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JOURNAL OF GEOPHYSICAL RESEARCH, VOL. 108, NO. B1, 2023, doi:10.1029/2001JB000632, 2003Strain distribution and fabric development modeledin active and ancient transpressive zonesKarel Schulmann, 1 Alan Bruce Thompson, 2 Ondrej Lexa, 1 and Josef Ježek 3Received 23 May 2001; revised 26 April 2002; accepted 20 May 2002; published 16 January 2003.[1] A model based on kinematics of transpression allows the measurable internalparameters (simultaneous strain, fabric, and vertical elevation) to be simulated in relationto the macroscopically determined external parameters of transpressive zones (i.e., zonewidth, velocity, angle of convergence, and zone depth). We present a diagram ofconvergence angle against time for homogeneous transpression, where isolines of strainintensity D, strain symmetry K, and vertical elevation of rock samples are superposed.However, the distribution of internal strain parameters is sensitive to three types of strainpartitioning: (1) Discrete partitioning results in general decrease of finite strainaccumulations and in increase of pure shear component, (2) ductile partitioning splits thetranspressional domain into a pure shear zone where strain accumulations decreases and ina wrench-dominated zone where strain accumulations increases, and (3) viscositypartitioning is marked by different strain rates in zones of different viscosity and therefore bydifferent strain parameters. INDEX TERMS: 8025 Structural Geology: Mesoscopic fabrics; 8110Tectonophysics: Continental tectonics—general (0905); 0905 Exploration Geophysics: Continental structures(8109, 8110); KEYWORDS: transpression, strain partitioning, exhumation, oblique convergenceCitation: Schulmann, K., A. B. Thompson, O. Lexa, and J. Ježek, Strain distribution and fabric development modeled in active andancient transpressive zones, J. Geophys. Res., 108(B1), 2023, doi:10.1029/2001JB000632, 2003.1. Introduction[2] Modern tectonic studies face the problem of understandingthe relationships between small-scale structuresand large-scale geometry in orogenic zones. The linksbetween the external and internal parameters governingthe problem are particularly important. These factors maybe viewed as far-field causes related to local effects. Weexamine here these relationships in ancient and activetranspressive zones. External structural parameters are representedby the geometry of orogenic zones (i.e., zone width(distance between colliding plates), obliquity (angle ofconvergence) and depth of the transpressive zone. Irregularitiesof plate boundaries (shape of indenting block), andthe velocity and duration of plate convergence) may alsoplay an important role. Internal (local) structural parametersthat can be examined are fabric and strain intensity, symmetryof fabrics, orientations of strain axes, pressure (depth)memory, and metamorphic facies of the rocks. Theseinternal structural parameters are determined by the interactionsof the external forces with local lithological heterogeneitiesand rheologies in the transpressive zone.[3] Relative motion of lithospheric plates on a sphericalsurface is such that the plate convergence vectors are often1 Institute of Petrology and Structural Geology, Faculty of Science,Charles University, Prague, Czech Republic.2 Department Erdwissenschaften, ETH Zurich, Switzerland.3 Institute of Applied Mathematics and Computer Science, Faculty ofScience, Charles University, Prague, Czech Republic.Copyright 2003 by the American Geophysical Union.0148-0227/03/2001JB000632$09.00not orthogonal to plate boundaries [McKenzie and Parker,1967; Dewey, 1975]. These plate boundaries experiencecombined transcurrent and convergent displacements associatedwith development of deformation zones of differentsize. Within continental blocks, the deformation is not onlyrestricted to active plate boundaries but occurs within zonesof weakness inside rigid continental domains [e.g., Tommasiand Vauchez, 1997] and can be approximately described asa deformation of a weak zone bounded by rigid blocks withsteep parallel walls. All the mentioned types of deformationzones can be more or less described by a model called‘‘transpression,’’ introduced first by Harland [1971], developedby Sanderson and Marchini [1984], and elaborated bymany others. Despite its simplicity, it seems that the modelstill has much to contribute toward our understanding of thenature of convergent orogeny. In this work we develop themodel to quantify the effects of external (macroscopic)parameters on temporal development of internal strainparameters in transpressive (obliquely convergent) weakzones of finite width.2. Structural Definition of Transpression andProblems to Be Solved[4] The classical zone of transpressive deformation is atabular weak region subjected between its steep walls to asimultaneous pure shear and simple shear. In the model ofSanderson and Marchini [1984] the material is able to slipfreely upward (vertically extruded) along the walls of thetranspression zone. The transpressive deformation zonedefined by Sanderson and Marchini [1984] was also limiteddownward by a rigid horizontal plate (like a rigid floor),ETG 6 - 169
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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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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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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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HEAT SOURCES AND EXHUMATION MECHANI
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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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ClickHereforFullArticleJOURNAL OF G
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ORIGIN OF FELSIC MIGMATITES 31Ó 20
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ORIGIN OF FELSIC MIGMATITES 39Grain
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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 49stron
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ORIGIN OF FELSIC MIGMATITES 51Cmı
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