Geochemistry trace elements

Zindler A, Hart SR (1986) Chemical geodynamics. Aim Rev Earth Planet Sci 14 493-571 Zindler A, Standigel H, Batiza R (1984) Isotope and trace element geochemistry of young Pacific seamounts implications for the scale of upper mantle heterogeneity. Earth Planet Sci Lett 70 175-190... 

Geology appears to be the main determinant of trace-element contents and mineralogical form - as defined using selective extractions. There is no indication that landuse per se has had a significant general effect on soil trace element geochemistry. 

Pearce J.A. 1996, A user s guide to basalt discrimination diagrams. In Wyman, D.A. (ed) Trace Element Geochemistry of Volcanic Rocks Applications for Massive Sulphide Exploration. Geological Association of Canada, Short Course Notes, v.12, p.79-113. 

Collier, R. and Edmond, J. (1984). The trace element geochemistry of marine biogenic particulate matter, Prog. Oceanogr., 13, 113-199. 

Mauk, J. L. and Hancock, R. G. Y. (1998). Trace element geochemistry of native copper from the White Pine mine, Michigan (USA) implications for sourcing artefacts. Archaeometry 40 97-107. 

This standard state is adopted for solutions in which, as already stated, the condition of solute is distinguished from that of solvent. Moreover, it is (implicitly) adopted in trace element geochemistry (see chapter 10). 

Although this equation reduces to an identity whenever solute-solvent interactions are embodied in the definition of the Henry s law standard state (cf section 10.2), it must be noted that K[ is the molar ratio of trace element i in the two phases and not the weight concentration ratio usually adopted in trace element geochemistry. As we will see later in this section, this double conversion (from activity ratio to molar ratio, and from molar ratio to weight concentration ratio) complicates the interpretation of natural evidence in some cases. To avoid ambiguity, we define here as conventional partition coefficients (with the same symbol K ) all mass concentration ratios, to distinguish them from molar ratios and equilibrium constants. 

We have already noted that the double conversion from activity ratio to weight concentration ratio implicit in trace element geochemistry may involve complexities that must be carefully evaluated in the interpretation of natural evidence. Let us consider, for instance, the distribution of Ni between clinopyroxene and silicate liquid. Eigure lO.lOA shows the effect of temperature on the conven-... 

The fractionation factor a represents the relative distribution of heavy and light isotopes in the two phases at equihbrium (somewhat similar to the normalized distribution coefficient adopted in trace element geochemistry cf section 10.8) ... 

Ewart A. and Taylor S. R. (1969). Trace element geochemistry of rhyolitic volcanic rocks. Central North Island, New Zealand. Phenocryst data. Contrib. Mineral Petrol, 22 127-138. 

Harrison W. J. (1977). An experimental study of the partitioning of samarium between garnet and liquid at high pressures. In Papers Presented to the International Conference on Experimental Trace Elements Geochemistry, Sedona, Arizona. 

Lesher, M., Goodwin, A.M., Campbell, I.H., Gorton, M.P. 1986. Trace-element geochemistry of ore-associated and barren, felsic metavolcanic rocks in the Superior Province, Canada. Canadian Journal of Earth Sciences, 23, 222-237. 

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