Partitioning biotite

Ferry J. M. and Spear F. S. (1978). Experimental calibration of the partitioning of Fe and Mg between biotite and garnet. Contrib. Mineral Petrol, 66 113-117. 

Goldman D. S. and Albee A. L. (1977). Correlation of Mg/Fe partitioning between garnet and biotite with 0/ 0 partitioning between quartz and magnetite. Amer. Jour. Set, 277 750-767. 

Dahl, P. S., Wehn, D. C. Feldman, S. G. (1993) The systematics of trace-element partitioning between coexisting muscovite and biotite in pelitic schists from the Black Hills, South Dakota. Geochim. Cosmochim. Acta, 57, (in press). 

Trioctahedral micas, such as phlogopite or biotite, are characterized by four distinct cation lattice sites tetrahedral (Z) sites occupied by silicon and aluminum octahedral (Y) sites, denoted Ml and M2, occupied by Al, Cr, Fe +, Ti, Fe +, Mg, and Mn and a large 12-fold coordinated interlayer X-site occupied by potassium, sodium, calcium, and other large cations. The low partition coefficients for lanthanides, uranium and thorium in phlogopite (<2X 10 ) indicate, however, that large highly charged cations cannot... 

Icenhower J. and London D. (1995) An experimental sffidy of element partitioning among biotite muscovite and coexisting... 

P-T conditions are ordinarily calculated based on the T-dependence of a cation partitioning equilibrium (e.g., Fe-Mg exchange between garnet and biotite), and the F-dependence of a net-transfer equilibrium (e.g., anorthite = grossular + aluminosilicate -h quartz). Most barometers have moderate slopes, so the calculated P depends moderately on T. The basic problem... 

Mother G, Robert J-L (1986) Titanium in muscovites from two mica granites substitutional mechanisms and partition with coexisting biotite. N Jahrb Mineral Abh 153 147-161 Morandi N, Nannetti MC, Pirani R, Resmi U (1984) La mica verde delle rocce di contatto nelTarea Predazzo-Monzoni. Rend Soc It Mineral Petrol 39 677-693 Muller F, Drits VA, Plangon A. Besson G (2000b) Dehydration of Fe, Mg-rich dioctahedral micas. (I) Structural transformation. Clay Mineral 35 491-504... 

Figure 10. A plot of age excess vs concentration in the grain boundary fluid for an open system. Solid lines are those derived from the mineral/fluid partition coefficients (6.6 x 10 to 2.6 x 10 ) for K-feldspar, dashed lines are those for another mineral with higher partition coefficients such as biotite. The shaded area indicates concentrations of (atmospheric) argon found in near surface ground waters and some deeper waters (Smith and Kennedy 1983 Torgersen et al. 1989 Kipfer et al. 2002, this volume). The vertical line indicates the current limit of excess argon concentration found in crustal fluids (Harrison et al. 1994).

Zhn C, Sveijensky DA (1992) F-Cl-OH partitioning between biotite and apatite. Geochim Cosmochim Acta 56 3435-3467... 

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