Abstract
The concentration of Fe3+ in mantle minerals determines many of their physical and chemical properties. Traditionally iron in major mantle phases has been assumed to be predominantly Fe2+, but results from both high-pressure experiments and inclusions in diamonds from the lower mantle suggest that approximately half of the iron in lower mantle (Mg,Fe)(Si,Al)O3 perovskite is Fe3+. This paper reviews the current state of knowledge of iron oxidation state and oxygen fugacity in the mantle based on Mossbauer results from natural and synthetic samples, and discusses new ideas that have arisen from these results.
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