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Geological history of oxygen: Difference between revisions

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<br />Stages 4 & 5 (0.85 Ga–present): O<sub>2</sub> sinks filled, the gas accumulates.<ref>http://rstb.royalsocietypublishing.org/content/361/1470/903.full.pdf</ref>]] <br />Stages 4 & 5 (0.85 Ga–present): O<sub>2</sub> sinks filled, the gas accumulates.<ref>http://rstb.royalsocietypublishing.org/content/361/1470/903.full.pdf</ref>]]


Before ] evolved, Earth's ] had no {{clarify span|free|date=December 2012}} ] (O<sub>2</sub>). Oxygen was first produced by ] ] organisms that emitted O<sub>2</sub> as a waste product. These organisms lived long before the first build-up of oxygen in the atmosphere,<ref>{{cite doi|10.1130/G22360.1}}</ref> perhaps as early as 3.5 billion years ago. The oxygen they produced would have almost instantly been removed from the atmosphere by weathering of reduced minerals, most notably iron. This 'mass rusting' led to the deposition of ]. Oxygen only began to persist in the atmosphere in small quantities about 50 million years before the start of the ].<ref name=Anabar2007>{{cite doi|10.1126/science.1140325}}</ref> This mass oxygenation of the atmosphere resulted in rapid buildup of free oxygen. At current atmospheric rates, today's concentration of oxygen could be produced by photosynthesisers in 2,000 years.<ref name=Dole1965>{{cite doi|10.1085/jgp.49.1.5}}</ref> Of course, in the ], photosynthesis was slower in the ], and the levels of O<sub>2</sub> attained were modest (<10% of today's) and probably fluctuated greatly; oxygen may even have disappeared from the atmosphere again around {{ma|1900}}<ref name='Frei2009'>{{cite doi|10.1038/nature08266}}</ref> These fluctuations in oxygen had little direct effect on life, with ]s not observed until the appearance of complex life around the start of the ] period, {{Ma|Cambrian|round=2}}.<ref name=Butterfield2007>{{cite doi|10.1111/j.1475-4983.2006.00613.x}}</ref> The presence of {{chem|O|2}} provided life with new opportunities. Aerobic metabolism is more efficient than anaerobic pathways, and the presence of oxygen undoubtedly created new possibilities for life to explore.<ref name="Freeman">{{cite book|last=Freeman|first=Scott|title=Biological Science, 2nd|publisher=Pearson – Prentice Hall| year=2005|location=Upper Saddle River, NJ|pages=214, 586|isbn=0-13-140941-7}}</ref>{{rp|214, 586}} An atmospheric oxygen level about 2% by volume is necessary to make compounds such as ]s, used by all animals; thus high atmospheric oxygen levels are needed for large life-forms.<ref name="Butterfield2009"/> Before ] evolved, Earth's ] had no free ] (O<sub>2</sub>). Oxygen was first produced by ] ] organisms that emitted O<sub>2</sub> as a waste product. These organisms lived long before the first build-up of oxygen in the atmosphere,<ref>{{cite doi|10.1130/G22360.1}}</ref> perhaps as early as 3.5 billion years ago. The oxygen they produced would have almost instantly been removed from the atmosphere by weathering of reduced minerals, most notably iron. This 'mass rusting' led to the deposition of ]. Oxygen only began to persist in the atmosphere in small quantities about 50 million years before the start of the ].<ref name=Anabar2007>{{cite doi|10.1126/science.1140325}}</ref> This mass oxygenation of the atmosphere resulted in rapid buildup of free oxygen. At current atmospheric rates, today's concentration of oxygen could be produced by photosynthesisers in 2,000 years.<ref name=Dole1965>{{cite doi|10.1085/jgp.49.1.5}}</ref> Of course, in the ], photosynthesis was slower in the ], and the levels of O<sub>2</sub> attained were modest (<10% of today's) and probably fluctuated greatly; oxygen may even have disappeared from the atmosphere again around {{ma|1900}}<ref name='Frei2009'>{{cite doi|10.1038/nature08266}}</ref> These fluctuations in oxygen had little direct effect on life, with ]s not observed until the appearance of complex life around the start of the ] period, {{Ma|Cambrian|round=2}}.<ref name=Butterfield2007>{{cite doi|10.1111/j.1475-4983.2006.00613.x}}</ref> The presence of {{chem|O|2}} provided life with new opportunities. Aerobic metabolism is more efficient than anaerobic pathways, and the presence of oxygen undoubtedly created new possibilities for life to explore.<ref name="Freeman">{{cite book|last=Freeman|first=Scott|title=Biological Science, 2nd|publisher=Pearson – Prentice Hall| year=2005|location=Upper Saddle River, NJ|pages=214, 586|isbn=0-13-140941-7}}</ref>{{rp|214, 586}} An atmospheric oxygen level about 2% by volume is necessary to make compounds such as ]s, used by all animals; thus high atmospheric oxygen levels are needed for large life-forms.<ref name="Butterfield2009"/>


