Amphibole and biotite were the principal mafic minerals precipitated during the magmatic and post-magmatic (including hydrothermal) crystallisation stages of coeval metaluminous to slightly peraluminous syenogranites and peralkaline alkali-feldspar granites of the Mandira Granite Massif, in the post-collisional A-type Graciosa Province, S-SE Brazil. Magmatic calcic (ferro-ferri-hornblende and hastingsite) amphiboles occur in the metaluminous syenogranites, whereas calcic (ferro-edenite), sodic–calcic (ferro-ferri-winchite) and sodic (arfvedsonite and riebeckite) amphiboles occur in peralkaline alkali-feldspar granites. Rare earth element (REE) contents decrease from hornblende to winchite and riebeckite, and the partition coefficients indicate increasing compatibility from light rare earth elements (LREE) to heavy rare earth elements (HREE), with a marked preference for the HREE over the LREE in the sodic–calcic and, particularly, the sodic amphiboles. Post-magmatic calcic- (ferro-actinolite) and sodic- (riebeckite) amphiboles are also present in the peralkaline granites. Magmatic biotite (annite) is dominant in syenogranites, whereas post-magmatic annite and late-to post-magmatic annite evolving to siderophyllite occurs in the peralkaline granites. Typical hydrothermal phyllosilicates are chlorite (chamosite) in syenogranites and related greisens, and ferri-stilpnomelane which is present in both peralkaline granites and metaluminous syenogranites. Lithostatic pressure estimates suggest that the main granites were emplaced under pressures of ~93–230 MPa, with close-to-liquidus temperatures varying from ~830°C for syenogranites to ~900°C for the peralkaline granites. The original magmas crystallised mainly under relatively reduced (buffered at ~ –1 ≤ QFM ≤ 0), and more oxidising (somewhat above QFM) environments, respectively. Chlorite, replacing biotite in syenogranites and as the main mineral in the related greisens, permits the temperature of the main hydrothermal event to have taken place between 250 and 272°C. Estimated log (fHF/fHCl) values from biotite compositions vary from ~ –2 to –1 (syenogranites) and ~ –3.5 to –2 (peralkaline granites) and indicate F preference over Cl in the hydrothermal fluid phase.

角闪石和黑云母是在碰撞后 A 型 Graciosa 的 Mandira 花岗岩地块的同期金属铝质至微铝质正长花岗岩和过碱性碱长石花岗岩的岩浆和后岩浆（包括热液）结晶阶段沉淀的主要基性矿物省，S-SE 巴西。岩浆钙质角闪石（铁-铁-角闪石和黑斯廷石）角闪石出现在金属铝质正长花岗岩中，而钙质（铁-伊丹岩）、钠-钙质（铁-铁-温奇石）和钠（阿弗德钠石和里贝克石）角闪石出现在高碱性碱长石中花岗岩。稀土元素（REE）含量从角闪石到菱闪石和里贝克石，分配系数表明从轻稀土元素（LREE）到重稀土元素（HREE）的相容性增加，在钠钙闪石，尤其是钠闪石中，HREE 明显优于 LREE。过碱性花岗岩中也存在岩浆后钙质（铁阳起石）和钠闪石（riebeckite）角闪石。岩浆黑云母（安妮岩）在正长花岗岩中占主导地位，而后岩浆岩浆岩和晚期至后岩浆岩浆演化为铁蜡岩的花岗岩则出现在过碱性花岗岩中。典型的热液层状硅酸盐是正长花岗岩和相关灰岩中的绿泥石（菱镁矿），以及同时存在于过碱性花岗岩和金属铝质正长花岗岩中的铁-硅铁矿。岩石静压估计表明，主要花岗岩在约 93-230 MPa 的压力下就位，接近液相线的温度从正花岗岩的约 830°C 到高碱性花岗岩的约 900°C 不等。原始岩浆主要分别在相对还原（缓冲在 ~ –1 ≤ QFM ≤ 0）和更多氧化（略高于 QFM）环境下结晶。绿泥石取代了正长花岗岩中的黑云母并作为相关灰岩中的主要矿物，使得主要热液事件的温度发生在 250 至 272°C 之间。估计日志 (来自黑云母组合物的f HF / f HCl ) 值从 ~ –2 到 –1（正长花岗岩）和 ~ –3.5 到 –2（高碱性花岗岩）变化，表明在热液流体相中 F 优先于 Cl。