JASEM ISSN 1119-8362 Full-text Available Online at J. Appl. Sci. Environ. Manage. September, 2009 All rights reserved www.bioline.org.br/ja Vol. 13(3) 9 - 12 Mathematical Modelling of Tsunami Propagation 1EZE, C. L.; 2UKO, D. E.; 3GOBO, A. E.; 4SIGALO, F. B.; 5ISRAEL-COOKEY, C. 1& 3Institute of Geosciences and Space Technology, Rivers State University of Science and Technology, Port Harcourt, Nigeria. 2& 4Department of Physics, Rivers State University of Science and Technology, Port Harcourt, Nigeria. 5Department of Mathematics and Computer, Rivers State University of Science and Technology, Port Harcourt, Nigeria. [email protected] Phone: 08033108660 ABSTRACT: The generation of tsunamis with the help of a simple dislocation model of an earthquake and their propagation in the basin are discussed. In this study, we examined the formation of a tsunami wave from an initial sea surface displacement similar to those obtained from earthquakes that have generated tsunami waves and its propagation through the sea to the shore. Linear shallow water wave equations were employed to explain the propagation of the waves in the open sea while nonlinear wave equations were introduced to explain the behaviour of the wave near the shore. The influence of the Coriolis force on the propagation of tsunami was shown to become very important when the tsunami travel distance is significant in relations to the earth’s complete rotation time. The group velocity of tsunami waves which is the velocity of wave energy propagation and its independence on the wave number was demonstrated. @ JASEM The term shallow water wave describes a wave which describe tsunami wave generation, propagation and has a wavelength much greater than the depth of the interaction with complicated topography such as bays water it is propagating through. Tsunamis, which or harbours and the resulting flooding has advanced have very long wavelengths (10’s to 100’s km) to the stage where they are useful tools for always travel as shallow water waves even in deep determining the tsunami hazard in local regions. The oceans. Although there are other causes of tsunamis, most common model used to describe tsunami about 90% of tsunamis of the world are bound up generation, propagation and flooding is the linear, with underwater earthquakes (Jaiwal et al., 2008). shallow water, long wave model that neglects both Three stages of tsunami development are usually the shoaling effect of the shore and the Coriolis effect distinguished: (a) formation of a localized initial during a long tsunami travel. Nonlinear wave disturbance and its evolution near the source; (b) equations are very important at the shore where most propagation of waves in the open ocean; (c) of the damages by tsunami are experienced while propagation of waves in shallow water and on the Coriolis effect must be considered for teletsunami. shore. The development of numerical models to 200 180 160 140 120 100 80 60 Shallow-water wave group velocity (m/s) velocity group wave Shallow-water 40 20 0 0 500 1000 1500 2000 2500 3000 3500 4000 Water depth Figure 1.: Tsunami velocity as a function of water depth * Corresponding author: 1Eze, C. L. Mathematical Modelling of Tsunami Propagation JASEM ISSN 1119-8362 Full-text Available Online at J. Appl. Sci. Environ. Manage.10 September, 2009 All rights reserved www.bioline.org.br/ja Vol. 13(3) 9 - 12 about 4 km whereas tsunami wavelengths are 300- 400 km making the treatment of tsunami waves as Tsunami wave propagations shallow waves in the ocean valid (Fuji et al., 2001). The shallow water wave equations describe a number Tsunami waves at the shore of physical features including wave dynamics where Shallow water approximation is valid if the water disturbances in the sea surface height are moving as depth is much less than the wavelength (λ). In this waves. The basic linear shallow water wave equation case, H << λ, kH << 1, and of’ tsunami generation by small bottom deformations in homogeneous ocean of constant depth H tanh(kH ) = kH and nonlinear effects can be neglecting the stresses at the surface and bottom, the neglected. Coriolis force, and the viscous terms are given as: As the long wave with small amplitude enters δU δη shallow coastal waters, the solution contradicts the + gH = 0 (1) assumptions of the shallow water wave equation. δt δx Tsunami wave propagating over the continental shelf towards the shoreline is transformed mainly by δV δη shoaling, refraction and reflection. In this region, + gH = 0 (2) δt δy nonlinearities cannot be neglected anymore and the full nonlinear shallow water equations must be δη δU δV applied to solve the problem (Casulli and Walters + + = 0 (3) 2000). Guyenne and