For other uses, see Tsunami (disambiguation).

A tsunami (Japanese: 津波 [tsɯnami], lit. 'harbor wave';[1] English pronunciation: /(t)suːˈnɑːmi/ (t)soo-NAH-mee) or tidal wave is a series of water waves (called a tsunami wave train[2]) caused by the displacement of a large volume of a body of water, usually an ocean, but can occur in large lakes. Tsunamis are a frequent occurrence in Japan; approximately 195 events have been recorded.[3] Due to the immense volumes of water and energy involved, tsunamis can devastate coastal regions.

Earthquakes, volcanic eruptions and other underwater explosions (including detonations of underwater nuclear devices), landslides and other mass movements, meteorite ocean impacts or similar impact events, and other disturbances above or below water all have the potential to generate a tsunami.

The Greek historian Thucydides was the first to relate tsunami to submarine earthquakes,[4][5] but understanding of tsunami's nature remained slim until the 20th century and is the subject of ongoing research. Many early geological, geographical, and oceanographic texts refer to tsunamis as "seismic sea waves."

Some meteorological conditions, such as deep depressions that cause tropical cyclones, can generate a storm surge, called a meteotsunami, which can raise tides several metres above normal levels. The displacement comes from low atmospheric pressure within the centre of the depression. As these storm surges reach shore, they may resemble (though are not) tsunamis, inundating vast areas of land. Such a storm surge inundated Burma in May 2008.


The term tsunami comes from the Japanese, meaning "harbor" (tsu, ) and "wave" (nami, ). (For the plural, one can either follow ordinary English practice and add an s, or use an invariable plural as in the Japanese.[6])

Tsunami are sometimes referred to as tidal waves. In recent years, this term has fallen out of favor, especially in the scientific community, because tsunami actually have nothing to do with tides. The once-popular term derives from their most common appearance, which is that of an extraordinarily high tidal bore. Tsunami and tides both produce waves of water that move inland, but in the case of tsunami the inland movement of water is much greater and lasts for a longer period, giving the impression of an incredibly high tide. Although the meanings of "tidal" include "resembling"[7] or "having the form or character of"[8] the tides, and the term tsunami is no more accurate because tsunami are not limited to harbours, use of the term tidal wave is discouraged by geologists and oceanographers.

There are only a few other languages that have a native word for this disastrous wave. In the Tamil language, the word is aazhi peralai. In the Acehnese language, it is ië beuna or alôn buluëk [9] (Depending on the dialect. Note that in the fellow Austronesian language of Tagalog, a major language in the Philippines, alon means "wave".) On Simeulue island, off the western coast of Sumatra in Indonesia, in the Defayan language the word is smong, while in the Sigulai language it is emong.[10]

Generation mechanisms

The principal generation mechanism (or cause) of a tsunami is the displacement of a substantial volume of water or perturbation of the sea.[11] This displacement of water is usually attributed to either earthquakes, landslides, volcanic eruptions, or more rarely by meteorites and nuclear tests [12] [13]. The waves formed in this way are then sustained by gravity. It is important to note that tides do not play any part in the generation of tsunamis, hence referring to tsunamis as 'tidal waves' is inaccurate.

Seismicity generated tsunamis

Tsunamis can be generated when the sea floor abruptly deforms and vertically displaces the overlying water. Tectonic earthquakes are a particular kind of earthquake that are associated with the earth's crustal deformation; when these earthquakes occur beneath the sea, the water above the deformed area is displaced from its equilibrium position [14]. More specifically, a tsunami can be generated when thrust faults associated with convergent or destructive plate boundaries move abruptly, resulting in water displacement, due to the vertical component of movement involved. Movement on normal faults will also cause displacement of the seabed, but the size of the largest of such events is normally too small to give rise to a significant tsunami.

Tsunamis have a small amplitude (wave height) offshore, and a very long wavelength (often hundreds of kilometers long), which is why they generally pass unnoticed at sea, forming only a slight swell usually about Script error above the normal sea surface. They grow in height when they reach shallower water, in a wave shoaling process described below. A tsunami can occur in any tidal state and even at low tide can still inundate coastal areas.

