Isua Greenstone Belt

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Isua Greenstone Belt
Nuuk Location.jpg
The general location of the Isua Greenstone belt (Nuuk Region)
Highest point
Elevation5 m (16 ft)
Length35 km (22 mi) [1][2]
Area3,000 km2 (1,200 sq mi)
Orogeny357 million years to form
Age of rockArchean
Type of rocktonalite, mafic rocks, metasedimentary rocks, banded iron formations, granite and granodiorite

The Isua Greenstone Belt is an Archean greenstone belt in southwestern Greenland. The belt is aged between 3.7 and 3.8 billion years.[2] The belt contains variably metamorphosed mafic volcanic and sedimentary rocks. The occurrence of boninitic geochemical signatures, characterized by extreme depletion in trace elements that are not fluid mobile, offers evidence that plate tectonic processes in which lithic crust is melted may have been responsible for the creation of the belt.[1] Another theory posits that the belt formed via a process known as vertical plate tectonics.[3]

In 2016 melting snow revealed putative 3.7-billion-year-old stromatolite fossils, which would be the oldest by several hundred million years thus far discovered on Earth.[4] If confirmed, the discovery of complex stromatolite structures at Isua so early in the history of the Earth would suggest that life first evolved on Earth over 4 billion years ago.[4] There is currently debate over whether the specimens are indeed biogenic, which has been disputed by another research team that visited the site.[5]


The Isua Greenstone Belt, also known as the Isua supracrustal belt since it is composed of supracrustal rock deposited upon basement rock strata, is located in the southwestern portion of Greenland, in the Isukasia terrane,[1] near the Nuuk capital region.[6] The greenstone belt is made up of metamorphosed mafic volcanic and sedimentary rocks that are usually juxtaposed by mylonites or fault boundaries. By using uranium-lead dating on zircon and titanite, the tectonic history was dated to be approximately 3,700–3,600 million years old. The Isua Greenstone has been studied by Earth scientists due to evidence the area holds for early Earth plate tectonics, since it houses one of the oldest, best-preserved ancient plate tectonic sequences.[7] In addition, the area is large, exposed, and there are areas that have experienced relatively low deformation and alteration to the original rock sequences.[2] The Isua Greenstone is divided into a northern and a southern section by the Ivinnguit Fault, shown on the map below right. The northern area of the Isua Greenstone Belt is mainly composed of amphibolite rocks, volcanic rocks, upper mantle peridotite, and layered gabbros; a suite which suggests crustal shortening.[2]

Scientists have used different methods to determine how the Isua Greenstone Belt formed. Some conclude that it formed at an ancient ocean-ocean convergent zone, where subduction-caused partial melting and metasomatism of the mantle as well as the intrusion of tonalites partially melted the overlying supracrustal rocks and created the first continental crust. However, the geological evolution of the Isua Greenstone Belt remains controversial, as scientists try to come to a consensus on how it formed: whether due to such a subduction zone or to some other former process like vertical plate tectonics. Ultimately, a specific conclusion of how the Isua Greenstone Belt formed has not been reached, but some pieces of the puzzle have been proposed.

Scientific methods[edit]

In an attempt to understand the origin of the Isua Greenstone Belt, scientists have used several different methods. These include enlisting U-Pb zircon dating that measures the decay of uranium to lead in zircons using sensitive high-resolution ion microprobe (SHRIMP), analysing elemental chemistry and composition, rendering three-dimensional features on paper using the stereographic projections that geologists call "stereonets", and assessing lithologic associations.[2] In addition to information gathered directly from the rocks, scientists have also used observations of the placement of the rocks and how they are separated into units: this is a more kinematic approach to the area. In addition, zoned garnets from different areas of the Isua Greenstone Belt have been used in garnet-biotite geothermometry, which has been used to determine the timing of metamorphism.[7] Scientists have tried to relate their findings to modern day proxies of subduction zones and other tectonic events.


