Geofluids
Volume 2020 (2020), Article ID 8855439, 14 pages
https://doi.org/10.1155/2020/8855439

Research Article

Experimental and Numerical Study on Hydromechanical Coupled Deformation Behavior of Beishan Granite considering Permeability Evolution

Z. H. Wang,1,2 W. G. Ren,³ Y. L. Tan,1,2 and Heinz Konietzky⁴

¹State Key Laboratory of Mining Disaster Prevention and Control Cofounded by Shandong Province and the Ministry of Science and Technology, Shandong University of Science and Technology, Qingdao Shandong 266590, China
²College of Energy and Mining Engineering, Shandong University of Science and Technology, Qingdao Shandong 266590, China
³School of Mechanics and Civil Engineering, China University of Mining and Technology, Beijing 100083, China
⁴Geotechnical Institute, TU Bergakademie Freiberg, Gustav-Zeuner-Str. 1, 09596 Freiberg, Germany

Correspondence should be addressed to Z. H. Wang; skd996340@sdust.edu.cn

Received 25 May 2020; Revised 12 July 2020; Accepted 21 July 2020; Published 5 August 2020

Academic Editor: Qiqing Wang

Copyright © 2020 Z. H. Wang et al. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

Abstract.

Beishan granite is a potential host rock for a high-level radioactive waste (HLW) repository in China. Understanding the hydromechanical (HM) behavior and permeability evolution of Beishan granite is important for the HLW repository safety. Therefore, the granite of Beishan in Gansu province was studied. HM coupled tests are carried out on Beishan granite under different pore pressures. The results show that the initial pressure difference has little influence on permeability measurement before dilatancy starts. However, after onset of dilatancy, the permeability increases with the increasing initial pressure difference. The initial permeability of Beishan granite is about under a confining pressure of 20 MPa. In the initial loading phase, the permeability shows a relatively large reduction. Then, the permeability almost keeps constant until dilatancy starts. From dilatancy point to peak stress, permeability increases linearly with volumetric strain. The proposed permeability evolution rule is implemented into a numerical code to perform HM coupled simulations. The simulation results show that the damaged zone first appears at the model boundary and then extends to the inside, forming high volumetric strain areas. And it provides seepage channels for fluid flow. The macroscopic fracture patterns indicate that pore pressure accelerates rock degradation during HM coupling. The obtained results help to understand the damage mechanisms of granite caused by pore pressures and are of great importance for the safety of a HLW repository.

1. Introduction

Disposal of high-level radioactive waste (HLW) deep underground is one of the most challenging research subjects in rock engineering. The biggest difficulty is the proof of safe and long-term isolation of the HLW from the biosphere. Granite, characterized by high strength and low permeability, is one of the preferred host rocks for geological disposal of HLW. China plans to build a HLW repository in the granite strata of Beishan, Gansu Province [1, 2]. Therefore, the understanding of the hydromechanical (HM) coupled behavior and permeability evolution of Beishan granite is of great significance to ensure the long-term safety of the HLW repository.

As a heterogeneous material, rock contains microcracks. The failure process of rock associated with crack propagation has been well studied [3–8]. On the other hand, cracks provide seepage channels for fluid flow. The fluid flow in the crack network will accelerate the rock failure process, which has influence on rock strength and deformation [9–12]. Therefore, after years of research, the permeability evolution during the rock failure process has gradually attracted the attention of researchers. Brace et al. [13] and Zoback et al. [14] studied the permeability of Westerly granite. Their results indicate that permeability has strong dependence on effective pressure and increases gradually after dilatancy threshold. Hydrostatic compression and triaxial compression tests were conducted on Inada granite by Kiyama et al. [15]. The results show that permeability increases proportionally to the dilatation between the onset of dilatancy and the peak strength. Liu et al. [16] investigated the permeability evolution of granite gneiss during triaxial creep tests. They demonstrate that the permeability remains stable in the steady creep stage and increases rapidly in the accelerated creep stage. For granite, Chen [17] revealed that the permeability decreases when confining pressure is larger and increases when pore water pressure is larger under compressive stress conditions. Yi et al. [18], Heiland and Raab [19], Alam et al. [20], and Zhang et al. [21] studied permeability evolution of different rock types under compression. The results show similar permeability evolution trends, in which the permeability decreases at the stage of volumetric compaction and increases at the stage of volumetric dilation.

