S. Chakraborty^{1} , S. C. Mandal^{2} , A. K. Das^{3} , N. Sarkar^{4} , A. Lahiri^{5}
^{1, 2, 5}Department of Mathematics, Jadavpur University, Kolkata, 700032, India
^{3}Department of Geology, Asutosh College, 92, S. P. Mukherjee Road, Kolkata, 700026, India
^{4}Department of Applied Mathematics, University of Calcutta, Kolkata, 700009, India
^{4}Corresponding author
Mathematical Models in Engineering, Vol. 2, Issue 2, 2016, p. 114134.
https://doi.org/10.21595/mme.2016.17621
Received 26 August 2016; accepted 27 October 2016; published 31 December 2016
Copyright © 2016 JVE International Ltd.
In this paper, the theory of coupled thermoelasticity in three dimension is employed for triclinic halfspace, subjected to time dependent heat source on the boundary of the space which is traction free and is considered in the context of GreenNaghdi model of type II (thermoelasticity without energy dissipation) of generalized thermoelasticity. Normal mode analysis is used to the nondimensional coupled equations. Finally, the resulting equations are written in the form of a vectormatrix differential equation which is then solved by eigenvalue approach. Numerical results for the temperature, thermal stresses, and displacements are presented graphically and analyzed. Mathematical results shown in thermoelastic curves were supplemented by tectonic movements of elastic lithospheric plates.
Keywords: anisotropic solid, GreenNaghdi model II, normal mode analysis, eigenvalue approach, lithostatic pressure and lithospheric plates.
The classical uncoupled theory of thermoelasticity, predicts two phenomena not consistent with experimental results. The heat conduction equation of this theory i) does not contain any elastic terms, but the fact is that the elastic changes produces heat effects and ii) the heat conduction equation is of parabolic type predicting infinite speeds of propagation for heat waves, which means that the theory classical of thermoelasticity (CT) predicts finite for predominantly elastic disturbances but an infinite speed for predominantly thermal disturbances, which are coupled together. This means that a part of every solution of the equations extends to infinity. To overcome this paradox inherent in the theory of classical uncoupled theory of thermoelasticity, Biot [1] introduced the theory of coupled thermoelasticity.
To eliminate the second shortcoming Lord and Shulman [2] (LS model) introduce a theory of generalized thermoelasticity with one relaxation time parameter, by modification of Fourier’s law, replaced heat flux and its time derivatives. In LS model the heat conduction equation is hyperbolic type and is closely connected with the theories of “second sound”. This theory was extended for anisotropic body by Dhaliwal and Sherief [3]. The uniqueness of the solutions for this theory was proved under different conditions by Ignaczak [4, 5]. Green and Lindsay [6] (GL model) modified not only heat conduction equation but also equation of motion in the coupled theory without violating Fourier’s law by introducing two relaxation time parameters. Along with the theories, Green and Naghdi [79] (GN model) also proposed another three generalized theories of thermoelasticity by introducing “thermal displacement gradient” among the independent constitutive variables and named as Type I, II and III. Among these models, type I [7] is same as classical heat equation which is based on Fourier’s law where the theories are linearized. The type II [9] and type III [8] model permit finite speed of wave propagation. The basic difference of type II from type I and type III is that it does not contain dissipation of thermal energy whereas type III contains dissipation of energy. The type II and Type III are also known as thermoelasticity without energy dissipation (TEWOED) and thermoelasticity with energy dissipation (TEWED). Several investigations relating to TEWOED theory have been studied by Roy Choudhury and Bandyopadhyay [10], Roy Choudhury and Dutta [11], Sharma and Chouhan [12], Chandrasekharaiah and Srinath [13], Sarkar and Lahiri [14] and Bachher et al. [MME15]. The effect of magnetic field in generalized thermoelasticity with internal heat source in half space was investigated by Othman et al. [16]. Pal and Acharya [17] studied the effects of inhomogeneity on the surface waves in anisotropic media. Recently, Pal et al. [18] investigated the wave propagation in an inhomogeneous anisotropic generalized thermoelastic solid. They have also shown by graphically that quasiP wave, quasiS wave and thermal wave are discontinuous at certain angle and with a jump as well.
