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116 L. BARATOUX ETAL.Plagioclase - eastern belt[1001 (010) (001).,7, ...... .. . . . . . ~,,. . :~':. .' ..~_s kQ...'........,....._~...:/r ....' .:.-,~.~ :- -.~ '...: ,'9 MD = 3.36 9 MD = 6.24 9 MD = 3.63.e-...........,, ~ .......-.-" :? ,::..,...9 MD = 3.28 9 MD = 2,83 9 MD = 2.54.,..,"E --9 MD = 3.33 9 MD = 3.99 9 MD = 3.33-.; ~&~-41 . --.,.."" :'. ".,. f" """~.-. ):: ..........., ,,~ ..Lower hemisphere 9 MD = 2.71 9 MD = 2.67 9 MD = 2.63Fig. 13. Point and contour pole figures of plagioclase CPO in the eastern belt (lower hemisphere, equal areaprojections). Diagrams are contom'ed as multiples (0.5, 1.0, 1.5, 2.0, 2.5 .... x ) of uniform distribution. MD ismaximum density of data in the contour diagrams. Foliation is represented by the horizontal line, lineation istrending E-W.(El) show progressive reorientation of the crystallographicplanes (100) towards the foliationdirection and c-axes [001] towards the lineation(Fig. t6a). Cleavage planes { 110} cluster parallelto the foliation as well. The asymmetry of theCPO fabric is consistent with the dextral shearzone cross-cutting the porphyroclast under theangle of ~20 ~ with respect to the mylonitic foliation.The CPO of hornblende in the ultramylonite(E3) displays a strong maximum of polesto the (100) and {110} planes (Fig. 16b) clusteringnormal to the foliation (I--2.9 for (100)).The c-axes trend in the direction of lineation.Such CPO patterns suggest that the (100)[001]slip system could be activated. Inclination ofdata with respect to the mylonitic foliation dueto dextral shear is present. Similar fabric asymmetry,interpreted as the result of a non-coaxialstrain, has been described in eclogite faciesglaucophanites (Zucali et al. 2002).Hornblende CPO in the augen mylonite (W 1)from the western belt form a cluster of (100)planes subparallel to the mylonitic foliationand c-axes parallel to the lineation. However, afew grains occur with a different orientation(Fig. 16c). In the banded mylonite (W2), the(100) planes and c-axes reveal similar orientationas in the augen mylonite but the maxima are lesspronounced (Fig. 16d). The I parameters areslightly lower in the banded mylonite (W2) comparedto the augen mylonite (W1). This CPOpattern is consistent with activation of the(100)[001] slip system. No asymmetry withrespect to the shear plane occurs.Discussion and conclusionsRecrystallization and deformationmechanisms of plagioclaseThe early deformation stage in plagioclase in theeastern amphibolite facies metagabbro belt ismarked by undulatory extinction, twinning, andfracturing, which are typical for low temperature268
TEXTURES OF NATURALLY DEFORMED METAGABBROS 117Lineationsa) upper hemisphere a-coo) a-(~oo)Protomylonite {.-'..:: "_~.'.~.~E1Plagioclase - eastern belt=219Poles to foliationsa*(100)a*(100)~ M D = 3.91 9D = 3.60, 9a*(100) a'(100) a*(100) a*(100)N=160 N:'.~-...:.Mylonite , .....E2-pl 1 ~!-'".:=o .;MyloniteE2-p12D=3,53 9D=2.839a*(lOO) a*(lO0) a*(lOO) a*(lOO)= 160, ", o-N=I ~ 0oUltramyloniteE3MD = 2,95 9D = 3.20 9a'(~00) a'(10o) a'0 00) a'(100)N = 200D=4, 9 D=4.b) ~ IPF Reference frame 12~~0Directions [uvw] _ Poles to planes (hkl) /o/o21O1 ~' 1~1~10,~~ O l O O l O ~ o i - oFig. 14. (a) Inverse pole figures of plagioclase CPO in the eastern belt (upper hemisphere, equal area projections).Projections of lineations are presented as point and contour diagrams in the left, projections of poles to foliations are inthe fight side of the figure. N is the number of plotted points. Diagrams are contoured as multiples (0.5, 1.0, 1.5, 2.0,2.5 .... • ) of uniform distribution. MD is maximum density of data in the contour diagrams. Large circle and square inthe protomylonite represent two porpbyroclasts. (b) The crystallographic reference frame.and/or high differential stress (Tullis & Yund1987, 1992; Rosenberg & Sttinitz 2003). Smallgrains concentrated in these fractures exhibittypical features of dynamic recrystallizationsuch as bulging and subgrain rotation. However,some of them might have developed bycrushing of the host grain or by heterogeneousnucleation (StiJnitz et al. 2003; Rosenberg &Sttinitz 2003). Twin-free grains adjacent totwinned host grains (see Fig. 3b), compositionalresemblance of recrystallized grains to hostgrains, and strong CPO (Lister et al. 1978) mayindicate a recrystallization mechanism by subgrainrotation. This recrystallization mechanismis also supported by small average grain sizes,small aspect ratios and weak SPO of newgrains. A fairly small degree of GBPO for plagioclase-plagioclaseboundaries is in agreementwith subequant shapes of equidimensional newgrains, thus favouring the hypothesis of subgrain269
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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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J. KonopaÂsek et al. / Journal of
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JOURNAL OF GEOPHYSICAL RESEARCH, VO
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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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Author's personal copyK. Schulmann
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HEAT SOURCES AND EXHUMATION MECHANI
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ORIGIN OF FELSIC MIGMATITES 33durin
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ORIGIN OF FELSIC MIGMATITES 35(a)Ty
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ORIGIN OF FELSIC MIGMATITES 37(a)Pl
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ORIGIN OF FELSIC MIGMATITES 39Grain
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ORIGIN OF FELSIC MIGMATITES 41(a)(b
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ORIGIN OF FELSIC MIGMATITES 43(a)(b
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ORIGIN OF FELSIC MIGMATITES 45Fig.
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ORIGIN OF FELSIC MIGMATITES 47produ
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ORIGIN OF FELSIC MIGMATITES 49stron
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ORIGIN OF FELSIC MIGMATITES 51Cmı
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ORIGIN OF FELSIC MIGMATITES 53easte
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104 J. FRANĚK ET AL.in terms of th
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106 J. FRANĚK ET AL.Fig. 2. Struct
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108 J. FRANĚK ET AL.(a)perthite po
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110 J. FRANĚK ET AL.(a)(b)(c) (d)
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112 J. FRANĚK ET AL.Table 1. Repre
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116 J. FRANĚK ET AL.(a)(b)Fig. 10.
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120 J. FRANĚK ET AL.Table 2. Quant
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130 J. FRANĚK ET AL.Southern Bohem
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