The Yilgarn Craton appears to have been assembled between ~2.94 and 2.63 Ga by the accretion of a multitude of formerly present blocks or terranes of existing continental crust, most of which formed between 3.2 Ga and 2.8 Ga.
This accretion event is recorded by widespread granite and granodiorite intrusions, which comprise over 70% of the Yilgarn craton; voluminous tholeiiticbasalt and komatiitevolcanism;[3] regional metamorphism and deformation as well as the emplacement of the vast majority of the craton's endowment in gold mineralisation.
These accretion events occurred in several phases, probably by accretion of continental fragments separated by pauses in subduction, with renewed activity occurring episodically.
The craton is primarily composed of approximately 2.8 billion year old (~2.8 Ga) granite-gneiss metamorphic terrain (the Southwestern Province and Western Gneiss Belt), and three granite-greenstone terrains (the North-East Goldfields, the Southern Cross and the greenschist metamorphic Murchison Provinces). Some greenstone belts and granites are as old as 3.1-2.9 Ga, and some are younger, at ~2.75-2.65 Ga.
The craton is one of the distinct physiographic provinces of the West Australian Shield physiographic division, which comprises the Stirling-Mount Barren Block, Darling Hills, and Recherche Shelf sections.
Western Gneiss Terrane
The Western Gneiss Terrane is a series of polydeformed high-grade early Archaean metamorphic belts, composed predominantly of feldspathic leucocratic granulite gneisses, which represent some of the oldest crustal fragments on Earth.[4] The Western Gneiss Terrane is distinct from the remainder of the Yilgarn Craton in that the latter has a predominance of metavolcanic rocks, both felsic and mafic, whereas the former consists of high-grade metasediments and gneisses of unknown protolith.
The Western Gneiss Terrane is exposed along the western half of the northern margin of the Yilgarn Craton as the Narryer Gneiss Terrane, a composite of heavily polydeformed feldspathic metagranite and metasedimentary amphibolite-grade gneisses and migmatites, dated at greater than 3.3 Ga and up to 3.8 Ga in age, flanked by the Murgoo Gneiss Terrane (2.95 Ga), as well as sheets of 2.75 Ga to 2.6 Ga granite, obductedophiolite sheets (the Trillbar Complex) and some 2.4 Ga to 2.0 Ga Proterozoic gneiss belts.
On the western edge of the Yilgarn Craton, partially covered by Phanerozoic sedimentary basins and in faulted contact with the 2.7 Ga to 2.55 Ga Yilgarn tectonic domains, lies the Jimperding Gneiss Complex of 2.75 to 2.65 Ga age, composed primarily of micaceous quartzite, quartz-feldspar-biotite-garnet gneiss, andalusite and sillimaniteschists, banded iron formation and other exotics, intruded by minor masses of porphyritic granite.
Detrital zircons in the Jimperding Gneiss Complex range in age from 3267 ± 30Ma to 3341 ± 100Ma, with metamorphic overgrowth dated at 3180Ma.
On the southwest of the Yilgarn Craton the Balingup Gneiss Complex is situated inboard from the Early Proterozoic Leeuwin Complex of metamorphic rocks. The Balingup Complex consists primarily of metasedimentary paragneiss, granite orthogneiss, with minor layers of calc-silicate, ultramafic and ortho-amphibolite gneiss. The metamorphic grade is considered to be peak granulite facies, but the majority has preserved peak amphibolite facies assemblages.
In total, the Western Gneiss Terrane sub-blocks represent an earlier substrate upon which the majority of the Yilgarn Craton's about 2.70 to 2.55Ga greenstone metavolcanic belts have been deposited and into which the voluminous Archaean trondhjemite-tonalite-granodiorite suite and trondhjemite-tonalite-diorite suite granites were emplaced.
Murchison Province
The Murchison Province is exposed in the western and northern third of the Yilgarn Craton. The Province is bounded by major transcrustal structures which separate it from the surrounding tectonic provinces of the craton and the Western Gneiss Belt.
The Murchison Province Stratigraphy, after Watkins (1990), is divided into six basic structural-stratigraphic components - two greenstone belt metavolcanic-metasedimentary sequences and four suites of granitoids.
Luke Creek Group metavolcanics
Mount Farmer Group
Early granodiorite-monzogranite intrusive suite (now pegmatite-banded orthogneiss)
Monzogranite Suite (now folded, metagranite)
Two post-tectonic differentiated suites of granitoid rocks
The structural framework in the northeastern Yilgarn craton was largely shaped by transpression that led to the development of folds, reverse faults, sinistral strike-slip movement on NNW-trending regional shear zones, followed by regional folding and shortening. The later occurred in overlapping tectonic processes. The first deformation event is poorly understood but appears to have involved N-S thrusting.