On the other hand, important progress has been made in numerical simulation of HM coupled processes in rocks, especially in the DECOVALEX project [22, 23]. A flow-stress-damage (FSD) coupling model considering permeability evolution is proposed by Tang et al. [24]. And this FSD model is used to investigate the behavior of fluid flow and damage evolution under hydraulic conditions. Rutqvist et al. [25] linked two codes—TOUGH2 and FLAC3D—for analysis of coupled THM processes, in which the coupling module containing nonlinear stress versus permeability functions is taken into account. Tan and Konietzky [26] proposed a micromechanical numerical model to simulate the HM coupled behavior of granite at the grain-sized level. It reveals the importance of tensile micro cracks for enhanced permeability, and linear correlations between volumetric strain and permeability are observed by numerical simulations. Lu et al. [27] presented a coupled continuum-based HM modeling approach using a two-scale conceptual model representing realistic rock material containing microfractures. This model is validated against failure under compression and replicates typical AE characteristics and permeability evolution.

This paper presents HM coupling tests carried out on Beishan granite under different pore pressures. The influence of initial pressure difference () on permeability monitored by the transient pulse method is discussed. The permeability evolution of Beishan granite under compression is revealed. In addition, a heterogeneous numerical model is established to simulate the deformation and damage process under HM coupling considering volumetric strain and permeability evolution.

2. Permeability Measurements by the Transient Pulse Method

In most cases, permeability can be measured either by using the constant head method [28, 29] or the transient pulse method [30–33]. However, due to the low permeability of granite, it will take a long time for the fluid to reach a steady flow by using the constant head method. Compared with the constant head method, fluid does not need to achieve a steady flow by using the transient pulse method. Therefore, it will consume less time. And the transient method has higher accuracy for low permeability rocks. As a result, in this study, the transient pulse method is used.

The test principle of transient pulse method is shown in Figure 1. At the beginning, a constant pore pressure is maintained in the sample and adjacent upper and lower fluid reservoir. Then, the pressure in the upper reservoir is instantaneously increased and the pressure decay at both reservoirs is monitored. The pressure difference can be described by

with as permeability (m²), as viscosity of fluid (water at 20°C: 10⁻³ Pa·s), as the compression coefficient of fluid (water: ), as cross-sectional area of sample (m²), as the height of the sample (m), as the volume of upper reservoir (m³), as the volume of the lower reservoir (m³), as the duration time (s), as the pore pressure of the upper reservoir at time (MPa), as the pore pressure of the lower reservoir at time (MPa), and as the initial differential pressure between upper and lower fluid reservoir (MPa). In general, equals ; thus, Equation (1) can be rewritten as

with as the final differential pressure between the upper and lower fluid reservoirs (MPa).

(a)

(b)

Figure 1: Simplified schematic of the transient pulse method: (a) testing system and (b) measuring pressure decay over time.

3. Laboratory Test Settings

3.1. Preparation of Rock Specimens

The granite samples were taken from the Beishan area, Gansu Province, China. The specimens, with a diameter of 50 mm and length of 100 mm, were prepared according to ISRM recommendations [34]. If readers want to know the basic properties and components of Beishan granite, please refer to literature [35, 36].

3.2. Test Facility

The HM coupled tests were carried out with a MTS815 Flex Test GT (see Figure 2) rock mechanical testing machine. This machine has a maximum loading capacity of 4,700 kN and can supply a maximum confining pressure of 140 MPa [37]. Axial and lateral strains are measured by extensometers.

Figure 2: Rock mechanics experimental system of MTS815 and installation of sample.

3.3. Testing Procedure

Four specimens were prepared for HM coupled testing. Before the tests, the specimens were immersed in water for 72 hours in the vacuum suction device to reach the saturated state [38]. For the HM coupled tests, first, a vertical load of about 2 kN was applied in order to fix the position of the specimen. Then, the desired confining pressure (20 MPa in all HM coupled tests) was reached with a constant loading rate of 0.05 MPa/s to ensure that the specimen was under uniform hydrostatic stresses [39]. Pore pressures were set to 2, 4, 6, and 8 MPa, which mirror the maximum potential water pressure at different buried depths in the Beishan region [38]. The desired pore pressure was reached with a constant rate of 1 MPa/min. Afterwards, the axial stress was increased with a constant loading rate of 30 kN/min. During the process of loading, the transient pulse method was used to measure the permeability of Beishan granite at different strain levels. Stress and strain were kept constant during the permeability testing.

