ABSTRACT
On 26 December 2004, a great earthquake of magnitude of 9.3 had struck the active subduction corridor along the eastern margin of Indian lithosphere. Its epicentre, 3.7◦N 95◦E, lies close to northwest boundary of Sumatra where the trench appear to bend a little and be intersected by nearly northsouth running oceanic feature. Such features entering subduction way act as barriers to cause large stress to build, which eventually released in form of major earthquake (Raval, 2005). As a consequence of great energy release and associated land movements in the marine region, tsunami was produced in the eastern part of the Indian Ocean and spread with speed of approximately 800-900 km per hour on its eastern path. It reached the Andaman-Nicobar Islands, east coast of Sri Lanka and Tamil Nadu and then further north along the east coast up to Orissa and in the west coast up to Quilon. On reaching shallow water along the coast line, the large energy of the seismic waves get transformed into very forceful tidal waves of great height causing vast devastation there.
