Boring Billion

The Boring Billion, otherwise referred to as the Barren Billion, the Dullest Time in Earth's History, and Earth’s Middle Ages, is the time period between 1.8 and 0.8 billion years ago (Gya) spanning the middle Proterozoic eon, characterized by more or less tectonic stability, climatic stasis, and stalled evolution. It is bordered by two different oxygenation and glacial events, but the Boring Billion itself had very low oxygen levels and no evidence of glaciation. The oceans may have been oxygen- and nutrient-poor and sulfidic (euxinia), populated by mainly anoxygenic cyanobacteria, a type of photosynthetic bacteria which uses hydrogen sulfide (H2S) instead of water and produces sulfur instead of oxygen. This is known as a Canfield ocean. Such composition may have caused the oceans to be black- or milky-turquoise instead of blue.

Despite such adverse conditions, eukaryotes may have evolved around the beginning of the Boring Billion, and adopted several novel adaptations, such as various organelles and possibly sexual reproduction, and diversified into plants, animals, and fungi. Such advances may have been important precursors to the evolution of large, complex life later in the Cambrian explosion. However, prokaryotic cyanobacteria were the dominant lifeforms during this time, and likely supported an energy-poor food-web with a small number of protists at the apex level. The land was likely inhabited by prokaryotic cyanobacteria and eukaryotic proto-lichens, the latter more successful here probably due to the greater availability of nutrients than offshore ocean waters.


In 1995, geologists Roger Buick, Davis Des Marais, and Andrew Knoll reviewed the apparent lack of major biological, geological, and climatic events during the Mesoproterozoic era 1.6 to 1 billion years ago (Gya), and, thus, described it as "the dullest time in Earth's history".[1] The term "Boring Billion" was first coined in 1998 by paleontologist Martin Brasier and geologist John Lindsay to refer to the time between about 2 and 1 Gya, which was characterized by climatic and tectonic stability, and low nutrient abundance, based on rocks from Mount Isa and McArthur Basin, Queensland.[2] In 2005, Australian geologist George Williams used the term "Barren Billion" to refer to a period of apparent glacial stagnation in Kimberley, Western Australia from 1.8 to 0.8 Gya.[3] In 2014, geologists Peter Cawood and Chris Hawkesworth called the time between 1.7 and 0.75 Gya "Earth's Middle Ages" due to a lack of evidence of tectonic movement.[4]

The Boring Billion is now largely cited as spanning about 1.8 to 0.8 Gya, contained within the Proterozoic eon, mainly the Mesoproterozoic. The Boring Billion is characterized by geological, climatic, and by-and-large evolutionary stasis, with low nutrient abundance.[5][6][7][8][9]

In the time leading up to the Boring Billion, Earth experienced the Great Oxygenation Event due to the evolution of oxygenic photosynthetic cyanobacteria, and the resultant Huronian glaciation (Snowball Earth), formation of the UV-blocking ozone layer, and oxidation of several metals.[10] Boring Billion oxygen levels dramatically dropped.[10] It was ended by the breakup of the supercontinent Rodinia, a second oxygenation event, and another Snowball Earth in the Cryogenian period.[4][11]

Tectonic stasis

Reconstruction of Columbia (above, 1.6 Gya) and Rodinia after break-up (below, 0.75 Gya)

The evolution of Earth's biosphere, atmosphere, and hydrosphere has long been linked to the supercontinent cycle, where the continents aggregate and then drift apart. The Boring Billion saw the evolution of two supercontinents: Columbia (or Nuna) and Rodinia.[12]

The supercontinent Columbia formed between 2.0 and 1.7 Ga and remained intact until at least 1.3 Ga. Geological and paleomagnetic evidence suggest that Columbia underwent only minor changes to form the supercontinent Rodinia from 1.1 to 0.9 Ga. Paleogeographic reconstructions suggest that the supercontinent assemblage was located in equatorial and temperate climate zones, and there is little or no evidence for continental fragments in polar regions.[12]

Due to the lack of evidence of sediment build-up (on passive margins) which would occur as a result of rifting,[13] the supercontinent probably did not break up, and rather was simply an assemblage of juxtaposed proto-continents and cratons. There is no evidence of rifting until the formation of Rodinia, 1.25 Gya in North Laurentia, and 1 Gya in East Baltica and South Siberia.[5][4] However, breakup did not occur until 0.75 Gya, marking the end of the boring billion.[4] This tectonic stasis may have been related in ocean and atmospheric chemistry.[5][8][4]

It is possible the asthenosphere–the molten layer of Earth's mantle that tectonic plates essentially float and move around upon–was too hot to sustain modern plate tectonics at this time. Instead of vigorous plate recycling at subduction zones, plates were linked together for billions of years until the mantle cooled off enough. The onset of this component of plate tectonics may have been aided by the cooling and thickening of the crust that, once initiated, caused plate subduction to be anomalously strong, occurring at the end of the boring billion.[4]

