View source for Earth:Great Oxidation Event

{{short description|Paleoproterozoic surge in atmospheric oxygen}}
[[File:Precambrian Evolution of Life.png|thumb|Timescale]]
[[Image:Oxygenation-atm-2.svg|thumb|upright=2|O<sub>2</sub> build-up in the [[Earth's atmosphere]]. Red and green lines represent the range of the estimates while time is measured in billions of years ago (Ga).

{{unbulleted list
| Stage 1 (3.85–2.45 Ga): Practically no O<sub>2</sub> in the atmosphere. The oceans were also largely anoxic – with the possible exception of O<sub>2</sub> in the shallow oceans.
| Stage 2 (2.45–1.85 Ga): O<sub>2</sub> produced, rising to values of 0.02 and 0.04 atm, but absorbed in oceans and seabed rock.
| Stage 3 (1.85–0.85 Ga): O<sub>2</sub> starts to [[Physics:Outgassing|gas out]] of the oceans, but is absorbed by land surfaces. No significant change in oxygen level.
| Stages 4 and 5 (0.85 Ga – present): Other O<sub>2</sub> reservoirs filled; gas accumulates in atmosphere.<ref>{{cite journal |author= Holland, Heinrich D. |title=The oxygenation of the atmosphere and oceans |journal=Philosophical Transactions of the Royal Society: Biological Sciences |volume=361 |date=19 May 2006 |issue=1470 |pages=903–915 |doi=10.1098/rstb.2006.1838 |pmid=16754606 |pmc=1578726 }}</ref>
}}]]

The '''Great Oxidation Event''' ('''GOE''') or '''Great Oxygenation Event''', also called the '''Oxygen Catastrophe''', '''Oxygen Revolution''', '''Oxygen Crisis''' or '''Oxygen Holocaust''',<ref>
{{cite book 
|first1=Lynn
|last1=Margulis
|first2=Dorion
|last2=Sagan
|title=Microcosmos: Four Billion Years of Microbial Evolution
|year=1986
|publisher=University of California Press
|location=California
|chapter=Chapter 6, "The Oxygen Holocaust"
|page=99
|isbn=9780520210646
|chapter-url=https://books.google.com/books?id=eo_sMMRxgAUC&dq=oxygen+holocaust&pg=PA99
}}</ref> was a time interval during the [[Earth:Early Earth|Early Earth]]'s [[Earth:Paleoproterozoic|Paleoproterozoic]] era when the [[Earth:Atmosphere of Earth|Earth's atmosphere]] and the shallow ocean first experienced a rise in the concentration of [[Chemistry:Oxygen|oxygen]].<ref name="Lyons 307–315">{{Cite journal |last1=Lyons |first1=Timothy W. |last2=Reinhard |first2= Christopher T. |last3= Planavsky |first3= Noah J. |date=February 2014 |title=The rise of oxygen in Earth's early ocean and atmosphere |journal=Nature |volume=506 |issue=7488 |pages=307–315 |doi= 10.1038/nature13068 |pmid=24553238 |bibcode=2014Natur.506..307L |s2cid=4443958 }}</ref> This began approximately 2.460–2.426&nbsp;Ga (billion years) ago during the [[Earth:Siderian|Siderian]] period and ended approximately 2.060&nbsp;Ga ago during the [[Earth:Rhyacian|Rhyacian]].<ref name="GumsleyEtAl2017PNAS">{{cite journal |last1=Gumsley |first1=Ashley P. |last2=Chamberlain |first2=Kevin R. |last3=Bleeker |first3=Wouter |last4=Söderlund |first4=Ulf |last5=De Kock |first5=Michiel O. |last6=Larsson |first6=Emilie R. |last7=Bekker |first7=Andrey |date=6 February 2017 |title=Timing and tempo of the Great Oxidation Event |journal=Proceedings of the National Academy of Sciences of the United States of America |volume=114 |issue=8 |pages=1811–1816 |language=en |doi=10.1073/pnas.1608824114 |issn=0027-8424 |pmc=5338422 |pmid=28167763 |doi-access=free }}</ref> Geological, [[Physics:Isotope|isotopic]], and chemical evidence suggests that biologically produced molecular oxygen ([[Chemistry:Oxygen#Allotropes|dioxygen]] or O<sub>2</sub>) started to accumulate in Earth's atmosphere and changed it from a weakly [[Astronomy:Reducing atmosphere|reducing atmosphere]] practically devoid of oxygen into an [[Chemistry:Redox|oxidizing]] one containing abundant free oxygen,<ref>{{cite book |last1=Sosa Torres |first1=Martha E. |last2=Saucedo-Vázquez |first2=Juan P. |last3=Kroneck |first3=Peter M.H. |title=Sustaining Life on Planet Earth: Metalloenzymes Mastering Dioxygen and Other Chewy Gases |chapter=The Magic of Dioxygen |publisher=Springer |year=2015 |isbn= 978-3-319-12414-8 |editor1=Kroneck, Peter M.H. |editor2=Sosa Torres, Martha E. |series=Metal Ions in Life Sciences volume 15 |pages= 1–12 |volume=15 |doi=10.1007/978-3-319-12415-5_1 |pmid=25707464}}</ref> with oxygen levels being as high as 10% of their present atmospheric level by the end of the GOE.<ref>{{cite journal |last1=Ossa Ossa |first1=Frantz |last2=Spangenberg |first2=Jorge E. |last3=Bekker |first3=Andrey |last4=König |first4=Stephan |last5=Stüeken |first5=Eva E. |last6=Hofmann |first6=Axel |last7=Poulton |first7=Simon W. |last8=Yierpan |first8=Aierken |last9=Varas-Reus |first9=Maria I. |last10=Eickmann |first10=Benjamin |last11=Andersen |first11=Morten B. |last12=Schoenberg |first12=Ronny |date=15 September 2022 |title=Moderate levels of oxygenation during the late stage of Earth's Great Oxidation Event |journal=[[Earth:Earth and Planetary Science Letters|Earth and Planetary Science Letters]] |volume=594 |page=117716 |doi=10.1016/j.epsl.2022.117716 |hdl=10481/78482 |doi-access=free |hdl-access=free }}</ref>

The sudden injection of highly reactive free oxygen, toxic to the then-mostly anaerobic biosphere, may have caused the extinction of many organisms on Earth—mostly [[Biology:Archaea|archaea]]l [[Biology:Colony|colonies]] that used [[Chemistry:Retinal|retinal]] to utilize green-spectrum light energy and power a form of [[Biology:Anoxygenic photosynthesis|anoxygenic photosynthesis]] (see [[Earth:Purple Earth hypothesis|Purple Earth hypothesis]]). Although the event is inferred to have constituted a mass extinction,<ref>{{cite news |last1=Plait |first1=Phil |title=Poisoned Planet |url=https://slate.com/technology/2014/07/the-great-oxygenation-event-the-earths-first-mass-extinction.html |access-date=8 July 2019 |work=Slate |date=28 July 2014}}</ref> due in part to the great difficulty in surveying microscopic organisms' abundances, and in part to the extreme age of fossil remains from that time, the Great Oxidation Event is typically not counted among conventional lists of "[[Biology:Extinction event|great extinctions]]", which are implicitly limited to the [[Earth:Phanerozoic|Phanerozoic]] eon. In any case, [[Chemistry:Isotope geochemistry|isotope geochemistry]] data from [[Chemistry:Sulfate mineral|sulfate mineral]]s have been interpreted to indicate a decrease in the size of the [[Biology:Biosphere|biosphere]] of >80% associated with changes in [[Earth:Nutrient|nutrient]] supplies at the end of the GOE.<ref>{{Cite journal |last1=Hodgskiss |first1=Malcolm S. W. |last2=Crockford |first2=Peter W. |last3=Peng |first3=Yongbo |last4=Wing |first4=Boswell A. |last5=Horner |first5=Tristan J. |date=2019-08-27 |title=A productivity collapse to end Earth's Great Oxidation |journal=Proceedings of the National Academy of Sciences of the United States of America |language=en |volume=116 |issue=35 |pages=17207–17212 |doi=10.1073/pnas.1900325116 |issn=0027-8424 |pmc=6717284 |pmid=31405980|doi-access=free }}</ref>

The GOE is inferred to have been caused by [[Biology:Cyanobacteria|cyanobacteria]] that evolved [[Biology:Porphyrin|porphyrin]]-based [[Earth:Photosynthesis|photosynthesis]], which produces dioxygen as a byproduct. The increasing oxygen level eventually depleted the reducing capacity of [[Chemistry:Ferrous|ferrous]] compounds, [[Chemistry:Hydrogen sulfide|hydrogen sulfide]] and [[Earth:Atmospheric methane|atmospheric methane]], and compounded by [[Earth:Huronian glaciation|a global glaciation]], devastated the [[Biology:Microbial mat|microbial mat]]s around the Earth's surface. The subsequent adaptation of surviving archaea via [[Biology:Symbiogenesis|symbiogenesis]] with aerobic [[Biology:Proteobacteria|proteobacteria]] (which went [[Biology:Endosymbiont|endosymbiont]] and became [[Biology:Mitochondria|mitochondria]]) may have led to the rise of [[Biology:Eukaryote|eukaryotic]] organisms and the subsequent [[Biology:Evolution|evolution]] of multicellular life-forms.<ref>{{cite journal |last1= Schirrmeister |first1= Bettina E. |last2= de Vos |first2=Jurriaan M. |last3=Antonelli |first3=Alexandre |last4=Bagheri |first4=Homayoun C. |title= Evolution of multicellularity coincided with increased diversification of cyanobacteria and the Great Oxidation Event |journal=Proceedings of the National Academy of Sciences of the United States of America |date=29 January 2013 |volume=110 |issue= 5 |pages=1791–1796 |doi=10.1073/pnas.1209927110 |pmid=23319632 |pmc=3562814 |bibcode= 2013PNAS..110.1791S |doi-access= free}}
* {{cite press release |date=17 January 2013 |title=Great Oxidation Event: More oxygen through multicellularity |website=ScienceDaily |url=https://www.sciencedaily.com/releases/2013/01/130117084856.htm}}</ref><ref>{{Cite journal |last=Crockford |first=Peter W. |last2=Kunzmann |first2=Marcus |last3=Bekker |first3=Andrey |last4=Hayles |first4=Justin |last5=Bao |first5=Huiming |last6=Halverson |first6=Galen P. |last7=Peng |first7=Yongbo |last8=Bui |first8=Thi H. |last9=Cox |first9=Grant M. |last10=Gibson |first10=Timothy M. |last11=Wörndle |first11=Sarah |last12=Rainbird |first12=Robert |last13=Lepland |first13=Aivo |last14=Swanson-Hysell |first14=Nicholas L. |last15=Master |first15=Sharad |date=2019-05-20 |title=Claypool continued: Extending the isotopic record of sedimentary sulfate |url=https://www.sciencedirect.com/science/article/pii/S0009254119300804 |journal=Chemical Geology |volume=513 |pages=200–225 |doi=10.1016/j.chemgeo.2019.02.030 |issn=0009-2541}}</ref><ref>{{Cite journal |last=Crockford |first=Peter W. |last2=Bar On |first2=Yinon M. |last3=Ward |first3=Luce M. |last4=Milo |first4=Ron |last5=Halevy |first5=Itay |date=November 2023 |title=The geologic history of primary productivity |url=https://linkinghub.elsevier.com/retrieve/pii/S0960982223012861 |journal=Current Biology |language=en |volume=33 |issue=21 |pages=4741–4750.e5 |doi=10.1016/j.cub.2023.09.040}}</ref>

