Abstract
δ 18O values of unaltered olivine and pyroxene phenocrysts in boninites from several areas range from 5.8 to 7.4 and indicate that the source for most boninites is more 18O-rich than MORBs and other oceanic basalts. The source for oxygen and other major elements is most likely a refractory portion of the mantle having a δ 18O value of up to 7.0 to which must be added a small amount of H2O-rich fluid to induce partial melting. This fluid, which is derived from subducted crust, is the vehicle for LREEs including Nd. The variable, normally low ɛ Nd values typical of boninites do not correlate with the δ 18O values.
Post eruptive exchange of oxygen in the glass of boninites with that of sea water at low temperatures (<150° C) produces δ 18O values of >10 in optically fresh glass. Hydration of the glass has increased the water contents of most boninites from estimated magmatic values of 1–2 wt% to 2–4 wt% and produced δD values of < −80, which may be lower than the original magmatic δD values. In contrast to most submarine pillow basalts, the magmatic volatile composition of boninite lavas has been extensively modified as a result of post eruptive interaction with seawater.
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Kyser, T.K., Cameron, W.E. & Nisbet, E.G. Boninite petrogenesis and alteration history: constraints from stable isotope compositions of boninites from Cape Vogel, New Caledonia and Cyprus. Contr. Mineral. and Petrol. 93, 222–226 (1986). https://doi.org/10.1007/BF00371324
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DOI: https://doi.org/10.1007/BF00371324