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</html>";s:4:"text";s:9888:"It is also rich in Ba (827 ppm), %r (365 ppm) and REE (233 ppm). The numbers refer to the position of the respective boundaries at that percentage of SiO2. acknowledges NSF grants EAR9627814 and EAR-9814280. At least a portion of this variation is likely to be contributed by a mantle-derived component, because this increase in K2O away from a subduction zone is also seen in island arc lavas, where a continental contribution is lacking (Dickenson, 1975). E-mail: rfrost@uwyo.edu. B., Currie, K. L. & Chappell, B. W. (, Zhao, J.-X., Shiraishi, K., Ellis, D. J. Light-colored rock such as granite that has high silica content is called? 63 0 obj
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Sources of data are the same as for Figs 1b and 8. It has long been postulated that crystallization of anhydrous silicates drives a melt to higher Fe/(Fe + Mg) ratios, whereas the early crystallization of magnetite inhibits iron enrichment during differentiation (Osborn, 1959). 3), which is probably related to differences in source rock composition (Nabelek et al., 1992), as well as the degree of melting (Holtz & Johannes, 1991; Patiño Douce & Beard, 1996; Patiño Douce & Harris, 1998). The major difference lies in the fact that the S-types are invariably peraluminous (by definition), whereas the I-types are mostly metaluminous. Chappell & White, 1974; Collins et al., 1982; White & Chappell, 1983; King et al., 1997), it is important to see how they fit into our classification (Fig. %PDF-1.7
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This pressure effect is largely the result of decreases with pressure in the extent of polymerization for all olivine + orthopyroxene-saturated … (a) FeOtot/(FeOtot + MgO) vs wt % SiO2 and (b) Na2O + K2O – CaO vs wt % SiO2. (a) K2O vs Na2O and (b) Na2O + K2O – CaO vs K2O diagrams comparing the compositional trends of Archean tonalitic gneisses and Mesozoic granites of the Cordilleran batholiths for rocks with 69–71 wt % SiO2. For example, the Fe-number is most strongly affected by the differentiation paths followed by the magmas. & Stewart, J. 3) indicates that MALI can also be affected by the composition of crustally derived melt. (a) FeO/(FeO + MgO) vs wt % SiO2. Sources of data: Viljoen & Viljoen (1969), Barton (1975), Hurst et al. 11), do not? Thus, their geochemical features must reflect this variety of inputs, each of which may or may not be related to tectonic setting. 9b). The effect of alkalis on the silica content of melts equilibrated with magnesian olivine and orthopyroxene is reduced at higher pressure, such that silica enrichments in alkali-rich melts will be small if the equilibration pressure is greater than ∼1.5 GPa. & Erskine, B. This term adequately indicates that the granitoids in the Cordilleran batholiths are calcic or calc-alkalic and that they lack marked iron enrichment. (b) Na2O + K2O – CaO vs wt % SiO2. The paper benefited greatly from reviews by J. L. Anderson, B. Barbarin, J. Hogan, and C. Miller. Na2O + K2O – CaO vs H2O diagram showing the effect of pressure and the abundance of water on the composition of melt produced during experimental melting of a biotite gneiss and pelitic biotite–muscovite schist. The aluminum saturation index is predominantly determined by the composition of the source region and the nature of the melting process. This means that the ASI of a granitic rock is mostly a function of the sources of a magma, with peraluminous magmas formed from hydrous melting of mafic rocks (Ellis & Thompson, 1986) or by melting of pelitic or semi-pelitic rocks (Holtz & Johannes, 1991). 10). This trend results because increasing water pressure produces increased melting of plagioclase at the expense of micas (Patiño Douce & Harris, 1998). There are A-type granitoids that are peraluminous (Anderson & Thomas, 1985). (, Barker, F., Millard, H. T. & Lipman, P. W. (, Collins, B. J., Beams, S. D., White, A. J. R. & Chappell, B. W. (, Cullers, R. L., Koch, R. J. This arises from the fact that the geochemical compositions of granitic magmas reflect the compositions of their source rocks rather than their tectonic setting (e.g. However, it is possible, perhaps likely, that leucogranitic crustal melts make major contributions to the silica-rich magmas in other settings (Figs 4–6), leading to a significant mixing component in the trends used to define our compositional groupings. The wide range in modified alkali–lime index from peraluminous leucogranites (Fig. endstream
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Data from Landenberger & Collins (1996) and AGSO (Australian Geological Survey Organization) database (http://www.agso.gov.au/geochemistry/rockchem/). Magnesian granitoids in contrast are probably related to island arc magmas, which follow relatively oxidizing differentiation trends. Sources: Gardiner & Reynolds (1931, 1937), Anderson (1937), Nicholls (1951), Hall (1966, 1972), Haslam (1968), Leake (1974), Sweetman (1987) and Weiss & Troll (1989). Such freedom will permit a more comprehensive view of granite petrogenesis and the remarkable range of processes and environments in which granitic rocks form. Data from Holtz & Johannes (1991) (3 and 5 kbar) and Patiño Douce & Harris (1998) (6 and 10 kbar). These rocks are predominantly alkali–calcic and magnesian, although at silica abundances >70% some of these granitoids are calc-alkalic. Furthermore, many granitic systems are demonstrably open to a variety of chemical inputs. h�b```"7V�&!b`��0p��P�P�
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