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Mantle oxidation state

Topic: Chemistry

 From HandWiki - Reading time: 8 min
Short description: 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]

Thermodynamic description of oxidation state

Mantle oxidation state can be quantified as the oxygen fugacity ([math]\displaystyle{ fO_2 }[/math]) of the system within the framework of thermodynamics. A higher oxygen fugacity implies a more oxygen-rich and more oxidized environment. At each given pressure-temperature conditions, for any compound or element M that bears the potential to be oxidized by oxygen, we can write[8][9]

[math]\displaystyle{ M+\frac{x}{2}O_2\rightleftharpoons MO_x }[/math]

For example, if M is Fe, the redox equilibrium reaction can be Fe+1/2O2=FeO; if M is FeO, the redox equilibrium reaction can be 2FeO+1/2O2=Fe2O3.

Gibbs energy change associated with this reaction is therefore

[math]\displaystyle{ \Delta G= G(MO_x)-G(M)=\frac{x}{2}RT lnfO_2 }[/math]

Along each isotherm, the partial derivation of ΔG with respect to P is ΔV,

[math]\displaystyle{ \frac{\partial \Delta G}{\partial P_{|T}}={\Delta V} }[/math].[10]

Combining the 2 equations above,

[math]\displaystyle{ \frac{\partial (lnfO_2))}{\partial P|_T}=\frac{2}{xRT}\Delta V }[/math].

Therefore,

[math]\displaystyle{ logfO_2(P)=logfO_2(1bar)+(\frac{0.8686}{RT})\int_{1bar}^{P} \Delta VdP }[/math] (note that ln(e as the base) changed to log(10 as the base) in this formula.

For a closed system, there might exist more than one of these equilibrium oxidation reactions, but since all these reactions share a same [math]\displaystyle{ fO_2 }[/math], examining one of them would allow extraction of oxidation state of the system.

Pressure effect on oxygen fugacity

The physics and chemistry of mantle largely depend on pressure. As mantle minerals are compressed, they are transformed into other minerals at certain depths. Seismic observations of velocity discontinuities and experimental simulations on phase boundaries both verified the structure transformations within the mantle. As such, the mantle can be further divided into three layers with distinct mineral compositions.

Mantle Mineral Composition[11]
Mantle Layer Depth Pressure Major Minerals
Upper Mantle ~10- 410km ~1- 13 GPa Olivine, Orthopyroxene, Clinopyroxene, Garnet
Transition Zone 410- 660 km 13- 23 GPa Wadsleyite, Ringwoodite, Majoritic Garnet
Lower Mantle 660- 2891 km 23- 129 GPa Ferropericlase, Bridgmanite, Ca-perovskite

Since mantle mineral composition changes, the mineral hosting environment for polyvalent elements also alters. For each layer, the mineral combination governing the redox reactions is unique and will be discussed in detailed below.

Upper mantle

Between depths of 30 and 60 km, oxygen fugacity is mainly controlled by Olivine-Orthopyroxene-Spinel oxidation reaction.

[math]\displaystyle{ 6Fe_2SiO_4+O_2\rightleftharpoons3Fe_2Si_2O_6+2Fe_3O_4 }[/math]

Under deeper upper mantle conditions, Olivine-Orthopyroxene-Garnet oxygen barometer[12] is the redox reaction that is used to calibrate oxygen fugacity.
[math]\displaystyle{ 4Fe_2SiO_4+2FeSiO_3+O_2\rightleftharpoons2Fe_3^{2+}Fe_2^{3+}Si_3O_{12} }[/math]

In this reaction, 4 mole of ferrous ions were oxidized to ferric ions and the other 2 mole of ferrous ions remain unchanged.

Transition zone

Garnet-Garnet[13] reaction can be used to estimate the redox state of transition zone.

[math]\displaystyle{ 2Ca_3Al_2Si_3O_{12}+\frac{4}{3}Fe_3Al_2Si_3O_{12}+2.5Mg_4Si_4O_{12}+O_2 \rightleftharpoons2Ca_3Fe_2Si_3O_{12}+\frac{10}{3}Mg_3Al_2Si_3O_{12}+SiO_2 }[/math]

A picture of garnet crystals.Garnet, a major mineral in transition zone, controls the oxidation state there.

A recent study[13] showed that the oxygen fugacity of transition referred from Garnet-Garnet reaction is -0.26 [math]\displaystyle{ logfO_2 }[/math] to +3 [math]\displaystyle{ logfO_2 }[/math] relative to the Fe-FeO (IW, iron- wütstite) oxygen buffer.

Lower mantle

Disproportionation of ferrous iron at lower mantle conditions also affect the mantle oxidation state. This reaction is different from the reactions mentioned above as it does not incorporate the participation of free oxygen.

