Computer Science
Scientific paper
Jul 1992
adsabs.harvard.edu/cgi-bin/nph-data_query?bibcode=1992metic..27q.288s&link_type=abstract
Meteoritics, vol. 27, no. 3, volume 27, page 288
Computer Science
1
Scientific paper
Coexisting orthopyroxene (opx) and olivine (ol) in silicate inclusions of IAB-iron meteorites have different Fe/(Fe+Mg) ratios. Ferrosilite (fs) contents of opx are higher than fayalite contents (fa) of ol (e.g., Bunch and Keil 1970). Non-ideal solid solution of fs in opx and/or fa in ol is generally assumed. We reinvestigated the equilibrium Fe-Mg distribution between coexisting ol+opx in the system MgO-FeO-SiO2 (von Seckendorff and O'Neill 1992). Reversal experiments at high- Mg compositions were performed from 900 to 1600 degrees C at 16 and 20 kbar using a barium borosilicate flux. The data could be fitted to a simple thermodynamic model with ol and opx treated as regular solutions and this model was found to describe satisfactorily the literature data extending down to 700 degrees C. For Fe/(Fe+Mg) between 0.05 to 0.15 we find KD^ol-opx close to one from 1600 to 700 degrees C, virtually independent of pressure and temperature. Fig. 1 shows experimental results at the Mg-rich end. Error bars mark 1-sigma standard deviations. Ol is in all cases more Fe-rich than coexisting opx, except for a single run at 1000 degrees C that probably did not reach equilibrium because of slow reaction kinetics. Two calculated distribution curves (1300, 700 degrees C at 16 kbar) lie close together indicating the absence of any significant temperature dependence of the exchange reaction at the Mg- rich end of the system. IAB-silicate inclusions plot outside the range of experimental data (Fig. 1). Although some previous models for Fe-Mg exchange between ol and opx (e.g., Sack 1980) extrapolate to KD<1 at temperatures near 500 degrees C, such models reproduce the experimental data (700 to 1600 degrees C) less well, than our updated model. In addition, temperatures at 500 degrees C are probably too low to allow Fe diffusion in opx. Two pyroxene equilibration temperatures of IAB-silicate inclusions are around 900-1000 degrees C suggesting a similar closure temperature for Fe diffusion in opx. Because of this and because of the essentially temperature-independent Fe-Mg distribution between ol and opx from 1600 to 700 degrees C, we conclude that the Fe-Mg distribution between ol and opx in IAB-silicate inclusion does not reflect thermodynamic equilibrium. As Fe-diffusion in ol is faster than in opx, redistribution of Fe in ol should have occurred at a temperature below the closure temperature for Fe-diffusion in opx. We suggest that FeO in ol was reduced to Fe metal by some species such as C, P, S, etc. A lower limit for the temperature of the reducing event is provided by Ca-zoning in ol, which develops below 650 degrees C (Kohler et al. 1991). Since strong FeO zoning in ol is absent, reduction of FeO in ol should have occurred above 650 degrees C, assuming similar diffusion coefficients for Ca and Fe in ol. References: Bunch T.E. and Keil K. (1970) Contrib. Mineral. Petrol. 25, 297-340. Kohler T., Palme H. and Brey G. (1991) N. Jb. Miner. Mh. 9, 423-431. Sack R.O. (1980) Contrib. Mineral. Petrol. 71, 257-269. v. Seckendorff V. and O'Neill H.St.C. (1992) Contr. Min. Petrol. (submitted).
O'Neill Hugh St. C.
Palme Herbert
Seckendorff V. V.
Zipfel Jutta
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