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1995, International Journal of Rock Mechanics and Mining Sciences & Geomechanics Abstracts
Veins formed in a variety of rock types and tectonic environments were measured at seven field locations to determine a general scaling relationship between the length and opening displacement (aperture). For these naturally formed extension fractures displacement-length profiles for both single-and multiplesegment veins display centrally located maxima and gently tapered displacement gradients at the tips. This geometry is consistent with elastic-plastic crack growth models, which also predict linear scaling between length and displacement. The geometry is used to estimate stresses of formation for the veins. Length-maximum displacement plots for single-segment fractures show data clustered along linear trends. Similar plots for multiple-segment fractures show greater scatter and are marginally better fit by a square root function than by a line. The geometries of multiple-segment veins are consistent with elastic models for crack-tip stress interactions. Aspect ratios for single-segment fracture sets vary between 1 x 1~ 3 and 8 x 10 -`3 , consistent with tensional fracture strengths roughly an order of magnitude lower than compressive shear strengths implied by shear displacement-length ratios recorded for faults, which are about 10 2.
Journal of Structural Geology, 2008
Displacement-length data from faults, joints, veins, igneous dikes, shear deformation bands, and compaction bands define two groups. The first group, having a power-law scaling relation with a slope of n ¼ 1 and therefore a linear dependence of maximum displacement and discontinuity length (D max ¼ gL), comprises faults and shear (non-compactional or non-dilational) deformation bands. These shearingmode structures, having shearing strains that predominate over volumetric strains across them, grow under conditions of constant driving stress, with the magnitude of near-tip stress on the same order as the rock's yield strength in shear. The second group, having a power-law scaling relation with a slope of n ¼ 0.5 and therefore a dependence of maximum displacement on the square root of discontinuity length (D max ¼ aL 0.5 ), comprises joints, veins, igneous dikes, cataclastic deformation bands, and compaction bands. These opening-and closing-mode structures grow under conditions of constant fracture toughness, implying significant amplification of near-tip stress within a zone of small-scale yielding at the discontinuity tip. Volumetric changes accommodated by grain fragmentation, and thus control of propagation by the rock's fracture toughness, are associated with scaling of predominantly dilational and compactional structures with an exponent of n ¼ 0.5.
Journal of Structural Geology, 2000
Journal of Geophysical Research, 2003
1] Observations of natural fracture dimensions have sparked a continuing debate as to the nature of the fundamental relationship between fracture aperture (maximum opening) and length. On the basis of theoretical fracture mechanics, some have argued aperture-tolength scaling should be linear. This relationship implies that all fractures in a given population have the same driving stress regardless of fracture length, arguably a state that is difficult to reconcile with fracture propagation criteria. Also, some field observations indicate sublinear aperture-to-length scaling that is apparently inconsistent with the linear elastic fracture mechanics theory. In this work, a nonlinear aperture-to-length relationship is derived, still based on linear elastic fracture mechanics in a homogeneous body, but incorporating subcritical and critical (equilibrium law) fracture propagation criteria. The new hypothesis postulates that fractures of different lengths preserved in a body of rock are all in the same condition with respect to propagation (i.e., they all have the same stress intensity factor). This requires that fractures have driving stresses that vary inversely with the square root of fracture length, producing fracture apertures that scale with length to the 1/2 power. Under these conditions, fracture aspect ratio (aperture/length) decreases with increasing fracture length to the negative 1/2 power. Linear aperture-to-length scaling is still considered a possibility but is attributed to a relaxed, postpropagation mechanical state. Deviations in fracture aperture-to-length relationships from these idealized models can result from mechanical fracture interaction, fracture segmentation into en echelon arrays, and three dimensional effects in stratabound fractures.