Map of lithological units that make up the Isua Greenstone Belt. Combined image from Nutman et al., 2007 and T Naerra et al., 2012.[2][8]

Efforts to depict initial lithologies and tectonic formations of the Isua Greenstone Belt have been difficult due to the immense episodes of regional metamorphism the area has experienced,[9] which is why most efforts have been focused on the northern complex, called the Isukasia Terrane,[2] where the rocks have experienced a lower metamorphic grade.[2] There are several lithologies that make up the Isua Greenstone Belt and the main rock types have been located and mapped. These include the Amitsoq Tonalite-Trondhjemite-Granodiorite (TTG) orthogneisses, pillow lavas and pillow breccias, banded iron formations, granodiorites, and metasedimentary rocks. In addition, the area contains other, less prevalent, lithologies such as meta-chert, and mafic volcanic rocks.[10] Although there is still some debate on the kinematics of how each rock type was formed, the map at right shows a part of the Isua Supracrustal belt; these rock types are clues to the formation of the greenstone belt and have been extensively mapped. The map illustrates the entire greenstone belt area, with rock types and locations, found on the southwestern portion of Greenland. Below the map is a general timeline that shows when each rock was intruded into the greenstone belt.[2]

1) Tonalitic Amitsoq orthogneisses:[11]

  • These rocks were most likely formed from the underplate melting of oceanic crust.
  • The protoliths of these rocks were most likely a basalt, komatiite, and chert assemblage, or tonalite.[12]
  • The major deformation event that created the gneiss from tonalite occurred before diorite inclusions, at a time between 3.698 and 3.659 billion years ago.[13]
  • The chemistry of the tonalite-trondhjemite-granodiorite (TTG) show significant indication of being derived from a mix of old crust and younger mantle sources, the product of a hydrated basaltic slab being subducted and then mixed with components of the mantle.[9] After these were melted, they intruded into the overlying basaltic crust.[12]
This is a cartoon image of the types of rocks that were formed and when during the evolution of the Isua Greenstone Belt NOTE: The y-axis does not have a value and placement of the different lithologies along the vertical axis has no importance in this image.[2]

2) Pillow lavas and pillow breccias:

  • The presence of these rocks indicate that there was liquid water available at the time of formation.
  • The pillow lavas are the largest stratigraphic unit in the area (at approximately 6 km2 (2.3 sq mi) and they make up the central portion of the Isua Greenstone Belt.[10] They were tested to see how Ba/La (barium and lanthanum) and Ba/Nb (barium and niobium) isotopes trended when plotted against each other. The samples had very similar results to that of modern basalts. This indicated that there was most likely a sediment cover on the subducting oceanic crust in the Archean.[14]
  • In some areas, mainly in the northern area, the pillow basalts have been completely altered into a garbenschiefer-like amphibolite.[10] However, there is some debate on whether it was formed from an intrusion or a volcanic sediment pile.[10]
  • The pillow breccias found in the Isua Greenstone Belt are interesting in part because of the particular quartz inclusions found in them. there are quartz crystals found that are unstrained, formed before metamorphism and contain fluid inclusions. The fluid inclusions came from two main sources: pure methane and a high saline aqueous fluid. This is further evidence to support that the pillow breccias came from a sea-floor hydrothermal system, approximately 3.75 billion years ago.[10]

3) Banded Iron Formations:

  • Interlayered iron and chert, called Banded Iron Formations (BIFs), are the most common sedimentary rock found in the Isua Greenstone Belt.[15]
  • The BIFs in this area offer a relationship between the rocks and seafloor hydrothermal alteration.[16]
  • The banded iron formations found contain rare-earth elements and positive europium and or negative cerium anomalies. This pattern is coincident with the chemical precipitation of solutions that contained seawater and iron (Fe), an input that most likely came from diverging oceanic plates.[16]

4) Peridotites:

  • Specifically abyssal peridotites were thought to have been found.
  • These are usually found deep within oceanic crust and are brought to the surface of the Earth through obduction.
  • One of the major arguments of scientists for a subduction environment is the presence of an ophiolite sequence.[2]


