|UTC time||2004-12-26 00:58:53|
|Local date||26 December 2004|
|Depth||30 km (19 mi)|
|Areas affected||Indian Ocean coastline areas|
|Max. intensity||IX (Violent)|
The 2004 Indian Ocean earthquake and tsunami (also known as the Boxing Day Tsunami and, by the scientific community, the Sumatra–Andaman earthquake) occurred at 07:58:53 in local time (UTC+7) on 26 December, with an epicentre off the west coast of northern Sumatra, Indonesia. It was an undersea megathrust earthquake that registered a magnitude of 9.1–9.3 Mw, reaching a Mercalli intensity up to IX in certain areas. The earthquake was caused by a rupture along the fault between the Burma Plate and the Indian Plate.
A series of massive tsunami waves grew up to 30 m (100 ft) high once heading inland, after being created by the underwater seismic activity offshore. Communities along the surrounding coasts of the Indian Ocean were severely affected, and the tsunamis killed an estimated 227,898 people in 14 countries, making it one of the deadliest natural disasters in recorded history. The direct results caused major disruptions to living conditions and commerce in coastal provinces of surrounded countries, including Aceh, Indonesia, Sri Lanka, Tamil Nadu, India and Khao Lak, Thailand. Banda Aceh reported the largest number of deaths.
The earthquake was the third-largest ever recorded and had the longest duration of faulting ever observed; between eight and ten minutes. It caused the planet to vibrate as much as 10 mm (0.4 in), and also remotely triggered earthquakes as far away as Alaska. Its epicentre was between Simeulue and mainland Sumatra. The plight of the affected people and countries prompted a worldwide humanitarian response, with donations totalling more than US$14 billion.
The 2004 Indian Ocean earthquake was initially documented as having a moment magnitude of 8.8. In February 2005, scientists revised the estimate of the magnitude to 9.0. Although the Pacific Tsunami Warning Center has accepted these new numbers, the United States Geological Survey has so far not changed its estimate of 9.1. A 2006 study estimated a magnitude of Mw 9.1–9.3; Hiroo Kanamori of the California Institute of Technology estimates that Mw 9.2 is representative of the earthquake's size.
The hypocentre of the main earthquake was approximately 160 km (100 mi) off the western coast of northern Sumatra, in the Indian Ocean just north of Simeulue island at a depth of 30 km (19 mi) below mean sea level (initially reported as 10 km or 6.2 mi). The northern section of the Sunda megathrust ruptured over a length of 1,300 km (810 mi). The earthquake (followed by the tsunami) was felt in Bangladesh, India, Malaysia, Myanmar, Thailand, Sri Lanka and the Maldives. Splay faults, or secondary "pop up faults", caused long, narrow parts of the seafloor to pop up in seconds. This quickly elevated the height and increased the speed of waves, destroying the nearby Indonesian town of Lhoknga.
Indonesia lies between the Pacific Ring of Fire along the north-eastern islands adjacent to New Guinea, and the Alpide belt that runs along the south and west from Sumatra, Java, Bali, Flores to Timor. The 2002 Sumatra earthquake is believed to have been a foreshock, preceding the main event by over two years.
Great earthquakes, such as the 2004 Indian Ocean earthquake, are associated with megathrust events in subduction zones. Their seismic moments can account for a significant fraction of the global seismic moment across century-scale periods. Of all the moment released by earthquakes in the 100 years from 1906 through 2005, roughly one-eighth was due to the 2004 Indian Ocean earthquake. This quake, together with the Good Friday earthquake (Alaska, 1964) and the Great Chilean earthquake (1960), account for almost half of the total moment.
Since 1900, the only earthquakes recorded with a greater magnitude were the 1960 Great Chilean earthquake (Magnitude 9.5) and the 1964 Good Friday earthquake in Prince William Sound (Magnitude 9.2). The only other recorded earthquakes of magnitude 9.0 or greater were off Kamchatka, Russia, on 4 November 1952 (magnitude 9.0) and Tōhoku, Japan (magnitude 9.1) in March 2011. Each of these megathrust earthquakes also spawned tsunamis in the Pacific Ocean. In comparison to the 2004 Indian Ocean earthquake, the death toll from these earthquakes was significantly lower, primarily because of the lower population density along the coasts near affected areas, the much greater distances to more populated coasts, and the superior infrastructure and warning systems in MEDCs (More Economically Developed Countries) such as Japan.
Other huge megathrust earthquakes occurred in 1868 (Peru, Nazca Plate and South American Plate); 1827 (Colombia, Nazca Plate and South American Plate); 1812 (Venezuela, Caribbean Plate and South American Plate) and 1700 (western North America, Juan de Fuca Plate and North American Plate). All of them are believed to be greater than magnitude 9, but no accurate measurements were available at the time.
The 2004 Indian Ocean earthquake was unusually large in geographical and geological extent. An estimated 1,600 km (1,000 mi) of fault surface slipped (or ruptured) about 15 m (50 ft) along the subduction zone where the Indian Plate slides (or subducts) under the overriding Burma Plate. The slip did not happen instantaneously but took place in two phases over several minutes: Seismographic and acoustic data indicate that the first phase involved a rupture about 400 km (250 mi) long and 100 km (60 mi) wide, 30 km (19 mi) beneath the sea bed—the largest rupture ever known to have been caused by an earthquake. The rupture proceeded at about 2.8 km/s (1.7 mi/s; 10,000 km/h; 6,300 mph), beginning off the coast of Aceh and proceeding north-westerly over about 100 seconds. After a pause of about another 100 seconds, the rupture continued northwards towards the Andaman and Nicobar Islands. The northern rupture occurred more slowly than in the south, at about 2.1 km/s (1.3 mi/s; 7,600 km/h; 4,700 mph), continuing north for another five minutes to a plate boundary where the fault type changes from subduction to strike-slip (the two plates slide past one another in opposite directions).
The Indian Plate is part of the great Indo-Australian Plate, which underlies the Indian Ocean and Bay of Bengal, and is moving north-east at an average of 60 mm/a (2.4 in/year). The India Plate meets the Burma Plate (which is considered a portion of the great Eurasian Plate) at the Sunda Trench. At this point, the India Plate subducts beneath the Burma Plate, which carries the Nicobar Islands, the Andaman Islands, and northern Sumatra. The India Plate sinks deeper and deeper beneath the Burma Plate until the increasing temperature and pressure drive volatiles out of the subducting plate. These volatiles rise into the overlying plate, causing partial melting and the formation of magma. The rising magma intrudes into the crust above and exits the Earth's crust through volcanoes in the form of a volcanic arc. The volcanic activity that results as the Indo-Australian Plate subducts the Eurasian Plate has created the Sunda Arc.
As well as the sideways movement between the plates, the 2004 Indian Ocean earthquake resulted in a rise of the seafloor by several metres, displacing an estimated 30 km3 (7.2 cu mi) of water and triggering devastating tsunami waves. The waves radiated outwards along the entire 1,600 km (1,000 mi) length of the rupture (acting as a line source). This greatly increased the geographical area over which the waves were observed, reaching as far as Mexico, Chile, and the Arctic. The raising of the seafloor significantly reduced the capacity of the Indian Ocean, producing a permanent rise in the global sea level by an estimated 0.1 mm (0.004 in).
Aftershocks and other earthquakes
Numerous aftershocks were reported off the Andaman Islands, the Nicobar Islands and the region of the original epicentre in the hours and days that followed. The magnitude 8.7 2005 Nias–Simeulue earthquake, which originated off the coast of the Sumatran island of Nias, is not considered an aftershock, despite its proximity to the epicentre, and was most likely triggered by stress changes associated with the 2004 event. The earthquake produced its own aftershocks (some registering a magnitude of as high as 6.1) and presently ranks as the third-largest earthquake ever recorded on the moment magnitude or Richter magnitude scale.