== Early atmosphere ==
{{Main|Earth:Paleoatmosphere}}

The composition of the [[Earth:Atmosphere of Earth#History of Earth's atmosphere|Earth's earliest atmosphere]] is not known with certainty. However, the bulk was likely [[Chemistry:Nitrogen|nitrogen]], {{chem2|N2}}, and [[Chemistry:Carbon dioxide|carbon dioxide]], {{chem2|CO2}}, which are also the predominant nitrogen-and-carbon-bearing gases produced by volcanism today. These are relatively inert gases. Oxygen, {{chem2|O2}}, meanwhile, was present in the atmosphere at just 0.001% of its present atmospheric level.<ref>{{cite journal |last1=Pavlov |first1=A. A. |last2=Kasting |first2=J. F. |date=5 July 2004 |title=Mass-Independent Fractionation of Sulfur Isotopes in Archean Sediments: Strong Evidence for an Anoxic Archean Atmosphere |url=https://www.liebertpub.com/doi/abs/10.1089/153110702753621321 |journal= Astrobiology|volume=2 |issue=1 |pages=27–41 |doi=10.1089/153110702753621321 |pmid=12449853 |access-date=25 September 2022}}</ref><ref>{{cite journal |last1=Zhang |first1=Shuichang |last2=Wang |first2=Xiaomei |last3=Wang |first3=Huajian |last4=Bjerrum |first4=Christian J. |last5=Hammarlund |first5=Emma U. |last6=Costa |first6=M. Mafalda |last7=Connelly |first7=James N. |last8=Zhang |first8=Baomin |last9=Su |first9=Jin |last10=Canfield |first10=Donald E. |date=4 January 2016 |title=Sufficient oxygen for animal respiration 1,400 million years ago |url=https://www.researchgate.net/publication/289365657 |journal=Proceedings of the National Academy of Sciences of the United States of America |volume=113 |issue=7 |pages=1731–1736 |doi=10.1073/pnas.1523449113 |pmid=26729865 |pmc=4763753 |bibcode=2016PNAS..113.1731Z |doi-access=free |access-date=13 August 2023}}</ref> The Sun shone at about 70% of its current brightness 4 billion years ago, but there is strong evidence that liquid water existed on Earth at the time. A warm Earth, in spite of a faint Sun, is known as the [[Faint young Sun paradox|faint young Sun paradox]].<ref name="kastings-1993">{{cite journal |last1=Kasting |first1=J. |title=Earth's early atmosphere |journal=Science |date=12 February 1993 |volume=259 |issue=5097 |pages=920–926 |doi=10.1126/science.11536547 |pmid=11536547 |s2cid=21134564 }}</ref> Either {{chem2|CO2}} levels were much higher at the time, providing enough of a [[Earth:Greenhouse effect|greenhouse effect]] to warm the Earth, or other [[Chemistry:Greenhouse gas|greenhouse gas]]es were present. The most likely such gas is [[Chemistry:Methane|methane]], {{chem2|CH4}}, which is a powerful greenhouse gas and was produced by early forms of life known as methanogens. Scientists continue to research how the Earth was warmed before life arose.<ref name="shaw-2998">{{cite journal |last1=Shaw |first1=George H. |title=Earth's atmosphere – Hadean to early Proterozoic |journal=Geochemistry |date=August 2008 |volume=68 |issue=3 |pages=235–264 |doi=10.1016/j.chemer.2008.05.001 |bibcode=2008ChEG...68..235S }}</ref>

An atmosphere of {{chem2|N2}} and {{chem2|CO2}} with trace amounts of {{chem2|H2O}}, {{chem2|CH4}}, [[Chemistry:Carbon monoxide|carbon monoxide]] ({{chem2|CO}}), and [[Chemistry:Hydrogen|hydrogen]] ({{chem2|H2}}) is described as a weakly [[Astronomy:Reducing atmosphere|reducing atmosphere]].<ref name="Kasting 2014 pp. 157–175">{{cite book|last=Kasting|first=J.F.|title=Treatise on Geochemistry|chapter=Modeling the Archean Atmosphere and Climate|publisher=Elsevier|year=2014|doi=10.1016/b978-0-08-095975-7.01306-1|pages=157–175|isbn=9780080983004}}</ref> Such an atmosphere contains practically no oxygen. The modern atmosphere contains abundant oxygen (nearly 21%), making it an oxidizing atmosphere.<ref name="weichert-2002">{{cite journal |last1=Wiechert |first1=U. H. |title=GEOLOGY: Earth's Early Atmosphere |journal=Science |date=20 December 2002 |volume=298 |issue=5602 |pages=2341–2342 |doi=10.1126/science.1079894|pmid=12493902 |s2cid=128858098 }}</ref> The rise in oxygen is attributed to [[Earth:Photosynthesis|photosynthesis]] by [[Biology:Cyanobacteria|cyanobacteria]], which are thought to have evolved as early as 3.5 billion years ago.<ref>{{cite journal |last1=Baumgartner |first1=Raphael J. |last2=Van Kranendonk |first2=Martin J. |last3=Wacey |first3=David |last4=Fiorentini |first4=Marco L. |last5=Saunders |first5=Martin |last6=Caruso |first6=Stefano |last7=Pages |first7=Anais |last8=Homann |first8=Martin |last9=Guagliardo |first9=Paul |title=Nano−porous pyrite and organic matter in 3.5-billion-year-old stromatolites record primordial life |journal=Geology |date=2019-11-01 |volume=47 |issue=11 |pages=1039–1043 |doi=10.1130/G46365.1 |bibcode=2019Geo....47.1039B |s2cid=204258554 |url=https://discovery.ucl.ac.uk/id/eprint/10087275/1/Baumgartner%20et%20al%202019%20accepted.pdf }}</ref>

The current scientific understanding of when and how the Earth's atmosphere changed from a weakly reducing to a strongly oxidizing atmosphere largely began with the work of the American geologist Preston Cloud in the 1970s.<ref name="kastings-1993"/> Cloud observed that [[Earth:Detritus (geology)|detrital]] sediments older than about 2 billion years contained grains of [[Chemistry:Pyrite|pyrite]], [[Chemistry:Uraninite|uraninite]],<ref name="kastings-1993"/> and [[Chemistry:Siderite|siderite]],<ref name="weichert-2002"/> all minerals containing reduced forms of iron or uranium that are not found in younger sediments because they are rapidly oxidized in an oxidizing atmosphere. He further observed that continental [[Earth:Red beds|red beds]], which get their color from the oxidized ([[Chemistry:Iron(III)|ferric]]) mineral [[Chemistry:Hematite|hematite]], began to appear in the geological record at about this time. [[Earth:Banded iron formation|Banded iron formation]] largely disappears from the geological record at 1.85 Ga, after peaking at about 2.5 Ga.<ref name="trendall-2002">{{cite book |doi=10.1002/9781444304312.ch3 |chapter=The Significance of Iron-Formation in the Precambrian Stratigraphic Record |title=Precambrian Sedimentary Environments |year=2002 |last1=Trendall |first1=A. F. |pages=33–66 |isbn=978-1-4443-0431-2 }}</ref> Banded iron formation can form only when abundant dissolved [[Chemistry:Ferrous|ferrous]] iron is transported into [[Earth:Depositional environment|depositional basins]], and an oxygenated ocean blocks such transport by oxidizing the iron to form insoluble ferric iron compounds.<ref name="Cox et al 2013">{{cite journal |last1=Cox |first1=Grant M. |last2=Halverson |first2=Galen P. |last3=Minarik |first3=William G. |last4=Le Heron |first4=Daniel P. |last5=Macdonald |first5=Francis A. |last6=Bellefroid |first6=Eric J. |last7=Strauss |first7=Justin V. |title=Neoproterozoic iron formation: An evaluation of its temporal, environmental and tectonic significance |journal=Chemical Geology |date=December 2013 |volume=362 |pages=232–249 |doi=10.1016/j.chemgeo.2013.08.002 |bibcode=2013ChGeo.362..232C |s2cid=56300363 |url=http://nrs.harvard.edu/urn-3:HUL.InstRepos:33717509 }}</ref> The end of the deposition of banded iron formation at 1.85 Ga is therefore interpreted as marking the oxygenation of the deep ocean.<ref name="kastings-1993"/> Heinrich Holland further elaborated these ideas through the 1980s, placing the main time interval of oxygenation between 2.2 and 1.9 Ga.<ref name="shaw-2998"/>

Constraining the onset of atmospheric oxygenation has proven particularly challenging for geologists and geochemists. While there is a widespread consensus that initial oxygenation of the atmosphere happened sometime during the first half of the [[Earth:Paleoproterozoic|Paleoproterozoic]], there is disagreement on the exact timing of this event. Scientific publications between 2016 and 2022 have differed in the inferred timing of the onset of atmospheric oxygenation by approximately 500 million years; estimates of 2.7 Ga,<ref>{{cite journal |last1=Large |first1=Ross R. |last2=Hazen |first2=Robert M. |last3=Morrison |first3=Shaunna M. |last4=Gregory |first4=Dan D. |last5=Steadman |first5=Jeffrey A. |last6=Mukherjee |first6=Indrani |date=May 2022 |title=Evidence that the GOE was a prolonged event with a peak around 1900 Ma |journal=Geosystems and Geoenvironment |volume=1 |issue=2 |page=100036 |doi=10.1016/j.geogeo.2022.100036 |doi-access=free }}</ref> 2.501-2.434 Ga<ref>{{Cite journal |last1=Warke |first1=Matthew R. |last2=Di Rocco |first2=Tommaso |last3=Zerkle |first3=Aubrey L. |last4=Lepland |first4=Aivo |last5=Prave |first5=Anthony R. |last6=Martin |first6=Adam P. |last7=Ueno |first7=Yuichiro |last8=Condon |first8=Daniel J. |last9=Claire |first9=Mark W. |date=16 June 2020 |title=The Great Oxidation Event preceded a Paleoproterozoic "snowball Earth" |journal=Proceedings of the National Academy of Sciences of the United States of America |language=en |volume=117 |issue=24 |pages=13314–13320 |doi=10.1073/pnas.2003090117 |issn=0027-8424 |pmc=7306805 |pmid=32482849|doi-access=free }}</ref> 2.501-2.225 Ga,<ref name="Hodgskiss-2021">{{Cite journal |last1=Hodgskiss |first1=Malcolm S.W. |last2=Sperling |first2=Erik A. |date=20 October 2021 |title=A prolonged, two-step oxygenation of Earth's early atmosphere: Support from confidence intervals |url=https://doi.org/10.1130/G49385.1 |journal=Geology |volume=50 |issue=2 |pages=158–162 |doi=10.1130/g49385.1 |s2cid=244621056 |issn=0091-7613}}</ref> 2.460-2.426 Ga,<ref name="GumsleyEtAl2017PNAS" /> 2.430 Ga,<ref>{{Cite journal |last1=Poulton |first1=Simon W. |last2=Bekker |first2=Andrey |last3=Cumming |first3=Vivien M. |last4=Zerkle |first4=Aubrey L. |last5=Canfield |first5=Donald E. |last6=Johnston |first6=David T. |date=April 2021 |title=A 200-million-year delay in permanent atmospheric oxygenation |url=https://www.nature.com/articles/s41586-021-03393-7 |journal=Nature |language=en |volume=592 |issue=7853 |pages=232–236 |doi=10.1038/s41586-021-03393-7 |pmid=33782617 |s2cid=232419035 |issn=1476-4687|hdl=10023/24041 |hdl-access=free }}</ref> and 2.33 Ga have been given.<ref>{{Cite journal |last1=Luo |first1=Genming |last2=Ono |first2=Shuhei |last3=Beukes |first3=Nicolas J. |last4=Wang |first4=David T. |last5=Xie |first5=Shucheng |last6=Summons |first6=Roger E. |date=2016-05-06 |title=Rapid oxygenation of Earth's atmosphere 2.33 billion years ago |journal=Science Advances |language=en |volume=2 |issue=5 |pages=e1600134 |doi=10.1126/sciadv.1600134 |issn=2375-2548 |pmc=4928975 |pmid=27386544}}</ref> Factors limiting calculations include an incomplete [[Earth:Geologic record|sedimentary record]] for the Paleoproterozoic (e.g., because of [[Earth:Subduction|subduction]] and [[Earth:Metamorphism|metamorphism]]), uncertainties in [[Physics:Radiometric dating|depositional ages]] for many ancient [[Earth:Sedimentary rock|sedimentary units]], and uncertainties related to the interpretation of different geological/geochemical [[Chemistry:Isotope geochemistry|proxies]]. While the effects of an incomplete geological record have been discussed and quantified in the field of [[Biology:Paleontology|paleontology]] for several decades, particularly with respect to the evolution and extinction of organisms (the Signor–Lipps effect), this is rarely quantified when considering geochemical records and may therefore lead to uncertainties for scientists studying the timing of atmospheric oxygenation.<ref name="Hodgskiss-2021" />

== Geological evidence ==
Evidence for the Great Oxidation Event is provided by a variety of petrological and geochemical markers that define this [[Earth:Geological event|geological event]].

