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158O. Lexa et al. / Journal of Structural Geology 26 (2004) 155–161Fig. 3. Stereographic projection showing influence of interlimb angle. The range of section planes showing shear-band geometry increases with interlimb angleof folds affecting main anisotropy.Fig. 4. Stereographic projections showing influence of angle between fold axial plane and main anisotropy. The probability of occurrence of opposite shearcriteria decreases with decreasing angle of axial plane and plane of main anisotropy.104
O. Lexa et al. / Journal of Structural Geology 26 (2004) 155–161 159Fig. 5. Structural elements from studied area. (a) Poles to main Alpine metamorphic anisotropy showing girdle distribution around the axis sub-parallel tohinges of late Alpine folds—116 measurements; (b) orientation of stretching lineation—68 measurements; (c) distribution of poles to main fracture systemsdeveloped in studied area (Hók et al., 2001) overlaid by shaded areas indicating ‘apparent’ fold sections in which shear-band geometry can be observed; (d)rose diagram of main fracture directions in studied area (Hók et al., 2001). Note that a main maximum of fracture orientations coincides with orientations ofapparent fold sections. All data are plotted on Schmidt net and projected from lower hemisphere. In (a) and (b), the contour levels are even multiples of standarddeviation.folding, which generated a crenulation cleavage. The foldaxes are generally sub-parallel to the stretching lineation(Fig. 5). Most of the studies on the kinematic andtectonic evolution of this region are based on the use ofshear-bands and asymmetric porphyroclasts as kinematicindicators. These studies have resulted in the generallyaccepted model of post-orogenic, orogen-parallel extension(Plašienka et al., 1999; Lupták et al., 2000; Janáket al., 2001). In contrast to the interpretation given byprevious workers in which the major extensionaldeformation post-dates the episode of compression, astudy by these authors shows that extension was the firstAlpine deformation in the area and that this pre-dates thecompressional stage of tectonic evolution (Lexa et al.,2003). The extensional phase is highly asymmetrical andlocally non-coaxial. The majority of the studied outcropsshow that we are dealing with oblique sections acrosssmall-scale folds, which are likely to be misinterpreted asshear-bands (Fig. 6).In order to evaluate the probability of encounteringoblique sections with shear-band like geometry in aparticular field area, we need to identify the dominantgeometries of the small-scale folds and, moreover, wehave to understand the distribution of surfaces on whichthe structures are observed. It should be pointed out thatthe majority of observations are from natural rather thanman-made outcrops, where the orientation of the exposedsurfaces is controlled mainly by fractures (typicallyjoints). In addition, sections that are sub-parallel to thelineations are specifically selected as being appropriatefor the study of kinematic indicators. We plotted therange of sections with shear-band like geometry, therange of naturally occurring fractures and the distributionof lineations on a stereographic projection (Fig. 5c),which shows that there is a high probability of systematicallyobserving oblique sections across the small-scalefolds showing opposite shear-band geometries. Wepropose that such field observations led some authors105
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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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EXHUMATION IN LARGE HOT OROGEN 297R
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HEAT SOURCES AND EXHUMATION MECHANI
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CONTRASTING TEXTURAL RECORD OF TWO
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Contrasting microstructures and def
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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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B10210ZÁVADA ET AL.: EXTREME DUCTI
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ClickHereforFullArticleJOURNAL OF G
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B10406SCHULMANN ET AL.: RHEOLOGY OF
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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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