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By J. G. Fitton, Bridget Gilfillan Upton

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Earth planet. Sci. Lett. 46, 323-34. OLAFSSON, M. & EGGLER, D. H. 1983. Phase relations of amphibole, amphibole-carbonate, and phlogo- Mantle metasomatism pite-carbonate peridotite: petrologic constraints on the asthenosphere. Earth planet. Sci. Lett. 64, 305-15. OLDENBURG, D. W. 1981. Conductivity structure of oceanic upper mantle beneath the Pacific plate. Geophys. J. R. astron. Soc. 65, 359-94. O'REILLY, S. Y. & GRIFFIN, W. L. 1984. Sr isotopic heterogeneity in primitive basaltic rocks, southeastern Australia: correlations with mantle metasomatism.

L. 1984. Sr isotopic heterogeneity in primitive basaltic rocks, southeastern Australia: correlations with mantle metasomatism. Contrib. Mineral. Petrol. 87, 220-30. PRESNALL, D. C. 1969. The geometrical analysis of partial fusion. Am. J. Sci. 267, 1178-94. SCLATER, J. , JAUPART, C. & GALSON, D. 1980. The heat flow through oceanic and continental crust and the heat loss of the Earth. Rev. Geophys. Space Phys. 18, 269-311. , HAGER, B. H. & JAYS, J. F. 1982. Melt segregation from partially molten source regions: the importance of melt density and source region size.

1987), Menzies (1983, and references cited therein), Menzies & Wass (1983), Cohen et al. (1984) and Menzies & Halliday (1984). Other data are taken from the references given in the caption to Fig. 4. z4 M. Menzies Contamination with significant amounts of crust is unlikely because of the rapidity with which these melts must reach the surface in order to maintain their load of high-density inclusions and diamonds. Furthermore, the extremely high concentrations of Sr (678-1845 ppm) and Nd (48-336 ppm) would require mixing with a highly radiogenic crustal component or stoping and assimilation of considerable amounts of crust.

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