Thermal equation of state of Al- and Fe-bearing phase D

Konstantin D. Litasov, Eiji Ohtani, Yu Nishihara, Akio Suzuki, Kenichi Funakoshi

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19 Citations (Scopus)

Abstract

Pressure-volume-temperature relations have been measured to 20.6 GPa and 1273 K for Fe- and Al-bearing phase D (Mg0.99Fe0.12 Al0.09Si1.75H2.51O6) using synchrotron X-ray diffraction with SPEED-MkII multianvil press at SPring-8 facility. The analysis of room temperature data fitted to a third-order Birch-Murnaghan equation of state (EOS) yields V0 = 85.32 ± 0.02 Å3; K0 = 141.5 ± 3 GPa and K' = 6.2 ± 0.4. The pressure was calibrated using the Au EOS by Anderson et al. (1989). Fixing K'to, 4.0, gives K0 = 155.3 ± 0.8 GPa. These values are consistent with thermal EOS analysis as well as previous estimations for Fe-Al-bearing and Fe-Al-free phase D. A fit to high-temperature P-V-T data using Birch-Murnaghan EOS yields V0 = 85.32 ± 0.02 Å3 ; K0 = 139.6 ± 3.0 GPa; K'= 6.6 ± 0.4; (∂KT/∂T)p= - 0.023 (8) GPa K-1 and zero-pressure thermal expansion α = a0 + a1 T with a0 = 3.4 (2) × 10-5 K-1 and a1 = 0.4 (6) × 10-8 K-1. The estimated Anderson-Grüneisen parameter is δT = 4.9. Lattice dynamical approach using the Mie-Grüneisen-Debye EOS yields Grüneisen parameter γ0 = 1.09 ± 0.09 and q = 0.42 ± 0.97, if Debye temperature χ0 fixed at 920 K, as calculated from sound velocities. The EOS from this study enables the accurate estimation of the density of phase D in a pyrolitic composition under deep mantle conditions. The density reduction of hydrated subducting, slab (∼1 wt.% H2O) in the lower mantle due to the presence of ∼7% of phase D would be 1.0%.

Original languageEnglish
Article numberB08205
JournalJournal of Geophysical Research: Solid Earth
Volume113
Issue number8
DOIs
Publication statusPublished - 2008 Aug 4

ASJC Scopus subject areas

  • Geophysics
  • Geochemistry and Petrology
  • Earth and Planetary Sciences (miscellaneous)
  • Space and Planetary Science

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