The Isua Greenstone Belt offers up some complications because of the tectonics that have occurred in the area. Subduction and plate tectonics overall, is a means for explaining heat transfer within the Earth, which was an important process in early Earth.[3] The Isua Greenstone Belt is also an important area on the globe because it in particular contains the only evidence on the Earth that holds record for deformation before 3.2 billion years ago.[3]

Some scientists have observed geometric patterns in the area and have attributed it to a certain type of tectonic event called a thrust nappe.[17] The klippe is the isolated block of the nappe overlying autochthonous material. This geologic formation is evidence of thrusting plate motion, towards the south in this particular region.[17] A thrust suggests that this area did experience subduction in the Archean.[17] The implications of this come from studies of the deformational behavior, rheology, and strength of the Archean crust, all of which has been proposed to be very similar to the current crust.[17]


Evidence from zoned garnets can give insight into the metamorphic history of an area.[7] What one scientist found was that there were three main episodes of garnet growth in the Isua Greenstone Belt, meaning there were three main metamorphic events.[7] Specifically, the garnets were studied in terms of overgrowth patterns using iron-magnesium rich rim, manganese rich cores, then by a calcium-rich rims and cores. In addition, the presence of these overgrowths and their oscillatory zoned nature leads scientists to believe that the metamorphism occurred due to fluid-like metasomatism. Manganese is suggestive of prograde metamorphism.[7] Overall it has been suggested that there were three metamorphic events, occurring 3.74 billion years ago, 3.69 billion years ago, and at 2.8 billion years ago.

Results of several studies[edit]

The following table shows, in a condensed form, the efforts of many scientists and the evidence that they found, as well as their idea of what it could mean for the formation of early Archean continental crust.

What was found What it could mean Why
The presence of peridotite, which is usually found in ophiolite sequences This indicates horizontal movement of plates [3] Ophiolite sequences have to be obducted onto continental crust in order to be observed
The enrichment of LREE and depletion of Ti and Nb in mafic amphibolites found in the Istaq Gneiss Complex [2] The rocks were derived from arc-related basalts [2] Using subduction zone proxy of modern-day plate tectonics, LREEs come from a depleted mantle
Tonalites contain minorquartz-diorites which have high Mg (magnesium) contents Some mantle melt was included within the derivation of rocks[2] Current day proxies with plate tectonics also contain high magnesium quartz-diorites
Zircons were found that formed at temperatures of >900 °C [2] Must have formed from an original source and not from the surrounding country rock Zircons would have been melted had they come from the country, or preexisting, rock
Hafnium isotope evidence shows crustal reworking over 3.2 billion years ago[8] There was a crustal evolutionary period between about 3.9–3.5 billion years ago, which then led a transition period, eventually leading to a modern-day style plate tectonics at approximately 3.2 billion years ago[8] This is evidence of reworking and changing of protolith

Much of this evidence has been used to describe modern day plate tectonics. A problem with this is that Archean plate tectonics could have been vastly different than the processes that are occurring on Earth today.

Proposed origin of continental crust[edit]

This image shows what the likely scenarios were for the formation of tonalites. From Nutman et. all 2007.[2]

The easiest way to think about the Isua Greenstone Belt is in two parts: a north and a south which are broken up by a fault. The northern terrane is dominated by tonalites and is the least metamorphosed section.[18] It also contains zircon ages of approximately 3710-3690 million years old. The southern portion of the Isua Greenstone Belt contains approximately 3900-3810 million year old zircons with an abundance of amphibolite, schist, carbonate rock, volcanics, pillow lavas, and ultramafics.[19] The northern portion makes up the area where many scientific studies have been conducted and offers up the evidence leading scientists to propose the following hypothesis.

Formation of the Isua Greenstone Belt[edit]

A reconstruction of the origin of continental crust, which formed the greenstone belt, using geochemical, lithological, and structural clues,[20] is predicated upon two assumptions: first, new Hadean crust formed laterally by the expelling and lateral accretion of mafic to ultramafic lavas. Then stabilization occurred through the re-melting of the crust.

