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Paleoclimatology(British spelling,palaeoclimatology) is the scientific study ofclimatespredating the invention ofmeteorological instruments,when no direct measurement data were available.[1]As instrumental records only span a tiny part ofEarth's history,the reconstruction of ancient climate is important to understand natural variation and the evolution of the current climate.

Paleoclimatology uses a variety ofproxymethods fromEarthandlife sciencesto obtain data previously preserved withinrocks,sediments,boreholes,ice sheets,tree rings,corals,shells,andmicrofossils.Combined with techniques to date the proxies, the paleoclimate records are used to determine the past states ofEarth's atmosphere.

The scientific field of paleoclimatology came to maturity in the 20th century. Notable periods studied by paleoclimatologists include the frequentglaciationsthat Earth has undergone, rapid cooling events like theYounger Dryas,and the rapid warming during thePaleocene–Eocene Thermal Maximum.Studies of past changes in the environment and biodiversity often reflect on the current situation, specifically the impact of climate onmass extinctionsand biotic recovery and currentglobal warming.[2][3]

History

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Main articles:History of climate change scienceandHistorical climatology

Notions of a changing climate most likely evolved inancient Egypt,Mesopotamia,theIndus ValleyandChina,where prolonged periods of droughts and floods were experienced.[4]In the seventeenth century,Robert Hookepostulated that fossils of giant turtles found inDorsetcould only be explained by a once warmer climate, which he thought could be explained by a shift in Earth's axis.[4]Fossils were, at that time, often explained as a consequence of a biblical flood.[5]Systematic observations of sunspots started by amateur astronomerHeinrich Schwabein the early 19th century, starting a discussion of the Sun's influence on Earth's climate.[4]

The scientific study of paleoclimatology began to take shape in the early 19th century, when discoveries about glaciations and natural changes in Earth's past climate helped to understand thegreenhouse effect.It was only in the 20th century that paleoclimatology became a unified scientific field. Before, different aspects of Earth's climate history were studied by a variety of disciplines.[5]At the end of the 20th century, the empirical research into Earth's ancient climates started to be combined with computer models of increasing complexity. A new objective also developed in this period: finding ancient analog climates that could provide information about currentclimate change.[5]

Reconstructing ancient climates

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Preliminary results from aSmithsonian Institutionproject, showing Earth's average surface temperature over the past 500 million years[6][7]
Palaeotemperature graphs placed together
The oxygen content in the atmosphere over the last billion years
Main article:Proxy (climate)

Paleoclimatologists employ a wide variety of techniques to deduce ancient climates. The techniques used depend on which variable has to be reconstructed (this could betemperature,precipitation,or something else) and how long ago the climate of interest occurred. For instance, the deep marine record, the source of most isotopic data, exists only on oceanic plates, which are eventuallysubducted;the oldest remaining material is200million yearsold. Older sediments are also more prone to corruption bydiagenesis.This is due to the millions of years of disruption experienced by the rock formations, such as pressure, tectonic activity, and fluid flowing. These factors often result in a lack of quality or quantity of data, which causes resolution and confidence in the data decrease over time.

Specific techniques used to make inferences on ancient climate conditions are the use of lake sediment cores and speleothems. These utilize an analysis of sediment layers and rock growth formations respectively, amongst element-dating methods utilizing oxygen, carbon and uranium.

Proxies for climate

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Direct Quantitative Measurements

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The Direct Quantitative Measurements method is the most direct approach to understand the change in a climate. Comparisons between recent data to older data allows a researcher to gain a basic understanding of weather and climate changes within an area. There is a disadvantage to this method. Data of the climate only started being recorded in the mid-1800s. This means that researchers can only utilize 150 years of data. That is not helpful when trying to map the climate of an area 10,000 years ago. This is where more complex methods can be used.[8]

Ice

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Mountainglaciersand the polarice caps/ice sheetsprovide much data in paleoclimatology. Ice-coring projects in the ice caps ofGreenlandandAntarcticahave yielded data going back several hundred thousand years, over 800,000 years in the case of theEPICAproject.

