By A C Ries, R W H Butler and R H Graham, A. C. Ries, R. W. H. Butler, R. H. Graham
This specified e-book, in reminiscence and party of the paintings of Professor Mike Coward, is set the deformation of the continental lithosphere. The gathered papers talk about geometry, structural ideas, tactics and difficulties in a variety 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, local stories of the Irumide Belt (central Africa), Taurus Mountains (Turkey), better 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)
P. & PARK, R. G. 1987. The role of mid crustal shear zones in the Early Proterozoic evolution of the Lewisian. In: PARK, R. G. & TARNEY, J. (eds) Evolution of the Lewisian and Comparable Precanlbrian High Grade Terrains. Geological Society, London, Special Publications, 27, 127-138. COWARD, M. , FRANCIS, P. , GRAHAM, R. H. & WATSON, J. V. 1970. Large Scale Laxfordian structures of the Outer Hebrides in relation to those of the Scottish Mainland. Tectonophysics, 10, 425435. 25 DEARNLEY, R. 1962.
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. This could also explain the tapered shapes of the boudin ends, rather than the blunt ends to be expected when a strong layer is boudinaged.
The fabric in the gneiss at E (Fig. 3e) is also inclined to the dyke to its immediate SW, except in the 3 cm wide zone adjacent to the dyke where it is deflected. Again the main fabric is interpreted as Inverian (significant Laxfordian strain being restricted to the 3 cm wide border region). This suggests that the fabric in the SW part of Figure 4 is mainly Inverian, even though it is parallel to the foliated dykes. The Inverian NW-SE fabrics in the SW of Figure 4 are heterogeneous on a metre scale.