 Article
 Open Access
 Published:
Wave propagation in a prestressed anisotropic generalized thermoelastic medium
Earth, Planets and Space volume 62, pages381–390(2010)
Abstract
Four attenuated waves propagate in a prestressed anisotropic generalized thermoelastic medium. The propagation phenomenon in this medium is explained through two systems. One of them, relating the temperature variation in the medium to the particle displacement, is free from the explicit effect of prestress. The other system defines Christoffel equations for the medium. These equations are modified with a matrix, which involves phase direction and prestress components. A propagationattenuation plane is defined for given directions of propagation and attenuation of plane harmonic waves. A finite nondimensional parameter defines the inhomogeneity strength of an attenuated wave. A complex vector is defined to calculate complex velocities of the four waves from the complex roots of a quartic equation. The complex slowness vector of the attenuated wave in the medium is resolved to calculate its propagation (phase) velocity, quality factor and angle of attenuation. Numerical example is considered to study the propagation characteristics of each of the four attenuated waves in the prestressed medium. The presence of anisotropic symmetries and anelasticity are also considered in the medium. Effect of prestress is analyzed on the propagation characteristics of each of the four attenuated waves.
1. Introduction
The crustal rocks are always subjected to stresses. The slow process of creep inside the earth creates a differential stress environment (Hanks and Raleigh, 1980; McGarr, 1980) in the crust, which is responsible for the preferential alignments in the Earth, ranging from mineral orientations, grains, or microcracks to sedimentary folds or regional fractures. The difference between confined tectonic stress and porefluid pressure conducts the flow of fluid to a reservoir through the connected cracks. For the presence of prestress or aligned cracks, an elastic medium behaves anisotropic to wave propagation. Hence, the almost universal presence of anisotropy is observed in many types of rocks at many depths and in many geological and tectonic environments. Two recent studies (Prikazchikov and Rogerson, 2003; Sharma, 2005) contribute to the understanding of wave propagation characteristics of anisotropic materials under initial stress. A latest book by Carcione (2007) explains the importance of anisotropy for wave propagation studies in real materials.
Temperature variations play a significant role in the modification of cracks and the flow of fluid (Paulsson et al., 1994). These modifications in microcracks are responsible for the dynamism around geothermal reservoirs and the sedimentary basins. Stixrude and LithgowBertelloni (2005) have argued the merit of fundamental thermodynamic relations as the basis for the description of thermoelastic behaviour of insitu minerals. Theory of thermoelasticity is used to understand such dynamical systems that involve interactions between mechanical work and thermal changes. Few generalised theories of thermoelasticity have been defined with the introduction of relaxation in temperature field. The theory with one relaxation time (Lord and Shulman, 1967) is termed as LS theory and another with two relaxation times (Green and Lindsay, 1972) is termed as GL theory. Using these modified theories, a large number of problems have been studied on the propagation of plane waves in generalized thermoelastic media (ElKaramany et al., 2002; Sharma et al., 2003). Sharma et al. (2000) studied plane harmonic waves in orthotropic thermoelastic materials. In a recent study (Sharma, 2006), the author considered the general anisotropy in thermoelastic medium and derived a mathematical model to calculate the complex velocities of four waves in the medium. Correspondence was, also, established between the generalised theory of thermoelasticity and the homogenization based (u, p) theory of poroelasticity.
The attenuation of waves in thermoelastic medium comes from the memory effects allowed to heat conduction. However, a more realistic scheme is defined with memory effects allowed for all the constitutive properties of thermoelastic coupling. Giorgi et al. (2001) studied a linear theory for thermoviscoelastic materials but with thermal behaviour represented through the heat conduction equation. Generalizations of ElKaramany et al. (2002) and ElKaramany and Ezzat (2002) described and established relaxation effects in mechanical properties as well as thermomechanical coupling in thermoviscoelastic media. Analogous to the correspondence principle in classical elasticity, the complex values of appropriate constitutive quantities may define the timeharmonic material dissipation in thermoviscoelastic medium (Caviglia and Morro, 2005).
The present study considers the propagation and attenuation of inhomogeneous waves, in a prestressed anisotropic generalized thermoelastic (hereafter, referred as SAGT) medium. In a similar study (Sharma, 2005), the author studied the propagation of homogeneous waves in anisotropic poroelastic medium in the presence of initial stress. But, for the use of Biot’s theory of poroelasticity (Biot, 1956) in this paper, the present work can not be obtained through the poroelasticthermoelastic correspondence (Sharma, 2006). Moreover, the inhomogeneous propagation of attenuated waves is considered in the present work. The complex slowness vector of an inhomogeneous wave is constructed with its propagation direction and inhomogeneity strength. Numerical examples are computed to analyze the propagation characteristics of the attenuated waves in the elastic/viscoelastic media of different anisotropies. Anisotropic variations in propagation characteristics are also analysed for an isotropic medium prestressed with hydrostatic pressure.
2. Definition of the Problem
The problem is to study the wave propagation in SAGT medium. The attenuated waves of four types can propagate in the medium. The polarisations of these waves may not be along the dynamical axes. The problem may be explained through the following steps.

