Wikipedia

Deep carbon cycle

The deep carbon cycle (or slow carbon cycle) is geochemical cycle (movement) of carbon through the Earth's mantle and core. It forms part of the carbon cycle and is intimately connected to the movement of carbon in the Earth's surface and atmosphere. By returning carbon to the deep Earth, it plays a critical role in maintaining the terrestrial conditions necessary for life to exist. Without it, carbon would accumulate in the atmosphere, reaching extremely high concentrations over long periods of time.[1]

Deep earth carbon

Because the deep Earth is inaccessible to drilling, not much is conclusively known about the role of carbon in it. Nonetheless, several pieces of evidence—many of which come from laboratory simulations of deep Earth conditions—have indicated mechanisms for the element's movement down into the lower mantle, as well as the forms that carbon takes at the extreme temperatures and pressures of this layer. Furthermore, techniques like seismology have led to greater understanding of the potential presence of carbon in the Earth's core. Studies of the composition of basaltic magma and the flux of carbon dioxide out of volcanoes reveals that the amount of carbon in the mantle is greater than that on the Earth's surface by a factor of one thousand.[2]

Quantity of carbon

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There are about 44,000 gigatonnes of carbon in the atmosphere and oceans. A gigatonne is one billion metric tonnes, equivalent to the mass of water in over 400,000 Olympic-size swimming pools.[3] Large as this quantity is, it only amounts to a small fraction of one percent of Earth's carbon. Over 90% may reside in the core, most of the rest being in the crust and mantle.[4]

In the photosphere of the Sun, carbon is the fourth most abundant element. The Earth likely started with a similar ratio but lost a lot of it to evaporation as it accreted. Even accounting for evaporation, however, the silicates making up the crust and mantle of the Earth have a carbon concentration that is five to ten times less than in CI chondrites, a form of meteor that is believed to represent the composition of the solar nebula before the planets formed. Some of this carbon may have ended up in the core. Depending on the model, carbon is predicted to contribute between 0.2 and 1 percent by weight in the core. Even at the lower concentration, this would account for half Earth's carbon.[5]

Estimates of the carbon content in the upper mantle come from measurements of the chemistry of mid-ocean ridge basalts (MORBs). These must be corrected for degassing of carbon and other elements. Since the Earth formed, the upper mantle has lost 40–90% of its carbon by evaporation and transport to the core in iron compounds. The most rigorous estimate gives a carbon content of 30 parts per million (ppm). The lower mantle is expected to be much less depleted – about 350 ppm.[6]

Lower mantle

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Carbon principally enters the mantle in the form of carbonate-rich sediments on tectonic plates of ocean crust, which pull the carbon into the mantle upon undergoing subduction. Not much is known about carbon circulation in the mantle, especially in the deep Earth, but many studies have attempted to augment our understanding of the element's movement and forms within said region. For instance, a 2011 study demonstrated that carbon cycling extends all the way to the lower mantle. The study analysed rare, super-deep diamonds at a site in Juina, Brazil, determining that the bulk composition of some of the diamonds' inclusions matched the expected result of basalt melting and crystallisation under lower mantle temperatures and pressures.[7] Thus, the investigation's findings indicate that pieces of basaltic oceanic lithosphere act as the principal transport mechanism for carbon to Earth's deep interior. These subducted carbonates can interact with lower mantle silicates and metals, eventually forming super-deep diamonds like the one found.[8]

Carbon reservoirs in the mantle, crust and surface.[6]
Reservoir gigatonne C
Above surface  
Continental crust and lithosphere  
Oceanic crust and lithosphere  
Upper mantle  
Lower mantle  

Carbonates descending to the lower mantle form other compounds besides diamonds. In 2011, carbonates were subjected to an environment similar to that of 1800 km deep into the Earth, well within the lower mantle. Doing so resulted in the formations of magnesite, siderite, and numerous varieties of graphite.[9] Other experiments—as well as petrologic observations—support this claim, finding that magnesite is actually the most stable carbonate phase in the majority of the mantle. This is largely a result of its higher melting temperature.[10] Consequently, scientists have concluded that carbonates undergo reduction as they descend into the mantle before being stabilised at depth by low oxygen fugacity environments. Magnesium, iron, and other metallic compounds act as buffers throughout the process.[11] The presence of reduced, elemental forms of carbon like graphite would indicate that carbon compounds are reduced as they descend into the mantle.

