Effect of oxygen fugacity on the H2O storage capacity of forsterite in the carbon-saturated systems

Sokol, Alexander G.; Palyanov, Yury N.; Kupriyanov, Igor N.; Litasov, Konstantin D.; Polovinka, Mariya P.

doi:10.1016/j.gca.2010.05.032

Cited by 33 publications

(8 citation statements)

References 65 publications

(99 reference statements)

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“…Solubility of water is the maximum amount of water that can be incorporated in minerals under given thermodynamic conditions (Demouchy & Bolfan-Casanova, 2016) and can be described with an Arrhenian formalism with dependencies on pressure, temperature, silica activity, water fugacity, oxygen fugacity, major oxide composition, and other trace elements such as trivalent cations or Ti in olivine (Berry et al, 2007;D. Zhao, 2004;Gaetani et al, 2014;Keppler, 2006;Padrón-Navarta & Hermann, 2017;Sokol et al, 2010).…”

Section: Solubility and Partitioning Of Structural Water In Mantle MImentioning

confidence: 99%

“…Solubility of water is the maximum amount of water that can be incorporated in minerals under given thermodynamic conditions (Demouchy & Bolfan‐Casanova, 2016) and can be described with an Arrhenian formalism with dependencies on pressure, temperature, silica activity, water fugacity, oxygen fugacity, major oxide composition, and other trace elements such as trivalent cations or Ti in olivine (Berry et al., 2007; D. Zhao, 2004; Gaetani et al., 2014; Keppler, 2006; Padrón‐Navarta & Hermann, 2017; Sokol et al., 2010).

C_{w} = A f_{H_{2} O}^{m} f_{O_{2}}^{q} e x p ((), \frac{- P normalΔ V α_{e l} X_{e l}}{R T})

where

f_{H_{2} O}

and

f_{O_{2}}

are oxygen and water fugacities, m and q are exponent values that may change depending on the defect speciation of the mineral, and α el and X el are the contribution constant and molar fraction of the effective chemical constituent, respectively (Keppler, 2006).…”

Section: Introductionmentioning

confidence: 99%

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MATE: An Analysis Tool for the Interpretation of Magnetotelluric Models of the Mantle

Özaydın

Selway

2020

Geochem Geophys Geosyst

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Interpretation of electrical conductivity anomalies observed in magnetotelluric models provides an important opportunity to understand the nature of the lithospheric mantle and its dynamics. Over the course of the last two decades, a great number of experimental petrology studies have been carried out which can be utilized to construct electrical conductivity distribution models for a given composition and geotherm. We have developed an open‐source software (MATE, Mantle Analysis Tool for Electromagnetics) with an easy‐to‐use graphical interface that creates such theoretical models. The program is developed in such a way that additional effects and models can be added very easily. To investigate the conductivity distribution of the cratonic mantle, a series of experiments was made. Results indicate that it is of utmost importance to analyze the magnetotelluric models using accurate compositions, water distributions, and geometric models. Hence, using only olivine conductivity models can lead to erroneous interpretations of both conductivity and estimated water content. Analysis of the potential causes for conductive anomalies shows that the upper and lower lithospheric mantle can be interpreted separately with the transition between them at 75–125 km. Conductive anomalies in the upper lithospheric mantle (<1,000 Ωm) are likely to be explained by the existence of well‐connected minor phases associated with metasomatic fluids, whereas in the lower lithospheric mantle, hydration and/or well‐connected minor phases (e.g., phlogopite or amphibole) can explain conductive anomalies.

