Abstract. We present new models for the activity of iron (γFe) in solid face-centered cubic (fcc) and liquid FePt
alloy at high temperature and pressure to facilitate their use as sliding buffer
redox sensors under extreme conditions. Numerous experimental studies of
γFe in FePt alloy at 100 kPa have produced a wide spread of
values. By favoring high-temperature studies that are more likely to have
produced equilibrium measurement and excluding experiments for compositions
and temperatures that probably encountered ordered or unmixed low-temperature phases, we regress an asymmetric Margules activity–composition
model with parameters WFePtfcc=-121.5±2.1 kJ mol−1 and WPtFefcc=-93.3±4.3 kJ mol−1.
These values are close to the widely used model of Kessel et al. (2001), but
for Pt-rich compositions they predict larger Fe activities and
correspondingly more reduced oxygen fugacities. Activity–composition
relations in liquid FePt are calibrated from direct measurements of
activities and, most sensitively, from the trace of the Fe–Pt liquidus.
Together, these yield asymmetric Margules parameters of
WFePtliq=-124.5 kJ mol−1 and
WPtFeliq=-94.0 kJ mol−1. The effects of pressure
on both fcc and liquid FePt alloy are considered from excess-volume relations.
Both solid and liquid alloy display significant positive excess volumes of mixing.
Extraction of the excess volume of mixing for fcc FePt alloy requires filtering
data for ordered low-temperature phases and corrections for the effects of
magnetostriction on Fe-rich compositions which exhibit “Invar” behavior.
Applied at high temperatures and pressures, both solid and liquid FePt
alloys have strongly negative deviations from ideality at low pressure,
which become closer to ideal at high pressure. These models provide a
provisional basis for the calculation of aFe in high-temperature, high-pressure experiments that, when combined with estimates of aFeO, allow
characterization of fO2 under conditions relevant to magma oceans, core
formation, and differentiation processes in the lower mantle of Earth or
on other terrestrial planets. Improvements in these models require new
constraints on the equation of state of FePt fcc alloy and documentation of the
high-pressure melting relations in the system Fe–Pt.