Corresponding author: A. Neuville, Advanced Material and Complex System group, Department of Physics, University of Oslo, PO Box 1048, Blindern, Oslo 0316, Norway. (email@example.com)
 The characteristics of the hydro-thermal flow which occurs when a cold fluid is injected into a hot fractured bedrock depend on the morphology of the fracture. We consider a sharp triangular asperity, invariant in one direction, perturbing an otherwise flat fracture. We investigate its influence on the macroscopic hydraulic transmissivity and heat transfer efficiency, at fixed low Reynolds number. In this study, numerical simulations are done with a coupled lattice Boltzmann method that solves both the complete Navier-Stokes and advection-diffusion equations in three dimensions. The results are compared with those obtained under lubrication approximations which rely on many hypotheses and neglect the three-dimensional (3-D) effects. The lubrication results are obtained by analytically solving the Stokes equation and a two-dimensional (integrated over the thickness) advection-diffusion equation. We use a lattice Boltzmann method with a double distribution (for mass and energy transport) on hypercubic and cubic lattices. Beyond some critical slope for the boundaries, the velocity profile is observed to be far from a quadratic profile in the vicinity of the sharp asperity: the fluid within the triangular asperity is quasi-static. We find that taking account of both the 3-D effects and the cooling of the rock, are important for the thermal exchange. Neglecting these effects with lubrication approximations results in overestimating the heat exchange efficiency. The evolution of the temperature over time, toward steady state, also shows complex behavior: some sites alternately reheat and cool down several times, making it difficult to forecast the extracted heat.
 Conductive and convective transport of heat or chemical species, is omnipresent in Earth sciences [Stephansson et al., 2004; Steefel et al., 2005], within porous or fractured media. Some technologies related to chemical transport, like radioactive storage [Cvetkovic et al., 2004; Amaziane et al., 2008; Halecky et al., 2011; Hoteit et al., 2004] or well acidizing requires a good resolution of advection-diffusion of chemical concentration [Szymczak and Ladd, 2009; Cardenas et al., 2007]. The transport is influenced by the temperature which may play a role by modifying (1) the fluid transport—notably by natural convection, (2) the chemical constants of the reactions, or (3) the geometry of the porous medium. For instance, some chemical reactions or rheological rock transformations only occur in given ranges of temperature (e.g., decarbonation, dehydration of sediments, decomposition of kerogen [e.g., Mollo et al., 2011; Petersen et al., 2010]). Thermal fracturing can result from chemical reactions generating gas [Kobchenko et al., 2011], from thermal stress [Lan et al., 2013; Bergbauer et al., 1998], or from hydro-thermal stress, when injecting hot or cold fluid into a rock. Temperature monitoring is, for example, necessary to prevent potential damages of well installations. Apart from fracturing processes, other changes of geometry of the porous medium can also occur during injection of cold or warm fluid in Enhanced Geothermal Systems (EGS) because of poroelastic effects [Gelet et al., 2012] and also because of chemical reactions like acidizing. Exploitation of EGS requires also the heat exchange to be efficient and durable. An important step is, therefore, to understand the hydro-thermal coupling between fluid and rock; this is the aim of our present modeling.
 Hydraulic transport mostly occurs in fractures. It was shown under lubrication approximations and steady state conditions, that the complexity of the fracture topography influences the hydrothermal exchange when a cold fluid is injected into a hot fractured bedrock [Neuville et al., 2010]. More specifically, the lubrication approximations state that the aperture and its wall topographies vary smoothly so that the velocity field is parallel to the main plane of the fracture (the component of the hydraulic flow perpendicular to the main fracture plane is neglected), and that the thermal diffusion only occurs in the directions perpendicular to the main plane of the fracture. For this modeling, the rock temperature was also supposed to be constant. In other models, as, e.g., in the study of Natarajan and Kumar , the heat diffusion in the rock is considered, but with a simplified fluid flow. Some features which are observed in nature, like fluid recirculation and time-dependent temperature at the pumping well, can, however, not be explained with this model. We, therefore, wish to go beyond this lubrication assumption and be especially able to observe effects due to highly variable morphology of the fluid-rock interface. Indeed, even if many fluid-rock interface topographies or fracture apertures are statistically self-affine (multi-scale property) [Brown and Scholz, 1985; Bouchaud, 1997; Neuville et al., 2012; Candela et al., 2009], it is very often possible to observe some isolated asperities with sharp variations of the topography, for instance, along cleavage planes [Neuville et al., 2012] or due to particle detachment, or along stylolite teeth [Renard et al., 2004; Ebner et al., 2010; Koehn et al., 2012; Laronne Ben-Itzhak et al., 2012; Rolland et al., 2012]. The roughness of the fracture can also be perturbed by intersections with other fractures [Nenna and Aydin, 2011] or, for microfractures, by the matrix porosity [Renard et al., 2009].