Since the beginning of the ] period, {{chem|O|2}} levels have fluctuated between 15% and 30% of atmospheric volume.<ref name=Berner1999>{{cite pmid|10500106}}</ref> Towards the end of the ] period (about 300&nbsp;million years ago) atmospheric {{chem|O|2}} levels reached a maximum of 35% by volume,<ref name="Berner1999"/> which may have contributed to the large size of insects and amphibians at this time.<ref name=Butterfield2009>{{cite doi|10.1111/j.1472-4669.2009.00188.x}}</ref> Whilst human activities, such as the burning of ]s, have an impact on relative carbon dioxide concentrations, their impact on oxygen levels is less significant.<ref name="Emsley2001">{{cite book|title=Nature's Building Blocks: An A-Z Guide to the Elements|last=Emsley|first=John|publisher=Oxford University Press|year=2001|location=Oxford, England, UK|isbn=0-19-850340-7|chapter= Oxygen|pages=297–304}}</ref> Since the beginning of the ] period, {{chem|O|2}} levels have fluctuated between 15% and 30% of atmospheric volume.<ref name=Berner1999>{{cite pmid|10500106}}</ref> Towards the end of the ] period (about 300&nbsp;million years ago) atmospheric {{chem|O|2}} levels reached a maximum of 35% by volume,<ref name="Berner1999"/> which may have contributed to the large size of insects and amphibians at this time.<ref name=Butterfield2009>{{cite doi|10.1111/j.1472-4669.2009.00188.x}}</ref> Whilst human activities, such as the burning of ]s, have an impact on relative carbon dioxide concentrations, their impact on oxygen levels is less significant.<ref name="Emsley2001">{{cite book|title=Nature's Building Blocks: An A-Z Guide to the Elements|last=Emsley|first=John|publisher=Oxford University Press|year=2001|location=Oxford, England, UK|isbn=0-19-850340-7|chapter= Oxygen|pages=297–304}}</ref>

Revision as of 01:40, 4 December 2012

O2 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).
Stage 1 (3.85–2.45 Ga): Practically no O2 in the atmosphere.
Stage 2 (2.45–1.85 Ga): O2 produced, but absorbed in oceans & seabed rock.
Stage 3 (1.85–0.85 Ga): O2 starts to gas out of the oceans, but is absorbed by land surfaces and formation of ozone layer.
Stages 4 & 5 (0.85 Ga–present): O2 sinks filled, the gas accumulates.

Before photosynthesis evolved, Earth's atmosphere had no free oxygen (O2). Oxygen was first produced by photosynthetic prokaryotic organisms that emitted O2 as a waste product. These organisms lived long before the first build-up of oxygen in the atmosphere, perhaps as early as 3.5 billion years ago. The oxygen they produced would have almost instantly been removed from the atmosphere by weathering of reduced minerals, most notably iron. This 'mass rusting' led to the deposition of banded iron formations. Oxygen only began to persist in the atmosphere in small quantities about 50 million years before the start of the Great Oxygenation Event. This mass oxygenation of the atmosphere resulted in rapid buildup of free oxygen. At current atmospheric rates, today's concentration of oxygen could be produced by photosynthesisers in 2,000 years. Of course, in the absence of plants, photosynthesis was slower in the Precambrian, and the levels of O2 attained were modest (<10% of today's) and probably fluctuated greatly; oxygen may even have disappeared from the atmosphere again around 1,900 million years ago These fluctuations in oxygen had little direct effect on life, with mass extinctions not observed until the appearance of complex life around the start of the Cambrian period, 538.8 million years ago. The presence of O
2 provided life with new opportunities. Aerobic metabolism is more efficient than anaerobic pathways, and the presence of oxygen undoubtedly created new possibilities for life to explore. An atmospheric oxygen level about 2% by volume is necessary to make compounds such as collagens, used by all animals; thus high atmospheric oxygen levels are needed for large life-forms.

Since the beginning of the Cambrian period, O
2 levels have fluctuated between 15% and 30% of atmospheric volume. Towards the end of the Carboniferous period (about 300 million years ago) atmospheric O
2 levels reached a maximum of 35% by volume, which may have contributed to the large size of insects and amphibians at this time. Whilst human activities, such as the burning of fossil fuels, have an impact on relative carbon dioxide concentrations, their impact on oxygen levels is less significant.

