to preventing catastrophic damage to the environment and people along the coast. In the Impulse model, the

generation of a tsunami depends on the impulse force generated during the event. Understanding tsunamis

begins with simulating the tsunami generation process. This process involves simulating both the motion of

the seafloor and the subsequent motion of the water above for tsunamis caused by underwater earthquakes.

This modeling strategy can mimic all three stages of a tsunami: generation, propagation, and run-up. Three

separate earthquake tsunami events—the 1755 Lisbon earthquake, the 1964 Alaska earthquake, the 2004

Sumatra earthquake are each investigated in this research. To demonstrate its relevance to current events and

various ocean locations, the results of these events are compared and confirmed with the observed data.

Analyzing the parameters used in this modeling study and identifying the parameter that has the most

influence will demonstrate their significance in tsunami generation. The seabed displacement profile, seawater

More than 70% of the Earth's surface is covered by

water, and underwater disruptions resulting from

earthquakes, landslips, volcanic eruptions, or

meteorite impacts can lead to tsunamis, posing

occurrence worldwide, they most frequently

happen in the Pacific Ocean due to seismic and

volcanic activity associated with tectonic plate

boundaries in the Pacific Ring of Fire. The earliest

known tsunami occurred around 479 BC when a

generation phase was simulated using seismic

information on the impulse force produced during

the earthquake. The tsunami propagation phase

was constructed with the aid of the Boussinesq

approximation and solitary wave theory, [7].

During this phase, the complete spectrum of

tsunami characteristic changes was evaluated

along the wave propagation path. The link between

the direction of propagating waves and the

topography of the beach was used to design the

wave height at the coast, tsunami travel duration,

and the tsunami's earliest arrival time, all

influencing how a tsunami behaves.

magnitude of Mw = 9.2, surpassed all previous

records for size, [8], [9]. Early calculations placed

the rupture's length, parallel to the Alaska-Aleutian

trench's strike, between 600 and 800 km, [10], [11]

and its rupture velocity, [12], [13], between 3 and

3.5 km/s. The rupture extended from Prince

Sumatra-Andaman earthquake, with a magnitude

larger than 9.3, occurred when the Indian Oceanic

plate was being subducted beneath the Burma plate

and a portion of the Sunda plate, [15].

calculations indicated a maximum slip height

force by saltwater are the forces opposing the

seabed from displacement, an impulse force (F) is

exerted on the seabed to displace it. The motion of

the shifting seabed can be derived with the use of

deformation. The seafloor is rigid, and

impermeable; the flow is irrotational; the fluid is

ideal; surface tension is disregarded; the pressure

at the free surface is constant; the wave height is

the pressure at the free surface is nil, the wave

height (H) is smaller than the wavelength (L).

Using equation (6) to obtain the pressure changes

at the bottom during the earthquake event, vertical

acceleration is omitted for the long wave

on the seawater owing to the displacement of the

uses a bottom pressure recorder to help determine

the bottom pressure when a tsunami is coming.

The following information is needed for this

on bathymetry, earthquake, and tsunami events,

respectively. Here, the origin is assumed to be the

earthquake epicenter. The distance from the

epicenter is indicated by the length in latitude and

longitude.

The fault boundary line is mathematically

determined using the curve fitting approach, which

aids in discretizing the fault line into intervals

based on rupture velocity. The sea surface

deformation can be calculated by using the

(i) Data on seabed deformation;

(ii) Properties of deep-ocean tsunami waves;

(iii) Tsunami wave characteristics at the shore;

(iv) Travel duration of the tsunami wave to reach

Ocean—are used to test the applicability of the

Impulse modelling method. In order for the

across the three continents of Asia, Europe, and

North America, tsunami wave propagation

analyses were conducted. In this paper, the

following historical tsunami events are analyzed:

The Great Lisbon earthquake struck Portugal, the

Iberian Peninsula, and Northwest Africa on

November 1 at approximately 9:40 local time.

Everything close by was nearly completely

destroyed by the earthquake's aftermath, including

subsequent flames and a wave. Seismologists

believe the Lisbon earthquake had a magnitude of

Table 2. Earthquake information data for the 1755

Lisbon earthquake tsunami (U.S. Geological

Near the epicenter 52.67 m maximum vertical

displacement of the fault was calculated.

values of tsunami generating parameter

Table 7 shows the results of the first tsunami

wave to reach the defined destination by using the

tsunami. From the historical data, the tsunami

table is obtained. By comparing the results of

Table 7. The initial tsunami wave's outcomes at the

tsunami wave height at each location from the

1755 Lisbon earthquake is shown in Table 8.

potentially inconsequential, discrepancy between

historical and estimated tsunami wave heights near

the shore, which can be corrected in the future.

The average percentage of accuracy of estimated

Table 8. Relationship between the historical

(NOAA) and estimated 1755 Lisbon earthquake-

tsunami wave height at the destinations

Fig. 6: Modelling study area of the 1964

Earthquake

tsunami. The slip of the fault is estimated by

Kannamori calculations to be 114.62 m for a dip

vertical displacement of the fault was calculated.

The rupture propagated towards the westward

direction, the South Pacific plate is subducted

under the North American plate. It is determined

that the maximum height of the seafloor increase

and the horizontal displacement are 17.93 m and

113.21 m, respectively. The propagated tsunami

Table 10. 1964 Alaska earthquake – Estimated

values of tsunami generating parameter

westward in the fault boundary, It took 411.47

seconds to reach the rupture length of 699.59 km.

The total time for rupture is estimated as 411.47

Table 11. The seabed deformation along the fault

tsunami wave travel time to reach destinations