 
Carbon outgassing processes[12]

Nonetheless, polymorphism alters carbonate compounds' stability at different depths within the Earth. To illustrate, laboratory simulations and density functional theory calculations suggest that tetrahedrally-coordinated carbonates are most stable at depths approaching the core–mantle boundary.[13][9] A 2015 study indicates that the lower mantle's high pressures cause carbon bonds to transition from sp2 to sp3 hybridised orbitals, resulting in carbon tetrahedrally bonding to oxygen.[14] CO3 trigonal groups cannot form polymerisable networks, while tetrahedral CO4 can, signifying an increase in carbon's coordination number, and therefore drastic changes in carbonate compounds' properties in the lower mantle. As an example, preliminary theoretical studies suggest that high pressures cause carbonate melt viscosity to increase; the melts' lower mobility as a result of the property changes described is evidence for large deposits of carbon deep into the mantle.[15]

Accordingly, carbon can remain in the lower mantle for long periods of time, but large concentrations of carbon frequently find their way back to the lithosphere. This process, called carbon outgassing, is the result of carbonated mantle undergoing decompression melting, as well as mantle plumes carrying carbon compounds up towards the crust.[16] Carbon is oxidised upon its ascent towards volcanic hotspots, where it is then released as CO2. This occurs so that the carbon atom matches the oxidation state of the basalts erupting in such areas.[17]

Core

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Although the presence of carbon in the Earth's core is well-constrained, recent studies suggest large inventories of carbon could be stored in this region. Shear (S) waves moving through the inner core travel at about fifty percent of the velocity expected for most iron-rich alloys.[18] Considering the core's composition is widely believed to be an alloy of crystalline iron with a small amount of nickel, this seismographic anomaly points to another substance's existence within the region. One theory postulates that such a phenomenon is the result of various light elements, including carbon, in the core.[18] In fact, studies have utilised diamond anvil cells to replicate the conditions in the Earth's core, the results of which indicate that iron carbide (Fe7C3) matches the inner core's sound and density velocities considering its temperature and pressure profile. Hence, the iron carbide model could serve as evidence that the core holds as much as 67% of the Earth's carbon.[19] Furthermore, another study found that carbon dissolved in iron and formed a stable phase with the same Fe7C3 composition—albeit with a different structure than the one previously mentioned.[20] Hence, although the amount of carbon potentially stored in the Earth's core is not known, recent research indicates that the presence of iron carbides could be consistent with geophysical observations.

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    Movement of oceanic plates—which carry carbon compounds—through the mantle
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    Two models of the carbon content in Earth
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    Analysis of shear wave velocities has played an integral role in the development of knowledge about carbon's existence in the core
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    Diagram of carbon tetrahedrally bonded to oxygen

Fluxes

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Major fluxes of carbon to, from, and within the Earth’s exogenic and endogenic systems
Values give the maximum and minimum fluxes since 200 million years ago. The two major boundaries highlighted are
the Mohorovičić discontinuity (crust-mantle boundary; Moho) and the lithosphere-asthenosphere boundary (LAB).[21]