We know that materials in the earth are not homogeneous although their elastic properties vary with depth from one region to another. The variation may be gradual; there are also discontinuities that separate media with different densities and elastic properties. Anisotropy causes the largest variation of seismic velocities and changes in the direction of seismic waves. Achenbach [19] studied reflection and transmission of wave in infinite elastic plate. Several investigations relating to reflection and transmission of elastic waves in anisotropic media have been studied by Nayfeh [20], Pal and Chattopadhyay [21], Chattopadhyay and Rogerson [22], Sharma [23] and Chattopadhyay et al. [24]. Mensch and Rasolofosaon [25] studied the elastic wave velocities in anisotropic media, generalizing Thomson’s parameters, $\delta $ and $\gamma $. Abbas and Othman [26] investigated the propagation of plane waves in fiberreinforced, anisotropic halfspace under effect of hydrostatic initial in LS model. The analysis of Lame waves in anisotropic thin plates in generalized thermoelasticity was discussed by Verma [27]. Zhou and Greenhalgh [28], Grechka [29] studied elastic wave group velocities for (generalized) anisotropic medium. The petrophysical study of velocity of waves in anisotropic shale was analyzed by Vernik and Liu [30], Kumar and Gupta [31] investigated the plane wave propagation in anisotropic thermoelastic medium having fractional order derivative and void in the context of three phase lag model and two phase lag model. Recently Othman et.al. [32] studied the effect of rotation on three dimensional generalized thermoelasticity in the context of GreenNagdhi type II for homogeneous isotropic elastic half space.
The thermoelastic stress behavior and strain calculations due to timedependent thermal perturbation in homogeneous plates have significant applications in tectonic movements of more homogeneous rigid plates e.g., basaltic oceanic plates subjected to heat sources of hot magmatic plumes of deeper mantle origin. Thus the deduction and modifications of thermoelastic stresses in proportion to the degree of reheating of the elastic lithosphere are explained in various hotspot thermal models (Zhu and Wiens [33]). The aim of the present research article to study the distribution of stresses, strains and temperature for an anisotropic half space subjected to a time dependent heat source on the boundary of the space which is traction free in the context of GreenNaghdi model – II. Normal mode analysis technique and eigenvalue approach have been used to solve the problem. Finally, numerical results are presented graphically and analyzed. Some applications have been also given.
In the absence of body forces and inner heat sources, the field equations for linear thermoelastic homogeneous anisotropic body in the context of GreenNagdhi model II [9], Othman et al. [32] are as follows:
The equations of motion:
Heat conduction equation of Green Nagdhi theory of type II:
The DuhamelNeumann constitutive equations are:
Strain – displacement relation:
The comma notation is used for derivatives with respect to space variables ${x}_{i}$ and superimposed dot represents time differentiation.
We shall consider a triclinic linear thermoelastic anisotropic halfspace solid which fills the region $\mathrm{\Omega}=\left\{({x}_{1},{x}_{2},{x}_{3}):\mathrm{}0\le {x}_{1}\mathrm{\infty},\mathrm{}\mathrm{\infty}{x}_{2}\mathrm{\infty},\mathrm{}\mathrm{\infty}{x}_{3}\mathrm{\infty}\right\}$ and subjected to time dependent heat sources on the boundary plane to the surface ${x}_{1}=0$. The body is initially at rest and the surface ${x}_{1}=0$ is assumed to be traction free.
For three dimensional plane waves in a homogeneous anisotropic elastic medium, the components of displacement vector have the form:
where $t$ is the time variable and ${x}_{i}$ ($i=$1, 2, 3) denotes the respective orthogonal Cartesian coordinate axes. Using Hooke’s law, the stressstraintemperature relations in a triclinic medium can be written as follows:
The equations of motion in absence of body forces and heat sources are as follows:
