A paleoatmosphere (or palaeoatmosphere) is an atmosphere, particularly that of Earth, at some unspecified time in the geological past.
When regarding geological history of Earth, the paleoatmosphere can be chronologically divided into the Hadean first atmosphere, which resembled the compositions of the solar nebula; the Archean second atmosphere (also known as the prebiotic atmosphere), which became nitrogen-abundant due to volcanic outgassing and meteoric injections during the Late Heavy Bombardment; and the Proterozoic and Phanerozoic third atmosphere, which started to contain free oxygen due to biotic photosynthesis.
Composition
editThe composition of Earth's paleoatmosphere can be inferred today from the study of the abundance of proxy materials such as iron oxides and charcoal and the fossil data, such as the stomatal density of fossil leaves in geological deposits. Although today's atmosphere is dominated by nitrogen (about 78%), oxygen (about 21%), and argon (about 1%), the pre-biological atmosphere is thought to have been a highly[citation needed] reducing atmosphere, having virtually no free oxygen, virtually no argon, which is generated by the radioactive decay of 40K, and to have been dominated by nitrogen, carbon dioxide and methane.
Appreciable concentrations of free oxygen were probably not present until about 2,500 million years ago (Myr). After the Great Oxidation Event, quantities of oxygen produced as a by-product of photosynthesis by cyanobacteria (sometimes erroneously referred to as blue-green algae) began to exceed the quantities of chemically reducing materials, notably dissolved iron. By the beginning of the Cambrian period 541 Ma, free oxygen concentrations had increased sufficiently to enable the evolution of multicellular organisms. Following the subsequent appearance, rapid evolution and radiation of land plants, which covered much of the Earth's land surface, beginning about 450 Ma, oxygen concentrations reached and later exceeded current values (about 21%) during the early Carboniferous, when atmospheric carbon dioxide was drawn down below current concentrations (about 400 ppm) by oxygenic photosynthesis.[1][2][3] This may have contributed to the Carboniferous rainforest collapse during the Moscovian and Kasimovian ages of the Pennsylvanian subperiod.
Indirect measurements
editGeological studies of ancient rock formations can give information on paleoatmospheric composition, pressure, density, etc. at specific points in Earth's history.
Density and pressure
editA 2012 study looked at the imprints made by falling raindrops onto freshly deposited volcanic ash, laid down in the Archean Eon 2,700 Ma in the Ventersdorp Supergroup, South Africa. They linked the terminal velocity of the raindrops directly to the air density of the paleoatmosphere and showed that it had less than twice the density of the modern atmosphere, and likely had similar if not lower density.[4]
A similar study in 2016 looked at the size distribution of gas bubbles in basaltic lava flows that solidified at sea level also during the Archean (~2,700 Ma). They found an atmospheric pressure of only 0.23 ± 0.23 bar (23 kPa).[5]
Both results contradict theories[citation needed] that suggest the Archean was kept warm during the Faint Young Sun period by extremely high levels of carbon dioxide or nitrogen.
Oxygen content
editA 2016 study performed mass spectrometry on air bubbles trapped inside rock salt deposited 813 Myr ago. They detected an oxygen content of 10.9%, much higher than had been expected from indirect measures. This suggested the Neoproterozoic oxygenation event may have happened much earlier than previously thought.[6]
See also
edit- Prebiotic atmosphere – Second atmosphere on Earth
- Atmosphere of Earth#Evolution of Earth's atmosphere
- Great Oxidation Event#The early atmosphere – Paleoproterozoic surge in atmospheric oxygen
- Paleoclimatology – Study of changes in ancient climate
- Reducing atmosphere – Atmosphere containing reducing agents
References
edit- ^ Berner, Robert A. (1998). "The carbon cycle and CO
2 over Phanerozoic time: the role of land plants". Philosophical Transactions of the Royal Society. 353 (1365): 75–82. doi:10.1098/Rstb.1998.0192. PMC 1692179. - ^ Berner, Robert A. (1997). "The rise of plants: their effect on weathering and atmospheric CO
2". Science. 276: 544–546. doi:10.1126/Science.276.5312.544. S2CID 128649732. - ^ Beerling, David J.; Berner, Robert A. (2005). "Feedbacks and the coevolution of plants and atmospheric CO
2". Proceedings of the National Academy of Sciences. 102 (5). USA: 1302–1305. Bibcode:2005PNAS..102.1302B. doi:10.1073/Pnas.0408724102. PMC 547859. PMID 15668402. - ^ Som, Sanjoy M.; Catling, David C.; Harnmeijer, Jelte P.; Polivka, Peter M.; Buick, Roger (2012). "Air density 2.7 billion years ago limited to less than twice modern levels by fossil raindrop imprints". Nature. 484.7394 (7394): 359–362. Bibcode:2012Natur.484..359S. doi:10.1038/nature10890. PMID 22456703. S2CID 4410348.
- ^ Som, Sanjoy M.; Buick, Roger; Hagadorn, James W.; Blake, Tim S.; Perreault, John M.; Harnmeijer, Jelte P.; Catling, David C. (2016). "Earth's air pressure 2.7 billion years ago constrained to less than half of modern levels". Nature Geoscience. 9 (6): 448–451. Bibcode:2016NatGe...9..448S. doi:10.1038/ngeo2713.
- ^ Blamey, Nigel J. F.; Brand, Uwe; Parnell, John; Spear, Natalie; Lécuyer, Christophe; Benison, Kathleen; Meng, Fanwei; Ni, Pei (2016). "Paradigm shift in determining Neoproterozoic atmospheric oxygen". Geology. 44 (8): 651. Bibcode:2016Geo....44..651B. doi:10.1130/G37937.1. hdl:2164/6234.