Nonetheless, major magmatic events still occurred, namely the formation (via magma plume) of the 220,000 km2 (85,000 sq mi) central Australian Musgrave Province from 1.22 to 1.12 Gya,[14] and the 2,700,000 km2 (1,000,000 sq mi) Canadian Mackenzie Large Igneous Province 1.27 Gya;[15] and plate tectonics were still active enough to build mountains, with several orogenies known from the time, such as the Grenville orogeny.[16]

Climatic stability

There is little evidence of significant climatic variability during this time period.[6][17] Climate was likely not primarily dictated by solar luminosity, because, if it were, all water on the planet would have been locked up in ice–which was not the case according to the fossil record–[18]because the sun was 5–18% less intense than today (faint young Sun paradox).[19] In fact, the Boring Billion is unique in a sense that it seems to lack any evidence of significant periods of prolonged glaciations, which can be observed in regular periodicity in other parts of Earth's geologic history.[18] High CO2 could not have been a main driver because levels would have needed to be 30 to 100 times greater than pre-industrial levels[19] and produced substantial ocean acidification[18] to prevent ice formation, which also did not occur. Mesoproterozoic CO2 levels may have been comparable to those of the Phanerozoic eon, perhaps 7 to 10 times today's levels.[20]

A higher abundance of other greenhouse gases, namely methane produced by prokaryotes, may have compensated the low CO2 levels; an ice-free world may have been achieved with a methane concentration of 140 parts per million (ppm).[20][19] However, methanogenic prokaryotes could not have produced so much methane, implying some other greenhouse gas, probably nitrous oxide was elevated, perhaps to 3 ppm (10 times today's levels). Based on presumed greenhouse gas concentrations, equatorial temperatures during the Mesoproterozoic may have been about 295–300 K (22–27 °C; 71–80 °F), in the tropics 290 K (17 °C; 62 °F), at 60° 265–280 K (−8–7 °C; 17–44 °F), and the poles 250–275 K (−23–2 °C; −10–35 °F);[21] and the global average temperature about 19 °C (66 °F), which is 4°C (7.2°F) warmer than today. Temperatures at the poles were estimated to have dropped below freezing in winter, allowing for temporary sea ice formation and snowfall, but there were likely no permanent ice sheets.[9]

It has also been proposed that, because the intensity of cosmic rays has been shown to be positively correlated to cloud cover, and cloud cover reflects light back out into space and reduces global temperatures, lower rates of bombardment during this time due to reduced star formation in the galaxy caused less cloud cover and stayed glaciation events, maintaining a warm climate.[18][22] Also, some combination of weathering intensity which would have reduced CO2 levels by oxidation of exposed metals, cooling of the mantle and reduced geothermal heat and volcanism, and increasing solar intensity and solar heat may have reached an equilibrium barring ice formation.[6]

Conversely, glacial movements over a billion years ago may not have left many remnants today, and an apparent lack of evidence could simply be due to the incompleteness of the fossil record rather than absence. Further, the low oxygen and solar intensity levels may have prevented the formation of the ozone layer, which traps greenhouse gasses in the atmosphere and increases temperatures via the greenhouse effect, which would have caused glaciation.[23][24][25] However, not much oxygen is necessary to sustain the ozone layer, and levels during the Boring Billion may have been high enough for it.[26] though the Earth may still have been more heavily bombarded by UV radiation than today.[27]

Oceanic composition

The oceans seem to have had low concentrations of key nutrients thought to be necessary for complex life, namely molybdenum, iron, nitrogen, and phosphorus, in large part due to a lack of oxygen and resultant oxidation necessary for these geochemical cycles.[28][29][30] However, nutrients were more abundant in terrestrial environments, such as lakes or nearshore environments closer to continental runoff.[31]

In general, the oceans may have had an oxygenated surface layer, a sulfidic middle layer,[32][33][34] and suboxic bottom layer.[35][36] The predominantly sulfidic composition may have caused the oceans to be a black- and milky-turquoise color instead of blue.[37]


Earth's geologic record indicates two events associated with significant increases in oxygen levels on Earth, with one occurring between 2.4 and 2.1 Gya, known as the Great Oxygenation Event, and the second occurring an approximate 0.8 Ga.[38] The intermediary period, during the boring billion, is thought have had low oxygen levels (which minor fluctuations), leading to widespread anoxic waters.[33]

The oceans may have been distinctly stratified, with surface water oxygenated,[32][33][34] and deep water suboxic (less than 1 μM oxygen),[36] the latter possibly maintained by lower levels of hydrogen (H2) and H2S output by deep sea hydrothermal vents which otherwise would have been reduced by the oxygen.[35] However, the decomposition of sinking organic matter would have leeched oxygen from deep waters.[39][33]

The sudden drop in O2 after the Great Oxygenation Event–indicated by δ13C levels to have been loss of 10 to 20 times the current volume of atmospheric oxygen–is known as the Lomagundi Excursion Event, and is the most prominent carbon isotope event in Earth's history.[40][41][42] Oxygen levels may have been less than 0.1 to 2% of modern day levels, which would have effectively stalled the evolution of complex life during the boring billion.[38][34] Oxic conditions would have become dominant at the second oxygenation event with the proliferation of aerobic activity over anaerobic,[32][33][39] but conditions likely lasted until about 0.55 Gya corresponding with Ediacaran biota and the Cambrian explosion.[43][44]