=== Continental indicators ===
[[Earth:Paleosol|Paleosol]]s, detrital grains, and red beds are evidence of low oxygen levels.<ref name="Catling-2017"/> Paleosols (fossil soils) older than 2.4&nbsp;billion years old have low iron concentrations that suggest anoxic [[Earth:Weathering|weathering]].<ref>{{cite journal |last1=Utsunomiya |first1=Satoshi |last2=Murakami |first2=Takashi |last3=Nakada |first3=Masami |last4=Kasama |first4=Takeshi |date=January 2003 |title=Iron oxidation state of a 2.45&nbsp;Byr-old paleosol developed on mafic volcanics |journal=Geochimica et Cosmochimica Acta |volume=67 |issue=2 |pages=213–221 |doi=10.1016/s0016-7037(02)01083-9 |bibcode=2003GeCoA..67..213U}}</ref> Detrital grains composed of pyrite, siderite, and uraninite (redox-sensitive detrital minerals) are found in sediments older than ca. 2.4&nbsp;Ga.<ref name="Johnson-2014">{{Cite journal |last1=Johnson |first1=Jena E. |last2=Gerpheide |first2=Aya |last3=Lamb |first3=Michael P. |last4=Fischer |first4=Woodward W. |date=27 February 2014 |title=O<sub>2</sub>constraints from Paleoproterozoic detrital pyrite and uraninite |url=https://doi.org/10.1130/B30949.1 |journal=Geological Society of America Bulletin |volume=126 |issue=5–6 |pages=813–830 |doi=10.1130/b30949.1 |issn=0016-7606}}</ref> These minerals are only stable under low oxygen conditions, and so their occurrence as detrital minerals in [[Earth:Fluvial sediment processes|fluvial]] and deltaic sediments are widely interpreted as evidence of an anoxic atmosphere.<ref name="Johnson-2014" /><ref>{{Cite journal |last1=Hofmann |first1=Axel |last2=Bekker |first2=Andrey |last3=Rouxel |first3=Olivier |last4=Rumble |first4=Doug |last5=Master |first5=Sharad |date=September 2009 |title=Multiple sulphur and iron isotope composition of detrital pyrite in Archaean sedimentary rocks: A new tool for provenance analysis |journal=[[Earth:Earth and Planetary Science Letters|Earth and Planetary Science Letters]] |volume=286 |issue=3–4 |pages=436–445 |doi=10.1016/j.epsl.2009.07.008 |bibcode=2009E&PSL.286..436H |hdl=1912/3068 |hdl-access=free }}</ref> In contrast to redox-sensitive detrital minerals are red beds, red-colored [[Earth:Sandstone|sandstone]]s that are coated with hematite. The occurrence of red beds indicates that there was sufficient oxygen to oxidize iron to its ferric state, and these represent a marked contrast to sandstones deposited under anoxic conditions which are often beige, white, grey, or green.<ref>{{cite journal |last1=Eriksson |first1=Patrick G. |last2=Cheney |first2=Eric S. |date=January 1992 |title=Evidence for the transition to an oxygen-rich atmosphere during the evolution of red beds in the lower proterozoic sequences of southern Africa |journal=Precambrian Research |volume=54 |issue=2–4 |pages=257–269 |doi=10.1016/0301-9268(92)90073-w |bibcode=1992PreR...54..257E }}</ref>

=== Banded iron formation ===
[[Earth:Banded iron formation|Banded iron formations]] are composed of thin alternating layers of [[Earth:Chert|chert]] (a fine-grained form of [[Chemistry:Silicon dioxide|silica]]) and iron oxides ([[Chemistry:Magnetite|magnetite]] and hematite). Extensive deposits of this rock type are found around the world, almost all of which are more than 1.85 billion years old and most of which were deposited around 2.5 Ga. The iron in banded iron formations is partially oxidized, with roughly equal amounts of ferrous and ferric iron.<ref name="trendall-blockley-2004">{{cite encyclopedia |chapter=Precambrian iron-formation |first1=A.F. |last1=Trendall |first2=J.G. |last2=Blockley |title=Evolution of the Hydrosphere and Atmosphere |editor1-first=P.G. |editor1-last=Eriksson |editor2-first=W. |editor2-last=Altermann |editor3-first=D.R. |editor3-last=Nelson |editor4-first=W.U. |editor4-last=Mueller |editor5-first=O. |editor5-last=Catuneanu |encyclopedia=Developments in Precambrian Geology |series=Developments in Precambrian Geology |volume=12 |year=2004 |pages=359–511 |doi=10.1016/S0166-2635(04)80007-0 |isbn=978-0-444-51506-3 }}</ref> Deposition of a banded iron formation requires both an anoxic deep ocean capable of transporting iron in soluble ferrous form, and an oxidized shallow ocean where the ferrous iron is oxidized to insoluble ferric iron and precipitates onto the ocean floor.<ref name="Cox et al 2013"/> The deposition of banded iron formations before 1.8 Ga suggests the ocean was in a persistent ferruginous state, but deposition was episodic and there may have been significant intervals of [[Earth:Euxinia|euxinia]].<ref name="Canfield-2011">{{cite journal |last1=Canfield |first1=Donald E. |last2=Poulton |first2=Simon W. |date=2011-04-01 |title=Ferruginous Conditions: A Dominant Feature of the Ocean through Earth's History |journal=Elements |volume=7 |issue=2 |pages=107–112 |doi=10.2113/gselements.7.2.107 }}</ref> The transition from deposition of banded iron formations to manganese oxides in some strata has been considered a key tipping point in the timing of the GOE because it is believed to indicate the escape of significant molecular oxygen into the atmosphere in the absence of ferrous iron as a reducing agent.<ref>{{cite journal |last1=Lantink |first1=Margriet L. |last2=Oonk |first2=Paul B. H. |last3=Floor |first3=Geerke H. |last4=Tsikos |first4=Harilaos |last5=Mason |first5=Paul R. D. |date=February 2018 |title=Fe isotopes of a 2.4 Ga hematite-rich IF constrain marine redox conditions around the GOE |url=https://www.sciencedirect.com/science/article/abs/pii/S0301926817303273 |journal=Precambrian Research |volume=305 |pages=218–235 |doi=10.1016/j.precamres.2017.12.025 |access-date=29 December 2022}}</ref>

=== Iron speciation ===
Black laminated [[Chemistry:Shale|shale]]s, rich in organic matter, are often regarded as a marker for [[Earth:Anoxic waters|anoxic]] conditions. However, the deposition of abundant organic matter is not a sure indication of anoxia, and burrowing organisms that destroy [[Earth:Lamination (geology)|lamination]] had not yet evolved during the time frame of the Great Oxygenation Event. Thus laminated black shale by itself is a poor indicator of oxygen levels. Scientists must look instead for geochemical evidence of anoxic conditions. These include ferruginous anoxia, in which dissolved ferrous iron is abundant, and euxinia, in which [[Chemistry:Hydrogen sulfide|hydrogen sulfide]] is present in the water.<ref name=tracking-euxenia>{{cite journal |last1=Lyons |first1=Timothy W. |last2=Anbar |first2=Ariel D. |last3=Severmann |first3=Silke |last4=Scott |first4=Clint |last5=Gill |first5=Benjamin C. |date=May 2009 |title=Tracking Euxinia in the Ancient Ocean: A Multiproxy Perspective and Proterozoic Case Study |journal=[[Earth:Annual Review of Earth and Planetary Sciences|Annual Review of Earth and Planetary Sciences]] |volume=37 |issue=1 |pages=507–534 |doi=10.1146/annurev.earth.36.031207.124233 |bibcode=2009AREPS..37..507L }}</ref>

Examples of such indicators of anoxic conditions include the degree of pyritization (DOP), which is the ratio of iron present as pyrite to the total reactive iron. Reactive iron, in turn, is defined as iron found in oxides and oxyhydroxides, carbonates, and reduced sulfur minerals such as pyrites, in contrast with iron tightly bound in silicate minerals.<ref>{{cite journal |last1=Scholz |first1=Florian |last2=Severmann |first2=Silke |last3=McManus |first3=James |last4=Noffke |first4=Anna |last5=Lomnitz |first5=Ulrike |last6=Hensen |first6=Christian |title=On the isotope composition of reactive iron in marine sediments: Redox shuttle versus early diagenesis |journal=[[Chemistry:Chemical Geology|Chemical Geology]] |date=December 2014 |volume=389 |pages=48–59 |doi=10.1016/j.chemgeo.2014.09.009|bibcode=2014ChGeo.389...48S }}</ref> A DOP near zero indicates oxidizing conditions, while a DOP near 1 indicates euxinic conditions. Values of 0.3 to 0.5 are transitional, suggesting anoxic bottom mud under an oxygenated ocean. Studies of the Black Sea, which is considered a modern model for ancient anoxic ocean basins, indicate that high DOP, a high ratio of reactive iron to total iron, and a high ratio of total iron to aluminum are all indicators of transport of iron into a euxinic environment. Ferruginous anoxic conditions can be distinguished from euxenic conditions by a DOP less than about 0.7.<ref name=tracking-euxenia/>

The currently available evidence suggests that the deep ocean remained anoxic and ferruginous as late as 580 Ma, well after the Great Oxygenation Event, remaining just short of euxenic during much of this interval of time. Deposition of banded iron formation ceased when conditions of local euxenia on continental platforms and shelves began precipitating iron out of upwelling ferruginous water as pyrite.<ref name="Canfield-2011"/><ref name="Catling-2017"/><ref name=tracking-euxenia/>

=== Isotopes ===
Some of the most persuasive evidence for the Great Oxidation Event is provided by the [[Chemistry:Mass-independent fractionation|mass-independent fractionation]] (MIF) of sulfur. The chemical signature of the MIF of sulfur is found prior to 2.4–2.3&nbsp;Ga but disappears thereafter.<ref>{{Cite journal|last=Farquhar |first=J. |s2cid=12287304 |date=2000-08-04 |title=Atmospheric Influence of Earth's Earliest Sulfur Cycle |journal=Science |volume=289 |issue=5480 |pages=756–758 |doi=10.1126/science.289.5480.756 |pmid=10926533 |bibcode=2000Sci...289..756F }}</ref> The presence of this signature all but eliminates the possibility of an oxygenated atmosphere.<ref name="weichert-2002"/>

