The effect of water on the electrical conductivity of olivine

Wang, Duojun; Mookherjee, Mainak; Xu, Yongfu; Karato, Shun‐ichiro

doi:10.1038/nature05256

Cited by 360 publications

(481 citation statements)

References 27 publications

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“…Although there is still some disagreement between different laboratory measurements, the balance of evidence suggests that hydrogen enhances conductivity (Yoshino et al, 2006;Wang et al, 2006). Calculations suggest that the transition from dry lithospheric mantle to a "damp" asthenosphere (Hirth et al 2000) would result in about an order-of-magnitude increase in conductivity (Karato 1990;Hirth and Kohlstedt 2003).…”

Section: Discussionmentioning

confidence: 99%

The elusive lithosphere–asthenosphere boundary (LAB) beneath cratons

Eaton

Darbyshire

Evans

et al. 2009

Lithos

393

288

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The lithosphere-asthenosphere boundary (LAB) is a first-order structural discontinuity that accommodates differential motion between tectonic plates and the underlying mantle. Although it is the most extensive type of plate boundary on the planet, its definitive detection, especially beneath cratons, is proving elusive. Different proxies are used to demarcate the LAB, depending on the nature of the measurement. Here we compare interpretations of the LAB beneath three The seismic LAB beneath cratons is typically regarded as the base of a high-velocity mantle lid, although some workers infer its location based on a distinct change in seismic anisotropy.Surface-wave inversion studies provide depth-constrained velocity models, but are relatively insensitive to the sharpness of the LAB. The S-receiver function method is a promising new seismic technique with complementary characteristics to surface-wave studies, since it is 2 sensitive to sharpness of the LAB but requires independent velocity information for accurate depth estimation. Magnetotelluric (MT) observations have, for many decades, imaged an "electrical asthenosphere" layer at depths beneath the continents consistent with seismic lowvelocity zones. This feature is most easily explained by the presence of a small amount of water in the asthenosphere, possibly inducing partial melt. Depth estimates based on various proxies considered here are similar, lending confidence that existing geophysical tools are effective for mapping the LAB beneath cratons.

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Section: Discussionmentioning

confidence: 99%

The elusive lithosphere–asthenosphere boundary (LAB) beneath cratons

Eaton

Darbyshire

Evans

et al. 2009

Lithos

393

288

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“…Aside from the chemical composition, other available alternative causes for high conductivity anomalies can be considered, such as water in nominally anhydrous minerals (Wang et al, 2006;Yang, 2011;Karato, 2009, 2014a), interconnected saline (or aqueous) fluids (Hashim et al, 2013;Shimojuku et al, 2014;Sinmyo and Keppler, 2017;Guo et al, 2015;Li et al, 2018), partial melting (Wei et al, 2001;Maumus et al, 2005;Gaillard et al, 2008;Ferri et al, 2013;Laumonier et al, 2015Laumonier et al, , 2017Ghosh and Karki, 2017), interconnected secondary high conductivity phases (e.g., FeS, Fe 3 O 4 ; Jones et al, 2005;Bagdassarov et al, 2009;Padilha et al, 2015), dehydration of hydrous minerals (Wang et al, 2012(Wang et al, , 2017Manthilake et al, 2015Manthilake et al, , 2016Hu et al, 2017;Sun et al, 2017a, b;Chen et al, 2018) and graphite films on mineral grain boundaries (Freund, 2003;Pous et al, 2004;Chen et al, 2017). In consideration of the similar formation conduction and geotectonic environments, the Himalaya-Tibetan orogenic system was compared with the Dabie-Sulu UHPM belt and explained high electrical conductivity anomalies.…”

Section: Geophysical Implicationsmentioning

confidence: 99%

Effect of chemical composition on the electrical conductivity of gneiss at high temperatures and pressures

Dai

Sun

et al. 2018

Solid Earth

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Abstract. The electrical conductivity of gneiss samples with different chemical compositions (W A = Na 2 O + K 2 O + CaO = 7.12, 7.27 and 7.64 % weight percent) was measured using a complex impedance spectroscopic technique at 623-1073 K and 1.5 GPa and a frequency range of 10 −1 to 10 6 Hz. Simultaneously, a pressure effect on the electrical conductivity was also determined for the W A = 7.12 % gneiss. The results indicated that the gneiss conductivities markedly increase with total alkali and calcium ion content. The sample conductivity and temperature conform to an Arrhenius relationship within a certain temperature range. The influence of pressure on gneiss conductivity is weaker than temperature, although conductivity still increases with pressure. According to various ranges of activation enthalpy (0.35-0.52 and 0.76-0.87 eV) at 1.5 GPa, two main conduction mechanisms are suggested that dominate the electrical conductivity of gneiss: impurity conduction in the lower-temperature region and ionic conduction (charge carriers are K + , Na + and Ca 2+ ) in the higher-temperature region. The electrical conductivity of gneiss with various chemical compositions cannot be used to interpret the high conductivity anomalies in the Dabie-Sulu ultrahigh-pressure metamorphic belt. However, the conductivity-depth profiles for gneiss may provide an important constraint on the interpretation of field magnetotelluric conductivity results in the regional metamorphic belt.

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“…Based on these studies, the water storage capacity in the upper mantle and transition zone has been estimated [Hirschmann et al, 2005]. Constraints on the water content in these regions were also inferred based on the results of electrical conductivity measurements on olivine [Wang et al, 2006], orthopyroxene [Dai and Karato, 2009b], wadsleyite and ringwoodite [Dai and Karato, 2009c;Huang et al, 2005]. However, these studies are incomplete since these minerals occupy only $40-80% of these regions, and the robustness of results of these studies hinges upon the degree to which the remaining mineral phases influence the hydrogen solubility and distribution.…”

Section: Introductionmentioning

confidence: 99%

Solubility of water in pyrope‐rich garnet at high pressures and temperature

Mookherjee

Karato

2010

Geophysical Research Letters

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[1] The water solubility in pyrope-rich garnet was determined between pressures of 5-9 GPa and temperatures of 1373 -1473 K under silica activity and oxygen fugacity similar to those expected in the Earth's upper mantle. We found that pyrope-rich garnet has substantial water solubility up to $0.1 wt% under these conditions. In addition, the water content in garnet varied as a function of chemical conditions. In particular, the variation in water fugacity (and Mg#) caused a variation in water partitioning with olivine (D H 2 O ol/py ). The substantial water solubility in pyrope-rich garnet under deep upper mantle conditions might have significant influence on physical and transport properties.Citation: Mookherjee, M., and S. Karato (2010), Solubility of water in pyrope-rich garnet at high pressures and temperature, Geophys. Res. Lett., 37, L03310,

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The effect of water on the electrical conductivity of olivine

Cited by 360 publications

References 27 publications

The elusive lithosphere–asthenosphere boundary (LAB) beneath cratons

The elusive lithosphere–asthenosphere boundary (LAB) beneath cratons

Effect of chemical composition on the electrical conductivity of gneiss at high temperatures and pressures

Solubility of water in pyrope‐rich garnet at high pressures and temperature

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