In addition, in order to study the influence of initial pressure difference () on the transient pulse method, three initial pressure differences were used to measure permeability under the same strain levels during loading. The initial pressure differences were set to 3.4, 5.4, and 7.4 MPa, which is close to the potential water pressure at different buried depths in the Beishan region. And if the initial pressure difference is small, it is not conducive to monitor the pressure decay for Beishan granite because of low permeability. Two specimens (BSS-1 and BSS-2) were used for this task.

4. Test Results

4.1. Influence of Initial Pressure Difference () on Measurement Results of the Transient Pulse Method

The permeability measured by different initial pressure differences under the same strain levels is shown in Tables 1 and 2 and Figure 3. For a confining pressure of 20 MPa, the initial permeability values measured by different initial pressure differences are quite similar. Because of the unique heterogeneity of each sample, the measured permeability will always show some minor differences.

Table 1: Permeability test results for specimen BSS-1 for three different initial pressure differences.

Axial strain (%)
Axial stress (MPa)
Permeability ()

3.4 MPa
5.4 MPa
7.4 MPa

0
0
3.77
2.97
2.33

0.386
38.6
1.05
1.30
1.34

0.629
79.3
1.03
1.12
1.29

0.855
123.8
0.55
1.08
1.26

1.066
165.6
0.94
1.29
1.65

1.240
201.8
1.45
1.92
2.36

1.528
256.6
3.43
5.30
7.54

2.337
81.8
72.74
55.31
59.57

Table 2: Permeability test results for specimen BSS-2 for three different initial pressure differences.

Axial strain (%)
Axial stress (MPa)
Permeability ()

3.4 MPa
5.4 MPa
7.4 MPa

0
0
1.32
1.24
0.64

0.414
48.7
0.71
0.66
0.66

0.716
106.1
0.78
0.50
0.47

0.940
150.1
0.48
0.56
0.48

1.163
200.0
0.75
0.61
0.70

1.425
252.5
1.33
1.12
1.54

1.855
315.6
5.81
9.86
15.36

2.011
79.5
13.56
16.07
17.74

2.599
75.9
13.25
14.08
14.69

(a)

(b)

Figure 3: Permeability for different initial differential pressures (a) BSS-1 (b) BSS-2.

At the initial stage of loading, due to the closure of micro cracks, permeability decreases. Before onset of dilatancy, the permeability changes little. After onset of dilatancy, permeability is increasing. Also, the permeability increases with the increasing initial pressure difference. For instance, the permeability measured for sample BSS-2 under the initial pressure difference of 7.4 MPa () around the peak stress is 2.64 times of that measured under the initial pressure difference of 3.4 MPa (). After the peak stress, permeability becomes unstable due to the thrived macro cracks in the sample. The permeability in the post failure region is not discussed in this study.

4.2. Stress Strain Curves of HM Coupled Tests

Figure 4 shows the stress-strain curves of Beishan granite under different pore pressures. With increasing pore pressure, maximum axial strain and peak stress decrease.

Figure 4: Stress strain curves of Beishan granite under different pore pressures [40].

4.3. Permeability Evolution of HM Coupled Tests

The permeability measured during HM coupled testing is shown in Table 3 and Figure 5. It can be concluded that the initial permeability of Beishan granite is maintained at about under the confining pressure 20 MPa. On the whole, the permeability first decreases slowly and then increases gradually during loading. The general trend of permeability evolution is the same for different pore pressures.

Table 3: Permeability evolution under different pore pressures.

Sample
Pore pressure (MPa)
Permeability/

1sta
2nd
3rd
4th
5th
6th
7th
8th

HM-1
2
5.8
2.78
4.91
6.5
20.29(pb)
22.71
22.89
25.49

HM-2
4
1.29
0.51
0.38
1.14(p)
3.04
3.74
5.38
—

HM-3
6
0.95
0.29
0.48
1.3
2.46
5.85
10.7(p)
32.78

HM-4
8
2.29
1.48
1.77
3.84
7.03
11.51
13.17(p)
26.16

a”1st” represents the first time to measure permeability. b”P” represents the permeability measured around peak stress.

(a)

(b)

(c)

(d)

(e)

(f)

(g)

(h)

Figure 5: Permeability evolution of Beishan granite during HM coupling. (a, b) Pore pressure of 2 MPa, (c, d) pore pressure of 4 MPa, (e, f) pore pressure of 6 MPa, and (g, h) pore pressure of 8 MPa.