The Murchison Province contains the Yarrabubba crater, which is the oldest dated meteoriteimpact crater, at 2229 ± 5 Ma. The crater is heavily eroded and no surface expression remains of the original structure. The primary trace is an elliptical aero-magnetic anomaly, measuring approximately 20km by 11km, as well as the presence of shock-recrystallised minerals. This impact may have ended the Huronian glaciation by climate forcing with a significant pulse of greenhouse gases, as the age broadly overlaps with the youngest glacial deposits.[2]
Southern Cross Province
The Southern Cross Province lies in the central area of the Yilgarn craton. The Marda–Diemalsgreenstone belt in the Southern Cross Terrane can be divided into three layers: the lower greenstone belt (ca. 3.0 Ga) characterized by mafic volcanic rock and banded iron formation, a felsic-intermediate volcanism layer, and an upper sedimentary layer (ca. 2.73 Ga) of calc-alkaline volcanic (Marda Complex) and clastic sedimentary rocks (Diemals Formation).[5]
East–West orogeny (ca. 2730–2680 Ma) occurred in two stages; an earlier folding phase and a late phase that resulted in deposition and deformation of the Diemals Formation. Subsequent orogeny (ca. 2680–2655 Ma) resulted in shear zones and arcuate structures.
The lithostratigraphy of the Marda–Diemalsgreenstone belt are similar to the northern Murchison Terrane, but has older greenstones and deformation events than the southern Eastern Goldfields Terrane. This indicates that the Eastern Goldfields Terrane may have accreted to an older Murchison–Southern Cross granite–greenstone nucleus.
Eastern Goldfield Province
The Archaean Norseman-Wiluna Greenstone Belt[6] in the Eastern Goldfield Province contains most of Australia's lode gold deposits, including the famous Kalgoorlie Golden Mile containing the Super Pit.
These gold deposits are generally of large tonnage and are confined to the volcanic-intrusive-sedimentary sequences of the greenstone belts and not the granites. There is a pattern of gold distribution along the Archean Boulder-Lefroy shear zone.
Extrusive komatiites (ultramafic volcanic rocks) occur along the Norseman-Wiluna Greenstone Belt. A change from volcanic-dominated to plutonic-dominated magmatism occurred in the Norseman-Wiluna Greenstone Belt approximately 2685–2675 Ma. Voluminous high-Ca granite intrusions occurred 2670–2655 Ma.[7] Much of the gold was deposited between 2650–2630 Ma, with much of this associated with strike-slip reactivation of earlier faults (normal and reverse).
An earlier gold event 2660-2655 Ma was associated with major extension (normal faulting and granite doming) resulting in the formation of late basins and the intrusion of mantle-derived magmas (syenites and Mafic-type granites/porphyries) and tight anticlockwise PTt paths.
Bounding terranes
The Yilgarn Craton is bound on all sides by younger terranes of various ages, but predominantly of Proterozoic age. The boundaries between the various flanking terranes provide considerable evidence of the post-Archaean events which have involved the Yilgarn Craton.
Perth Basin
The Yilgarn Craton is bound on the western side by the Perth Basin, of Jurassic age, and is separated from this basin by the Darling Fault. The Perth Basin is considered to be a rift fill basin formed on a passive margin.
Gascoyne Complex
The Perth Basin is bound on the north by the Gascoyne Complex,[8]Glengarry Basin and Yerrida Basin, which are all part of a middle Proterozoic mobile belt which leads east to the Musgrave Block. The Gascoyne complex and other metamorphic belts of this age including reactivation of the Yarlarweelor Gneiss and Narryer Gneiss Terrane, indicate prolonged multi-phased strike-slip movement (relative to the Yilgarn Craton margin) from the late Archaean through to neoproterozoic and even into the Palaeozoic.[9]
Albany-Fraser Orogen
The Yilgarn Craton is bounded on the east-southeast by the ~1,300 Ma Albany-Fraser Orogen, composed primarily of amphibolite to greenschist facies sedimentary protolith gneisses, migmatites and granites. The Albany-Fraser Orogen displays both subduction-related and prolonged strike-slip tectonic structures and is intimately interconnected with the other Proterozoic basins and mobile belts of Australia.
