The cation exchange equilibria Muscovite+ NH 4 Cl⇔ Tobelite+ KCl KAl 2 AlSi 3 O 10( OH) 2+ NH 4 Cl aq ⇔ NH 4 Al 2 AlSi 3 O 10( OH) 2+ KCl aq K- feldspar+ NH 4 Cl⇔ Buddingtonite+ KCl KAlSi 3 O 8+ NH 4 Cl aq ⇔ NH 4 AlSi 3 O 8+ KCl aq are determined by hydrothermal experiments at 400, 500, 600 °C at 400 MPa, and piston cylinder experiments at 500, 600 °C at 1500 MPa along the entire K–NH 4 compositional range. The composition of solid phases are determined by XRD, EMP and FTIR-methods, NH 4–K ratios in coexisting 2–3 molal chloride solutions by ion chromatography. Muscovite–tobelite and K-feldspar–buddingtonite form complete solid solutions series at all conditions. Consistent phase relations and mass balances indicate equilibrium between solid solutions and fluids. In both the (K,NH 4)-muscovite and (K,NH 4)-feldspar-fluid systems, NH 4 strongly fractionates into the fluid. In the range from 400 to 600 °C, 400 to 1500 MPa, fractionations are slightly temperature and pressure-dependent. The distribution coefficient K D solid- fluid = X NH 4 solid X K solid X K fluid X NH 4 fluid varies within the experimental range from 0.10 at X K bulk=0.81 to 0.46 at X K bulk=0.20 for muscovite-fluid, and from 0.05 at X K bulk=0.91 to 0.70 at X K bulk=0.15 for feldspar-fluid. NH 4 is preferentially incorporated into feldspar relative to mica with K D fsp-ms ranging between 1.36 and 2.0 at 400 MPa, and between 1.13 and 1.5 at 1500 MPa as X K bulk varies from 0.15 to 0.89. Results are evaluated thermodynamically assuming equal mixing of NH 4Cl and KCl in the fluid. Mixing energies of solids were estimated using multidimensional regression and a regular solution model. For the muscovite–tobelite equilibrium, values of Δ s°=−11.7 J K −1 mol −1, Δ v°=−2.1 J MPa −1 mol −1, and W=4.6 kJ mol −1, and for the K-feldspar–buddingtonite equilibrium, Δ s°=−8.8 J K −1 mol −1, Δ v°=−1.1 J MPa −1 mol −1, and W=5.4 kJ mol −1 were derived. Results are used to calculate partition coefficients D among phases at very low NH 4 bulk concentrations. Between 400 and 600 °C, D NH 4 fluid-ms ranges from 7 to 8 at 400 MPa and is 5 at 1500 MPa. D NH 4 fluid-ms is 6 to 7 at 400 MPa, and about 5 at 1500 MPa. D NH 4 fsp-ms is between 1 and 1.2 at all conditions. Partition coefficients are valid for NH 4 contents of up to several hundred ppm in mica and feldspar, well within the concentration range observed in many rocks. Combining the data with that of K–NH 4-partitioning between phlogopite and fluid results in D NH 4 phl-ms≈3.5 and D NH 4 phl-ms≈3 at 550 °C, 200 to 400 MPa. NH 4 concentrations in coexisting muscovite, biotite, and K-feldspar from a variety of rocks show near-equilibrium distributions. NH 4–K-partitioning between major K-bearing minerals and saline fluids allows for assessment of the dehydration history of metamorphic rocks. During prograde metamorphism, water is progressively produced by dehydration reactions and expelled along rock's P– T path. Nitrogen is subsequently removed due to preferred fractionation of NH 4 into fluids. The remaining NH 4 is continuously redistributed among muscovite and biotite, and at higher grades, K-feldspar with biotite as the main solid phase carrier of ammonium. The large fractionation effect of NH 4 among most phases highlights its potential as tracer of devolatilization processes and fluid–rock interactions.
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