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110 J. FRANĚK ET AL.(a)(b)(c) (d) (f)(e)(g)(h)Fig. 6. BSE images of S1 layering. (a–f) Inclusions in the large perthite grains reflect peak metamorphic assemblage. A microchemicalprofile across garnet in (f) is presented in Fig. 7. (g) Grt–Ky–Pl-rich S1 band containing biotite, which grows parallel to S2. (h)K-feldspar-rich band enclosing kyanite with typical well-developed plagioclase corona.decreasing grossular, increasing pyrope and almandine,and flat X Fe (Alm 0.52Þ0.61 Grs 0.23Þ0.04 Prp 0.22Þ0.28Sps 0.00–0.01 ; X Fe =Fe⁄ (Fe + Mg) = 0.70, Fig. 7b).The X Fe of biotite in the matrix ranges from 0.33 to 0.35with Ti = 0.21)0.26 (pfu based on 22 oxygen).Recrystallized K-feldspar and plagioclase are zonedfrom core to rim, with Or 77 fi 97 Ab 23 fi 03 An 0.0 andOr 02 fi 01 Ab 81 fi 77 An 18 fi 21 , respectively. Kyanite,Ó 2010 Blackwell Publishing Ltd348
PRECURSOR AND RHEOLOGY OF VARISCAN GRANULITES 111(a)(b)Fig. 7. (a) Ternary plot of feldspar compositions acquired from microchemical analyses of perthite recrystallization and S2 fabric.Similar bulk compositions of parental perthites and shielded matrix are contrasted against areal analyses of deformed matrix. Zoningof plagioclase and to a lesser extent also of K-feldspar are highlighted in the description of data clusters. (b) Microchemical profileacross garnet enclosed in large perthite showing a wide flat grossular-rich core, gradual compositional zoning at both rims and almostconstant X Fe across the whole crystal.both included in perthite and in the matrix, issurrounded by a plagioclase corona.The studied sample H296-S1A lacks biotite inclusionsin the perthite porphyroclasts, and because biotiteand garnet inclusions in perthite are generally rare,the other five samples from the same macroscopicallyhomogeneous outcrop were analysed to test whetherthere is a difference in composition between biotite andgarnet inclusions in perthite and those in the matrix.The biotite X Fe ranges from 0.23 to 0.40 andTi = 0.15)0.34 pfu, and there is no clear differencebetween biotite inclusions and biotite in the matrix(Table 1). Garnet in other thin sections shows the samezoning as that from the sample H296-S1A, but additionallya decrease in X Fe to 0.68 at some garnet rimswas detected.The composition of the large unzoned perthitegrains was acquired in several samples from the sameoutcrop by areal analyses performed by scanning ofregions containing 100 plagioclase exsolution lamellae.It corresponds on average to 68.2% Or, 27.3% Aband 4.5% An (Fig. 7a). The K-feldspar domains ofperthite porphyroclasts contain on average 87.1% Or,12.3% Ab and 0.6% An. The relict perthite porphyroclastsreveal two generations of plagioclase exsolutionlamellae (e.g. Fig. 6c). The coarser exsolution lamellae,presumably older, exhibit elongated braided shapesand are 0.8% Or, 76.7% Ab and 22.5% An in composition.The second micro- to crypto-perthitic generationof exsolution lamellae was not analysed becauseof its small thickness. Detailed feldspar compositionsstudied in relation to the recrystallization mechanismsfor individual deformation episodes are given below.P–T path for S1 and S2 fabricsA pseudosection was calculated using THERMOCALC 3.30(Powell & Holland, 1988) and DATASET 5.5 (Holland &Powell, 1998; November 2003 upgrade), in the systemNCKFMASHTO (Na 2 O–CaO–K 2 O–FeO–MgO–Al 2 O 3 –SiO 2 –H 2 O–TiO 2 –O) with biotite and meltmodels from White et al. (2007), garnet from Dieneret al. (2008), ilmenite from White et al. (2000), feldsparfrom Holland & Powell (2003), white mica fromCoggon & Holland (2002) and cordierite from theTHERMOCALC documentation (Powell & Holland, 2004).Mineral composition isopleths x(g, bi) = Fe ⁄ (Fe +Mg), z(g) = Ca ⁄ (Ca + Fe + Mg) and t(bi) =XTi(M1) were plotted for garnet and biotite. Theanalysed composition of the sample H296-S1A (inwt% SiO 2 = 71.98, TiO 2 = 0.42, Al 2 O 3 = 13.53,FeO = 2.1, MnO = 0.03, MgO = 0.73, CaO = 1.93,Ó 2010 Blackwell Publishing Ltd349
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“It strikes me that all our knowl
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Contentsviii4.7 Schulmann, Konopás
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Dedicated to my wife Markéta, daug
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Foreword 2First topic “Quantitati
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Foreword 4source and freely availab
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1. Quantitative analysis of deforma
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Chapter 2Mechanisms of lower crusta
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2. Mechanisms of lower crustal flow
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Chapter 3Quantitative analyses ofme
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3. Quantitative analyses of metamor
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Bibliography 42Culshaw, N., Beaumon
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Bibliography 44sources and trigger
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Bibliography 46Skrzypek, E., Štíp
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Journal of Structural Geology 23 20
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DTD 5ARTICLE IN PRESSJournal of Str
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DTD 5ARTICLE IN PRESSL. Baratoux et
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Table 1Statistical values of the qu
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Table 2Summary of parameters derive
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J. metamorphic Geol., 2008, 26, 273
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EXHUMATION IN LARGE HOT OROGEN 275m
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Probabi l irequencyProbabi l ireque
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EXHUMATION IN LARGE HOT OROGEN 279y
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EXHUMATION IN LARGE HOT OROGEN 281N
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EXHUMATION IN LARGE HOT OROGEN 283w
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EXHUMATION IN LARGE HOT OROGEN 285a
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EXHUMATION IN LARGE HOT OROGEN 287w
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EXHUMATION IN LARGE HOT OROGEN 289T
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EXHUMATION IN LARGE HOT OROGEN 291O
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EXHUMATION IN LARGE HOT OROGEN 293r
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EXHUMATION IN LARGE HOT OROGEN 295B
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EXHUMATION IN LARGE HOT OROGEN 297R
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CONTRASTING TEXTURAL RECORD OF TWO
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TEXTURES OF NATURALLY DEFORMED META
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1.0--0.9__Mg~(Mg2++Fe2+)9 Core of p
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' ~'-----2~--~----TEXTURES OF NATUR
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ClickHereforFullArticleJOURNAL OF G
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