Add Journal to My Library
Geophysical Journal International
, Volume 213 (2) – May 1, 2018

7 pages

/lp/ou_press/effect-of-hydro-mechanical-coupling-on-natural-fracture-network-G0eFEXDtCB

- Publisher
- The Royal Astronomical Society
- Copyright
- © The Author(s) 2018. Published by Oxford University Press on behalf of The Royal Astronomical Society.
- ISSN
- 0956-540X
- eISSN
- 1365-246X
- D.O.I.
- 10.1093/gji/ggy028
- Publisher site
- See Article on Publisher Site

Summary In sedimentary basin context, numerous phenomena, depending on the geological time span, can result in natural fracture network formation. In this paper, fracture network and dynamic fracture spacing triggered by significant sedimentation rate are studied considering mode I fracture propagation using a coupled hydro-mechanical numerical methods. The focus is put on synthetic geological structure under a constant sedimentation rate on its top. This model contains vertical fracture network initially closed and homogeneously distributed. The fractures are modelled with cohesive zone model undergoing damage and the flow is described by Poiseuille’s law. The effect of the behaviour of the rock is studied and the analysis leads to a pattern of fracture network and fracture spacing in the geological layer. Fracture and flow, high-pressure behavior, Geomechanics, Numerical modelling, Sedimentary basin processes 1 INTRODUCTION Natural fracture network are widely spread in sedimentary basins and can occur in various context involving erosion, tectonic loading or a compaction disequilibrium due to significant sedimentation rate. Depending on the geological time span and the sedimentary basin history, numerous phenomena can lead to a decrease in horizontal effective stress and then gather favourable conditions to fracture onset. In basin modelling, the knowledge of fracturing processes enhances the description of overpressure history, which is a key issue to predict actual overpressures, the fluid content of the underground, the potential locations of hydrocarbon storage and the matrix equivalent permeability. The difficulty in fracture network modelling is to create realistic model due to the lack of subsurface data (Nelson 2001) and to handle the modelling of the complex physical phenomena involved. Previous papers have studied fracture network within sedimentary rock (Bai & Pollard 2000a; Becker & Gross 1996; Helgeson & Aydin 1991; Priest & Hudson 1976; Rozhko et al.2007) and fracture initiation and propagation (Simpson et al 2001; Vu et al.2017). Bai & Pollard (2000a) have shown that in the case of opening mode fracture, the normal stress between two neighbouring fractures can change from tensile to compressive depending on the critical ratio of the fracture spacing to layer thickness (approximately equal to 1). Nevertheless, outcrop’s observation shows ratio of the fracture spacing to layer thickness lower than this critical value (Ladeira & Price 1981; Bai & Pollard 2000b; Narr & Suppe 1991; Gross 1993). Thus, Bai & Pollard (2000a) called to mind other potential mechanisms such as overburden load and/or fluid pressure to explain closely spaced fractures at depth (Narr & Suppe 1991; Rives et al.1992; Becker & Gross 1996). In this paper, natural vertical opening-mode fracture network and dynamic fracture spacing induced by significant sedimentation rate are studied using a coupled hydro-mechanical simulator. Assumption of vertical fracture can be considered as a relevant hypothesis in our case of low ratio of horizontal total stress to vertical stress (Pollard & Aydin 1988; Guy et al.2010). A particular emphasis is put on a synthetic geological structure on which a constant sedimentation rate is imposed on its top. This synthetic geological structure contains vertical fracture network paths initially closed and homogeneously distributed. The Fractures are modelled with cohesive zone model undergoing damage and the flow in the fractures is described by Poiseuille’s law. The damage parameter affects both the mechanical and the hydraulic opening of the fracture as discussed by Ouraga et al. (2017). For the numerical simulations, the code Porofis based on finite element modelling (FEM) is used. In the following, the model and governing equations are briefly described and then the effect of hydro-mechanical parameters is studied to analyse fracture network and fracture spacing in sedimentary basins. 