Other aftershocks of up to magnitude 6.6 continued to shake the region daily for three or four months. As well as continuing aftershocks, the energy released by the original earthquake continued to make its presence felt well after the event. A week after the earthquake, its reverberations could still be measured, providing valuable scientific data about the Earth's interior.
The 2004 Indian Ocean earthquake came just three days after a magnitude 8.1 earthquake in the sub-antarctic Auckland Islands, an uninhabited region west of New Zealand, and Macquarie Island to Australia's north. This is unusual since earthquakes of magnitude eight or more occur only about once per year on average. The U.S. Geological Survey sees no evidence of a causal relationship between these events.
The 2004 Indian Ocean earthquake is thought to have triggered activity in both Leuser Mountain and Mount Talang, volcanoes in Aceh along the same range of peaks, while the 2005 Nias–Simeulue earthquake had sparked activity in Lake Toba, an ancient crater in Sumatra.
The energy released on the Earth's surface (ME, which is the seismic potential for damage) by the 2004 Indian Ocean earthquake was estimated at 1.1×1017 joules (110 PJ; 26 Mt). This energy is equivalent to over 1,500 times that of the Hiroshima atomic bomb, but less than that of Tsar Bomba, the largest nuclear weapon ever detonated. The total physical work done MW (and thus energy) by the quake was 4.0×1022 joules (40 ZJ), the vast majority underground, which is over 360,000 times more than its ME, equivalent to 9,600 gigatons of TNT equivalent (550 million times that of Hiroshima) or about 370 years of energy use in the United States at 2005 levels of 1.08×1020 joules (108 EJ). The only recorded earthquakes with a larger MW were the 1960 Chilean and 1964 Alaskan quakes, with 2.5×1023 joules (250 ZJ) and 7.5×1022 joules (75 ZJ) respectively.
The earthquake generated a seismic oscillation of the Earth's surface of up to 200–300 mm (8–12 in), equivalent to the effect of the tidal forces caused by the Sun and Moon. The seismic waves of the earthquake were felt across the planet; as far away as the U.S. state of Oklahoma, where vertical movements of 3 mm (0.12 in) were recorded. By February 2005, the earthquake's effects were still detectable as a 20 μm (0.02 mm; 0.0008 in) complex harmonic oscillation of the Earth's surface, which gradually diminished and merged with the incessant free oscillation of the Earth more than four months after the earthquake.
Because of its enormous energy release and shallow rupture depth, the earthquake generated remarkable seismic ground motions around the globe, particularly due to huge Rayleigh (surface) elastic waves that exceeded 10 mm (0.4 in) in vertical amplitude everywhere on Earth. The record section plot displays vertical displacements of the Earth's surface recorded by seismometers from the IRIS/USGS Global Seismographic Network plotted with respect to time (since the earthquake initiation) on the horizontal axis, and vertical displacements of the Earth on the vertical axis (note the 1 cm scale bar at the bottom for scale). The seismograms are arranged vertically by distance from the epicentre in degrees. The earliest, lower amplitude signal is that of the compressional (P) wave, which takes about 22 minutes to reach the other side of the planet (the antipode; in this case near Ecuador). The largest amplitude signals are seismic surface waves that reach the antipode after about 100 minutes. The surface waves can be clearly seen to reinforce near the antipode (with the closest seismic stations in Ecuador), and to subsequently encircle the planet to return to the epicentral region after about 200 minutes. A major aftershock (magnitude 7.1) can be seen at the closest stations starting just after the 200-minute mark. The aftershock would be considered a major earthquake under ordinary circumstances but is dwarfed by the mainshock.
The shift of mass and the massive release of energy slightly altered the Earth's rotation. The exact amount is not yet known, but theoretical models suggest the earthquake shortened the length of a day by 2.68 microseconds, due to a decrease in the oblateness of the Earth. It also caused the Earth to minutely "wobble" on its axis by up to 25 mm (1 in) in the direction of 145° east longitude, or perhaps by up to 50 or 60 mm (2.0 or 2.4 in). Because of tidal effects of the Moon, the length of a day increases at an average of 15 microseconds per year, so any rotational change due to the earthquake will be lost quickly. Similarly, the natural Chandler wobble of the Earth, which in some cases can be up to 15 m (50 ft), will eventually offset the minor wobble produced by the earthquake.
There was 10 m (33 ft) movement laterally and 4–5 m (13–16 ft) vertically along the fault line. Early speculation was that some of the smaller islands south-west of Sumatra, which is on the Burma Plate (the southern regions are on the Sunda Plate), might have moved south-west by up to 36 m (120 ft), but more accurate data released more than a month after the earthquake found the movement to be about 200 mm (8 in). Since movement was vertical as well as lateral, some coastal areas may have been moved to below sea level. The Andaman and Nicobar Islands appear to have shifted south-west by around 1.25 m (4 ft 1 in) and to have sunk by 1 m (3 ft 3 in).
In February 2005, the Royal Navy vessel HMS Scott surveyed the seabed around the earthquake zone, which varies in depth between 1,000 and 5,000 m (550 and 2,730 fathoms; 3,300 and 16,400 ft). The survey, conducted using a high-resolution, multi-beam sonar system, revealed that the earthquake had made a considerable impact on the topography of the seabed. 1,500 m-high (5,000 ft) thrust ridges created by previous geologic activity along the fault had collapsed, generating landslides several kilometres wide. One such landslide consisted of a single block of rock some 100 m (330 ft) high and 2 km (1.2 mi) long. The momentum of the water displaced by tectonic uplift had also dragged massive slabs of rock, each weighing millions of tonnes, as far as 10 km (6 mi) across the seabed. An oceanic trench several kilometres wide was exposed in the earthquake zone.
The TOPEX/Poseidon and Jason-1 satellites happened to pass over the tsunami as it was crossing the ocean. These satellites carry radars that measure precisely the height of the water surface; anomalies in the order of 500 mm (20 in) were measured. Measurements from these satellites may prove invaluable for the understanding of the earthquake and tsunami. Unlike data from tide gauges installed on shores, measurements obtained in the middle of the ocean can be used for computing the parameters of the source earthquake without having to compensate for the complex ways in which proximity to the coast changes the size and shape of a wave.
The sudden vertical rise of the seabed by several metres during the earthquake displaced massive volumes of water, resulting in a tsunami that struck the coasts of the Indian Ocean. A tsunami that causes damage far away from its source is sometimes called a teletsunami and is much more likely to be produced by the vertical motion of the seabed than by horizontal motion.
The tsunami, like all others, behaved differently in deep water than in shallow water. In deep ocean water, tsunami waves form only a low, broad hump, barely noticeable and harmless, which generally travels at high speed of 500 to 1,000 km/h (310 to 620 mph); in shallow water near coastlines, a tsunami slows down to only tens of kilometres per hour but, in doing so, forms large destructive waves. Scientists investigating the damage in Aceh found evidence that the wave reached a height of 24 m (80 ft) when coming ashore along large stretches of the coastline, rising to 30 m (100 ft) in some areas when travelling inland. Radar satellites recorded the heights of tsunami waves in deep water: maximum height was at 600 mm (2 ft) two hours after the earthquake, the first such observations ever made.
According to Tad Murty, vice-president of the Tsunami Society, the total energy of the tsunami waves was equivalent to about 5 megatons of TNT (21 PJ), which is more than twice the total explosive energy used during all of World War II (including the two atomic bombs) but still a couple of orders of magnitude less than the energy released in the earthquake itself. In many places, the waves reached as far as 2 km (1.2 mi) inland.
