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2+ ratio of 0.05 or less. Samples were encapsulated in Mo, Re, or Fe capsules and heated at 1600°C {appropriate for 660-km depth [J. M. Brown and T. J. Shankland, Geophys. J. R. Astron. Soc. 66, 579 (1981)]} or 1500°C for 3 hours after pressuriziation to either 20.4 GPa (for spinel-bearing assemblages) or 25 GPa (for perovskite). Multianvil assemblies and pressure calibrations have been described previously (13, 15). The products were examined by x-ray diffraction, and compositions were determined with the JEOL 8600 electron microprobe at the University of Bristol. All compositions were determined by averaging 10 or more individual point analyses. Experimental data given in Table 1.
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4 olivine, which, at 25 GPa and 1600°C, decomposed into a fine intergrowth of perovskite and magnesiowüstite. Because individual crystals were not resolvable with the electron microprobe, the variation of Fe# with Si content was used to extrapolate to end-member compositions in the same manner as that used by Guyot et al. (10) and Fei et al. (8). We obtained an Fe# of 0.04 ± 0.02 for perovskite and 0.15 ± 0.02 for magnesiowüstite.
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13
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24
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9544255746
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note
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Multianvil experiments were performed at the Bayerisches Geoinstitut under the European Community "Human Capital and Mobility - Access to Large Scale Facilities" programme (contract ERBCH-GECT940053 to D.C.R.). B.J.W. acknowledges the support of the Alexander von Humboldt Stiftung during preparation of the manuscript.
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