With the help of Eq. (5) and (6), equations of motion (7) become:
The generalized heat conduction Eq. (2) is written as:
To transform the above equations in nondimensional forms, we introduce the following nondimensional variables:
where $l$ is some standard length.
Using the parameters defined in Eq. (10), the nondimensional forms of the equations of motion, heat conduction equation and stress components can be obtained as (omitting primes for convenience):
where:
For the solution of the Eqs. (11) and (12), the physical variables can be decomposed in terms of normal modes [14] in the following form:
where $i=\sqrt{1}$, $\omega $ is the angular frequency and $a$, $b$ are the wave numbers along ${x}_{2}$ and ${x}_{3}$ directions respectively.
Substituting from Eq. (14) in Eqs. (11)(13), we obtain (omitting ‘*’ for convenience):
where ${a}_{ij}$, ${b}_{ij}$, ${m}_{ij}$ and ${h}_{ij}$ ($i$, $j=$1, 2, 3) are given in the Appendix 1.
Eqs. (15)(18) can be written in vectormatrix differential equation [14, 34] as follows:
where $\underset{\_}{v}\left({x}_{1}\right)={\left[{u}_{1}{u}_{2}{u}_{3}\theta {u}_{\mathrm{1,1}}{u}_{\mathrm{2,1}}{u}_{\mathrm{3,1}}{\theta}_{,1}\right]}^{T}\left({x}_{1}\right)$, $\underset{\_}{A}=\left[\begin{array}{ll}{L}_{11}& {L}_{12}\\ {L}_{21}& {L}_{22}\end{array}\right]$.
In the coefficient matrix $\underset{\_}{A}$ of order 8, ${L}_{11}$ is the null matrix of order 4, ${L}_{12}$ is the identity matrix of order 4 and the matrices ${L}_{21}$, ${L}_{22}$ are given in the Appendix 1.
For the solution of the vectormatrix differential Eq. (25), we apply the method of eigenvalue approach as in Santra et al. [35]. The characteristic equation of matrix $\underset{\_}{A}$ is given by:
The roots (eigenvalues of the matrix $\underset{\_}{A}$) of the characteristic Eq. (26) are of the form $\lambda =\pm {\lambda}_{i}$ ($i=$1, 2, 3, 4).
The eigenvector ${\underset{\_}{X}}_{\lambda}$ corresponding to the eigenvalue $\lambda $ can be calculated as:
where:
and ${f}_{ij}$ ($i$, $j=$ 1, 2, 3) are given in the Appendix 1.
From Eq. (27), we can calculate the eigenvalue ${\underset{\_}{X}}_{i}\mathrm{}[i=1\mathrm{}(1\left)\mathrm{}8\right]$ corresponding to the eigenvalue $\lambda ={\lambda}_{i}\mathrm{}[i=1\mathrm{}(1\left)\mathrm{}8\right]$. For our further reference, we use the following notations:
As in Lahiri et al. [36], the general solution of Eq. (25) which is regular as ${x}_{1}\to +\mathrm{\infty}$ can be written as:
where the terms containing exponential of growing nature in the space variables ${x}_{1}$ has been discarded due to the regularity condition of the solution at $+\mathrm{\infty}$ and the arbitrary constants ${A}_{i}$ are to be determined from the boundary conditions of the problem.
Thus, the field variables can be written from Eq. (29) for ${x}_{1}\ge 0$ as:
The simplified form of Eqs. (31)(36) can be written as:
where ${R}_{ij}={R}_{ij}\left({x}_{1}\right)$, $[i=1\mathrm{}(1)\mathrm{}6,\mathrm{}j=1\mathrm{}(1\left)\mathrm{}4\right]$ are given in the Appendix 2.
In order to determine the arbitrary constants ${A}_{i}$, we need to consider the boundary conditions at the surface ${x}_{1}=$ 0. The boundary conditions are taken as follows [14]:
I. Mechanical Boundary Condition: the boundary of the halfspace ${x}_{1}=$0 has no traction everywhere i.e.:
II. The thermal boundary condition is taken as:
where ${q}_{n}$ denotes the normal components of the heat flux vector, $\gamma $ is the Biot’s number, $\gamma \to 0$ corresponding thermally insulated boundary and $\gamma \to +\mathrm{\infty}$represents isothermal boundary condition. The function $r(0,{x}_{2},{x}_{3},t)$ represents the intensity of the applied heat sources. With the help of Eq. (14), Eqs. (38) and (39) become (omitting ‘*’ for convenience):
Substituting from the boundary Eq. (40) and (41) into the Eqs. (30)(33), we get following simultaneous equations satisfy by ${A}_{1}$, ${A}_{2}$, ${A}_{3}$ and ${A}_{4}$:
Solving the above systems of four Eq. (42), we get: ${A}_{i}={\mathrm{\Delta}}_{i}/\mathrm{\Delta}$ ($i=$1, 2, 3, 4), where ${\mathrm{\Delta}}_{i}$ and $\mathrm{\Delta}$ are given in Appendix 2.
In view of illustrating the theoretical results obtained, we now present some numerical results. Since $\omega $ is complex, we take $\omega ={\omega}_{0}+i\varsigma $. The numerical constants are given in Table 1.
Table 1. The numerical constants
Constants