Because the 1,600 km (1,000 mi) fault affected by the earthquake was in a nearly north–south orientation, the greatest strength of the tsunami waves was in an east–west direction. Bangladesh, which lies at the northern end of the Bay of Bengal, had few casualties despite being a low-lying country relatively near the epicentre. It also benefited from the fact that the earthquake proceeded more slowly in the northern rupture zone, greatly reducing the energy of the water displacements in that region.
Coasts that have a landmass between them and the tsunami's location of origin are usually safe; however, tsunami waves can sometimes diffract around such landmasses. Thus, the state of Kerala was hit by the tsunami despite being on the western coast of India, and the western coast of Sri Lanka suffered substantial impacts. Distance alone was no guarantee of safety, as Somalia was hit harder than Bangladesh despite being much farther away.
Because of the distances involved, the tsunami took anywhere from fifteen minutes to seven hours to reach the coastlines. The northern regions of the Indonesian island of Sumatra were hit quickly, while Sri Lanka and the east coast of India were hit roughly 90 minutes to two hours later. Thailand was struck about two hours later despite being closer to the epicentre because the tsunami travelled more slowly in the shallow Andaman Sea off its western coast.
The tsunami was noticed as far as Struisbaai in South Africa, about 8,500 km (5,300 mi) away, where a 1.5 m-high (5 ft) tide surged on shore about 16 hours after the earthquake. It took a relatively long time to reach Struisbaai at the southernmost point of Africa, probably because of the broad continental shelf off South Africa and because the tsunami would have followed the South African coast from east to west. The tsunami also reached Antarctica, where tidal gauges at Japan's Showa Base recorded oscillations of up to a metre (3 ft 3 in), with disturbances lasting a couple of days.
Some of the tsunami's energy escaped into the Pacific Ocean, where it produced small but measurable tsunamis along the western coasts of North and South America, typically around 200 to 400 mm (7.9 to 15.7 in). At Manzanillo, Mexico, a 2.6 m (8 ft 6 in) crest-to-trough tsunami was measured. As well, the tsunami was large enough to be detected in Vancouver, which puzzled many scientists, as the tsunamis measured in some parts of South America were larger than those measured in some parts of the Indian Ocean. It has been theorized that the tsunamis were focused and directed at long ranges by the mid-ocean ridges which run along the margins of the continental plates.
Early signs and warnings
Despite a delay of up to several hours between the earthquake and the impact of the tsunami, nearly all of the victims were taken by surprise. There were no tsunami warning systems in the Indian Ocean to detect tsunamis or to warn the general population living around the ocean. Tsunami detection is not easy because while a tsunami is in deep water, it has little height and a network of sensors is needed to detect it.
Tsunamis are more frequent in the Pacific Ocean than in other oceans because of earthquakes in the "Ring of Fire". Although the extreme western edge of the Ring of Fire extends into the Indian Ocean (the point where the earthquake struck), no warning system exists in that ocean. Tsunamis there are relatively rare despite earthquakes being relatively frequent in Indonesia. The last major tsunami was caused by the 1883 eruption of Krakatoa. Not every earthquake produces large tsunamis: on 28 March 2005, a magnitude 8.7 earthquake hit roughly the same area of the Indian Ocean but did not result in a major tsunami.
The first warning sign of a possible tsunami is the earthquake itself. However, tsunamis can strike thousands of kilometres away where the earthquake is felt only weakly or not at all. Also, in the minutes preceding a tsunami strike, the sea often recedes temporarily from the coast, something which was observed on the eastern side of the rupture zone of the earthquake such as around the coastlines of Aceh, Phuket island, and Khao Lak area in Thailand, Penang island of Malaysia, and the Andaman and Nicobar islands. Around the Indian Ocean, this rare sight reportedly induced people, especially children, to visit the coast to investigate and collect stranded fish on as much as 2.5 km (1.6 mi) of exposed beach, with fatal results. However, not all tsunamis cause this "disappearing sea" effect. In some cases, there are no warning signs at all: the sea will suddenly swell without retreating, surprising many people and giving them little time to flee.
One of the few coastal areas to evacuate ahead of the tsunami was on the Indonesian island of Simeulue, close to the epicentre. Island folklore recounted an earthquake and tsunami in 1907, and the islanders fled to inland hills after the initial shaking and before the tsunami struck. These tales and oral folklore from previous generations may have helped the survival of the inhabitants. On Maikhao Beach in north Phuket City, Thailand, a 10-year-old British tourist named Tilly Smith had studied tsunamis in geography at school and recognised the warning signs of the receding ocean and frothing bubbles. She and her parents warned others on the beach, which was evacuated safely. John Chroston, a biology teacher from Scotland, also recognised the signs at Kamala Bay north of Phuket, taking a busload of vacationers and locals to safety on higher ground.
Anthropologists had initially expected the aboriginal population of the Andaman Islands to be badly affected by the tsunami and even feared the already depopulated Onge tribe could have been wiped out. Many of the aboriginal tribes evacuated and suffered fewer casualties, however. Oral traditions developed from previous earthquakes helped the aboriginal tribes escape the tsunami. For example, the folklore of the Onges talks of "huge shaking of ground followed by high wall of water". Almost all of the Onge people seemed to have survived the tsunami.
The tsunami devastated the northwestern coastlines of Sumatra, especially in the Aceh province, about 20 minutes after the initial earthquake. Banda Aceh, the closest major city was particularly affected, suffering severe casualties. Eyewitnesses described three large waves, with the first wave rising gently to the foundation of the buildings, followed minutes later by a sudden withdrawal of the sea near the port of Ulee Lheue. This was succeeded by the appearance of two large black-coloured steep waves which travelled inland into the capital city. Video footage revealed black torrents of water moving at high speed, rolling by windows of a two-story residential area situated about 3.2 km (2.0 mi) inland. Additionally, amateur footage recorded in the middle of the city captured an approaching black surge flowing down the city streets, full of debris, inundating them. The city experienced the highest number of human casualties, with about 167,000 people perishing directly from the tsunami.
The level of destruction was extreme on the northwestern flank of the city in the areas immediately inland of the aquaculture ponds, and directly facing the Indian Ocean. The tsunami height was reduced from 12 m (39 ft) at Ulee Lheue to 6 m (20 ft) a further 8 km (5.0 mi) to the northeast. The inundation was observed to extend 3–4 km (1.9–2.5 mi) inland throughout the city. Within 2–3 km (1.2–1.9 mi) of the shoreline, houses, except for strongly-built reinforced concrete ones with brick walls, which seemed to have been partially damaged by the earthquake before the tsunami attack, were swept away or destroyed by the tsunami. The area toward the sea was wiped clean of nearly every structure, while closer to the river, dense construction in a commercial district showed the effects of severe flooding. The flow depth at the city was just at the level of the second floor, and there were large amounts of debris piled along the streets and in the ground-floor storefronts. In the seaside section of Ulee Lheue, the flow depths were over 9 m (30 ft). Footage showed evidence of back-flowing of the Aceh River, carrying debris and people from destroyed villages at the coast and transporting them up to 40 km (25 mi) inland.
A group of small islands: Weh, Breueh, Nasi, Teunom, Bunta, Lumpat and Batee island lie just north of the capital city. The tsunami effects on two of the islands, Breueh Island and Nasi, were extreme, with a runup of 10–20 m (33–66 ft) on the west-facing shores. Coastal villages were destroyed by the tsunami waves. On Pulau Weh, however, the island experienced strong surges in the port of Sabang, yet there was little damage with a reported runup values of 3–5 m (9.8–16.4 ft), sheltered from the direct tsunami attack by the islands to the southwest.
