Abstract
The process of stress-strain accumulation near earthquake faults during the aseismic period has become a subject of research during the last few decades. It is noted that seismic waves, generated by an earthquake, result in a considerable disturbance in a seismic region causing a movement of the free surface. Such ground movements are not observed during the aseismic period. But a slow quasi-static aseismic surface displacement of the order of few cms. per year or less can be observed during the aseismic period which indicates a slow sub-surface process of stress-strain accumulation. Keeping this in view we here consider an aseismically creeping, buried, finite strike-slip fault inclined to the vertical at an arbitrary angle. The fault is situated in an elastic layer over an elastic half-space representing the lithosphere-asthenosphere system. An analytical study for displacement, stress and strain due to creeping effect has been carried out for a buried, finite, inclined fault. The solutions for displacement, stress and strain are then found before the onset of fault slip and then superpose the effect of fault slip using Laplace transform and suitable mathematical techniques of Green’s function. The analytical results and the graphical presentations show that the inclination of the fault and the velocities of the fault movement has noticeable effect on displacements, stresses and strains.
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The first author is thankful to DST, New Delhi, India, for its financial support under INSPIRE fellowship, without which this research would not have been possible.
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Appendix
Appendix
1.1 Appendix-I (Solutions of displacement, stress and strain in the absence of fault movements)
Let
where \(A_i,~ B_i,~ C_i (i = 1,2),~ F_i ~\text {and} ~F'_i~ (i= 1,2,3)\) are to be determined.
Now
Taking Laplace transformation of Eq. (12) we get
Now comparing Eqs. (26) with (28) and (27) with (29) we get
Since \(F_1\), \(F_2\), \(F'_1\) and \(F'_2\) are functions of \(y_1,~ y_2,~ y_3 ~\text {and}~ p\), \((\frac{\partial F_1}{\partial y_2}+ \frac{\partial F_2}{\partial y_1})\) and \((\frac{\partial F'_1}{\partial y_2}+ \frac{\partial F'_2}{\partial y_1})\) can not be in general equal to g(p) and h(p) except for some particular cases.
Then \((\frac{\partial F_1}{\partial y_2}+ \frac{\partial F_2}{\partial y_1})_{|y_2|\rightarrow \infty } =(\frac{\partial F'_1}{\partial y_2}+ \frac{\partial F'_2}{\partial y_1})_{|y_2|\rightarrow \infty } =0\)
On \(y_3 = 0\)
At \(y_3 = h_1\)
and
Taking Laplace transform on expression of \( \tau _{13}\) and \(\tau '_{13}\) given in Eqs. (2) and (3) and putting the value of \(\bar{u_1}, \bar{u_3}, \bar{u_1}', \bar{u_3}'\) from Eq. (25) we get
Similarly
and also
Let \({(\tau _{13})_0} = {(\tau '_{13})_0} = \tau _{h_1}\) at \(y_3 = h_1\)
Then putting the value of \(\bar{\tau _{13}} ~\text {and} ~\bar{\tau _{13}}'\) in Eq. (35) and since at \(y_3 = h_1\)
\(F_1 = F'_1~ \text {and}~ F_3 = F'_3\) then we get
In our model, we consider the case where \(\tau _{h_1} = 0\). Then an obvious solution for \(F_1, F_3, F'_1, F'_3~\) is
So \(c_1 = 0\)
Then Eq. (25) becomes
Taking Laplace transform on Eqs. (2) and (3) except on \(\tau _{13}\) and \(\tau '_{13}\) and using equation (37) we get in elastic layer
and in elastic half-space
Taking Laplace transform on boundary conditions (6) and (7) we get
(\(y'_2 = 0,~ 0 \le y'_3 \le D,~ t \ge 0\)) and
(\(y'_2 = 0,~ 0 \le y'_3 \le D,~ t \ge 0\))
From Eq. (38) as \(-L \le y'_1 \le L\), \(y'_2 = 0\) and \(0 \le y'_3 \le D\)
Therefore
Taking Laplace transform on boundary condition (8) we get
Then form Eq. (39)
Also at \(y_3 = 0\)
From Eq. (40)
So \(c_2 = 0\)[Since from (32) \(\frac{\partial F_2}{\partial y_3} = 0]\)
From Eq. (41)
Since \(B_2\) is a function of p and \(F_2\) is a function of \(y_1\), \(y_2\), \(y_3\), p, so in general \(\frac{\partial F_2}{\partial y_2}\) can not equal to \(B_2\) except particular cases.
Therefore
Taking Laplace transform on boundary condition (10) we get
From Eq. (46)
Therefore
So, \(F_2 = {\frac{1}{\mu _1}([\tau _{\infty }(p) - \frac{1}{p}\tau _{\infty }(0)]- 2[h(p) + g(p)])}y_1\)
Therefore \(\bar{u_1} = \frac{(u_1)_0}{p} + 2 h(p) y_2\)
Taking inverse Laplace Transform we get
For elastic layer
and for elastic half-space
Now for elastic layer \((0 \le y_3 \le h_1,~ |y_2| < \infty )\)
and similarly for elastic half-space \((y_3 \ge h_1,~|y_2| < \infty )\)
We assume \(u_i\) = \((u_i)_1\), \(\tau _{ij}=(\tau _{ij})_1\) (i, = 1,2,3), \(e_{12} = (e_{12})_1\) and \(e_{13} = (e_{13})_1\) for elastic layer and \(u'_i\) = \((u'_i)_1\), \(\tau '_{ij}=(\tau '_{ij})_1\) (i, = 1,2,3), \(e'_{12} = (e'_{12})_1\) and \(e'_{13} = (e'_{13})_1\) for elastic half-space in the absence of fault movement.