In 1998, geologist Donald Canfield proposed what is now known as the Canfield ocean hypothesis. Canfield claimed that increasing levels of oxygen in the atmosphere at the Great Oxygenation Event would have reacted with and oxidized continental iron pyrite (FeS2) deposits, with sulfate (SO42−) as a byproduct, which was transported into the sea. Sulfate-reducing microorganisms converted this to hydrogen sulfide (H2S), dividing the ocean into a somewhat oxic surface layer, and a sulfidic layer beneath, with anoxygenic bacteria living at the border, metabolizing the H2S and creating sulfur as a waste product. This created widespread euxinic conditions in middle-waters, an anoxic state with a high sulfur concentration, which was maintained by the bacteria.[32][33][45][32][46][39][34]


During the Boring Billion, there is a conspicuous lack of banded iron formations–which form in the upper water column of the ocean, with the iron deriving from the deep sea–seemingly ceasing after 1.85 around the world. Canfield said that oceanic SO42− reduced all the iron in the anoxic deep sea, as opposed to oxygen as previously supposed.[32] Iron could have been metabolized by anoxygenic bacteria.[47] It has also been proposed that the 1.85 Ga Sudbury meteor impact mixed the previously stratified Canfield ocean via tsunamis, interaction between vaporized seawater and the oxygenated atmosphere, oceanic cavitation, and massive runoff of destroyed continental margins into the sea. Resultant suboxic deep waters due to oxygenated surface water mixing with anoxic deep water would have oxidized deep-water iron, preventing it from being transported and deposited on continental margins.[35]

Nonetheless, iron-rich (ferrous) waters did exist, such as the 1.4 Ga Xiamaling Formation of Northern China, which perhaps was fed by deep water hydrothermal vents. Ferrous conditions also indicate anoxic bottom water in this area, as oxic conditions would have oxidized all the iron.[47]


Low nutrient abundance may have caused increased photosymbiosis–where one organism is capable of photosynthesis and the other metabolizes the waste product–among prokaryotes (bacteria and archaea), and the emergence of eukaryotes. Bacteria, Archaea, and Eukaryota are the three domains, the highest taxonomic ranking. Eukaryotes are distinguished from prokaryotes by a nucleus and membrane-bound organelles, and all multicellular organisms are eukaryotes.[2]


Prokaryotes were the dominant lifeforms throughout the Boring Billion.[10][48][32] Anoxygenic cyanobacteria are thought to have been the dominant photosynthesizers, metabolizing the abundant H2S in the oceans. However, in iron-rich waters, cyanobacteria may have suffered from iron poisoning, especially in offshore waters were iron-rich deep water mixed with surface waters, and were outcompeted by other bacteria which could metabolize both iron and H2S. However, iron poisoning could have been abated by silica-rich waters or biomineralization of iron within the cell.[49]

Microfossils indicate the presence of cyanobacteria, green and purple sulfur bacteria, methane-producing archaea or bacteria, sulfate-metabolizing bacteria, methane-metabolizing archaea or bacteria, iron-metabolizing bacteria, anoxygenic photosynthetic bacteria, and nitrogen-metabolizing bacteria.[49]


Eukaryotes may have arisen around the beginning of the Boring Billion,[7] coinciding with the accretion of Columbia, which could have somehow increased oceanic oxygen levels.[11] However, multicellular eukaryotes possibly already evolved by this time, with the earliest claimed fossil evidence dating to the Great Oxygenation Event with jellyfish-like Francevillian biota.[50] Following this, eukaryotic evolution was rather slow,[10] possibly due to the euxinic conditions of the Canfield ocean and a lack of key nutrients and metals[4][7] which prevented large, complex life with high energy requirements from evolving.[23] Euxinic conditions would have also decreased the solubility of iron[32] and molybdenum,[51] essential metals in nitrogen fixation. A lack of dissolved nitrogen would have favored prokaryotes over eukaryotes, as the former can metabolize gaseous nitrogen.[52]

Nonetheless, the diversification of crown group eukaryotic macroorganisms seems to have started about 1.6–1 Gya,[54] seemingly coinciding with an increase in key nutrient concentrations.[7] According to phylogenetic analysis, plants diverged from animals and fungi about 1.6 Gya; animals and fungi about 1.5 Gya; Bilaterians and cnidarians (animals respectively with and without bilateral symmetry) about 1.3 Gya; sponges 1.35 Gya;[55] and Ascomycota and Basidiomycota (the two divisions of the fungus subkingdom Dikarya) 0.97 Gya.[55] The earliest known fungus dates to 1.01–0.89 Gya from Northern Canada.[56] Multicellular eukaryotes had probably evolved about 2–1.4 Gya, thought to be the descendants of colonial unicellular aggregates.[57][58] The earliest known red algae mats date to 1.6 Gya.[53] Early multicellular eukaryotes likely mainly aggregated into stromatolite mats.[11]

