Abstract
Monazite is the most abundant REE mineral that is formed in a wide range of geochemical conditions. This mineral is the most widespread in the felsic magmatic rocks, and it occurs in alkaline rocks, their pegmatites, and definite metamorphic complexes. Since, besides REEs, it contains significant amounts of Th and U cations, an increasing number of works in recent decades have focused on the use of this mineral for geochronological dating. Moreover, monazite and, more precisely, its compositional specifics in different phases of granitoid intrusions are employed not only for dating, but also for understanding the physicochemical evolution of magmatic complexes. In particular, significant differences were found between the compositions of predominant primary monazite in the two-mica Ireteba granites, southern Nevada (with an age of ~64 Ma), and late (secondary) monazite, which replaces it and is restricted to the influence zones of Late Miocene granite plutons (~14‐18 Ma). The replacement occurred at temperatures below 400 ° C and was expressed in a significant decrease in the content of the huttonite (ThSiO 4 ) end member with a simultaneous increase in the La/Sm and Sm/Y ratios. There is an article [2] dedicated to a detailed SHRIMP study of monazite from the Middle Archean greenschist metamorphic rocks of the Pilbara craton, Western Australia. It was shown that metamorphic monazite is represented by three generations corresponding to different “growth stages.” The La, Sm, Y, and Th distribution mapping combined with U‐Pb dating revealed the presence of distinct cores and rims in some crystals and provided insight into a hidden spatiotemporal pattern of distribution of fluid flows related to tectonic processes. Additionally, the authors of [3] demonstrated that a similar technique can be applied to determine the main trends in monazite evolution during formation of highgrade granulite-facies rocks in gneisses contained in the Challenger Au deposit (South Australia). The determination of Ce, Nd, Sm, Eu, and Gd contents in this mineral made it possible to trace the formation of its compositional domains towards the core: growth during partial melting in the closed system.
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