On April 1, 1946, a magnitude-7.8 (Richter Scale) earthquake occurred near the Aleutian Islands, Alaska. It generated a tsunami which inundated Hilo on the island of Hawai'i with a Script error high surge. The area where the earthquake occurred is where the Pacific Ocean floor is subducting (or being pushed downwards) under Alaska.

Examples of tsunami at locations away from convergent boundaries include Storegga about 8,000 years ago, Grand Banks 1929, Papua New Guinea 1998 (Tappin, 2001). The Grand Banks and Papua New Guinea tsunamis came from earthquakes which destabilized sediments, causing them to flow into the ocean and generate a tsunami. They dissipated before traveling transoceanic distances.

The cause of the Storegga sediment failure is unknown. Possibilities include an overloading of the sediments, an earthquake or a release of gas hydrates (methane etc.)

The 1960 Valdivia earthquake (Mw 9.5) (19:11 hrs UTC), 1964 Alaska earthquake (Mw 9.2), and 2004 Indian Ocean earthquake (Mw 9.2) (00:58:53 UTC) are recent examples of powerful megathrust earthquakes that generated tsunamis (known as teletsunamis) that can cross entire oceans. Smaller (Mw 4.2) earthquakes in Japan can trigger tsunamis (called local and regional tsunamis) that can only devastate nearby coasts, but can do so in only a few minutes.

In the 1950s, it was discovered that larger tsunamis than had previously been believed possible could be caused by giant landslides. This phenomena rapidly displace large water volumes, as energy from falling debris or expansion transfers to the water at a rate faster than the water can absorb. Their existence was confirmed in 1958, when a giant landslide in Lituya Bay, Alaska, caused the highest wave ever recorded, which had a height of 524 metres (over 1700 feet). The wave didn't travel far, as it struck land almost immediately, killing 2 people fishing in the bay, whilst the other boat amazingly managed to ride the wave. Scientists named these waves megatsunami.

Scientists discovered that extremely large landslides from volcanic island colapses can generate megatsunami, that can travel trans-oceanic distances.


File:Propagation du tsunami en profondeur variable.gif

While everyday wind waves have a wavelength (from crest to crest) of about Script error and a height of roughly Script error, a tsunami in the deep ocean has a wavelength of about Script error. Such a wave travels at well over Script error, but due to the enormous wavelength the wave oscillation at any given point takes 20 or 30 minutes to complete a cycle and has an amplitude of only about Script error.[15] This makes tsunamis difficult to detect over deep water. Ships rarely notice their passage.

As the tsunami approaches the coast and the waters become shallow, wave shoaling compresses the wave and its velocity slows below Script error. Its wavelength diminishes to less than Script error and its amplitude grows enormously, producing a distinctly visible wave. Since the wave still has such a long wavelength, the tsunami may take minutes to reach full height. Except for the very largest tsunamis, the approaching wave does not break (like a surf break), but rather appears like a fast moving tidal bore.[16] Open bays and coastlines adjacent to very deep water may shape the tsunami further into a step-like wave with a steep-breaking front.

When the tsunami's wave peak reaches the shore, the resulting temporary rise in sea level is termed 'run up'. Run up is measured in metres above a reference sea level.[16] A large tsunami may feature multiple waves arriving over a period of hours, with significant time between the wave crests. The first wave to reach the shore may not have the highest run up.[17]

About 80% of tsunamis occur in the Pacific Ocean, but are possible wherever there are large bodies of water, including lakes. They are caused by earthquakes, landslides, volcanic explosions, and bolides.


If the first part of a tsunami to reach land is a trough—called a drawback—rather than a wave crest, the water along the shoreline recedes dramatically, exposing normally submerged areas.

A drawback occurs because the water propagates outwards with the trough of the wave at its front. Drawback begins before the wave arrives at an interval equal to half of the wave's period. Drawback can exceed hundreds of meters, and people unaware of the danger sometimes remain near the shore to satisfy their curiosity or to collect fish from the exposed seabed. During the Indian Ocean tsunami, the sea withdrew and many people went onto the exposed sea bed to investigate.[citation needed] Photos show people walking on the normally submerged areas with the advancing wave in the background.[citation needed] Few survived.[citation needed]

Scales of intensity and magnitude

As with earthquakes, several attempts have been made to set up scales of tsunami intensity or magnitude to allow comparison between different events.[18]

Intensity scales

The first scales used routinely to measure the intensity of tsunami were the Sieberg-Ambraseys scale, used in the Mediterranean Sea and the Imamura-Iida intensity scale, used in the Pacific Ocean. The latter scale was modified by Soloviev, who calculated the Tsunami intensity I according to the formula

\,\mathit{I} = \frac{1}{2} + \log_{2} \mathit{H}_{av}

where \mathit{H}_{av} is the average wave height along the nearest coast. This scale, known as the Soloviev-Imamura tsunami intensity scale, is used in the global tsunami catalogues compiled by the NGDC/NOAA and the Novosibirsk Tsunami Laboratory as the main parameter for the size of the tsunami.