The 1.2 Ga red alga Bangiomorpha is the earliest known sexually reproducing and meiotic lifeform,[59] and, based on this, these adaptations evolved 2–1.4 Gya.[7] However, these may have evolved well before the last common ancestor of eukaryotes given that meiotic eukaryotes use the same proteins specific for the task, perhaps stretching to as far back as the hypothesized RNA world.[60]

Cell organelles probably originated from free-living cyanobacteria (symbiogenesis)[10][61][62][7] possibly after the evolution of phagocytosis (engulfing other cells) with the removal of the rigid cell wall which was only necessary for asexual reproduction.[10] Mitochondria had already evolved in the Great Oxygenation Event, but plastids used in plants for namely photosynthesis are thought to have appeared about 1.6–1.5 Gya.[55] Histones likely appeared during the Boring Billion to help organize and package the increasing amount of DNA in eukaryotic cells into nucleosomes.[10] Hydrogenosomes used in anaerobic activity may have originated in this time from an archaeon.[63][61]

Given the evolutionary landmarks achieved by eukaryotes, this time period could be considered an important precursor to the Cambrian explosion about 0.54 Gya, and the evolution of relatively large, complex life.[10]


Due to the marginalization of large food particles, such as algae, in favor of cyanobacteria and prokaryotes which do not transmit as much energy to higher trophic levels, a complex food web likely did not form, and large lifeforms with high energy demands could not evolve. Such a food web probably only sustained a small number of protists as, in a sense, apex predators.[48]

The presumably oxygenic photosynthetic eukaryotic acritarchs, perhaps a type of microalga, inhabited the Mesoproterozoic surface waters.[64] Their population may have been largely limited by nutrient availability rather than predation because species have been reported to have survived for hundreds of millions of years, but after 1 Gya, species duration dropped to about 100 Ma, perhaps due to increased herbivory by early protists. This is consistent with species survival dropping to 10 Ma just after the Cambrian explosion and the expansion of herbivorous animals.[65]

Life on land

Some of the earliest evidence of the prokaryotic colonization of land dates to before 3 Gya,[66] possibly as early as 3.5 Gya.[67] During the Boring Billion, land may have been inhabited mainly by cyanobacterial mats.[10][68][69][70][71] Dust would have supplied an abundance of nutrients and a means of dispersal for surface-dwelling microbes, though microbial communities could have also formed in caves and freshwater lakes and rivers.[27][72] By 1.2 Gya, microbial communities may have been abundant enough to have affected weathering, erosion, sedimentation, and various geochemical cycles,[69] and expansive microbial mats could indicate biological soil crust was abundant.[27]

The earliest terrestrial eukaryotes may have been lichen fungi about 1.3 Ga,[73] which grazed on the microbial mats.[27] Abundant eukaryotic microfossils from the freshwater Scottish Torridon Group seems to indicate eukaryotic dominance in non-marine habitats by 1 Gya,[74] probably due to increase nutrient availability in areas closer to the continents and continental runoff.[31] These lichen may have later facilitated plant colonization 0.75 Gya in some manner.[73] A massive increase in terrestrial photosynthetic biomass seems to have occurred about 0.85 Gya, indicated by a flux in terrestrially-sourced carbon, which may have increased oxygen levels enough to support an expansion of multicellular eukaryotes.[75]