1.2 Appendix-II (Solution of displacements, stresses and strains after the commencement of fault creep)
The displacements, stresses and strains after the commencement of fault creep have been found in the form given in equation (18) and (19), where \((u_i)_1,~ (u'_i)_1 (i = 1,2,3),~ (\tau _{ij})_1, ~(\tau '_{ij})_1, (e_{12})_1,~(e_{13})_1,~ (e'_{12})_1,~(e'_{13})_1\) \((i, j = 1, 2, 3)\) are given by equation (48), (49), (50) and (51) and \((u_i)_2,~ (u'_i)_2 ~(i = 1,2,3),~ (\tau _{ij})_2,~ (\tau '_{ij})_2 ~(i, j = 1, 2, 3),~ (e_{12})_2,~(e_{13})_2,~ (e'_{12})_2,~(e'_{13})_2\) satisfy Eq. (2) to (11), (16), (17). This boundary value problem involving \((u_i)_2,~ (u'_i)_2~ (i = 1,2,3),~ (\tau _{ij})_2, ~(\tau '_{ij})_2, ~ (i, j = 1, 2, 3,~(e_{12})_2,~(e_{13})_2,~ (e'_{12})_2,~(e'_{13})_2\) can be solved by using modified Green’s function technique developed by Maruyama (1966) and Rybicki (1971) and correspondence principle. According to them we get,
where \(Q_1(y_1, y_2, y_3),~ Q_2(y_1, y_2, y_3)\) are field points in the layer and half-space respectively and \(P(x_1, x_2, x_3)\) is any point on the fault F and \([(u_1)_2(p)]\) is the magnitude of discontinuity of \(u_1\) across F and G and \(G'\) are Green’s function.
where
Here
where
where \(\gamma _1 =\frac{\mu _2}{\mu _1}~\text {and} ~ \mu _1, ~\mu _2 \) are rigidity of elastic layer and elastic half-space respectively and \(\lambda \) is Lame’s constant, \(h_1\) is the thickness of elastic layer.
Now assume \(d = x_3 + y_3,~ d_1 = x_2 - y_2,~ d_2 = x_3 - y_3,~ d_3 = x_1 - y_1 \) and \(d_4 = x_1 + y_1\)
Then
Therefore \(G(P, Q_1) = \frac{\partial }{\partial x_2} G_{12(1)}(P, Q_1) - \frac{\partial }{\partial x_2} G_{13(1)}(P, Q_1)\)
and
\(P(x_1, x_2, x_3)\) being a point on the fault F. Since the fault inclined at an angle \(\theta \) and depth is \(r_1\) from the free surface , then \( 0 \le x_2 \le D \cos \theta , ~0 \le x_3 \le D \sin \theta ~\text {and}~ x_2 = x_3~ \cot \theta \). A change in co-ordinate from \((x_1, x_2, x_3)\) to \((x'_1, x'_2, x'_3) \) connected by the relations :
From \( x_2 = x_3 ~\cot \theta \) we get \(x'_2 = 0\)
Then \(x_1 = x'_1,\) \(x_2 = x'_3 \cos \theta \), \(x_3 = x'_3 \sin \theta + r_1\) and \(d x_1 = d x'_1\), \(d x'_2 = 0\), \(d x_3 = \sin \theta ~d x'_3\)
Since the co-ordinate of the end points of the fault are taken w.r.t prime co-ordinate system as A \((-L, 0, 0)\) and B (L, 0, 0) respectively then the limit of the integration of \(x'_1\) is \(-L\) to L. Also w.r.t prime co-ordinate system the width of the fault is D then the limit of \(x'_3\) is taken as 0 to D.
Then \( \bar{(u_1)_2}(Q_1)= \int _{-L}^{L} \int _{0}^{D} U_1 (p)f(x'_1, x'_3)G(P, Q_1) \sin \theta ~dx'_3 dx'_1\)
Taking inverse Laplace transform we get,
where \(H(t_1)\) is the Heaviside step function, \(t_1 = t - T_1\) and
where
Taking inverse Laplace transform we get,
where \(H(t_1)\) is the Heaviside step function and \(t_1 = t - T_1\)
and \(\psi (y_1, y_2, y_3 ) = \int _{-L}^{L} \int _{0}^{D} f(x'_1, x'_3)G'(P, Q_2) ~\sin \theta ~ dx'_3~ dx'_1\)
where
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Kundu, P., Sarkar (Mondal), S. & Mondal, D. Creeping effect across a buried, inclined, finite strike-slip fault in an elastic-layer overlying an elastic half-space. Int J Geomath 12, 2 (2021). https://doi.org/10.1007/s13137-020-00170-y
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DOI: https://doi.org/10.1007/s13137-020-00170-y