Lhoknga is a small coastal community about 13 km (8.1 mi) southwest of Banda Aceh, located on a flat coastal plain in between two rainforest-covered hills, overlooking a large bay and famous for its large swathe of white sandy beach and surfing activities. The town was among the first settlements located on the west coast, to be impacted by the initial tsunami wave. The bathymetry of the seafloor favoured the development of large surfing-type tsunami waves. The locals reported 10 to 12 waves, with the second and third waves being the highest and most destructive. Interviews with the local people and fishers revealed that about 10–15 minutes after the earthquake, the sea dramatically receded and exposed coral reefs. In the distant horizon, gigantic vertical black waves about 30 m (98 ft) high made explosion-like sounds as it broke and approached the shore. The first wave came rapidly landward from the southwest as a turbulent bore about 0.5–2.5 m (1 ft 8 in–8 ft 2 in) high. The second and third waves were 15–30 m (49–98 ft) high at the coast and appeared like gigantic surfing waves but "taller than the coconut trees and was like a mountain". The second wave was the largest; it came from the west-southwest within five minutes of the first wave. The tsunami stranded cargo ships and barges, as well as destroying a cement factory near the Lampuuk coast, where evidence showed the tsunami reached the third level of a building.
Meulaboh, a remote coastal city, was among the hardest hit by the tsunami. The waves arrived after the sea receded about 500 m (1,600 ft), followed by an advancing small tsunami. The second and third destructive waves arrived later, which exceeded the height of the coconut trees. The inundation distance is about 5 km (3.1 mi). Other towns on Aceh's west coast hit by the disaster included Leupung, Lhokruet, Lamno, Patek, Calang, and Teunom. Affected or destroyed towns on the region's north and east coast were Pidie Regency, Samalanga, Panteraja, and Lhokseumawe. The high fatality rate in the area was mainly due to lack of preparation of the community towards a tsunami and limited knowledge and education among the population regarding the natural phenomenon. Helicopter surveys showed entire settlements virtually destroyed with destruction within miles inland, and only some mosques left standing.
The tsunami heights in Sumatra:
- 15–30 m (49–98 ft) on the west coast of Aceh
- 6–12 m (20���39 ft) on the Banda Aceh coast
- 6 m (20 ft) on the Krueng Raya coast
- 5 m (16 ft) on the Sigli coast
- 3–6 m (9.8–19.7 ft) on the north coast of Weh Island directly facing the tsunami source
- 3 m (9.8 ft) on the opposite side of the coast of Weh Island facing the tsunami
The island country of Sri Lanka, located about 1,700 km (1,100 mi) from Sumatra, was ravaged around 2 hours after the earthquake. Reports indicated that the tremors were not felt by the population. The tsunami first struck on the eastern coastline and subsequently refracted around the southern point of Sri Lanka (Dondra Head). The refracted tsunami waves inundated the southwestern part of Sri Lanka after some of its energy was reflected from impact with the Maldives.
The first tsunami waves initially caused a small flood (positive wave) as it struck the Sri Lankan coastline. Moments later, the ocean floor was exposed to as much as 1 km (0.62 mi) in places due to drawback (negative wave), which was followed by a massive second tsunami wave. The construction of seawalls and breakwaters reduced the power of waves at some locations.
The largest run-up measured was at 12.5 m (41 ft) with inundation distance of 390–1,500 m (1,280–4,920 ft) in Yala. In Hambantota, tsunami run-ups measured 11 m (36 ft) with the greatest inundation distance of 2 km (1.2 mi). Tsunami run-up measurements along the Sri Lankan coasts are at 2.4–4.11 m (7 ft 10 in–13 ft 6 in). Tsunami waves measured on the east coast ranged from 4.5–9 m (15–30 ft) at Pottuvill to Batticaloa at 2.6–5 m (8 ft 6 in–16 ft 5 in) in the northeast around Trincomalee and 4–5 m (13–16 ft) in the west coast from Moratuwa to Ambalangoda.
Sri Lanka tsunami height survey:
- 9 m (30 ft) at Koggala
- 6 m (20 ft) at Galle port
- 4.8 m (16 ft) around the Galle coast
- 8.7 m (29 ft) at Nonagama
- 4.9 m (16 ft) at Weligama
- 4 m (13 ft) at Dodundawa
- 4.7 m (15 ft) at Ambalangoda
- 4.7 m (15 ft) at Hikkaduwa Fishery Harbour
- 10 m (33 ft) at Kahawa
- 4.8 m (16 ft) at North Beach of Beruwala
- 6 m (20 ft) at Paiyagala
A regular passenger train operating between Maradana and Matara was derailed and overturned by the tsunami and claimed at least 1,700 lives, the largest single rail disaster death toll in history. Estimates based on the state of the shoreline and a high-water mark on a nearby building place the tsunami 7.5–9 m (25–30 ft) above sea level and 2–3 m (6 ft 7 in–9 ft 10 in) higher than the top of the train.
In Sri Lanka, the civilian casualties were second only to those in Indonesia. The eastern shores of Sri Lanka were hardest hit since they face the epicentre of the earthquake. The southwestern shores were hit later, but the death toll was just as severe. The southwestern shores are a hotspot for tourists and fishing. The degradation of the natural environment in Sri Lanka contributed to the high death tolls. Approximately 90,000 buildings, many wooden houses, were destroyed.
The 2004 tsunami travelled via Andaman Sea and hit the southwest coast of Thailand, which was about 500 km (310 mi) from the epicentre. The region is heavily visited by foreigners and locals alike during the Christmas season and is internationally famed for its luxurious resorts and hotels with picturesque beautiful beaches. Many tourists were caught off-guard by the tsunami, as they had no prior warning. Major tourist locations damaged include the western shoreline of Phuket island, the Khao Lak resort town in Phang Nga province, the Phi Phi islands, the Surin Islands and Similan archipelago, coastal areas of the provinces of Krabi, Satun, Ranong, and Trang and small offshore islands like Ko Racha Yai. Approximately 5,400 people were killed, and 3,100 were reported missing.
Khao Lak and others on the mainland
- 6–10 m (20–33 ft) in Khao Lak
- 3–6 m (9.8–19.7 ft) along the west coast of Phuket island
- 3 m (9.8 ft) along the south coast of Phuket island
- 2 m (6 ft 7 in) along the east coast of Phuket island
- 4–6 m (13–20 ft) on the Phi Phi Islands
- 19.6 m (64 ft) at Ban Thung Dap
- 5 m (16 ft) at Ramson
- 6.8 m (22 ft) at Ban Thale Nok
- 5 m (16 ft) at Hat Praphat (Ranong Coastal Resources Research Station)
- 6.3 m (21 ft) at Thai Mueang District
- 6.8 m (22 ft) at Rai Dan
The province of Phang Nga was the most affected area in Thailand. The quiet resort town of Khao Lak was hit by the tsunami about 2 hours after the earthquake and had the largest death toll in Thailand. A maximum inundation of approximately 2 km (1.2 mi) and the inundated depths were 4–7 m (13–23 ft) in Khao Lak, inundating the third floor of a resort hotel. Tsunami heights in Khao Lak were much higher than on Phuket Island. The reason for the difference seems to have been caused by the local bathymetry off Khao Lak. According to interviews, the leading wave produced an initial depression, called a tsunami drawback or "disappearing sea" effect and the second wave was larger.[page needed]
Phuket and other islands
At Phuket island, many west coast beaches were affected. At Patong Beach, a tourist mecca, tsunami heights were 5–6 m (16–20 ft) and the inundated depth was about 2 m (6 ft 7 in). Tsunami heights became lower from the west coast, the south coast to the east coast of the island. On Karon Beach on the west coast, the coastal road was built higher than the shore, protecting a hotel which was behind it. On the east coast of Phuket Island, the tsunami height was about 2 m (6 ft 7 in). In one river mouth, many boats were damaged. The tsunami moved counter-clockwise around Phuket Island, as was the case at Okushiri Island in the 1993 Hokkaido earthquake. According to interviews, the leading wave produced an initial depression, and the second wave was the largest.