Different isotopes of a chemical element have slightly different atomic masses. Most of the differences in geochemistry between isotopes of the same element scale with this mass difference. These include small differences in molecular velocities and diffusion rates, which are described as mass-dependent fractionation processes. By contrast, MIF describes processes that are not proportional to the difference in mass between isotopes. The only such process likely to be significant in the geochemistry of sulfur is [[Astronomy:Photodissociation|photodissociation]]. This is the process in which a molecule containing sulfur is broken up by solar ultraviolet (UV) radiation. The presence of a clear MIF signature for sulfur prior to 2.4 Ga shows that UV radiation was penetrating deep into the Earth's atmosphere. This in turn rules out an atmosphere containing more than traces of oxygen, which would have produced an [[Physics:Ozone layer|ozone layer]] that would have shielded the lower atmosphere from UV radiation. The disappearance of the MIF signature for sulfur indicates the formation of such an ozone shield as oxygen began to accumulate in the atmosphere.<ref name="weichert-2002"/><ref name="Catling-2017"/> MIF of sulphur also indicates the presence of oxygen in that oxygen is required to facilitate repeated redox cycling of sulphur.<ref>{{cite journal |last1=Fakhraee |first1=Mojtaba |last2=Hancisse |first2=Olivier |last3=Canfield |first3=Donald Eugene |last4=Crowe |first4=Sean A. |last5=Katsev |first5=Sergei |date=22 April 2019 |title=Proterozoic seawater sulfate scarcity and the evolution of ocean–atmosphere chemistry |url=https://www.nature.com/articles/s41561-019-0351-5?error=cookies_not_supported&code=08d6cc6f-9d29-4dd5-a6e0-c047e85b7884 |journal=[[Earth:Nature Geoscience|Nature Geoscience]] |volume=12 |issue=5 |pages=375–380 |doi=10.1038/s41561-019-0351-5 |s2cid=146026944 |access-date=20 December 2022}}</ref>

MIF provides clues to the Great Oxygenation Event. For example, oxidation of manganese in surface rocks by atmospheric oxygen leads to further reactions that oxidize chromium. The heavier <sup>53</sup>Cr is oxidized preferentially over the lighter <sup>52</sup>Cr, and the soluble oxidized chromium carried into the ocean shows this enhancement of the heavier isotope. The chromium isotope ratio in banded iron formation suggests small but significant quantities of oxygen in the atmosphere before the Great Oxidation Event, and a brief return to low oxygen abundance 500 Ga after the GOE. However, the chromium data may conflict with the sulfur isotope data, which calls the reliability of the chromium data into question.<ref name="Frei20093">{{cite journal |last1=Frei |first1=R. |last2=Gaucher |first2=C. |last3=Poulton |first3=S.W. |last4=Canfield |first4=D.E. |year=2009 |title=Fluctuations in Precambrian atmospheric oxygenation recorded by chromium isotopes |journal=Nature |volume=461 |issue=7261 |pages=250–253 |bibcode=2009Natur.461..250F |doi=10.1038/nature08266 |pmid=19741707 |s2cid=4373201 }}</ref><ref>{{cite journal |last1=Lyons |first1=Timothy W. |last2=Reinhard |first2=Christopher T. |title=Oxygen for heavy-metal fans |journal=Nature |date=September 2009 |volume=461 |issue=7261 |pages=179–180 |doi=10.1038/461179a |pmid=19741692 |s2cid=205049360 |doi-access=free }}</ref> It is also possible that oxygen was present earlier only in localized "oxygen oases".<ref name="kerr_2005">{{cite journal |last1=Kerr |first1=R. A. |title=Earth Science: The Story of O<sub>2</sub> |journal=Science |date=17 June 2005 |volume=308 |issue=5729 |pages=1730–1732 |doi=10.1126/science.308.5729.1730|pmid=15961643 |s2cid=129684672 }}</ref> Since chromium is not easily dissolved, its release from rocks requires the presence of a powerful acid such as [[Chemistry:Sulfuric acid|sulfuric acid]] (H<sub>2</sub>SO<sub>4</sub>) which may have formed through bacterial oxidation of pyrite. This could provide some of the earliest evidence of oxygen-breathing life on land surfaces.<ref>{{cite journal |last1=Konhauser |first1=Kurt O. |last2=Lalonde |first2=Stefan V. |last3=Planavsky |first3=Noah J. |last4=Pecoits |first4=Ernesto |last5=Lyons |first5=Timothy W. |last6=Mojzsis |first6=Stephen J. |last7=Rouxel |first7=Olivier J. |last8=Barley |first8=Mark E. |last9=Rosìere |first9=Carlos |last10=Fralick |first10=Phillip W. |last11=Kump |first11=Lee R. |last12=Bekker |first12=Andrey |title=Aerobic bacterial pyrite oxidation and acid rock drainage during the Great Oxidation Event |journal=Nature |date=October 2011 |volume=478 |issue=7369 |pages=369–373 |doi=10.1038/nature10511 |pmid=22012395 |bibcode=2011Natur.478..369K |s2cid=205226545}}
* {{cite news |author=Wynne Parry |date=25 October 2011 |title=Evidence of Earliest Oxygen-Breathing Life on Land Discovered |work=Live Science |url=http://www.livescience.com/16714-oxygen-breathing-life-chromium.html}}</ref>

Other elements whose MIF may provide clues to the GOE include carbon, nitrogen, transitional metals such as [[Chemistry:Molybdenum|molybdenum]] and iron, and non-metal elements such as [[Chemistry:Selenium|selenium]].<ref name="Catling-2017"/>

=== Fossils and biomarkers ===

While the GOE is generally thought to be a result of oxygenic photosynthesis by ancestral cyanobacteria, the presence of cyanobacteria in the [[Earth:Archean|Archaean]] before the GOE is a highly controversial topic.<ref>{{Cite journal|last1=Catling|first1=David C.|last2=Zahnle|first2=Kevin J.|date=February 2020|title=The Archean atmosphere|journal=Science Advances|language=en|volume=6|issue=9|pages=eaax1420|doi=10.1126/sciadv.aax1420|issn=2375-2548|pmc=7043912|pmid=32133393|bibcode=2020SciA....6.1420C}}</ref> Structures that are claimed to be fossils of cyanobacteria exist in rock formed 3.5 Ga.<ref name="Schopf-2006">{{Cite journal |last=Schopf |first=J. William |date=29 June 2006 |title=Fossil evidence of Archaean life |journal=Philosophical Transactions of the Royal Society B: Biological Sciences |volume=361 |issue=1470 |pages=869–885 |doi=10.1098/rstb.2006.1834 |pmc=1578735 |pmid=16754604}}</ref> These include microfossils of supposedly cyanobacterial cells and macrofossils called [[Earth:Stromatolite|stromatolite]]s, which are interpreted as colonies of microbes, including cyanobacteria, with characteristic layered structures. Modern stromatolites, which can only be seen in harsh environments such as Shark Bay in Western Australia, are associated with cyanobacteria, and thus fossil stromatolites had long been interpreted as the evidence for cyanobacteria.<ref name="Schopf-2006" /> However, it has increasingly been inferred that at least some of these Archaean fossils were generated abiotically or produced by non-cyanobacterial phototrophic bacteria.<ref>{{Cite journal |last1=Bosak |first1=Tanja |last2=Knoll |first2=Andrew H. |last3=Petroff |first3=Alexander P. |date=30 May 2013 |title=The Meaning of Stromatolites |url=https://www.annualreviews.org/doi/10.1146/annurev-earth-042711-105327 |journal=[[Earth:Annual Review of Earth and Planetary Sciences|Annual Review of Earth and Planetary Sciences]] |volume=41 |issue=1 |pages=21–44 |doi=10.1146/annurev-earth-042711-105327 |bibcode=2013AREPS..41...21B |issn=0084-6597}}</ref>

Additionally, Archaean sedimentary rocks were once found to contain [[Biology:Biomarker|biomarker]]s, also known as [[Astronomy:Biosignature|chemical fossils]], interpreted as fossilized membrane lipids from cyanobacteria and [[Biology:Eukaryote|eukaryote]]s. For example, traces of 2α-methylhopanes and steranes that are thought to be derived from cyanobacteria and eukaryotes, respectively, were found in the [[Earth:Pilbara|Pilbara]] of Western Australia.<ref>{{Cite journal |last1=Brocks |first1=Jochen J. |last2=Logan |first2=Graham A. |last3=Buick |first3=Roger |last4=Summons |first4=Roger E. |date=13 August 1999 |title=Archean Molecular Fossils and the Early Rise of Eukaryotes |url=https://www.science.org/lookup/doi/10.1126/science.285.5430.1033 |journal=Science |volume=285 |issue=5430 |pages=1033–1036 |doi=10.1126/science.285.5430.1033 |pmid=10446042 |bibcode=1999Sci...285.1033B}}</ref> [[Chemistry:Sterane|Sterane]]s are diagenetic products of sterols, which are biosynthesized utilizing molecular oxygen. Thus, steranes can additionally serve as an indicator of oxygen in the atmosphere. However, these biomarker samples have since been shown to have been contaminated, and so the results are no longer accepted{{according to whom |date=November 2023}}.<ref>{{Cite journal |last1=French |first1=Katherine L. |last2=Hallmann |first2=Christian |last3=Hope |first3=Janet M. |last4=Schoon |first4=Petra L. |last5=Zumberge |first5=J. Alex |last6=Hoshino |first6=Yosuke |last7=Peters |first7=Carl A. |last8=George |first8=Simon C. |last9=Love |first9=Gordon D. |url=https://www.researchgate.net/publication/275586228 |date=27 April 2015 |title=Reappraisal of hydrocarbon biomarkers in Archean rocks |journal=Proceedings of the National Academy of Sciences of the United States of America |volume=112 |issue=19 |pages=5915–5920 |doi=10.1073/pnas.1419563112 |pmid=25918387 |pmc=4434754 |bibcode=2015PNAS..112.5915F |doi-access=free |access-date=13 August 2023}}</ref>

=== Other indicators ===
Some elements in marine sediments are sensitive to different levels of oxygen in the environment such as the [[Chemistry:Transition metal|transition metal]]s [[Chemistry:Molybdenum|molybdenum]]<ref name=tracking-euxenia/> and [[Chemistry:Rhenium|rhenium]].<ref>{{Cite journal |last1=Anbar |first1=Ariel D. |last2=Rouxel |first2=Olivier |s2cid=130960654 |date=May 2007 |title=Metal Stable Isotopes in Paleoceanography |journal=Annual Review of Earth and Planetary Sciences |volume=35 |issue=1 |pages=717–746 |doi=10.1146/annurev.earth.34.031405.125029 |bibcode=2007AREPS..35..717A }}</ref> Non-metal elements such as selenium and iodine are also indicators of oxygen levels.<ref>{{cite journal |last1=Stüeken |first1=E.E. |last2=Buick |first2=R. |last3=Bekker |first3=A. |last4=Catling|first4=D. |last5=Foriel |first5=J. |last6=Guy |first6=B.M. |last7=Kah |first7=L.C. |last8=Machel |first8=H.G. |last9=Montañez |first9=I.P. |date=2015-08-01 |title=The evolution of the global selenium cycle: Secular trends in Se isotopes and abundances |journal=Geochimica et Cosmochimica Acta |volume=162 |pages=109–125 |doi=10.1016/j.gca.2015.04.033 |bibcode=2015GeCoA.162..109S |doi-access=free }}</ref>

