Petrology and Li-Be-B geochemistry of muscovite-biotite granite and associated pegmatite near Yellowknife, Canada

Kretz, Ralph; Loop, John; Hartree, R.

doi:10.1007/bf00375339

Cited by 26 publications

(11 citation statements)

References 33 publications

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“…The partition ratio for Cs of series 6 (Table 10) is similar to that found experimentally (Icenhower and London 1995), but lower than that found in Viseu area (Neves 1997). However Ba favours muscovite rather than biotite (Tables 4-9) as found by Albuquerque (1975), Lee et al (1981), Kretz et al (1989), Jolliff et al (1992) and Bea et al (1994), but experimental data shows the preference of Ba for biotite (Icenhower and London 1995).…”

Section: Distribution Coefficientssupporting

confidence: 80%

“…Rare data were found in the literature on Nb and Zn of coexisting biotite and muscovite from granitic rocks, but they prefer biotite rather than coexisting muscovite (Jolliff et al 1992;Neves 1977) as in this study. Li is more concentrated in biotite than in coexisting muscovite (Tables 4 to 9) as found by Carron and Lagache (1972), Albuquerque (1975), Kretz et al (1989), Jolliff et al (1992), Bea et al (1994) and Neves (1997).…”

Section: Distribution Coefficientssupporting

confidence: 66%

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Geochemistry of Coexisting Biotite and Muscovite of Portuguese Peraluminous Granitic Differentiation Series

et al. 2002

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In nine Portugese peraluminous Hercynian granitic series of differentiation, Cr, V, Sc and Ba decrease, whereas Nb, Zn, Sn, Li, Rb and Cs increase in the sequence of micas crystallization. Commonly equilibrium was not attained for trace elements between coexisting primary biotite and muscovite. Correlations of Cr, V, Nb, Li, Rb and Cs were found for biotite-muscovite pairs. The same correlation has a different slope in distinct series due to distinct degree of fractional crystallization, but also to solid-liquid reequilibration during late-magmatic evolution, as suggested by regression lines, which do not generally pass through the origin. Most trace elements partition in favour of biotite, while Sn, Sc, Sr and Ba prefer muscovite. These micas probably crystallized simultaneously as suggested by intergrowths. The partition ratio for Cs is one series is similar to that found experimentally.

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Section: Distribution Coefficientssupporting

confidence: 80%

Section: Distribution Coefficientssupporting

confidence: 66%

Geochemistry of Coexisting Biotite and Muscovite of Portuguese Peraluminous Granitic Differentiation Series

et al. 2002

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“…The chemical composition of group 4 gneiss (Table 1) is similar to that of muscovite-biotite granite, found elsewhere in the Canadian Shield (Kretz et al, 1989), except that Ca, Fe and Mg are higher by a factor of 2-3. Thus garnet within the gneiss was possibly produced by the reaction, Experimental studies by Dahl (1968) and Hsu (1968) confirm that reactions to produce Fe-Mn garnet from biotite or chlorite are continuous reactions, and reactions analogous to (a) must also be continuous (Kretz, 1993).…”

Section: Geologysupporting

confidence: 64%

Section: Geologysupporting

confidence: 64%

Shape, size, spatial distribution and composition of garnet crystals in highly deformed gneiss of the Otter Lake area, Québec, and a model for garnet crystallization

Kretz¹

2006

Journal Metamorphic Geology

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Garnet-biotite-(sillimanite) gneiss ($700°C, 7 kbar) of the Otter Lake area in the Western Grenville Province (Canadian Shield) occurs as granitic gneiss (group 4) that forms a large part of the Otter Complex, and as widely distributed, more heterogenous metasedimentary gneiss (group 2). In one sample of group 4 gneiss (Qtz 25 Pl 34 Kfs 28 Bt 10 Grt 2.5 Sil 1 ) the true diameter (determined by serial grinding) of subhedral garnet crystals ranges from 0.2 to 3.0 mm, with a mode at 1.0 mm. Nearestneighbour measurements in this sample, and in surfaces of nine additional samples (all <5% garnet) confirm that garnet crystals are distributed mainly at random; slight clustering was detected in two samples. In one sample of group 4 gneiss, microprobe analyses on sections through crystal centres (obtained by serial slicing), reveal that small crystals and margins to large crystals contain more Fe and Mn and less Mg than the broad central regions of large crystals. Based on these and previous results, together with theoretical considerations, a crystallization model is proposed, in which, (i) garnet was produced by the continuous reaction, Ms + Bt + Qtz fi Grt + Kfs + H 2 O, (ii) nucleation occurred by the random selection of randomly distributed Ms-Bt-Qtz triple junctions, (iii) the rate of linear growth remained constant, and (iv) as temperature increased, the rate of nucleation first increased slowly, then remained nearly constant, and finally declined. Within-population compositional homogenization was followed, on cooling, by local Fe-Mg-Mn exchange with biotite.

