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. 2011 Oct 20;108(44):17901-17904. doi: 10.1073/pnas.1110594108

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Fig. 3. — Thermal conductivity models computed from our results using Hashin-Shtrikman averaging (28) for aggregates of 20% Pe + 80% Pv (top) and 20% Pe_Fe20 + 80% Pv_Fe03 (bottom). The mantle geotherm is constructed by combining a 1,600 K pyrolite adiabat (29) with a superadiabatic temperature increase in the bottom 200 km through the thermal boundary layer to reach the range of temperature estimates for the core-mantle boundary (30, 31). Temperatures in the thermal boundary layer thus increase from 2,600 ± 200 K at its top to at the CMB.

Inline graphic — Thermal conductivity models computed from our results using Hashin-Shtrikman averaging (28) for aggregates of 20% Pe + 80% Pv (top) and 20% Pe_Fe20 + 80% Pv_Fe03 (bottom). The mantle geotherm is constructed by combining a 1,600 K pyrolite adiabat (29) with a superadiabatic temperature increase in the bottom 200 km through the thermal boundary layer to reach the range of temperature estimates for the core-mantle boundary (30, 31). Temperatures in the thermal boundary layer thus increase from 2,600 ± 200 K at its top to at the CMB.