The Phi Phi Islands are a group of small islands that were affected by the tsunami. The north bay of Phi Phi Don Island opens to the northwest in the direction of the tsunami. The measured tsunami height on this beach was 5.8 m (19 ft). According to some eyewitness accounts, the tsunami came from the north and south. The ground level was about 2 m (6 ft 7 in) above sea level, and there were many cottages and hotels. The south bay opens to the southeast and faces in the opposite direction from the tsunami. Further, Phi Phi Le Island shields the port of Phi Phi Don Island. The measured tsunami height was 4.6 m (15 ft) in the port.
The tsunami arrived in the states of Andhra Pradesh and Tamil Nadu along the southeast coast of the Indian mainland shortly after 9:00 a.m. At least two hours later, it arrived in the state of Kerala along the southwest coast. Tamil Nadu, the union territory of Pondicherry and Kerala were extensively damaged, while Andhra Pradesh sustained moderate damage. There were two to five waves of varying height that coincided with the local high tide in some areas. The tsunami runup height measured in mainland India by Ministry of Home Affairs includes:
- 3.4 m (11 ft) at Kerala, inundation distance of 0.5–1.5 km (0.31–0.93 mi) with 250 km (160 mi) of coastline affected
- 4.5 m (15 ft) at the southern coastline of Tamil Nadu, inundation distance of 0.2–2 km (0.12–1.24 mi) with 100 km (62 mi) of coastline affected
- 5 m (16 ft) at the eastern coastline of Tamil Nadu facing tsunami source, inundation distance of 0.4–1.5 km (0.25–0.93 mi) with 800 km (500 mi) of coastline affected
- 4 m (13 ft) at Pondicherry, inundation distance of 0.2–2 km (0.12–1.24 mi) with 25 km (16 mi) of coastline affected
- 2.2 m (7 ft 3 in) at Andhra Pradesh, inundation distance of 0.2–1 km (0.12–0.62 mi) with 985 km (612 mi) of coastline affected
Tamil Nadu and Puducherry
The tsunami run-up was only 1.6 m (5 ft 3 in) in areas in the state of Tamil Nadu shielded by the island of Sri Lanka but was 4–5 m (13–16 ft) in coastal districts such as Nagapattinam in Tamil Nadu directly across from Sumatra. On the western coast, the runup elevations were 4.5 m (15 ft) at Kanyakumari District in Tamil Nadu and 3.4 m (11 ft) each at Kollam and Ernakulam districts in Kerala. The time between the waves varied from about 15 minutes to 90 minutes. The tsunami varied in height from 2–10 m (6 ft 7 in–32 ft 10 in) based on survivor's accounts.
The worst affected area in Tamil Nadu was Nagapattinam district, with 6,051 fatalities reported by a 5 m (16 ft) tsunami, followed by Cuddalore district, with many villages destroyed. The 13 km (8.1 mi) Marina Beach in Chennai was battered by the tsunami which swept across the beach taking morning walkers unaware. Besides that, a 108 m (354 ft) black muddy tsunami ravaged the city of Karaikal, where 492 lives were lost. The city of Pondicherry, protected by seawalls was relatively unscathed.
The tsunami effects varied greatly across different coastal areas according to the number of waves experienced, the inundation distance and height of waves, and the population density of the area, and topological and geographical features. Besides these factors, the number of lives lost was influenced by exposure to previous disasters and local disaster management capability. Most of the people killed were members of the fishing community. The tsunami travelled 2.5 km (1.6 mi) at its maximum inland at Karaikal, Puducherry. The inundation distance varied between 1,006–500 m (3,301–1,640 ft) in most areas, except at river mouths, where it was more than 1 km (0.62 mi). Areas with dense coconut groves or mangroves had much smaller inundation distances, and those with river mouths or backwaters saw larger inundation distances. Presence of seawalls at the Kerala and Tamil Nadu coasts reduced the impact of the waves. However, when the seawalls were made of loose stones, the stones were displaced and carried a few metres inland.
Others on the mainland
The state of Kerala experienced tsunami-related damage in three southern densely populated districts, Ernakulam, Alappuzha, and Kollam, due to diffraction of the waves around Sri Lanka. The southernmost district of Thiruvananthpuram, however, escaped damage, possibly due to the wide turn of the diffracted waves at the peninsular tip. Major damage occurred in two narrow strips of land bound on the west by the Arabian Sea and on the east by the Kerala backwaters. The waves receded before the first tsunami with the highest fatality reported from the densely populated Alappad panchayat (including the villages of Cheriya Azhikkal and Azhikkal) at Kollam district, caused by a 4 m (13 ft) tsunami.
Many villages in the state of Andhra Pradesh were destroyed. In the Krishna district, the tsunami created havoc in Manginapudi and on Machalipattanam Beach. The most affected was Prakasham District, recording 35 deaths, with maximum damage at Singraikonda. Given the enormous power of the tsunami, the fishing industry suffered the greatest. Moreover, the cost of damage in the transport sector was reported in the tens of thousands.
Andaman and Nicobar Islands
The tsunami arrived in the Andaman and Nicobar Islands minutes after the earthquake causing extensive devastation to the islands' environment. Specifically, the Andaman Islands were moderately affected while the island of Little Andaman and the Nicobar Islands were severely affected by the tsunami. The tsunami survey was carried out in Little Andaman, South Andaman, mainly in and around Port Blair, Car Nicobar along the Kankana-Mus sector, and Great Nicobar.
In South Andaman, based on local eyewitnesses, there were three tsunami waves. Of the three, the third was the most devastating. Flooding occurred at the coastlines of the islands and low-lying areas inland, connected to open sea through creeks. Inundation was observed, along the east coast of South Andaman Island, restricted to Chidiyatapu, Burmanallah, Kodiaghat, Beadnabad, Corbyn's cove and Marina Park/Aberdeen Jetty areas. Along the west coast, the inundation was observed around Guptapara, Manjeri, Wandoor, Collinpur and Tirur regions. Several near-shore establishments and numerous infrastructures such as seawalls and a 20 MW diesel-generated power plant at Bamboo Flat were extensively damaged.
Results of the tsunami survey in South Andaman along Chiriyatapu, Corbyn's Cove and Wandoor beaches:
- 5 m (16 ft) in maximum tsunami height with a run-up of 4.24 m (13.9 ft) at Chiriyatapu Beach
- 5.5 m (18 ft) in maximum tsunami height and run-up at Corbyn's Cove Beach
- 6.6 m (22 ft) in maximum tsunami height and run-up of 4.63 m (15.2 ft) at Wandoor Beach
Meanwhile, in the Little Andaman, tsunami waves impinged on the eastern shore of this island 25 to 30 minutes after the earthquake in a four-wave cycle of which the fourth one was most devastating with a wave height of about 10 m (33 ft). The tsunami water destroyed settlements at Hut Bay within a range of 1 km (0.62 mi) from the seashore. Run up level up to 3.8 m (12 ft) have been measured.