  • Air trapped within fallensnowbecomes encased in tiny bubbles as the snow is compressed into ice in the glacier under the weight of later years' snow. The trapped air has proven a tremendously valuable source for direct measurement of the composition of air from the time the ice was formed.
  • Layering can be observed because of seasonal pauses in ice accumulation and can be used to establish chronology, associating specific depths of the core with ranges of time.
  • Changes in the layering thickness can be used to determine changes in precipitation or temperature.
  • Oxygen-18quantity changes (δ18O) in ice layers represent changes in average ocean surface temperature. Water molecules containing the heavier O-18 evaporate at a higher temperature than water molecules containing the normalOxygen-16isotope. The ratio of O-18 to O-16 will be higher as temperature increases but it also depends on factors such as water salinity and the volume of water locked up in ice sheets. Various cycles in isotope ratios have been detected.
  • Pollenhas been observed in the ice cores and can be used to understand which plants were present as the layer formed. Pollen is produced in abundance and its distribution is typically well understood. A pollen count for a specific layer can be produced by observing the total amount of pollen categorized by type (shape) in a controlled sample of that layer. Changes in plant frequency over time can be plotted through statistical analysis of pollen counts in the core. Knowing which plants were present leads to an understanding of precipitation and temperature, and types of fauna present.Palynologyincludes the study of pollen for these purposes.
  • Volcanic ashis contained in some layers, and can be used to establish the time of the layer's formation. Volcanic events distribute ash with a unique set of properties (shape and color of particles, chemical signature). Establishing the ash's source will give a time period to associate with the layer of ice.

A multinational consortium, theEuropean Project for Ice Coring in Antarctica(EPICA), has drilled an ice core in Dome C on the East Antarctic ice sheet and retrieved ice from roughly 800,000 years ago.[9]The international ice core community has, under the auspices of International Partnerships in Ice Core Sciences (IPICS), defined a priority project to obtain the oldest possible ice core record from Antarctica, an ice core record reaching back to or towards 1.5 million years ago.[10]

Dendroclimatology

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Main article:Dendroclimatology

Climatic information can be obtained through an understanding of changes in tree growth. Generally, trees respond to changes in climatic variables by speeding up or slowing down growth, which in turn is generally reflected by a greater or lesser thickness in growth rings. Different species however, respond to changes in climatic variables in different ways. A tree-ring record is established by compiling information from many living trees in a specific area. This is done by comparing the number, thickness, ring boundaries, and pattern matching of tree growth rings.

The differences in thickness displayed in the growth rings in trees can often indicate the quality of conditions in the environment, and the fitness of the tree species evaluated. Different species of trees will display different growth responses to the changes in the climate. An evaluation of multiple trees within the same species, along with one of trees in different species, will allow for a more accurate analysis of the changing variables within the climate and how they affected the surrounding species.[11]

Older intact wood that has escaped decay can extend the time covered by the record by matching the ring depth changes to contemporary specimens. By using that method, some areas have tree-ring records dating back a few thousand years. Older wood not connected to a contemporary record can be dated generally with radiocarbon techniques. A tree-ring record can be used to produce information regarding precipitation, temperature, hydrology, and fire corresponding to a particular area.

Sedimentary content

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On a longer time scale, geologists must refer to the sedimentary record for data.

  • Sediments, sometimes lithified to form rock, may contain remnants of preserved vegetation, animals, plankton, orpollen,which may be characteristic of certain climatic zones.
  • Biomarker molecules such as thealkenonesmay yield information about their temperature of formation.
  • Chemical signatures, particularlyMg/Caratio ofcalciteinForaminiferatests, can be used to reconstruct past temperature.
  • Isotopic ratios can provide further information. Specifically, theδ18Orecord responds to changes in temperature and ice volume, and theδ13Crecord reflects a range of factors, which are often difficult to disentangle.
Sea floor core sample labelled to identify the exact spot on the sea floor where the sample was taken. Sediments from nearby locations can show significant differences in chemical and biological composition.
Sedimentary facies

On a longer time scale, the rock record may show signs ofsea levelrise and fall, and features such as"fossilised" sand dunescan be identified. Scientists can get a grasp of long-term climate by studyingsedimentary rockgoing back billions of years. The division of Earth history into separate periods is largely based on visible changes in sedimentary rock layers that demarcate major changes in conditions. Often, they include major shifts in climate.

