Abstract
Apparent differences in the distribution of Fe (super ++) between olivine and calcium-poor pyroxene are correlated with the differing geological environment of the specimens. The data examined cover igneous rocks, peridotite nodules in igneous rocks, peridotite lenses in gneiss, schist, etc., meteorites, and some thermal and regional metamorphic rocks. . . . The hypothesis that all igneous rocks in the magnesian composition range contain disequilibrium assemblages is consistent with the observations and with expectations based upon the experimentally determined behavior of silicate melts in artificial systems. The olivine nodules in basalts appear to belong with the products of igneous crystallization, as do some orogenic belt peridotite intrusives.
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