Average models for calculating the shock equation of state of alloy and mixture

Young, G.; Liu, Xun; Leng, Chunwei; Huang, Huisheng

doi:10.7567/1347-4065/ab1c1e

Cited by 3 publications

(2 citation statements)

References 16 publications

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“…

Δ E_{T}

is the change in the internal energy due to isothermal compression,

Δ E_{T} = \int_{V_{0 m}}^{V} T_{0} C_{V} \frac{γ}{V} d V - \int_{V_{0 m}}^{V} P_{T} d V,

where

V_{0 m}

is the specific volume of the FeO metal phase. The internal energy was deduced from our previous report (Young, et al., 2019). In Equation 5, both the Grüneisen parameter (

γ

) and specific heat capacity at constant volume (

C_{V}

) include the lattice and electronic contributions:

γ = (γ_{N} C_{V N} + γ_{e} C_{V e}) / C_{V},

C_{V} = C_{V N} + C_{V e},

…”

Section: Resultsmentioning

confidence: 99%

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Equation of State for Fe‐9.0 wt% O up to 246 GPa: Implications for Oxygen in the Earth's Outer Core

et al. 2021

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Oxygen has been proposed as a potential major light element because it is the most abundant element on Earth. The partition experiments of siderophile elements between silicate melts and liquid metals also indicate that oxygen is a plausible candidate for a light element dissolved in the Earth's outer core (Fischer, 2015; Frost et al., 2010; Ozawa et al., 2009; Takafuji et al., 2005). The impact of oxygen on the density and sound velocity of Fe-rich melts is critical for interpreting the composition, dynamics, and evolution of the Earth's core. However, the amount of oxygen in the core is still a topic of debate. To examine the possibility of oxygen being the main light element in the Earth's outer core, the equation of sate (EoS) and phase relations of FeO were measured by static compression and shock wave loading. Fischer et al. (2011a, 2011b) performed X-ray diffraction measurements using a laser-heated diamond anvil cell to achieve the EoS of FeO, and determined that ∼7.7 wt% oxygen is required in the outer core to match the seismologically determined density. Our previous shockwave data in the Fe-SO system showed negligible oxygen in the outer core since adding oxygen into liquid iron would not simultaneously reproduce the observed density and sound velocity profiles of the outer core (Huang et al., 2011). The liquid phase relation, especially, the Fe-FeO eutectic alloys, provides another clue to constrain the outer core composition. The latest melting data on Fe-O alloys up to 204 GPa in a diamond-anvil cell supported ∼13 wt% oxygen in the liquid outer core (Oka et al., 2019). A thermodynamic model developed by Komabayashi (2014) predicted ∼12 wt% oxygen in the eutectic liquid composition at 330 GPa, which contradicts the experimental results reported by Morard et al. (2017). Therefore, the constraint on the concentration of oxygen in the Earth's

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“…

Δ E_{T}

is the change in the internal energy due to isothermal compression,

Δ E_{T} = \int_{V_{0 m}}^{V} T_{0} C_{V} \frac{γ}{V} d V - \int_{V_{0 m}}^{V} P_{T} d V,

where

V_{0 m}

is the specific volume of the FeO metal phase. The internal energy was deduced from our previous report (Young, et al., 2019). In Equation 5, both the Grüneisen parameter (

γ

) and specific heat capacity at constant volume (

C_{V}

) include the lattice and electronic contributions:

γ = (γ_{N} C_{V N} + γ_{e} C_{V e}) / C_{V},

C_{V} = C_{V N} + C_{V e},

…”

Section: Resultsmentioning

confidence: 99%

“…where 0m V is the specific volume of the FeO metal phase. The internal energy was deduced from our previous report (Young, et al, 2019). In Equation 5, both the Grüneisen parameter ( ) and specific heat capacity at constant volume ( V C ) include the lattice and electronic contributions:…”

Section: Resultsmentioning

confidence: 99%