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

Paleoclimatology uses a variety of proxy methods from Earth and life sciences to obtain data previously preserved within rocks, sediments, boreholes, ice sheets, tree rings, corals, shells, and microfossils. Combined with techniques to date the proxies, the paleoclimate records are used to determine the past states of Earth's atmosphere.

The scientific field of paleoclimatology came to maturity in the 20th century. Notable periods studied by paleoclimatologists include the frequent glaciations that Earth has undergone, rapid cooling events like the Younger Dryas, and the rapid warming during the Paleocene–Eocene Thermal Maximum. Studies of past changes in the environment and biodiversity often reflect on the current situation, specifically the impact of climate on mass extinctions and biotic recovery and current global warming.[2][3]

History

Main articles: History of climate change science and Historical climatology

Notions of a changing climate probably evolved in ancient Egypt, Mesopotamia, the Indus Valley and China, where prolonged periods of droughts and floods were experienced.[4] In the seventeenth century, Robert Hooke postulated that fossils of giant turtles found in Dorset could only be explained by a once warmer climate, which he thought could be explained by a shift in Earth's axis.[4] Fossils were in that time often explained as a consequence of a Biblical flood.[5] Systematic observations of sunspots started by amateur astronomer Heinrich Schwabe in the early 19th century, starting a discussion of the Sun's influence on Earth's climate.[4]

The scientific study field of paleoclimatology began to further take shape in the early 19th century, when discoveries about glaciations and natural changes in Earth's past climate helped to understand the greenhouse 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 current climate change.[5]

Reconstructing ancient climates

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 be temperature, precipitation,or something else) and on 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 eventually subducted: the oldest remaining material is 200 million years old. Older sediments are also more prone to corruption by diagenesis. Resolution and confidence in the data decrease over time.

Proxies for climate

Ice

Mountain glaciers and the polar ice caps/ice sheets provide much data in paleoclimatology. Ice-coring projects in the ice caps of Greenland and Antarctica have yielded data going back several hundred thousand years, over 800,000 years in the case of the EPICA project.

  • Air trapped within fallen snow becomes 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-18 quantity 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 normal Oxygen-16 isotope. The ratio of O-18 to O-16 will be higher as temperature increases. It also depends on other factors such as the water's salinity and the volume of water locked up in ice sheets. Various cycles in those isotope ratios have been detected.
  • Pollen has 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. Palynology includes the study of pollen for these purposes.
  • Volcanic ash is contained in some layers, and can be used to establish the time of the layer's formation. Each volcanic event distributed ash with a unique set of properties (shape and color of particles, chemical signature). Establishing the ash's source will establish a range of time to associate with layer of ice.

A multinational consortium, the European 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.[6] 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.[7]

Dendroclimatology

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.

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

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, or pollen, which may be characteristic of certain climatic zones.
  • Biomarker molecules such as the alkenones may yield information about their temperature of formation.
  • Chemical signatures, particularly Mg/Ca ratio of calcite in Foraminifera tests, can be used to reconstruct past temperature.
  • Isotopic ratios can provide further information. Specifically, the δ18O record responds to changes in temperature and ice volume, and the δ13C record 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 of sea level rise and fall, and features such as "fossilized" sand dunes can be identified. Scientists can get a grasp of long-term climate by studying sedimentary rock going 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

Corals (see also sclerochronology)

Coral "rings" are similar to tree rings except that they respond to different things, such as the water temperature, freshwater influx, pH changes, and wave action. From there, certain equipment can be used to derive the sea surface temperature and water salinity from the past few centuries. The δ18O of coralline red 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.[8][9]

Landscapes and landforms

Within climatic geomorphology one approach is to study relict landforms to infer ancient climates.[10] Being often concerned about past climates climatic geomorphology is considered sometimes to be a theme of historical geology.[11] Climatic geomorphology is of limited use to study recent (Quaternary, Holocene) large climate changes since there are seldom discernible in the geomorphological record.[12]

Timing of proxies

The field of geochronology has 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 dating uses 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 is radiocarbon dating. In the air, cosmic rays constantly 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.[13]

Notable climate events in Earth history

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

See also: Atmosphere of Earth and History of Earth

Earliest atmosphere

The first atmosphere would have consisted of gases in the solar nebula, primarily hydrogen. In addition, there would probably have been simple hydrides such as those now found in gas giants like Jupiter and Saturn, notably water vapor, methane, and ammonia. As the solar nebula dissipated, the gases would have escaped, partly driven off by the solar wind.[14]

