Hostname: page-component-78c5997874-mlc7c Total loading time: 0 Render date: 2024-11-10T13:03:18.607Z Has data issue: false hasContentIssue false
  • English
  • Français

Trace element partitioning between wollastonite and silicate-carbonate melt

Published online by Cambridge University Press:  05 July 2018

K. M. Law ,
J. D. Blundy ,
B. J. Wood  and
K. V. Ragnarsdottir
K. M. Law
Affiliation:
CETSEI, Department of Earth Sciences, University of Bristol, Wills Memorial Building, Queens Road, Bristol BS8 1RJ, UK
J. D. Blundy*
Affiliation:
CETSEI, Department of Earth Sciences, University of Bristol, Wills Memorial Building, Queens Road, Bristol BS8 1RJ, UK
B. J. Wood
Affiliation:
CETSEI, Department of Earth Sciences, University of Bristol, Wills Memorial Building, Queens Road, Bristol BS8 1RJ, UK
K. V. Ragnarsdottir
Affiliation:
CETSEI, Department of Earth Sciences, University of Bristol, Wills Memorial Building, Queens Road, Bristol BS8 1RJ, UK
*
*E-mail: jon.blundy@bris.ac.uk
Get access Rights & Permissions [Opens in a new window]

Abstract

We have performed an experimental study of the influence of varying size and charge on cation partitioning between wollastonite and silicate-carbonate melt in the system CaCO3-SiO2. The experimental conditions (3 GPa, 1420°C) lie close to the wollastonite II tc/I tc phase boundary. Results for 1+, 2+, 3+ and 4+ partitioning show parabolic dependence of partition coefficients on ionic radius, which can be fitted to the elastic strain model of Blundy and Wood (1994), wherein partitioning is described using three parameters: site radius (r0), site elasticity (apparent Young's Modulus) and the ‘strain-free’ partition coefficient (D0) for an element with radius r0. The apparent Young's Modulus of the Ca site in wollastonite, obtained from modelling the 2+ partitioning data, is 99±3 GPa, similar to the bulk-crystal value for the polymorph wollastonite I tc. r0 decreases with increasing charge on the substituent cation, while D0 also shows an approximately parabolic dependence on charge, with a maximum for 2+ cations. Partition coefficients for divalent cations Zn, Co, Fe, Cd, Mn and Pb are lower than would be predicted from their ionic radii alone, indicating a preference for the melt. This may be a consequence either of cation-carbonate complexation in the melt, or of the more distorted nature of cation co-ordination environments in melts.

Keywords

trace element partitioningwollastonitemetasomatismcarbonate melt
Type
Research Article
Information
Mineralogical Magazine , Volume 64 , Issue 4 , August 2000 , pp. 651 - 661
Copyright
Copyright © The Mineralogical Society of Great Britain and Ireland 2000

Access options

Get access to the full version of this content by using one of the access options below. (Log in options will check for institutional or personal access. Content may require purchase if you do not have access.)

