Arcuate fold and cleavage patterns in the southeastern part of the Anglo–Brabant Fold Belt (Belgium): tectonic implications

Sintubin, Manuel

doi:10.1016/s0040-1951(99)00133-x

Cited by 33 publications

(77 citation statements)

References 19 publications

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“…The main features associated with this deformation event are folds with a moderately to well-developed cogenetic cleavage (e.g. Sintubin, 1997Sintubin, , 1999Debacker, 2001;Debacker et al, 2005a and references therein).…”

Section: Anglo-brabant Deformation Belt (Belgium)mentioning

confidence: 99%

“…3;Vandenven, 1967;Debacker et al, 1999;Belmans, 2000;Debacker, 2001). This Silurian rim, predominantly consisting of pelitic, distal turbidite deposits (Verniers and Van Grootel, 1991), is characterised by gentle to close, upright to moderately inclined, decametre-to hectometre-scale folds, with well-developed convergent cleavage fans (Kaisin, 1933;Mortelmans, 1953;Legrand, 1967;Sintubin, 1997Sintubin, , 1999Debacker et al, 1999). Although the convergent cleavage fans were initially attributed to a poly-phase deformation (Kaisin, 1933;Mortelmans, 1953;Vandenven, 1967;Legrand, 1967), more recent studies show that this fanning is much more likely the result of a single-phase progressive deformation (Debacker et al, 1999;Belmans, 2000;Debacker, 2001Debacker, , 2002Herbosch et al, 2002).…”

Section: Anglo-brabant Deformation Belt (Belgium)mentioning

confidence: 99%

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Contractional kink bands formed by stress deflection along pre-existing anisotropies? Examples from the Anglo-Brabant Deformation Belt (Belgium) and the North Dobrogea Orogen (Romania)

Debacker

Seghedi

Belmans

et al. 2008

Journal of Structural Geology

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a b s t r a c tKink bands within two slate belts, the Anglo-Brabant Deformation Belt (Belgium) and the North Dobrogea Orogen (Romania), reveal similar problems with respect to linking kink band geometries to expected palaeostress directions. In the North Dobrogea Orogen, the two opposite kink band sets of two different systems of conjugate kink bands develop for a wide variety of cleavage orientations. In the Anglo-Brabant Deformation Belt, the occurrence of the two opposite kink band sets of a conjugate kink band system opposes the expected occurrence. In both cases, this can be attributed to stress deflection along a pre-existing anisotropy. Moreover, the presence of kink bands in the North Dobrogea Orogen with curving kink axes (and curving kink band boundaries) also puts doubt on the direct relationship between kink band geometry and stress. The idea of stress deflection along a pre-existing anisotropy and the strong control of the pre-existing anisotropy on the kink band geometry and orientation has important implications for the use of kink bands as regional palaeostress indicators. Depending on the relative intensity and relative orientation of the pre-existing fabrics (here bedding and cleavage), different mechanisms of kink band development may operate. Depending on the mechanism, different solutions in terms of inferred palaeostress direction may exist.

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Section: Anglo-brabant Deformation Belt (Belgium)mentioning

confidence: 99%

Section: Anglo-brabant Deformation Belt (Belgium)mentioning

confidence: 99%

Contractional kink bands formed by stress deflection along pre-existing anisotropies? Examples from the Anglo-Brabant Deformation Belt (Belgium) and the North Dobrogea Orogen (Romania)

Debacker

Seghedi

Belmans

et al. 2008

Journal of Structural Geology

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“…At present, there is evidence only for a single progressive deformation event, currently considered to have taken place between the Llandovery and the end of the Early Devonian, possibly continuing into the Eifelian (Debacker 2001;Debacker et al 2002;Verniers et al 2002). The main features associated with this deformation are folds with a welldeveloped, cogenetic cleavage (Sintubin 1997a(Sintubin , 1999Debacker 2001;Debacker et al 2002;Verniers et al 2002).…”

Section: Geological Settingmentioning

confidence: 99%

Transitional geometries between gently plunging and steeply plunging folds: an example from the Lower Palaeozoic Brabant Massif, Anglo-Brabant deformation belt, Belgium

Debacker

Sintubin

Verniers

2004

JGS

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Although many studies have dealt with markedly different fold orientations and associated cleavage-fold relationships within individual, single-phase deformed fold belts, there are very few descriptions of possible gradual, transitional fold geometries. The Lower Cambrian steep core of the singlephase deformed Brabant Massif contains steeply plunging, west-facing folds with a Z-shaped asymmetry, whereas the Ordovician-Silurian southern rim consists of gently plunging, upward facing folds. A gradual transition is observed between these end-member orientations, in a NW-SE-trending zone 1-1.5 km wide, in which the folds appear to be strongly curvilinear and locally downward facing. The structural geometries within this transition zone are described in detail and the geometric changes analysed in the light of the fold transition. The strongly variable fold orientations are tentatively attributed to a bulk oblate tectonic strain. The transition zone overlies an aeromagnetic lineament, classically interpreted as a dextral shear zone. The steeply plunging folds, the transition zone and the aeromagnetic lineaments are all attributed to a local dextral transpression, in which deformation is partitioned both vertically and laterally. The results indicate that within zones of heterogeneous transpression, the different deformation domains are not necessarily always fault bounded.

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“…The validation of a numerical model with respect to kinematic constraints of basement blocks and cleavage-fold relationships is based on regional mapping of cleavage patterns and finite strain patterns in weak metasedimentary formations. There is a range of natural examples in which the basement (composed of gneisses and granites) behaves as a rigid promontory of irregular shape with respect to weakly metamorphosed mechanically weak slates (Sintubin, 1999;Lexa and Schulmann, 1999). In agreement with Woodcock et al (1988) and Mansy et al (1999) the cleavage-fold patterns in such deformable weak rocks reflects the geometry and direction of movement of rigid blocks.…”

Section: Tectonic Implicationsmentioning

confidence: 99%

Strain partitioning in front of an obliquely convergent indenter

Ježek¹,

Schulmann²,

Thompson³

2002

Stephan Mueller Spec. Publ. Ser.

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Abstract.A model is presented that combines the traditional approach to transpression with the thin viscous sheet approximation of the lithosphere, to study deformation in front of an obliquely colliding indenter. The model produces a zone dominated by lateral simple shear (orogen parallel transcurrent movements) close to the indenter and a zone of dominant pure shear (orogen perpendicular pure shear/thrusting regions) further away from the indenting boundary. The relative width of simple shear dominated zone with respect to the more distant pure shear domain in terms of the angle of convergence is discussed. The possibility of development of transcurrent faults in front of an indenting plate is enhanced by the reactivation of fabric anisotropy created progressively during indentation.

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Arcuate fold and cleavage patterns in the southeastern part of the Anglo–Brabant Fold Belt (Belgium): tectonic implications

Cited by 33 publications

References 19 publications

Contractional kink bands formed by stress deflection along pre-existing anisotropies? Examples from the Anglo-Brabant Deformation Belt (Belgium) and the North Dobrogea Orogen (Romania)

Contractional kink bands formed by stress deflection along pre-existing anisotropies? Examples from the Anglo-Brabant Deformation Belt (Belgium) and the North Dobrogea Orogen (Romania)

Transitional geometries between gently plunging and steeply plunging folds: an example from the Lower Palaeozoic Brabant Massif, Anglo-Brabant deformation belt, Belgium

Strain partitioning in front of an obliquely convergent indenter

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