i)
The propagation of plane harmonic waves may be explained through two systems of equations. One of them relates the waveinduced temperature in the medium to the displacement of its particles. The other system provides modified Christoffel equation for the medium. The Christoffel equations are solved into a quartic equation. The four roots of this equation define the complex velocities of the four attenuated waves in SAGT medium.

ii)
The inhomogeneity of an attenuated wave in the medium is represented through an inhomogeneity parameter (δ). For a wave, of given inhomogeneity (value of δ), propagating along a given direction , bisection method is used to calculate a parameter (β) to represent homogeneous attenuation. The parameter β is used, further, to calculate the phase velocity, quality factor and attenuation angle of the wave considered.

iii)
The numerical examples are considered to compute the propagation characteristics (velocity, attenuation) of each of the four inhomogeneous waves in SAGT medium. The presence of anisotropic symmetries and anelasticity in the medium is considered in the numerical models.
3. SAGT (prestressed anisotropic generalized thermoelastic) Medium
3.1 Basic equations
A homogeneous anisotropic thermally conducting elastic solid is considered at a uniform temperature T_{ o }, in the undisturbed state. Insitu equilibrium is obtained in the presence of homogeneous initial stresses defined by a symmetric tensor S_{ ij }. Following Biot (1965) the equations for wave motion in this medium, in the absence of body forces and thermal sources, are given by
where, K_{ ij } is (positivedefinite) thermal conductivity tensor. The thermoelastic coupling is represented by (nonsingular) tensor α_{ ij }. ρ and C_{ e } are density and specific heat at constant strain, respectively. The 1 and 2 values of the index m in Kronecker delta δ_{ jm }, represent, respectively, the LordShulman (LS) and GreenLindsay (GL) theories of thermoelasticity. Two thermal relaxation times are given by τ_{ o } ≥ τ_{1} ≥ 0. u_{ i } are the components of average displacements of the material particles. T denotes variations in the temperature of the medium in disturbed state. ω_{ ij } = (u_{ i,j } − u_{ j,i })/2 are components of rotation. The incremental stresses σ_{ ij } in the medium are expressed as
where, the fourth rank asymmetric tensor c_{ ijkl } (= C_{ jikl } = c_{ ijlk }) represents isothermic elastic constants of the medium. Another property, given by
ensures the existence of strain energy density function for the medium (Biot, 1965). All the indices (except m) can take values of 1, 2, 3. Repeated index implies summation. The dot and comma notations denote (partial) differentiation with respect to time and space, respectively.
3.2 Plane harmonic waves
For propagation of plane harmonic waves, the unknowns (u_{ j } and T) is written as
where, the components (S_{1}, S_{2}, S_{3}) define the polarization vector S for the displacement of the particles in the medium. The vector p = (p_{1}, p_{2}, p_{3}) defines slowness of the waves. Analogous to Sharma (2006), the propagation phenomenon of plane harmonic waves in the SAGT medium is explained through two systems. One of them, given by
relates the displacement (u) of particles to the temperature change (T) in the medium.
The other system represents the modified Christoffel equations and is given by
where, and are the complex relaxation times. The matrix Σ, given by
represents the effect of prestress on the wave propagation in SAGT medium. The absence of prestress components S_{ ij } in relation (6), implies that the prestress has no direct effect on waveinduced temperature T. However, the effect of prestress on the displacement (u_{ i }) results in a change in T. A nontrivial solution of the Christoffel equations is ensured by a determinantal equation. Writing slowness p = N/V, such that row matrix N satisfies NN^{T} = 1, this equation is given by
where, and matrix Z_{ N } = Z(N, N), as defined in Appendix. For thermal conductivity K = K_{ o }K_{ a } with anisotropy defined by matrix K_{ a }, and coupling tensor α = α_{o}α_{ a } with anisotropy defined by matrix α_{ a }, we have and
In Eq. (8), the matrices Y and Σ_{ N } represent the effects of thermoelastic coupling and prestress, respectively, on the propagation of elastic waves. With the substitution of Σ_{ N }= 0, this equation governs the anisotropic propagation of thermoelastic wave (Sharma, 2006). 3.3 Four attenuated waves
Following the procedure explained in Sharma (2006), the determinantal Eq. (8) is solved into a quartic equation in h (= V^{2}). This equation may be written as