See also


  1. Buick, R.; Des Marais, D. J.; Knoll, A. H. (1995-06-20). "Stable isotopic compositions of carbonates from the Mesoproterozoic Bangemall group, northwestern Australia". Chemical Geology. 123 (1–4): 153–171. Bibcode:1995ChGeo.123..153B. doi:10.1016/0009-2541(95)00049-R. PMID 11540130.
  2. Brasier, M. D.; Lindsay, J. F. (1998). "A billion years of environmental stability and the emergence of eukaryotes: new data from northern Australia". Geology. 26 (6): 555–558. doi:10.1130/0091-7613(1998)026<0555:ABYOES>2.3.CO;2. PMID 11541449.
  3. Williams, G. E. (2005). "Subglacial meltwater channels and glaciofluvial deposits in the Kimberley Basin, Western Australia: 1.8 Ga low-latitude glaciation coeval with continental assembly". Journal of the Geological Society. 162 (1): 111–124. doi:10.1144/0016-764903-157.
  4. Cawood, Peter A.; Hawkesworth, Chris J. (2014-06-01). "Earth's middle age". Geology. 42 (6): 503–506. Bibcode:2014Geo....42..503C. doi:10.1130/G35402.1. ISSN 0091-7613.
  5. Roberts, Nick M. W. (1 November 2013). "The boring billion? – Lid tectonics, continental growth and environmental change associated with the Columbia supercontinent". Geoscience Frontiers. Thematic Section: Antarctica – A window to the far off land. 4 (6): 681–691. doi:10.1016/j.gsf.2013.05.004.
  6. Young, Grant M. (2013-05-01). "Precambrian supercontinents, glaciations, atmospheric oxygenation, metazoan evolution and an impact that may have changed the second half of Earth history". Geoscience Frontiers. 4 (3): 247–261. doi:10.1016/j.gsf.2012.07.003.
  7. Mukherjee, I.; Large, R. R.; Corkrey, R.; Danyushevsky, L. V. (2018). "The Boring Billion, a slingshot for Complex Life on Earth". Scientific Reports. 8 (4432): 4432. doi:10.1038/s41598-018-22695-x. PMC 5849639. PMID 29535324.
  8. Holland, Heinrich D. (2006-06-29). "The oxygenation of the atmosphere and oceans". Philosophical Transactions of the Royal Society of London B: Biological Sciences. 361 (1470): 903–915. doi:10.1098/rstb.2006.1838. ISSN 0962-8436. PMC 1578726. PMID 16754606.
  9. Peng, L.; Yonggang, L.; Yongyun, H.; Yun, Y.; Pisarevsky, S. A. (2019). "Warm Climate in the "Boring Billion" Era". Acta Geologica Sinica. 93: 40–43. doi:10.1111/1755-6724.14239.
  10. Lenton, T.; Watson, A. (2011). Revolutions that made the Earth. pp. 242–261. doi:10.1093/acprof:oso/9780199587049.003.0013. ISBN 9780199587049.
  11. Brooke, J. L. (2014). Climate Change and the Course of Global History: A Rough Journey. Cambridge University Press. pp. 40–42. ISBN 978-0-521-87164-8.
  12. Evans, D. A. D. (2013). "Reconstructing pre-Pangean supercontinents". Geological Society of America Bulletin. 125 (11–12): 1735–1751. Bibcode:2013GSAB..125.1735E. doi:10.1130/b30950.1.
  13. Bradley, Dwight C. (2008-12-01). "Passive margins through earth history". Earth-Science Reviews. 91 (1–4): 1–26. Bibcode:2008ESRv...91....1B. doi:10.1016/j.earscirev.2008.08.001.
  14. Gorczyk, W.; Smithies, H.; Korhonen, F.; Howard, H.; de Gromard, R. Q. (2015). "Ultra-hot Mesoproterozoic evolution of intracontinental central Australia". Geoscience Frontiers. 6 (1): 23–37. doi:10.1016/j.gsf.2014.03.001.
  15. Bryan, S. E.; Ferrari, L. (2013). "Large igneous provinces and silicic large igneous provinces: Progress in our understanding over the last 25 years". GSA Bulletin. 125 (7–8): 1055. doi:10.1130/B30820.1.
  16. Tollo, R. P.; Corriveau, L.; McLelland, J.; Bartholomew, M. J. (2004). "Proterozoic tectonic evolution of the Grenville orogen in North America: An introduction". In Tollo, R. P.; Corriveau, L.; McLelland, J.; Bartholomew, M. J. (eds.). Proterozoic tectonic evolution of the Grenville orogen in North America. Geological Society of America Memoir. 197. pp. 1–18. ISBN 978-0-8137-1197-3.
  17. Brasier, M.D. (1998). "A billion years of environmental stability and the emergence of eukaryotes: New data from northern Australia". Geology. 26 (6): 555. Bibcode:1998Geo....26..555B. doi:10.1130/0091-7613(1998)026<0555:ABYOES>2.3.CO;2.
  18. Veizer, J. (2005). "Celestial Climate Driver: A Perspective from Four Billion Years of the Carbon Cycle". Geoscience Canada. 32 (1). ISSN 1911-4850.
  19. Fiorella, R.; Sheldon, N. (2017). "Equable end Mesoproterozoic climate in the absence of high CO2". Geology. 45 (3): 231–234. doi:10.1130/G38682.1.