The reworked crust can be attributed to the burial, most likely through subduction, of hydrated materials, such as basalt, that were formed in the Hadean.[21] Additionally, the source for tested rock samples came from a mantle depleted in titanium and niobium and enriched in lead, strontium, barium, rubidium, and light rare-earth elements, which, taken together, are indicative of arc-related basalts.[2] The diorites found in the area are high in magnesium and REE (rare-earth elements), which suggest further that the rocks were formed from a mixture of the mantle and remelted basaltic crust.[9] Overall, the presence of tonalite-trondhjemite-granodiorites, as well as the iron present for the banded iron formations (BIFs), are determined to have been caused by hydrothermal alteration at high temperatures.[20] BIFs are typically found in intra-oceanic, arc or forearc settings, which are associated with convergent boundaries. The intrusions were formed when upwelling asthenosphere partially melted thick overlying oceanic crust.[20] It is thought that the melting and reworking of oceanic crust formed the early Archean continental crust. In addition, the eclogite residues, formed by the partial melting of the oceanic crust, subsequently became a part of the sub-continental lithospheric mantle. By using uranium-lead dating on zircons, scientists were able to determine that the process of creating the Isua Greenstone Belt took approximately 300 million years.[2]

Many pieces of evidence are brought together to support the theory that the formation of continental crust must have started with the subduction of hot oceanic crust. This subducting slab melted, and the rising magma gravitationally differentiated into a more granitic composition, characteristic of continental crust. The result of testing and putting together information has led scientists to believe that crustal growth began approximately 3.8 billion years ago.[2] and continued building slowly, in a sequence of comparatively brief episodes. Then crust quickly stabilized about 2.975 billion years ago.[16] The schematic image above right shows two possible flat subduction mechanisms that could create the tonalite plutons seen in the greenstone belt.[2] However, this theory of crustal formation has been questioned by many scientists.


In the scientific community, studies are still being conducted that hope to solve the big question of the Isua Greenstone Belt: What processes caused its formation? This area remains under controversy in the scientific community because it is arguable that there were different tectonic processes, or styles, occurring in Archean times that would have affected the outcome of what we see today: a mass of very old rocks surrounded by younger rocks that have been heavily altered in some areas and are separated by tectonic and depositional contacts.[2] The Isua Greenstone Belt is the only place in the world that does not conform entirely to the idea of vertical plate tectonics (an idea that is still debated).

Some of the problems are:

  1. There are few zircons available for dating.
  2. Deformation in the area has destroyed important information.[2]
  3. The isotopic chemistry is known, but is only attributed to current day proxies, which may have been different in the Archean.
  4. There is very little preserved mafic crust from the Archean.[2]

Alternative hypothesis[edit]

Vertical plate tectonics[edit]

There is an alternate idea that early Earth plate tectonics began by vertical movement of the lithosphere, rather than the modern horizontal tectonics. This theory rejects the idea of subduction and arc accretion in the formation of greenstone belts. It suggests that convective overturn due to density differences between the overlying mafic sequence (greenstone) and partially molten granitic middle crust is responsible for the observed formations.[22]

Similar evidence[edit]

The Isua Greenstone Belt is an anomaly in terms of the other greenstone belts in the world. It is the only greenstone belt that has preserved deformational events from greater than 3.2 Ga[2] and contains peridotites (indicating an obducted ophiolite sequence). However, as compared to the Pilbara Craton and the Barberton Greenstone Belts, which have alternate evolution theories, there are a few similarities.[3]

  • The greenstone belts took a period of about 300 million years to form.
  • They contain similar protoliths.[3]
  • Each went through cycles of deformation.
  • They all contain TTG sequences.
  • These TTGs represent similar temperature and pressure conditions of formation (either 1.5 or 3.0 GPa and between 1000 °C and 1200 °C).[3]
  • Contain evidence of low pressure and high temperature generation of tonalite plutons.