Journal of Structural Geology, 1992
Abstraet--A plane strain model for a fault is presented that takes into account the inelastic deformation involved in fault growth. The model requires that the stresses at the tip of the fault never exceed the shear strength of the surrounding rock. This is achieved by taking into account a zone, around the perimeter of the fault surface, where the fault is not well developed, and in which sliding involves frictional work in excess of that required for sliding on the fully developed fault. The displacement profiles predicted by the fault model taper out gradually towards the tip of the fault and compare well with observed displacement profiles on faults. Using this model it is found that both (1) the shape of the displacement profile, and (2) the ratio of maximum displacement to fault length are a function of the shear strength of the rock in which the fault forms. For the case of a fault loaded by a constant remote stress, the displacement is linearly related to the length of the fault and the constant of proportionality depends on the shear strength of the surrounding rock normalized by its shear modulus. Using data from faults in different tectonic regions and rock types, the in situ strength of intact rock surrounding a fault is calculated to be on the order of 100 MPa (or a few kilobars). These estimates exceed, by perhaps a factor of 10, the strength of a well developed fault and thus provide an upper bound for the shear strength of the crust. It is also shown that the work required to propagate a fault scales with fault length. This result can explain the observation that the fracture energy calculated for earthquake ruptures and natural faults are several orders of magnitude greater than that for fractures in laboratory experiments.
International Journal of Rock Mechanics and Mining Sciences, 2000
Several aspects of fracture arrays are reviewed brie¯y and discussed. The terminology applied to progressive or multi-stage brittle deformation in rock masses is improved by noting fundamental mechanical dierences in fracture type and the kinematic coupling between dilatant mixed-mode crack displacements and wing cracks developed at the fracture tips. An array of initially mixed-mode (I±II) cracks will evolve under remote tensile least principal stress and with increasing strain to a dilatant, mode-I crack array oriented approximately perpendicular to the remote tensile stress. This progressive fracture growth thus defeats predictions of fracture-set orientation and displacement based only on a Mohr circle estimate of initial elastic stress (valid in the rock mass only at the earliest stages of fracture nucleation). Slow, subcritical crack growth in rock is associated with distinctive changes in fracture population geometry, as shown by published numerical simulations of fracture±network evolution. An increase in the stress corrosion index promotes joint clustering and signi®cant changes in joint length±frequency that may lead to characteristic dierences in the statistics of large-strain fracture populations. These geometric clues can be used to re®ne estimates of strength and deformability of rock masses and to infer classes of physico-chemical processes acting at the fracture tips during the development of the fracture population.
International Journal of Rock Mechanics and Mining Sciences & Geomechanics Abstracts, 1995
Journal of Structural Geology, 2018
Whatever the processes involved in the natural fracture development in the subsurface, fracture patterns are often affected by the local stress field during propagation. This homogeneous or heterogeneous local stress field can be of mechanical and/or tectonic origin. In this contribution, we focus on the fracture-pattern development where active faults perturb the stress field, and are affected by fluid pressure and sliding friction along the faults. We analyse and geomechanically model two fractured outcrops in UK (Nash Point) and in France (Les Matelles). We demonstrate that the observed local radial joint pattern is best explained by local fluid pressure along the faults and that observed fracture pattern can only be reproduced when fault friction is very low (µ < 0.2). Additionally, in the case of sub-vertical faults, we emphasize that the far field horizontal stress ratio does not affect stress trajectories, or fracture patterns, unless fault normal displacement (dilation or contraction) is relatively large.
