Abstract
The oxygen isotope composition of genetically related minerals is known to form a compact common field of values, the area of which depends only on variations in physicochemical parameters of the mineralforming medium. After a mineral has formed, the oxygen isotope composition does not change only if the mineral has not been transformed completely as a result of melting, chemical replacement, or other such reactions changing the primary structure. Therefore, the oxygen isotope composition has long served as an indicator of specific conditions for the formation both of minerals and rocks in general. We have studied samples of corundum-bearing garnet‐amphibole‐phlogopite plagiogneiss of the Proterozoic age from the Chupa Sequence of the Belomorian Complex of the Khitostrov deposit (Fig. 1).
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