2 MODEL AND GOVERNING EQUATIONS One of the most important mechanisms involved in natural fracturing in sedimentary basins is the fluid overpressure (Luo & Vasseur 2002; Secor 1965; Mandl 2005). In a sedimentary basin, overpressures are generally due to mechanisms such as mechanical compaction, hydrocarbon maturation, or mineralogical reactions that produce additional pore pressure. Fracture onset occurs when the fluid pressure in a defect reaches the limit tensile strength of the porous media (Ouraga et al.2017; Fisher et al.1995). Numerous studies have given mechanical or hydraulic explanation for fracture network spacing (Bai & Pollard 2000a; Gross 1993; Hobbs 1967; Mandl 2005). Nevertheless, in sedimentary basins the coupling between hydraulic and mechanical processes is dominant (Engelder & Fisher 1994; Li et al.2012). Fracture network is studied from an equivalent model of a synthetic two layer model composed of a caprock formation with a low permeability over a highly permeable reservoir (Fig. 1). This equivalent model already considered for the modelling of single fracture propagation in sedimentary basins has been widely described in (Ouraga et al.2017). Thus, by considering that the permeability of the caprock formation is smaller than the permeability of the reservoir, under significant sedimentation rate, the flow from the reservoir to the sealing formation is low enough to represent a negligible part of the amount of fluid in the reservoir. The reservoir can thus be considered as undrained, and the pore pressure in this case reads to (Ouraga et al.2017) \begin{equation} p(t)=\frac{-b_r}{\frac{3(1-\nu _{r})K_{r}}{M_r(1+\nu _{r})}+b_r^2}\sigma _{v}, \end{equation} (1)where br, Mr, νr, Kr are respectively the Biot’s coefficient and modulus, Poisson’s coefficient and bulk modulus of the reservoir. σv(t) is the vertical stress that evolves linearly with time. In the present case to describe the deposit of sediments over time, this vertical stress is imposed on the top of the model and a constant sedimentation rate is assumed. The lower bound of the caprock is loaded with the pore pressure corresponding to the pressure within the reservoir (eq. 1). The pressure at the top of the model is taken as a reference pressure and the context is globally oedometric. It means that the vertical displacement of the basement and the horizontal displacement of the two lateral sides of this model are blocked. The principle to initiate fracture is that the low permeability of the caprock prevents overpressure dissipation under significant sedimentation rate (Osborne & Swarbrick 1997). This increase of pore pressure by hydro-mechanical coupling leads to an increase of horizontal total stress in the model and with a homogeneous medium does not allow to initiate fractures. Nevertheless, with a perturbation of pore pressure from abnormal conditions such as existing defect associated with a heterogeneity (Fig. 1a), fractures can be initiated. For the numerical simulation of fractures onset and their propagation, the caprock has a height of 20 m and extend over a length of 48 m. Cohesive joint elements initially closed are introduced into the mesh of the caprock on predetermined vertical paths, and corresponding to potential fracture propagation paths (Fig. 1b). It can be considered as a relevant hypothesis in the context of low horizontal total stress to vertical stress ratio. The space between the predetermined vertical paths is 4 m. Each cohesive joint element in the caprock formation is divided into two parts. The first part is the hydraulic defect. The hydraulic defect in this model is initially mechanically closed and represents the hydraulic perturbations resulting from material defects such as roots, shells or bioturbations, which can be inserted in the material during the sedimentation. This defect is around 1 m length and is very permeable with a dimensionless parameter $$\lambda =\frac{C_{f}\mu }{2 \pi k L}> 100$$ (with Cf the fracture’s conductivity, k the matrix permeability, and L the fracture’s length). In this framework, with a ratio of fracture conductivity to the matrix permeability λ > 100, the pressure is constant along the defect and equal to the pressure in the reservoir. In the second part of the cohesive zone, the parameter λ is closed to 0, which means that this part is initially inexistent for hydraulic computation. Mechanical and