 Investigations on the validity of the lubrication approximation, based on the study of some geometrical parameters have been performed, e.g., by Zimmerman and Bodvarsson ; Oron and Berkowitz ; and Nicholl et al. . Without the lubrication approximation, i.e., with full solving of the Navier-Stokes equation, the hydraulic behavior in channels or fracture with sinusoidal walls were studied, e.g., by Brown et al. ; Waite et al. ; and Bernabé and Olson  with lattice gas methods. It was shown that for a sinusoid with a short wavelength and large amplitude compared to the mean aperture, the hydraulic aperture is smaller than that expected with the lubrication approximation. Errors on the hydraulic aperture, computed with a lubrication approximation, have been analytically obtained by Zimmerman and Bodvarsson  and experimentally by Oron and Berkowitz ; and Nicholl et al. . In these studies, the fluid flow was reported to be important in the middle of the channel, while it is quasi-stagnant in the sharp hollows of the walls. Eddies were numerically observed in this quasi-stagnant zones [Brown et al., 1995; Brush and Thomson, 2003; Boutt et al., 2006; Cardenas et al., 2007; Andrade Jr. et al., 2004] in various fracture geometries, including realistic fracture geometries. These eddies are similar to those analytically predicted by Moffatt , who studied eddies formation in a corner between two intersecting planes, when the flow is imposed to be tangential to the planes at an infinite distance from the corner. Microfluidics has also been investigated using lattice Boltzmann methods (LBM) [e.g., Harting et al.2010].
 On the one hand, many studies exist about the coupling between the fully solved hydraulic behavior—solving of the Navier-Stokes equation—and solute or particle transport, or dispersion in general [Boutt et al., 2006; Cardenas et al., 2007; Drazer and Koplik, 2001, 2002; Flekkøy, 1993; Yeo, 2001; Johnsen et al., 2006; Niebling et al., 2010; Vinningland et al., 2012].
 On the other hand, few studies take into account the fully solved hydraulic flow with the heat transfer, when a cold fluid is injected into a fracture embedded in a hot solid. In the absence of flow, the stationary problem of heat transport across a fractal interface was studied, e.g., by Grebenkov et al. . Even if both heat and solute transport are described with advection-diffusion equation, many differences exist due to different boundary conditions and different range of parameters. Andrade Jr. et al.  solved the temperature field when a warm fluid is injected within a two-dimensional (2-D) channel delimited by walls whose topographies follow Koch fractals, using the “Semi-Implicit Method for Pressure Linked Equations” algorithm developed by Patankar . In his study, the walls of the channel were, however, set at a constant temperature. Other studies regarding cooling issues of electrical devices have also been done [e.g., Young and Vafai, 1998 and references therein], but in contrast to the current study, the thermal boundary conditions used in these works are less relevant for natural problems (for instance, insulated walls are used). Another branch of algorithms for heat solving are based on lattice Boltzmann methods (LBM). The LBM [e.g., Wolf-Gladrow, 2005] are very suitable to model the complexity of hydrothermal transport in a rough fracture morphology, whatever the slopes of the morphology (i.e., without any conditions on the smoothness of the morphology). As the algorithms require only local operations (while other numerical methods requires, e.g., inversion of matrices depending on the geometry of the entire porous medium), they handle complex boundaries very well. Several methods have been proposed: multispeed scheme (a density distribution is used, with additional speeds and high order velocity terms in the equilibrium distribution), hybrid method (hydraulic flow is solved with LBM, and heat transport is solved with another method), and double distribution. A review of these methods can be found in Lallemand and Luo ; and Luan et al. . Most of the problems solved so far with LBM deal with benchmarks that consist in close systems (square cavity with impermeable walls). In this paper we will examine the limits of the lubrication approximation and the model developed in Neuville et al. . After briefly recalling the fundamentals of this model, we describe the numerical methods used for our modeling outside the lubrication approximations. We chose a LBM with a double distribution method, where the hydraulic flow is independent of the temperature. The chosen lattices for the flow and temperature variables are respectively hypercubic and cubic, with a single lattice speed for each lattice. This choice is seldom used in literature, but it is suitable for three-dimensional (3-D) mass and heat transport modeling [d'Humières et al., 1986; Wolf-Gladrow, 2005; Hiorth et al., 2008]. Despite the methods being implemented in 3-D, for simplicity reasons, the parameter exploration is done in two dimensions, translational invariance being assumed along the third dimension. For a self-affine aperture, the contribution of each asperity on the total hydraulic and thermal exchanges is difficult to single out. For this reason, here we chose as a simpler situation to focus on one single asperity. We can thus lead a precise quantitative study of the flow organization and properties in space and time as function of flow speed, asperity size and shape, and heat transport properties.
 We will thus explore the behavior of the flow in a fracture with a triangular asperity, as function of the asperity size. We will compare the results directly to the lubrication approximation results and establish when this one fails to model correctly the mass and heat transport.
