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To investigate the failure behavior of foliated or layered rock materials, many scholars derived a number of constitutive laws and failure criteria for transversely isotropic rocks [11,12,13,14]. These constitutive laws and failure criteria agreed well with the experimental data of many investigators in terms of prediction of strength and deformation, but they were difficult to be used to characterize crack evolution during the loading process. Accordingly, substantial studies were carried out on the strength, deformation characteristics, and failure behavior of transversely isotropic rocks by both experimental and numerical methods [15,16,17,18]. Tien et al.  investigated 3D macroscopic-fractured surfaces of simulated transversely isotropic rocks by reconstructing unrolled images from a rotary scanner and divided the failure modes into four kinds: sliding failure along discontinuities, tensile fracture across the discontinuities, tensile-split along the discontinuities, and sliding failure across the discontinuities. Yin and Yang  studied three kinds of transversely isotropic rock-like specimens with different bedding thickness ratios under conventional triaxial compression and divided the failure modes into three kinds: tensile-split along the core axes (0, 15, and 30), shear-sliding along the bedding plane (45, 60, and 75), and split along the vertical bedding plane (90). Furthermore, the development of the Digital Image Correlation method (DIC) [21,22,23], Acoustic Emission techniques (AE) [24,25,26,27], and Scanning Electron Microscopic observation (SEM) was found to be suitable for capturing the progressive failure process and understanding the failure mechanism of the rock. The aforementioned studies show that the failure mode transforms from tensile splitting across discontinuities to shear slip along discontinuities, and finally to tensile splitting along discontinuities with increasing foliation angle.
Energy Dispersive Spectroscopy (EDS) has been widely used in the mineral composition analysis of rock materials with the advantage of easy operation, quick analysis, and low cost. By scanning the region within the 1 μm fracture surface, the element from Beryllium (Be) to Uranium (U) could be identified [42,43]. In this study, four rock fractures were selected from the parallel and vertical surface of the foliation plane in specimens under dry and water-saturated conditions. All experiments were repeated twice by changing the scanning region and magnification. As illustrated in Table 3, the contents of Sodium, Magnesium, and Calcium are more extensive in specimens under dry conditions, and the content of potassium is more extensive in specimens under water-saturated conditions. This result indicates that the amount of biotite contained in phyllite participated in the hydration reaction, resulting in the Potassium ions (Na+) in biotite being replaced by other macromolecules or the ions of Sodium (Na+), Magnesium (Mg+), and Calcium (Ca+). Due to the radii of these replaced macromolecules or ionic being larger than the radius of Potassium ions (Na+), some tensile cracks initiate and propagate from biotite cleavage, and then small fragments gradually divorce from the edge of biotite cleavage. Thus, the presence of water could contribute to accelerating the evolution of micro-cracks. Furthermore, the contents of Silicon, Calcium, and Iron are more extensive on the fracture surface that is vertical to the foliation plane, and the contents of Aluminium and Titanium are more extensive on the fracture surface parallel to the foliation plane. This indicates that the biotite on the foliation plane is larger than that on the vertical foliation plane and the quartz on the foliation plane is less than that on the vertical foliation plane, reflecting that the mineral composition distribution of phyllite is anisotropic.
(3) With the help of AE, DIC, and SEM techniques, the experiments show that foliation angle and water content have a significant influence on crack evolution. The water acts on biotite and clay minerals that are the main components of phyllite, and it contributes to the initiation, propagation, and coalescence of numerous microcracks. Furthermore, the tensile micro-cracks are the main reason for the failure of the phyllite, especially for saturated groups. From viewpoint of macro-cracks, the initiation shear crack is dominant at lower foliation angles, i.e., 0, 30, 45, and 60, and the influence of foliation planes on the crack propagation path increases with the foliation angle increasing. At higher foliation angles, such as 90, tensile cracks initiate and extend along the vertical foliation plane, and finally cause the tensile fracture in foliations from outside to inside.