Sedimentary basin cover
The Yilgarn Craton is partially covered by onlapping sedimentary basins of Palaeozoic and Phanerozoic age in the east and north-east, including the Canning Basin. It is bounded on the western edge by the Darling Scarp and Darling Fault which separate the Yilgarn Craton from the Perth Basin to the west, and is covered by several remnant sedimentary basins of Jurassic age such as the Collie Sub-Basin.
The Yilgarn Craton also has a considerable Tertiary and younger sedimentary veneer of palaeochannel deposits derived from prolonged erosion, sedimentation and redeposition of older cover sequences and regolith as well as the Archaean basement itself.
The Yilgarn craton is believed to have remained at or above sea level for a considerable length of time.[10] Some of the Yilgarn regolith is the oldest in the world, recording weathering events as early as the Cretaceous Period. This has been created by the generally subtropical latitudes and conditions of the Yilgarn craton, with minimal to no glaciation and generally flat topographical relief resulting in comparatively minor erosion.
The regolith is extremely deeply weathered, in some areas completely converted to saprolite up to 100 metres below surface. This is considered to have been produced during Caenozoic to Palaeocene tropical conditions, as evidenced by mottled duricrust which records fossilised tree roots, some over 60 million years old. Previous weathering events have been recorded in magnetically remnant ferruginouslaterite of a Jurassic age, at about 180 Ma.
The regolith of the Yilgarn impacts directly on the flora and fauna, as some of the soil is essentially fossilised. Much of the groundwater of the Yilgarn is hypersaline, with some being supersaturated in salt. This renders swathes of land barren, with significant salt lakes, and high saline water tables. The origin of this salt is thought to be from precipitation of sea salt carried over the Australian landmass for the past several dozen million years, and the high evaporation rate leaving the salt behind.
The greenstone belts of the Yilgarn Craton include:
Southern Cross Greenstone Belt
Norseman-Wiluna Belt
Duketon Belt
Gullewa Greenstone Belt
Economic geology
The Yilgarn Craton is Australia's premier mineral province. It attracts more than half of Australia's minerals exploration expenditure, and produces two thirds of all gold and most of the nickel mined in Australia. The craton contains some 30% of the world's known gold reserves,[citation needed][disputed–discuss] about 20% of the world's nickel reserves, 80% of the world's tantalum reserves, considerable iron ore, copper, zinc and minor lead reserves. The craton contains significant platinum, vanadium, hard-rock titanium and considerable iron ore resources.
Iron ore is currently recovered from several areas in the Yilgarn Craton, although it is a much smaller set of mines than those in the Pilbara Craton. Iron ore is mined at Koolyanobbing, north of Kalgoorlie from hematite weathered banded iron formation, at Mount Gibson, Weld Range and Jack Hills in the Western Gneiss Terrane from hematite banded iron formation to produce direct-shipping ore.
The Karara Iron Ore Project is the only operational magnetite mine in the Yilgarn Craton, however, other magnetite iron ore deposits are being investigated as a source of magnetite ore in the Albany-Fraser Complex, where a large deposit is being proposed at Southdown. The Jack Hills, Weld Range and Mount Gibson banded iron formations, as well as banded iron formations around Yalgoo, are also considered potential sources of magnetite iron ore, although no operations are as yet running on this type of ore.
Further away from the coast, deposits of banded iron formation at Wiluna and Laverton are also under investigation, although infrastructure is considered too poor to render these deposits economic.
Gold
The Yilgarn Craton is host to around 4% of the world's economically demonstrably recoverable reserves (EDR) of gold.[citation needed][disputed–discuss]
Major gold deposits occur at Kalgoorlie, Kambalda, Mount Magnet, Boddington, Laverton and Wiluna, and are hosted in greenstone belts. These form linear belts of mafic, ultramafic and felsic volcanics, intercalated with sedimentary sequences, and have been deformed and metamorphosed. The mode of occurrence of the gold mineralisation tends to be small- to medium-sized structurally controlled lodes, shears, and quartz veins.
A key feature beneath many of the region's gold deposits are granite-cored domes at a range of scales. These provided an architecture that focussed fluid metals into the upper crust's depositional sites.
Signatures of the mantle are found in many large deposits, including melts from metasomatised mantle wedge as well as lamprophyres. Debate continues whether these mantle rocks were a fluid and/or metal source, or simply reflect a favourable pathway.