2 Methods for Hydrothermal Modeling
2.1 Solving Under Lubrication Approximations
 The lubrication approximation holds in the laminar regime, at small Reynolds number, for fluids flowing into a fracture whose aperture and both wall topographies show smooth variations. Under these assumption, the Navier-Stokes equation reduces to the Reynolds equation [Pinkus and Sternlicht, 1961; Brown, 1987]:
where ∇p is the local 2-D pressure gradient, and a(x,y) is the fracture aperture. With (unitary vector) as the direction of the macroscopic pressure gradient, the velocity expresses as
where z1and z2are the out of plane coordinates of the fracture walls related to the aperture by z2−z1=a, and ηis the dynamic viscosity of the fluid. The aperture of a fracture a is partially characterized by its mean geometrical aperture, A, and by the standard deviation of the aperture. The hydraulic behavior can be partially characterized by the flow across the aperture, q, defined as
The hydraulic aperture H is classically defined [Guyon et al., 2001] from the component of q along the macroscopic gradient direction, qx:
where F is the norm macroscopic pressure gradient, and 〈.〉 refers to the x−y space averaging. For parallel plates geometry, qis a constant vector and H=A. The thermal behavior of a fluid injected in a fracture (with a self-affine aperture) embedded in a constantly warm rock was modeled in Neuville et al., [2010, 2011] under the so-called thermal lubrication approximation. In their solving, several terms are discarded in the heat equation: for instance, the conduction occurs only perpendicularly to the fracture mean plane (z), and the convection is neglected along z. The thermal exchange balance in a stationary regime resumes in
where χf is the thermal diffusivity of the fluid, is the Nusselt number, classically used to evaluate the thermal efficiency in reference with the conductive heat flow, and
is a temperature averaged across the aperture, weighted by the velocity. For a parallel plates geometry, it can be shown, under assumptions over the temperature gradient, that Nu=70/17 [Turcotte and Schubert, 2002; Neuville et al., 2010]. In this method, the temperature profile across the aperture follows a quartic law. It was shown [Neuville et al., 2010] that for a self-affine aperture, the averaged temperature law over the ydirection, , defined as
can be approximated by
where is imposed at the inlet of the fracture, Tr is the temperature of the wall (interface fluid-solid), and R is a thermal length, obtained from a linear regression. For parallel plates separated by A0, and Tr fixed, R is equal to
Note that any change of the thermal length can also be interpreted in terms of Nusselt number variation.
2.2 Full Solving, Using Coupled Lattice Boltzmann Methods (LBM)
2.2.1 Solving the Mass Transport with FCHC LBM
 In LBM, fictitious particles move and collide on a lattice. Operations conserve mass and momentum at mesoscopic scale. Using appropriate rules and lattice topology, it can be shown that the Navier-Stokes equation can be recovered at macroscopic scale [e.g., Rothman and Zaleski, 1997; Chopard and Droz, 1998; Wolf-Gladrow, 2005]. The distribution of mass density is denoted as fi, where the index i refers to the direction of propagation of the particles moving with a velocity ci on the lattice. We choose a “Face-Centered-Hypercubic” (FCHC) lattice. This is a four-dimensional lattice with suitable topological properties to solve the Navier-Stokes equation [d'Humières et al., 1986] in three dimensions. The N=24 vectors defining the lattice directions are , (0,±1,±1,0), (0,0,±1,±1), (0,±1,0,±1), (±1,0,±1,0), (±1,0,0,±1), with , where δt and δx are the time and space steps, respectively. The total density and the macroscopic velocity u at each node M are computed with (OM being the position vector):
 For the collision phase, a standard BGK scheme (Bhatnagar, Gross, and Krook, [Bhatnagar et al., 1954; Qian et al., 1992]) is used. The linearized collision term depends on a constant of relaxation λ, which is linked to ν=η/ρ the kinematic viscosity of the fluid [Rothman and Zaleski, 1997] by
The macroscopic pressure gradient between the inlet and outlet of the fracture is implemented through a volumetric force that intervenes during the collision phase at each lattice node.
 It can be shown that the density of the fluid is linked to the velocity by p=ρ(δx2/(2(δt)2)−u2/4) [Rothman and Zaleski, 1997]. This modeling of Navier-Stokes equation holds for compressible flows in the incompressibility limit, at small Mach number (ratio between the velocity and the sound speed on the lattice—here, equal to ). The Knudsen number (ratio between the average distance between two collisions and the macroscopic scale of the system) should also be small.
2.2.2 Solving the Heat Transport With 3-D Cubic LBM
 The transport of the heat is solved using a coupled lattice Boltzmann method, using a second particle distribution, gi, which represents the internal energy distribution of the particles moving with the velocity bi. It is assumed that the heat is passively transported by the fluid: viscous heat dissipation is neglected, as well as the viscosity dependence with the temperature. Using square lattices and appropriate collision rules, it has been shown [Wolf-Gladrow, 2005; Hiorth et al., 2008] that the LBM solves advection-diffusion equation. The internal energy and its flux are conserved during the collision phase, which is done with a BGK scheme, exactly as in, e.g., Hiorth et al. . We choose a 3-D cubic lattice. Its NT=6 base vectors, , are defined by (±1,0,0), (0,±1,0), (0,0,±1), and b=δx/δt. This network is a sublattice of the 3-D projection, perpendicularly to fourth direction, of the FCHC lattice. The temperature at each node M and the internal energy flux are given by
2.2.3 LBM Boundary Conditions
 Let us consider a fractured medium, where the macroscopic pressure gradient in the fluid is aligned with the direction: the fluid is injected at the inlet (x=0) and pumped out at the outlet of the system (x=Lx). The unitary vectors , , and define an orthonormal frame, and this porous medium is discretized with a cubic mesh. The center of each mesh is a fluid or a solid node.
 The porous medium geometry and the flow are supposed to be periodic in x and y. At the interface between the fluid and the solid, non-slip boundary condition are chosen. This is implemented using the full-way bounce-back boundary condition [Rothman and Zaleski, 1997] for the mass particle distributions. This bounce-back operation is done for particle distributions fi(OM), where M is a solid node, and OM+ciδtis in the fluid. For these nodes, the mass distributions fi of the bounced-back nodes are exchanged with fi+12, where the direction i+12 is opposite to the direction i. This is done instead of a collision operation. The propagation phase is then done normally on these nodes. For this bounce-back boundary condition, the interface fluid-solid is supposed to be located half-way between the bounced-back node and the fluid nodes (Figure 1).
