H2O storage capacity of olivine at 5-8 GPa and consequences for dehydration partial melting of the upper mantle

The H2O storage capacities of peridotitic minerals place crucial constraints on the onset of hydrous partial melting in the mantle. The storage capacities of minerals in equilibrium with a peridotite mineral assemblage ("peridotite-saturated" minerals) are lower than when the minerals coexist only with fluid because hydrous partial melt is stabilized at a lower activity of H2O. Here, we determine peridotite-saturated olivine H2O storage capacities from 5 to 8 GPa and 1400-1500 degrees C in layered experiments designed to grow large (similar to 100-150 mu m) olivine crystals in equilibrium with the full hydrous peridotite assemblage (melt+ol+opx+gar+cpx). The peridotite-saturated H2O storage capacity of olivine at 1450 degrees C rises from 57 +/- 26 ppm (by wt.) at 5 GPa to 254 +/- 60 ppm at 8 GPa. Combining these with results of a parallel study at 10-13 GPa (Tenner et al., 2011, CMP) yields a linear relation applicable from 5 to 13 GPa for peridotite-saturated H2O storage capacity of olivine at 1450 degrees C, C-H2O(olivine)(ppm) = 57.6(+/- 16) x P(GPa)-169(+/- 18). Storage capacity diminishes with increasing temperature, but is unaffected by variable total H2O concentration between 0.47 and 1.0 wt%. Both of these are as predicted for the condition in which the water activity in the melt is governed principally by the cryoscopic requirement of melt stability for a given temperature below the dry solidus. Measured olivine storage capacities are in agreement or slightly greater than those predicted by a model that combines data from experimental freezing point depression and olivine/melt partition coefficients of H2O (Hirschmann et al., 2009). Considering the temperature along the mantle geotherm, as well as available constraints on garnet/olivine and pyroxene/olivine partitioning of H2O (D-H2O(gar/ol),D-H2O(px/ol)), we estimate the peridotite H2O storage capacity in the low velocity zone. The C-H2O required to initiate melting between 150 and 250 km depth is between 270 and 855 ppm. We conclude that hydrous partial melting does not occur at these depths for H2O concentrations (50-200 ppm) typical of the convecting upper mantle sampled by mid-ocean ridge basalts. (C) 2012 Elsevier B.V. All rights reserved.