The complex coefficients C_{ j }, for a numerical model of SAGT medium, are functions of phase vector N. Four complex roots (say, h_{ j }; j = 1, 2, 3, 4) of this equation explain the existence and propagation of four attenuated waves in SAGT medium. The four waves are identified with the algebraic expressions of these roots. The attenuated waves corresponding to h_{1}, h_{2}, h_{3}, h_{4} are called the qP, qS1, qS2, qT waves, respectively. For any of these four waves, the complex velocity (V) corresponding to the complex vector N is calculated from the corresponding value of h. Thus obtained, slowness vector (i.e., p=N/V) for the wave may be used to calculate its polarization from the system of Eqs. (6).
3.4 Inhomogeneous plane waves
In a dissipative medium, an attenuated wave may be homogeneous or inhomogeneous. An angle between propagation vector and attenuation vector, in general, represents the inhomogeneous character of a plane wave. The phase vector N, in real space, yields same direction for propagation vector and attenuation vector and, hence, represents the homogeneous waves. So, an inhomogeneous wave may be represented, only, with N as a complex (dual) vector.
Consider a plane that contains propagation vector (along, say, ) and attenuation vector of inhomogeneous plane wave. Let, this plane be formed with two orthogonal unit vectors and . The complex slowness vector (p) is, then, expressed as
where, the nondimensional parameter δ measures the inhomogeneity strength of the attenuated wave. A nonzero value of δ, in (−1, 1), represents the deviation of inhomogeneous wave from its homogeneous version (i.e., δ = 0). The coefficient of homogeneous attenuation (β) and propagation velocity (υ) are the real unknowns, to be determined for given propagation direction , orthogonal direction and inhomogeneity parameter δ. The expression p=N/V, such that N.N = 1, of complex slowness vector is used in (10) to yield
Note that, the phase vector N is a vector function of only one (real) unknown, i.e., β. This implies that the complex velocity V = V (N), also, becomes a function of β, such that V^{2} = h(β) = h_{ R } + ıh_{ I }. The complex value h = h(N), for each of the four waves, is available as one of the roots of quartic equation (9). The second equation in (11), then, written as
yields
an equation to be solved for β using a bisection method, and
to calculate υ^{2} for β obtained from (13). A positive h_{ R } and β^{2} < 1 − δ^{2} ensure a positive value for υ^{2}. Equation (13) has a root in , when h_{ I } < 0. If h_{ I } > 0, then, this root lies in . This implies that opposite signs of β and h_{ I } ensures a positive value for υ^{2}.
The coefficient of homogeneous attenuation β is calculated for each of the inhomogeneous waves in SAGT medium. It is used, further, to define quality factor (Q) and angle (γ) of attenuation, as follows.
4. Numerical Examples
Propagation of an attenuated wave is characterised by its phase velocity (υ) and quality factor of attenuation (Q). In general, the inhomogeneity of an attenuating wave is represented through the difference in the directions of its propagation vector and attenuation vector. In other words, an angle (γ) between equiamplitude plane and equiphase plane of an attenuating plane wave represent its inhomogeneous character. To avoid forbidden directions (Krebes and Le, 1994) for γ, an inhomogeneity of an attenuated wave is defined with the nondimensional inhomogeneity parameter (δ). The relation (15) relates the angle γ to the parameter δ. Hence, phase velocity (υ), quality factor (Q) and attenuation angle (γ) are the main propagation characteristics of an inhomogeneous wave. These characteristics are the functions of δ and, in anisotropic media, these are the functions of propagation direction also. Variations of these characteristics with propagation direction explain the anisotropic behaviour of inhomogeneous waves. The value of δ defines a general attenuated wave varying from homogenous propagation (δ = 0) to evanescent wave (β = 0). The arbitrary anisotropy always provides a liberty to consider any realistic anisotropy with symmetries.
The procedures discussed in this study constitute a general mathematical model for propagation of plane harmonic waves in SAGT medium. The use of the derived model in analyzing the propagation characteristics of a realistic thermoelastic medium may be explained through numerical examples. Dolomite rock (Rasolofosaon and Zinszner, 2002) of density 2727 kg/m^{3} is considered as SAGT medium and, in twosuffixed notations, its anisotropic elastic constants (in GPa) are given by