Second atmosphere

The next atmosphere, consisting largely of nitrogen, carbon dioxide, and inert gases, was produced by outgassing from volcanism, supplemented by gases produced during the late heavy bombardment of Earth by huge asteroids.[14] 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.[15] 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 billion years ago.[16] 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 early temperature record of Earth with the exception of one cold glacial phase about 2.4 billion years ago. In the late Archaean eon, an oxygen-containing atmosphere began to develop, apparently from photosynthesizing cyanobacteria (see Great Oxygenation Event) which have been found as stromatolite fossils from 2.7 billion years ago. The early basic carbon isotopy (isotope ratio proportions) was very much in line with what is found today, suggesting that the fundamental features of the carbon cycle were established as early as 4 billion years ago.

Third atmosphere

The constant rearrangement of continents by plate tectonics influences 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 the Great Oxygenation Event, and its appearance is indicated by the end of the banded 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 a reducing atmosphere to an oxidizing atmosphere. O2 showed major variations until reaching a steady state of more than 15% by the end of the Precambrian.[17] The following time span was the Phanerozoic eon, during which oxygen-breathing metazoan life forms began to appear.

The amount of oxygen in the atmosphere has fluctuated over the last 600 million years, reaching a peak of 35%[18] during the Carboniferous period, significantly higher than today's 21%. Two main processes govern changes in the atmosphere: plants use carbon dioxide from the atmosphere, releasing oxygen and the breakdown of pyrite and volcanic eruptions release sulfur into 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.[19]

Climate during geological ages

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

In 2020 scientists published a continuous, high-fidelity record of variations in Earth's climate during the past 66 million years and identified four climate 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.[20][21]

Precambrian climate

Main article: Precambrian

The climate of the late Precambrian showed some major glaciation events spreading over much of the earth. At this time the continents were bunched up in the Rodinia supercontinent. Massive deposits of tillites and anomalous isotopic signatures are found, which gave rise to the Snowball Earth hypothesis. As the Proterozoic Eon drew to a close, the Earth started to warm up. By the dawn of the Cambrian and the Phanerozoic, life forms were abundant in the Cambrian explosion with average global temperatures of about 22 °C.

Phanerozoic climate

Changes in oxygen-18 ratios 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.[22] Royer et al. 2004[23] 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 by plate tectonics can 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 to Antarctica were home to deciduous forests rather than ice sheets.

The relatively warm local minimum between Jurassic and Cretaceous goes along with an increase of subduction and mid-ocean ridge volcanism[24] due to the breakup of the Pangea supercontinent.

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 present ice age. Some of the most severe fluctuations, such as the Paleocene-Eocene Thermal Maximum, may be related to rapid climate changes due to sudden collapses of natural methane clathrate reservoirs in the oceans.[25]

A similar, single event of induced severe climate change after a meteorite impact has been proposed as reason for the Cretaceous–Paleogene extinction event. Other major thresholds are the Permian-Triassic, and Ordovician-Silurian extinction events with various reasons suggested.

Quaternary climate

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,[26] red curve is atmospheric CO2 concentrations,[27] and brown curve is dust fluxes.[28][29] 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 Quaternary geological period includes the current climate. There has been a cycle of ice ages for the past 2.2–2.1 million years (starting before the Quaternary in the late Neogene Period).

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

Main article: Climate forcing

Climate forcing is the difference between radiant energy (sunlight) received by the Earth and the outgoing longwave radiation back to space. Such radiative forcing is quantified based on the CO2 amount in the tropopause, in units of watts per square meter to the Earth's surface.[30] Dependent on the radiative balance of incoming and outgoing energy, the Earth either warms up or cools down. Earth radiative balance originates from changes in solar insolation and the concentrations of greenhouse gases and aerosols. Climate change may be due to internal processes in Earth sphere's and/or following external forcings.[31]

Internal processes and forcings

The Earth's climate system involves the atmosphere, biosphere, cryosphere, hydrosphere, and lithosphere,[32] 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 Earth climate sensitivity, in response to the sum of forcings.