Values

Constants

Values

${c}_{11}$

16.248 GPa

${c}_{22}$

11.88 GPa

${c}_{33}$

12.216 GPa

${c}_{12}$

1.48 GPa

${c}_{13}$

2.4 GPa

${c}_{14}$

–1.152 GPa

${c}_{15}$

0 GPa

${c}_{16}$

–0.561 GPa

${c}_{23}$

1.032 GPa

${c}_{24}$

0.912 GPa

${c}_{25}$

1.608 GPa

${c}_{26}$

1.248 GPa

${c}_{34}$

–0.672 GPa

${c}_{35}$

0.216 GPa

${c}_{36}$

–0.216 GPa

${c}_{44}$

5.64 GPa

${c}_{45}$

2.16 GPa

${c}_{46}$

0 GPa

${c}_{55}$

5.88 GPa

${c}_{56}$

0 GPa

${c}_{66}$

6.91 GPa

$\rho $

2.4 kgm^{1}

${\epsilon}_{1}$

0.0221

${\epsilon}_{2}$

0.0143

${\epsilon}_{3}$

0.0174

${k}_{11}^{*}$

1.13×10^{2} Wm^{1} deg^{1}

${k}_{22}^{*}$

1.17×10^{2} Wm^{1} deg^{1}

${k}_{33}^{*}$

1.21×10^{2} Wm^{1} deg^{1}

In order to study the characteristic of stresses, strains and temperature, we have drawn several graphs for different values of the space variable ${x}_{1}$, time $t$, ${r}^{\mathrm{*}}$ and $\omega $, we conclude the following observations:
1) In Fig. 1 and 2 we see the variation of dimensionless stress components, for fixed values of $\omega =$ 4, ${r}^{*}=$ 20 and $t=$0.8 verses space variable ${x}_{1}$.
• The nature of normal and shearing stresses are almost same with respect to wave propagation.
• The numerical values of ${\tau}_{11}$, ${\tau}_{22}$ and ${\tau}_{33}$ gradually increase within the region 0$\le {x}_{1}\le $0.3, then gradually decrease and finally vanish as ${x}_{1}$ increases further.
• The numerical value of ${\tau}_{11}$_{}is much higher than ${\tau}_{22}$ and ${\tau}_{33}$ near the stress free boundary ${x}_{1}=$0.
• The nondimension shearing stresses${\tau}_{12}\text{,}$${\tau}_{13}$ and ${\tau}_{23}$ start from nonzero value and continuously decrease and finally tends to zero as ${x}_{1}$ increases.
Fig. 1. Distribution of Stresses for $t=$0.8 and $\omega =$4 verses ${x}_{1}$
Fig. 2. Distribution of Stresses for $t=$0.8 and $\omega =$4 verses ${x}_{1}$
Fig. 3. Distribution of Shearing Strains for $t=$0.3 and $\omega =$3 verses ${x}_{1}$
Fig. 4. Distribution of Shearing Strains for $t=$0.3 and $\omega =$3 verses ${x}_{1}$
Fig. 5. Distribution of temperature for $\omega =$2 and ${x}_{2}={x}_{3}=$0.5 verses ${x}_{1}$
2) In Fig. 3 and 4 we notice the variation of dimensionless strain components for fixed values of $\omega =$ 3, ${r}^{*}=$ 20 and $t=$0.6 verses space variable ${x}_{1}$.
• Absolute values of strain components gradually decrease as space variable ${x}_{1}$ increases and finally vanish.
• The strain components ${e}_{11}$, ${e}_{22}$ and ${e}_{12}$_{}are_{}extensive whereas_{}${e}_{33}$_{}and ${e}_{23}$_{}are compressive.
• The characteristic of ${e}_{11}$, ${e}_{22}$ and ${e}_{12}$ are same with respect to wave propagation.
• The nondimensional shearing strain components ${e}_{13}$_{}is compressive within the region 0$\le {x}_{1}\le $0.15 and extensive beyond ${x}_{1}\ge $ 0.15 and finally vanish.
3) Fig. 5 represents the variation of nondimensional temperature $\theta $ for fixed time, when $\omega =$ 2, ${r}^{\mathrm{*}}=$ 20 and ${x}_{2}={x}_{3}=\mathrm{}$0.5 verses ${x}_{1}$.
• Temperature gradually decreases as space variable ${x}_{1}$ increases for all time.
• For fixed ${x}_{1}$, $\theta $ gradually increases as time t increases.
4) Figs. 69 represent the variations of stresses and strains for fixed time when ${r}^{\mathrm{*}}=$ 20 and ${x}_{1}={x}_{2}={x}_{3}=$ 0.5 verses $\omega $ ($\le $1).
• From these figures it is clear that ${\tau}_{22}$ and ${\tau}_{12}$ (normal and shearing stresses), ${e}_{22}$ and ${e}_{13}$ (normal and shearing strains) are discontinuous in the neighborhood of $\omega =$ 0.6 for $t=$ 0.1, $t=$ 0.5 and $t=$ 0.8.
• ${\tau}_{22}$ is extensive except in the region 0.58 $\le \omega \le $ 0.64 for all $t=$ 0.1, $t=$ 0.5 and $t=$ 0.8.
• ${\tau}_{12}$ is compressive except in the region 0.57 $\le \omega \le $ 0.59 for all $t=$ 0.1, 0.5 and 0.8.
