 and references therein). Lindsay (IN: Benbow and Lindsay, 1988) interprets an Early Miocene )Longfordian) age for the conformably underlying thin limestone at Seven Mile Swamps in AMC 316-5.|16-MAY-23
26243|Yarle Sandstone|Defn author|Benbow, M.C.|16-MAY-23
26243|Yarle Sandstone|Comments|This definition has been manually copied from the definition reference - no formal Definition Card received.|16-MAY-23
26243|Yarle Sandstone|References|See SA Quarterly Notes, Vol 113 for list of 17 bibliographic references.|16-MAY-23
26243|Yarle Sandstone|Defn Reference|Benbow, M.C, 1990. The Yarle Sandstone: a Miocene coastal terrigenous sequence of the Eucla Platform. South Australia. geological Survey. Quarterly Geological Notes, 113:2-6.|16-MAY-23
24601|Younghusband Conglomerate|Name source|Mount Younghusband outcrops in the Denison Inlier in the northern Peake and Denison Ranges, 10 km northeast of Warrina R.S., Warrina 1:100 000 sheet area, Warrina 1:250 000 sheet area; metric ref: 6886250.|16-MAY-23
24601|Younghusband Conglomerate|Type section locality|27 metres of clastic sediments outcropping on the eastern margin of the Coominaree Mine Block (Lower Proterozoic basement), 1.2 km north of Coominaree Mine. The lower part (12 m thick) contains coarse clastic sediments. The upper 15 m is mainly argillaceous. Metric ref: Type Section 6853275, 59645. The unit was first described by Thomson (1966).|16-MAY-23
24601|Younghusband Conglomerate|Extent|The unit outcrops along a strike length of 7 km, 3.5 km southwest of "Peake" ruins on Warrina. Other small outcrops occur 3 km south of War Loan Mine and 1.2 km north of Coominaree Mine.|16-MAY-23
24601|Younghusband Conglomerate|Thickness range|Variable up to 27 m.|16-MAY-23
24601|Younghusband Conglomerate|Lithology|Basal quartzitic breccia, red-brown shale and sandstone at the top.|16-MAY-23
24601|Younghusband Conglomerate|Relationships and boundaries|Overlies Lower Proterozoic basement rocks (Peake Metamorphics) with angular unconformity. Reworked basement clasts recognised in the basal breccia. The unit is lenticular. In the type section it is conformably overlain by the Coominaree Dolomite while 3.5 km southwest of "Peake" ruins the Younghusband Conglomerate is disconformably overlain by the Cadlareena Volcanics (Ambrose and Flint, in prep.).|16-MAY-23
24601|Younghusband Conglomerate|Age reasons|Basal Adelaidean-Callanna Beds (Willouran); an angular unconformity with Lower Proterozoic basement rocks is observed 3.5 km southwest of "Peake" ruins.|16-MAY-23
24601|Younghusband Conglomerate|Proposed publication|Rep. Invest., Geol. Surv. SA|16-MAY-23
24601|Younghusband Conglomerate|References|01/31599|16-MAY-23
24601|Younghusband Conglomerate|Proposer|Ambrose G.J., Coats R.P.|16-MAY-23