 The temperature field is supposed to be periodic along y direction. The temperature is imposed in x=0, z=0, and z=Lz, where Lz is the height of our system in the z direction. In this study, the rock is maintained at temperature at the borders in z=Lz and z=0. At the inlet of the system, in x=0, the rock and fluid are maintained respectively at , and . At the outlet of the system, the temperature is forced to at solid nodes (Dirichlet condition), and T(x=Lx)=T(x=Lx−δx) in liquid (von Neumann condition). In our program, the temperature at these nodes is imposed through an “equilibrium scheme” [Huang et al., 2011]: at the end of each time step and at the next collision step, the distributions giof these boundary nodes are set at the next collision step to the equilibrium distribution , computed with the desired temperature. For the nodes located at the outlet in the fluid, our boundary condition is equivalent, at first order, to zero temperature gradient along the xdirection. The considered systems are long enough so that the beginning of the systems is almost not influenced by outlet conditions (this boundary condition only creates a local artifact at the outlet). At the initial time, the rock and fluid have a temperature of respectively and .
3 Geometry and Hydrothermal Regime Studied
 We focus on the hydrothermal behavior within a fracture with a very simple geometry: it is a fracture with flat walls parallel to the x−yplane, perturbed by a single asperity with sharp edges (Figure 2). The fracture aperture a(x) is invariable along the ydirection. In cross-view (x−zplane), the asperity has a triangle shape characterized by its width L, depth d, and abscissa position x0:
where Λis the unitary triangle function:
 For all the computations done with LBM in this study, the fracture is embedded in a solid whose dimension are (Lx,Lz)=(200 mm,89.5 mm). This medium can be completely seen in Figure 4a. The bottom wall of the fracture intersects the x−z plane in z=39.75 mm, and the asperity is characterized by (A0,x0)=(10 mm,5 mm) while d and L vary. The lattice discretization is δx=0.5 mm and δt=0.1250 s.
 The LBM simulations are done at low Reynolds number: Re=0.17, where it is computed as Re=2AuM/(3ν) with uMbeing the maximum velocity within a flat fracture separated by two parallel plates, of aperture A0, estimated from the classical cubic law [Guyon et al., 2001].
 For the thermal parameters, two different thermal diffusivity values are used in LBM for the fluid and the solid. The ratio of both χf/χr=0.17 corresponds to the typical ratio of diffusivity values for crystalline rocks (of order of 1 mm2/s [Drury, 1987]) and water (at 100°C, 0.17 mm2/s, [Taine and Petit, 2003]). The Péclet number, defined as Pe=uMA/χfis set to 45.96. The orders of magnitude of Reynolds and Péclet numbers that we use are compatible with the lubrication approximations.
4 Results: Example of Application
4.1 Illustration of the Hydraulic Behavior
4.1.1 Hydraulic Lubrication Approximation for a Triangular Asperity
 The lubrication velocity is computed using equation (2). For an aperture which is invariant along y, the Reynolds equation (1) simplifies to
and the hydraulic flow is constant:
where K is a constant. By integrating the pressure gradient between the inlet and outlet of the fracture, one gets
where Fis the pressure gradient imposed between the inlet and outlet of the fracture. K is calculated analytically for the considered geometry (equation (13)), by noticing that:
4.1.2 Fully Resolved Hydraulic Behavior Compared to the Lubrication Approximation
 Let us first comment on the precision of the lattice Boltzmann (LB) results. We have some errors that come from the chosen implementation of the boundary conditions combined to the type of LBM. Because the fluid is slightly compressible with LBM, the averaged flow qx is not constant (the relative standard deviation of qxis 0.39% for the geometry in Figure 2b), and, therefore, the hydraulic aperture slightly varies according to the x domain where it is computed. We chose to compute H at the asperity scale, i.e., for x0≤x≤x0+L. For the case of a parallel flat wall fracture separated by A0=10 mm, with a flow characterized by Re=0.17, solved with steps δx=0.5 mm, and δt=0.125 s, the absolute error on the computed velocity, defined as is 5.3610−4 mm/s. The relative error, defined as is 3.22%. The relative error on the hydraulic aperture computed in this case is 1.11%. In order to take into account this numerical error, the comparison between LB and lubrication results is done using normalized hydraulic apertures. The hydraulic aperture obtained from the LBM calculation and the one obtained from the lubrication approximation are respectively normalized in this way and . and are the hydraulic apertures in parallel plate geometry, computed respectively with the LBM (discretized aperture) and with the lubrication approximation. We note also an error on the direction of the velocity vectors in the deepest part of the corner, for velocity vectors whose norm are of order 10−5 mm/s, i.e., very low velocity compared to the average velocity (see Figure 2). In the zones where artifacts at very low velocities were observed, the thermal exchange is mainly led by diffusive exchanges. Therefore, we believe that the error in the direction does not influence much the thermal exchange. Note that lattice Boltzmann methods with better precision are also available, like those with a modified equilibrium distribution [He and Luo, 1997] or those with two relaxation times [e.g., Talon et al., 2012].