• From Fig. 8, it is clear that ${e}_{22}$ is always positive within the region 0 $\le \omega \le $ 1 although it has a discontinuity at $\omega $ 0.59.
• Fig. 9 depicted that ${e}_{13}$ is always negative within the region 0 $\le \omega \le $ 1 although it has a discontinuity at $\omega =$ 0.59.
• ${\tau}_{22}$, ${\tau}_{12}$, ${e}_{22}$ and ${e}_{13}$ are maximum (absolute value) for $t=$ 0.8 within the region 0 $\le \omega \le $1.
• Nature of discontinuities of ${\tau}_{11}$, ${\tau}_{33}$, ${\tau}_{23}$ and ${\tau}_{13}$ are almost same as ${\tau}_{22}$ and ${\tau}_{12}$.
• The discontinuities of other strain components and ${e}_{11}$, ${e}_{33}$, ${e}_{12}$ and ${e}_{23}$ are also same as ${e}_{22}$ and ${e}_{13}$.
Fig. 6. Distribution of ${\tau}_{22}$ for fixed ${x}_{1}={x}_{2}={x}_{3}=$ 0.5 and ${r}^{\mathrm{*}}=$20 for different values of $\omega $
Fig. 7. Distribution of ${\tau}_{12}$ for fixed ${x}_{1}={x}_{2}={x}_{3}=$ 0.5 and ${r}^{\mathrm{*}}=$ 20 for different values of $\omega $
Fig. 8. Distribution of ${e}_{22}$ for fixed ${x}_{1}={x}_{2}={x}_{3}=$ 0.5 and ${r}^{\mathrm{*}}=$20 for different values of $\omega $
Fig. 9. Distribution of ${e}_{13}$ for fixed ${x}_{1}={x}_{2}={x}_{3}=$ 0.5 and ${r}^{\mathrm{*}}=$20 for different values of $\omega $
5) Figs. 1012 depict the distribution of stresses ${\tau}_{11}$, ${\tau}_{12}$ and ${\tau}_{23}$ for 0$<\omega \le $1 and time t in the fixed plane ${x}_{1}=$ 0.3 when ${r}^{\mathrm{*}}=$ 200.
• Fig. 10 shows that normal stress ${\tau}_{11}$ is discontinuous within 0.59$\le \omega \le $0.61 for all values of time $t$ (0 $<t<$0.3). Numerical values of ${\tau}_{11}$ slowly increases with time for fixed $\omega $. On the other hand for fixed time $t$, ${\tau}_{11}$ changes rapidly when 0.61$\le \omega \le $1.0 for 0 $<t\le $ 0.3.
• From Fig. 11 it is clear that shearing stress ${\tau}_{12}$ is compressive for 0 $\le \omega \le $1.0 and 0 $<t<$0.3 except at the point of discontinuity 0.58 $<\omega <$0.59. The characteristic of ${\tau}_{12}$ is same for all time when $\omega $ is fixed and vice versa.
• Fig. 12 represents the distribution of the shearing stress ${\tau}_{23}$ which is extensive for 0 $<\omega \le $ 1 and 0 $<t<$ 0.3. It can be noticed that ${\tau}_{23}$ is discontinuous within 0.58 $<\omega <$ 0.60. ${\tau}_{23}$ gradually decreases for fixed time t when 0.2 $<\omega <$0.57. Beyond the discontinuity region for fixed $\omega $, ${\tau}_{23}$ steadily increases as time t increases._{}The numerical value of ${\tau}_{23}$ gradually decreases for fixed time as $\omega $ increases.
• The nature of ${\tau}_{13}$ is same as ${\tau}_{23}$_{.}
• The nature of wave propagation of ${\tau}_{22}$ and ${\tau}_{33}$ are same as ${\tau}_{11}$.
Fig. 10. Distribution of ${\tau}_{11}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 11. Distribution of ${\tau}_{12}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 12. Distribution of ${\tau}_{23}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 13. Distribution of ${e}_{33}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
6) Figs. 1316 represent distribution of strains ${e}_{33}$, ${e}_{12}$, ${e}_{23}$ and_{}${e}_{13}$ for $\omega $ (≤ 1) and time $t$ in the fixed plane ${x}_{1}=$ 0.3 when ${r}^{\mathrm{*}}=$ 200.
• Fig. 13 shows that the normal strain components ${e}_{33}$ is discontinuous for 0.58 $<\omega <$ 0.60 and 0 $<t\le $ 0.3. Also we see that ${e}_{33}$ gradually decreases for fixed time when 0.2 $<\omega <$ 0.56. For fixed $\omega $, ${e}_{33}$ steadily increases as time $t$ (0 $<t\le $ 0.3) increases.
