Fig. 1: The solidus temperature profile of primitive materials in Earth’s mid-mantle pressure range at different oxygen fugacities.
From: Melting at the base of a terrestrial magma ocean controlled by oxygen fugacity
Closed diamonds: this study (pyrolite composition at fO2 = IW + 2.0), including ±50 °C uncertainties (described in the note of Table 1); open diamonds: Ishii et al.19 (minimum solidus temperatures, indicated by the red arrows, for a pyrolite composition at estimated IW − 1.2); open circles: Herzberg et al.17 (KLB-1 peridotite composition, estimated IW − 1.2); open squares: Andrault et al.20 (chondritic mantle composition, oxygen fugacity not determined but more oxidized than IW − 1.2); crosses: Pierru et al.22 (pyrolitic mantle composition, oxygen fugacity estimated to be about IW + 2). All data are presented as mean values with ± standard errors (the latter when provided by the authors; Source Data Fig. 1). Dashed lines show predicted solidi at fO2 conditions invoked in siderophile element-based core formation models (IW − 1, IW − 2 and IW − 4), predicted based on equation (1).