In Malacca located on the island of Car Nicobar, there were three tsunami waves. The first wave came 5 minutes after the earthquake, preceded by the recession of seawater up to 600–700 m (2,000–2,300 ft). The second and third waves came in 10 minutes intervals after the first wave. The third wave was the strongest, with a maximum tsunami wave height of 11 m (36 ft). Waves nearly three stories high devastated the Indian Air Force base, located just south of Malacca. The maximum tsunami wave height of 11 m (36 ft). Inundation limit was found to be up to 1.25 km (0.78 mi) inland. The impact of the waves was so severe that four Oil tankers of IOC were thrown almost 800 m (2,600 ft) from the seashore near Malacca to Air force colony main gate. In Chuckchucha and Lapati, the tsunami arrived in a three-wave cycle with a maximum tsunami wave height of 12 m (39 ft).
In Campbell Bay of Great Nicobar island, the tsunami waves hit the area three times with an inundation limit of 250–500 m (820–1,640 ft). The first wave came within 5 minutes of the earthquake. The second and third waves came in 10-minute intervals after the first. The second wave was the strongest. Deadly tsunami waves wreaked havoc in this densely populated Jogindar Nagar area, situated 13 km (8.1 mi) south of Campbell Bay. According to local information,[attribution needed] tsunami waves attacked the area three times. The first wave came five minutes after the mainshock (0629 hrs.) with a marginal drop in sea level. The second wave came 10 minutes after the first one with a maximum height of 4.8 m (16 ft) and caused the major destruction. The third wave came within 15 minutes after the second with lower wave height. The maximum inundation limit due to tsunami water was about 500 m (1,600 ft).
At Port Blair, the water receded before the first wave, and the third wave was the tallest and caused the most damage. However, at Hut Bay, Malacca and Campbell Bay—locations south of Port Blair—the water level rose by about 1–2 m (3 ft 3 in–6 ft 7 in) from the average sea level before the first wave crashed ashore.
- 1.5 m (4 ft 11 in) at Diglipur and Rangat at North Andaman Island
- 8 m (26 ft) high at Campbell Bay on Great Nicobar Island
- 10–12 m (33–39 ft) high at Malacca (in Car Nicobar Island) and at Hut Bay on Little Andaman Island
- 3 m (9.8 ft) high at Port Blair on South Andaman Island
The significant shielding of Port Blair and Campbell Bay by steep mountainous outcrops contributed to the relatively low wave heights at these locations, whereas the open terrain along the eastern coast at Malacca and Hut Bay contributed to the great height of the tsunami waves
The tsunami severely affected the Maldives at a distance of 2,500 km (1,600 mi) from the epicentre. Identically to Sri Lanka, survivors reported three waves with the second wave being the most powerful. Being rich in coral reefs, the Maldives provides an opportunity for scientists to assess the impact of a tsunami on coral atolls. The significantly lower tsunami impact on the Maldives compared to Sri Lanka is mostly due to the topography and bathymetry of the atoll chain with offshore coral reefs, deep channels separating individual atolls and its arrival within low tide which decreased the power of the tsunami. After the tsunami, there was some concern that the country might be submerged entirely and become uninhabitable. However, this was proven untrue. The highest tsunami wave measured was 4 m (13 ft) at Vilufushi Island. The tsunami arrived approximately 2 hours after the earthquake. The greatest tsunami inundation occurred at North Male Atoll, Male island at 250 m (820 ft) along the streets. The Maldives tsunami wave analysis:
- 1.3–2.4 m (4 ft 3 in–7 ft 10 in) at North Male Atoll, Male Island
- 2 m (6 ft 7 in) at North Male Atoll, Huhule Island
- 1.7–2.8 m (5 ft 7 in–9 ft 2 in) at South Male Atoll, Embudhu Finothu
- 2.5–3.3 m (8 ft 2 in–10 ft 10 in) at Laamu Atoll, Fonadhoo Island
- 2.2–2.9 m (7 ft 3 in–9 ft 6 in) at Laamu Atoll, Gan Island
- 2.3–3 m (7 ft 7 in–9 ft 10 in) at North Male Atoll, Dhiffushi Island
- 2.2–2.4 m (7 ft 3 in–7 ft 10 in) at North Male Atoll, Huraa Island
- more than 1.5 m (4 ft 11 in) at North Male Atoll, Kuda Huraa Island
In Myanmar, the tsunami caused only moderate damage, which arrived between 2 and 5.5 hours after the earthquake. Although the country's western Andaman Sea coastline lies at the proximity of the rupture zone, there were smaller tsunamis than the neighbouring Thai coast, probably because the main tsunami source did not extend to the Andaman Islands. Another factor is that some coasts of Taninthayi Division were protected by offshore islands of the Myeik Archipelago. Based on scientific surveys from Ayeyarwaddy Delta through Taninthayi Division, it is revealed that tsunami heights along the Myanmar coast were between 0.4–2.9 m (1 ft 4 in–9 ft 6 in). Eyewitnesses often compared the December tsunami heights with the "rainy season high tide"; although at most locations, the tsunami height was similar or smaller than the "rainy season high tide" level.
Tsunami survey heights:
- 0.6–2.3 m (2 ft 0 in–7 ft 7 in) around the Ayeyarwady delta
- 0.9–2.9 m (2 ft 11 in–9 ft 6 in) at Dawei area
- 0.7–2.2 m (2 ft 4 in–7 ft 3 in) around Myeik
- 0.4–2.6 m (1 ft 4 in–8 ft 6 in) around Kawthaung
Interviews with local people indicate that they did not feel the earthquake in Taninthayi Division or Ayeyarwaddy Delta. The 71 casualties can be attributed to poor housing infrastructure and additionally, the fact that the coastal residents in the surveyed areas live on flat land along the coast, especially in the Ayeyarwaddy Delta, and that there is no higher ground to which to evacuate. The tsunami heights from the 2004 December earthquake were not more than 3 m (9.8 ft) along the Myanmar coast, the amplitudes are slightly large off the Ayeyarwaddy Delta, probably because the shallow delta cause a concentration in tsunami energy.
The tsunami travelled 5,000 km (3,100 mi) west across the open ocean before striking the East African country of Somalia. Around 289 fatalities were reported in the Horn of Africa, drowned by four tsunami waves. The hardest-hit was a 650 km (400 mi) stretch of the Somalia coastline between Garacad (Mudug region) and Xaafuun (Bari region), which forms part of the Puntland province. Most of the victims were reported along the low-lying Xaafuun Peninsula. The Puntland coast in northern Somalia was by far the area hardest hit by the waves to the west of the Indian subcontinent. The waves arrived around noon local time.
Consequently, tsunami runup heights vary from 5 m (16 ft) to 9 m (30 ft) with inundation distances varying from 44 m (144 ft) to 704 m (2,310 ft). The maximum runup height of almost 9 m (30 ft) was recorded in Bandarbeyla. An even higher runup point was measured on a cliff near the town of Eyl, solely on an eyewitness account.
The highest death toll was in Hafun, with 19 dead and 160 people presumed missing out of its 5000 inhabitants. This was the highest number of casualties in a single African town and the largest tsunami death toll in a single town to the west of the Indian subcontinent. In Xaafuun, small drawbacks were observed before the third and most powerful tsunami wave flooded the town.
The tsunami also reached Malaysia, mainly on the northern states such as Kedah, Perak and Penang and on offshore islands such as Langkawi island. Peninsular Malaysia was shielded by the full force of the tsunami due to the protection offered by the island of Sumatra, which lies just off the western coast.
Bangladesh escaped major damage and deaths because the water displaced by the strike-slip fault was relatively little on the northern section of the rupture zone, which ruptured slowly. In Yemen, the tsunami killed two people with a maximum runup of 2 m (6 ft 7 in).
The tsunami was detected in the southern parts of east Africa, where rough seas were reported, specifically on the eastern and southern coasts that face the Indian Ocean. A few other African countries also recorded fatalities; one in Kenya, three in Seychelles, ten in Tanzania, and South Africa, where two were killed as a direct result of the tsunami—the furthest from the epicentre.