== Hypotheses ==
{{Life timeline}}
The ability to generate oxygen via photosynthesis likely first appeared in the ancestors of cyanobacteria.<ref>{{cite journal |author1=Cardona, T. |author2=Murray, J. W. |author3=Rutherford, A. W. |title=Origin and Evolution of Water Oxidation before the Last Common Ancestor of the Cyanobacteria |journal=Molecular Biology and Evolution |volume=32 |issue=5 |pages=1310–1328 |date=May 2015 |doi=10.1093/molbev/msv024 |pmid=25657330 |pmc=4408414}}</ref> These organisms evolved at least 2.45–2.32 Ga<ref>{{cite journal |author=Tomitani, Akiko |title=The evolutionary diversification of cyanobacteria: Molecular–phylogenetic and paleontological perspectives |journal=PNAS |volume=103 |issue=14 |pages=5442–5447 |date=April 2006 |doi=10.1073/pnas.0600999103 |pmid=16569695 |pmc=1459374|bibcode=2006PNAS..103.5442T |doi-access=free }}</ref><ref>{{cite web|url=http://www.ucmp.berkeley.edu/bacteria/cyanofr.html |title=Cyanobacteria: Fossil Record |publisher=Ucmp.berkeley.edu |access-date=2010-08-26}}</ref> and probably as early as 2.7  Ga or earlier.<ref name="kastings-1993"/><ref>{{cite journal |last1=Dutkiewicz |first1=A. |last2=Volk |first2=H. |last3=George |first3=S.C. |last4=Ridley |first4=J. |last5=Buick |first5=R. |year=2006 |title=Biomarkers from Huronian oil-bearing fluid inclusions: An uncontaminated record of life before the Great Oxidation Event |journal=Geology |volume=34 |issue=6 |pages=437 |bibcode= 2006Geo....34..437D |doi=10.1130/G22360.1}}</ref><ref name="Lyons 307–315"/><ref name="ELSVR-201803062">{{cite journal |last=Caredona |first=Tanai |date=6 March 2018 |title=Early Archean origin of heterodimeric Photosystem&nbsp;I |journal=Heliyon |volume=4 |issue=3 |page=e00548 |doi=10.1016/j.heliyon.2018.e00548 |pmid=29560463 |pmc=5857716}}</ref><ref name="AST-201803072">{{cite web |last=Howard |first=Victoria |title=Photosynthesis originated a billion years earlier than we thought, study shows |url=https://www.astrobio.net/also-in-news/photosynthesis-originated-billion-years-earlier-thought-study-shows/ |date=7 March 2018 |work=[[Astronomy:Astrobiology Magazine|Astrobiology Magazine]] |access-date=23 March 2018 |archive-url=https://web.archive.org/web/20201001223438/https://www.astrobio.net/also-in-news/photosynthesis-originated-billion-years-earlier-thought-study-shows/ |archive-date=2020-10-01 |url-status=usurped}}</ref> However, oxygen remained scarce in the atmosphere until around 2.0 Ga,<ref name="shaw-2998"/> and banded iron formation continued to be deposited until around 1.85 Ga.<ref name="kastings-1993"/> Given the rapid multiplication rate of cyanobacteria under ideal conditions, an explanation is needed for the delay of at least 400 million years between the evolution of oxygen-producing photosynthesis and the appearance of significant oxygen in the atmosphere.<ref name="shaw-2998"/>

Hypotheses to explain this gap must take into consideration the balance between oxygen sources and oxygen sinks. Oxygenic photosynthesis produces organic carbon that must be segregated from oxygen to allow oxygen accumulation in the surface environment, otherwise the oxygen back-reacts with the organic carbon and does not accumulate. The burial of organic carbon, sulfide, and minerals containing ferrous iron (Fe{{sup|2+}}) is a primary factor in oxygen accumulation.<ref name="Holland-2002"/> When organic carbon is buried without being oxidized, the oxygen is left in the atmosphere. In total, the burial of organic carbon and pyrite today creates {{val|15.8|3.3|u=[[Tera-|T]]mol}} {{nowrap|(1 Tmol {{=}} 10<sup>12</sup> moles)}} of O{{sub|2}} per year. This creates a net O{{sub|2}} flux from the global oxygen sources.

The rate of change of oxygen can be calculated from the difference between global sources and sinks.<ref name="Catling-2017">{{Cite book |title=Atmospheric Evolution on Inhabited and Lifeless Worlds |last1=Catling |first1=David C. |last2=Kasting |first2=James F. |date=2017 |publisher={{wipe|Cambridge University Press}} |isbn=978-1-139-02055-8 |location=Cambridge |doi=10.1017/9781139020558 }}{{page needed|date=June 2021}}</ref> The oxygen sinks include reduced gases and minerals from [[Earth:Volcano|volcanoes]], [[Earth:Metamorphism|metamorphism]] and weathering.<ref name="Catling-2017"/> The GOE started after these oxygen-sink fluxes and reduced-gas fluxes were exceeded by the flux of O<sub>2</sub> associated with the burial of reductants, such as organic carbon.<ref name="University of Zurich-2013">{{cite web |url=https://www.sciencedaily.com/releases/2013/01/130117084856.htm |author=University of Zurich |title=Great Oxidation Event: More oxygen through multicellularity |date=17 January 2013 |website=ScienceDaily}}</ref> About {{val|12.0|3.3|u=Tmol}} of O{{sub|2}} per year today goes to the sinks composed of reduced minerals and gases from volcanoes, metamorphism, percolating seawater and heat vents from the seafloor.<ref name="Catling-2017"/> On the other hand, {{val|5.7|1.2|u=Tmol}} of O{{sub|2}} per year today oxidizes reduced gases in the atmosphere through photochemical reaction.<ref name="Catling-2017" /> On the early Earth, there was visibly very little oxidative weathering of continents (e.g., a lack of [[Earth:Red beds|red beds]]), and so the weathering sink on oxygen would have been negligible compared to that from reduced gases and dissolved iron in oceans.

Dissolved iron in oceans exemplifies O<sub>2</sub> sinks. Free oxygen produced during this time was chemically captured by dissolved iron, converting iron Fe and Fe<sup>2+</sup> to magnetite ({{chem2|Fe(2+)Fe2(3+)O4}}) that is insoluble in water, and sank to the bottom of the shallow seas to create banded iron formations.<ref name="University of Zurich-2013"/> It took 50&nbsp;million years or longer to deplete the oxygen sinks.<ref name="Anabar20072">{{cite journal |last1=Anbar |first1=A. |last2=Duan |first2=Y. |last3=Lyons |first3=T. |last4=Arnold |first4=G. |last5=Kendall |first5=B. |last6=Creaser |first6=R. |last7=Kaufman |first7=A. |last8=Gordon |first8=G. |last9=Scott |first9=C. |first10=J. |last10=Garvin |last11=Buick |first11=R. |year=2007 |title=A whiff of oxygen before the great oxidation event? |journal=Science |volume=317 |issue=5846 |pages=1903–1906 |bibcode=2007Sci...317.1903A |doi=10.1126/science.1140325 |pmid=17901330|s2cid=25260892 }}</ref> The rate of photosynthesis and associated rate of organic burial also affect the rate of oxygen accumulation. When land plants spread over the continents in the [[Earth:Devonian|Devonian]], more organic carbon was buried and likely allowed higher O<sub>2</sub> levels to occur.<ref>{{cite journal |last1=Dahl |first1=T.W. |last2=Hammarlund |first2=E.U. |last3=Anbar |first3=A.D. |last4=Bond |first4=D.P.G. |last5=Gill |first5=B.C. |last6=Gordon |first6=G.W. |last7=Knoll |first7=A.H. |last8=Nielsen |first8=A.T. |last9=Schovsbo |first9=N.H. |date=2010-09-30 |title=Devonian rise in atmospheric oxygen correlated to the radiations of terrestrial plants and large predatory fish |journal=Proceedings of the National Academy of Sciences |volume=107 |issue=42 |pages=17911–17915 |doi=10.1073/pnas.1011287107 |pmid=20884852 |pmc=2964239 |bibcode=2010PNAS..10717911D|doi-access=free }}</ref> Today, the average time that an O{{sub|2}} molecule spends in the air before it is consumed by geological sinks is about 2&nbsp;million years.<ref>{{Cite journal |last1=Catling |first1=David C. |last2=Claire |first2=Mark W. |date=August 2005 |title=How Earth's atmosphere evolved to an oxic state: A status report |journal=Earth and Planetary Science Letters |volume=237 |issue=1–2 |pages=1–20 |doi=10.1016/j.epsl.2005.06.013 |bibcode=2005E&PSL.237....1C }}</ref> That residence time is relatively short in geologic time; so in the [[Earth:Phanerozoic|Phanerozoic]], there must have been feedback processes that kept the atmospheric O{{sub|2}} level within bounds suitable for animal life.

=== Evolution by stages ===
Preston Cloud originally proposed that the first cyanobacteria had evolved the capacity to carry out oxygen-producing photosynthesis but had not yet evolved enzymes (such as [[Biology:Superoxide dismutase|superoxide dismutase]]) for living in an oxygenated environment. These cyanobacteria would have been protected from their own poisonous [[Biology:Reactive oxygen species|oxygen waste]] through its rapid removal via the high levels of reduced ferrous iron, Fe(II), in the early ocean. He suggested that the oxygen released by photosynthesis oxidized the Fe(II) to ferric iron, Fe(III), which precipitated out of the sea water to form banded iron formation.<ref name="cloud-1968">{{cite journal |last1=Cloud |first1=Preston E. |title=Atmospheric and Hydrospheric Evolution on the Primitive Earth. |journal=Science |volume=160 |number=3829 |year=1968 |pages=729–736 |doi=10.1126/science.160.3829.729 |jstor=1724303 |pmid=5646415 |bibcode=1968Sci...160..729C }}</ref><ref name= "Cloud_1973">{{cite journal |last1 = Cloud |first1=P. | doi = 10.2113/gsecongeo.68.7.1135| pages = 1135–1143| volume = 68| journal = Economic Geology| title = Paleoecological Significance of the Banded Iron-Formation| year = 1973 | issue = 7 }}</ref> He interpreted the great peak in deposition of banded iron formation at the end of the Archean as the signature for the evolution of mechanisms for living with oxygen. This ended self-poisoning and produced a population explosion in the cyanobacteria that rapidly oxygenated the ocean and ended banded iron formation deposition.<ref name="cloud-1968"/><ref name= "Cloud_1973"/> However, improved dating of Precambrian strata showed that the late Archean peak of deposition was spread out over tens of millions of years, rather than taking place in a very short interval of time following the evolution of oxygen-coping mechanisms. This made Cloud's hypothesis untenable.<ref name="trendall-2002"/> 

Most modern interpretations describe the GOE as a long, protracted process that took place over hundreds of millions of years rather than a single abrupt event, with the quantity of atmospheric oxygen fluctuating in relation to the capacity of oxygen sinks and the productivity of oxygenic photosynthesisers over the course of the GOE.<ref name="Lyons 307–315" /> More recently, families of bacteria have been discovered that closely resemble cyanobacteria but show no indication of ever having possessed photosynthetic capability. These may be descended from the earliest ancestors of cyanobacteria, which only later acquired photosynthetic ability by lateral gene transfer. Based on [[Biology:Molecular clock|molecular clock]] data, the evolution of oxygen-producing photosynthesis may have occurred much later than previously thought, at around 2.5 Ga. This reduces the gap between the evolution of oxygen photosynthesis and the appearance of significant atmospheric oxygen.<ref name="How Cyanobacteria went green">{{cite journal|last1=Blankenship|first1=Robert E.|date=31 March 2017|title=How Cyanobacteria went green|journal=Science|volume=355|issue=6332|pages=1372–1373|bibcode=2017Sci...355.1372B|doi=10.1126/science.aam9365|pmid=28360281|s2cid=37177062}}</ref>