hydraulic parameters are chosen such that the initial fracture has no mechanical influence on numerical simulation until fracture initiation which is associated with the onset of damage in the joint. Figure 1. View largeDownload slide (a) Conceptual model and mechanical boundary conditions, (b) finite element method (FEM) numerical simulation model with several vertical predetermined fracture paths, $$\alpha =\frac{b}{\frac{3(1-\nu _{r})K_{r}}{M(1+\nu _{r})}+b^2}\sigma _{a}$$. Figure 1. View largeDownload slide (a) Conceptual model and mechanical boundary conditions, (b) finite element method (FEM) numerical simulation model with several vertical predetermined fracture paths, $$\alpha =\frac{b}{\frac{3(1-\nu _{r})K_{r}}{M(1+\nu _{r})}+b^2}\sigma _{a}$$. The caprock is considered as a porous medium. We assume that the fluid’s compressibility is very low (usual water properties are considered), the porous medium is isotropic, the skeleton transformations are infinitesimal, and the behaviour of the porous material is poroelastic. We also assume that the fluid saturates the pore volume of the media and the flow in the porous media is governed by Darcy’s law. As discussed by Coussy (2004) and considering the assumptions above, the governing equation describing the skeleton deformation and the motion of fluid is given by: \begin{equation} \frac{1}{M}\frac{\partial p}{\partial t}={\rm div}\left(\frac{k}{\mu }\nabla p\right)-b\frac{\partial \epsilon _{v}}{\partial t} \end{equation} (2)where M and b, ∇, εv represent respectively the Biot’s modulus, the Biot’s coefficient, the gradient operator and the volumetric strain given by the trace of the strain tensor. For the mechanical computation the main equations are the equilibrium equation $${\rm div}(\underline{\underline{\sigma }})=0$$, and the constitutive law of the medium. In this study, by considering the poroelastic behaviour, the total stress applied into the medium is \begin{equation} \underline{\underline{\sigma }}=\underline{\underline{\underline{\underline{C}}}}:\underline{\underline{\epsilon }}-bp\underline{\underline{I}}, \end{equation} (3)where $$\underline{\underline{\underline{\underline{C}}}}$$ represents the elasticity tensor, and $$\underline{\underline{\epsilon }}$$ is the strain tensor. Sign convention of continuum mechanics is used, stress and strain are positive in tension. The flow within the fracture is governed by the Poiseuille’s law and the conductivity of the fracture is given by the cubic law. From the mass balance within the fracture, the fluid exchange between the porous medium and the fracture, the hypothesis of continuity of pressure between two fractures surfaces and the Poiseuille’s law, the pressure along the fracture surface (Pouya 2012) reads \begin{equation} {\rm div}\left(c_{f}\nabla _{s}p\right)=\frac{e}{K_{f}}\frac{\partial p}{\partial t}+\left\Vert v \right\Vert .n+\frac{\partial e}{\partial t} \end{equation} (4)where e is the fracture’s aperture, ∇s the tangent gradient in the local tangent plane to the fracture, Cf the conductivity in the fracture and Kf the fluid compressibility. The velocity v can be discontinuous with the value v+, v− on the two sides of the fracture and the operator ‖.‖ represents a jump across the fracture. The damage of cohesive joint is coupled with elasticity using the equation below: \begin{equation} \underline{\sigma _{J}}=\left(1-D\right)\underline{\underline{R}}\underline{u}, \end{equation} (5)where $$\underline{\sigma _{J}}$$, D, $$\underline{\underline{R}}$$, are respectively effective stress vector, the damage variable, and the stiffness tensor of the fracture. The vector $$\underline{u}$$ is the relative displacement of the joint element, and represents the jump of discontinuity between the two side of the fracture. For the mechanical problem the node on the cohesive joint are splitted (Fig. 2), to allow displacement discontinuities across fractures while for the hydraulic problem it is not necessary because the pressure in our case is the same on the two sides of the fracture. On each side of the fracture, the displacement and the pressure of node are the same that in the matrix. The continuity of the pressure at matrix/fracture interface with the eq. (4) ensure the mass balance equation as explained by Pouya (2012). For the numerical computations the coupling between mechanical and hydraulic problems is performed with a sequential solving