The remaining elements of nonsymmetric elastic tensor c_{ ij } are obtained through the relation defined in Appendix. The amount (in GPa) of initial stress in the medium is assumed through the matrix S = {1,0.11 Z_{2}, 0.09Z_{1};0.11 Z_{2}, 1.1, 0.1 Z_{1}; 0.09Z_{2}, 0.1 Z_{1}, 0.9}. A symmetric matrix {1, .1Z_{2}, .2Z_{1}; .1Z_{2}, 1.1, .15Z_{1}; .2Z_{1}, .15Z_{1}, .9} defines the anisotropies of thermal conductivity (K_{ a }) as well as of thermoelastic coupling (α_{ a }). It may be noted that the values (1, 1), (0, 1) and (0, 0) of (Z_{1}, Z_{2}) represent, respectively, the triclinic, monoclinic and orthotropic anisotropy in the model. Keeping in mind the values for metals, the assumed values for thermal coefficients of SAGT medium are given by T_{ o } = 300°K, α_{ o } = (2.)10^{−5}c_{11}/°K, C_{ e } = 400 J kg^{−1}/°K, K_{ o } = 400 W m^{−1}/°K. The relaxation times are assumed as τ_{ o } = 10^{−9} sec, τ_{1} = 0.95τ_{ o }.
For general direction (θ, ϕ), in threedimensional space, the propagation direction is defined by (sinθ cosϕ, sinθ sinϕ, cosθ). The vertical plane ϕ = 0.34π is the fixed propagationattenuation plane for numerical computation. In this plane, the propagation direction is considered with θ, varying from 0 to 90^{°} and the orthogonal vector is considered along θ + π/2. The three values of δ(= 0.01, 0.1, 0.4) are used to represent the variations in inhomogeneity strength of a wave. The smallest value (0.01) of δ represents a nearly homogeneous (or weakly inhomogeneous) wave. It was noted that the thermoelasticity theory (LS or GL) has only a negligible effect on the propagation characteristics of inhomogeneous waves. Hence, the numerical results are exhibited, only, for GL theory (i.e., m = 2). Three main anisotropies (triclinic, monoclinic, orthotropic) are considered in thermoelasticity as well as initialstress.
Figure 1 exhibits the anisotropic variations of phase velocity (υ), quality factor (Q^{−1}) and attenuation angle (γ) for the inhomogeneous thermoelastic qPwaves. The velocity plots show that the velocity of qPwave decreases with the increase of inhomogeneity (δ). This decrease is largest at θ = 0 but reduces on shifting away from this direction. The near similarity of velocity plots in three columns of the figure implies that the presence of a reflection symmetry in SAGT medium has a very little effect on the velocity of qPwaves. The second row of plots in this figure shows the anisotropic variations of attenuation with the inhomogeneity of wave. It is quite clear from these plots that the attenuation is increasing with the increase of δ. Moreover, the attenuations represented by nearly homogeneous waves (i.e., δ = 0.01) are negligible as compared to the attenuations from inhomogeneous waves. The effect of monoclinic symmetry is observed only for propagation near θ = 0. Q^{−1} is maximum for a value of θ near 40°. For propagation along θ = 90°, the effect of wave inhomogeneity is smallest (almost, negligible) on attenuation. The third row of plots in this figure shows the anisotropic variations of angle between directions of propagation and maximum attenuation. The inhomogeneity parameter has a very little effect on this angle. The qPwaves are nearly evanescent (i.e., γ = π/2) when propagate along θ = 0 and θ = 90^{°}. The evanescent character of these waves, even when they are nearly homogeneous (i.e., δ = 0.01), implies that the value of β is very small and, hence, a very small contribution of homogeneous waves to the total attenuation. The inhomogeneity angle increases on shifting the propagation away from these directions and gets its maximum around θ = 40^{°}. The presence of monoclinic symmetry has a significant effect on γ but only when θ is around 0.
Figure 2 shows the anisotropic variations of the propagation characteristics of qS1wave in SAGT medium. The velocity (υ) decreases with the increase of δ, mainly, near θ = 0. The anisotropic symmetries may not affect the magnitude of velocity much but do affect its variations with propagation direction. The magnitude of Q^{−1} increases with the increase of δ. For nearly homogeneous (or weakly inhomogeneous) waves (i.e., δ = 0.01),the value of Q^{−1} is negligible and remain unchanged with the change in propagation direction. This implies that contribution of homogeneous waves to attenuation is negligible. Presence of anisotropic symmetry affects the magnitude as well as directional variations of velocity of qS1wave. The larger value of δ (i.e., 0.4) shows its effect on γ. The value of γ near 90° implies the near evanescent and strongly inhomogeneous nature of qS1waves.