See also

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References

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  1. ^ "The Deep Carbon Cycle and our Habitable Planet". Deep Carbon Observatory. 3 December 2015. Archived from the original on 2020-07-27. Retrieved 2019-02-19.
  2. ^ Wilson, Mark (2003). "Where do Carbon Atoms Reside within Earth's Mantle?". Physics Today. 56 (10): 21–22. Bibcode:2003PhT....56j..21W. doi:10.1063/1.1628990.
  3. ^ Collins, Terry; Pratt, Katie (1 October 2019). "Scientists Quantify Global Volcanic CO2 Venting; Estimate Total Carbon on Earth". Deep Carbon Observatory. Archived from the original on 3 October 2019. Retrieved 17 December 2019.
  4. ^ Suarez, Celina A.; Edmonds, Marie; Jones, Adrian P. (1 October 2019). "Earth Catastrophes and their Impact on the Carbon Cycle". Elements. 15 (5): 301–306. doi:10.2138/gselements.15.5.301.
  5. ^ Li, Jie; Mokkherjee, Mainak; Morard, Guillaume (2019). "Carbon versus Other Light Elements in Earth's Core". In Orcutt, Beth N.; Daniel, Isabelle; Dasgupta, Rajdeep (eds.). Deep carbon : past to present. Cambridge University Press. pp. 40–65. doi:10.1017/9781108677950.011. ISBN 9781108677950. S2CID 210787128.
  6. ^ a b Lee, C-T. A.; Jiang, H.; Dasgupta, R.; Torres, M. (2019). "A Framework for Understanding Whole-Earth Carbon Cycling". In Orcutt, Beth N.; Daniel, Isabelle; Dasgupta, Rajdeep (eds.). Deep carbon : past to present. Cambridge University Press. pp. 313–357. doi:10.1017/9781108677950.011. ISBN 9781108677950. S2CID 210787128.
  7. ^ American Association for the Advancement of Science (15 September 2011). "Carbon cycle reaches Earth's lower mantle: Evidence of carbon cycle found in 'superdeep' diamonds From Brazil" (Press release). ScienceDaily. Retrieved 2019-02-06.
  8. ^ Stagno, V.; Frost, D. J.; McCammon, C. A.; Mohseni, H.; Fei, Y. (5 February 2015). "The oxygen fugacity at which graphite or diamond forms from carbonate-bearing melts in eclogitic rocks". Contributions to Mineralogy and Petrology. 169 (2): 16. Bibcode:2015CoMP..169...16S. doi:10.1007/s00410-015-1111-1. S2CID 129243867.
  9. ^ a b Fiquet, Guillaume; Guyot, François; Perrillat, Jean-Philippe; Auzende, Anne-Line; Antonangeli, Daniele; Corgne, Alexandre; Gloter, Alexandre; Boulard, Eglantine (2011-03-29). "New host for carbon in the deep Earth". Proceedings of the National Academy of Sciences. 108 (13): 5184–5187. Bibcode:2011PNAS..108.5184B. doi:10.1073/pnas.1016934108. PMC 3069163. PMID 21402927.
  10. ^ Dorfman, Susannah M.; Badro, James; Nabiei, Farhang; Prakapenka, Vitali B.; Cantoni, Marco; Gillet, Philippe (2018-05-01). "Carbonate stability in the reduced lower mantle" (PDF). Earth and Planetary Science Letters. 489: 84–91. Bibcode:2018E&PSL.489...84D. doi:10.1016/j.epsl.2018.02.035. OSTI 1426861. S2CID 134119145.
  11. ^ Kelley, Katherine A.; Cottrell, Elizabeth (2013-06-14). "Redox Heterogeneity in Mid-Ocean Ridge Basalts as a Function of Mantle Source". Science. 340 (6138): 1314–1317. Bibcode:2013Sci...340.1314C. doi:10.1126/science.1233299. PMID 23641060. S2CID 39125834.
  12. ^ Dasgupta, Rajdeep (December 10, 2011). The Influence of Magma Ocean Processes on the Present-day Inventory of Deep Earth Carbon. Post-AGU 2011 CIDER Workshop. Archived from the original on 24 April 2016. Retrieved 20 March 2019.
  13. ^ Litasov, Konstantin D.; Shatskiy, Anton (2018). "Carbon-Bearing Magmas in the Earth's Deep Interior". Magmas Under Pressure. pp. 43–82. doi:10.1016/B978-0-12-811301-1.00002-2. ISBN 978-0-12-811301-1.
  14. ^ Mao, Wendy L.; Liu, Zhenxian; Galli, Giulia; Pan, Ding; Boulard, Eglantine (2015-02-18). "Tetrahedrally coordinated carbonates in Earth's lower mantle". Nature Communications. 6: 6311. arXiv:1503.03538. Bibcode:2015NatCo...6.6311B. doi:10.1038/ncomms7311. PMID 25692448. S2CID 205335268.
  15. ^ Carmody, Laura; Genge, Matthew; Jones, Adrian P. (2013-01-01). "Carbonate Melts and Carbonatites". Reviews in Mineralogy and Geochemistry. 75 (1): 289–322. Bibcode:2013RvMG...75..289J. doi:10.2138/rmg.2013.75.10.
  16. ^ Dasgupta, Rajdeep; Hirschmann, Marc M. (2010-09-15). "The deep carbon cycle and melting in Earth's interior". Earth and Planetary Science Letters. 298 (1): 1–13. Bibcode:2010E&PSL.298....1D. doi:10.1016/j.epsl.2010.06.039.
  17. ^ Frost, Daniel J.; McCammon, Catherine A. (May 2008). "The Redox State of Earth's Mantle". Annual Review of Earth and Planetary Sciences. 36 (1): 389–420. Bibcode:2008AREPS..36..389F. doi:10.1146/annurev.earth.36.031207.124322.
  18. ^ a b "Does Earth's Core Host a Deep Carbon Reservoir?". Deep Carbon Observatory. 14 April 2015. Archived from the original on 2020-07-27. Retrieved 2019-03-09.
  19. ^ Li, Jie; Chow, Paul; Xiao, Yuming; Alp, E. Ercan; Bi, Wenli; Zhao, Jiyong; Hu, Michael Y.; Liu, Jiachao; Zhang, Dongzhou (2014-12-16). "Hidden carbon in Earth's inner core revealed by shear softening in dense Fe7C3". Proceedings of the National Academy of Sciences. 111 (50): 17755–17758. Bibcode:2014PNAS..11117755C. doi:10.1073/pnas.1411154111. PMC 4273394. PMID 25453077.
  20. ^ Hanfland, M.; Chumakov, A.; Rüffer, R.; Prakapenka, V.; Dubrovinskaia, N.; Cerantola, V.; Sinmyo, R.; Miyajima, N.; Nakajima, Y. (March 2015). "High Poisson's ratio of Earth's inner core explained by carbon alloying". Nature Geoscience. 8 (3): 220–223. Bibcode:2015NatGe...8..220P. doi:10.1038/ngeo2370.
  21. ^ Wong, Kevin; Mason, Emily; Brune, Sascha; East, Madison; Edmonds, Marie; Zahirovic, Sabin (2019). "Deep Carbon Cycling over the Past 200 Million Years: A Review of Fluxes in Different Tectonic Settings". Frontiers in Earth Science. 7: 263. Bibcode:2019FrEaS...7..263W. doi:10.3389/feart.2019.00263. S2CID 204027259.

Further reading

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