Chemical and O-isotope compositions of amphiboles and clinopyroxenes from A-type granites of the Papanduva Pluton, South Brazil: Insights into late- to post-magmatic evolution of peralkaline systems

•Amphibole and clinopyroxene are late- to post-magmatic phases.•Evolution trends are defined by increasing Na and Fe3 + and decreasing Ca and Fe2 +.•Composition of coexisting fluids controls the rare-earth element partitioning.•Oxygen isotope ratios positively correlate with increasing rock deformation.•Sub-magmatic deformation influenced the circulation of residual melts and fluids.

Clinopyroxene and amphibole are the main mafic minerals in peralkaline granites of the Papanduva Pluton, Morro Redondo Complex, one of the most important granitic occurrences within the Graciosa A-type Province, S-SE Brazil. Clinopyroxene is present as three distinct late- to post-magmatic textural generations of aegirine, as well as post-magmatic aegirine–augite. Amphibole is predominantly magmatic ferrorichterite and arfvedsonite, and post-magmatic riebeckite. Major and trace element compositions reveal evolutionary trends characterized by increasing Fe3 + and Na and decreasing Fe2 +, Ca, HFSE, and REE contents from core to crystal rims; trace element and REE partitioning is controlled by the composition of the coexisting melts or fluid phases, as well as by crystal chemistry. δ18O values for minerals investigated range from + 2.3 to + 6.4‰ and correlate both with increasing degrees of alkalinity and quasi-solidus (sub-magmatic) deformation affecting several granites of the Papanduva Pluton. These deformation events played a significant role in the concentration and circulation of residual melts and fluid phases from which amphiboles and clinopyroxenes precipitated. Combined textural, chemical, and O isotope findings suggest that these fluids evolved through more oxidizing (close to the FMQ buffer), alkali- (i.e. peralkaline), fluorine-, and 18O-rich conditions, associated with higher abundances of HFSEs and REEs within a temperature interval between 750 and 700 °C (late-magmatic stages) and 400–450 °C (post-magmatic stages).

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