Nickel-PGE deposits
The greater Kambalda district hosts a world-class nickel-sulfide mining district with a total pre-mining resource of 2 megatons (Mt) of nickel metal. Approximately 1.1 Mt of nickel metal has been produced since 1967, at an average rate of 35,000 tons of nickel per year. The Kambalda Dome is located in the south-central part of the Archaean Norseman-Wiluna greenstone belt in the southeastern Yilgarn Craton. Kambalda type komatiitic nickel ore deposits are the primary source of nickel metal within the Yilgarn Craton.[11]
Base metals
Copper, lead and zinc are currently mined from Golden Grove and the newly developed Jaguar zinc mine. Minor amounts of copper have been recovered from several copper-bearing gold deposits such as those in the Gullewa Greenstone Belt, at Burtville south of Laverton, at Granny Smith and elsewhere.
The desert area encircling Kalgoorlie, with an area of 500,000 square kilometres, is theorised to host a 100 million tonne copper-zinc deposit. The geology of several volcanic belts in the Yilgarn Craton are strikingly similar to the world's great base-metal mines at Kidd Creek in Northern Ontario, Canada. Exploration for copper is continuing in several areas around Ravensthorpe, Balagundi, in the Yandall Belt, and the Duketon Belt, where large felsic volcanic packages are known to exist.
Rare-earth elements
The Yilgarn Craton may host up to 60% of the world's recoverable rare-earth elements, primarily in the Mount WeldCarbonatite. Smaller carbonatite occurrences at Ponton, near Laverton, and regionally within the eastern granite-gneiss and greenstone belts, may also prove economic.
Uranium
The Yilgarn Craton and its cover sequences are host to a significant percentage of the world's endowment in economically demonstrable and recoverable reserves (EDR) of uranium. Most uranium is hosted within palaeochannels derived from granites of the Yilgarn Craton and/or its flanking Proterozoic orogens, and this metal is deposited within Tertiary or younger palaeodrainage and current drainage systems. Examples include Yeelirrie, Mulga Rock[10] and Lake Way-Centipede.
Kenorland is a hypothetical Neoarchean supercontinent. If it existed, it would have been one of the earliest known supercontinents on Earth. It is thought to have formed during the Neoarchaean Era c. 2.72 billion years ago by the accretion of Neoarchaean cratons and the formation of new continental crust. It comprised what later became Laurentia, Baltica, Western Australia and Kalaharia.
Greenstone belts are zones of variably metamorphosed mafic to ultramafic volcanic sequences with associated sedimentary rocks that occur within Archaean and Proterozoic cratons between granite and gneiss bodies.
Diabase, also called dolerite or microgabbro, is a mafic, holocrystalline, subvolcanic rock equivalent to volcanic basalt or plutonic gabbro. Diabase dikes and sills are typically shallow intrusive bodies and often exhibit fine-grained to aphanitic chilled margins which may contain tachylite.
Ultramafic rocks are igneous and meta-igneous rocks with a very low silica content, generally >18% MgO, high FeO, low potassium, and are composed of usually greater than 90% mafic minerals. The Earth's mantle is composed of ultramafic rocks. Ultrabasic is a more inclusive term that includes igneous rocks with low silica content that may not be extremely enriched in Fe and Mg, such as carbonatites and ultrapotassic igneous rocks.
Komatiite is a type of ultramafic mantle-derived volcanic rock defined as having crystallised from a lava of at least 18 wt% magnesium oxide (MgO). It is classified as a 'picritic rock'. Komatiites have low silicon, potassium and aluminium, and high to extremely high magnesium content. Komatiite was named for its type locality along the Komati River in South Africa, and frequently displays spinifex texture composed of large dendritic plates of olivine and pyroxene.
The Narryer Gneiss Terrane is a geological complex in Western Australia that is composed of a tectonically interleaved and polydeformed mixture of granite, mafic intrusions and metasedimentary rocks in excess of 3.3 billion years old, with the majority of the Narryer Gneiss Terrane in excess of 3.6 billion years old. The rocks have experienced multiple metamorphic events at amphibolite or granulite conditions, resulting in often complete destruction of original igneous or sedimentary (protolith) textures. Importantly, it contains the oldest known samples of the Earth's crust: samples of zircon from the Jack Hills portion of the Narryer Gneiss have been radiometrically dated at 4.4 billion years old, although the majority of zircon crystals are about 3.6-3.8 billion years old.
The geology of Australia includes virtually all known rock types, spanning a geological time period of over 3.8 billion years, including some of the oldest rocks on earth. Australia is a continent situated on the Indo-Australian Plate.