According to the U.S. Geological Survey, a total of 227,898 people died. Measured in lives lost, this is one of the ten worst earthquakes in recorded history, as well as the single worst tsunami in history. Indonesia was the worst affected area, with most death toll estimates at around 170,000. An initial report by Siti Fadilah Supari, the Indonesian Minister of Health at the time, estimated the death total to be as high as 220,000 in Indonesia alone, giving a total of 280,000 fatalities. However, the estimated number of dead and missing in Indonesia were later reduced by over 50,000. In their report, the Tsunami Evaluation Coalition stated, "It should be remembered that all such data are subject to error, as data on missing persons especially are not always as good as one might wish". A much higher number of deaths has been suggested for Myanmar based on reports from Thailand.
The tsunami caused severe damage and deaths as far as the east coast of Africa, with the furthest recorded fatality directly attributed to the tsunami at Rooi-Els, close to Cape Town, 8,000 km (5,000 mi) from the epicentre. In total, eight people in South Africa died due to high sea levels and waves.
Relief agencies reported that one-third of the dead appeared to be children. This was a result of the high proportion of children in the populations of many of the affected regions and because children were the least able to resist being overcome by the surging waters. Oxfam went on to report that as many as four times more women than men were killed in some regions because they were waiting on the beach for the fishers to return and looking after their children in the houses.
States of emergency were declared in Sri Lanka, Indonesia, and the Maldives. The United Nations estimated at the outset that the relief operation would be the costliest in human history. Then-UN Secretary-General Kofi Annan stated that reconstruction would probably take between five and ten years. Governments and non-governmental organizations feared that the final death toll might double as a result of diseases, prompting a massive humanitarian response.
In addition to a large number of local residents, up to 9,000 foreign tourists (mostly Europeans) enjoying the peak holiday travel season were among the dead or missing, especially people from the Nordic countries. The European nation hardest hit was Sweden, with a death toll of 543. Germany was close behind with 539 identified victims.
|Affected country[a]||Confirmed deaths||Estimated deaths[b]||Injured||Missing||Displaced||Ref|
The level of damage to the economy resulting from the tsunami depends on the scale examined. While local economies were devastated, the overall impact on the national economies was minor. The two main occupations affected by the tsunami were fishing and tourism. The impact on coastal fishing communities and the people living there, some of the poorest in the region, has been devastating with high losses of income earners as well as boats and fishing gear. In Sri Lanka artisanal fishery, where the use of fish baskets, fishing traps, and spears are commonly used, is an important source of fish for local markets; industrial fishery is the major economic activity, providing direct employment to about 250,000 people. In recent years the fishery industry has emerged as a dynamic export-oriented sector, generating substantial foreign exchange earnings. Preliminary estimates indicate that 66% of the fishing fleet and industrial infrastructure in coastal regions have been destroyed by the wave surges, which will have adverse economic effects both at local and national levels.
While the tsunami destroyed many of the boats vital to Sri Lanka's fishing industry, it also created a demand for fibreglass reinforced plastic catamarans in boatyards of Tamil Nadu. Since over 51,000 vessels were lost to the tsunami, the industry boomed. However, the huge demand has led to lower quality in the process, and some important materials were sacrificed to cut prices for those who were impoverished by the tsunami.
Some economists believe that damage to the affected national economies will be minor because losses in the tourism and fishing industries are a relatively small percentage of the GDP. However, others caution that damage to infrastructure is an overriding factor. In some areas drinking water supplies and farm fields may have been contaminated for years by saltwater from the ocean. Even though only coastal regions were directly affected by the waters of the tsunami, the indirect effects have spread to inland provinces as well. Since the media coverage of the event was so extensive, many tourists cancelled vacations and trips to that part of the world, even though their travel destinations may not have been affected. This ripple effect could especially be felt in the inland provinces of Thailand, such as Krabi, which acted as a starting point for many other tourist destinations in Thailand.
Both the earthquake and the tsunami may have affected shipping in the Malacca Straits, which separate Malaysia and the Indonesian island of Sumatra, by changing the depth of the seabed and by disturbing navigational buoys and old shipwrecks. In one area of the Strait, water depths were previously up to 1,200 m (4,000 ft), and are now only 30 m (100 ft) in some areas, making shipping impossible and dangerous. These problems also made the delivery of relief aid more challenging. Compiling new navigational charts may take months or years. However, officials hope that piracy in the region will drop off as a result of the tsunami.
Countries in the region appealed to tourists to return, pointing out that most tourist infrastructure is undamaged. However, tourists were reluctant to do so for psychological reasons. Even beach resorts in parts of Thailand which were untouched by the tsunami were hit by cancellations.
Beyond the heavy toll on human lives, the Indian Ocean earthquake has caused an enormous environmental impact that will affect the region for many years to come. It has been reported that severe damage has been inflicted on ecosystems such as mangroves, coral reefs, forests, coastal wetlands, vegetation, sand dunes and rock formations, animal and plant biodiversity and groundwater. Also, the spread of solid and liquid waste and industrial chemicals, water pollution and the destruction of sewage collectors and treatment plants threaten the environment even further, in untold ways. The environmental impact will take a long time and significant resources to assess.
According to specialists, the main effect is being caused by poisoning of the freshwater supplies and of the soil by saltwater infiltration and a deposit of a salt layer over arable land. It has been reported that in the Maldives, 16 to 17 coral reef atolls that were overcome by sea waves are without fresh water and could be rendered uninhabitable for decades. Uncountable wells that served communities were invaded by sea, sand, and earth; and aquifers were invaded through porous rock. Salted-over soil becomes sterile, and it is difficult and costly to restore for agriculture. It also causes the death of plants and important soil micro-organisms. Thousands of rice, mango, and banana plantations in Sri Lanka were destroyed almost entirely and will take years to recover. On the island's east coast, the tsunami contaminated wells on which many villagers relied for drinking water. The Colombo-based International Water Management Institute monitored the effects of saltwater and concluded that the wells recovered to pre-tsunami drinking water quality one and a half years after the event. The IWMI developed protocols for cleaning wells contaminated by saltwater; these were subsequently officially endorsed by the World Health Organization as part of its series of Emergency Guidelines.
The United Nations Environment Programme (UNEP) is working with governments of the region in order to determine the severity of the ecological impact and how to address it.[needs update] UNEP has decided to earmark a US$1,000,000 emergency fund and to establish a Task Force to respond to requests for technical assistance from countries affected by the tsunami. In response to a request from the Maldivian Government, the Australian Government sent ecological experts to help restore marine environments and coral reefs—the lifeblood of Maldivian tourism. Much of the ecological expertise has been rendered from work with the Great Barrier Reef, in Australia's northeastern waters.
The last major tsunami in the Indian Ocean was about A.D. 1400. In 2008, a team of scientists working on Phra Thong, a barrier island along the hard-hit west coast of Thailand, reported evidence of at least three previous major tsunamis in the preceding 2,800 years, the most recent from about 700 years ago. A second team found similar evidence of previous tsunamis in Aceh, a province at the northern tip of Sumatra; radiocarbon dating of bark fragments in the soil below the second sand layer led the scientists to estimate that the most recent predecessor to the 2004 tsunami probably occurred between A.D. 1300 and 1450.
The 2004 earthquake and tsunami combined is the world's deadliest natural disaster since the 1976 Tangshan earthquake. The earthquake was the third most powerful earthquake recorded since 1900. The deadliest known earthquake in history occurred in 1556 in Shaanxi, China, with an estimated death toll of 830,000, though figures from this period may not be as reliable.
