Pilbara Craton
Stratigraphic range: Age Archean[1] Pha. Proterozoic Archean Had.
Satellite view in 2013 of Pilbara Craton
Type	Geological formation
Area	Estimated 250,000 km2 (97,000 sq mi),[1] Pilbara IRBA v7 region 178,231.26 km2 (68,815.47 sq mi)[2]
Thickness	up to 20 km (12 mi)
Lithology
Primary	Granite
Other	Greenstone
Location
Region	Western Australia
Country	Australia
Type section
Named for	Pilbara
Named by	See Pilbara#Etymology
Map of Australia with the Pilbara region highlighted in red.

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KEY

Pilbara Craton subregions:

PIL01 -

Chichester

PIL02 -

Fortescue

PIL03 -

Hamersley

PIL04 -

Roebourne

Carnarvon subregion:

CAR01 -

Cape Range

Gascoyne subregion:

GAS01 -

Ashburton

Pilbara Craton part of the continental lithosphere using version 7 of IBRA classification. The geo-ecosystems of the PIL02(Fortescue) area in particular are usually on much younger exposed rock formations (< 1.7 Ga) than the lithology discussed in this article.

The Pilbara Craton is an old and stable part of the continental lithosphere located in the Pilbara region of Western Australia.

The Pilbara Craton is one of only two pristine Archaean 3.8–2.7 Ga (billion years ago) crusts identified on the Earth, along with the Kaapvaal Craton in South Africa. The youngest rocks are 1.7 Ga old in the historic area assigned to the Craton.^[1] Both locations may have once been part of the Vaalbara supercontinent or the continent of Ur.

There are two subregional geographical classification regimes used, being:

1. The Interim Biogeographic Regionalisation for Australia based upon interacting geo-ecosystems
2. Based on geology alone where the eastern continuous oldest portion is called the Eastern Pilbara Craton and younger surface lithologies within the larger craton have different names.

Geology

The most important part of the Pilbara Craton to understand the early Earth crust is called the Eastern Pilbara Craton, where still exposed today, are crustal rocks that are up to 3.8 billion years old and intrusive granitic domes along with greenstone belts that are about 3.5 to 3.2 billion years old.^[1] The geology was reassessed in 2007 with the separation out from the geologically named Pilbara Craton of a thick succession of interbedded clastic or chemical sedimentary rocks and volcanic rocks forming the Fortescue, Hamersley, and Turee Creek basins that are usually aged from 2.78–2.42 billion years old and the younger volcano-sedimentary Ashburton Basin aged from 2.21–1.79 billion years ago.^[1] A surface region between the Fortescue and Hamersley basins is even younger, at less than 1.7 billion years old, as are the surrounding geo-ecosystems surface rocks to the Pilbara Craton. It is important to note that to the east and south of the Eastern Pilbara Craton there are significant outcrops of the very old rocks and that these are confined to the traditional area of the Pilbara Craton which is inferred to be subsurface for more than half its area.^[1]

Mineralogy

There are extensive high quality iron ore deposits and also economic to mine gold, silver, copper, nickel, lead, zinc, molybdenum, vanadium and fluorite deposits.^[1]

Evidence of earliest life

Evidence of the earliest known life on land may have been found in 3.48-billion-year-old geyserite and other related mineral deposits (often found around hot springs and geysers) uncovered in the Dresser Formation in the Pilbara Craton.^[3][4][5] Biogenic sedimentary structures (microbialites) such as stromatolites and MISS were described from tidal, lagoonal and subtidal coastal settings that can be reconstructed from the Dresser stratigraphy as well.^[6] The rocks of the Dresser Formation display evidence of haematite alteration that may have been microbially influenced.^[7]

The earliest direct evidence of life on Earth may be fossils of microorganisms permineralized in 3.465-billion-year-old Australian Apex chert rocks.^[8][9] However, the evidence for the biogenicity of these microstructures has been thoroughly debated.^[10][11] Originally, 11 taxa were described from a deposit thought to be located at the mouth of a river due to certain characteristics like rounded and sorted grains.^[12][13] Extensive field mapping and petrogenetic analysis has since shown the setting for the purported microfossils to be hydrothermal^[14][15] and this is widely supported.^{[16][17][18][19]} Consequently, many alternative abiotic explanations have been proposed for the filamentous microstructures including carbonaceous rims around quartz spherules and rhombs,^[14][15] witherite self-assembled biomorphs^[20] and haematite infilled veinlets.^[21] The carbonaceous matter composing the filaments has also been repeatedly examined with Raman spectroscopy^[14][22][21] which has yielded mixed interpretations of results and is therefore regarded by many to be unreliable for determining biogenicity when used alone.^[23][24] Perhaps the most compelling argument to date is based on high spatial resolution electron microscopy like scanning and transmission electron microscopy.^[19] This study concludes that the nano-scale morphology of the filaments and the distribution of the carbonaceous matter are inconsistent with a biological origin for the filaments. Instead, it is more likely that the hydrothermal conditions have assisted in the heating, hydration and exfoliation of potassium micas on which barium, iron and carbonate have secondarily been adsorbed.

Carbonaceous structures appearing to be of biological origin have also been discovered in the 3.47 billion year-old Mount Ada Basalt, a rock layer that is a few million years older than the Apex chert. However, the biogenicity of these supposed fossils has also been disputed, with some studies finding abiotic processes to be a more likely culprit for their formation.^[11]

Additional potential bioindicators from the Precambrian have been found in the region, including carbonaceous microfossils in the northeastern Pilbara Craton.^[25]