Evidence for both situations[edit]

Subduction zone Vertical plate tectonics
The presence of peridotite (which is related to ophiolite sequences) indicates horizontal movement of plates [3] Studies have shown that Archean TTGs are formed primarily through melting of the host rock, meaning it does not indicate subduction-related arc magmatism.[22]
> 3.2 Ga deformation event Similar protoliths as the Pilbara Craton and Barberton Craton
Garnet growths suggest fluid-related metasomatism [7] Low geothermal gradients and low pressure conditions are representative of downward advection in the mantle [3]
Depletions in titanium and niobium and enrichments in lead, strontium, barium, and light rare-earth elements suggest arc-related basalts A decrease in the crustal growth rate approximately 3.2 Ga ago. This would indicate a time when plate tectonics (along with the crustal balance with subduction and convergence) actually began.[3]

Discovery of early life[edit]

Because of its age, the Isua Greenbelt has long been the focus of studies seeking to identify signs of early terrestrial life. In 1996, geologist Steve Mojzsis and colleagues hypothesized that isotopically light carbon in the structure's carbon-rich layers was suggestive of biological activity having occurred there. "Unless some unknown abiotic process exists which is able both to create such isotopically light carbon and then selectively incorporate it into apatite grains, our results provide evidence for the emergence of life on Earth by at least 3,800 Myr before present."[23]

In August 2016, an Australia-based research team presented evidence that the Isua Greenstone Belt contains the remains of stromatolite microbial colonies that formed approximately 3.7 billion years ago.[4][24] However, their interpretations are controversial.[4][5][25] If these structures are stromatolites, they predate the oldest previously known stromatolites, found in the Dresser Formation in western Australia, by 220 million years.[4]

The complexity of the stromatolites found at Isua, if they are indeed stromatolites, suggest that life on Earth was already sophisticated and robust by the time of their formation, and that the earliest life on Earth likely evolved over 4 billion years ago.[4] This conclusion is supported in part by the instability of Earth's surface conditions 3.7 billion years ago, which included intense asteroid bombardment.[26] The possible formation and preservation of fossils from this period indicate that life may have evolved early and prolifically in Earth's history.[26]

The stromatolite fossils appear wavy and dome-shaped, are typically 1–4 cm (0.4–1.6 in) high, and were found in iron- and magnesium-rich dolomites that had recently been exposed by melting snow.[24] The surrounding rocks suggest that the stromatolites may have been deposited in a shallow marine environment.[4] While most rocks in the Isua Greenstone Belt are too metamorphically altered to preserve fossils, the area of stromatolite discovery may have preserved original sedimentary rocks and the fossils inside them.[26] However, some geologists interpret the structures as the result of deformation and alteration of the original rock.[5]

The ISB sedimentary layers containing the possible stromatolites overlay volcanic rocks that are dated to 3.709 billion years old and are capped by dolomite and banded iron formations with thorium-uranium zircons dated to 3.695 ± 0.4 billion years old. All layers, including those bordering the stromatolites, experienced metamorphism and deformation after deposition, and temperatures not exceeding 550 °C (1,000 °F).[4][5]

The identity of the ISB features as stromatolites is controversial, because similar features may form through non-biological processes.[26][5] Some geologists interpret the textures above the putative stromatolites as sand accumulation against their sides during their formation, suggesting that the features arose during the sedimentary process, and not through later, metamorphic deformation.[25][4][26] However, others suggest that the rocks are so altered that any sedimentary interpretations are inappropriate.[5]

In 2016, geologist and areologist Abigail Allwood stated that the discovery of Isua stromatolites makes the emergence of life on other planets, including Mars early after its formation, more probable.[26] However in 2018, she and a team of additional geologists published a paper that raises significant questions as to the origin of the structures, interpreting them as arising from deformation.[5] Thus, the ISB stromatolites remain a subject of ongoing investigation.[24]

See also[edit]