Earth and Planetary Science Letters, 2011
a b s t r a c t Editor: T.M. Harrison Keywords: fracture network 4D analog experiments fractal
Journal of Structural Geology, 2006
This work is a 2D numerical contribution to the problem of fault and fracture interaction in layered rocks, focusing on fracture aperture. We investigate the influence of an underlying normal fault on the aperture of open fractures in bonded multilayers submitted to vertical shortening and horizontal lengthening. The tests are carried out using the finite element code Franc 2D under plane strain conditions. It is first shown that the presence of a straight normal fault affects the aperture of the above fractures. The fractures located in two very local areas near the upper tip of the fault, one in the hanging wall and one in the footwall, tend to open, whereas the neighboring fractures tend to close. The increases in aperture are systematically greater in the footwall than in the hanging wall. Furthermore, the two areas with increased fracture aperture move towards the footwall when the dip of the fault increases. Second, the case of more complex underlying faults with restraining/releasing bends is studied. These models have similar results to those observed in the case of the straight underlying fault, with two areas of increased fracture aperture. The increases in fracture aperture are comparable with the case of the straight fault in the hanging wall, but are larger in the footwall. The contrasting behaviors of fractures described in the experiments are interpreted as a consequence of changes in the stress field in the central fractured layer caused by the presence of the underlying fault. They may provide a guide to explain fluid flow in fault tip areas. Finally, the case of fracture corridors (swarms of closely spaced fractures) is addressed. It is shown that, whatever the characteristics of the underlying fault, the total aperture of a corridor formed by three equally spaced fractures is equal to 1.41-1.69 times the aperture of a single fracture located at the same place in the fractured layer. This strongly suggests that these structures may act as preferential geological drains, with important consequences in terms of fluid flow. q
Geological Society, London, Special Publications, 2005
Statistical properties of crack-seal veins are investigated with a view to assessing stress release fluctuations in crustal rocks. Crack-seal patterns correspond to sets of successive parallel fractures that are assumed to have propagated by a subcritical crack mechanism in the presence of a reactive fluid. They represent a time-sequence record of an aseismic and anelastic process of rock deformation. The statistical characteristics of several crack-seal patterns containing several hundreds of successive cracks have been studied. Samples were collected in three different areas, gold-bearing quartz veins from Abitibi in Canada, serpentine veins from the San Andreas system in California and calcite veins from the Apennine Mountains in Italy. Digitized pictures acquired from thin sections allow accurate measurement of crack-seal growth increments. All the samples show the same statistical behaviour regardless of their geological origin. The crack-seal statistical properties are describ...
2005
Abstract Fracture and vein patterns in the brittle crust of the Earth contain information on the stress and strain field during deformation. Natural examples of fracture and vein patterns can have complex geometries including combinations of extension and conjugate shear fractures. Examples are conjugate joint systems that are oriented with a small angle to the principal stress axis and veins that show an oblique opening direction.
Journal of structural geology, 1983
2001
A statistical view of fracture extension apertures and amplitudes in rocks is presented. We show that both the aperture and amplitude of fractures possess a log-logistic distribution. It is found that this distribution is applicable equally to open and mineralized fractures. The physical implications of this point are discussed.
Journal of Structural Geology, 2011
In this paper, we describe an outcrop to characterize the effect of fracture spacing and type on larger scale effective elasticity, which is measured for the first time in-situ with a Schmidt hammer. The outcrop is dominated by lime mudstones and belongs to the deformation zone of the St Clément fault, in southern France. Our results suggest that small spacing of faults, open fractures and styolites leads to lesser effective Young's modulus, whereas small sealed fracture spacing leads to greater effective Young's modulus. These relationships are compatible with theoretical models of effective elasticity. Using Amadei and Savage (1993) approach, we define a non-linear model that relates Schmidt hammer rebound to spacing by fracture type. A hemisphere with a radius of 40 to w200 cm is the rheological volume characterized by the Schmidt hammer. Results of model inversion demonstrate that variations of Schmidt hammer rebound over the outcrop can be used to estimate fracture type and stiffness. Stiffness of sealed fractures is 2e3 orders of magnitude greater than the stiffness of faults, stylolites and open fractures. This result is consistent with an increase of the rate of interseismic stress build-up of major faults with sealing of fractures in their damage zone.
Physical Review Letters, 1996
Fault-fracture patterns have been studied in slabs of clay during extensional deformations. Fractures nucleate and grow on many scales. A new scaling relation is proposed for the length l of a fracture as a function of the area l ϳ A b , with the same exponent b 0.68 6 0.03 for many deformation types. A consequence of this scaling relation is that the width of a fracture scales with the length as w ϳ l ͑12b͒͞b . A spring network model is shown to reproduce the pattern, both visually and statistically, with the same scaling exponents. [S0031-9007(96)
SEG Technical Program Expanded Abstracts 1993, 1993
Shear-wave splitting in sedimentary basins and above small earthquakes in a wide range of geological and tectonic domains typically displays evidence for azimuthal shear-wave velocity anisotropy of between 1% and 5%. Interpreted as the effects of parallel vertical fractures, microcracks, and preferentially oriented pore-space, these percentages of anisotropy are equivalent to crack densities of = 0.01 and 0.05 with normalized mean crack diameters of 0.43 and 0.74, respectively. The only exceptions are percentages of anisotropy exceeding 10% > 0.1) observed in near-surface rocks where there is pronounced jointing.