===Nutrient famines===
Another possibility is that early cyanobacteria were starved for vital nutrients, and this checked their growth. However, a lack of the scarcest nutrients, iron, nitrogen, and phosphorus, could have slowed but not prevented a cyanobacteria population explosion and rapid oxygenation. The explanation for the delay in the oxygenation of the atmosphere following the evolution of oxygen-producing photosynthesis likely lies in the presence of various oxygen sinks on the young Earth.<ref name="shaw-2998"/>

====Nickel famine====
Early [[Earth:Chemosynthesis|chemosynthetic organisms]] likely produced [[Chemistry:Methane|methane]], an important trap for molecular oxygen, since methane readily oxidizes to [[Chemistry:Carbon dioxide|carbon dioxide]] (CO<sub>2</sub>) and water in the presence of [[Physics:Ultraviolet|UV radiation]]. Modern methanogens require [[Chemistry:Nickel|nickel]] as an [[Biology:Cofactor (biochemistry)|enzyme cofactor]]. As the [[Earth:Earth's crust|Earth's crust]] cooled and the supply of volcanic nickel dwindled, oxygen-producing algae began to outperform methane producers, and the oxygen percentage of the atmosphere steadily increased.<ref>{{cite web |url=http://www.scientificamerican.com/podcast/episode/breathing-easy-thanks-to-great-oxid-09-04-13/ |title=Breathing Easy Thanks to the Great Oxidation Event |publisher=Scientific American |access-date=2016-04-06}}</ref> From 2.7 to 2.4&nbsp;Ga the rate of deposition of nickel declined steadily from a level 400&nbsp;times that of today.<ref>{{cite journal |last1=Konhauser |first1=Kurt O. |last2=Pecoits |first2=Ernesto |last3=Lalonde |first3=Stefan V. |last4=Papineau |first4=Dominic |last5=Nisbet |first5=Euan G. |last6=Barley |first6=Mark E. |last7=Arndt |first7=Nicholas T. |last8=Zahnle |first8=Kevin |last9=Kamber |first9=Balz S. |title=Oceanic nickel depletion and a methanogen famine before the Great Oxidation Event |journal=Nature |date=April 2009 |volume=458 |issue=7239 |pages=750–753 |doi=10.1038/nature07858 |pmid=19360085 |bibcode=2009Natur.458..750K |s2cid=205216259 }}</ref> This nickel famine was somewhat buffered by an uptick in sulfide weathering at the start of the GOE that brought some nickel to the oceans, without which methanogenic organisms would have declined in abundance more precipitously, plunging Earth into even more severe and long-lasting [[Earth:Greenhouse and icehouse Earth|icehouse]] conditions than those seen during the [[Earth:Huronian glaciation|Huronian glaciation]].<ref name="MethanogenesisSulphideWeathering">{{cite journal |last1=Wang |first1=Shui-Jiong |last2=Rudnick |first2=Roberta L. |last3=Gaschnig |first3=Richard M. |last4=Wang |first4=Hao |last5=Wasylenki |first5=Laura E. |date=4 March 2019 |title=Methanogenesis sustained by sulfide weathering during the Great Oxidation Event |url=https://www.nature.com/articles/s41561-019-0320-z |journal=[[Earth:Nature Geoscience|Nature Geoscience]] |volume=12 |issue=4 |pages=296–300 |doi=10.1038/s41561-019-0320-z |s2cid=134715298 |access-date=11 November 2022}}</ref>

=== Increasing flux ===
One hypothesis argues that the GOE was the immediate result of photosynthesis, although the majority of scientists suggest that a long-term increase of oxygen is more likely.<ref>{{Cite journal |last1=Kirschvink |first1=Joseph L. |last2=Kopp |first2=Robert E. |date=2008-08-27 |title=Palaeoproterozoic ice houses and the evolution of oxygen-mediating enzymes: the case for a late origin of photosystem&nbsp;II |journal=Philosophical Transactions of the Royal Society&nbsp;B: Biological Sciences |volume=363 |issue=1504 |pages=2755–2765 |doi=10.1098/rstb.2008.0024 |pmid=18487128 |pmc=2606766 }}</ref> Several model results show possibilities of long-term increase of carbon burial,<ref>{{Cite journal |last1=des Marais |first1=David J. |last2=Strauss |first2=Harald |last3=Summons |first3=Roger E. |last4=Hayes |first4=J.M. |date=October 1992 |title=Carbon isotope evidence for the stepwise oxidation of the Proterozoic environment |journal=Nature |volume=359 |issue=6396 |pages=605–609 |doi=10.1038/359605a0 |pmid=11536507 |bibcode=1992Natur.359..605M |s2cid=4334787 }}</ref> but the conclusions are indeterminate.<ref>{{Cite journal|last1=Krissansen-Totton |first1=J. |last2=Buick |first2=R. |last3=Catling|first3=D.C. |date=2015-04-01 |title=A statistical analysis of the carbon isotope record from the Archean to Phanerozoic and implications for the rise of oxygen |journal=American Journal of Science |volume=315 |issue=4 |pages=275–316 |doi=10.2475/04.2015.01 |bibcode=2015AmJS..315..275K |s2cid=73687062 }}</ref>

=== Decreasing sink ===
In contrast to the increasing flux hypothesis, there are several hypotheses that attempt to use decrease of sinks to explain the GOE.<ref name="MechanismsGOE">{{cite journal |last1=Luo |first1=Genming |last2=Zhu |first2=Xiangkun |last3=Wang |first3=Shuijiong |last4=Zhang |first4=Shihong |last5=Jiao |first5=Chaoqun |date=22 June 2022 |title=Mechanisms and climatic-ecological effects of the Great Oxidation Event in the early Proterozoic |url=https://link.springer.com/article/10.1007/s11430-021-9934-y? |journal=Science China Earth Sciences |volume=65 |issue=9 |pages=1646–1672 |doi=10.1007/s11430-021-9934-y |s2cid=250065550 |access-date=12 November 2022}}</ref> One theory suggests that the composition of the volatiles from [[Physics:Volcanic gas|volcanic gases]] was more oxidized.<ref name="Holland-2002">{{cite journal |last=Holland |first=Heinrich D. |date=November 2002 |title=Volcanic gases, black smokers, and the great oxidation event |journal=Geochimica et Cosmochimica Acta |volume=66 |issue=21 |pages=3811–3826 |doi=10.1016/s0016-7037(02)00950-x |bibcode=2002GeCoA..66.3811H }}</ref> Another theory suggests that the decrease of metamorphic gases and [[Earth:Serpentinite|serpentinization]] is the main key of GOE. Hydrogen and methane released from metamorphic processes are also lost from Earth's atmosphere over time and leave the crust oxidized.<ref name="Catling 839–843">{{Cite journal |last=Catling |first=D.C. |date=2001-08-03 |title=Biogenic Methane, Hydrogen Escape, and the Irreversible Oxidation of Early Earth |journal=Science |volume=293 |issue=5531 |pages=839–843 |doi=10.1126/science.1061976 |pmid=11486082 |bibcode=2001Sci...293..839C|s2cid=37386726 }}</ref> Scientists realized that hydrogen would escape into space through a process called methane photolysis, in which methane decomposes under the action of ultraviolet light in the upper atmosphere and releases its hydrogen. The escape of hydrogen from the Earth into space must have oxidized the Earth because the process of hydrogen loss is chemical oxidation.<ref name="Catling 839–843"/> This process of hydrogen escape required the generation of methane by methanogens, so that methanogens actually helped create the conditions necessary for the oxidation of the atmosphere.<ref name="kerr_2005"/>

===Tectonic trigger===
[[File:Black-band ironstone (aka).jpg|thumb|right|2.1-billion-year-old rock showing banded iron formation]]
One hypothesis suggests that the oxygen increase had to await tectonically driven changes in the Earth, including the appearance of shelf seas, where reduced organic carbon could reach the sediments and be buried.<ref>{{cite journal |first1=T.M. |last1=Lenton |first2=H.J. |last2=Schellnhuber |first3=E. |last3=Szathmáry |date=2004 |title=Climbing the co-evolution ladder |journal=Nature |volume=431 |pmid=15496901 |issue=7011 |pages=913 |doi=10.1038/431913a |bibcode=2004Natur.431..913L|s2cid=27619682 |doi-access=free }}</ref> The burial of reduced carbon as graphite or diamond around subduction zones released molecular oxygen into the atmosphere.<ref>{{cite journal |last1=Duncan |first1=Megan S. |last2=Dasgupta |first2=Rajdeep |date=25 April 2017 |title=Rise of Earth's atmospheric oxygen controlled by efficient subduction of organic carbon |url=https://www.nature.com/articles/ngeo2939 |journal=[[Earth:Nature Geoscience|Nature Geoscience]] |volume=10 |issue=1 |pages=387–392 |doi=10.1038/ngeo2939 |access-date=2 May 2023}}</ref><ref>{{cite journal |last1=Eguchi |first1=James |last2=Seales |first2=Johnny |last3=Dasgupta |first3=Rajdeep |date=2019 |title=Great Oxidation and Lomagundi events linked by deep cycling and enhanced degassing of carbon |journal=[[Earth:Nature Geoscience|Nature Geoscience]] |doi=10.1038/s41561-019-0492-6 |volume=13 |issue=1 |pages=71–76 |pmid=31807138 |pmc=6894402 |bibcode=2020NatGe..13...71E }}</ref> The appearance of oxidised magmas enriched in sulphur formed around subduction zones confirms changes in tectonic regime played an important role in the oxygenation of Earth's atmosphere.<ref>{{cite journal |last1=Meng |first1=Xuyang |last2=Simon |first2=Adam C. |last3=Kleinsasser |first3=Jackie M. |last4=Mole |first4=David R. |last5=Kontak |first5=Daniel J. |last6=Jugo |first6=Peter J. |last7=Mao |first7=Jingwen |last8=Richards |first8=Jeremy P. |date=28 November 2022 |title=Formation of oxidized sulfur-rich magmas in Neoarchaean subduction zones |url=https://www.nature.com/articles/s41561-022-01071-5 |journal=[[Earth:Nature Geoscience|Nature Geoscience]] |volume=15 |issue=1 |pages=1064–1070 |doi=10.1038/s41561-022-01071-5 |s2cid=254175442 |access-date=2 May 2023}}</ref> 

The newly produced oxygen was first consumed in various chemical reactions in the oceans, primarily with iron. Evidence is found in older rocks that contain massive banded iron formations apparently laid down as this iron and oxygen first combined; most present-day [[Earth:Iron ore|iron ore]] lies in these deposits. It was assumed oxygen released from cyanobacteria resulted in the chemical reactions that created rust, but it appears the iron formations were caused by anoxygenic phototrophic iron-oxidizing bacteria, which does not require oxygen.<ref>{{cite journal |last1=Köhler |first1=Inga |last2=Konhauser |first2=Kurt O |last3=Papineau |first3=Dominic |last4=Bekker |first4=Andrey |last5=Kappler |first5=Andreas |title=Biological carbon precursor to diagenetic siderite with spherical structures in iron formations |journal=Nature Communications |date=June 2013 |volume=4 |issue=1 |pages=1741 |doi=10.1038/ncomms2770 |pmid=23612282 |bibcode=2013NatCo...4.1741K |doi-access=free}}
*{{cite web |date=25 April 2013 |title=Iron in primeval seas rusted by bacteria |website=Phys.org |url=https://phys.org/news/2013-04-iron-primeval-seas-rusted-bacteria.html}}</ref> Evidence suggests oxygen levels spiked each time smaller land masses collided to form a super-continent. Tectonic pressure thrust up mountain chains, which eroded releasing nutrients into the ocean that fed photosynthetic cyanobacteria.<ref>{{cite web |url=http://www.scientificamerican.com/podcast/episode/5C271294-EE45-D925-BEBBEF03016A7CF4/ |title=Abundant Oxygen Indirectly Due to Tectonics |last=American |first=Scientific |website=Scientific American |access-date=2016-04-06}}</ref>

