Phase relationships of S‐type granite with H<sub>2</sub>O to 35 kbar: Muscovite granite from Harney Peak, South Dakota

Huang, Wei‐Cheng; Wyllie, Peter J.

doi:10.1029/jb086ib11p10515

Cited by 193 publications

(72 citation statements)

References 39 publications

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“…The mineral assemblage in the veins indicates formation from a hydrous melt with a granitic composition, for which the solidus temperature is typically about 650-700 8C at a pressure of about 0.3 GPa (e.g. Merrill et al, 1970;Cox et al, 1979;Huang and Wyllie, 1981). The aplites and pegmatites are primarily composed of feldspar, quartz, biotite, locally green amphibole and accessory apatite, titanite, zircon, opaques, carbonate and white mica.…”

Section: Discordant Pegmatite and Aplite Veinsmentioning

confidence: 99%

Magma-driven hydraulic fracturing and infiltration of fluids into the damaged host rock, an example from Dronning Maud Land, Antarctica

Engvik

Bertram

Kalthoff

et al. 2005

Journal of Structural Geology

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Excellent outcrops in Dronning Maud Land, Antarctica, provide unique insight into the mode and extent of fluid infiltration into metamorphic and plutonic rocks in the middle crust. The fluids are liberated from pegmatitic veins and give rise to alteration halos. In the alteration halos, the conspicuous change in colour is correlated with (1) hydration mineral reactions, and (2) high density of microcracks in quartz and feldspar exceeding that observed in the unaltered host rock by an order of magnitude. The field relations indicate that the veins originated as melt-driven hydraulic fractures, sealed by pegmatite and aplite crystallising from volatile-rich melts, with the alteration halo being the wake of the process zone formed at the tip of the propagating fractures. It is proposed that (1) the size of the alteration zone and the width of the vein are correlated, resulting in higher values of both these quantities for cracks propagating at higher velocities and consequently higher crack propagation toughnesses; (2) the damage zone is characterised by a transient state of high permeability which was short-lived due to rapid healing and sealing of microcracks; (3) the infiltration and retrogression of the high-grade rocks can be considered as a quasi-instantaneous process on geologic time scales with a duration of hours to weeks. q

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Section: Discordant Pegmatite and Aplite Veinsmentioning

confidence: 99%

Magma-driven hydraulic fracturing and infiltration of fluids into the damaged host rock, an example from Dronning Maud Land, Antarctica

Engvik

Bertram

Kalthoff

et al. 2005

Journal of Structural Geology

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“…Muscovite crystallises at lower temperatures and higher pressures relative to cordierite, which crystallises at higher temperatures and lower pressures (e.g. Huang and Wyllie, 1981;Monier and Robert, 1986;Clarke, 1995). The current mineral assemblage of the granites must therefore correlate to reactions involving muscovite and cordierite for G1 and G3 granites respectively (see also Charoy, 1986;Villaseca et al, 2008).…”

Section: Accepted M Manuscriptmentioning

confidence: 99%

“…There have been numerous experimental studies constraining melting reaction P-T conditions for pelites and greywackes (e.g. Huang and Wyllie, 1981;Patiño Douce and Johnston, 1991;Vielzeuf and Montel, 1994;Johnson et al, 2008). Partial melting of greywackes occurs through muscovite melting [6.1-6.2] followed by biotite melting at higher temperatures on a clockwise P-T-t path through incongruent melting reactions [6.3-6.4]: …”

Section: Partial Melting Conditionsmentioning

confidence: 99%

The petrogenesis of the Early Permian Variscan granites of the Cornubian Batholith: Lower plate post-collisional peraluminous magmatism in the Rhenohercynian Zone of SW England

Simons

Shail

Andersen

2016

Lithos

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The Early Permian Cornubian Batholith was generated during an extensional regime following Variscan convergence within the Rhenohercynian Zone of SW England. Its component granites can be classified, using mineralogical, textural and geochemical criteria, into five main types, all of which are peraluminous (A/CNK >1.1): G1 (two-mica), G2 (muscovite), G3 (biotite), G4 (tourmaline) and G5 (topaz). G1 granites formed through up to 20% muscovite and minor biotite dehydration melting of a metagreywacke source at moderate temperatures and pressures (731-806°C, >5 kbar). Younger G3 granites formed through higher temperature, lower pressure (768-847°C, <4 kbar) biotite-dominated melting of a similar source. Partial melting was strongly influenced by the progressive lower-mid crustal emplacement of mafic igneous rocks during post-Variscan extension and a minor (<5-10%) mantle-derived component in the granites is possible. Two distinct fractionation series, G1-G2 and G3-G4, are defined using whole rock geochemical and mineral chemical data.Variations in the major elements, Ba, Sr and Rb indicate that G1 and G3 granites underwent 15-30% fractionation of an assemblage dominated by plagioclase, alkali feldspar and biotite to form, more evolved G2 and G4 granites respectively. Decreasing whole rock abundances of Zr, Th and REE support fractionation of zircon, monazite, apatite and allanite. Subsolidus alteration in G2 and G4 granites is indicated by non-primary muscovite and tourmaline and modification of major and trace element trends for G3-G4 granites, particularly for P 2 O 5 and Rb. Topaz (G5) granites show low Zr, REE and extreme enrichment in Rb (up to 1530 ppm) and Nb (79 ppm) that cannot be related in a straightforward manner to continued differentiation of the G1-G2 or G3-G4 series. Instead, they are considered to represent partial melting, mediated by granulite facies fluids, of a biotite-rich restite following extraction of

