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By Oagile Dikinya

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47), n is determined by the orientation of the fractures, which reflects the effect of the orientation of the fractures on the fluid flow. r and b0 represent the size or the scale of the Stress/Strain-Dependent Properties of Hydraulic Conductivity for Fractured Rocks 25 fractures; they retrain the fluid flow through the fractures from their developing magnitude. W is a parameter introduced to show the impact of the connectivity of the fracture network on fluid flow. Finally, f(β) is a function used to demonstrate the coupling effect between fluid flow and stress state.

2 predict similar results and the predicted hydraulic conductivity is in the magnitude of 10−5 cm/s and close to in-situ hydraulic observations, but the anisotropy in hydraulic conductivity manifests due to non-uniform distribution of fractures. Compared with the hydraulic conductivity of the shallow rock mass, the predicted hydraulic conductivity for the rock mass in larger depth with the same fracture network decreases in 2 orders of magnitude due to the closure of the fractures applied by the in-situ stresses, but the anisotropic property of the hydraulic conductivity remains, which suggests that the occurrence of the fractures has a significant impact on permeability.

0°), the excavation-induced tangential hydraulic conductivity ratios, kθ/k0, predicted by our model are very close to the results presented in Liu et al. (1999). For radial hydraulic conductivity ratios, kr/k0, however, deviation occurs in the vicinity of the excavation. e. θ=90°). Clearly, these deviations are largely resulted from the facts that (1) Different strain distribution patterns are assumed in the elastic model in Liu et al. (1999) and in our elastoplastic model; (2) Different methods are used to compute the strain increments of fractures.

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