• Fig. 14 display the distribution of strain components ${e}_{12}$ which is discontinuous for 0.58 $<\omega <$ 0.60 and 0 $<t\le $0.3. For fixed time $t$, ${e}_{12}$ gradually decreases within the region 0.2 < $\omega $ ≤ 0.40 and then slowly increases in 0.4 $<\omega \le $ 0.58. After the location of the discontinuity, ${e}_{12}$ gradually increases as $\omega $ increases. Nothing significant changes can be noticed for fixed $\omega $ when time $t$ changes.
• Fig. 15 depicts that the strain component ${e}_{23}$ is discontinuous when 0.56 $<\omega <$ 0.60 for all time 0 $<t\le $ 0.3. Also we can notice that ${e}_{23}$ is positive like ${e}_{33}$ for 0 $<\omega \le $1 and 0 $<t\le $0.3. For fixed $\omega $, ${e}_{23}$ increases as time t increases.
• Fig. 16 represents the distribution of strain component ${e}_{13}$ which is discontinuous within the region 0.58 $<\omega <$ 0.60 for all time 0 $<t\le $ 0.3.
Fig. 14. Distribution of ${e}_{12}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 15. Distribution of ${e}_{23}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 16. Distribution of ${e}_{13}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 17. Distribution of $\theta $ for fixed ${x}_{1}={x}_{2}={x}_{3}=$ 0.8, ${r}^{\mathrm{*}}=$ 200 and different values of $\omega $, $t$
7) Fig. 17 displays the distribution of temperature $\theta $ for different values of $\omega $ and time $t$. For fixed time, $\theta $ gradually decreases for 0 $<\omega <$ 0.56. Temperature is maximum for all time 0.56 $<\omega <$ 0.60 and then gradually decreases. For fixed $\omega $, $\theta $ slowly increases as time $t$ increases.
8) Figs. 1820 are drawn to show the distribution of normal and shearing stresses for 0 $<\omega \le $ 10 and 0 $<t\le $ 0.5 in the fixed plane ${x}_{1}=$ 0.3 when ${r}^{\mathrm{*}}=$ 200.
• From Fig. 18 it is clear that significant changes occur within 3.5 $<\omega <$ 7.5 and 2.5$\le t\le $0.4. For fixed $\omega $, ${\tau}_{11}$ gradually increases as time $t$ (0.25$\le t\le $0.45) increases and gradually decreases for fixed time when 0 $<\omega <$ 10.
• Fig. 19 shows that shearing stress ${\tau}_{12}$ gradually increases for fixed $\omega $ (2 $\le \omega \le $10) when $t$ (0 $\le t\le $0.4). It can be noted that ${\tau}_{12}$ is maximum when $\omega =$ 10 and $t=$ 0.4.
• Fig. 20 depicts that for fixed time, ${\tau}_{13}$ gradually decreases as $\omega $ increases which is more prominent for $t=$ 0.4 and 0 $<\omega <$ 8. After attending the minimum value ${\tau}_{13}$ gradually increases for 8 $<\omega <$ 10 and 0.35 $\le t\le $0.4.
• Nature of ${\tau}_{22}$ and ${\tau}_{33}$ are almost same as ${\tau}_{11}$.
9) Figs. 2124 show the distribution of strains in the fixed plane ${x}_{1}=$ 0.3 when ${r}^{\mathrm{*}}=$ 200 for different values of $\omega $ and $t$.
Fig. 18. Distribution of ${\tau}_{11}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 19. Distribution of ${\tau}_{12}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 20. Distribution of ${\tau}_{13}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 21. Distribution of ${e}_{11}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 22. Distribution of ${e}_{33}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 23. Distribution of ${e}_{12}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
• Figs. 21 and 22 represent the distributions of the normal strain components. We notice that ${e}_{11}$ is negative for all 0 $<\omega \le $ 10 and 0 $<t<$0.4 while ${e}_{33}$ is positive. Numerical value of ${e}_{11}$ gradually tends to zero when $\omega $ tends to 10 and $t$ tends to 0.4. On the other hand ${e}_{33}$ becomes zero when $\omega =$ 10 and $t=$ 0.4.
• Fig. 23 depicts the distribution of the shearing strain ${e}_{12}$. Characteristic of ${e}_{12}$ is almost same as ${e}_{11}$.
• Fig. 24 shows that for fixed $\omega $, numerical value of ${e}_{13}$ gradually increasing as time $t$ increases. For fixed time $t$, ${e}_{13}$ slowly increases as $\omega $ increases.