The plots in Fig. 3 explains the anisotropic variations of υ, Q^{−1} and γ for qS2wave. The effect of inhomogeneity parameter is similar to as observed for qS1wave. However, the variations with propagation directions are quite different, mainly in the presence of anisotropic symmetries.
The anisotropy in the medium has a significant effect on the propagation of qS2wave. The behavior of anisotropic variations seem to be quite sensitive to the larger (between 0.1 to 0.4) values of δ. Similar to qS1wave, the value of γ is around 90^{°}.
Figure 4 shows the propagation characteristics of slowest (qT) wave in the medium, with propagation direction (θ) and inhomogeneity parameter (δ). These variations in case of triclinic anisotropy are much different from those for monoclinic and orthotropic anisotropies. The qTwave experience the largest (Q^{−1} is around 1) attenuation among all the four waves in the medium. The angle (γ) between propagation and attenuation direction is much away from 90° and varies a lot with the value of δ. For δ = 0.01, the zero value of γ implies that the qTwave propagates as a homogeneous wave. That means the homogeneous qTwaves are contributing much to the attenuation, contrary to the three faster waves in the medium. The attenuation (Q^{−1}) and inhomogeneity angle (γ) of the weakly inhomogeneous waves are not changing with the direction of propagation.
The attenuations exhibited in above figures are due to the thermoelastic character of the medium. The other source of the intrinsic attenuation may be the anelastic nature of the medium. The complex elastic constants for a viscoelastic medium are defined as c_{ ij } (1 − ı∊). To check the effect of anelasticity, the propagation characteristics are computed for three values (0, 0. 02, 0. 05) of ∊. The variations of υ, Q^{−1}, γ of the four waves with propagation direction are exhibited in Fig. 5. The waves are inhomogeneous (δ = 0.2) and medium is general anisotropic (i.e., triclinic). The first row of plots in this figure implies that viscoelasticity in the medium may not have any effect on the phase velocities of any of the four waves. However, attenuation angles γ and Q^{−1} of three faster waves are increasing with ∊. The only exception is qTwave, which is not affected by the anelastic nature of the medium.
The plots in Fig. 6 present the percent change in velocity (υ), attenuation amount (Q^{−1}) and attenuation angle (γ) due to the presence of prestress. Three values of ∊ = 0, 0.02, 0.05 represent the variations in the anelastic character of the medium. Numerical results show that the slowest (qT) wave is unaffected by the presence or absence of prestress. Hence, in Fig. 6, the results are exhibited, only, for three faster waves. From the first row of plots it is noted that effect of prestress is more on slower waves. However, the change is not more than 0.3 percent and hence may not be significant. The plots in the second row in the figure imply that the effect of prestress is quite large on the attenuation but only for propagation along some particular directions. The effect of prestress on Q may change with the viscoelastic character of the medium. Similar to velocities, the effect of prestress on attenuation angle may not be considered significant.
The anisotropy in the medium is of two types. One is inherent elastic anisotropy and other is due to the presence of prestress. The stressinduced anisotropy may, also, be observed in an isotropic elastic medium. So, the computations are carried out to calculate the propagation characteristics of attenuated waves in an isotropic thermoelastic medium (with nonzero elastic constants c_{11} = c_{22} = c_{33} = 110 GPa, c_{44} = c_{55} = c_{66} = 24 GPa, c_{12} = c_{21} = c_{13} = c_{31} = c_{23} = c_{32} = c_{11} − 2c_{66}) in the presence hydrostatic prestress (S = I GPa). All the waves are inhomogeneous with δ = 0.2. It is calculated that qPwave and qTwave behave isotropic with constant values of (υ, Q^{−1}, γ),given by (6.224 km/s, 0.02, 87°) and (0.1713 km/s, 1, 26.5°), respectively. However, the effect of stressinduced anisotropy is observed on two splitshear (qS1, qS2) waves. Figure 7 exhibits, the anisotropic variations of υ, Q^{−1} and γ for qS1 and qS2 waves. The anisotropy induced by hydrostatic prestress is affecting mainly the velocities. The presence of anelasticity does not show much effect on this anisotropic behavior.
5. Concluding Remarks
The numerical results in previous section are computed only for some particular numerical models of SAGT medium. Hence, the analysis of these results may not qualify for generalization. However, the few noticeable points may be explained as follows.