of the two problems and iteration between them. The sequential solving used here consists in solving the flow problem first through considering constant the total mean stress field. Once the flow problem is computed, the mechanical problem is solved by frozen the pressure in eqs (3) and (5) and the volumetric strain term in eq. (2) and the change of the fracture aperture in eq. (4) are computed explicitly (Kim et al.2010; Guy et al.2012). Figure 2. View largeDownload slide The mesh around the cohesive zone. Figure 2. View largeDownload slide The mesh around the cohesive zone. The evolution of the fracture is controlled by the failure criterion (Fig. 3) proposed by Pouya & Bemani (2015) and is defined as followed: \begin{equation} F\left(\tau ,\sigma _{n},D\right)=\tau ^2-\sigma _{n}^2{\rm tan}^2\varphi +2g\left(D\right)\sigma _{c}\sigma {n}-g^2\left(D\right)C^2 \end{equation} (6)where C represents the cohesion on intact cohesive fractures, τ, σn, φ are respectively the shear stress, the normal stress the friction angle and \begin{equation} \sigma _{c}=\frac{C^2+\sigma _{R}^2{\rm tan}^2\varphi }{2\sigma _{R}}, \end{equation} (7)with σR the limit tensile strength of the intact joints. This criterion depends on the damage and expressed the decohesion of the cohesive fracture under normal and shear stresses. It describes the transition from an intact cohesive fracture with cohesion and a tensile strength to a completely damage fracture with friction. As seen in Fig. 3, at the final stage of damage this failure criterion becomes identical to a Mohr Coulomb criterion with only a friction angle. The function g(D) in this failure criterion varies between 0 and 1, and controls the transition from intact to damage fracture. This function is obtained by using the consistency condition of the failure criterion and it is given by \begin{equation} g(D)=(1-D)(1-\beta ln(1-D)) \end{equation} (8)with D = 0, for an intact rock and g(D) = 1 and for completely damage fracture D = 1 and g(D) = 0. Figure 3. View largeDownload slide Evolution of the failure criterion from intact cohesive fracture to final damage fracture (Pouya & Bemani 2015) Figure 3. View largeDownload slide Evolution of the failure criterion from intact cohesive fracture to final damage fracture (Pouya & Bemani 2015) In this study, the evolution of the damage parameter affects also both the joint stiffness and the fracture aperture (Ouraga et al.2017). It depends on the relative elastic displacement limit of the cohesive fracture u0. Under a displacement u0 the damage D remains equal to zero and increases exponentially with the normal joint displacement un (Pouya & Bemani 2015) \begin{equation} D=1-e^{-\frac{\left(u_{n}-u_{0}\right)}{\beta u_{0}}} ,u_{n}\ge u_{0} \end{equation} (9)where β characterizes material ductility and varies in [0, ∞[. High β represents a ductile material on the contrary β = 0 represents a brittle material. 3 RESULTS AND DISCUSSION The numerical simulations have been carried out considering a ductile and a brittle caprock. The parameters shown in Table 1 are used for numerical fracture network initiation and propagation modelling. These parameters are realistic compared to data of poroelastic constant for water-saturated rocks (Atkinson & Meredith 1987; Touloukian et al.1989). In our modelling, the behaviour of the media is controlled by the parameter β (Pouya 2015) for fixed hydro-mechanical parameters and the results of the simulation are plotted in Fig. 4. This figure gives the evolution of pressure fields over time, and the evolution of the geometry of the fracture patterns. In Fig. 4(a), β = 5 and as discussed by Pouya & Bemani (2015) the caprock is clearly ductile, while in Fig. 4(b), β = 0.8 and the caprock behaviour is brittle. Fracture onset in the case of brittle media starts at 1.5 Myr after the sedimentation and the spacing between fractures is 4 m. This spacing corresponds to the predetermined fracture paths in the media. After the initiation, all fractures have an average length of about 1.5 m in both cases. This jump corresponds to the mechanical opening of the hydraulic defect (1 m) and a numerical perturbation in the hydro-mechanical coupling that converges during the computation. Once fractures are initiated the spacing between fractures and their propagation are controlled by the behaviour of the caprock. During the propagation, when the fracture length reaches