Grilli (2002) have set the limit δt δx δy of shallow-water and deep-water dispersion relations η is the vertical displacement of the water surface at H < λ /11 and H > λ 4 respectively. Detailed above the e quipotential surface, t is elapse bathymetric information and assumed wave length at time, U and V are the horizontal and vertical the shore are required to set these boundaries in the components of the water surface, x and y are the ocean. Tsunami evolution is very important near spatial coordinates of the wave and g is the gravity shore where the waves are dangerous and destructive. acceleration (Li and Raichlen, 2001., Zahibo, et al., The assumptions underlying the tsunami wave 2003). equations at the open sea fail near the shore and the Combining these equations it can be shown that bottom topography must be considered. To obtain a ∂2η solution we assume a simple form for the bottom − gH∇2η = 0 (4) ∂t 2 topography such that The corresponding equation in one-dimension h(x) = −ax (8) derived from equation (4) is: where h(x) is the variable depth of the basin, x axis ∂2η ∂2η is directed to the shoreline and s is a constant. Under − gH = 0 (5) ∂t 2 ∂x2 this condition the tsunami wave takes the form of nonlinear wave equation: This equation has a wave form and we thus introduce i()kx−ϖt ∂η ∂u ∂η a wave solution in the form η ≈ e . Inserting + u + g = 0 (9) this expression into equation (5) we find that ∂t ∂x ∂x i()kx−ϖt ∂η ∂ η ≈ e is a solution if and only if : + []()h +η u = 0 (10) ∂t ∂x ω = gH k (6) where ω is the wave frequency in radian and k is Tsunami equations with Coriolis The equations that neglect the Coriolis acceleration the wave number. can be regarded as valid only as long as the tsunami Equation (6) is the dispersion relation and travel distance remains insignificant in relations to characterizes how the frequency must be related to the earth’s complete rotation time. When a tsunami the wave number in order to fulfill equation (5). propagates over long distances, the Coriolis Using ordinary theory for surface waves, the acceleration terms must be introduced to account for dispersion relation is therefore: 2 the fact that the earth, frame of reference with respect ω = gk tanh()kH (7) to which the wave is propagating, is rotating. This shows that the tsunami waves must be The rotation of the earth can strongly affect the considerably longer than the depth of the ocean for tsunami characteristics near the region of formation the results of their treatment as shallow waves to be of tsunamis. Owing to the rotation of the earth, each valid. The average depth of the Pacific Ocean is moving particle of the water is under the influence of * Corresponding author: 1Eze, C. L. Mathematical Modelling of Tsunami Propagation 11 a Coriolis force. Therefore, tsunami generation is waves will tend to bend towards areas with shallow generally accompanied by the formation of internal water since according to Snell’s law; waves tend to waves and vortical motions (Johnson, 2003). bend towards areas with lower propagation speed. During this process some part of the energy, which is Thus, when long ocean waves enter a coastline the transmitted to the ocean with the seismic bottom wave propagation will change direction such that the motions, accumulates in the region of the waves more or less will come in perpendicular to the disturbance. This leads to a reduction of the coastline. For this reason capes usually receive more barotropic wave energy and tsunami amplitude. The wave power that bays. direction of the tsunami radiation varies and the energy flow transferred by the waves is redistributed The group velocity variation computed from the (Pelinovsky et al., 2001) average depth (4000 m) of the Pacific Ocean to the The integrated equations for linear long waves with shore as the water depth approaches zero is shown in Coriollis force in the spherical coordinate system Figure 1. The group velocity could be as much as 200 (longitude ϕ and latidute θ ) can be shown to be m/s which is about the speed of sound in air. As the wave speed decreases, the wave amplitude increases. ∂Q gH ∂η ϕ = − fQ (11) The amplitude of shallow water waves is ∂t Rsinθ ∂ϕ θ approximately: A C ∂Qθ gH ∂η s = d (17) = − fQθ (12) ∂t R ∂θ Ad Cs f = 2Ωcosθ where As and Cs are shallow water amplitude and velocity, and A and C are deep water amplitude and where R is the radius of the earth, Q is the flow rate d d velocity. This approximation fails for breaking waves and Ω is the rotation vector of the earth otherwise the amplitude would increase to infinity as water depth approaches zero. In order to keep their Phase and group velocities frequency constant, their wavelength decreases.