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156O. Lexa et al. / Journal of Structural Geology 26 (2004) 155–161Fig. 1. Shear band geometry and definition of angles a, b and g according toPlatt and Vissers (1980).perpendicular to the intersection of CCC and SBC with theolder foliation.With the advent of modern kinematic analysis in structuralgeology in the early 1980’s, the XZ plane of finite strainellipsoid became extremely important. This plane is traditionallydefined as a plane parallel to the stretching lineation andperpendicular to the foliation. However, the stretchinglineation in phyllites or phyllonites can be difficult to define,and it can be easily confused with corrugations or intersectionlineation. Moreover, the presence of well-defined shear bandson a rock surface in the field is in many cases considered asatisfactory indicator to consider this surface as an XZ plane.Because, shear bands are such noticeable structures and theirkinematic significance is straightforward, these structureshave been widely used as first order kinematic indicators inmany orogenic belts (Behrmann, 1987).This paper aims to demonstrate that: (1) distinguishingbetween CCC and SBC is not always an easy task, (2) unlessthis is fully appreciated there is a great danger ofmisinterpretation when the shear bands are used as kinematicindicators, and (3) the CCC and SBC can appear identicalwhen seen on flat outcrop surfaces or in thin sections.2. Geometrical characteristics of oblique sections of foldsFolding or flow partitioning are commonly presented intwo dimensions while geological structures are threedimensional(3D) features. In order to justify the use ofthe two-dimensional (2D) analyses to investigate a threedimensionalproblem, certain assumptions are made.Because the displacement fields predicted by the 2D-theoryare limited to a plane (usually one of the principal planes ofthe strain ellipsoid), it is assumed that displacement isidentical in any parallel plane and therefore that theresulting fold structures are cylindrical. As a result, theaxes of the folds are perpendicular to the plane ofthe displacement field. Based on these assumptions wewill consider 2D sections normal to the fold axes to be ‘true’sections and all other sections ‘apparent’.Geometrically, shear-bands can be characterized by threeangles a, b and g (Fig. 1), corresponding to the relativeangles of the limbs, hinge trace and enveloping surface(Platt and Vissers, 1980). In order for the fold or flexureprofiles to have shear-band geometry, a should have a valuebetween 10 and 508, while b and g should range between 10and 258, so that the interlimb angle exceeds 1308. Platt andVissers (1980) show that these angles are mean values fromobservations in the field, for example from the Beticmovement zone (Behrmann, 1987). We will show that for agiven fold profile in the ‘true’ section (i.e. a section normalto the fold axis; Fig. 2) there is a specific range of ‘apparent’sections (i.e. a section oblique to the fold axis; Fig. 2) inwhich the fold profiles satisfy the geometrical criteria ofshear-bands.Apparent sections through three-dimensional cylindrical,coaxial folds can be treated as fold axis parallel projectionsof ‘true’ fold section onto the section plane. When ax þby þ cz ¼ 0 is the equation of a section plane and ( p, q, r)isthe vector parallel to the fold axis in an arbitrarily chosenreference frame, then the coordinates ½x yzŠ of points in a‘true’ section and the coordinates ½x 0 y 0 z 0 Š of points on an‘apparent’ section are related to each other by matrixequation:23bq þ cr 2ap 2arD D D2bp ap þ cr 2br½x yzŠ6 D D D¼½x 0 y 0 z 0 Š7642cpD2cqDap þ bqDwhere D ¼ðap þ bq þ crÞ.The 2D coordinates on the chosen section are obtained ascoefficients of linear combinations of any two perpendicularunit vectors coplanar with the section plane. We developeda simple MATLABw script, which visualises any sectionprofile across a given fold geometry and determine the threeangles a, b and g (Fig. 1) for the oblique section profile.Using this script we can examine any section across a fixedfold geometry and determine which of them satisfies thegeometric requirements for shear-bands. The results arepresented in a stereographic projection (Figs. 3 and 4)sharing the area containing poles to sections that satisfy theshear-band criteria. The area of sections exhibiting shearbandlike geometry is shaded on the basis of the interlimbangle a (Fig. 1).Sections through symmetrical folds generally have foldprofiles with an asymmetric geometry (Fig. 3) and theplanes on which the apparent fold geometry satisfies theshear-band criteria fall into two distinct groups separated bythe fold axial plane. These two groups contain poles tosections on which shear-band geometry exhibit opposingasymmetry, i.e. opposing ‘shear-sense’ criteria. The area ofthese domains on a stereographic projection, i.e. the range oforientations of section planes in space that display shearbandgeometries is related to the interlimb angle of thesymmetrical folds, so as the interlimb angle increasestowards 1808, the range of suitable sections displayingshear-band geometry increases.Sections across asymmetric folds that display shear-band75102
O. Lexa et al. / Journal of Structural Geology 26 (2004) 155–161 157Fig. 2. (a) Block diagrams of folded anisotropy and ‘apparent’ fold sections showing shear-band geometries. (b) Orientation of apparent fold sectionsexhibiting opposite sense of shear criteria. (c), (d) Principle of presentation of ‘apparent’ fold sections in stereographic projection.geometries are shown in Fig. 4. It can be seen that the range ofsections suggesting a sinistral and dextral ‘sense of shear’ isunequal in this example and a preferred enlargement of onegroup occurs. This asymmetry is controlled by the anglebetween the fold axial plane and the main anisotropy (Fig. 4).3. Geological exampleIn the Vepor basement of the Central WesternCarpathians, a flat-lying mylonitic foliation containing awell-developed stretching lineation is affected by late103
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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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TEXTURES OF NATURALLY DEFORMED META
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ORIGIN OF FELSIC MIGMATITES 39Grain
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ORIGIN OF FELSIC MIGMATITES 45Fig.
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ORIGIN OF FELSIC MIGMATITES 51Cmı
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104 J. FRANĚK ET AL.in terms of th
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