Taking the pore pressure of 8 MPa as an example, combined with the volumetric strain development, the permeability evolution of Beishan granite under loading can be roughly divided into the following stages. In the first stage (i.e., the initial stage of loading), micro cracks begin to close, which leads to a decrease of sample volume and loss of some seepage channels. Therefore, the decrease of permeability is relatively large compared to the initial permeability (for instance, reduction by 40% under pore pressure of 4 MPa). In the second stage, as the axial stress continues to increase, the volume of the specimen decreases. But there is possibility that new micro cracks are generated. Thus, the permeability almost keeps constant. After the dilatancy point, micro cracks are reactivated gradually and interact with each other, which leads to crack coalescence and provides new seepage channels. The permeability increases gradually with increasing volumetric strain. It can be concluded from Figures 5(b), 5(d), 5(f), and 5(h) that there is a linear relationship between permeability and volumetric strain from dilatancy point to peak stress. At peak stress, permeability can increase by an order of magnitude compared with the initial permeability (see sample HM-3). After the peak stress, the seepage behavior changes from porous medium seepage to fractured medium seepage. In this stage, the permeability changes greatly, which is beyond the scope of this study.

According to tests results, the permeability evolution of Beishan granite in respect to volumetric strain can be roughly divided into two stages before reaching the peak stress, as shown in Figure 6. For the fractured medium seepage in the post peak stage, it is not possible to predict permeability just by volumetric strain. Before the dilatancy threshold , permeability decreases with decreasing volumetric strain. It can be approximately expressed as linear relationship, and the linear coefficient is set to . From dilatancy threshold to peak stress , permeability increases linearly with increasing volumetric strain. The correlation coefficients (see Figure 5) confirm the correctness of linear fitting, and the linear coefficient is set to . The relationships can be expressed by

where initial permeability (m²) and volumetric strain. It can be deduced from test data that is much greater than .

Figure 6: Simplified illustration of permeability evolution in HM coupling processes in Beishan granite.

5. HM Coupled Simulations

5.1. Model Description and Setup

In order to study the stress strain state inside the specimen, a heterogeneous cylindrical model with 50 mm in diameter and 100 mm in length is established in the explicit Finite Difference code FLAC3D as shown in Figure 7. The model has 96000 zones and 100521 gridpoints. For the HM coupled simulations, the confining pressure is set to 20 MPa. A compressive displacement rate of 5e-8 m/step is assigned on the top and bottom faces of the model. Permeable boundaries are applied at the top and bottom of the model. The pore pressure is fixed on the top and bottom of the model to simulate constant fluid pressure. A strain-softening model is used for mechanics, and an isotropic Darcy model is used for the fluid flow. All input parameters are listed in Tables 4 and 5. And the parameters in Tables 4 and 5 are consistent with the HM coupled test.

Figure 7: Schematic diagram of Beishan granite model.

Table 4: Mechanical parameters of Beishan granite.

Elastic modulus (GPa)
Poisson’s ratio
Dilation (°)
Density (kg/m³)
Cohesion (MPa)
Friction (°)
Tension (MPa)

Initial
Residual
Initial
Residual
Initial
Residual

28.6
0.122
17
2700
29.74
21.24
51
31.44
7.66
0

Table 5: Hydraulic parameters of Beishan granite.

Fluid modulus (GPa)
Fluid density (kg/m³)
Initial permeability (m²)
Porosity (%)
Saturation

2.2
1000
2.5810⁻¹⁸
0.02
1

5.2. Determination of Linear Correlation Coefficients

According to Section 4.3, the permeability has a linear relationship with volumetric strain. And volumetric strain of elements can be directly obtained in FLAC3D. Therefore, the permeability is updated during the numerical simulation. However, the linear relationships cannot be applied to describe the permeability evolution of the elements directly. Therefore, the linear coefficients need to be calibrated by several numerical simulations [41].

First, simulation of the conventional triaxial compression (CTC) test under confining pressure of 20 MPa is conducted. A compressed numerical model (see Figure 8(a)) before the dilatancy threshold is chosen to determine the linear coefficient , and a damaged numerical model beyond the dilatancy threshold (see Figure 8(b)) is chosen to determine the linear coefficient . The initial permeability is set as . The two models are used to simulate steady flow with different linear coefficients, and the results are shown in Figure 9. According to the flow rate, and fit the lab results.

(a)

(b)

Figure 8: Volumetric strain for confining pressure of 20 MPa: (a) compressed stage and (b) damaged stage.