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“…The extrapolation into the H 2 O undersaturated region is possible using the experimental results on Ab + Or + Qtz + H 2 O + CO 2 (to 10 kbar, Ebadi & Johannes 1991) and 15 kbar (Keppler 1989 but without excess H 2 O, fluid-absent (dehydration) melting occurs at temperatures higher than appropriate H 2 O-saturated solidi. In the P-T diagram of Figure 4, the dehydration melting of muscovite granite (Huang & Wyllie 1981), of Mus + Ab + Qtz (Peto & Thompson 1974;Peto 1976) and the dehydration melting interval for Bio + Plag + Qtz (LeBreton & Thompson 1988;Vielzeuf & Holloway 1988) are shown relative to the haplogranite melting results of Figure 3 and the alkali feldspar critical curve (AFC).…”

Section: Dehydration Melting Of Mica Relative To the Haplogranite Systemmentioning

confidence: 99%

Fertility of crustal rocks during anatexis

Thompson

1996

Earth and Environmental Science Transactions of the Royal Socie

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After many years of systematic experimental investigations, it is now possible to quantify the conditions for optimum fertility to melt production of most common crustal rock types as functions of temperature and a HlO , to about 30 kbar pressure. Quartzo-feldspathic melting produces steady increases in melt proportion with increasing temperature. The exact melt fraction depends on the mineral mode relative to quartz-feldspar eutectics and the temperatures of mica dehydration melting reactions. Mica melting consumes SiO 2 from residual quartz during the formation of refractory Al,SiO 5 , orthopyroxene, garnet or cordierite.A simple graphical interpretation of experimental results allows a deduction of the proportions of mica and feldspar leading to optimum fertility. In effect, the mica dehydration melting reactions, at specific pressure and a HiO , are superimposed on quartz-feldspar melting relations projected onto Ab-An-Or. Fertility to melt production varies with the mica to feldspar ratio and pressure. Pelites are more fertile than psammites at low pressures (e.g. 5 kbar), especially if they contain An 40 to An 50 plagioclase. At higher pressure (e.g. 10-20 kbar) and for rocks containing albitic plagioclase, psammites are more fertile than pelites. For a typical pelite (e.g. with An 25 at 20 kbar), the cotectic with muscovite lies at higher a H2O (*0-6) and X Ab (*0-42) than with biotite (a H , o :*0-35; X Ab *O-32), thus dehydration melting of muscovite requires 10% more plagioclase for fertility than does biotite.The first melts from dehydration melting of muscovite (with Plg + Qtz) are more sodic and form at lower temperatures than the first melts from Bio + Plg + Qtz. With increasing pressure, to at least 30 kbar, granite minimum and mica dehydration melts become more sodic. This indicates that fl H 2 o °f such melts is greater than 0-3.

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Phase relationships of S‐type granite with H₂O to 35 kbar: Muscovite granite from Harney Peak, South Dakota

Cited by 193 publications

References 39 publications

Magma-driven hydraulic fracturing and infiltration of fluids into the damaged host rock, an example from Dronning Maud Land, Antarctica

Magma-driven hydraulic fracturing and infiltration of fluids into the damaged host rock, an example from Dronning Maud Land, Antarctica

The petrogenesis of the Early Permian Variscan granites of the Cornubian Batholith: Lower plate post-collisional peraluminous magmatism in the Rhenohercynian Zone of SW England

Fertility of crustal rocks during anatexis

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Phase relationships of S‐type granite with H2O to 35 kbar: Muscovite granite from Harney Peak, South Dakota

Cited by 193 publications

References 39 publications

Magma-driven hydraulic fracturing and infiltration of fluids into the damaged host rock, an example from Dronning Maud Land, Antarctica

Magma-driven hydraulic fracturing and infiltration of fluids into the damaged host rock, an example from Dronning Maud Land, Antarctica

The petrogenesis of the Early Permian Variscan granites of the Cornubian Batholith: Lower plate post-collisional peraluminous magmatism in the Rhenohercynian Zone of SW England

Fertility of crustal rocks during anatexis

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Phase relationships of S‐type granite with H₂O to 35 kbar: Muscovite granite from Harney Peak, South Dakota