By C. Aydinalp
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Extra info for An Introduction to the Study of Mineralogy
In the A horizons, where most OM resides, the iron oxide fraction of the basaltic soil was associated with a very minor proportion of the OM. Overall, it was climate differences between the two granitic soils, rather than differences in the mineral composition of the parent materials, that resulted in the most obvious mineral effect on C. In the cooler granitic soil, more intense leaching has promoted the formation of more reactive clay and hence more mineral-bound C per unit clay. The impetus of this study was to evaluate the mineral density separation method in the context of understanding the role of parent material and mineralogy in organic matter storage and turnover.
S. (1979). A re-evaluation of the Mössbauer spectroscopy of calcic amphiboles, American Mineralogist, Vol. 64, pp. S. R. (1977). The identification of Fe2+ in the M(4) site of calcic amphiboles, American Mineralogist, Vol. 62, pp. B. (1963). M. & Powell, R. (1984). A garnet-hornblende geothermometer: calibration, testing and application to the Pelona schist, Southern California, Journal of Metamorphic Geology, Vol. 2, pp. C. (1983). The crystal chemistry of the amphiboles, Canadian Mineralogist, Vol.
C / % 100 b. f. g. 5 Fig. 5 a-d. The carbon and nitrogen chemistry of the A horizons plotted against the midpoint of each density fraction. The basalt soil is represented by closed symbols and the granite soils are represented by open symbols. The proportion of total C (Ct) in each density fraction, i, is Ct(ix) = %C(ix) Mt(ix) %Cbulk(avg) , where, x is the laboratory replicate for i. Reported Ct values are the mean of two laboratory replicates. Nt is calculated analogously. ) for Mt, C, N, 13C, and 15N is the absolute standard error of the mean of laboratory replicates (n=4 for mass fractions and n=2 for others).
An Introduction to the Study of Mineralogy by C. Aydinalp