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7, 8, A and B, 26, and 27, A–C). Only the degree of dispersion, but not the shapes, of blocks changes from boudinaged bed packages to blocks in shaly matrix (Figs. 7B, 8, and 9). The origin of blocks is related to a fracture boudinage in the limestone and siltstone-sandstone beds. More sets of calcite-filled veins that are almost orthogonal to the bedding are present in the blocks (Figs. 7B and 27A). These sets commonly predetermined the surfaces along which the blocks separated, giving the classic sharp, angular, and prismatic shape.

B: The differential deformation of the siliciclastic and the calcareous intervals of a mixed turbidite bed of unit UCE1. blocks in shaly matrix. The common planar attitude of pseudobedding and bedding is the sum of the interaction of different mesoscale to macroscale structures. Macroscale to mesoscale observations. Large-scale duplications of part of the sequence are evident where thick beds are a marker or where it is possible to recognize the polarity of bedding (Figs. 7B and 25). The duplications are evidenced by the overturning of a large section of the sequence, some tens of meters in thickness over some tens of meters in length (Fig.

Some blocks are the relicts of pinch and swell boudinage of limestones (Figs. 27F and 29A) and sandstones-siltstones. The boudinage, commonly associated with fault troughs (Hoedemaeker, 1973), occurred by plastic accommodation of rocks without observable mesoscopic or microscopic discontinuities. Some sandstone-siltstone blocks are the relicts of rootless, noncylindrical folds, with marked thickening of the hinge (Figs. 27G and 29B) and curved axial planes. Folding occurred by the plastic accommodation of the sandstones and siltstones, and is associated with discontinuous, curving, and anastomosing veins filled by the darkest and finest siltstone.

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