note to typesetters: aSiO 2 and fO 2 , used throughout, are sub sub, i.e. SiO
and O ]]
AbstractThe diffusion and substitution mechanisms and Cr in forsterite were studied as a function of crystallographic orientation and the chemical potentials of all four components in the system MgO-SiO 2 -Cr-O. Oxygen fugacity (fO 2 ) was varied over 15.4 log units at 1400 °C and was fixed at iron-wüstite equilibrium for a temperature series (1200-1500 °C). The valence state changes of Cr along some diffusion profiles was also investigated using X-ray absorption near edge structure spectroscopy.Cr diffusion was found to be anisotropic (fastest along the c axis), and considerably faster in the presence of protoenstatite (high silica activity, aSiO 2 ) than in the presence of periclase (low aSiO 2 ). Cr diffusion profiles were longer at lower fO 2 with more extreme diffusive anisotropy at higher fO 2 . Determined Cr diffusion coefficients were similar to those of Fe-Mg inter-diffusion in olivine at equivalent conditions. The diffusivity of Cr was found to be a function of its own concentration, but, as an approximation, Cr diffusion (in m 2 /s) along the c axis of pure forsterite, at an fO 2 corresponding to iron-wüstite at 200 µg/g Cr could be described using:. .where R is the gas constant in kJ/Kmol and T is the temperature in Kelvin.In forsterite, the valence state ratio of chromium (Cr 2+ ΣC , whe e ΣC Cr 2+ +Cr 3+ ) changed systematically along diffusion profiles. The equilibrium Cr 2+ ΣC ati imposed by the fO 2 of the experiment was observed at the diffusion interface, and this changed to a constant value in the crystal interior. Cr 3+ always substitutes onto an octahedral site in olivine. At high aSiO 2 , Cr 3+ uses M site vacancies ([vac]) for charge balance (i.e. C a SiO ), whereas at low aSiO 2 a new mechanism was observed with charge balance achieved by Mg 2+ on the tetrahedral site producing a ' pinel type' ub tituti n, C O . Cr 2+ always substitutes directly for Mg 2+ , forming the C SiO substitution. Comparative experiments using San Carlos olivine showed slightly faster Cr diffusion, a lesser concentration dependence of diffusion and no Cr valence state change along diffusion profiles. Diffusion in olivine exerts control over mantle rheology (e.g. Ricoult and Kohlstedt, 1985), electrical conductivity (e.g. Karato, 1990) and retention of trace and major element signatures in melt inclusions (e.g. Gaetani and Watson, 2000; Spandler et al., 2007). Frozen diffusion profiles can yield timescales of volcanic and magmatic processes (e.g. Costa and Dungan, 2005; Peslier et al., 2015; Ruprecht and Plank, 2013) and rates of diffusion partially determine closure temperatures of radiogenic dating systems (Dodson, 1973; Tirone, 1999, 2001). Therefore, it is not surprising that the effects of pressure, temperature, oxygen fugacity (fO 2 ), chemical activity (e.g. aSiO 2 ) and isotopic mass on diffusion in olivine have been thoroughly investigated (Brady and Cherniak, 2010; Chakraborty, 2010 and references therein), such that ...