2007
9.3.8 Interpretation of Z Fractures……………………………………689 9.3.9 Stratigraphy and the Spatial Arrangement of Opening-mode Fractures…………………………………………………...……690 x x 9.4. Data Sets………………………………………………………….……694 9.4.1 Fracture Categories in Rock Samples…………………………..694 9.4.2 Quantitative Characterization…………………………..………696 9.4.3 Layer 1 at Escalera Canyon (Escalera 1) ………………………701 9.4.4 Layer 2 at Escalera Canyon (Escalera 2) ………………………721 9.4.5 Layer 3 at Escalera Canyon (Escalera 3) ………………………733 9.4.6 Layer OO1 at Escalera Canyon (Escalera OO1) …….…………737 9.4.7 Layer OO12 at Escalera Canyon (Escalera OO12) ….…………751
Journal of Structural Geology, 2000
Spacings of opening-mode fractures (joints and veins) in layered sedimentary rocks often scale with the layer thickness. Field observations reveal that the ratio of fracture spacing to the thickness of the fractured layer, S/T f , ranges from less than 0.1 to greater than 10. There is a critical spacing to layer thickness ratio that de®nes the condition of fracture saturation, and explains the observed spacing ratios between 0.8 and 1.2. Values of S/T f > 1.2 are explained as the results of the fracturing process having not reached the saturation level. To explain ratios of S/T f < 0.8, we study the possibility for further fracture in®lling, by considering¯aw distributions between adjacent fractures loaded by extension of the layer. Results show that in®lling fractures grow more easily from¯aws located near the interface than from those in the middle of the fractured layer. The propagation of a¯aw located in the middle of the fractured layer is unstable, but for the¯aw to propagate toward the interfaces, its height has to be greater than a critical size. This critical size decreases with increasing S/T f. The propagation behavior of a¯aw with one of its tips at the interface depends on S/T f. The propagation is unstable when S/T f is greater than a critical value. When S/T f is less than this critical value, the propagation is ®rst unstable, then stable, and then unstable again. An in®lling fracture can cut through the fractured layer only if S/T f is greater than another critical value, otherwise the in®lling fracture can only partially cut the fractured layer. For models with the same elastic constants for the fractured layer and the neighboring layers, this critical value is 0.546, and the minimum spacing to layer thickness ratio of fractures formed by the in ®lling process under extension is 0.273.
2015
A statistical view of fracture extension apertures and amplitudes in rocks is presented. We show that both the aperture and amplitude of fractures possess a log-logistic distribution. It is found that this distribution is applicable equally to open and mineralized fractures. The physical implications of this point are discussed. 1
Proceedings of the 3rd Unconventional Resources Technology Conference, 2015
In this paper, we discuss an approach that utilizes microseimicity associated with hydraulic fracture stimulations to characterize the evolution of deformation over time and the behavior of the rock mass. In applying these concepts through examples we look at moving beyond conventional static interpretations to reveal processes that play important roles in the dynamic expansion of a fracture network. Here, we introduce a parameterization that considers the diffusivity of the observed microseismicity that can be related to the ease in which the inelastic seismic deformation field can diffuse (Difusivity Index), the degree of deformation for a given stress and therefore the susceptibility of a rock mass to fracturing (Fracability Index), and the Seismic Efficiency, which is related to the energy budget of the failure process as related to the presence of fluids as opposed to stress-induced failures. Based on our observations, we suggest that Fracability Index can be used to identify regions of deformation and high stress associated with potential barriers to flow. Further, heterogeneity in the Diffusivity Index can be related to the advancement of the frac whereas Seismic Efficiency is a good indicator of stimulation extent, defining differences between stress induced and fluid induced fracturing. Our observations suggest that these dynamic parameters can be used to characterize the dynamic growth of fracture networks and assess design stimulation effectiveness.
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