===Bistability===
Another hypothesis posits a model of the atmosphere that exhibits [[Bistability|bistability]]: two [[Steady state|steady state]]s of oxygen concentration. The state of stable low oxygen concentration (0.02%) experiences a high rate of methane oxidation. If some event raises oxygen levels beyond a moderate threshold, the formation of an ozone layer shields UV rays and decreases methane oxidation, raising oxygen further to a stable state of 21% or more. The Great Oxygenation Event can then be understood as a [[Physics:Phase transition|transition]] from the lower to the upper steady states.<ref>{{Cite journal |author1=Goldblatt, C. |author2=Lenton, T.M. |author3=Watson, A.J. |date=2006 |title=Bistability of atmospheric oxygen and the Great Oxidation |journal=Nature |volume=443 |issue=7112 |pages=683–686 |doi=10.1038/nature05169 |pmid=17036001 |bibcode=2006Natur.443..683G |s2cid=4425486 }}</ref><ref>{{Cite journal |last1=Claire |first1=M.W. |last2=Catling |first2=D.C. |last3=Zahnle |first3=K.J. |date=December 2006 |title=Biogeochemical modelling of the rise in atmospheric oxygen |journal=Geobiology |volume=4 |issue=4 |pages=239–269 |doi=10.1111/j.1472-4669.2006.00084.x |s2cid=11575334 }}</ref>

===Increasing photoperiod===
Cyanobacteria tend to consume nearly as much oxygen at night as they produce during the day. However, experiments demonstrate that cyanobacterial mats produce a greater excess of oxygen with longer photoperiods. The rotational period of the Earth was only about six hours shortly after its formation 4.5 Ga but increased to 21 hours by 2.4 Ga in the Paleoproterozoic. The rotational period increased again, starting 700 million years ago, to its present value of 24 hours. The total amount of oxygen produced by the cyanobacteria remained the same with longer days, but the longer day, the more time oxygen has to diffuse into the water.<ref>{{cite journal |last1=Klatt |first1=J. M. |last2=Chennu |first2=A. |last3=Arbic |first3=B. K. |last4=Biddanda |first4=B. A. |last5=Dick |first5=G. J. |title=Possible link between Earth's rotation rate and oxygenation |journal=Nature Geoscience |date=2 August 2021 |volume=14 |issue=8 |pages=564–570 |doi=10.1038/s41561-021-00784-3|bibcode=2021NatGe..14..564K |s2cid=236780731 |doi-access=free }}</ref><ref>{{cite journal |last1=Pennisi |first1=Elizabeth |title='Totally new' idea suggests longer days on early Earth set stage for complex life |journal=Science |date=2 August 2021 |doi=10.1126/science.abl7415|s2cid=242885564 }}</ref><ref>[https://eos.org/articles/longer-days-likely-boosted-earths-early-oxygen Longer Days Likely Boosted Earth's Early Oxygen – Eos.org]</ref>

==Consequences of oxygenation==

Eventually, oxygen started to accumulate in the atmosphere, with two major consequences.
* Oxygen likely oxidized [[Earth:Atmospheric methane|atmospheric methane]] (a strong greenhouse gas) to carbon dioxide (a weaker one) and water. This weakened the greenhouse effect of the Earth's atmosphere, causing planetary cooling, which has been proposed to have triggered a series of ice ages known as the [[Earth:Huronian glaciation|Huronian glaciation]], bracketing an age range of 2.45–2.22&nbsp;Ga.<ref>{{Cite encyclopedia |last=Bekker |first=Andrey |title=Huronian Glaciation |year=2014 |encyclopedia=Encyclopedia of Astrobiology |pages=1–8 |editor-last=Amils |editor-first=Ricardo |publisher=Springer Berlin Heidelberg |doi=10.1007/978-3-642-27833-4_742-4 |isbn=978-3-642-27833-4 |editor2-last=Gargaud |editor2-first=Muriel |editor3-last=Cernicharo Quintanilla |editor3-first=José |editor4-last=Cleaves |editor4-first=Henderson James}}</ref><ref name="Kopp20052">{{Cite journal |author1=Kopp, Robert E. |author2=Kirschvink, Joseph L. |author3=Hilburn, Isaac A. |author4=Nash, Cody Z. |date=2005 |title=The Paleoproterozoic snowball Earth: A climate disaster triggered by the evolution of oxygenic photosynthesis |journal=Proceedings of the National Academy of Sciences of the United States of America |volume=102 |issue=32 |pages=11131–11136 |bibcode=2005PNAS..10211131K |doi=10.1073/pnas.0504878102 |pmc=1183582 |pmid=16061801|doi-access=free }}</ref><ref name="NS2">{{cite magazine |url=https://www.newscientist.com/article/mg20527461.100-first-breath-earths-billionyear-struggle-for-oxygen.html |title=First breath: Earth's billion-year struggle for oxygen |magazine=New Scientist |issue=2746 |date=5 February 2010 |first=Nick |last=Lane}}</ref>
* The increased oxygen concentrations provided a new opportunity for biological diversification, as well as tremendous changes in the nature of chemical interactions between rocks, sand, clay, and other geological substrates and the Earth's air, oceans, and other surface waters. Despite the natural recycling of [[Chemistry:Organic matter|organic matter]], life had remained energetically limited until the widespread availability of oxygen. The availability of oxygen greatly increased the [[Physics:Thermodynamic free energy|free energy]] available to living organisms, with global environmental impacts. For example, [[Biology:Mitochondria|mitochondria]] evolved after the GOE, giving organisms the energy to exploit new, more complex morphologies interacting in increasingly complex ecosystems, although these did not appear until the late Proterozoic and Cambrian.<ref>{{cite journal |last1=Sperling |first1=Erik |last2=Frieder |first2=Christina |last3=Raman |first3=Akkur |last4=Girguis |first4=Peter |last5=Levin |first5=Lisa |last6= Knoll |first6=Andrew |date=Aug 2013 |title=Oxygen, ecology, and the Cambrian radiation of animals |journal=Proceedings of the National Academy of Sciences of the United States of America |volume=110 |issue=33 |pages=13446–13451 |bibcode=2013PNAS..11013446S |doi=10.1073/pnas.1312778110 |pmc=3746845 |pmid=23898193|doi-access=free }}</ref>

{{clear}}

[[File:GlaciationsinEarthExistancelicenced annotated.jpg|thumb|upright=3.5|center| Timeline of glaciations, shown in blue.]]

{{clear}}

===Mineral diversification===
{{Main|Earth:Mineral evolution}}
The Great Oxygenation Event triggered an explosive growth in the diversity of [[Earth:Mineral|mineral]]s, with many elements occurring in one or more oxidized forms near the Earth's surface.<ref>{{Cite journal|last1=Sverjensky|first1=Dimitri A. |last2=Lee |first2=Namhey |date=2010-02-01 |title=The Great Oxidation Event and Mineral Diversification |journal=Elements |volume=6 |issue=1 |pages=31–36 |doi=10.2113/gselements.6.1.31 }}</ref> It is estimated that the GOE was directly responsible for more than 2,500 of the total of about 4,500&nbsp;minerals found on Earth today. Most of these new minerals were formed as hydrated and oxidized forms due to dynamic [[Earth:Mantle (geology)|mantle]] and [[Earth:Crust (geology)|crust]] processes.<ref name="sciam1">{{cite magazine |url=http://www.scientificamerican.com/article.cfm?id=evolution-of-minerals |title=Evolution of Minerals |magazine=Scientific American |date=March 2010}}</ref>
{{Simple Horizontal timeline

|caption=Million years ago. [[Earth:Age of Earth|Age of Earth]] = 4,560
|collapsible=yes
|row1=note
|row1-1-at=-2500
|row1-1-text=GOE
|row1-2-at=-2100
|row1-2-text=End of Huronian glaciation

|row2=timeline
|row2-1-to=-635
|row2-2-to=0

|row4=scale

|from=-2500
|to=0
|axis-nudge=-1em
|inc=200

}}

=== Cyanobacteria evolution ===
In field studies done in Lake Fryxell, Antarctica, scientists found that mats of oxygen-producing cyanobacteria produced a thin layer, one to two&nbsp;millimeters thick, of oxygenated water in an otherwise [[Earth:Anoxic waters|anoxic environment]], even under thick ice. By inference, these organisms could have adapted to oxygen even before oxygen accumulated in the atmosphere.<ref name="sumner">{{cite journal |last5=Doran |first5=Peter T. |last4=Jungblut |first4=Anne D. |last3=Mackey |first3=Tyler J. |last2=Hawes |first2=Ian |last1=Sumner |first1=Dawn Y. |date=2015-10-01 |title=Antarctic microbial mats: A modern analog for Archean lacustrine oxygen oases |journal=Geology |volume=43 |issue=10 |pages=887–890 |doi=10.1130/G36966.1 |bibcode=2015Geo....43..887S |hdl=10092/12361 |s2cid=55557643 |url=https://digitalcommons.lsu.edu/cgi/viewcontent.cgi?article=1604&context=geo_pubs |hdl-access=free}}
* {{cite press release |date=1 September 2015 |title=Oxygen oasis in Antarctic lake reflects Earth in distant past |website=ScienceDaily |url=https://www.sciencedaily.com/releases/2015/09/150901140759.htm}}</ref> The evolution of such oxygen-dependent organisms eventually established an equilibrium in the availability of oxygen, which became a major constituent of the atmosphere.<ref name=sumner/>