(a)

(b)

Figure 9: Flow rates and corresponding coefficients: (a) and (b) .

5.3. HM Coupled Simulation Results

The proposed permeability evolution rule (Equation (3)) is implemented into FLAC3D. The pore pressures correspond to the HM coupling tests. Figure 10 shows stress-strain curves obtained from simulations. Taking the pore pressure of 8 MPa as an example, the deformation and permeability evolution for different observation points (marked in Figure 11) are shown in Figures 12-15.

Figure 10: Simulated stress-strain curves for different pore pressures under 20 MPa confining pressure.

Figure 11: Simulated stress-strain curve for pore pressure of 8 MPa under confining pressure of 20 MPa.

(a)

(b)

(c)

(d)

(e)

Figure 12: Evolution of maximum stress tensor (Pa) for simulated HM coupled test: (a) initial compressed stage, (b) elastic stage, (c) peak stress point, (d) stress drop stage, and (e) residual stage.

(a)

(b)

(c)

(d)

(e)

Figure 13: Evolution of volumetric strain for simulated HM coupled test: (a) initial compressed stage, (b) elastic stage, (c) peak stress point, (d) stress drop stage, and (e) residual stage.

(a)

(b)

(c)

(d)

(e)

Figure 14: Evolution of permeability () for simulated HM coupled test: (a) initial compressed stage, (b) elastic stage, (c) peak stress point, (d) stress drop stage, and (e) residual stage.

(a)

(b)

(c)

(d)

(e)

Figure 15: Evolution of discharge vectors (m/s) for simulated HM coupled test: (a) initial compressed stage, (b) elastic stage, (c) peak stress point, (d) stress drop stage, and (e) residual stage.

Some conclusions can be drawn from the numerical simulations. In the quasi elastic stage (points a and b), the stress state is nearly homogeneous; volumetric strain decreases with increasing axial stress, and all elements are compressed; permeability is decreasing and fluid flow is restricted. In brief, there is no damage at this stage. At the peak stress (point c), the stress distribution is no longer uniform; volumetric strain increases especially close to the model boundary; therefore, permeability and flow rate increase near the model boundary. During the stress drop (point e), local tensile stresses appear; volumetric strain increases rapidly and forms serval shear bands, which develop from the model boundary to the inside. And it provides several seepage channels with high permeability for fluid flow. In the residual stage (point e), the tensile stress area expands; the volumetric strain bands become wider and interact with each other.

The macroscopic fracture patterns for samples under different pore pressures are shown in Figure 16. With the increase of pore pressure, the volumetric strain band channels increase. In other words, macroscopic fractures become pronounced with increasing pore pressure. It indicates that the pore pressure accelerates rock degradation during HM coupling.

(a)

(b)

(c)

(d)

Figure 16: Volumetric strain () at stage e under different fluid pressures: (a) pore pressure of 2 MPa, (b) pore pressure of 4 MPa, (c) pore pressure of 6 MPa, and (d) pore pressure of 8 MPa.

6. Conclusion

HM coupled tests are carried out on Beishan granite under different pore pressures. The permeability evolution is studied. And numerical simulations are conducted to study the stress state and deformation process. Based on the results, the following conclusions can be drawn.

Before dilatancy, the initial pressure difference () has little influence on permeability measurement by using the transient pulse method. However, after dilatancy, the permeability increases with the increasing initial pressure difference. Overall, the permeability evolution trends are the same.

The initial permeability of Beishan granite maintains at the order under the confining pressure 20 MPa. In the initial loading phase, the permeability shows a relatively large reduction. Then, the permeability almost keeps constant. From onset of dilatancy to peak stress, the permeability increases linearly with the volumetric strain. A rule of relating permeability evolution with volumetric strain is proposed.

The simulation results show that the damaged zone first appears close to the model boundary and then extends to the inside, forming local high volumetric strain areas. And it provides seepage channels for fluid flow. The macroscopic fracture patterns indicate that pore pressure accelerates rock degradation during HM coupling.

In the future, more tests are needed for further investigating permeability evolution and fracturing characteristics of Beishan granite subjected to different confining stresses and pore pressures.

Data Availability

The data used to support the findings of this study are available from the corresponding author upon request.

Conflicts of Interest

The authors declare that they have no competing financial interests or personal relationships that could have influenced the work reported in this paper.

Acknowledgments

This work was supported by the Major Program of Shandong Province Natural Science Foundation (ZR2018ZA0603) and the National Natural Science Foundation of China (51674266).

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