  1. ^ a b c Bennett, Vickie C.; Nutman, Allen P. (April 2014). Isua Supracrustal Belt, West Greenland: Geochronology. Encyclopedia of Scientific Dating Methods. pp. 1–4. doi:10.1007/978-94-007-6326-5_109-1. ISBN 978-94-007-6326-5.
  2. ^ a b c d e f g h i j k l m n o p q r s t u v w x Nutman, Allen P.; Friend, Clark R.L.; Horie, Kenji; Hidaka, Hiroshi (2007). The Itsaq Gneiss Complex of Southern West Greenland and the Construction of Eorarchean Crust at Convergent Plate Boundaries (PDF). Developments in Precambrian Geology. 15. pp. 187–218. doi:10.1016/S0166-2635(07)15033-7. ISBN 9780444528100. Retrieved 3 September 2016.
  3. ^ a b c d e f g h i j Moore, William B.; Webb, Alexander G. (26 September 2013). "Heat-pipe Earth". Nature. 501 (7468): 501–5. Bibcode:2013Natur.501..501M. doi:10.1038/nature12473. PMID 24067709.
  4. ^ a b c d e f g h i Nutman, Allen; Bennett, Vickie; Friend, Clark; Van Kranendonk, Martin; Chivas, Allan (2016). "Rapid emergence of life shown by discovery of 3,700-million-year-old microbial structures". Nature. 537 (7621): 535–538. Bibcode:2016Natur.537..535N. doi:10.1038/nature19355. PMID 27580034.
  5. ^ a b c d e f g Allwood, Abigail C. (2018). "Reassessing evidence of life in 3,700-million-year-old rocks of Greenland". Nature. 563 (7730): 241–244. Bibcode:2018Natur.563..241A. doi:10.1038/s41586-018-0610-4. PMID 30333621.
  6. ^ Bennett, Vickie C.; Nutman, Allen P. (2014). Isua Supracrustal Belt, West Greenland: Geochronology. Australia. p. 1. doi:10.1007/978-94-007-6326-5_109-1. ISBN 978-94-007-6326-5.
  7. ^ a b c d e f Rollinson, Hugh (5 February 2003). "Metamorphic history suggested by garnet-growth chronologies in the Isua Greenstone Belt, West Greenland". Precambrian Research. 126 (3–4): 181–196. Bibcode:2003PreR..126..181R. doi:10.1016/s0301-9268(03)00094-9.
  8. ^ a b c Naerra, T.; Schersten, A.; Rosing, M. T.; Kemp, A. I. S.; Hoffman, J. E.; Kokfelt, T.F.; Whitehouse, M. J. (May 2012). "Hafnium isotope evidence for a transition in the dynamics of continental growth 3.2 Gyr ago". Nature. 485 (7400): 627–630. Bibcode:2012Natur.485..627N. doi:10.1038/nature11140. PMID 22660324.
  9. ^ a b c Hugh, Rollinson. "TTG Genesis and Archaean Crustal Growth". GEMRU. Archived from the original on 2006-05-14.
  10. ^ a b c d e Appel, Peter W.; Rollinson, Hugh R.; Touret, Jacques L.R. (15 November 2001). "Remnants of an Early Archean (>3.75 Ga) sea-floor hydrothermal system in the Isua Greenstone Belt". Precambrian Research. 112 (1–2): 27–49. Bibcode:2001PreR..112...27A. doi:10.1016/s0301-9268(01)00169-3.
  11. ^ Museum of Evolving Earth. "Geology of the Isua supracrustal belt". Tokyo Institute of Technology.
  12. ^ a b Rollinson, Hugh (1999). "TTG Genesis and Archaean Crustal Growth". Journal of Conference Abstracts. 4 (1).
  13. ^ Crowley, J.L; Myers, J.S.; Dunning, G.R. (2002). "Timing and nature of multiple 3700–3600 Ma tectonic events in intrusive rocks north of the Isua greenstone belt, southern West Greenland". Geological Society of America Bulletin. 114 (10): 1311–1325. doi:10.1130/0016-7606(2002)114<1311:tanomm>;2.
  14. ^ Jenner, F.E; Bennett, Vickie E.; Friend, Allen P.; Clark, R.L.; Norman, M.D.; Yaxley, G. (15 April 2009). "Evidence for subduction at 3.8 Ga; geochemistry of arc-like metabasalts from the southern edge of the Isua supracrustal belt". Chemical Geology. 261 (1–2): 82–97. Bibcode:2009ChGeo.261...83J. doi:10.1016/j.chemgeo.2008.09.016.
