2.04 - Mineralogy of the Earth – Trace Elements and Hydrogen in the Earth’s Transition Zone and Lower Mantle

Abstract

We review the experimental and theoretical constraints on the distribution of trace elements in the transition zone and lower mantle, with particular emphasis on refractory lithophile elements and H2O. We begin with a summary of element partitioning between high-pressure minerals of transition zone and lower mantle and coexisting silicate melts. Mineral–melt partitioning of trace elements in the deep Earth obeys the elastic strain model with partition coefficients showing a near-parabolic dependence on ionic radius for cations of fixed charge. Experiments also indicate that many elements (e.g. Zr, Hf, U, Th) which are incompatible in upper mantle minerals are compatible in Mg- and Ca-perovskites of the lower mantle. The high partition coefficients of, for example, 3+ and 4+ cations into the Ca-site of Ca-perovskite arise from the ease with which excess charge is compensated in the perovskite structure by creation of cation vacancies. One important implication is that, despite being a volumetrically minor phase, Ca-perovskite contains most of the heat-producing elements Th and U in the deep Earth, as well as being the principal host of the rare earth elements. Measured mineral-melt partition coefficients for deep mantle minerals also indicate that there cannot be large volumes of a majoritic or perovskitic reservoir isolated in the lower mantle since the ‘magma ocean’ stage of early Earth history. Given this constraint, any such region would have geochemical characteristics similar to those of the HIMU component of oceanic basalts while downward migration of dense melts in equilibrium with Ca-perovskite could, in principle, lead to formation of a complementary reservoir, unradiogenic in Pb and with a subchondritic 142Nd/144Nd ratio.