Examples:

External forcings

  • The Milankovitch cycles determine 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.[33]
  • Human changes of the composition of the atmosphere or land use.[33]

Mechanisms

On timescales of millions of years, the uplift of mountain ranges and subsequent weathering processes of rocks and soils and the subduction of tectonic plates, are an important part of the carbon cycle.[34][35][36] The weathering sequesters CO2, by the reaction of minerals with chemicals (especially silicate weathering with CO2) and thereby removing CO2 from the atmosphere and reducing the radiative forcing. The opposite effect is volcanism, responsible for the natural greenhouse effect, by emitting CO2 into the atmosphere, thus affecting glaciation (Ice Age) cycles. James Hansen suggested that humans emit CO2 10,000 times faster than natural processes have done in the past.[37]

Ice sheet dynamics and continental positions (and linked vegetation changes) have been important factors in the long term evolution of the earth's climate.[38] There is also a close correlation between CO2 and temperature, where CO2 has a strong control over global temperatures in Earth history.[39]

See also

References

Notes

  1. ^ Bradley, Raymond (2015). Paleoclimatology: Reconstructing Climates of the Quaternary. Oxford: Elsevier. p. 1. ISBN 978-0-12-386913-5.
  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. PMC 2596898. PMID 18198148.
  3. ^ Cronin 2010, p. 1
  4. ^ a b c Fairbridge, Rhodes (31 October 2008). "history of paleoclimatology". In Gornitz, Vivien (ed.). Encyclopedia of Paleoclimatology and Ancient Environments. Springer Nature. pp. 414–426. ISBN 978-1-4020-4551-6.
  5. ^ a b c Cronin, Thomas M. (1999). Principles of Paleoclimatology. Columbia University Press. pp. 8–10. ISBN 9780231503044.
  6. ^ 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. PMID 17615306. S2CID 30125808.
  7. ^ "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". Retrieved 22 September 2011.
  8. ^ 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. S2CID 129376515.
  9. ^ 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. PMID 12867972. S2CID 6088699.
  10. ^ Gutiérrez, Mateo; Gutiérrez, Francisco (2013). "Climatic Geomorphology". Treatise on Geomorphology. Vol. 13. pp. 115–131.
  11. ^ 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. ISBN 978-0-444-51794-4.
  12. ^ Goudie, A.S. (2004). "Climatic geomorphology". In Goudie, A.S. (ed.). Encyclopedia of Geomorphology. pp. 162–164.
  13. ^ Cronin 2010, pp. 32–34.
  14. ^ a b Zahnle, K.; Schaefer, L.; Fegley, B. (2010). "Earth's Earliest Atmospheres". Cold Spring Harbor Perspectives in Biology. 2 (10): a004895. doi:10.1101/cshperspect.a004895. PMC 2944365. PMID 20573713.
  15. ^ B. Windley: The Evolving Continents. Wiley Press, New York 1984
  16. ^ J. Schopf: Earth's Earliest Biosphere: Its Origin and Evolution. Princeton University Press, Princeton, N.J., 1983
  17. ^ Christopher R. Scotese, Back to Earth History: Summary Chart for the Precambrian, Paleomar Project
  18. ^ Beerling, David (2007). The emerald planet: how plants changed Earth's history. Oxford University press. p. 47. ISBN 9780192806024.
  19. ^ Peter Ward:[1] Out of Thin Air: Dinosaurs, Birds, and Earth's Ancient Atmosphere
  20. ^ "High-fidelity record of Earth's climate history puts current changes in context". phys.org. Retrieved 8 October 2020.
  21. ^ 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. ISSN 0036-8075. PMID 32913105. S2CID 221593388. Retrieved 8 October 2020.
  22. ^ Came, Rosemarie E.; Eiler, John M.; Veizer, Jan; Azmy, Karem; Brand, Uwe; Weidman, Christopher R (September 2007). "Coupling of surface temperatures and atmospheric CO2 concentrations during the Palaeozoic era" (PDF). Nature. 449 (7159): 198–201. Bibcode:2007Natur.449..198C. doi:10.1038/nature06085. PMID 17851520. S2CID 4388925.
  23. ^ Royer, Dana L.; Berner, Robert A.; Montañez, Isabel P.; Tabor, Neil J.; Beerling, David J. (July 2004). "CO2 as a primary driver of Phanerozoic climate". GSA Today. 14 (3): 4–10. doi:10.1130/1052-5173(2004)014<4:CAAPDO>2.0.CO;2.