Magnitude scales

The first scale that genuinely calculated a magnitude for a tsunami, rather than an intensity at a particular location was the ML scale proposed by Murty & Loomis based on the potential energy.[18] Difficulties in calculating the potential energy of the tsunami mean that this scale is rarely used. Abe introduced the tsunami magnitude scale \mathit{M}_{t}, calculated from,

\,\mathit{M}_{t} = {a} \log h + {b} \log R = \mathit{D}

where h is the maximum tsunami-wave amplitude (in m) measured by a tide gauge at a distance R from the epicenter, a, b & D are constants used to make the Mt scale match as closely as possible with the moment magnitude scale.[19]

Warnings and predictions

File:Dart tsunamicover.jpg

Drawbacks can serve as a brief warning. People who observe drawback (many survivors report an accompanying sucking sound), can survive only if they immediately run for high ground or seek the upper floors of nearby buildings. In 2004, ten-year old Tilly Smith of Surrey, England, was on Maikhao beach in Phuket, Thailand with her parents and sister, and having learned about tsunamis recently in school, told her family that a tsunami might be imminent. Her parents warned others minutes before the wave arrived, saving dozens of lives. She credited her geography teacher, Andrew Kearney.

In the 2004 Indian Ocean tsunami drawback was not reported on the African coast or any other eastern coasts it reached. This was because the wave moved downwards on the eastern side of the fault line and upwards on the western side. The western pulse hit coastal Africa and other western areas.

A tsunami cannot be precisely predicted, even if the magnitude and location of an earthquake is known. Geologists, oceanographers, and seismologists analyse each earthquake and based on many factors may or may not issue a tsunami warning. However, there are some warning signs of an impending tsunami, and automated systems can provide warnings immediately after an earthquake in time to save lives. One of the most successful systems uses bottom pressure sensors that are attached to buoys. The sensors constantly monitor the pressure of the overlying water column. This is deduced through the calculation:

\,\! P = \rho gh

P = the overlying pressure in newtons per metre square,
ρ = the density of the seawater= 1.1 x 103 kg/m3,
g = the acceleration due to gravity= 9.8 m/s2 and
h = the height of the water column in metres.

Hence for a water column of 5,000 m depth the overlying pressure is equal to

\,\! P = \rho gh=\left(1.1 \times 10^3 \ \frac{\mathrm{kg}}{\mathrm{m}^3}\right)\left(9.8 \ \frac{\mathrm{m}}{\mathrm{s}^2}\right)\left(5.0 \times 10^3 \ \mathrm{m}\right)=5.4 \times 10^7 \ \frac{\mathrm{N}}{\mathrm{m}^2}=54 \ \mathrm{MPa}

or about 5500 tonnes-force per square metre.

Regions with a high tsunami risk typically use tsunami warning systems to warn the population before the wave reaches land. On the west coast of the United States, which is prone to Pacific Ocean tsunami, warning signs indicate evacuation routes. In Japan, the community is well-educated about earthquakes and tsunamis, and along the Japanese shorelines the tsunami warning signs are reminders of the natural hazards together with a network of warning sirens, typically at the top of the cliff of surroundings hills [20].

The Pacific Tsunami Warning System is based in Honolulu, Hawaiʻi. It monitors Pacific Ocean seismic activity. A sufficiently large earthquake magnitude and other information triggers a tsunami warning. While the subduction zones around the Pacific are seismically active, not all earthquakes generate tsunami. Computers assist in analysing the tsunami risk of every earthquake that occurs in the Pacific Ocean and the adjoining land masses.