  15. ^ Fedo, Christopher M.; Myers, John S.; Appel, Peter W. (June 2001). "Depositional setting and paleogeographic implications of Earth's oldest supracrustal rocks, the >3.7 Ga Isua Greenstone belt, West Greenland". Sedimentary Geology. 141–142: 61–77. Bibcode:2001SedG..141...61F. doi:10.1016/s0037-0738(01)00068-9.
  16. ^ a b c Polat, Ali; Frei, Robert (20 April 2005). "The origin of early Archean banded iron formations and of continental crust, Isua, southern West Greenland". 138. Cite journal requires |journal= (help)
  17. ^ a b c d Hanmer, Simon; Greene, David C. (20 April 2000). "A modern structural regime in the Paleoarchean (f3.64 Ga); Isua Greenstone Belt, southern West Greenland". Tectonophysics. 346 (3–4): 201–222. Bibcode:2002Tectp.346..201H. doi:10.1016/s0040-1951(02)00029-x.
  18. ^ Nutman, Allen P.; Friend, Clark R.L.; Paxton, Shane (August 2009). "Detrital zircon sedimentary provenance ages for the Eoarchaean Isua supracrustal belt southern West Greenland; juxtaposition of an imbricated ca. 3700 Ma juvenile arc against an older complex with 3920–3760 Ma components". Precambrian Research. 172 (3–4): 212–233. Bibcode:2009PreR..172..212N. doi:10.1016/j.precamres.2009.03.019.
  19. ^ Appel, Peter W.U; Fedo, Christopher M.; Moorbath, Stephen; Myers, John S. (1998). "Early Archaean Isua supracrustal belt,West Greenland: pilot study of the Isua Multidisciplinary Research Project" (PDF). Geology of Greenland Survey Bulletin. 180: 94–99. Archived from the original (PDF) on 2008-12-07. Retrieved 2014-11-14.
  20. ^ a b c Polat, Ali; Frei, Robert (20 April 2005). "The origin of early Archean banded iron formations and of continental crust, Isua, south Western Greenland". Precambrian Research (138): 151–157. Cite journal requires |journal= (help)
  21. ^ van Kranendonk, Martin J.; Smithies, Hugh R.H.; Bennett, Vickie (26 October 2007). Earth's Oldest Rocks. Amsterdam, The Netherlands: Elsevier. ISBN 978-0-444-52810-0.
  22. ^ a b Van Kranendonk, Martin J. (2011). "Cool greenstone drips and the role of partial convective overturn in Barberton greenstone belt evolution". Journal of African Earth Sciences. 60 (5): 346–352. Bibcode:2011JAfES..60..346V. doi:10.1016/j.jafrearsci.2011.03.012.
  23. ^ Mojzsis SJ, Arrhenius G, McKeegan KD, Harrison TM, Nutman AP, Friend CR (1996). "Evidence for life on Earth before 3,800 million years ago". Nature. 384 (6604): 55–59. Bibcode:1996Natur.384...55M. doi:10.1038/384055a0. hdl:2060/19980037618. PMID 8900275.CS1 maint: uses authors parameter (link)
  24. ^ a b c Pease, Roland (31 August 2016). "Wavy Greenland rock features 'are oldest fossils'". BBC. Retrieved 31 August 2016.
  25. ^ a b Nutman, Allen P.; Bennett, Vickie C.; Friend, Clark R. L.; Van Kranendonk, Martin J.; Rothacker, Leo; Chivas, Allan R. (2019-09-01). "Cross-examining Earth's oldest stromatolites: Seeing through the effects of heterogeneous deformation, metamorphism and metasomatism affecting Isua (Greenland) ∼3700 Ma sedimentary rocks". Precambrian Research. 331: 105347. doi:10.1016/j.precamres.2019.105347. ISSN 0301-9268.
  26. ^ a b c d e f Allwood, Abigail (31 August 2016). "Geology: Evidence of life in Earth's oldest rocks". News and Views. Nature.