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Chapter 10 - Waves

This chapter focuses on the phenomena associated waves on bodies of water (oceans, lakes, etc.)
In oceanography, waves are:

• Short-term changes in sea level.
• A wave is energy moving through water.

Waves are generated by a "disturbing force" - something that transmits energy into a fluid medium (such as wind blowing on water). A pebble hitting a puddle generates a splash that creates ripples (tiny waves) that propagate away from the source (Figure 10-2). The ripples grow smaller as they move away from the splash (source) until they diffuse away with increasing distance, or when it encounters the edge of the puddle.

Click on thumbnail images for a larger view.

Wave crashing on shore
Fig. 10-1. A wave crashing onshore releases energy.

Wind is the disturbing force for waves in the ocean and large bodies of water. Waves are also generated by earthquakes, landslides, and volcanic eruptions (producing tsunamis), and tides are produced by gravitational interactions between the Earth, Moon and Sun.

Types of waves

Wind Waves
Gravity Tides
• Height = range from small ripples up to 60 feet (sometimes higher)
• Speed = 10 – 75 mph
• Periods = 5 – 25 sec.
• Height = open ocean less than 2 feet;
-- onshore up to 300 feet
• Speed = jetliner speeds 400-500 mph
• Wavelength = 100’s of kilometers
• Periods = minutes
Height = up to 50 feet plus
Period 12 ½ to 25 hours

(discussed in Chapter 10)

See: BIGGEST WAVE in the World surfed 100ft at Carlos Burle Portugal (YouTube video)

Splash with ripples
Fig. 10-2. A splash is an example of a disturbing force creating waves.

Terms Used To Describe Waves

Crest - the highest part of a passing linear wave
Trough - the lowest part of a passing linear wave

- Wavelength (L) = Distance between waves
- Period (T) = Time between passing waves
- Height (h) = Height from crest to trough (same as "amplitude")
- Water depth (d) = Average water depth - determines wave behavior

Characteristics of Waves

Ocean waves are created by wind blowing over water. The distance between two wave crests or two wave troughs is called the wavelength. Wave height is the vertical distance between the highest (crest) and lowest (trough) parts of a wave. (Figure 10-3). Wave period is the time interval between passing wave crests (completing one cycle) and are measured as wave crests pass a stationary point (such as waves passing a buoy or pole on a pier)(Figure 10-4).
Fig. 10-3. Wavelength and wave height of wave cycles.
Swells approaching a coastline
Fig. 10-4. Waves approaching a shoreline arrive at cyclic intervals called a period.

Wave Speed and Wave Energy

Wave speed is a function of wavelength and wave period, and is related to the wind velocity where the waves form.

Wave speed (c) is the distance the wave travels divided by the time it takes to travel that distance. Wave speed is determined by dividing the wavelength (L) by the wave period (T). [c = L/T]. Wave period is the average of how many seconds pass between a series of wave crests moving past a stationary object in the water, such as a post on a pier or a buoy.

What is important is the combination of the wave height and wave period. Wave period is directly related to the speed the wave is traveling. The longer the period, the faster the wave, and the more energy in contains.
The greater the period the faster the wave moves (Figure 10-5). Also, the greater the period, typically the higher the wave breaks as it approaches the shore.  
Wave speed compared with period
Fig. 10-5. Comparison of wavelength to wave speed and wave period.

Wave Base

The wave base, which is the depth of influence of a passing water wave, it is about half the wavelength of passing water waves. At depths greater than half the wavelength wave motion dies out—the water motion is less than 4% of its value at the water surface and is generally insignificant.

Wave Orbits and Orbital Depth

Passing waves create a circular current in the water. This is revealed by the orbit-like motion of particles in the water. The orbital motion of a wave is greatest at the surface and diminishes with depth. Orbital depth is the depth to which the orbital motion of the wave energy can be felt. Orbital depth is equal to half of the wavelength. At the sea surface, orbital diameter is equal to wave height. As depth increases, less wave energy can be felt. The orbital depth is the depth where zero wave energy remains. For example, if a wave at the surface has a height of 4 meters and a wavelength of 48 m, then the depth where no motion from the wave exists is 48/2 or 24 meters.