 Figure 2a shows the velocity norm under lubrication approximation (cross-section view), for a fracture with an asperity characterized by (d,L)=(20 mm,50 mm). This has to be compared with Figure 2b, which shows the velocity norm and vectors at steady state across the fracture aperture, computed with the LBM. The difference of the velocity norms is in addition shown in Figure 3a. In this configuration, the fluid flows within the asperity and the main flow direction changes gently in accordance with the topography of the walls. The velocity field fully resolved and the one solved with the lubrication approximation show some similarities. However, some details are not captured with the lubrication approximation, notably in the deepest part of the corner where the full computation locally shows fluid at rest. It is computed that and for the geometry shown in Figure 2a, with (d,L)=(20 mm,50 mm). Those values only differ by 1.15%, i.e., the lubrication approximation still holds on average.
 Let us depart further from the smooth geometry where the lubrication assumptions apply. The same geometry as previously is used, but L is set to L=10 mm, so that the geometry has a steeper topography. Similarly to Figures 2a and 2b, Figures 2c and 2d, respectively show the lubrication and fully resolved velocity fields. Here it is very clear that both are very different (see also Figure 3b). In the asperity, a separation zone is observed: fluid velocities are very small, and Figure 2e shows that the fluid recirculates as if being trapped. The velocity profile is consequently very different from a quadratic profile as in equation (2). For the geometry shown in Figures 2c and 2d, (d,L)=(20 mm,10 mm), it is computed that and . Therefore, it means that macroscopically the lubrication approximation is still a good estimation is this case. It is however clear that locally, within the asperity, the lubrication approximation is not valid.
 Fractures with a bump (asperity with d<0) that reduces the aperture are also investigated. Figures 2f and 2g show the lubrication and fully resolved velocity fields. The main differences are the two small separation zones with low velocities that appear just before and after the bump (Figure 3c), in the corners with obtuse angles. This small asperity reduces the hydraulic aperture of 3.0%, with and .
4.2 Illustration of the Thermal Behavior
4.2.1 Thermal Lubrication Approximation for a Triangular Asperity
 For an aperture which is invariant along y, the hydraulic flow q is constant (equation (16)), and . By assuming that the rock temperature Tris constant, equation (5) simplifies into a first-order linear ordinary differential equation with constant coefficients, which has for solution (in a stationary regime) the following:
For the considered geometry (equation (13)), can be computed analytically and expressed as a function of R (equation (9)). The solution is
This solution is shown in plot (a) of Figure 5 and plots (a', b', c') of Figure 6, where as a function of x is plotted for several geometries. Within the lubrication approximation, the slope of as a function of x (equation (20)) is the same before and after the asperity, (i.e., for x≤x0 and for x≥x0+L), and it is given by 1/R, where R is defined in the lubrication regime with equation (9), q being computed from equations. (16) to (18). Both straight lines have however different ordinates at the origin. This comes from the complicated behavior within the asperity zone. As a consequence, the fit of with a single straight line, following equation (8), clearly does not capture the details of the thermal exchange. In Figure 6, plot (e), the linear fits done for the restricted range 0≤x≤55 mm (in the vicinity of the inlet) are shown. The negative inverse of the slope of these fits is named R1lub(reported values in Table 1), and it can be compared to the R values. For hollow asperities (d>0), R1lub>R. It means that, according to this solution, the heat exchange efficiency is reduced around the corner, compared to the heat exchange efficiency far from the corner. On the contrary, for bumps d<0, R1lub<R. The linear fit of the second part (far from the inlet), for 55≤x≤150 mm, results in a thermal length R2lub analytically always equal to R. Indeed, since x0 and Lvalues fulfill, by choice, x0+L≤55 mm, this second fit is systematically done after the asperity.
Table 1. Thermal Lengths Obtained for Various Triangular Geometries, Obtained From Equation (9) (for R) and From the Fits of the Curves a
Cf. Figures 5 and 6. Subscripts 1 and 2 refer to the range of values where the fit has been done (x≤55 mm and 55≤x≤150 mm). “flat wr” and “flat nr” stand for flat geometry with and without rock temperature variation, respectively.
4.2.2 Fully Resolved Thermal Behavior Compared to the Lubrication Approximation
 In this section, we first comment qualitatively on the maps of the temperature obtained with LBM for few different asperities in a stationary regime. The comparison to the lubrication approximation is then done quantitatively using average temperatures curves, from which thermal lengths are computed. The transient regime is also discussed at the end of this subsection.
 Figure 4 shows the temperature map at steady state corresponding to the hydraulic behavior illustrated in Figure 2. The shape of the isotherm lines within the fluid are strongly correlated with the hydraulic flow. For (d,L)=(20 mm,50 mm), the cold fluid is clearly advected into the asperity. On the contrary, for (d,L)=(20 mm,10 mm), the deepest part of the asperity is not affected by the injection of the cold fluid (very low velocities in this separated flow zone), and it heats up fast by conduction. As a consequence, the fluid within this second fracture is warmer (e.g., compare isolines T=80°C in Figures 4a and 4b). For the narrower fracture, Figure 4c, with (d,L)=(−5 mm,5 mm), the reduction of the hydraulic flow (and , respectively for (d,L)=(−5 mm,5 mm) and (d,L)=(20 mm,50 mm)) inhibits the propagation of the cold fluid. This fluid consequently heats up in a shorter distance (better conductive transport) than for the two other cases. The rock cools down by conduction: the wall temperature is inferior to the rock temperature at the border of the system (150°C), especially where the rock is surrounded by cold fluid, for instance in Figure 4c, at (x,z)=(10 mm,45 mm).