Sclerochronology

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Corals (see alsosclerochronology)

Coral “rings'' share similar evidence of growth to that of trees, and thus can be dated in similar ways. A primary difference is their environments and the conditions within those that they respond to. Examples of these conditions for coral include water temperature, freshwater influx, changes in pH, and wave disturbances. From there, specialized equipment, such as the Advanced Very High Resolution Radiometer (AVHRR) instrument, can be used to derive thesea surface temperatureand water salinity from the past few centuries. Theδ18Oofcorallinered algae provides a useful proxy of the combined sea surface temperature and sea surface salinity at high latitudes and the tropics, where many traditional techniques are limited.[12][13]

Landscapes and landforms

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Withinclimatic geomorphology,one approach is to studyrelict landformsto infer ancient climates.[14]Being often concerned about past climates climatic geomorphology is considered sometimes to be a theme ofhistorical geology.[15]Evidence of these past climates to be studied can be found in the landforms they leave behind. Examples of these landforms are those such as glacial landforms (moraines, striations), desert features (dunes, desert pavements), and coastal landforms (marine terraces, beach ridges).[16]Climatic geomorphology is of limited use to study recent (Quaternary,Holocene) large climate changes since there are seldom discernible in the geomorphological record.[17]

Timing of proxies

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The field ofgeochronologyhas scientists working on determining how old certain proxies are. For recent proxy archives of tree rings and corals the individual year rings can be counted, and an exact year can be determined.Radiometric datinguses the properties of radioactive elements in proxies. In older material, more of the radioactive material will have decayed and the proportion of different elements will be different from newer proxies. One example of radiometric dating isradiocarbon dating.In the air,cosmic raysconstantly convert nitrogen into a specific radioactive carbon isotope,14C.When plants then use this carbon to grow, this isotope is not replenished anymore and starts decaying. The proportion of 'normal' carbon and Carbon-14 gives information of how long the plant material has not been in contact with the atmosphere.[18]

Notable climate events in Earth history

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See also:List of periods and events in climate history,Timeline of glaciation,andHistory of Earth

Knowledge of precise climatic events decreases as the record goes back in time, but some notable climate events are known:

History of the atmosphere

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See also:Atmosphere of EarthandHistory of Earth

Earliest atmosphere

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Thefirst atmospherewould have consisted of gases in thesolar nebula,primarilyhydrogen.In addition, there would probably have been simplehydridessuch as those now found in gas giants likeJupiterandSaturn,notablywatervapor,methane,andammonia.As the solar nebula dissipated, the gases would have escaped, partly driven off by thesolar wind.[19]

Second atmosphere

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The next atmosphere, consisting largely ofnitrogen,carbon dioxide,and inert gases, was produced by outgassing fromvolcanism,supplemented by gases produced during thelate heavy bombardmentof Earth by hugeasteroids.[19]A major part of carbon dioxide emissions were soon dissolved in water and built up carbonate sediments.

Water-related sediments have been found dating from as early as 3.8 billion years ago.[20]About 3.4 billion years ago, nitrogen was the major part of the then stable "second atmosphere". An influence of life has to be taken into account rather soon in the history of the atmosphere because hints of early life forms have been dated to as early as 3.5 to 4.3 billion years ago.[21]The fact that it is not perfectly in line with the 30% lower solar radiance (compared to today) of the early Sun has been described as the "faint young Sun paradox".

The geological record, however, shows a continually relatively warm surface during the complete earlytemperature recordof Earth with the exception of one cold glacial phase about 2.4 billion years ago. In the lateArchaeaneon, an oxygen-containing atmosphere began to develop, apparently from photosynthesizingcyanobacteria(seeGreat Oxygenation Event) which have been found asstromatolitefossils from 2.7 billion years ago. The early basic carbon isotopy (isotope ratioproportions) was very much in line with what is found today, suggesting that the fundamental features of thecarbon cyclewere established as early as 4 billion years ago.