The Gascoyne Complex is a terrane of Proterozoic granite and metamorphic rock in the central-western part of Western Australia. The complex outcrops at the exposed western end of the Capricorn Orogen, a 1,000 km-long arcuate belt of folded, faulted and metamorphosed rocks between two Archean cratons; the Pilbara craton to the north and the Yilgarn craton to the south. The Gascoyne Complex is thought to record the collision of these two different Archean continental fragments during the Capricorn Orogeny at 1830–1780 Ma.
The Gawler Craton covers approximately 440,000 square kilometres of central South Australia. Its Precambrian crystalline basement crustal block was cratonised ca. 1550–1450 Ma. Prior to 1550 Ma the craton comprised a number of active Proterozoic orogenic belts extending back in time to at least 2450 Ma.
Kambalda type komatiitic nickel ore deposits are a class of magmatic iron-nickel-copper-platinum-group element ore deposit in which the physical processes of komatiite volcanology serve to deposit, concentrate and enrich a Fe-Ni-Cu-(PGE) sulfide melt within the lava flow environment of an erupting komatiite volcano.
The Emily Ann and Maggie Hays nickel deposits are situated 117 km west of the town of Norseman, Western Australia, within the Lake Johnston Greenstone Belt.
The Slave Craton is an Archaean craton in the north-western Canadian Shield, in Northwest Territories and Nunavut. The Slave Craton includes the 4.03 Ga-old Acasta Gneiss which is one of the oldest dated rocks on Earth. Covering about 300,000 km2 (120,000 sq mi), it is a relatively small but well-exposed craton dominated by ~2.73–2.63 Ga greenstones and turbidite sequences and ~2.72–2.58 Ga plutonic rocks, with large parts of the craton underlain by older gneiss and granitoid units. The Slave Craton is one of the blocks that compose the Precambrian core of North America, also known as the palaeocontinent Laurentia.
The Kaapvaal Craton, along with the Pilbara Craton of Western Australia, are the only remaining areas of pristine 3.6–2.5 Ga crust on Earth. Similarities of rock records from both these cratons, especially of the overlying late Archean sequences, suggest that they were once part of the Vaalbara supercontinent.
The Barberton Greenstone Belt is situated on the eastern edge of the Kaapvaal Craton in South Africa. It is known for its gold mineralisation and for its komatiites, an unusual type of ultramafic volcanic rock named after the Komati River that flows through the belt. Some of the oldest exposed rocks on Earth are located in the Barberton Greenstone Belt of the Eswatini–Barberton areas and these contain some of the oldest traces of life on Earth, second only to the Isua Greenstone Belt of Western Greenland. The Makhonjwa Mountains make up 40% of the Baberton belt. It is named after the town Barberton, Mpumalanga.
The Widgiemooltha Komatiite is a formation of komatiite in the Yilgarn Craton of Western Australia.
The geology of Zimbabwe in southern Africa is centered on the Zimbabwe Craton, a core of Archean basement composed in the main of granitoids, schist and gneisses. It also incorporates greenstone belts comprising mafic, ultramafic and felsic volcanics which are associated with epiclastic sediments and iron formations. The craton is overlain in the north, northwest and east by Proterozoic and Phanerozoic sedimentary basins whilst to the northwest are the rocks of the Magondi Supergroup. Northwards is the Zambezi Belt and to the east the Mozambique Belt. South of the Zimbabwe Craton is the Kaapvaal Craton separated from it by the Limpopo Mobile Belt, a zone of deformation and metamorphism reflecting geological events from Archean to Mesoproterozoic times. The Zimbabwe Craton is intruded by an elongate ultramafic/mafic igneous complex known as the Great Dyke which runs for more than 500 km along a SSW/NNE oriented graben. It consists of peridotites, pyroxenites, norites and bands of chromitite.
The Eastern Pilbara Craton is the eastern portion of the Pilbara Craton located in Western Australia. This region contains variably metamorphosed mafic and ultramafic greenstone belt rocks, intrusive granitic dome structures, and volcanic sedimentary rocks. These greenstone belts worldwide are thought to be the remnants of ancient volcanic belts, and are subject to much debate in today's scientific community. Areas such as Isua and Barberton which have similar lithologies and ages as Pilbara have been argued to be subduction accretion arcs, while others suggest that they are the result of vertical tectonics. This debate is crucial to investigating when/how plate tectonics began on Earth. The Pilbara Craton along with the Kaapvaal Craton are the only remaining areas of the Earth with pristine 3.6–2.5 Ga crust. The extremely old and rare nature of this crustal region makes it a valuable resource in the understanding of the evolution of the Archean Earth.