i)
The slower is an elastic wave, more it is affected by the presence of anisotropic symmetry. The presence of anisotropic symmetries have a very significant effect on the variations of velocity with propagation direction. The negligible effect of anisotropic symmetry on the velocities of qP and qT waves may indicate that the quasilongitudinal waves are less sensitive to the presence of anisotropic symmetry.

ii)
The attenuations represented by weakly inhomogeneous (i.e., δ = 0.01) faster waves are negligible. This implies that the large attenuation in a dissipative medium may be explained only with strongly inhomogeneous waves. The values of γ near 90^{°} imply the nearevanescent character of inhomogeneous waves in the dissipative medium.

iii)
The qTwaves experience the largest attenuation among all the four waves in the medium. The angle (γ) between propagation and attenuation direction of qTwave is much away from 90^{°} and varies a lot with the value of δ.For δ = 0.01, the significant value of Q^{−1} and zero value of γ implies that attenuated qTwave propagates as a homogeneous wave. That means, homogeneous qTwaves may be able to explain large attenuation also, contrary to the three faster waves in the medium.

iv)
Viscoelasticity in the medium may not have any effect on the phase velocities of any of the four waves. However, the attenuation angles (γ) and coefficients (Q^{−1}) of three faster waves increase with ∊. The exception is qTwave, which is not affected by the anelastic nature of the medium.

v)
The propagation of quasithermal (qT) wave may not be affected with the presence of prestress in SAGT medium. The other three waves may not be changing their velocities and attenuation angle with the presence of prestress. However, prestress may affect the attenuation of these waves but only for few propagation directions. This implies that, to affect the velocities of the waves, the prestress values should be much greater than that assumed in the numerical model.