a certain value, some fractures, one of every two fractures stop their propagation and begin to close. Thus the spacing between fractures propagating is multiplied by two. In the ductile caprock as seen in Fig. 4(a), one of every two fractures seems to close when the fracture length become close to their spacing. In the brittle one, fractures are closed later during their propagation (Fig. 4b). These results allow us to establish a link between the evolution of the spacing and the length of the active fractures depending on the caprock hydro-mechanical properties. The evolution of growing fracture length and the spacing between growing fractures over time are plotted in Fig. 5. Figure 4. View largeDownload slide Fractures propagation and pressure evolution in the case of a ductile caprock (a) and of a brittle caprock (b) Figure 4. View largeDownload slide Fractures propagation and pressure evolution in the case of a ductile caprock (a) and of a brittle caprock (b) Figure 5. View largeDownload slide Evolution of fracture’s length and of the average spacing between fractures in a ductile caprock (a) and in a brittle caprock (b) Figure 5. View largeDownload slide Evolution of fracture’s length and of the average spacing between fractures in a ductile caprock (a) and in a brittle caprock (b) Table 1. Input data for simulation. Property E (GPa) ν( − ) k(m2) β Caprock 10 0.23 10−21 m2 0.8 / 5 Reservoir 1 0.2 – – Overburden 200 m Myr−1 Fracture Rtt (GPa m−1) Rtt (GPa m−1) Rnt = Rtn (GPa m−1) σR (MPa) C (MPa) φ(°) 50 50 0 1 0.5 25 Property E (GPa) ν( − ) k(m2) β Caprock 10 0.23 10−21 m2 0.8 / 5 Reservoir 1 0.2 – – Overburden 200 m Myr−1 Fracture Rtt (GPa m−1) Rtt (GPa m−1) Rnt = Rtn (GPa m−1) σR (MPa) C (MPa) φ(°) 50 50 0 1 0.5 25 View Large In the ductile case (Fig. 5a) the spacing between the fractures evolves with their length. The Fig. 5(a) justifies the hypothesis made with the analysis of the Fig. 4. In fact, according the green and the blue curve, that respectively represent the active fracture length and the average of the spacing between fractures in Fig. 5(a), one of every two fracture fractures closes when the fracture length become close to their spacing. Graphically, we find this process when these two curves begin to collapse. On the contrary, in the brittle caprock (Fig. 5b) the fractures (one of every two fractures) begin to close when the ratio of fracture length to the spacing becomes clearly smaller than their length (Fig. 5b). As discussed by Bai & Pollard (2000b), these fractures are called closely spaced fractures. In this paper to explain closely spaced fractures, we have focused on the interaction and diffusion between fractures after the initiation (Fig. 6) and the behaviour of the caprock. In the Fig. 6, the pressure evolution for several periods of time is plotted in a cross section along the line AA΄ (refer to Fig. 4) of the caprock. This cross section is about at 1.5 m from the lower bound of the caprock. Figure 6. View largeDownload slide Pressure in a cross-section along the line AA’ (refer to Fig. 4) of the caprock for a ductile (a) and brittle (b) behaviour. Figure 6. View largeDownload slide Pressure in a cross-section along the line AA’ (refer to Fig. 4) of the caprock for a ductile (a) and brittle (b) behaviour. In this figure each peak of pressure corresponds to the pressure within the fracture in the ductile (Fig. 6a) and the brittle (Fig. 6b) caprock. The blue curve in Fig. 6 represents the pressure during fracture onset in both cases. In this curve the pressure within all fractures are identical and the effect of diffusion between fractures in the brittle case is not yet established 6(b). The time of fracture onset in this case is very smaller than that in the ductile caprock because, fractures initiate when the limit tensile strength is reached. On the contrary, with β = 5 the softening behaviour of the cohesive model leads to a delay in the propagation of fractures compared to the case of a brittle media, when the limit tensile strength is reached. In fact, the stress at the fracture tips in the ductile caprock must exceed the limit tensile stress to initiate and then to propagate fractures. Therefore, the brittle caprock fracture onset occur in a stress state less compressive than in the ductile case. Thus, the amount of fluid exchange and the flow between fracture and the matrix are small enough during the fracture