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“…SPGs occur throughout the province from the vicinity of Yellowknife near the Great Slave Lake (e.g. Prosperous Granite; Kretz, 1989) to the Contwoyto Lake area in the north-central part of the craton (Contwoyto Intrusive Suite; King et al, 1992;Davis et al, 1994). Metasedimentary protoliths of the YKS, probably quartzo-feldspathic metagreywackes of the Burwash Basin, have been proposed as the source rock of the SPGs (Drury, 1979;Meintzer, 1987;Davis et al, 1994).…”

Section: Slave Craton Canadamentioning

confidence: 99%

Strongly Peraluminous Granites across the Archean–Proterozoic Transition

Bucholz

Spencer

2019

Journal of Petrology

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Strongly peraluminous granites (SPGs) form through the partial melting of metasedimentary rocks and therefore represent archives of the influence of assimilation of sedimentary rocks on the petrology and chemistry of igneous rocks. With the aim of understanding how variations in sedimentary rock characteristics across the Archean–Proterozoic transition might have influenced the igneous rock record, we compiled and compared whole-rock chemistry, mineral chemistry, and isotope data from Archean and Paleo- to Mesoproterozoic SPGs. This time period was chosen as the Archean–Proterozoic transition broadly coincides with the stabilization of continents, the rise of subaerial weathering, and the Great Oxidation Event (GOE), all of which left an imprint on the sedimentary rock record. Our compilation of SPGs is founded on a detailed literature review of the regional geology, geochronology, and inferred origins of the SPGs, which suggest derivation from metasedimentary source material. Although Archean and Proterozoic SPGs are similar in terms of mineralogy or major-element composition owing to their compositions as near-minimum melts in the peraluminous haplogranite system, we discuss several features of their mineral and whole-rock chemistry. First, we review a previous analysis of Archean and Proterozoic SPGs biotite and whole-rock compositions indicating that Archean SPGs, on average, are more reduced than Proterozoic SPGs. This observation suggests that Proterozoic SPGs were derived from metasedimentary sources that on average had more oxidized bulk redox states relative to their Archean counterparts, which could reflect an increase in atmospheric O2 levels and more oxidized sedimentary source rocks after the GOE. Second, based on an analysis of Al2O3/TiO2 whole-rock ratios and zircon saturation temperatures, we conclude that Archean and Proterozoic SPGs formed through partial melting of metasedimentary rocks over a similar range of melting temperatures, with both ‘high-’ and ‘low-’temperature SPGs being observed across all ages. This observation suggests that the thermo-tectonic processes resulting in the heating and melting of metasedimentary rocks (e.g. crustal thickening or underplating of mafic magmas) occurred during generation of both the Archean and Proterozoic SPGs. Third, bulk-rock CaO/Na2O, Rb/Sr, and Rb/Ba ratios indicate that Archean and Proterozoic SPGs were derived from partial melting of both clay-rich (i.e. pelites) and clay-poor (i.e. greywackes) source regions that are locality specific, but not defined by age. This observation, although based on a relatively limited dataset, indicates that the source regions of Archean and Proterozoic SPGs were similar in terms of sediment maturity (i.e. clay component). Last, existing oxygen isotope data for quartz, zircon, and whole-rocks from Proterozoic SPGs show higher values than those of Archean SPGs, suggesting that bulk sedimentary 18O/16O ratios increased across the Archean–Proterozoic boundary. The existing geochemical datasets for Archean and Proterozoic SPGs, however, are limited in size and further work on these rocks is required. Future work must include detailed field studies, petrology, geochronology, and constraints on sedimentary source ages to fully interpret the chemistry of this uniquely useful suite of granites.

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Petrology and Li-Be-B geochemistry of muscovite-biotite granite and associated pegmatite near Yellowknife, Canada

Cited by 26 publications

References 33 publications

Geochemistry of Coexisting Biotite and Muscovite of Portuguese Peraluminous Granitic Differentiation Series

Geochemistry of Coexisting Biotite and Muscovite of Portuguese Peraluminous Granitic Differentiation Series

Shape, size, spatial distribution and composition of garnet crystals in highly deformed gneiss of the Otter Lake area, Québec, and a model for garnet crystallization

Strongly Peraluminous Granites across the Archean–Proterozoic Transition

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