TY - JOUR
T1 - Occurrence and origin of andalusite in peraluminous felsic igneous rocks
AU - Clarke, D. Barrie
AU - Dorais, Michael
AU - Barbarin, Bernard
AU - Barker, Dan
AU - Cesare, Bernardo
AU - Clarke, Geoffrey
AU - El Baghdadi, Mohamed
AU - Erdmann, Saskia
AU - Förster, Hans Jürgen
AU - Gaeta, Mario
AU - Gottesmann, Bärbel
AU - Jamieson, Rebecca A.
AU - Kontak, Daniel J.
AU - Koller, Friedrich
AU - Gomes, Carlos Leal
AU - London, David
AU - Morgan VI, George B.
AU - Neves, Luis J.P.F.
AU - Pattison, David R.M.
AU - Pereira, Alcides J.S.C.
AU - Pichavant, Michel
AU - Rapela, Carlos W.
AU - Renno, Axel D.
AU - Richards, Simon
AU - Roberts, Malcolm
AU - Rottura, Alessandro
AU - Saavedra, Julio
AU - Sial, Alcides Nobrega
AU - Toselli, Alejandro J.
AU - Ugidos, Jose M.
AU - Uher, Pavel
AU - Villaseca, Carlos
AU - Visonà, Dario
AU - Whitney, Donna L.
AU - Williamson, Ben
AU - Woodard, Henry H.
N1 - Funding Information:
This paper has been many years in development, and during that time several people, including Gordon Brown, Andrew Henry, Robert MacKay, Llewellyn Pearce, and Monica Rampoldi, have provided invaluable technical and logistical support, for which we express our gratitude. More recently, Calvin Miller and Alberto Patiño Douce provided valuable detailed reviews that led to considerable improvements in the manuscript. In addition, Barrie Clarke acknowledges the essential support of a research grant from the Natural Sciences and Engineering Research Council of Canada.
PY - 2005/3
Y1 - 2005/3
N2 - Andalusite occurs as an accessory mineral in many types of peraluminous felsic igneous rocks, including rhyolites, aplites, granites, pegmatites, and anatectic migmatites. Some published stability curves for And = Sil and the water-saturated granite solidus permit a small stability field for andalusite in equilibrium with felsic melts. We examine 108 samples of andalusite-bearing felsic rocks from more than 40 localities world-wide. Our purpose is to determine the origin of andalusite, including the T-P-X controls on andalusite formation, using eight textural and chemical criteria: size-compatibility with grain sizes of igneous minerals in the same rock; shape-ranging from euhedral to anhedral, with no simple correlation with origin; state of aggregation-single grains or clusters of grains; association with muscovite-with or without rims of monocrystalline or polycrystalline muscovite; inclusions--rare mineral inclusions and melt inclusions; chemical composition-andalusite with little significant chemical variation, except in iron content (0·08-1·71 wt % FeO); compositional zoning--concentric, sector, patchy, oscillatory zoning cryptically reflect growth conditions; compositions of coexisting phases-biotites with high siderophyllite-eastonite contents (Al iv ≈ 2·68 ± 0·07 atoms per formula unit), muscovites with 0·57-4·01 wt % FeO and 0·02-2·85 wt % TiO2, and apatites with 3· 53 ± 0·18 wt % F. Coexisting muscovite-biotite pairs have a wide range of F contents, and FBt = 1·612F Ms + 0·015. Most coexisting minerals have compositions consistent with equilibration at magmatic conditions. The three principal genetic types of andalusite in felsic igneous rocks are: Type 1 Metamorphic-(a) prograde metamorphic (in thermally metamorphosed peraluminous granites), (b) retrograde metamorphic (inversion from sillimanite of unspecified origin), (c) xenocrystic (derivation from local country rocks), and (d) restitic (derivation from source regions); Type 2 Magmatic-(a) peritectic (water-undersaturated, T↑) associated with leucosomes in migmatites, (b) peritectic (water-undersaturated, T↓), as reaction rims on garnet or cordierite, (c) cotectic (water-undersaturated, T↓) direct crystallization from a silicate melt, and (d) pegmatitic (water-saturated, T↓), associated with aplite-pegmatite contacts or pegmatitic portion alone; Type 3 Metasomatic-(water-saturated, magma-absent), spatially related to structural discontinuities in host, replacement of feldspar and/or biotite, intergrowths with quartz. The great majority of our andalusite samples show one or more textural or chemical criteria suggesting a magmatic origin. Of the many possible controls on the formation of andalusite (excess Al2O 3, water concentration and fluid evolution, high Be-B-Li-P, high F, high Fe-Mn-Ti, and kinetic considerations), the two most important factors appear to be excess Al2O3 and the effect of releasing water (either to strip alkalis from the melt or to reduce alumina solubility in the melt). Of particular importance is the evidence for magmatic andalusite in granites showing no significant depression of the solidus, suggesting that the And = Sil equilibrium must cross the granite solidus rather than lie below it. Magmatic andalusite, however formed, is susceptible to supra- or sub-solidus reaction to produce muscovite. In many cases, textural evidence of this reaction remains, but in other cases muscovite may completely replace andalusite leaving little or no evidence of its former existence.
