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652 O. LEXA ET AL.(a)(b)Fig. 3. Geological cross-sections A–A¢ and B–B¢ (shown in Fig. 2) of the Stare´ Město belt disclosing major structures, lithology of individual units and major tectonic boundaries.Equal-area, lower-hemisphere stereoplots show D 1 ,D 2 and D 3 planar and linear structures. Each stereoplot is contoured at regular multiples of distribution. Drawings are madeaccording to field photographs and field notes and show principal structural features.Ó 2005 Blackwell Publishing Ltd234
CONTRASTING TEXTURAL RECORD OF TWO METAMORPHIC EVENTS 653Structures in Variscan granodioriteThe Variscan granodiorite sill is syntectonicallyemplaced between the mylonitic metagabbro to thewest, and the banded amphibolite complex to the east(Parry et al., 1997). The structural pattern of thegranodiorite sill varies from SW to NE along thelength of the intrusion (Figs 2 & 3). The magmatic tosubsolidus foliation (S 2 ) dips to the NW and bears anintense subhorizontal mineral lineation (L 2 ) defined byan alignment of amphibole (Fig. 3a,b). Rare lock-upshear-bands filled with residual melt indicate a dextralsense of shear. In the south, the granodiorite does notform a continuous body but occurs as numerous sills insurrounding amphibolites and anatectic metasediments(Fig. 3b). The granodiorite locally forms dykesemplaced along conjugate steep brittle–ductile NW–SEor NE–SW trending shear zones at high angle to theinitially flat-lying S 1 foliation (Fig. 3a,b).Structures of mylonitic metagabbrosAlthough the western metagabbro belt was stronglyreworked during the Variscan orogeny, magmaticstructures are preserved in the low-strain domains(Fig. 4c). Here, the metagabbro exhibits either amedium-grained isotropic texture and homogeneouscomposition, or layering marked by alternating layersof variable grain size ranging from a few mm up to 2 cm(Fig. 4c). The mylonitic metagabbros exhibit thedevelopment of S 2 mylonitic foliation, defined byalternating monomineralic ribbons of recrystallizedplagioclase and amphibole (Figs 4c & 5c). This foliationdips at medium to high angles to the WNW.Towards the south, the foliation tends to becomesubvertical (Fig. 2b). A strong mineral L 2 lineation isdefined by recrystallized aggregates of amphibole and isassociated with numerous kinematic indicators suggestingdextral shearing. The S 2 foliation is locallyaffected by late F 3 folds with hinges sub-parallel to L 2lineation or by development of S 3 crenulation cleavage.The complete structural and kinematic coherency betweenthe metagabbros and underlying granodiorite sillsuggests their common Variscan deformation history.The eastern metagabbro was affected by heterogeneousshear zones (Fig. 4d) during the Variscan deformation.The metagabbros are strongly mylonitized atthe upper and lower contacts with the hangingwall andFig. 4. Field photographs showing main structural features of important lithologies of the Stare´ Meˇsto belt. (a) Metamorphic layeringM 1 of banded amphibolite complex. (b) Extensional melt-filled shear-bands D 1 in tonalitic migmatitic gneiss of the banded amphibolitecomplex. (c) Coarse-grained C-O metagabbro (left photograph) mylonitized during D 2 (right photograph) from western belt. (d)Coarse-grained C-O metagabbro mylonitized by localized shear zones during D 2 from eastern belt.Ó 2005 Blackwell Publishing Ltd235
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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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SCHULMANN ET AL.: STRAIN DISTRIBUTI
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5 - 2 LEXA ET AL.: COLLISION IN WES
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156O. Lexa et al. / Journal of Stru
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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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J. metamorphic Geol., 2011, 29, 79-
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ClickHereforFullArticleJOURNAL OF G
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B10406SCHULMANN ET AL.: RHEOLOGY OF
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J. metamorphic Geol., 2008, 26, 29-
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ORIGIN OF FELSIC MIGMATITES 31Ó 20
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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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114 J. FRANĚK ET AL.at these P-T c
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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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124 J. FRANĚK ET AL.Fig. 16. Inter
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126 J. FRANĚK ET AL.development of
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128 J. FRANĚK ET AL.Behrmann, J.H.
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130 J. FRANĚK ET AL.Southern Bohem
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