Gabon is situated at the northwestern margin of the Congo Craton—a region of stable, ancient crust—and preserves very ancient rock units across 75% of the country, with overlying sedimentary units from the Cretaceous and other more recent periods.
The geology of Mozambique is primarily extremely old Precambrian metamorphic and igneous crystalline basement rock, formed in the Archean and Proterozoic, in some cases more than two billion years ago. Mozambique contains greenstone belts and spans the Zimbabwe Craton, a section of ancient stable crust. The region was impacted by major tectonic events, such as the mountain building Irumide orogeny, Pan-African orogeny and the Snowball Earth glaciation. Large basins that formed in the last half-billion years have filled with extensive continental and marine sedimentary rocks, including rocks of the extensive Karoo Supergroup which exist across Southern Africa. In some cases these units are capped by volcanic rocks. As a result of its complex and ancient geology, Mozambique has deposits of iron, coal, gold, mineral sands, bauxite, copper and other natural resources.
The geology of Tanzania began to form in the Precambrian, in the Archean and Proterozoic eons, in some cases more than 2.5 billion years ago. Igneous and metamorphic crystalline basement rock forms the Archean Tanzania Craton, which is surrounded by the Proterozoic Ubendian belt, Mozambique Belt and Karagwe-Ankole Belt. The region experienced downwarping of the crust during the Paleozoic and Mesozoic, as the massive Karoo Supergroup deposited. Within the past 100 million years, Tanzania has experienced marine sedimentary rock deposition along the coast and rift formation inland, which has produced large rift lakes. Tanzania has extensive, but poorly explored and exploited natural resources, including coal, gold, diamonds, graphite and clays.
References
↑ Earlier known as Yilgarn BlockGeological Survey of Western Australia (1975), The Geology of Western Australia, Western Australia Geological Survey, ISBN978-0-7244-6084-7 , section Yilgarn Block by I. R. Williams page 33–81.
↑ Chen, She Fa, John E. Greenfield, David R. Nelson, Angela Riganti, and Steven Wyche. (2003) "Lithostratigraphy and tectonic evolution of contrasting greenstone successions in the central Yilgarn Craton, Western Australia". Precambrian Research, Vol. 127, Issues 1-3 , 10 November, pp. 249–266.
↑ Swager, C. P., Witt W. K., Griffin A. L., Ahmat A. L., Hunter W. M., McGoldrick P. J. & Wyche, S., 1992. Late Archaean Granite-Greenstones of the Kalgoorlie Terrane, Yilgarn Craton, Western Australia in The Archaean: Terrains, Processes and Metallogeny, University of Western Australia, Publication 22, pp. 39–49.
↑ Hammond, R. L. & Nisbett B. W., 1992. Towards a Structural and Tectonic Framework for the central Norseman-Wiluna Greenstone Belt, Western Australia in The Archaean: Terrains, Processes and Metallogeny, University of Western Australia, Publication 22, pp. 39–49.
↑ Moresi, Louis, Peter van der Borgh, and Roberto F. Weinberg. (2003) "Timing of deformation in the Norseman-Wiluna Belt, Yilgarn Craton, Western Australia". Precambrian Research, Vol. 120, Issues 3-4, 10 February, pp. 219–239.
↑ Cawood, P. A. and Tyler, I. M., 2004. Assembling and reactivating the Proterozoic Capricorn Orogen: lithotectonic elements, orogenies, and significance. Precambrian Research, 128, p. 201–218.
↑ Sheppard, S., Occhipinti, S. A. and Nelson, D. R., 2005. Intracontinental reworking in the Capricorn Orogen, Western Australia: the 1680–1620 Ma Mangaroon Orogeny. Australian Journal of Earth Sciences, 52, p. 443–460.
1 2 Anand R.; Paine M. "Regolith Geology of the Yilgarn Craton, Western Australia". Australian Journal of Earth Sciences. 49 (1). doi:10.1046/j.1440-0952.2002.00912.x.
↑ Hill R. E. T, Barnes S. J., Gole M. J., and Dowling S. E., 1990. Physical volcanology of komatiites; A field guide to the komatiites of the Norseman-Wiluna Greenstone Bel, Eastern Goldfields Province, Yilgarn Block, Western Australia, Geological Society of Australia. ISBN0-909869-55-3.
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