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ETG 6 - 8 SCHULMANN ET AL.: STRAIN DISTRIBUTIONFigure 5. Vertical elevation rate for transpression expressed in terms of angle of convergence (a) andtime parameter (k t ) for different base depths, RFD = 40, 70 km, and different original sample depths z 0 =30, 60 km. The curves show elevation achieved by these samples in a given time. For example, in Figure5a (RFD = 40 km, z 0 = 30 km) for convergence angle a =80° sample is elevated to depth 10 km after k t =1.2. For the case of R vd = 0.1 the time of elevation corresponds to 12 Myr.deformation, where the rest of lateral displacement and thewhole across strike shortening are accommodated, can bededuced using our hypothetical strain map (Figure 6). Toevaluate the influence of partitioning on strain parameters,recalculation of values R vd and a are made using theequations (B1) and (B2) (in Appendix B) or they can betaken from Figure 7. The effect of discrete partitioning onfinite strain parameters is expressed by a virtual increase ofconvergence angle and decrease of R vd (decrease of plateconvergence velocity or increase of weak zone width). Thusfor a transpression zone with an angle of convergence of45°, R vd equal 0.1, and with 50% of lateral displacementconsumed by discrete faults, we use values of a 0 = 63.43°0and R vd = 0.079 (Figure 7). For 10 Myr of convergencewithout discrete partitioning, finite strain parameters are D =1.64 and K = 0.58. When discrete partitioning accommodates50% of the lateral displacement, the finite strainparameters are D = 0.9 and K = 0.8.[35] Ductile partitioning splits the deformed domain intoa pure shear zone (PSZ) and a wrench-dominated zone(WDZ). We assume that the pure shear-across-strike shorteningand elevation are homogeneously distributed acrossthe whole system, while simple shear-lateral displacement isaccommodated only in the WDZ. We examine developmentof strain parameters for different widths of the WDZ,expressed as ratio p 2 of the width of WDZ and the widthof the whole transpressional zone. Such a partitioning ofpure shear and simple shear within transpressional zones isresponsible for decomposition of the velocity gradienttensor into two separate tensors according to equations(C1) and (C2) (in Appendix C).[36] While the evolution of strain parameters in the PSZmay be obvious, the evolution of strain parameters in theWDZ zones is less so. The results of calculations for WDZzones of different width are shown in Figure 8. Fifty percentof ductile partitioning (Figure 8a) exhibits a similar patternof strain parameters as a nonpartitioned system. Nevertheless,the domain with horizontal lineation and the domainof oblate symmetry are both slightly enlarged. This isrelated to the shift of the lineation switch, which occurs76
SCHULMANN ET AL.: STRAIN DISTRIBUTION ETG 6 - 9Figure 6. Superposition of strain intensity (D), strain symmetry (K ), and sample elevation for variousvalues of RFD and initial sample depth z 0 , plotted in terms of angle of convergence (a) and time parameter(k t ). The values of D show a strong dependence on R vd and time (but not much on a)fora =20° to 90°;fora
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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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2. Mechanisms of lower crustal flow
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Page 54 and 55: Bibliography 42Culshaw, N., Beaumon
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Page 58 and 59: Bibliography 46Skrzypek, E., Štíp
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DTD 5ARTICLE IN PRESSL. Baratoux et
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Table 2Summary of parameters derive
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DTD 5ARTICLE IN PRESSL. Baratoux et
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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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HEAT SOURCES AND EXHUMATION MECHANI
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EXTRUSIONOFLOWERCRUSTINVARISCANOROG
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J. metamorphic Geol., 2005, 23, 649
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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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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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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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