References

Beattie, P. (1994) Systematics and energetics of trace-element partitioning between olivine and silicate melts: Implications for the nature of mineral/melt partitioning. Chem. Geol., 117, 57–71.CrossRefGoogle Scholar
Blundy, J.D. and Dalton, J.A. (2000) An experimental comparison of clinopyroxene-melt partitioning in silicate and carbonate systems and implications for mantle metasomatism. Contrib. Mineral. Petrol.(in press).CrossRefGoogle Scholar
Blundy, J.D. and Wood, B.J. (1994) Prediction of crystal-melt partition coefficients from elastic moduli. Nature, 372, 452–4.CrossRefGoogle Scholar
Blundy, J.D., Robinson, J.A.C. and Wood, B.J. (1998) Heavy REE are compatible in clinopyroxene on the spinel lherzolite solidus. Earth Planet. Sci. Lett., 160, 493–504.CrossRefGoogle Scholar
Chatterjee, N.D., Johannes, W. and Leistner, H. (1984) The system CaO-Al2O3-SiO2-H2O: new phase equilibria data, some calculated phase relations, and their petrological applications. Contrib. Mineral. Petrol., 88, 1–13.CrossRefGoogle Scholar
Dawson, J.B. (1998) Peralkaline nephelinite-natrocarbonatite relationships at Oldoinyo Lengai, Tanzania. J. Petrol., 39, 2077–94.CrossRefGoogle Scholar
Dawson, J.B., Pyle, D.M. and Pinkerton, H. (1996) Evolution of natrocarbonatite from a wollastonite nephelinite parent: evidence from the June, 1993 eruption of Oldoinyo Lengai, Tanzania. J. Geol., 104, 41–54.CrossRefGoogle Scholar
Essene, E. (1974) High-pressure transformations in CaSiO3 . Contrib. Mineral. Petrol., 45, 247–50.CrossRefGoogle Scholar
Fletcher, D.A., McMeeking, R.F. and Parkin, D. (1996) The United Kingdom Chemical Database Service. J. Chem. Information Comp. Sci., 36, 746–9.CrossRefGoogle Scholar
Frost, D.J. and Wood, B.J. (1997) Experimental measurements of fugacity of CO2 and graphite/diamond stability from 35-77 GPa at 925 to 1650°C. Geochim. Cosmochim. Acta, 61, 1565–74.CrossRefGoogle Scholar
Gold, D.P. (1966) The minerals of the Oka carbonatite and alkaline complex, Oka, Quebec. Pp. 109–25 in Mineralogical Society of India, I.M.A. Volume (Naidu, P.R.J., editor). Mysore University, India.Google Scholar
Hazen, R.M and Finger, L.W. (1979) Bulk modulus-volume relationship for cation-anion polyhedra. J. Geophys. Res., 84, 6723–8.CrossRefGoogle Scholar
Huang, W.L. and Wyllie, P.J. (1975) Melting and subsolidus phase relations for CaSiO3 to 35 kbars pressure. Amer. Mineral., 60, 213–7.Google Scholar
Huang, W.L., Wyllie, P.J. and Nehru, C.E. (1980) Subsolidus and liquid phase relations in the system CaO-SiO2-CO2 to 30 kbars with geological applications. Amer. Mineral., 65, 285–301.Google Scholar
Irving, A.J. and Frey, F.A. (1984) Trace element abundances in megacrysts and their host basalts: constraints on partition coefficients and megacryst genesis. Geochim. Cosmochim. Acta, 48, 1201–21.CrossRefGoogle Scholar
Law, K.M. (1999) Controls on trace element partitioning in carbonate systems. PhD thesis, Univ. Bristol, UK.Google Scholar
Press, W.H., Teukolsky, S.A., Vetterling, W.T. and Flannery, B.P. (1992) Numerical Recipes in C, (2nd edition). Cambridge University Press.Google Scholar
Purton, J.A., Allan, N.L., Blundy, J.D. and Wasserman, E.A. (1996) Isovalent trace element partitioning between minerals and melts: A computer simulation study. Geochim. Cosmochim. Acta, 60, 4977–87.CrossRefGoogle Scholar
Purton, J.A., Blundy, J.D. and Allan, N.L. (2000) Computer simulation of high temperature forsteritemelt partitioning. Amer. Mineral. (submitted).Google Scholar
Shannon, R.D. (1976) Revised effective ionic radii and systematic studies of interatomic distances in halides and chalcogenides. Acta Crystallogr., A32, 751–6.CrossRefGoogle Scholar
Swamy, V. and Dubrovinsky, L.S. (1997) Thermodynamic data for the phases in the CaSiO3 system. Geochim. Cosmochim. Acta, 61, 1181–91.CrossRefGoogle Scholar
Van Westrenen, W., Blundy, J.D. and Wood, B.J. (1999) Crystal-chemical controls on trace element partitioning between garnet and anhydrous silicate melt. Amer. Mineral., 84, 838–47.CrossRefGoogle Scholar
Van Westrenen, W., Allan, N.L., Blundy, J.D., Purton, J.A. and Wood, B.J. (2000) Atomistic simulation of trace element incorporation into garnets-comparison with experimental garnet-melt partitioning data. Geochim. Cosmochim. Acta, 64, 1629–39.CrossRefGoogle Scholar
Withers, A.C. (1997) Water in the mantle. PhD thesis, Univ. Bristol, UK.Google Scholar
Wood, B.J. and Blundy, J.D (1997) A predictive model of rare element partitioning between clinopyroxene and anhydrous silicate melt. Contrib. Mineral. Petrol., 126, 166–81.CrossRefGoogle Scholar
Wood, B.J, Blundy, J.D. and Robinson, J.A.C. (1999) The role of clinopyroxene in generating U-series disequilibrium during mantle melting. Geochim. Cosmochim. Acta, 63, 1613–20.CrossRefGoogle Scholar