 The thermal behavior is now quantified in the same way as that in Neuville et al., [2010, 2011], i.e., by computing (Figure 5) as in equation (6). For reference, we first look at the results obtained in a fracture with flat parallel walls. Figure 5, plot a shows obtained with lubrication approximation: it is a straight line with a slope , with mm. This result is compared to a LB simulation performed with an imposed constant temperature rock—i.e., only the fluid temperature is computed. This plot (Figure 5, plot b) can be very well approximated with a single straight line of slope , where mm. This value is higher than , i.e., the thermal exchange is worse than expected from the lubrication approximation. In the lubrication approximation, the in-plane diffusion in the fluid is neglected. The difference between and means that the in-plane diffusion tends to inhibit the heat exchange.
 Then, we relax the hypothesis of constant rock temperature and look at the effect of the heat diffusion in the rock: the LB solving is done both in the rock and fluid. Two definitions of are proposed. The first way is to compute it as (Figure 5, plot c). In this expression, the cooling down of the rock intervenes only indirectly through its influence on . This plot is close to a linear plot with slope , where mm (fit performed for x≤55 mm). This value is much higher than and : it shows that the temperature evolution of the rock reduces by more than a factor 2 of the heat efficiency. The second way of defining takes into account the variability of the bottom wall temperature, Tr, which is computed as Tr(x)=T(x,z=39.5 mm). This definition of (Figure 5, plot d) emphasizes the dynamic of the fluid temperature compared to the wall temperature. Contrary to plots (a–c), plot (d) of Figure 5 is not a straight line. The beginning of this plot (for x≤55 mm) is approximated by a linear fit of slope , where mm. The concave curvature of plot (d) of Figure 5 around x=55 mm, however, attests a change of thermal regime. The second part of the curve is fitted with a straight line of slope , where mm. By choosing the Péclet number equal to 45.96, there is a good agreement between the thermal lengths and . Doing so, we have a reference case where the lubrication assumptions holds for the computation of the average temperature in the vicinity of the inlet of the fracture. The Péclet number significantly influences the agreement between and values. At higher values (e.g., Pe=500), the thermal lubrication approximation clearly loose its validity. Further in the fracture, the thermal length R2 is higher than : the thermal exchange efficiency between the wall and the fluid is lower than around the injection zone. This change of regime is not predicted by the lubrication approximation and does not appear with an imposed wall temperature. Here the rock temperature Tr evolves over time and is not anymore uniform at stationary regime along the fracture: this spatial variability leads to a spatial change of regime in the fluid temperature.
 Hereafter, the average temperature in LB simulations is computed with the second definition (i.e., using the space variable wall temperature Tr(x)=T(x,z=39.5 mm)), for other geometries (Figure 6). The full resolution solving plots (a, b, and c) are compared to the lubrication approximation (a', b', c'). In general, the lubrication approximation gives very different results, especially for large x. For negative d values (bumps), the LB computation shows that the temperature behavior changes at the abscissa corresponding to the edge of the corner (x0+L/2). Within the lubrication, it is possible, by adapting R in equation (20), to obtain a similar behavior for x<x0+L/2, but the change of slope in x=x0+L/2 cannot be modeled in this way, as attested by the poor quality of the fit shown in plot (d) of Figure 6. This change of slope might be linked to the change of the hydraulic flow, also occurring around the corner edge and not predicted by the lubrication approximation. For positive d values (hollow asperity), the corner geometry causes smoother variations in the slope of , than expected with the lubrication approximation. The incomplete modeling of the heat diffusion artificially implies sharper temperature variations. Some similarities in the variations have, however, been observed, notably for the highest values of (d,L) (e.g., Figure 6, plots b, b', and b”, close to the injection zone (x≤55 mm), providing that the thermal length is adjusted (32.3 mm instead of 46.2 mm for (d,L)=(20 mm,50 mm)).
 The quantification of the thermal behavior is done in the same way as previously (cf.4.2.1). Two thermal lengths R1 and R2 are defined by approximating with two linear fits on two x ranges. R1and R2 (reported in Table 1) respectively characterizes the thermal behavior in the vicinity and far from the injection zone, (i.e., for x≤55 mm and 55≤x≤150 mm). These values are commented in section. 5. The limit of 55 mm corresponds to the change of behavior observed with the flat fracture in LB (Figure 5, plot d). The range x≤55 mm also systematically includes the asperity: the temperature estimate in x=55 mm somehow reflects what would be observed by a temperature probe located there, investigating at the integrated effect of the morphology.
 The temperature of the fluid and rock evolves over time (Figure 7). First the fluid warms up, for instance at points b, c, e, h of Figure 7, whose temperature evolution is shown on plots b, c, e, and h in Figure 8. On the contrary, the points in the rock, which are close to the fluid, cool down fast (plots a and f in Figure 8). With a slower dynamic (intermediate time scale), the heat source maintaining the system borders at a hot temperature provides a heat flux that diffuses toward the walls (plots a and f in Figure 8), which causes their temperature to increase again. The temperature at points located far enough from the fluid (d, g), does not change as fast at early times; points (d, g) simply cool down in a monotonic way. Similar variations are observed for a flat fracture. The sudden slow down of the heating process of points e and h (around 2000 and 4000 s), located after the asperity can however specifically be attributed to the asperity (see for comparison, plot e-flat, obtained in a flat geometry). This variation is not observed at points (b) and (c), located in the fluid, close to the injection zone. Finally the temperature field decreases everywhere at larger time scales, and the system seems to reach a steady state. The variation of the temperature field over time is complex, as two points close to each other may have different variations. Some points reheat and cool down alternately several times, which makes it difficult to forecast the extracted heat.