vi)
The effect of anisotropy induced by hydrostatic prestress in an isotropic thermoelastic medium is observed only on two splitshear (qS1, qS2) waves. The isotropic propagation behavior of other two (qP, qT) waves is not affected by the presence this stressinduced anisotropy.
The work presented relates the geophysical properties (anisotropy, initialstress, thermoelasticity) of a realistic medium to its propagation characteristics (velocities, attenuation, polarizations, phase shift, reflection coefficients). For the presence of anelastic attenuation and anisotropic symmetries, these relations may provide improved constraints on thermal/compositional structure and deformational processes in the interior of Earth. When supported with a real data, these constraints may be used to understand a variety of geophysical problems. Few relevant problems are explained as follows.

a)
Seismic waves generated in Earth’s interior provide images that help us to better understand the pattern of mantle convection that drives plate motions. Anisotropy and dissipation, which also influence seismicwave propagation, may be characterized better to extract additional information on flow directions, temperature variations and the presence of partial melting (Romanowicz, 2008).

b)
The boundary between the core and mantle is one of the most enigmatic regions of Earth’s interior. It holds the key to understand a host of geophysical phenomena—including the formation of plumes in the mantle, interactions between core and mantle, and the ultimate fate of subducting slabs of crust that are driven into the interior by tectonic forces. Investigations of this region largely depend on interpreting the behaviour of seismic waves, which have shown that it is highly complex (Duffy, 2004)

c)
The MgSiO_{3} perovskite, generally accepted to be the major component of the lower mantle. It is found to be highly anisotropic in all portions of the lower mantle and the nature of anisotropy changes significantly with depth. Wentzcovitch et al. (1998) calculated anisotropy of seismic wave velocities as a function of pressure (depth). Anisotropy at the topmost lower mantle can be attributed to the preferred orientation of perovskite.

d)
Knowledge of the elastic properties of the dominant (Mg, Fe, Al)(Si, Al)O_{3} perovskite phase of the Earth’s lower mantle, including the pressure and temperature dependence of the bulk and shear moduli, is critical for analyses of its chemical composition and thermal regime including the significance of the lateral variations of seismic wave speeds (Jackson, 1998; Deschamps and Trampert, 2004; Mattern et al., 2005).

e)
The prediction of predrill overpressure is required for the monitoring of hydrocarbon production in the boreholes (Sayers et al., 2002).

