Abstract
Abstract Viscous components in Jura folding due to pressure solution include discrete stylolites in limestones and diffuse flowage, particularly viscous folding, in Triassic anhydrites. Though increase of equilibrium solubility on the boundary of the stressed solid is well understood, the kinetic aspects of transport of the solute by diffusion and the movement of pore water are not known quantitatively and can be assessed only qualitatively on the basis of observations in nature and laboratory experiments. Apparently the creation of secondary tectonic pore space — macroscopic shear and tension joints in limestones and microscopic dilatancy cracks in anhydrite — is essential; it is possibly the rate-determining process. Stylolites in limestones, though ubiquitous, are quantitatively negligible, the overwhelming mass transport having occurred along discrete surfaces of failure. Flow of anhydrite, on the other hand, has been essential for basal decollement and cushioning under the folds.
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