Third atmosphere

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The constant rearrangement of continents byplate tectonicsinfluences the long-term evolution of the atmosphere by transferring carbon dioxide to and from large continental carbonate stores. Free oxygen did not exist in the atmosphere until about 2.4 billion years ago, during theGreat Oxygenation Event,and its appearance is indicated by the end of thebanded iron formations.Until then, any oxygen produced by photosynthesis was consumed by oxidation of reduced materials, notably iron. Molecules of free oxygen did not start to accumulate in the atmosphere until the rate of production of oxygen began to exceed the availability of reducing materials. That point was a shift from areducingatmosphere to anoxidizingatmosphere. O2showed major variations until reaching a steady state of more than 15% by the end of the Precambrian.[22]The following time span was thePhanerozoiceon, during which oxygen-breathingmetazoan lifeforms began to appear.

The amount of oxygen in the atmosphere has fluctuated over the last 600 million years, reaching a peak of 35%[23]during theCarboniferousperiod, significantly higher than today's 21%. Two main processes govern changes in the atmosphere: plantsuse carbon dioxide from the atmosphere,releasing oxygen and the breakdown ofpyriteandvolcanic eruptionsreleasesulfurinto the atmosphere, which oxidizes and hence reduces the amount of oxygen in the atmosphere. However, volcanic eruptions also release carbon dioxide, which plants can convert to oxygen. The exact cause of the variation of the amount of oxygen in the atmosphere is not known. Periods with much oxygen in the atmosphere are associated with rapid development of animals. Today's atmosphere contains 21% oxygen, which is high enough for rapid development of animals.[24]

Climate during geological ages

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Timeline of glaciations, shown in blue
See also:Timeline of glaciation

In 2020 scientists published a continuous, high-fidelityrecord of variations in Earth's climate during the past 66 million yearsand identified fourclimate states,separated by transitions that include changing greenhouse gas levels and polar ice sheets volumes. They integrated data of various sources. The warmest climate state since the time of the dinosaur extinction, "Hothouse", endured from 56 Mya to 47 Mya and was ~14 °C warmer than average modern temperatures.[25][26]

Precambrian climate

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Main article:Precambrian

The Precambrian took place between the time when Earth first formed 4.6 billion years (Ga) ago, and 542 million years ago. The Precambrian can be split into two eons, the Archean and the Proterozoic, which can be further subdivided into eras.[27]The reconstruction of the Precambrian climate is difficult for various reasons including the low number of reliable indicators and a, generally, not well-preserved or extensive fossil record (especially when compared to the Phanerozoic eon).[28][29]Despite these issues, there is evidence for a number of major climate events throughout the history of the Precambrian:The Great Oxygenation Event,which started around 2.3 Ga ago (the beginning of the Proterozoic) is indicated bybiomarkerswhich demonstrate the appearance of photosynthetic organisms. Due to the high levels of oxygen in the atmosphere from the GOE,CH4levels fell rapidly cooling the atmosphere causing the Huronian glaciation. For about 1 Ga after the glaciation (2-0.8 Ga ago), the Earth likely experienced warmer temperatures indicated by microfossils of photosynthetic eukaryotes, and oxygen levels between 5 and 18% of the Earth's current oxygen level. At the end of the Proterozoic, there is evidence of global glaciation events of varying severity causing a 'Snowball Earth'.[30]Snowball Earth is supported by different indicators such as, glacial deposits, significant continental erosion calledthe Great Unconformity,and sedimentary rocks called cap carbonates that form after a deglaciation episode.[31]

Phanerozoic climate

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Changes inoxygen-18ratios over the last 500 million years, indicating environmental change
Main article:Phanerozoic

Major drivers for the preindustrial ages have been variations of the Sun, volcanic ashes and exhalations, relative movements of the Earth towards the Sun, and tectonically induced effects as for major sea currents, watersheds, and ocean oscillations. In the early Phanerozoic, increased atmospheric carbon dioxide concentrations have been linked to driving or amplifying increased global temperatures.[32]Royer et al. 2004[33]found a climate sensitivity for the rest of the Phanerozoic which was calculated to be similar to today's modern range of values.