  24. ^ Douwe G. Van Der Meer; Richard E. Zeebe; Douwe J. J. van Hinsbergen; Appy Sluijs; Wim Spakman; Trond H. Torsvik (February 2014). "Plate tectonic controls on atmospheric CO2 levels since the Triassic". PNAS. 111 (12): 4380–4385. Bibcode:2014PNAS..111.4380V. doi:10.1073/pnas.1315657111. PMC 3970481. PMID 24616495.
  25. ^ Frieling, Joost; Svensen, Henrik H.; Planke, Sverre; Cramwinckel, Margot J.; Selnes, Haavard; Sluijs, Appy (25 October 2016). "Thermogenic methane release as a cause for the long duration of the PETM". Proceedings of the National Academy of Sciences. 113 (43): 12059–12064. Bibcode:2016PNAS..11312059F. doi:10.1073/pnas.1603348113. ISSN 0027-8424. PMC 5087067. PMID 27790990.
  26. ^ Jouzel, J.; Masson-Delmotte, V.; Cattani, O.; Dreyfus, G.; Falourd, S.; Hoffmann, G.; Minster, B.; Nouet, J.; Barnola, J. M. (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. ISSN 0036-8075. PMID 17615306. S2CID 30125808.
  27. ^ Lüthi, Dieter; Le Floch, Martine; Bereiter, Bernhard; Blunier, Thomas; Barnola, Jean-Marc; Siegenthaler, Urs; Raynaud, Dominique; Jouzel, Jean; Fischer, Hubertus (15 May 2008). "High-resolution carbon dioxide concentration record 650,000–800,000 years before present" (PDF). Nature. 453 (7193): 379–382. Bibcode:2008Natur.453..379L. doi:10.1038/nature06949. ISSN 0028-0836. PMID 18480821. S2CID 1382081.
  28. ^ Lambert, F.; Delmonte, B.; Petit, J. R.; Bigler, M.; Kaufmann, P. R.; Hutterli, M. A.; Stocker, T. F.; Ruth, U.; Steffensen, J. P. (3 April 2008). "Dust-climate couplings over the past 800,000 years from the EPICA Dome C ice core". Nature. 452 (7187): 616–619. Bibcode:2008Natur.452..616L. doi:10.1038/nature06763. ISSN 0028-0836. PMID 18385736.
  29. ^ Lambert, F.; Bigler, M.; Steffensen, J. P.; Hutterli, M.; Fischer, H. (2012). "Centennial mineral dust variability in high-resolution ice core data from Dome C, Antarctica". Climate of the Past. 8 (2): 609–623. Bibcode:2012CliPa...8..609L. doi:10.5194/cp-8-609-2012.
  30. ^ IPCC (2007). "Concept of Radiative Forcing". IPCC. Archived from the original on 4 January 2014. Retrieved 14 April 2014.
  31. ^ IPCC (2007). "What are Climate Change and Climate Variability?". IPCC.
  32. ^ "Glossary, Climate system". NASA. March 2020.
  33. ^ a b "Annex III: Glossary" (PDF). IPCC AR5. Climate change may be due to natural internal processes or external forcings, such as modulations of the solar cycles, volcanic eruptions, and persistent anthropogenic changes in the composition of the atmosphere or in land use.
  34. ^ Caldeira, Ken (18 June 1992). "Enhanced Cenozoic chemical weathering and the subduction of pelagic carbonate". Nature. 357 (6379): 578–581. Bibcode:1992Natur.357..578C. doi:10.1038/357578a0. S2CID 45143101.
  35. ^ Cin-Ty Aeolus Lee; Douglas M. Morton; Mark G. Little; Ronald Kistler; Ulyana N. Horodyskyj; William P. Leeman; Arnaud Agranier (28 January 2008). "Regulating continent growth and composition by chemical weathering". PNAS. 105 (13): 4981–4986. Bibcode:2008PNAS..105.4981L. doi:10.1073/pnas.0711143105. PMC 2278177. PMID 18362343.
  36. ^ van der Meer, Douwe (25 March 2014). "Plate tectonic controls on Atmospheric CO2 since the Triassic". PNAS. 111 (12): 4380–4385. Bibcode:2014PNAS..111.4380V. doi:10.1073/pnas.1315657111. PMC 3970481. PMID 24616495.
  37. ^ James Hansen (2009). "The 8 Minute Epoch 65 million Years with James Hansen". University of Oregon. Archived from the original on 11 December 2021.
  38. ^ Royer, D. L.; Pagani, M.; Beerling, David J. (1 July 2012). "Geobiological constraints on Earth system sensitivity to CO2 during the Cretaceous and Cenozoic". Geobiology. 10 (4): 298–310. CiteSeerX 10.1.1.933.8880. doi:10.1111/j.1472-4669.2012.00320.x. PMID 22353368. S2CID 32023645.
  39. ^ Royer, Dana L. (1 December 2006). "CO2-forced climate thresholds during the Phanerozoic". Geochimica et Cosmochimica Acta. 70 (23): 5665–5675. Bibcode:2006GeCoA..70.5665R. doi:10.1016/j.gca.2005.11.031.

Bibliography

Library resources about
Paleoclimatology
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