===Origin of eukaryotes===
It has been proposed that a local rise in oxygen levels due to cyanobacterial photosynthesis in ancient microenvironments was highly toxic to the surrounding biota, and that this selective pressure drove the evolutionary transformation of an [[Biology:Archaea|archaea]]l lineage into the first [[Biology:Eukaryote|eukaryote]]s.<ref name="pmid20731852">{{cite journal |author1=Gross, J. |author2=Bhattacharya, D. |title=Uniting sex and eukaryote origins in an emerging oxygenic world |journal=Biol. Direct |volume=5|pages=53 |date=August 2010 |pmid=20731852 |pmc=2933680 |doi=10.1186/1745-6150-5-53 |doi-access=free }}</ref> [[Biology:Oxidative stress|Oxidative stress]] involving production of [[Biology:Reactive oxygen species|reactive oxygen species]] (ROS) might have acted in synergy with other environmental stresses (such as ultraviolet radiation and/or [[Earth:Desiccation|desiccation]]) to drive selection in an early archaeal lineage towards eukaryosis.  This archaeal ancestor may already have had [[Biology:DNA repair|DNA repair]] mechanisms based on DNA pairing and [[Biology:Homologous recombination|recombination]] and possibly some kind of cell fusion mechanism.<ref name="pmid29436502">{{cite journal |vauthors=Hörandl E, Speijer D |title=How oxygen gave rise to eukaryotic sex |journal=Proc. Biol. Sci. |volume=285 |issue=1872 |page=20172706 |date=February 2018 |pmid=29436502 |pmc=5829205 |doi=10.1098/rspb.2017.2706}}</ref><ref>{{cite book |doi=10.1007/978-3-319-65536-9_7 |chapter=Sexual Communication in Archaea, the Precursor to Eukaryotic Meiosis |title=Biocommunication of Archaea |year=2017 |last1=Bernstein |first1=Harris |last2=Bernstein |first2=Carol |pages=103–117 |isbn=978-3-319-65535-2 }}</ref> The detrimental effects of internal ROS (produced by [[Biology:Endosymbiont|endosymbiont]] proto-[[Biology:Mitochondrion|mitochondria]]) on the archaeal [[Biology:Genome|genome]] could have promoted the [[Biology:Origin and function of meiosis|evolution of meiotic sex]] from these humble beginnings.<ref name="pmid29436502"/> Selective pressure for efficient DNA repair of oxidative DNA damage may have driven the evolution of eukaryotic sex involving such features as cell-cell fusions, cytoskeleton-mediated chromosome movements and emergence of the nuclear membrane.<ref name="pmid20731852"/> Thus the evolution of eukaryotic sex and eukaryogenesis were likely inseparable processes that evolved in large part to facilitate DNA repair.<ref name="pmid20731852" /> The evolution of mitochondria, which are well suited for oxygenated environments, may have occurred during the GOE.<ref>{{Cite journal |last1=Mänd |first1=Kaarel |last2=Planavsky |first2=Noah J. |last3=Porter |first3=Susannah M. |last4=Robbins |first4=Leslie J. |last5=Wang |first5=Changle |last6=Kreitsmann |first6=Timmu |last7=Paiste |first7=Kärt |last8=Paiste |first8=Päärn |last9=Romashkin |first9=Alexander E. |last10=Deines |first10=Yulia E. |last11=Kirsimäe |first11=Kalle |last12=Lepland |first12=Aivo |last13=Konhauser |first13=Kurt O. |date=15 April 2022 |title=Chromium evidence for protracted oxygenation during the Paleoproterozoic |url=https://linkinghub.elsevier.com/retrieve/pii/S0012821X22001376 |journal=[[Earth:Earth and Planetary Science Letters|Earth and Planetary Science Letters]] |language=en |volume=584 |pages=117501 |doi=10.1016/j.epsl.2022.117501 |access-date=17 September 2023|hdl=10037/24808 |hdl-access=free }}</ref>

However, other authors express scepticism that the GOE resulted in widespread eukaryotic diversification due to the lack of robust evidence, concluding that the oxygenation of the oceans and atmosphere does not necessarily lead to increases in ecological and physiological diversity.<ref>{{Cite journal |last1=Fakhraee |first1=Mojtaba |last2=Tarhan |first2=Lidya G. |last3=Reinhard |first3=Christopher T. |last4=Crowe |first4=Sean A. |last5=Lyons |first5=Timothy W. |last6=Planavsky |first6=Noah J. |date=May 2023 |title=Earth's surface oxygenation and the rise of eukaryotic life: Relationships to the Lomagundi positive carbon isotope excursion revisited |url=https://linkinghub.elsevier.com/retrieve/pii/S0012825223000879 |journal=[[Earth:Earth-Science Reviews|Earth-Science Reviews]] |language=en |volume=240 |pages=104398 |doi=10.1016/j.earscirev.2023.104398 |access-date=17 September 2023}}</ref>

==== Lomagundi-Jatuli event ====
The rise in oxygen content was not linear: instead, there was a rise in oxygen content around 2.3 Ga, followed by a drop around 2.1 Ga. This rise in oxygen is called the '''Lomagundi-Jatuli event''' or '''Lomagundi event''',<ref>{{cite journal | url=https://www.sciencedirect.com/science/article/abs/pii/0301926875900182 | title=Precambrian sedimentary carbonates: carbon and oxygen isotope geochemistry and implications for the terrestrial oxygen budget | first1=Manfred | last1=Schidlowski | first2=Rudolf | last2=Eichmann | first3=Christian | last3=Junge | journal=Precambrian Research | year=1975 | volume=2 | issue=1 | pages=1–69 | doi=10.1016/0301-9268(75)90018-2| bibcode=1975PreR....2....1S }}</ref><ref>{{cite journal | url=https://www.sciencedirect.com/science/article/abs/pii/0016703776900107 | title=Carbon isotope geochemistry of the Precambrian Lomagundi carbonate province, Rhodesia | first1=Manfred | last1=Schidlowski | first2=Rudolf | last2=Eichmann | first3=Christian | last3=Junge | journal=Geochimica et Cosmochimica Acta | year=1976 | volume=40 | issue=4 | pages=449–455 | doi=10.1016/0016-7037(76)90010-7| bibcode=1976GeCoA..40..449S }}</ref><ref name="BauerGeo">{{Cite web|url=https://bauer.geoscience.wisc.edu/research/|title=Research}}</ref> (named for a district of Southern Rhodesia) and the time period has been termed Jatulian; it is currently considered to be part of the [[Earth:Rhyacian|Rhyacian]] period.<ref>{{cite journal | title=A molecular timescale for eukaryote evolution with implications for the origin of red algal-derived plastids | first1=Jürgen F. H. | last1=Strassert | first2=Iker | last2=Irisarri | first3=Tom A. | last3=Williams | first4=Fabien | last4=Burki | journal=Nature | year=2021 | volume=12 | issue=1 | page=1879 | doi=10.1038/s41467-021-22044-z| pmid=33767194 | pmc=7994803 | bibcode=2021NatCo..12.1879S | doi-access=free }}</ref><ref name="Mand2020">{{cite journal |last1=Mänd |first1=Kaarel |last2=Lalonde |first2=Stefan V. |last3=Robbins |first3=Leslie J. |last4=Thoby |first4=Marie |last5=Paiste |first5=Kärt |last6=Kreitsmann |first6=Timmu |last7=Paiste |first7=Päärn |last8=Reinhard |first8=Christopher T. |last9=Romashkin |first9=Alexandr E. |last10=Planavsky |first10=Noah J. |last11=Kirsimäe |first11=Kalle |last12=Lepland |first12=Aivo |last13=Konhauser |first13=Kurt O. |title=Palaeoproterozoic oxygenated oceans following the Lomagundi–Jatuli Event |journal=Nature Geoscience |date=April 2020 |volume=13 |issue=4 |pages=302–306 |doi=10.1038/s41561-020-0558-5 |bibcode=2020NatGe..13..302M |hdl=10037/19269 |s2cid=212732729 |hdl-access=free }}</ref><ref name="vankranendonk2012">{{cite book|last=Van Kranendonk|first=Martin J. |title=The geologic time scale 2012|date=2012|publisher=Elsevier|location=Amsterdam|isbn=978-0-44-459425-9|pages=359–365|edition=1st|editor=Felix M. Gradstein |editor2=James G. Ogg |editor3=Mark D. Schmitz |editor4=abi M. Ogg|chapter=16: A Chronostratigraphic Division of the Precambrian: Possibilities and Challenges|doi=10.1016/B978-0-444-59425-9.00016-0}}</ref> During the Lomagundi-Jatuli event, oxygen amounts in the atmosphere reached similar heights to modern levels, before returning to low levels during the following stage, which caused the deposition of black shales (rocks that contain large amounts of organic matter that would otherwise have been burned away by oxygen). This drop in oxygen levels is called the '''{{visible anchor|Shunga-Francevillian event}}'''. Evidence for the event has been found globally in places such as Fennoscandia and the Wyoming Craton.<ref name="Martin'sEarthScience">{{cite journal |last1=Martin |first1=Adam P. |last2=Condon |first2=Daniel J. |last3=Prave |first3=Anthony R. |last4=Lepland |first4=Aivo |date=December 2013 |title=A review of temporal constraints for the Palaeoproterozoic large, positive carbonate carbon isotope excursion (the Lomagundi–Jatuli Event) |url=https://www.sciencedirect.com/science/article/abs/pii/S0012825213001724 |journal=[[Earth:Earth-Science Reviews|Earth-Science Reviews]] |volume=127 |pages=242–261 |doi=10.1016/j.earscirev.2013.10.006 |access-date=12 December 2022}}</ref><ref name="Dashiqiao">{{cite journal |last1=Tang |first1=Hao-Shu |last2=Chen |first2=Yan-Jing |last3=Santosh |first3=M. |last4=Zhong |first4=Hong |last5=Wu |first5=Guang |last6=Lai |first6=Yong |date=28 January 2013 |title=C–O isotope geochemistry of the Dashiqiao magnesite belt, North China Craton: implications for the Great Oxidation Event and ore genesis |url=https://onlinelibrary.wiley.com/doi/full/10.1002/gj.2486 |journal=Geological Journal |volume=48 |issue=5 |pages=467–483 |doi=10.1002/gj.2486 |s2cid=140672677 |access-date=12 December 2022}}</ref> Oceans seem to have stayed rich in oxygen for some time even after the event ended.<ref name="Mand2020"/><ref>{{cite journal |last1=Kreitsmann |first1=T. |last2=Lepland |first2=A. |last3=Bau |first3=M. |last4=Prave |first4=A. |last5=Paiste |first5=K. |last6=Mänd |first6=K. |last7=Sepp |first7=H. |last8=Martma |first8=T. |last9=Romashkin |first9=A.E. |last10=Kirsimäe |first10=K. |title=Oxygenated conditions in the aftermath of the Lomagundi-Jatuli Event: The carbon isotope and rare earth element signatures of the Paleoproterozoic Zaonega Formation, Russia |journal=Precambrian Research |date=September 2020 |volume=347 |pages=105855 |doi=10.1016/j.precamres.2020.105855 |bibcode=2020PreR..347j5855K |hdl=10023/23503 |s2cid=225636859 |hdl-access=free }}</ref>

It has been hypothesized that eukaryotes first evolved during the Lomagundi-Jatuli event.<ref name="Mand2020" />

==See also==
* [[Earth:Boring Billion|Boring Billion]] – Earth history between 1.8 and 0.8 billion years ago, characterized by tectonic stability, climatic stasis, and a slow biological evolution with very low oxygen levels and no evidence of glaciation
* [[Earth:Geological history of oxygen|Geological history of oxygen]] – Timeline of the development of free oxygen in the Earth's oceans and atmosphere
* {{annotated link|Astronomy:Medea hypothesis}}
* {{annotated link|Earth:Pasteur point}}
* [[Earth:Purple Earth hypothesis|Purple Earth hypothesis]] – Hypothesis that early photosynthesis reflected purple light
* [[Astronomy:Rare Earth hypothesis|Rare Earth hypothesis]] – Hypothesis that complex extraterrestrial life is an extremely rare phenomenon
* {{annotated link|Earth:Stromatolite}}

==References==
{{Reflist}}

==External links==
* {{cite magazine |url=https://www.newscientist.com/article/mg20527461.100-first-breath-earths-billionyear-struggle-for-oxygen/ |title=First breath: Earth's billion-year struggle for oxygen |magazine=New Scientist |issue=2746 |date=5 February 2010 |first=Nick |last=Lane |access-date=8 October 2017 |archive-date=6 January 2011 |archive-url=https://web.archive.org/web/20110106141826/http://ptc-cam.blogspot.com/2010/02/first-breath-earths-billion-year.html |url-status=dead }}

{{Extinction}}

[[Category:Paleoproterozoic]]
[[Category:Origin of life]]
[[Category:Oxygen]]
[[Category:Evolution of the biosphere]]
[[Category:Extinction events]]
[[Category:Mass extinction timelines]]
[[Category:Meteorological hypotheses]]

{{Sourceattribution|Great Oxidation Event}}