By H. C. Heard, I. Y. Borg, N. L. Carter, C. B. Raleigh
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Published by way of the yank Geophysical Union as a part of the Geophysical Monograph Series.
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Extra info for Flow and Fracture of Rocks
16 PLASTICITY OF SYNTHETIC QUARTZ CRYSTALS 15 10 Fig. 6. Stress-strain curves for the crystal W4 loaded at 3-kb confining pressure at various temperatures. The strain rate is 10' sec 1 ; the orientation is O. may be accentuated by the fact that the temperature is near the hydrolytic weakening temperature. This strong dependence of mechanical properties on strain rate apparently explains, at least in part, why some of the stress-strain behavior reported here was not observed in crystals of high OH content by Heard and Carter , who initially loaded their specimens rapidly before continued straining at 10' sec'.
Of = p, ± (Eh/2R) (2) where Do,, is the differential axial compressive prestress, p, is the confining pressure, and R is the radius of curvature. The bending stress is tensile (negative) in the uppermost fibers and compressive in the lowermost ones. When a fiber stress reaches the breaking strength or the yield stress of the material, further deformation of the fold is inelastic, and a physical instability arises, the nature of which depends on the rheology of the material. This rheology in turn is intimately related to the mechanisms of inelastic deformation.
In the inflection region (location c) the axes form a girdle around the fold axis. 3. At the crest of the anticline (location d) at the uppermost fiber the axes are strongly oriented parallel to the fold axis. A composite diagram at d and g (from Figures 19 and 20) yields a girdle parallel to the axial plane of the Copyright American Geophysical Union Geophysical Monograph Series Flow and Fracture of Rocks Vol. 16 HANDIN ET AL. 21 anticline. Minor concentrations in both d and g are oriented east-west, parallel to the direction of axial shortening.
Flow and Fracture of Rocks by H. C. Heard, I. Y. Borg, N. L. Carter, C. B. Raleigh