Mineralogy of the Earth - Trace Elements and Hydrogen in the Earth's Transition Zone and Lower Mantle

B. J. Wood*, A. Corgne

*Corresponding author for this work

    Research output: Chapter in Book/Report/Conference proceedingChapter

    14 Citations (Scopus)

    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.Water-solubility measurements on deep mantle minerals demonstrate that wadsleyite and ringwoodite of the transition zone can dissolve much larger amounts of water (>2wt.%) than the low-pressure olivine polymorph (∼5000ppm). Maximum solubility does not, however, prove that high H2O contents are present in the Earth and the seismologically determined sharpness of the 410km discontinuity constrains the H2O content at this depth to about 400ppm by weight. Water-solubility measurements on the principal materials of the lower mantle are currently very scattered and there is a need for improvement of both synthesis and analytical methods. It is clear, however, that water is more soluble in the transition zone than in the lower mantle. These observations and mineral-melt partition coefficients for trace elements are not inconsistent with the transition zone 'water filter' hypothesis by which depleted upper mantle is generated by hydrous partial melting at 410km depth. The water-storage capacity of the upper mantle and the H2O contents of mid-ocean ridge basalts are, however, difficult to reconcile with this hypothesis.

    Original languageEnglish
    Title of host publicationTreatise on Geophysics
    PublisherElsevier
    Pages63-89
    Number of pages27
    Volume2
    Edition1st
    ISBN (Print)9780444527486
    DOIs
    Publication statusPublished - 2007

    Keywords

    • Lower mantle
    • Trace elements partitioning
    • Transition zone
    • Water solubility

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