The difference in global mean temperatures between a fully glacial Earth and an ice free Earth is estimated at 10 °C, though far larger changes would be observed at high latitudes and smaller ones at low latitudes.[citation needed]One requirement for the development of large scale ice sheets seems to be the arrangement of continental land masses at or near the poles. The constant rearrangement of continents byplate tectonicscan also shape long-term climate evolution. However, the presence or absence of land masses at the poles is not sufficient to guarantee glaciations or exclude polar ice caps. Evidence exists of past warm periods in Earth's climate when polar land masses similar toAntarcticawere home todeciduousforests rather than ice sheets.

The relatively warm local minimum betweenJurassicandCretaceousgoes along with an increase of subduction and mid-ocean ridge volcanism[34]due to the breakup of thePangeasupercontinent.

Superimposed on the long-term evolution between hot and cold climates have been many short-term fluctuations in climate similar to, and sometimes more severe than, the varying glacial and interglacial states of the presentice age.Some of the most severe fluctuations, such as thePaleocene-Eocene Thermal Maximum,may be related torapid climate changesdue to sudden collapses of naturalmethane clathratereservoirs in the oceans.[35]

A similar, single event of induced severe climate change after ameteorite impacthas been proposed as reason for theCretaceous–Paleogene extinction event.Other major thresholds are thePermian-Triassic,andOrdovician-Silurian extinction eventswith various reasons suggested.

Quaternary climate

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Ice core data for the past 800,000 years (x-axis values represent "age before 1950", so today's date is on the left side of the graph and older time on the right). Blue curve is temperature,[36]red curve is atmospheric CO2concentrations,[37]and brown curve is dust fluxes.[38][39]Note length of glacial-interglacial cycles averages ~100,000 years.
Holocene temperature variations
Main article:Quaternary
See also:List of large-scale temperature reconstructions of the last 2,000 years

The Quaternarygeological periodincludes the current climate. There has been a cycle ofice agesfor the past 2.2–2.1 million years (starting before the Quaternary in the lateNeogenePeriod).

Note in the graphic on the right the strong 120,000-year periodicity of the cycles, and the striking asymmetry of the curves. This asymmetry is believed to result from complex interactions of feedback mechanisms. It has been observed that ice ages deepen by progressive steps, but the recovery to interglacial conditions occurs in one big step.

The graph on the left shows the temperature change over the past 12,000 years, from various sources; the thick black curve is an average.

Climate forcings

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Main article:Climate forcing

Climate forcing is the difference betweenradiant energy(sunlight) received by the Earth and theoutgoing longwave radiationback to space. Suchradiative forcingis quantified based on the CO2amount in thetropopause,in units of watts per square meter to the Earth's surface.[40]Dependent on theradiative balanceof incoming and outgoing energy, the Earth either warms up or cools down. Earth radiative balance originates from changes in solarinsolationand the concentrations ofgreenhouse gasesandaerosols.Climate change may be due to internal processes in Earth sphere's and/or following external forcings.[41]

One example of a way this can be applied to study climatology is analyzing how the varying concentrations of CO2 affect the overall climate. This is done by using various proxies to estimate past greenhouse gas concentrations and compare those to that of the present day. Researchers are then able to assess their role in progression of climate change throughout Earth’s history.[42]

Internal processes and forcings

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The Earth'sclimate systeminvolves theatmosphere,biosphere,cryosphere,hydrosphere,andlithosphere,[43]and the sum of these processes from Earth's spheres is what affects the climate. Greenhouse gasses act as the internal forcing of the climate system. Particular interests in climate science and paleoclimatology focus on the study of Earthclimate sensitivity,in response to the sum of forcings. Analyzing the sum of these forcings contributes to the ability of scientists to make broad conclusive estimates on the Earth’s climate system. These estimates include the evidence for systems such as long term climate variability (eccentricity, obliquity precession), feedback mechanisms (Ice-Albedo Effect), and anthropogenic influence.[44]

Examples:

External forcings

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  • TheMilankovitch cyclesdetermine Earth distance and position to the Sun. The solar insolation is the total amount of solar radiation received by Earth.
  • Volcanic eruptions are considered an internal forcing.[45]
  • Human changes of the composition of the atmosphere or land use.[45]
  • Human activities causing anthropogenic greenhouse gas emissions leading to global warming and associated climate changes.
  • Large asteroids that have cataclysmic impacts on Earth’s climate are considered external forcings.[46]