  20. Kah, L. C.; Riding, R. (2007). "Mesoproterozoic carbon dioxide levels inferred from calcified cyanobacteria". Geology. 35 (9): 799–802. doi:10.1130/G23680A.1.
  21. Hren, M. T.; Sheldon, N. D. (2019). "Terrestrial microbialites provide constraints on the mesoproterozoic atmosphere". The Depositional Record. doi:10.1002/dep2.79.
  22. Shaviv, Nir J. (2003). "The spiral structure of the Milky Way, cosmic rays, and ice age epochs on Earth". New Astronomy. 8 (1): 39–77. arXiv:astro-ph/0209252. Bibcode:2003NewA....8...39S. doi:10.1016/S1384-1076(02)00193-8.
  23. Planavsky, Noah J.; Reinhard, Christopher T.; Wang, Xiangli; Thomson, Danielle; McGoldrick, Peter; Rainbird, Robert H.; Johnson, Thomas; Fischer, Woodward W.; Lyons, Timothy W. (31 October 2014). "Low Mid-Proterozoic atmospheric oxygen levels and the delayed rise of animals" (PDF). Science. 346 (6209): 635–638. Bibcode:2014Sci...346..635P. doi:10.1126/science.1258410. ISSN 0036-8075. PMID 25359975.
  24. Eyles, N. (2008). "Glacio-epochs and the supercontinent cycle after ∼ 3.0 Ga: Tectonic boundary conditions for glaciation". Palaeogeography, Palaeoclimatology, Palaeoecology. 258 (1–2): 89–129. doi:10.1016/j.palaeo.2007.09.021.
  25. Kasting, J. F.; Ono, S. (2006). "Palaeoclimates: the first two billion years". Philosophical Transactions of the Royal Society of London B: Biological Sciences. 361 (1470): 917–929. doi:10.1098/rstb.2006.1839. ISSN 0962-8436. PMC 1868609. PMID 16754607.
  26. Catling, D. C.; Kasting, J. F. (2017). Atmospheric Evolution on Inhabited and Lifeless Worlds. Cambridge University Press. p. 291. ISBN 978-1-316-82452-8.
  27. Beraldi-Campesi, H. (2013). "Early life on land and the first terrestrial ecosystems". Ecological Processes. 2 (1): 1–17. doi:10.1186/2192-1709-2-1.
  28. Anbar, A. D.; Knoll, A. H. (2002). "Proterozoic Ocean Chemistry and Evolution: A Bioinorganic Bridge?". Science. 297 (5584): 1137–1142. Bibcode:2002Sci...297.1137A. CiteSeerX doi:10.1126/science.1069651. ISSN 0036-8075. PMID 12183619.
  29. Fennel, K.; Follows, M; Falkowski, P. G. (2005). "The co-evolution of the nitrogen, carbon and oxygen cycles in the Proterozoic ocean". American Journal of Science. 305 (6–8): 526–545. Bibcode:2005AmJS..305..526F. doi:10.2475/ajs.305.6-8.526. ISSN 0002-9599.
  30. Kipp, M. A.; Stüeken, E. E. (2017). "Biomass recycling and Earth's early phosphorus cycle". Science Advances. 3 (11): eaao4795. doi:10.1126/sciadv.aao4795. PMID 29202032.
  31. Parnell, J.; Sprinks, S.; Andrews, S.; Thayalan, W.; Bowden, S. (2015). "High Molybdenum availability for evolution in a Mesoproterozoic lacustrine environment". Nature Communications. 6 (6996). doi:10.1038/ncomms7996.
  32. Canfield, D. E. (1998). "A new model for Proterozoic ocean chemistry". Nature. 396 (6710): 450–453. Bibcode:1998Natur.396..450C. doi:10.1038/24839. ISSN 0028-0836.
  33. Lyons, Timothy W.; Reinhard, Christopher T.; Planavsky, Noah J. (2014). "The rise of oxygen in Earth's early ocean and atmosphere". Nature. 506 (7488): 307–315. Bibcode:2014Natur.506..307L. doi:10.1038/nature13068. PMID 24553238.
  34. Large, R.; Halpin, J. A.; Danyushevsky, L. V. (2014). "Trace element content of sedimentary pyrite as a new proxy for deep-time ocean–atmosphere evolution". Earth and Planetary Science Letters. 389: 209–220. doi:10.1016/j.epsl.2013.12.020.
  35. Slack, J. F.; Cannon, W. F. (2009). "Extraterrestrial demise of banded iron formations 1.85 billion years ago". Geology. 37 (11): 1011–1014. doi:10.1130/G30259A.1.
  36. De Baar, H. J. W.; German, C. R.; Elderfield, H; van Gaans, P. (1988). "Rare earth element distributions in anoxic waters of the Cariaco Trench". Geochimica et Cosmochimica Acta. 52 (5): 1203–1219. doi:10.1016/0016-7037(88)90275-X.
  37. Gallardo, V. A.; Espinoza, C. (2008). "Evolution of ocean color" (PDF). Proceedings of the International Society for Optical Engineering. Instruments, Methods, and Missions for Astrobiology XI. 7097: 1–7. Bibcode:2008SPIE.7097E..0GG. doi:10.1117/12.794742.
  38. Qiu, Jane (2014). "Oxygen fluctuations stalled life on Earth". Nature. doi:10.1038/nature.2014.15529. Retrieved 24 February 2017.
  39. Johnston, D. T. (2009). "Anoxygenic photosynthesis modulated Proterozoic oxygen and sustained Earth's middle age". Proceedings of the National Academy of Sciences. 106 (40): 16925–16929. Bibcode:2009PNAS..10616925J. doi:10.1073/pnas.0909248106. PMC 2753640. PMID 19805080.