Before 2004, the tsunami created in both Indian and Pacific Ocean waters by the 1883 eruption of Krakatoa, thought to have resulted in anywhere from 36,000 to 120,000 deaths, had probably been the deadliest in the region. In 1782, about 40,000 people are thought to have been killed by a tsunami (or a cyclone) in the South China Sea. The deadliest tsunami before 2004 was Italy's 1908 Messina earthquake on the Mediterranean Sea where the earthquake and tsunami killed about 123,000.
Many health professionals and aid workers have reported widespread psychological trauma associated with the tsunami. Traditional beliefs in many of the affected regions state that a relative of the family must bury the body of the dead, and in many cases, no body remained to be buried. Women in Aceh required a special approach from foreign aid agencies, and continue to have unique needs.
The hardest-hit area, Aceh, is a religiously conservative Islamic society and has had no tourism nor any Western presence in recent years due to the insurgency between the Indonesian military and Free Aceh Movement (GAM). Some believe that the tsunami was divine punishment for lay Muslims shirking their daily prayers or following a materialistic lifestyle. Others have said that Allah was angry that Muslims were killing each other in an ongoing conflict. Saudi cleric Muhammad Al-Munajjid attributed it to divine retribution against non-Muslim vacationers "who used to sprawl all over the beaches and in pubs overflowing with wine" during Christmas break.
The widespread devastation caused by the tsunami led GAM to declare a cease-fire on 28 December 2004 followed by the Indonesian government, and the two groups resumed long-stalled peace talks, which resulted in a peace agreement signed 15 August 2005. The agreement explicitly cites the tsunami as a justification.
In a poll conducted in 27 countries, 15% of respondents named the tsunami the most significant event of the year. Only the Iraq War was named by as many respondents. The extensive international media coverage of the tsunami, and the role of mass media and journalists in reconstruction, were discussed by editors of newspapers and broadcast media in tsunami-affected areas, in special video-conferences set up by the Asia Pacific Journalism Centre.
The tsunami left both the people and government of India in a state of heightened alert. On 30 December 2004, four days after the tsunami, Terra Research notified the India government that its sensors indicated there was a possibility of 7.9 to 8.1 magnitude tectonic shift in the next 12 hours between Sumatra and New Zealand. In response, the Indian Minister of Home Affairs announced that a fresh onslaught of deadly tsunami was likely along the southern Indian coast and the Andaman and Nicobar Islands, even as there was no sign of turbulence in the region. The announcement generated panic in the Indian Ocean region and caused thousands to flee their homes, which resulted in jammed roads. The announcement was a false alarm, and the Home Affairs minister withdrew their announcement. On further investigation, the India government learned that the consulting company Terra Research was run from the home of a self-described earthquake forecaster who had no telephone listing and maintained a website where he sold copies of his detection system.
The tsunami had a severe humanitarian and political impact in Sweden. The hardest-hit country outside Asia, Sweden, lost 543 tourists, mainly in Thailand. The Persson Cabinet was heavily criticized for its inaction.
Smith Dharmasaroja, a meteorologist who had predicted that an earthquake and tsunami "is going to occur for sure" way back in 1994, was assigned the development of the Thai tsunami warning system. The Indian Ocean Tsunami warning system was formed in early 2005 to provide an early warning of tsunamis for inhabitants around the Indian Ocean coasts.
The changes in the distribution of masses inside the Earth due to the earthquake had several consequences. It displaced the North Pole by 25 mm (0.98 in). It also slightly changed the shape of the Earth, specifically by decreasing Earth's oblateness by about one part in 10 billion, consequentially increasing Earth's rotation a little and thus shortening the length of the day by 2.68 microseconds.
A great deal of humanitarian aid was needed because of widespread damage to the infrastructure, shortages of food and water, and economic damage. Epidemics were of particular concern due to the high population density and tropical climate of the affected areas. The main concern of humanitarian and government agencies was to provide sanitation facilities and fresh drinking water to contain the spread of diseases such as cholera, diphtheria, dysentery, typhoid and hepatitis A and hepatitis B.
There was also a great concern that the death toll could increase as disease and hunger spread. However, because of the initial quick response, this was minimized.
In the days following the tsunami, significant effort was spent in burying bodies hurriedly due to fear of disease spreading. However, the public health risks may have been exaggerated, and therefore this may not have been the best way to allocate resources. The World Food Programme provided food aid to more than 1.3 million people affected by the tsunami.
Nations all over the world provided over US$14 billion in aid for damaged regions, with the governments of Australia pledging US$819.9 million (including a US$760.6-million aid package for Indonesia), Germany offering US$660 million, Japan offering US$500 million, Canada offering US$343 million, Norway and the Netherlands offering both US$183 million, the United States offering US$35 million initially (increased to US$350 million), and the World Bank offering US$250 million. Also, Italy offered US$95 million, increased later to US$113 million of which US$42 million was donated by the population using the SMS system
According to USAID, the US has pledged additional funds in long-term U.S. support to help the tsunami victims rebuild their lives. On 9 February 2005, President Bush asked Congress to increase the U.S. commitment to a total of US$950 million. Officials estimated that billions of dollars would be needed. Bush also asked his father, former President George H. W. Bush, and former President Bill Clinton to lead a U.S. effort to provide private aid to the tsunami victims.
In mid-March, the Asian Development Bank reported that over US$4 billion in aid promised by governments was behind schedule. Sri Lanka reported that it had received no foreign government aid, while foreign individuals had been generous. Many charities were given considerable donations from the public. For example, in the United Kingdom, the public donated roughly £330,000,000 sterling (nearly US$600,000,000). This considerably outweighed the allocation by the government to disaster relief and reconstruction of £75,000,000 and came to an average of about £5.50 (US$10) donated by every citizen.
In August 2006, fifteen local aid staff working on post-tsunami rebuilding were found executed in northeast Sri Lanka after heavy fighting, the main umbrella body for aid agencies in the country said.
In popular culture
Film and television
- Children of Tsunami: No More Tears (2005), a 24-minute documentary
- The Wave That Shook The World (2005), educational television-series documentary about the tsunami
- Tsunami: The Aftermath (2006), a two-part television miniseries about its aftermath
- Hereafter (2010), a main character's life is affected after surviving the tsunami while on vacation
- Hafalan Shalat Delisa (2011), an Indonesian movie
- The Impossible (2012), an English-language Spanish film based on the story of María Belón and her family
- Kayal (2014), a Tamil drama film which culminates with the tsunami
- Paint the Sky with Stars, Selected Poetry in Remembrance of the Boxing Day Tsunami 2004 (2005) edited by Stephen Robert Kuta
- The Killing Sea (2006), two teenagers struggle to survive in the days after the tsunami
- Wave (2013), a memoir by Sonali Deraniyagala
- "12/26" by Kimya Dawson, about the event and the humanitarian efforts, from the perspective of a victim whose family died in the disaster
- Deaths in December 2004 – Notable people killed in the 2004 Indian Ocean tsunami
- List of earthquakes in 2004
- List of earthquakes in Japan
- List of natural disasters by death toll
- Lists of earthquakes
- List of conspiracy theories
- "Magnitude 9.1 – Off the West Coast of Sumatra". U.S. Geological Survey. Archived from the original on 17 August 2012. Retrieved 26 August 2012.
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|Wikimedia Commons has media related to 2004 Indian Ocean earthquake.|
|Wikisource has original text related to this article:|
- ReliefWeb's main page for this event.
- The Sumatra-Andaman Islands Earthquake – IRIS Consortium
- M9.1 Sumatra-Andaman Earthquake & Tsunami, 2004 – Amateur Seismic Centre (ASC)
- Asian Tsunami Anniversary – Thailand Tsunami Then and Now Comparison Series – Zoriah Miller
- The International Seismological Centre has a bibliography and/or authoritative data for this event.