10) Fig. 25 displays the temperature distribution for 2 $\le \omega \le $ 10 and 0 $<t\le $0.4. Temperature attains its maximum value when $\omega =$ 6 and $t=$0.4. Temperature increases slowly when 2 $\le \omega \le $ 6 and 0.15 $\le t\le $ 0.4 then gradually decreases.
Fig. 24. Distribution of ${e}_{13}$ for fixed ${x}_{1}=$ 0.3 and different values of$\mathrm{}\omega $, $t$
Fig. 25. Distribution of $\theta $ for fixed ${x}_{1}={x}_{2}={x}_{3}=$ 0.5, ${r}^{\mathrm{*}}=$ 200 and different values of $\omega $, $t$
Subsurface rocks are generally filled with cracks and pore spaces saturated with one or more fluids such as oils, water and gasses which can influence the mechanical behavior of rocks. Thermal expansion of existing fluids due to thermoporoelastic stress field causes gradual increase of fluid pressure in the intergranular spaces. If the fluid pressure (Pf) exceeds lithostatic pressure (Pl) by more than the tensile strength of the rock (usually small) the rock is likely to burst due to hydraulic fracturing and in the process fluid will migrate along the cracks developed (Fig. 26). The migration of oil and gas can be accentuated through these cracks into suitable structural traps producing voluminous oil and gas field in the rocks.
Fig. 26. Schematic diagram showing developments of hydraulic fracturing in matrix of rocks. ${P}_{l}$ = Lithostatic Pressure and ${P}_{f}$ = Fluid Pressure
According to linear elastic fracturing model three distinct modes of fracturing can be generated depending on the three different types of loading (Irwin [37]). In ModeI, the tensile forces are applied normal to the crack plane so that the crack planes are pulled apart enabling the crack more and more open (Fig. 27(a)). In ModeII, the cracked body is loaded by shear forces acting parallel to the crack surfaces, which slide over each other in the applied direction (Fig. 27(b)). In ModeIII the cracked body is also loaded by shear forces but parallel to the crack front and the fracture planes slide over each other out of the plane direction (Fig. 27(c)). In case of ModeIII, a large angle of sliding of rock blocks or plates may indicate a relative rotation of plates, resulting a significant amount of evolution of energy. A distinct discontinuity in the thermoelastic curves shown whenever the $\omega $ value of considerable amount rotated clockwise or anticlockwise (Fig. 27(c)) possibly indicates movements of plate with significant release of energy.
Fig. 27. Three types of fractures modes (Anderson [45])
a) Mode I. Opening mode
b) Mode II. Sliding mode
c) Mode III. Tearing mode
Thus, lithospheric plates, though rigid, must certainly undergo small elastic strains showing timedependent deformations or creep, even in very low levels of differential stress. Thus, the timedependent heat sources appear to produce significant stresses in the lithospheric plates resulting intraplate tectonics (Turcotte [38]). It has been appreciated that the midplate swells are the results of thermal perturbations of intraplate hot spot plumes as the plates move over the deep mantle thermal anomaly (Wilson [39]). The major uncertainties appear to be the variations of minimum depth of reheating with corresponding assumptions of surface heat flow anomalies. These constraints may result conservative estimation of the magnitude of the conductive heating in the elastic lithosphere. But the magnitudes of the calculated temperature perturbations and the related thermoelastic stress accumulation are significant as shown in the mathematical calculations. Shallow reheating depths and larger heat flow anomalies obviously increase the temperature perturbations within the lithosphere. The effect of higher heat flow may be partially compensated in case of deeper reheating depths. Thus, the application of thermoelastic stress analyses is more suitable for relatively thinner and homogeneous younger oceanic lithosphere. The geographical distributions of thermoelastic stresses and their orientations are highly significant for the tectonic evolution of the plates and can be measured by earthquake focal mechanism.
