By A C Ries, R W H Butler and R H Graham, A. C. Ries, R. W. H. Butler, R. H. Graham
This distinctive e-book, in reminiscence and get together of the paintings of Professor Mike Coward, is set the deformation of the continental lithosphere. The amassed papers speak about geometry, structural ideas, approaches and difficulties in quite a lot of tectonic settings and thereby replicate the breadth of Coward's pursuits. They surround the evolution of Precambrian basement gneiss terrains, the geometry and evolution of thrust platforms, basement involvement and structural inheritance in basins, syn-orogenic extension, salt tectonics, the implication of structural evolution on hydrocarbon prospectivity and structural controls on mineralization. Examples are drawn from the Lewisian and Moine Thrust Belt of NW Scotland, the Italian Apennines, NW Himalayas, the Cyclades, Oman, Zagros Mountains, Colombian Cordillera, Carpathians, North Sea, offshore Brazil, nearby reviews of the Irumide Belt (central Africa), Taurus Mountains (Turkey), higher South the USA, and from the Witwatersrand Basin of South Africa and the Antler Orogeny of SW united states.
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Additional info for Deformation of the Continental Crust: The Legacy of Mike Coward (Geological Society Special Publication No. 272)
The precise driving force for such deformation during dyke emplacement remains unclear, although partial collapse of an initially wide feeder dyke could play a role. An extreme result of 'primary pinch and swell' could be the boudinage of the molten sheet into lens-shaped pockets, even while still molten, and this may explain the geometries seen today (Fig. 6). It should be noted that the large dyke has a sinuous southern boundary which may also be a gentle pinch and swell structure. Small folds in dyke margins (G and H in Fig.
On its NE side are intense platy fabrics parallel to the contact, but on the SW side the migmatitic banding is at right angles to the contact. This large strain difference is best explained if the apophysis were present and acting as a less competent zone across which deformation was decoupled. However, the dykes have little or no fabric. One way to reconcile these apparently contradictory structures is to postulate that the deformation occurred partly during dyke emplacement. So, for example, deformation could decouple across the molten apophysis, which later crystallized with an isotropic texture.
H. & GRAHAM,R. H. (eds) 2007. Geological Society, London, Special Publications, 272, 27-45. 0305-8719/07/$15 9 The Geological Society of London 2007. 28 JOHN WHEELER Fig. 1. The main outcrops of the Lewisian Complex in NW Scotland. (3) Rotations of pre-existing markers, such as dykes, at the margins of high-strain zones. Rotations are a consequence of any imposed strain, but become more diagnostic of simple shear when more than one set of markers is available; for example, two sets of dykes (Escher et al.
Deformation of the Continental Crust: The Legacy of Mike Coward (Geological Society Special Publication No. 272) by A C Ries, R W H Butler and R H Graham, A. C. Ries, R. W. H. Butler, R. H. Graham