  40. Partin, C. A.; Bekker, A.; Planavsky, N. J.; Scott, C. T.; Gill, B. C.; Li, C.; Podkovyrov, V.; Maslov, A.; Konhauser, K. O. (1 May 2013). "Large-scale fluctuations in Precambrian atmospheric and oceanic oxygen levels from the record of U in shales". Earth and Planetary Science Letters. 369–370: 284–293. Bibcode:2013E&PSL.369..284P. doi:10.1016/j.epsl.2013.03.031.
  41. Bekker, A.; Holland, H. D. (1 February 2012). "Oxygen overshoot and recovery during the early Paleoproterozoic". Earth and Planetary Science Letters. 317–318: 295–304. Bibcode:2012E&PSL.317..295B. doi:10.1016/j.epsl.2011.12.012.
  42. Schröder, S.; Bekker, A.; Beukes, N. J.; Strauss, H.; Van Niekerk, H. S. (1 April 2008). "Rise in seawater sulphate concentration associated with the Paleoproterozoic positive carbon isotope excursion: evidence from sulphate evaporites in the ∼2.2–2.1 Gyr shallow-marine Lucknow Formation, South Africa". Terra Nova. 20 (2): 108–117. Bibcode:2008TeNov..20..108S. doi:10.1111/j.1365-3121.2008.00795.x. ISSN 1365-3121.
  43. Kah, L. C.; Lyons, T. W.; Frank, T. D. (2004). "Low marine sulphate and protracted oxygenation of the Proterozoic biosphere". Nature. 438 (7010): 834–838. doi:10.1038/nature02974. PMID 15483609.
  44. Och, L. M.; Shields-Zhou, G. A. (2012). "The Neoproterozoic oxygenation event: Environmental perturbations and biogeochemical cycling". Earth-Science Reviews. 110 (1–4): 26–57. doi:10.1016/j.earscirev.2011.09.004.
  45. Lyons, Timothy W.; Reinhard, Christopher T. (2009). "An early productive ocean unfit for aerobics". Proceedings of the National Academy of Sciences. 106 (43): 18045–18046. Bibcode:2009PNAS..10618045L. doi:10.1073/pnas.0910345106. ISSN 0027-8424. PMC 2775325. PMID 19846788.
  46. Boenigk, Jens; Wodniok, Sabina; Glücksman, Edvard (2015-03-31). Biodiversity and Earth History. Springer. ISBN 9783662463949.
  47. Canfield, D. E.; Zhang, S.; Wang, H.; Wang, X.; Zhao, W.; Su, J.; Bjerrum, C. J.; Haxen, E. R.; Hammarlund, E. U. (2018). "A Mesoproterozoic iron formation". Proceedings of the National Academy of Sciences. 115 (17): 3895–3904. doi:10.1073/pnas.1720529115. PMC 5924912. PMID 29632173.
  48. Gueneli, N.; McKenna, A. M.; Ohkouchi, N.; Boreham, C. J.; Beghin, J.; Javaux, E. J.; Brocks, J. J. (2018). "1.1-billion-year-old porphyrins establish a marine ecosystem dominated by bacterial primary producers". Proceedings of the National Academy of Sciences. 115 (30): 6978–6986. doi:10.1073/pnas.1803866115. PMC 6064987. PMID 29987033.
  49. Javaux, E. J.; Lepot, K. (2018). "The Paleoproterozoic fossil record: Implications for the evolution of the biosphere during Earth's middle-age". Earth-Science Reviews. 176: 68–86. doi:10.1016/j.earscirev.2017.10.001.
  50. El Albani, A.; Bengtson, S.; Canfield, D. E.; Bekkler, A. (2010). "Large colonial organisms with coordinated growth in oxygenated environments 2.1 Gyr ago". Nature. 466 (7302): 100–104. doi:10.1038/nature09166. PMID 20596019.
  51. Reinhard, C. T.; Planavsky, N. J.; Robbins, L. J.; Partin, C. A.; Gill, B. C.; Lalonde, S. V.; Bekker, A.; Konhauser, K. O.; Lyons, T. W. (2013). "Proterozoic ocean redox and biogeochemical stasis". Proceedings of the National Academy of Sciences. 110 (14): 5357–5362. Bibcode:2013PNAS..110.5357R. doi:10.1073/pnas.1208622110. ISSN 0027-8424. PMC 3619314. PMID 23515332.
  52. Anbar, A. D. (2002). "Proterozoic ocean chemistry and evolution: a bioinorganic bridge". Science. 297 (5584): 1137–1142. Bibcode:2002Sci...297.1137A. doi:10.1126/science.1069651. PMID 12183619.
  53. Bengtson, S.; Sallstedt, T.; Belivanova, V.; Whitehouse, M. (2017). "Three-dimensional preservation of cellular and subcellular structures suggests 1.6 billion-year-old crown-group red algae". PLoS Biology. 15 (3): e2000735. doi:10.1371/journal.pbio.2000735. PMC 5349422. PMID 28291791.
  54. Bengtson, S.; Belivanova, V.; Rasmussen, B.; Whitehouse, M. (2009). "The controversial "Cambrian" fossils of the Vindhyan are real but more than a billion years older". Proceedings of the National Academy of Sciences. 106 (19): 7729–7734. doi:10.1073/pnas.0812460106. PMC 2683128. PMID 19416859.