Mechanisms

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On timescales of millions of years, the uplift of mountain ranges and subsequentweatheringprocesses of rocks and soils and thesubductionoftectonic plates,are an important part of thecarbon cycle.[47][48][49]The weatheringsequesters CO2,by the reaction of minerals with chemicals (especiallysilicateweathering with CO2) and thereby removing CO2from the atmosphere and reducing the radiative forcing. The opposite effect isvolcanism,responsible for the naturalgreenhouse effect,by emitting CO2into the atmosphere, thus affectingglaciation(Ice Age) cycles.Jim Hansensuggested that humans emit CO210,000 times faster than natural processes have done in the past.[50]

Ice sheetdynamics and continental positions (and linked vegetation changes) have been important factors in the long term evolution of the Earth's climate.[51]There is also a close correlation between CO2and temperature, where CO2has a strong control over global temperatures in Earth's history.[52]

See also

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References

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Notes

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  1. ^Bradley, Raymond (2015).Paleoclimatology: Reconstructing Climates of the Quaternary.Oxford: Elsevier. p. 1.ISBN978-0-12-386913-5.
  2. ^Sahney, S. & Benton, M.J. (2008)."Recovery from the most profound mass extinction of all time".Proceedings of the Royal Society B: Biological Sciences.275(1636): 759–65.doi:10.1098/rspb.2007.1370.PMC2596898.PMID18198148.
  3. ^Cronin 2010,p. 1
  4. ^abcFairbridge, Rhodes (31 October 2008). "history of paleoclimatology". In Gornitz, Vivien (ed.).Encyclopedia of Paleoclimatology and Ancient Environments.Springer Nature. pp. 414–426.ISBN978-1-4020-4551-6.
  5. ^abcCronin, Thomas M. (1999).Principles of Paleoclimatology.Columbia University Press. pp. 8–10.ISBN9780231503044.
  6. ^"What's the hottest Earth's ever been?".www.climate.gov.NOAA.22 November 2023.Retrieved3 June2024.
  7. ^Soul, Laura (24 April 2018)."Leading Scientists Convene to Chart 500M Years of Global Climate Change".Smithsonian Magazine.Retrieved3 June2024.
  8. ^Saltzman, Barry (2002).Dynamical Paleoclimatology: Generalized Theory of Global Climate Change.Google Scholar: Academic Press.ISBN978-0-12-617331-4.Retrieved1 April2024.
  9. ^Jouzel, Jean; Masson-Delmotte, V.; Cattani, O.; Dreyfus, G.; Falourd, S.; Hoffmann, G.; Minster, B.; Nouet, J.; et al. (10 August 2007)."Orbital and Millennial Antarctic Climate Variability over the Past 800,000 Years"(PDF).Science.317(5839): 793–796.Bibcode:2007Sci...317..793J.doi:10.1126/science.1141038.PMID17615306.S2CID30125808.
  10. ^"Page 1 1 International Partnerships in Ice Core Sciences (IPICS) The oldest ice core: A 1.5 million year record of climate and greenhouse gases from Antarctica".Retrieved22 September2011.
  11. ^Frank, David; Esper, Jan; Zorita, Eduardo; Wilson, Rob (14 May 2010)."A noodle, hockey stick, and spaghetti plate: a perspective on high-resolution paleoclimatology".WIREs Climate Change.1(4): 507–516.Bibcode:2010WIRCC...1..507F.doi:10.1002/wcc.53.ISSN1757-7780.
  12. ^Halfar, J.; Steneck, R.S.; Joachimski, M.; Kronz, A.; Wanamaker, A.D. (2008). "Coralline red algae as high-resolution climate recorders".Geology.36(6): 463.Bibcode:2008Geo....36..463H.doi:10.1130/G24635A.1.S2CID129376515.