f)
The extent of fracturing in a region of a borehole, which is a vital factor in the extraction of oil and geothermal heat. The information on fracture distribution (from velocity inversion) is used to estimate the anisotropic permeability of the fracture rock system (Gibson and Toksoz, 1990).
References
Biot, M. A., The theory of propagation of elastic waves in a fluidsaturated porous solid, I. Lowfrequency range, II. Higher frequency range, J. Acoust. Soc. Am., 28, 168–191, 1956.
Biot, M. A., Mechanics of Incremental Deformation, John Wiley, New York, 1965.
Carcione, J. M., Wave Fields in Real Media: Wave Propagation in Anisotropic Anelastic, Porous and Electromagnetic Media, Elsevier, Amsterdam, The Netherlands, 2007.
Caviglia, G. and A. Morro, Harmonic waves in thermoviscoelastic solids, Int. J. Engng. Sci., 43, 1323–1336, 2005.
Deschamps, F. and J. Trampert, Towards a lower mantle reference temperature and composition, Earth Planet. Sci. Lett., 222, 161–175, 2004.
Duffy, T. S., Earth science: Deeper understanding, Nature, 430, 409–410, 2004.
ElKaramany, A. S. and M. A. Ezzat, The uniqueness and reciprocity theorems for generalised thermoviscoelasticity with two relaxation times, Int. J. Engng. Sci., 40, 1275–1284, 2002.
ElKaramany, A. S., M. A. Ezzat, and M. I. Othman, Statespace approach to twodimensional generalised thermoviscoelasticity with two relaxation times, Int. J. Engng. Sci., 40, 1251–1274, 2002.
Gibson, Jr. R. L. and M. N. Toksoz, Permeability estimation from velocity anisotropy in fractured rocks, J. Geophys. Res.95, 15643–15656, 1990.
Giorgi, C., M. G. Naso, and E. Vuk, Exponential stability in viscoelastic and elastic systems with thermal memory, Int. J. Differ. Eqs. Appl., 2, 55–91, 2001.
Green, A. E. and K. A. Lindsay, Thermoelasticity, J. Elasticity, 2, 1–7, 1972.
Hanks, B. C. and C. B. Raleigh, The conference on magnitude of deviatoric stresses in the earth’s crust and uppermost mantle, J. Geophys. Res., 85, 6083–6085, 1980.
Jackson, I., Elasticity, composition and temperature of the Earth’s lower mantle: a reappraisal, Geophys. J. Int., 134, 291–311, 1998.
Krebes, E. S. and L. H. T. Le, Inhomogeneous plane waves and cylindrical waves in anisotropic anelastic media, J. Geophys. Res., 99, 23899–23919, 1994.
Lord, H. W. and Y. Shulman, The generalized dynamic theory of thermoelasticity, J. Mech. Phys. Solids, 15, 299–309, 1967.
Mattern, E., J. Matas, Y. Ricard, and J. Bass, Lower mantle composition and temperature from mineral physics and thermodynamic modeling, Geophys. J. Int., 160, 973–990, 2005.
McGarr, A., Some constraints on levels of shear stress in the crust from observation and theory, J. Geophys. Res., 85, 6231–6238, 1980.
Paulsson, B. N. P., J. A. Meredith, Z. Wang, and J. W. Fairborn, The Steepbank crosswell seismic project: Reservoir definition and evaluation of steamflood technology in Alberta tar sands, The Leading Edge, 13, 737–747, 1994.
Prikazchikov, D. A. and G. A. Rogerson, Some comments on the dynamic properties of anisotropic and strongly anisotropic prestressed elastic solids, Int. J. Engng. Sci., 41, 149–171, 2003.
Rasolofosaon, P. N. J. and B. E. Zinszner, Comparison between permeability anisotropy and elasticity anisotropy of reservoir rocks, Geophysics, 67, 230–240, 2002.
Romanowicz, B., Using seismic waves to image Earth’s internal structure, Nature, 451, 266–268, 2008.
Sayers, C. M., G. M. Johnson, and G. Denyer, Predrill porepressure prediction using seismic data, Geophysics, 67, 1286–1292, 2002.
Sharma, M. D., Effect of initial stress on the propagation of plane waves in a general anisotropic poroelastic medium, J. Geophys. Res., 110, B11307, 2005.
Sharma, M. D., Wave propagation in anisotropic generalized thermoelastic medium, J. Thermal Stresses, 29, 629–642, 2006.
Sharma, J. N., V. Kumar, and S. P. Sud, Plane harmonic waves in orthotropic thermoelastic materials, J. Acoust. Soc. Am., 107, 293–305, 2000.
Sharma, J. N., V. Kumar, and D. Chand, Reflection of generalized thermoelastic waves from the boundary of a halfspace, J. Thermal Stresses, 26, 925–942, 2003.
Stixrude, L. and C. LithgowBertelloni, Thermodynamics of mantle mineralsI. Physical properties, Geophys. J. Int., 162, 610–632, 2005.
Wentzcovitch, R. M., B. B. Karki, S. Karato, and C. R. S. Da Silva, High pressure elastic anisotropy of MgSiO3 perovskite and geophysical implications, Earth Planet. Sci. Lett., 164, 371–378, 1998.
Author information
Affiliations
Corresponding author
Appendix A.
Appendix A.
A nonsymmetric square matrix of order six, {c_{ ij }},is used to denote the elastic properties of the medium in twosuffix notations. In the presence of initial stress (S_{ ij }) in the medium, the asymmetry of the elastic tensor (c_{ ij }) is expressed through the relations
Consider two row matrices U and V of three elements each. These matrices define the elements of a square matrix Z(U, V) of order three, as follows.
where V^{T} is the transpose of V and
are square matrices of order three.
Rights and permissions
About this article
Cite this article
Sharma, M.D. Wave propagation in a prestressed anisotropic generalized thermoelastic medium. Earth Planet Sp 62, 381–390 (2010). https://doi.org/10.5047/eps.2009.12.004
Received:
Revised:
Accepted:
Published:
Issue Date:
Key words
 Initial stress
 thermoelastic
 inhomogeneous waves attenuation