  55. Hedges, S. B.; Blair, J. E.; Venturi, M. L.; Shoe, J. L. (2004). "A molecular timescale of eukaryote evolution and the rise of complex multicellular life". BMC Evolutionary Biology. 4 (2): 2. doi:10.1186/1471-2148-4-2. PMC 341452. PMID 15005799.
  56. Loron, C. C.; François, C.; Rainbird, R. H.; Turner, E. C.; Borensztajn, S.; Javaux, E. J. (2019). "Early fungi from the Proterozoic era in Arctic Canada". Nature. 70 (7760): 232–235. doi:10.1038/s41586-019-1217-0. PMID 31118507.
  57. Cooper, G. M. (2000). "The Origin and Evolution of Cells". The Cell: A Molecular Approach (2nd ed.). Sinauer Associates.
  58. Niklas, K. J. (2014). "The evolutionary-developmental origins of multicellularity". American Journal of Botany. 101 (1): 6–25. doi:10.3732/ajb.1300314. PMID 24363320.
  59. DNA Repair as the Primary Adaptive Function of Sex in Bacteria and Eukaryotes. pp. 1–50. Archived from the original on 29 October 2013.
  60. Egel, R.; Penny, D. (2007). "On the Origin of Meiosis in Eukaryotic Evolution: Coevolution of Meiosis and Mitosis from Feeble Beginnings". Genome Dynamics and Stability. 3 (249–288): 249–288. doi:10.1007/7050_2007_036. ISBN 978-3-540-68983-6.
  61. Martin, W.; Müller, M. (1998). "The hydrogen hypothesis for the first eukaryote". Nature. 392 (6671): 37–41. Bibcode:1998Natur.392...37M. doi:10.1038/32096. ISSN 0028-0836. PMID 9510246.
  62. Timmis, J. N.; Ayliffe, Michael A.; Huang, C. Y.; Martin, W. (2004). "Endosymbiotic gene transfer: organelle genomes forge eukaryotic chromosomes". Nature Reviews Genetics. 5 (2): 123–135. doi:10.1038/nrg1271. PMID 14735123.
  63. Mentel, Marek; Martin, William (27 August 2008). "Energy metabolism among eukaryotic anaerobes in light of Proterozoic ocean chemistry". Philosophical Transactions of the Royal Society of London B: Biological Sciences. 363 (1504): 2717–2729. doi:10.1098/rstb.2008.0031. ISSN 0962-8436. PMC 2606767. PMID 18468979.
  64. Moczydlowska, M.; Landing, E.; Zang, W.; Palacios, T. (2011). "Proterozoic phytoplankton and timing of Chlorophyte algae origins". Palaeontology. 54 (4): 721–733. doi:10.1111/j.1475-4983.2011.01054.x.
  65. Stanley, S. M. (2008). "Predation defeats competition on the seafloor". Paleobiology. 31 (1): 12. doi:10.1666/07026.1.
  66. Homann, M.; et al. (2018). "Microbial life and biogeochemical cycling on land 3,220 million years ago". Nature Geoscience. 11 (9): 665–671. doi:10.1038/s41561-018-0190-9.
  67. Baumgartner, R. J.; van Kranendonk, M. J.; et al. (2019). "Nano−porous pyrite and organic matter in 3.5-billion-year-old stromatolites record primordial life". Geology. 47 (11): 1039–1043. doi:10.1130/G46365.1.
  68. Watanabe, Yumiko; Martini, Jacques E. J.; Ohmoto, Hiroshi (30 November 2000). "Geochemical evidence for terrestrial ecosystems 2.6 billion years ago". Nature. 408 (6812): 574–578. Bibcode:2000Natur.408..574W. doi:10.1038/35046052. ISSN 0028-0836. PMID 11117742.
  69. Horodyski, R. J.; Knauth, L. P. (1994). "Life on land in the precambrian". Science. 263 (5146): 494–498. Bibcode:1994Sci...263..494H. doi:10.1126/science.263.5146.494. ISSN 0036-8075. PMID 17754880.
  70. Retallack, Gregory J.; Mindszenty, Andrea (1 April 1994). "Well preserved late Precambrian Paleosols from Northwest Scotland". Journal of Sedimentary Research. 64 (2a): 264–281. doi:10.1306/D4267D7A-2B26-11D7-8648000102C1865D. ISSN 1527-1404.
  71. Horodyski, R. J.; Knauth, L. P. (1994). "Life on land in the precambrian". Science. 263 (5146): 494–498. Bibcode:1994Sci...263..494H. doi:10.1126/science.263.5146.494. ISSN 0036-8075. PMID 17754880.
  72. Prave, Anthony Robert (2002). "Life on land in the Proterozoic: Evidence from the Torridonian rocks of northwest Scotland". Geology. 30 (9): 811. Bibcode:2002Geo....30..811P. doi:10.1130/0091-7613(2002)030<0811:LOLITP>2.0.CO;2. Retrieved 5 March 2016.
  73. Heckman, D. S.; Geiser, D. M.; Eidell, B. R.; Stauffer, R. L.; Kardos, N. L.; Hedges, S. B. (2001). "Molecular Evidence for the Early Colonization of Land by Fungi and Plants". Science. 293 (5532): 494–498. doi:10.1126/science.263.5146.494.
  74. Strother, P. K.; Battison, L.; Brasier, M. D.; Wellman, C. H. (2011). "Earth's earliest non-marine eukaryotes". Nature. 473 (7348): 505–509. doi:10.1038/nature09943.
  75. Knauth, L. P. (2009). "The late Precambrian greening of the Earth". Nature. 460 (7256): 728–732. doi:10.1038/nature08213. PMID 19587681.
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