Most granitic batholiths contain plutons which are composed of low-variance mineral assemblages amenable to quantification of the P-T-f(O2)-f(H2O) conditions that characterise emplacement. Some mineral thermometers, such as those based on two feldspars or two Fe-Ti oxides, commonly undergo subsolidus re-equilibration. Others are more robust, including hornblende-plagioclase, hornblende-clinopyroxene, pyroxene-ilmenite, pyroxene-biotite, garnet-hornblende, muscovite-biotite and garnet-biotite. The quality of their calibration is variable and a major challenge resides in the large range of liquidus to solidus crystallisation temperatures that are incompletely preserved in mineral profiles. Further, the addition of components that affect K-d relations between non-ideal solutions remains inadequately understood. Estimation of solidus and near-solidus conditions derived from exchange thermometry often yield results > 700 degrees C and above that expected for crystallisation in the presence of an H2O-rich volatile phase. These results suggest that the assumption of crystallisation on an H2O-saturated solidus may not be an accurate characterisation of some granitic rocks. Vapour undersaturation and volatile phase composition dramatically affect solidus temperatures. Equilibria including hypersthene-biotite-sanidine-quartz, fayalite-sanidine-biotite, and annite-sanidine-magnetite (ASM) allow estimation of f(H2O). Estimates by the latter assemblage, however, are highly dependent on f(O2). Oxygen fugacity varies widely (from two or more log units below the QFM buffer to a few log units below the HM buffer) and can have a strong affect on mafic phase composition. Ilmenite-magnetite, quartz-ulvospinel-ilmenite-fayalite (QUILF), annite-sanidine-magnetite, biotite-almandine-muscovite-magnetite (BAMM), and titanite-magnetite-quartz (TMQ) are equilibria providing a basis for the calculation of f(O2). Granite barometry plays a critical part in constraining tectonic history. Metaluminous granites offer a range of barometers including ferrosilite-fayalite-quartz, garnet-plagioclase-hornblende-quartz and Al-in-hornblende. The latter barometer remains at the developmental stage, but has potential when the effects of temperature are considered. Likewise, peraluminous granites often cent ain mineral as semblages that enable pressure determinations, including gamet-biotite-muscovite-plagioclase and muscovite-biotite-alkali feldspar-quartz. Limiting pressures can be obtained from the presence of magmatic epidote and, for low-Ca pegmatites or aplites, the presence of subsolvus versus hypersolvus alkali feldspars. As with all barometers, the influence of temperature, f(O2), and choice of activity model are critical factors. Foremost is the fact that batholiths are not static features. Mineral compositions imperfectly record conditions acquired during ascent and over a range of temperature and pressure and great care must be taken in properly quantifying intensive parameters.