AB - Andalusite occurs as an accessory mineral in many types of peraluminous felsic igneous rocks, including rhyolites, aplites, granites, pegmatites, and anatectic migmatites. Some published stability curves for And = Sil and the water-saturated granite solidus permit a small stability field for andalusite in equilibrium with felsic melts. We examine 108 samples of andalusite-bearing felsic rocks from more than 40 localities world-wide. Our purpose is to determine the origin of andalusite, including the T-P-X controls on andalusite formation, using eight textural and chemical criteria: size-compatibility with grain sizes of igneous minerals in the same rock; shape-ranging from euhedral to anhedral, with no simple correlation with origin; state of aggregation-single grains or clusters of grains; association with muscovite-with or without rims of monocrystalline or polycrystalline muscovite; inclusions--rare mineral inclusions and melt inclusions; chemical composition-andalusite with little significant chemical variation, except in iron content (0·08-1·71 wt % FeO); compositional zoning--concentric, sector, patchy, oscillatory zoning cryptically reflect growth conditions; compositions of coexisting phases-biotites with high siderophyllite-eastonite contents (Al iv ≈ 2·68 ± 0·07 atoms per formula unit), muscovites with 0·57-4·01 wt % FeO and 0·02-2·85 wt % TiO2, and apatites with 3· 53 ± 0·18 wt % F. Coexisting muscovite-biotite pairs have a wide range of F contents, and FBt = 1·612F Ms + 0·015. Most coexisting minerals have compositions consistent with equilibration at magmatic conditions. The three principal genetic types of andalusite in felsic igneous rocks are: Type 1 Metamorphic-(a) prograde metamorphic (in thermally metamorphosed peraluminous granites), (b) retrograde metamorphic (inversion from sillimanite of unspecified origin), (c) xenocrystic (derivation from local country rocks), and (d) restitic (derivation from source regions); Type 2 Magmatic-(a) peritectic (water-undersaturated, T↑) associated with leucosomes in migmatites, (b) peritectic (water-undersaturated, T↓), as reaction rims on garnet or cordierite, (c) cotectic (water-undersaturated, T↓) direct crystallization from a silicate melt, and (d) pegmatitic (water-saturated, T↓), associated with aplite-pegmatite contacts or pegmatitic portion alone; Type 3 Metasomatic-(water-saturated, magma-absent), spatially related to structural discontinuities in host, replacement of feldspar and/or biotite, intergrowths with quartz. The great majority of our andalusite samples show one or more textural or chemical criteria suggesting a magmatic origin. Of the many possible controls on the formation of andalusite (excess Al2O 3, water concentration and fluid evolution, high Be-B-Li-P, high F, high Fe-Mn-Ti, and kinetic considerations), the two most important factors appear to be excess Al2O3 and the effect of releasing water (either to strip alkalis from the melt or to reduce alumina solubility in the melt). Of particular importance is the evidence for magmatic andalusite in granites showing no significant depression of the solidus, suggesting that the And = Sil equilibrium must cross the granite solidus rather than lie below it. Magmatic andalusite, however formed, is susceptible to supra- or sub-solidus reaction to produce muscovite. In many cases, textural evidence of this reaction remains, but in other cases muscovite may completely replace andalusite leaving little or no evidence of its former existence.
KW - Andalusite
KW - Granite
KW - Magmatic
KW - Origin
KW - Xenocrystic
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U2 - 10.1093/petrology/egh083
DO - 10.1093/petrology/egh083
M3 - Review article
AN - SCOPUS:20044379395
SN - 0022-3530
VL - 46
SP - 441
EP - 472
JO - Journal of Petrology
JF - Journal of Petrology
IS - 3
ER -