initiation in the brittle caprock (see blue curves in Fig. 6) to not allow an increase of the pore pressure far from fractures that could be induced by a flow from fractures to the matrix. In the red curve in Fig. 6(b) the pressure within all fractures are still identical with a length equal to 10 m with a spacing of 4 m. As seen in this figure, the pressure between fractures in the brittle caprock does not vary much while in the ductile caprock considering the red and green curves refer to the Fig. 6(a) the pressure drops in some fractures and halts their propagation by hydromechanical effects. In the brittle caprock, the diffusion effect becomes significant later at around 0.1 Myr after fracture initiation (Figs 6 b and 4b), and fractures have a length of 16 m. Therefore, the diffusion drops the pressure within some fractures. They begin to feel the influence of the neighbouring fractures and a pressure gradient is created within some fractures. Therefore, with the hydro-mechanical coupling and the compressive stress state between the fractures, the propagation criterion is no longer respected and the lips of fractures begin to close (one of every two fractures), the spacing between fracture increases and we find the same interaction between fractures as in the ductile case. Hence, according our results by considering a very low permeability caprock and a significant sedimentation rate, in the brittle case, it is more likely to have closely spacing fractures than in ductile one due to the effects of hydro-mechanical coupling. These results can be used to explain the formation of fracture corridors, and some patterns of fracture network in the rock under a significant sedimentation rate. 4 CONCLUSION In this paper, we have studied the effect of hydro-mechanical coupling and the mechanical properties of the caprock on the pattern of fracture network and their spacing under significant sedimentation rate. In a ductile caprock the spacing between fracture evolves and can be compared with its length of propagation. One of every two fractures closes when the length of the fracture becomes larger than their spacing. In fact, the influence distance of a fracture on the neighbouring fractures is roughly equivalent to its length in this case. During fractures propagation, the diffusion between them and the hydro-mechanical coupling affects the network evolution. In the brittle caprock case some fractures start to close, only when the diffusion between fracture begin to establish. Therefore, closely spaced fracture network can be formed when the fracture length is larger than the spacing between fractures before the diffusion process between fractures becomes significant. This result can explain in-situ observation of closely spaced fractures (Bai & Pollard 2000b; Ladeira & Price 1981) and of some patterns of fracture network under significant sedimentation rate. Finally, our modelling method and our cohesive fracture model can be considered as relevant to compute natural fracture network under sedimentation in a realistic context in single-phase fluid flow. The case of double-phase fluid flow could be integrated in an extended version of this model. Acknowledgements This work was funded by IFP Energies Nouvelles research program. The data for this paper are available by contacting the corresponding authors at zady.ouraga@ifpen.fr REFERENCES Atkinson B.K., Meredith P.G., 1987. Experimental fracture mechanics data for rocks and mineral, in Fracture Mechanics of Rock , pp. 477– 525, ed. Atkinson B.K., Academic Press. Google Scholar CrossRef Search ADS Bai T., Pollard D.D., 2000a. Fracture spacing in layered rocks: a new explanation based on the stress transition, J. Struct. Geol. , 22, 43– 57. Google Scholar CrossRef Search ADS Bai T., Pollard D.D., 2000b. Closely spaced fractures in layered rocks: initiation mechanism and propagation kinematics, J. Struct. Geol. , 22, 1409– 1425. Google Scholar CrossRef Search ADS Becker A., Gross M.R., 1996. Mechanism for joint saturation in mechanically layered rocks: an example from southern Israel, Tectonophysics , 257, 223– 237. Google Scholar CrossRef Search ADS Coussy O., 2004. Poromechanics , John Wiley & Sons Ltd. Engelder T., Fisher M.P., 1994. Influence of poroelastic behavior on the magnitude of minimum horizontal stress, Sh, in overpressure parts of sedimentary basins, Geology , 22, 946– 952. Fisher M.P., Gross