5 Results: Exploration of the Parameter Space
5.1 Hydraulic Aperture and Thermal Length Computation
 Exploration of the parameter space for d and L and their influence on the hydraulic aperture and the thermal length has been investigated. Figure 9a shows a color map of the normalized hydraulic aperture as a function of d and L. For d>0 (channel larger than A0with a hollow asperity), the permeability increases compared to a flat channel of aperture A0, as . For d<0 (channel narrower than A0 with a bump), the opposite behavior is observed . It is possible to divide the map in three areas that can be approximately separated with two straight lines. For d>0.4L(black dashed line), the hydraulic aperture for a given width L tends to be constant (vertical isolines on Figure 9a) whatever the depth d of the asperity is. On the contrary, for d<0.2L (black dash-dotted line), the hydraulic aperture tends to be constant for a given d (horizontal isolines). Among the explored β angles (defined as arctan(2d/L), in the range 0<β≤360°, not exhaustively explored), these limits correspond to the angles β<103° (d>0.4L) and β>136° (d<0.2L). This last limit angle is of the same order as the one obtained by Moffatt , whose study was done using slightly different flow assumptions. He showed that even at vanishing Reynolds number, eddies form in a corner between two intersecting planes when the angle exceeds 146°, when a shear flow is imposed far away from the corner. The presence of eddies is well supported in our case by almost zero velocity values and/or negative velocities observed in the middle of the corner (see Figure 2e). The flow in the corner is very small, almost separated from the main flow; it thus does not contribute significantly to the hydraulic flow.
 Figure 9b shows a map of the thermal lengths R1 (obtained from LB computation for range x≤55 mm), normalized by (constant value) as a function of d and L values. For any geometry with d>0 (hollow asperities), the thermal exchange around the asperity is inhibited compared to that within a flat fracture (). For d<0, the thermal exchange is, on the contrary, better (). For geometry with angle β>136° (d<0.2L), for a given depth d, R1 shows few variations. For the range 55≤x≤150 mm, the thermal length R2 was also computed. R2 is on average 2.3 times higher than : the thermal exchange is far less efficient than it is close to the injection zone. Far from the injection zone, the thermal exchange also does not vary much with the geometry. Indeed, on average, , with a standard deviation of 0.04).
5.2 Comparison to the Lubrication Approximation
 It is questionable if our parameter study may be compared to the results obtained in Neuville et al. . This latest study focused on the hydraulic aperture and thermal length obtained for self-affine fractures under lubrication approximation, using the analysis exposed in section 2.1. By contrast with the current study, the aperture studied in Neuville et al.  is self-affine, which means that using the Fourier decomposition, it is decomposed in , where k is the wave vector and scales as for k≠0. For such aperture, it was shown in Neuville et al.  that the hydraulic and thermal behavior can mostly be deduced from the highest wave lengths of the aperture. For a flat aperture perturbed with an isolated triangular shape, the situation is very different. Its power spectrum at the largest length scales not only depends on the triangular asperity shape, but also depends on the length of the flat area before and after the asperity. For a given pressure gradient, performing statistics (like calculating the hydraulic aperture, mean aperture, and standard deviation) at the asperity scale or over the full fracture scale provides very different results. We clearly see that HLB/A is dominated by the range where it is calculated and is therefore difficult to be compared with the values obtained under lubrication in Neuville et al. . For this reason, we compared (Figure 10) the hydraulic aperture to the one obtained under lubrication approximation , defined as done in section 4.1.2.
 Figure 10a shows the hydraulic aperture under lubrication . It can be noticed that the isoline shapes differ from that shown in Figure 9a: the hydraulic aperture computed under lubrication approximation evolves smoothly for a constant depth d or width L. It is also not possible to delimit the different zones separated by the straight lines as done for the LBM computation in section 5.1.
 Figure 10b shows . This ratio is always very close to 1, with a systematic characteristic: . It means that the hydraulic flow is very slightly overestimated with the lubrication approximation. However, it should be kept in mind that the hydraulic aperture only reflects an averaged permeability and not the local flow differences. We will now see if these local differences may be seen through the thermal behavior.
 Figure 11a shows a map of the thermal lengths R1, normalized by R1lub, which also varies with the geometry, as a function of d and L values. The domain can be separated in two. First, the geometries where R1/R1lub<1: for these geometries, the thermal exchange is actually better than expected from the lubrication approximation. These geometries correspond to asperities which are deep and large enough. This can be explained by the fact that the lubrication approximation does not take into account the local reduction of the hydraulic flow within the corner, which diminishes the convective heat transport and therefore favorites a better local heating up, by conduction. Second, the domain where R1/R1lub>1: for these geometries, the thermal exchange is not as good as expected from the lubrication approximation. Note that for the geometries with d<0, R1 is overestimated, as it is obtained from a fit done for x≤55 mm, while a change of regime occurs in the middle of the asperity (the thermal exchange is observed to be less efficient for x≥x0+L/2). Far from the inlet (Figure 11b), the lubrication approximation overestimates the heat exchange efficiency.