[math]\displaystyle{ 3Fe^{2+}(Fp)\rightleftharpoons Fe+2Fe^{3+}(Bdg) }[/math],[5][14]

FeO resides in the form of ferropericlase (Fp) and Fe2O3 resides in the form of bridgmanite (Bdg). There is no oxygen fugacity change associated with the reaction. However, as the reaction products differ in density significantly, the metallic iron phase could descend downwards to the Earth's core and get separated from the mantle. In this case, the mantle loses metallic iron and becomes more oxidized.

Implications for Diamond Formation

Diamond formed in the Earth's interior

The equilibrium reaction involving diamond is

Carbon Cycle involving deep Earth

[math]\displaystyle{ Mg_2Si_2O_6+2MgCO_3\rightleftharpoons2Mg_2SiO_4+2C(Diamond)+2O_2 }[/math].

Examining the oxygen fugacity of the upper mantle and transition enables us to compare it with the conditions (equilibrium reaction shown above) required for diamond formation. The results show that the [math]\displaystyle{ logfO_2 }[/math] is usually 2 units lower than the carbonate-carbon reaction[13] which means favoring the formation of diamond at transition zone conditions.

It has also been reported that pH decrease would also facilitate the formation of diamond in Mantle conditions.[15]

[math]\displaystyle{ HCOO^{-}+H^++H_{2,aq} \rightleftharpoons C_{diamond}+2H_2O }[/math]

[math]\displaystyle{ CH_3CH_2COO^-+H^+\rightleftharpoons3C_{diamond}+H_{2,aq}+2H_2O }[/math]

where the subscript aq means 'aqueous', implying H2 is dissolved in the solution.

Deep diamonds have become important windows to look into the mineralogy of the Earth's interior. Minerals not stable at the surface could possibly be found within inclusions of superdeep diamonds[16]-- implying they were stable where these diamond crystallized. Because of the hardness of diamonds, the high pressure environment is retained even after transporting to the surface. So far, these superdeep minerals brought by diamonds include ringwoodite,[17] ice-VII,[18] cubic δ-N2[19] and Ca-perovskite.[20]