M.R., Engelder T., Greenfield T., 1995. Finite-element analysis of the stress distribution around a pressurized crack in a layered elastic medium: implication for the spacing of fluid driven joint in bedded sedimentary rock, Tectonophysics , 247, 49– 64. Google Scholar CrossRef Search ADS Gross M.R., 1993. The origin and spacing of cross joint: example from Monterey Formation, Santa Barbara Coastline, California, J. Struct. Geol. , 15, 737– 751. Google Scholar CrossRef Search ADS Guy N., Seyedi D., Hild F., 2010. Hydro-mechanical model of geological CO2 storage and the study of possible caprock fracture mechanisms, Georisk , 4( 3), 110– 117. Guy N., Enchery G. GR., 2012. Numerical modeling of thermal EOR: comprehensive coupling of an AMR-based model of thermal fluid flow and geomechanics, Oil , 67( 6), 1019– 1027. Helgeson D.E., Aydin A., 1991. Characteristics of joint propagation across layer interface in sedimentary rocks, J. Struct. Geol. , 13( 8), 897– 911. Google Scholar CrossRef Search ADS Hobbs D.W. 1967. The formation of tension joint in sedimentary rocks: an explanation, Geol. Mag. , 104, 550– 556. Google Scholar CrossRef Search ADS Kim J., Tchelepi H., Juanes R., 2010. Stability accuracy and efficiency of sequential methods for coupled flow and geomechanics, in SPE Reservoir Simulation Symposium , The Woodlands, TX. Ladeira F.L., Price N.J., 1981. Relationship between fracture spacing and bed thickness., J. Struct. Geol. , 3, 179– 183. Google Scholar CrossRef Search ADS Li C.L., Tang C.A., Wang S.Y., 2012. A numerical investigation of fracture infilling and spacing in layered rocks subjected to hydro-mechanical loading, Rock Mech. Rock Eng. , 45, 753– 765. Luo X., Vasseur G., 2002. Natural hydraulic cracking: Numerical model and sensitivity study, Earth planet. Sci. Lett. , 201, 431– 446. Google Scholar CrossRef Search ADS Mandl G., 2005. Rocks Joint: The Mechanical Genesis , Springer, Heidelberg, pp. 27– 48. Narr W., Suppe J., 1991. Joint spacing in sedimentary rocks, J. Struct. Geol. , 13, 1037– 1048. Google Scholar CrossRef Search ADS Nelson R.A. 2001. Geological Analysis of Naturally Fractured Reservoir , 2nd edn, Gulf Professional Publishing. Osborne M., Swarbrick R., 1997. Mechanisms for generating overpressure in sedimentary basins, AAPG Bull. , 81, 1023– 1041. Ouraga Z., Guy N., Pouya A., 2017. Modeling of natural fracture initiation and propagation in basin sedimentation context, J. geophys. Res. , 122, 247– 261. Google Scholar CrossRef Search ADS Pollard D.D., Aydin A., 1988. Progress in understanding joint over the past century, Bull. geol. Soc. Am. , 100, 1181– 1204. Google Scholar CrossRef Search ADS Pouya A., 2012. Three-dimensional flow in fractured porous media: a potential solution based on singular integral equations, Adv. Water Resour. , 35, 30– 40. Google Scholar CrossRef Search ADS Pouya A., 2015. A finite element method for modeling coupled flow and deformation in porous fractured media, Int. J. Numer. Anal. Methods Geomech. , 39, 1836– 1852. Google Scholar CrossRef Search ADS Pouya A., Bemani Y., 2015. A damage-plasticity model for cohesive fractures, Int. J. Rock Mech. Min. Sci. , 73, 194– 202. Priest S., Hudson J.A., 1976. Discontinuity spacing in rocks, Int. J. Rock Mech. Min. Sci. , 13, 135– 148. Google Scholar CrossRef Search ADS Rives T., Razack M., Petti J.P., Rawnsley K., 1992. Joint spacing: analogue and numerical simulations, J. Struct. Geol. , 14, 925– 937. Google Scholar CrossRef Search ADS Rozhko A., Podladchikov Y., Renard F., 2007. Failure patterns caused by localized rise in pore-fluid overpressure and effective strength of rocks, Geophys. Res. Lett. , 34, L22,304, doi:10.1029/2007GL031696. Google Scholar CrossRef Search ADS Secor D., 1965. Role of fluid pressure in jointing, Am. J. Sci. , 263, 633– 646. Google Scholar CrossRef Search ADS Simpson G., Guéguen Y., Schneider F., 2001. Permeability enhancement due to microcrack dilantacy in the damage regime, J. geophys. Res. , 106, 3999– 4016. Google Scholar CrossRef Search ADS Touloukian Y.S., Judd W.R., Roy R.F., 1989. Physical Properties of Rocks and Minerals , Hemisphere. Vu M.N., Nguyen S.T., To Q.D., Dao N.H., 2017. Theoretical predicting of permeability evolution in damaged rock under compressive stress, Geophys. J. Int. , 209 ( 2), 1352– 1361. © The Author(s) 2018. Published by Oxford University Press on behalf of The Royal Astronomical Society.