Effects on life

The concentration of atmospheric oxygen is often cited as a possible contributor to large-scale evolutionary phenomena, such as the origin of the multicellular Ediacara biota, the Cambrian explosion, trends in animal body size, and other extinction and diversification events.

The large size of insects and amphibians in the Carboniferous period, where oxygen reached 35% of the atmosphere, has been attributed to the limiting role of diffusion in these organisms' metabolism. However, the biological basis for this correlation is not firm, and many lines of evidence show that oxygen concentration is not size-limiting in modern insects. Interestingly, there is no significant correlation between atmospheric oxygen and maximum body size elsewhere in the geological record. Ecological constraints can better explain the diminutive size of post-Carboniferous dragonflies - for instance, the appearance of flying competitors such as pterosaurs and birds and bats.

Rising oxygen concentrations have been cited as a driver for evolutionary diversification, although the physiological arguments behind such arguments are questionable, and a consistent pattern between oxygen levels and the rate of evolution is not clearly evident. The most celebrated link between oxygen and evolution occurs at the end of the last of the Snowball glaciations, where complex multicellular life is first found in the fossil record. Under low oxygen levels, regular 'nitrogen crises' could render the ocean inhospitable to life. More fundamentally, an oxygen concentration of at least 40% of present atmospheric levels is necessary for metazoans to produce biochemicals, such as collagen, that are essential to their existence. Models based on uniformitarian principles (i.e. extrapolating present-day ocean dynamics into deep time) suggest that such a level was only reached immediately before metazoa first appeared in the fossil record. Further, anoxic or otherwise chemically 'nasty' oceanic conditions that resemble those supposed to inhibit macroscopic life re-occur at intervals through the early Cambrian, and also in the late Cretaceous – with no apparent impact on lifeforms at these times. This might suggest that the geochemical signatures found in ocean sediments reflect the atmosphere in a different way before the Cambrian - perhaps as a result of the fundamentally different mode of nutrient cycling in the absence of planktivory.

External links

References

  1. http://rstb.royalsocietypublishing.org/content/361/1470/903.full.pdf
  2. Attention: This template ({{cite doi}}) is deprecated. To cite the publication identified by doi:10.1130/G22360.1, please use {{cite journal}} (if it was published in a bona fide academic journal, otherwise {{cite report}} with |doi=10.1130/G22360.1 instead.
  3. Attention: This template ({{cite doi}}) is deprecated. To cite the publication identified by doi:10.1126/science.1140325, please use {{cite journal}} (if it was published in a bona fide academic journal, otherwise {{cite report}} with |doi=10.1126/science.1140325 instead.
  4. Attention: This template ({{cite doi}}) is deprecated. To cite the publication identified by doi:10.1085/jgp.49.1.5, please use {{cite journal}} (if it was published in a bona fide academic journal, otherwise {{cite report}} with |doi=10.1085/jgp.49.1.5 instead.
  5. Attention: This template ({{cite doi}}) is deprecated. To cite the publication identified by doi:10.1038/nature08266, please use {{cite journal}} (if it was published in a bona fide academic journal, otherwise {{cite report}} with |doi=10.1038/nature08266 instead.
  6. ^ Attention: This template ({{cite doi}}) is deprecated. To cite the publication identified by doi:10.1111/j.1475-4983.2006.00613.x, please use {{cite journal}} (if it was published in a bona fide academic journal, otherwise {{cite report}} with |doi=10.1111/j.1475-4983.2006.00613.x instead.
  7. Freeman, Scott (2005). Biological Science, 2nd. Upper Saddle River, NJ: Pearson – Prentice Hall. pp. 214, 586. ISBN 0-13-140941-7.
  8. ^ Attention: This template ({{cite doi}}) is deprecated. To cite the publication identified by doi:10.1111/j.1472-4669.2009.00188.x, please use {{cite journal}} (if it was published in a bona fide academic journal, otherwise {{cite report}} with |doi=10.1111/j.1472-4669.2009.00188.x instead.
  9. ^ Attention: This template ({{cite pmid}}) is deprecated. To cite the publication identified by PMID 10500106, please use {{cite journal}} with |pmid=10500106 instead.
  10. Emsley, John (2001). "Oxygen". Nature's Building Blocks: An A-Z Guide to the Elements. Oxford, England, UK: Oxford University Press. pp. 297–304. ISBN 0-19-850340-7.
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