Several thermoelastic stress models applied to hotspot reheating show considerably higher deviatoric stresses for both slow and fast moving plates. Although the thermal stress fields orientations appear to be complex in pattern a horizontal extension at shallow depths and horizontal compressions near the bottom of the elastic lithosphere have been appreciated. The thermal stress configuration depends on the absolute plate velocity. Thus, fast moving plates do not get enough time for conducting heat into the poorly conducting elastic plates and as a result a large deviatoric thermal stress generates far downstream hotspot chain. While a slow moving plate appears to get enough time to interact with the underlying hotspot and creates a more circular and larger thermal field closer to the hotspot location. Obviously, the area of the thermal stress perturbation is much larger for a fast moving plate and has little or no effect to the earthquakes related to hotspots e.g., most of the earthquakes in Howaii Island (Zhu and Wiens [33], Koyanagi et al. [40], Ando [41]). However, in case of slow moving plates the effect of radial thermal stresses closer to the hotspot swells have convincingly shown direct relation to the shallow focus earthquakes (Stewart and Helmberger [42], Nishenko and Kafka [43], Bergman [44]). The focal depths of these earthquakes often mismatch to the predicted depths derived from varied thermal stress models. Thermoelastic stress structures studied in different hotspot swells show an extension perpendicular to the swell axis in shallow depths. The passage of magma through the upper part of the lithosphere is thought to be guided by this extensional stress direction. In case of moderate to slow movements of plates this tensional stresses appear to accumulate considerably long distances downstream from the hotspot location. Volcanic rejuvenation along island arcs may thus result long after the passage of hotspots. During this long time period any kind of changes in the direction of plates or rotation of plate motion, as discussed, may explain the significant changes in the initial hotspot chains as noted a 65 degrees change in direction of hotspot chain in Hawaii Island. To confirm the pattern of maximum thermal stress orientations more thermal stress modeling are appreciated near hotspots in association with earthquakes. Thus, mathematical calculations related to thermoelastic behavior of isotropic plates subjected to temperature perturbations and various boundary conditions may show certain pathways to solve many queries about the platetectonic processes and associated heat sources.
In this paper we derive the exact analytical expression for nondimensional stresses, strains and temperature of a homogeneous anisotropic half space medium of most general symmetry (triclinic) of thermoelasticity without energy dissipation (GN model II) is considered. The time dependent heat source is applied at the boundary of the half space. We observe the following conclusions based on the above analysis.
1) The time dependent heat source has a significant effect on the physical quantities.
2) The maximum changes occur near the heated region.
3) From Figs. 15, it is clear that the numerical values of physical quantities converge to zero as${x}_{1}$increases.
4) It is clear from Figs. 617 that the changes in the values of $\omega $ causes discontinuities of the physical quantities in the neighborhood of 0.56 $<\omega <$ 0.62.
5) Figs. 1825 depicts that the changes in the values of time $t$ and $\omega $ ($>$1) cause significant changes in all the physical quantities.