  13. ^Cobb, K.; Charles, C. D.; Cheng, H; Edwards, R. L. (2003). "El Nino/Southern Oscillation and tropical Pacific climate during the past millennium".Nature.424(6946): 271–6.Bibcode:2003Natur.424..271C.doi:10.1038/nature01779.PMID12867972.S2CID6088699.
  14. ^Gutiérrez, Mateo; Gutiérrez, Francisco (2013)."Climatic Geomorphology".Treatise on Geomorphology.Vol. 13. pp. 115–131.
  15. ^Gutiérrez, Mateo, ed. (2005). "Chapter 1 Climatic geomorphology".Developments in Earth Surface Processes.Vol. 8. pp. 3–32.doi:10.1016/S0928-2025(05)80051-3.ISBN978-0-444-51794-4.
  16. ^Douglas, Peter; Brenner, Mark; Curtis, Jason (27 February 2016)."Methods and future directions for paleoclimatology in the Maya Lowlands. Global and Planetary Change".doi:10.1016/j.gloplacha.2015.07.008.
  17. ^Goudie, A.S.(2004). "Climatic geomorphology". In Goudie, A.S. (ed.).Encyclopedia of Geomorphology.pp. 162–164.
  18. ^Cronin 2010,pp. 32–34.
  19. ^abZahnle, K.;Schaefer, L.;Fegley, B. (2010)."Earth's Earliest Atmospheres".Cold Spring Harbor Perspectives in Biology.2(10): a004895.doi:10.1101/cshperspect.a004895.PMC2944365.PMID20573713.
  20. ^B. Windley:The Evolving Continents.Wiley Press, New York 1984
  21. ^J. Schopf:Earth's Earliest Biosphere: Its Origin and Evolution.Princeton University Press, Princeton, N.J., 1983
  22. ^Christopher R. Scotese,Back to Earth History: Summary Chart for the Precambrian,Paleomar Project
  23. ^Beerling, David(2007).The emerald planet: how plants changed Earth's history.Oxford University press. p.47.ISBN9780192806024.
  24. ^Peter Ward:[1]Out of Thin Air: Dinosaurs, Birds, and Earth's Ancient Atmosphere
  25. ^"High-fidelity record of Earth's climate history puts current changes in context".phys.org.Retrieved8 October2020.
  26. ^Westerhold, Thomas; Marwan, Norbert; Drury, Anna Joy; Liebrand, Diederik; Agnini, Claudia; Anagnostou, Eleni; Barnet, James S. K.; Bohaty, Steven M.; Vleeschouwer, David De; Florindo, Fabio; Frederichs, Thomas; Hodell, David A.; Holbourn, Ann E.; Kroon, Dick; Lauretano, Vittoria; Littler, Kate; Lourens, Lucas J.; Lyle, Mitchell; Pälike, Heiko; Röhl, Ursula; Tian, Jun; Wilkens, Roy H.; Wilson, Paul A.; Zachos, James C. (11 September 2020)."An astronomically dated record of Earth's climate and its predictability over the last 66 million years"(PDF).Science.369(6509): 1383–1387.Bibcode:2020Sci...369.1383W.doi:10.1126/science.aba6853.hdl:11577/3351324.ISSN0036-8075.PMID32913105.S2CID221593388.Retrieved8 October2020.
  27. ^Goddéris, Yves; Ramstein, Gilles; Le Hir, Guillaume (2021), Ramstein, Gilles; Landais, Amaëlle; Bouttes, Nathaelle; Sepulchre, Pierre (eds.),"The Precambrian Climate",Paleoclimatology,Frontiers in Earth Sciences, Cham: Springer International Publishing, pp. 343–358,doi:10.1007/978-3-030-24982-3_26,ISBN978-3-030-24982-3,retrieved9 February2024
  28. ^Goddéris, Yves; Ramstein, Gilles; Le Hir, Guillaume (2021), Ramstein, Gilles; Landais, Amaëlle; Bouttes, Nathaelle; Sepulchre, Pierre (eds.),"The Precambrian Climate",Paleoclimatology,Frontiers in Earth Sciences, Cham: Springer International Publishing, pp. 343–358,doi:10.1007/978-3-030-24982-3_26,ISBN978-3-030-24982-3,retrieved9 February2024
  29. ^Cosgrove, Grace I. E.; Colombera, Luca; Mountney, Nigel P. (1 March 2024)."The Precambrian continental record: A window into early Earth environments".Precambrian Research.402:107286.Bibcode:2024PreR..40207286C.doi:10.1016/j.precamres.2023.107286.ISSN0301-9268.
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