Geophysical Journal International – Oxford University Press

**Published: ** May 1, 2018

Loading...

personal research library

It’s your single place to instantly

**discover** and **read** the research

that matters to you.

Enjoy **affordable access** to

over 12 million articles from more than

**10,000 peer-reviewed journals**.

All for just $49/month

Read as many articles as you need. **Full articles** with original layout, charts and figures. Read **online**, from anywhere.

Keep up with your field with **Personalized Recommendations** and **Follow Journals** to get automatic updates.

It’s easy to organize your research with our built-in **tools**.

Read from thousands of the leading scholarly journals from *SpringerNature*, *Elsevier*, *Wiley-Blackwell*, *Oxford University Press* and more.

All the latest content is available, no embargo periods.

## “Hi guys, I cannot tell you how much I love this resource. Incredible. I really believe you've hit the nail on the head with this site in regards to solving the research-purchase issue.”

Daniel C.

## “Whoa! It’s like Spotify but for academic articles.”

@Phil_Robichaud

## “I must say, @deepdyve is a fabulous solution to the independent researcher's problem of #access to #information.”

@deepthiw

## “My last article couldn't be possible without the platform @deepdyve that makes journal papers cheaper.”

@JoseServera

- Read unlimited articles
- Personalized recommendations
- No expiration
- Print 20 pages per month
- 20% off on PDF purchases
- Organize your research
- Get updates on your journals and topic searches

**$49/month**

Start Free Trial

14-day Free Trial

Best Deal — 39% off
### Annual Plan

- All the features of the Professional Plan, but for
**39% off**! - Billed annually
- No expiration
- For the normal price of 10 articles elsewhere, you get one full year of unlimited access to articles.

~~$588~~

**$360/year**

Start Free Trial

14-day Free Trial

Read and print from thousands of top scholarly journals.

System error. Please try again!

or

By signing up, you agree to DeepDyve’s Terms of Service and Privacy Policy.

Already have an account? Log in

Bookmark this article. You can see your Bookmarks on your DeepDyve Library.

To save an article, **log in** first, or **sign up** for a DeepDyve account if you don’t already have one.