File:Tsunami wall.jpg
File:Tsunami Evacuation Route signage south of Aberdeen Washington.jpg

As a direct result of the Indian Ocean tsunami, a re-appraisal of the tsunami threat for all coastal areas is being undertaken by national governments and the United Nations Disaster Mitigation Committee. A tsunami warning system is being installed in the Indian Ocean.

Computer models can predict tsunami arrival, usually within minutes of the arrival time. Bottom pressure sensors relay information in real time. Based on these pressure readings and other seismic information and the seafloor's shape (bathymetry) and coastal topography, the models estimate the amplitude and surge height of the approaching tsunami. All Pacific Rim countries collaborate in the Tsunami Warning System and most regularly practice evacuation and other procedures. In Japan, such preparation is mandatory for government, local authorities, emergency services and the population.

Some zoologists hypothesise that some animal species have an ability to sense subsonic Rayleigh waves from an earthquake or a tsunami. If correct, monitoring their behavior could provide advance warning of earthquakes, tsunami etc. However, the evidence is controversial and is not widely accepted. There are unsubstantiated claims about the Lisbon quake that some animals escaped to higher ground, while many other animals in the same areas drowned. The phenomenon was also noted by media sources in Sri Lanka in the 2004 Indian Ocean earthquake.[21][22] It is possible that certain animals (e.g., elephants) may have heard the sounds of the tsunami as it approached the coast. The elephants' reaction was to move away from the approaching noise. By contrast, some humans went to the shore to investigate and many drowned as a result.

It is not possible to prevent a tsunami. However, in some tsunami-prone countries some earthquake engineering measures have been taken to reduce the damage caused on shore. Japan built many tsunami walls of up to Script error to protect populated coastal areas. Other localities have built floodgates and channels to redirect the water from incoming tsunami. However, their effectiveness has been questioned, as tsunami often overtop the barriers. For instance, the Okushiri, Hokkaidō tsunami which struck Okushiri Island of Hokkaidō within two to five minutes of the earthquake on July 12, 1993 created waves as much as Script error tall—as high as a 10-story building. The port town of Aonae was completely surrounded by a tsunami wall, but the waves washed right over the wall and destroyed all the wood-framed structures in the area. The wall may have succeeded in slowing down and moderating the height of the tsunami, but it did not prevent major destruction and loss of life.[23]

Natural factors such as shoreline tree cover can mitigate tsunami effects. Some locations in the path of the 2004 Indian Ocean tsunami escaped almost unscathed because trees such as coconut palms and mangroves absorbed the tsunami's energy. In one striking example, the village of Naluvedapathy in India's Tamil Nadu region suffered only minimal damage and few deaths because the wave broke against a forest of 80,244 trees planted along the shoreline in 2002 in a bid to enter the Guinness Book of Records.[24] Environmentalists have suggested tree planting along tsunami-prone seacoasts. Trees require years to grow to a useful size, but such plantations could offer a much cheaper and longer-lasting means of tsunami mitigation than artificial barriers.


File:Samoa tsunami animation 20090929 samoa a.ogv
File:Chennai beach2.jpg
Main article: Historic tsunami

Destructive tsunamis have been recorded throughout history, for example there were 26 that caused 200 or more deaths in the last century alone.[25] Of these, many were recorded in the Asia–Pacific region, particularly around Japan and Indonesia.

Ancient history

As early as 426 B.C. the Greek historian Thucydides inquired in his book History of the Peloponnesian War about the causes of tsunami, and was the first to argue that ocean earthquakes must be the cause.[4][5]

The cause, in my opinion, of this phenomenon must be sought in the earthquake. At the point where its shock has been the most violent the sea is driven back, and suddenly recoiling with redoubled force, causes the inundation. Without an earthquake I do not see how such an accident could happen.[26]

The Roman historian Ammianus Marcellinus (Res Gestae 26.10.15-19) described the typical sequence of a tsunami, including an incipient earthquake, the sudden retreat of the sea and a following gigantic wave, after the 365 A.D. tsunami devastated Alexandria.[27][28]

2004 Indian Ocean tsunami

The 2004 Indian Ocean tsunami killed over 200,000[29] people with many bodies either being lost to the sea or unidentified.