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Section: Solubility and Partitioning Of Structural Water In Mantle MImentioning

confidence: 99%

C_{w} = A f_{H_{2} O}^{m} f_{O_{2}}^{q} e x p ((), \frac{- P normalΔ V α_{e l} X_{e l}}{R T})

where

f_{H_{2} O}

and

f_{O_{2}}

Section: Introductionmentioning

confidence: 99%

MATE: An Analysis Tool for the Interpretation of Magnetotelluric Models of the Mantle

Özaydın

Selway

2020

Geochem Geophys Geosyst

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“…However, current experimental data on water solubility in NAMs cannot be extrapolated to the critical region in the slab at 100-200 km depth where most dehydration reactions are taking place at temperatures lower than 800°C (Schmidt & Poli, 1998). The vast majority of previous experiments in olivine have been conducted in simple systems at supersolidus conditions (typically in the range of 1100-1500°C) or at pressures believed to be close to supercritical conditions of the fluid phase (e.g., Ardia et al, 2012;Bali et al, 2008;Férot & Bolfan-Casanova, 2012;Kohlstedt et al, 1996;Mosenfelder et al, 2006;Sokol et al, 2010;Withers & Hirschmann, 2008;Withers et al, 2011). At these extreme conditions the chemical potential of water (i.e., water fugacity) cannot be directly constrained by using an equation of state for pure H 2 O due to the increase of the mineral solubility in the coexisting fluid/melt (e.g., Bali et al, 2008;Hermann et al, 2006).…”

Section: Introductionmentioning

confidence: 99%

A Subsolidus Olivine Water Solubility Equation for the Earth's Upper Mantle

Padrón‐Navarta

Hermann

2017

JGR Solid Earth

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The pressure and temperature sensitivity of the two most important point hydrous defects in mantle olivine involving Si vacancies (associated to trace amounts of titanium [TiChu‐PD] or exclusively to Si vacancies [Si]) was investigated at subsolidus conditions in a fluid‐saturated natural peridotite from 0.5 to 6 GPa (approximately 20–200 km depth) at 750 to 1050°C. Water contents in olivine were monitored in sandwich experiments with a fertile serpentine layer in the middle and olivine and pyroxene sensor layers at the border. Textures and mineral compositions provide evidence that olivine completely recrystallized during the weeklong experiments, whereas pyroxenes displayed only partial equilibration. A site‐specific water solubility law for olivine has been formulated based on the experiments reconciling previous contradictory results from low‐ and high‐pressure experiments. The site‐specific solubility laws permit to constrain water incorporation into olivine in the subducting slab and the mantle wedge, as these are rare locations on Earth where fluid‐present conditions exist. Chlorite dehydration in the hydrated slab is roughly parallel to the isopleth of 50 ± 20 ppm wt H2O in olivine, a value which is independent of the pressure and temperature trajectory followed by the slab. Hydrous defects are dominated by [Si] under the relevant conditions for the mantle wedge affected by fluids coming from the slab dehydration (slab‐adjacent low viscosity/seismic low‐velocity channel, P > 3 GPa). In cold subduction zones at 5.5 km from the slab surface the storage capacity of the mantle wedge at depths of 100–250 km ranges from 400 to 2,000 ppm wt H2O.

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“…Finally, it should be noted that both reactions (5) and (6) can increase fO 2 in the system, since the hydrogen released in the two reactions diffuses out of the sample capsule, allowing hematite to form. In previous studies, similar experiments have been conducted on simplified peridotite systems under hydrous conditions, but rarely reported the formation of hematite (Sokol et al 2010;Litasov et al 2014). It is assumed that the double-capsule method used in these author's experiments (usually a reduced inner or outer capsule, e.g., Fe or graphite) and the hydrogen-rich transmitting medium put between the inner and outer capsules prevents the escape of hydrogen, thus inhibiting reactions (5) and (6) and thus preventing the formation of hematite.…”

Section: Scenario 2: Dehydrogenation-oxidationmentioning

confidence: 99%

Experimental constraints on formation of hematite in olivine at high pressures and temperatures

Zhang

Wang

et al. 2015

Phys Chem Minerals

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Effect of oxygen fugacity on the H2O storage capacity of forsterite in the carbon-saturated systems

Cited by 33 publications

References 65 publications

MATE: An Analysis Tool for the Interpretation of Magnetotelluric Models of the Mantle

MATE: An Analysis Tool for the Interpretation of Magnetotelluric Models of the Mantle

A Subsolidus Olivine Water Solubility Equation for the Earth's Upper Mantle

Experimental constraints on formation of hematite in olivine at high pressures and temperatures

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