See also

References

  1. ↑ Shearer, C.K.; Papike, J.J.; Karner, J.M. (2006-10-01). "Pyroxene europium valence oxybarometer: Effects of pyroxene composition, melt composition, and crystallization kinetics". American Mineralogist 91 (10): 1565–1573. doi:10.2138/am.2006.2098. ISSN 0003-004X. Bibcode: 2006AmMin..91.1565S. 
  2. ↑ 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. doi:10.1016/0009-2541(94)00140-4. ISSN 0009-2541. Bibcode: 1995ChGeo.120..223M. 
  3. ↑ Fischer, Rebecca A.; Nakajima, Yoichi; Campbell, Andrew J.; Frost, Daniel J.; Harries, Dennis; Langenhorst, Falko; Miyajima, Nobuyoshi; Pollok, Kilian et al. (2015-10-15). "High pressure metal–silicate partitioning of Ni, Co, V, Cr, Si, and O". Geochimica et Cosmochimica Acta 167: 177–194. doi:10.1016/j.gca.2015.06.026. ISSN 0016-7037. Bibcode: 2015GeCoA.167..177F. 
  4. ↑ 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" (in en). Geochimica et Cosmochimica Acta 72 (2): 574–589. doi:10.1016/j.gca.2007.10.006. Bibcode: 2008GeCoA..72..574C. 
  5. ↑ 5.0 5.1 5.2 Frost, 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. doi:10.1146/annurev.earth.36.031207.124322. ISSN 0084-6597. Bibcode: 2008AREPS..36..389F. 
  6. ↑ 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 
  7. ↑ Luth, R. W.; Stachel, T. (2015). "Diamond formation — Where, when and how?" (in English). Lithos Complete (220–223): 200–220. doi:10.1016/j.lithos.2015.01.028. ISSN 0024-4937. Bibcode: 2015Litho.220..200S. https://www.infona.pl//resource/bwmeta1.element.elsevier-c4cbc5bf-f8a5-3cb9-a8d8-53058b5d1a49. 
  8. ↑ Zhang, H.L.; Hirschmann, M.M.; Cottrell, E.; Withers, A.C. (2017). "Effect of pressure on Fe 3+ /ΣFe ratio in a mafic magma and consequences for magma ocean redox gradients". Geochimica et Cosmochimica Acta 204: 83–103. doi:10.1016/j.gca.2017.01.023. ISSN 0016-7037. Bibcode: 2017GeCoA.204...83Z. 
  9. ↑ Campbell, Andrew J.; Danielson, Lisa; Righter, Kevin; Seagle, Christopher T.; Wang, Yanbin; Prakapenka, Vitali B. (2009). "High pressure effects on the iron–iron oxide and nickel–nickel oxide oxygen fugacity buffers". Earth and Planetary Science Letters 286 (3–4): 556–564. doi:10.1016/j.epsl.2009.07.022. ISSN 0012-821X. Bibcode: 2009E&PSL.286..556C. 
  10. ↑ "Fundamental thermodynamic relation" (in en), Wikipedia, 2018-11-28, https://en.wikipedia.org/w/index.php?title=Fundamental_thermodynamic_relation&oldid=870980416, retrieved 2019-02-10 
  11. ↑ Frost, Daniel J. (2008-06-01). "The Upper Mantle and Transition Zone" (in en). Elements 4 (3): 171–176. doi:10.2113/GSELEMENTS.4.3.171. ISSN 1811-5209. 
  12. ↑ McCammon, C.; Kopylova, M. G. (2004-07-17). "A redox profile of the Slave mantle and oxygen fugacity control in the cratonic mantle". Contributions to Mineralogy and Petrology 148 (1): 55–68. doi:10.1007/s00410-004-0583-1. ISSN 0010-7999. Bibcode: 2004CoMP..148...55M. 
  13. ↑ 13.0 13.1 13.2 Kiseeva, Ekaterina S.; Vasiukov, Denis M.; Wood, Bernard J.; McCammon, Catherine; Stachel, Thomas; Bykov, Maxim; Bykova, Elena; Chumakov, Aleksandr et al. (2018-01-22). "Oxidized iron in garnets from the mantle transition zone". Nature Geoscience 11 (2): 144–147. doi:10.1038/s41561-017-0055-7. ISSN 1752-0894. Bibcode: 2018NatGe..11..144K. http://bib-pubdb1.desy.de/record/418155. 
  14. ↑ Rubie, David C.; Trønnes, Reidar G.; Catherine A. McCammon; Langenhorst, Falko; Liebske, Christian; Frost, Daniel J. (2004). "Experimental evidence for the existence of iron-rich metal in the Earth's lower mantle" (in en). Nature 428 (6981): 409–412. doi:10.1038/nature02413. ISSN 1476-4687. PMID 15042086. Bibcode: 2004Natur.428..409F. 
  15. ↑ Sverjensky, Dimitri A.; Huang, Fang (2015-11-03). "Diamond formation due to a pH drop during fluid–rock interactions". Nature Communications 6 (1): 8702. doi:10.1038/ncomms9702. ISSN 2041-1723. PMID 26529259. Bibcode: 2015NatCo...6.8702S. 
  16. ↑ Zhu, Feng; Li, Jie; Liu, Jiachao; Lai, Xiaojing; Chen, Bin; Meng, Yue (2019-02-18). "Kinetic Control on the Depth Distribution of Superdeep Diamonds" (in en). Geophysical Research Letters 46 (4): 1984–1992. doi:10.1029/2018GL080740. Bibcode: 2019GeoRL..46.1984Z. 
  17. ↑ Pearson, D. G.; Brenker, F. E.; Nestola, F.; McNeill, J.; Nasdala, L.; Hutchison, M. T.; Matveev, S.; Mather, K. et al. (2014-03-12). "Hydrous mantle transition zone indicated by ringwoodite included within diamond". Nature 507 (7491): 221–224. doi:10.1038/nature13080. ISSN 0028-0836. PMID 24622201. Bibcode: 2014Natur.507..221P. http://bib-pubdb1.desy.de/record/168146/files/10.1038_nature13080.pdf. 
  18. ↑ Tschauner, O.; Huang, S.; Greenberg, E.; Prakapenka, V. B.; Ma, C.; Rossman, G. R.; Shen, A. H.; Zhang, D. et al. (2018-03-09). "Ice-VII inclusions in diamonds: Evidence for aqueous fluid in Earth's deep mantle" (in en). Science 359 (6380): 1136–1139. doi:10.1126/science.aao3030. ISSN 0036-8075. PMID 29590042. Bibcode: 2018Sci...359.1136T. 
  19. ↑ Navon, Oded; Wirth, Richard; Schmidt, Christian; Jablon, Brooke Matat; Schreiber, Anja; Emmanuel, Simon (2017). "Solid molecular nitrogen ( δ -N 2 ) inclusions in Juina diamonds: Exsolution at the base of the transition zone" (in en). Earth and Planetary Science Letters 464: 237–247. doi:10.1016/j.epsl.2017.01.035. Bibcode: 2017E&PSL.464..237N. 
  20. ↑ Nestola, F.; Korolev, N.; Kopylova, M.; Rotiroti, N.; Pearson, D. G.; Pamato, M. G.; Alvaro, M.; Peruzzo, L. et al. (2018-03-07). "CaSiO3 perovskite in diamond indicates the recycling of oceanic crust into the lower mantle". Nature 555 (7695): 237–241. doi:10.1038/nature25972. ISSN 0028-0836. PMID 29516998. Bibcode: 2018Natur.555..237N. http://discovery.ucl.ac.uk/10049984/. 



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