According to an article in Geographical magazine (April 2008), the Indian Ocean tsunami of December 26, 2004 was not the worst that the region could expect. Professor Costas Synolakis of the Tsunami Research Center at the University of Southern California co-authored a paper in Geophysical Journal International which suggests that a future tsunami in the Indian Ocean basin could affect locations such as Madagascar, Singapore, Somalia, Western Australia, and many others.

As a weapon

There have been studies and some attempt to create tsunami waves as a weapon. In World War II, the army in New Zealand trialled explosives in the area of today's Shakespear Regional Park to create small tsunamis, an attempt which failed.[30]

See also


  1. "Tsunami Terminology". NOAA. Retrieved 2010-07-15. 
  2. Fradin, Judith Bloom and Dennis Brindell (2008). Witness to Disaster: Tsunamis. Witness to Disaster. Washington, D.C.: National Geographic Society. pp. 42, 43. 
  4. 4.0 4.1 Thucydides: “A History of the Peloponnesian War”, 3.89.1–4
  5. 5.0 5.1 Smid, T. C. (Apr., 1970). 'Tsunamis' in Greek Literature. Greece & Rome 17 (2nd ed.). pp. 100–104.  Check date values in: |date= (help)
  6. [a. Jap. tsunami, tunami, f. tsu harbour + nami waves.— Oxford English Dictionary]
  7. "Tidal", The American Heritage Stedman's Medical Dictionary. Houghton Mifflin Company. 11 November
  8. -al. (n.d.). Unabridged (v 1.1). Retrieved November 11, 2008,
  11. Haugen K, Løvholt F, Harbitz C, K (2005). "Fundamental mechanisms for tsunami generation by submarine mass flows in idealised geometries". Marine and Petroleum Geology 22: 209–217. doi:10.1016/j.marpetgeo.2004.10.016. 
  12. Margaritondo, G (2005). "Explaining the physics of tsunamis to undergraduate and non-physics students". European Journal of Physics 26 (3). 
  13. Voit, S.S (1987). "Tsunamis". Annual Review of Fluid Mechanics 19: 217–236. doi:10.1146/annurev.fl.19.010187.001245. 
  14. "How do earthquakes generate tsunamis?". University of Washington. 
  15., Tsunamis
  16. 16.0 16.1 "Life of a Tsunami". Western Coastal & Marine Geology. United States Geographical Survey. 22 October 2008. Retrieved 2009-09-09. 
  17. Prof. Stephen A. Nelson (28-Jan-2009). "Tsunami". Tulane University. Retrieved 2009-09-09.  Check date values in: |date= (help)
  18. 18.0 18.1 Gusiakov V. "Tsunami Quantification: how we measure the overall size of tsunami (Review of tsunami intensity and magnitude scales)" (PDF). Retrieved 2009-10-18. 
  19. Abe K. (1995). Estimate of Tsunami Run-up Heights from Earthquake Magnitudes. Tsunami: progress in prediction, disaster prevention, and warning. ISBN 9780792334835. Retrieved 2009-10-18. 
  20. Chanson, H. (2010). Tsunami Warning Signs on the Enshu Coast of Japan. Shore & Beach, Vol. 78, No. 1, pp. 52-54. ISSN 0037-4237.  External link in |title= (help)
  21. Lambourne, Helen (2005-03-27). "Tsunami: Anatomy of a disaster". BBC. 
  22. Kenneally, Christine (2004-12-30). "Surviving the Tsunami: What Sri Lanka's animals knew that humans didn't". Slate Magazine. 
  23. Script error
  24. Raman, Sunil (2005-03-27). "Tsunami villagers give thanks to trees". BBC. 
  25. NOAA. "Tsunami Events where (Year <= 2000 and Year >= 1901) and Deaths >= 200". Retrieved 21 June 2010. 
  26. Thucydides: “A History of the Peloponnesian War”, 3.89.5
  27. Kelly, Gavin (2004). "Ammianus and the Great Tsunami". The Journal of Roman Studies 94 (141): 141–167. doi:10.2307/4135013. 
  28. Stanley, Jean-Daniel & Jorstad, Thomas F. (2005), "The 365 A.D. Tsunami Destruction of Alexandria, Egypt: Erosion, Deformation of Strata and Introduction of Allochthonous Material"
  30. "The Hauraki Gulf Marine Park, Part 2". Inset to The New Zealand Herald. 3 March 2010. p. 9. 


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Template:Physical oceanography Template:Natural disasters

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