6 Discussion and Conclusion
 Our hydraulic results are coherent with literature: quasi-stagnant fluid is observed in the corners with small βangles. For the studied corner geometry, the hydraulic aperture obtained with the full resolution, although not very different, is systematically smaller than the one obtained with lubrication assumptions. Compared to fractures with parallel flat walls, the hydraulic aperture is systematically higher for the fractures with the triangular hollows and smaller for bump asperities: this is completely expected as the aperture is clearly either increased or reduced. For the asperities with β angle superior to 136°, the hydraulic aperture depends almost only on the depth of the asperities, while for β angle inferior to 103°, the hydraulic aperture depends almost only on the width of the asperities. The fluid trapped in deep asperities does not mix easily with the main flow. In order to mix better this trapped fluid and prevent stagnant fluid, it could be interesting to stimulate the system with oscillating pressure gradients. The oscillating frequency should be smaller than the diffusion time in the corner, i.e., smaller than d2/ν.
 For the heat exchange, we notice that the deep part of the corner, although insignificant in terms of hydraulic flux contribution, changes the heat exchange. Compared to fractures with parallel flat walls, the heat efficiency is systematically worse (factor 1 to 1.4) for the studied fractures with hollow asperities and better for the bumpy ones (factor 0.7 to 1). The hydraulic aperture only depends on the width of the asperity for β<103°. This feature is not recovered for the thermal lengths: this shows that the thermal exchange is even more dependent on the geometry shape than the hydraulic behavior. The fluid trapped in the corner is mostly sensitive to heat diffusive processes whose time scale depends on and , where df is the distance to the well-flowing fluid, and diis the distance to the fluid-rock interface. It means that the deepest point in the corner, which is in contact with the warm rock, transmits the heat of the rock to the main flowing fluid at latest after Δt=d2/χf, where d is the depth of the corner. When the main flow penetrates deeper in the corner, the distance between the flowing fluid and warm wall is reduced: we may think that this transfer time is reduced. This is, however, not necessarily true, since the volume of fluid trapped in the corner, as well as the surface of exchange (fluid-rock interface) also change and modify the heat exchange. For instance, very deep and thin asperities transmit very efficiently the heat from the rock. It is important to note that the temperature efficiency can, however, not be directly linked neither to the volume of the asperity nor to the ratio of the volume and surface of exchange. Another important parameter is the distance ds between the heat source and the fluid-rock interface: the variations of the wall temperature are sensitive to both time scales and . If both time scales are of the same order, the temperature fluctuates quickly and is very sensitive to local heterogeneities. On the field, it is very likely that ds>>df: the diffusion process transports the heat through long distances in the rock. This will bring slower dynamic in the temperature variation. Local temperature heterogeneities due to complex geometry of fracture will however still behave as local sources (cooler or warmer sites than the surroundings) and create short time scale variations. The forecast of pumped water temperature should therefore not rely on simple parameters, but should really take into account the geometry of the porous medium. The diffusive exchange is important not only in the corner but also more generally close to the fluid-rock interface, where the velocity is low. The advective heat transfer mostly occurs in the middle of the channel, where the velocity is high; this transfer is characterized by time scales of the order of Lx/u. In order to better mix the fluid between the zones where the advective process is efficient and those where the diffusive process occurs, it would be interesting to introduce some tortuosity in the fracture (with a typical length scale of the order of χf/u), or to stimulate the system by oscillating the pressure gradient with a time scale smaller than . The oscillations may locally introduce changes of direction of the flow and transverse velocity components, which may very efficiently mix the fluid. The computed thermal lengths can be associated to heat efficiencies. The heat exchange efficiency may also be defined in other ways, by computing the difference of the total energy flux between the inlet and outlet of the fluid.
 The full resolution of the temperature field computed with the lattice Boltzmann method shows that the heat efficiency evolves with the distance to the inlet of the fracture. This evolution can be attributed both to the asperity and the cooling of the rock. Two thermal lengths were therefore defined to evaluate the heat efficiency. Far enough from the inlet, the thermal lengths obtained with lubrication approximation are underestimated (of a factor 2.2 to 3.2-Figure 11b), which means that the heat efficiency is overestimated. Close to the injection point, the efficiency is either underestimated or overestimated, depending on the shape of the asperity. For deep and thin asperities, as well as rather flat asperities (asperities with small volume) and bump asperities, the thermal exchange efficiency is underestimated with the lubrication approximation of a factor 1 to 1.6. It is otherwise slightly overestimated (factor 0.7 to 1).
 The time variations of the heating and cooling of the fluid and the rock have also been studied. It was observed local and sudden slow downs of the heating process, probably caused by the asperity. A similar phenomena with a more complicated geometry could explain the sudden temperature variations during transient regime observed when pumping in geothermal systems.
 In spite of the simplicity of the studied fracture geometry, the observed hydrothermal exchanges are finally very complex. The local three-dimensional phenomena modify both the hydraulic and thermal macroscopic properties, in a different way. To extend this work on real field, it would be interesting to consider multiplicity of scales, either a distribution of asperity sizes or a network of fractures. At the field scale, it is not clear how much time will be necessary for a real steady state to be reached. This depends on the volume of the hydraulically stimulated rock and also on the distance and time dependency of the heat sources.
 We wish to thank K.J. Måløy, M. Erpelding, A. Cochard, F. Renard, L. Talon, and O. Aursjø for fruitful discussions. We acknowledge the financial support of the Research Council of Norway through the YGGDRASIL mobility grant for the project n°202527, the PETROMAKS project, the PICS program France-Norway, the ANR Landquake, the ITN FLOWTRANS, and the support of the CNRS INSU. We also thank the French network of Alsatian laboratories, REALISE.