Application of oxidation state to the study of the Earth's mantle
Oxygen fugacity range where common cation pairs dominate.Data for plotting are from Shearer et al., (2006).[1] IW represents Iron-Wüstite buffer and QFM represents Quartz-Fayalite-Magnetite buffer.
Mantle oxidation state (redox state) applies the concept of oxidation state in chemistry to the study of the Earth's mantle. The chemical concept of oxidation state mainly refers to the valence state of one element, while mantle oxidation state provides the degree of decreasing of increasing valence states of all polyvalent elements in mantle materials confined in a closed system. The mantle oxidation state is controlled by oxygen fugacity and can be benchmarked by specific groups of redox buffers.
Mantle oxidation state changes because of the existence of polyvalent elements (elements with more than one valence state, e.g. Fe, Cr, V, Ti, Ce, Eu, C and others). Among them, Fe is the most abundant (≈8 wt% of the mantle[2]) and its oxidation state largely reflects the oxidation state of mantle. Examining the valence state of other polyvalent elements could also provide the information of mantle oxidation state.
It is well known that the oxidation state can influence the partitioning behavior of elements[3][4] and liquid water[5] between melts and minerals, the speciation of C-O-H-bearing fluids and melts,[6] as well as transport properties like electrical conductivity and creep.[5]
The formation of diamond requires both reaching high pressures and high temperatures and a carbon source. The most common carbon source in deep Earth is not elemental carbon and redox reactions need to be involved in diamond formation. Examining the oxidation state can help us predict the P-T conditions of diamond formation and elucidate the origin of deep diamonds.[7]
^McDonough, W. F.; Sun, S. -s. (1995-03-01). "The composition of the Earth". Chemical Geology. Chemical Evolution of the Mantle. 120 (3): 223–253. Bibcode:1995ChGeo.120..223M. doi:10.1016/0009-2541(94)00140-4. ISSN 0009-2541.
^Fischer, Rebecca A.; Nakajima, Yoichi; Campbell, Andrew J.; Frost, Daniel J.; Harries, Dennis; Langenhorst, Falko; Miyajima, Nobuyoshi; Pollok, Kilian; Rubie, David C. (2015-10-15). "High pressure metal–silicate partitioning of Ni, Co, V, Cr, Si, and O". Geochimica et Cosmochimica Acta. 167: 177–194. Bibcode:2015GeCoA.167..177F. doi:10.1016/j.gca.2015.06.026. ISSN 0016-7037.
^Corgne, Alexandre; Keshav, Shantanu; Wood, Bernard J.; McDonough, William F.; Fei, Yingwei (2008). "Metal–silicate partitioning and constraints on core composition and oxygen fugacity during Earth accretion". Geochimica et Cosmochimica Acta. 72 (2): 574–589. Bibcode:2008GeCoA..72..574C. doi:10.1016/j.gca.2007.10.006.
^ abFrost, Daniel J.; McCammon, Catherine A. (2008-04-29). "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. ISSN 0084-6597.
^Holloway, John R.; Blank, Jennifer G. (1994-12-31), "Chapter 6. APPLICATION OF EXPERIMENTAL RESULTS TO C-O-H SPECIES IN NATURAL MELTS", Volatiles in Magmas, De Gruyter, pp. 187–230, doi:10.1515/9781501509674-012, ISBN 9781501509674
^Luth, R. W.; Stachel, T. (2015). "Diamond formation — Where, when and how?". Lithos. Complete (220–223): 200–220. Bibcode:2015Litho.220..200S. doi:10.1016/j.lithos.2015.01.028. ISSN 0024-4937.
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