Deep-Water Waves and Shallow-Water Waves

The depth of the water determines the character of wave behaviors.

Deep-water waves are waves passing through water greater than half of its wavelength. Deep-water waves are waves of oscillation. A wave of oscillation is a wave in the open ocean where movement in the water below a passing wave is in a vertical circular motion.

Shallow-water waves are waves that are interacting with the seabed in depths less than half it wavelength. Shallow-water waves are called waves of transition because they change character as the move shoreward and dissipate their energy interacting with the seabed.

Type of wave Define Orbit Speed
Deep water wave (wave of oscillation) d > L/2 Circle L/T
Shallow water wave (wave of transition) d < L/20 Elliptical √gd
• L/2 to L/20 is a transitional wave
• Speed of a shallow water wave is dependent on water depth
• G = gravitational constant 9.8 m/s2

Wind Waves Approaching the Shore:
• As a wave approaches shallow water its begins to transform when it's orbital depth comes in contact with the seabed (when d < L/2).
• The friction caused by waves interacting with the seabed causes waves to slow down as the move onshore.
• The friction of the seabed begins to slow the bottom of the wave; whereas the top of the wave does not slow as quickly..
• Circular motion within the wave becomes interrupted and becomes elliptical.
• As waves approach the beach, their wavelengths (L) and velocity decrease. However the period (T) stays the same. The shortening of the wavelength results in an increase in wave height as it moves into shallow water.
• A wave breaks when the water depth (d) is about the same as the wave height (h). Where a wave curls over on itself is called a breaker.
Breakers then turn into a turbulent front called "surf" that moves onto the beach.
• When the dying wave runs up on the beach and then retreats it is called "swash."

Wave oscillation
Fig. 10-6. Orbital oscillations in deep and shallow waves.
Fig. 10-7. Waves of oscillation, breakers, and waves of transition moving onto the beach.
Waves of transition approaching the beach
Fig. 10-8. Waves of transition build up, break, and become surf before ending on the beach as swash.
Wave cresting during a high swell in the Atlantic, Puerto Rico
Fig. 10-9. A breaking wave (with surfer in Puerto Rico)


When a wave approaches shore, the base of the wave encounters the bottom—the front of the wave slows down and the back overtakes the front. This forces the water into a peak that curves forward. This peak will eventually fall forward in a tumbling rush of foam and water called a breaker. Waves break on or near shore, they also crash over reefs or offshore sandbars if water depths are shallow.

Wave steepness
is the ratio of height to wavelength. When wave steepness exceeds a ratio of 1:7, breakers form.

Example: If a moving wave has a height of one foot and a length from crest to crest of 8 feet, then the ratio is 1:8 and this wave is not going to break. However, if the height is 1 foot and the length decreases to 6 feet, then the ratio is 1:6, then the wave has now become steep enough that the crest topples and the wave breaks.

Slope of the seabed/beach creates different kinds of "Breakers"

There are three types of breaking waves: spilling breakers, plunging breakers, and surging breakers. Breakers may be one or a combination of these types.

Gentle slopes produce spilling breakers. Spilling breakers begin far from shore and take a relatively longer time to reach the beach. The breaking crest slides down the front of the wave in a flurry of foam as the wave moves shoreward. Spilling breakers give surfers a long slow ride.

Moderate slopes
produce plunging breakers. Plunging breakers build up rapidly into a steeply leaning crest. The crest curls further forward of the rest of the wave before crashing down in the surf zone. Plunging breakers are dangerous because the crash into shallow water.

Steep slopes produce surging breakers. Surging breakers occur where waves slam directly on the shoreline. With no gentle slope the waves surge onto a steep beach, producing no tumbling surf. Surging breakers also create huge splashes on a rocky cliff shoreline.
Spilling breakers at Torrey Pines Beach Plunging breaker Surging waves on a Hawaii black sand beach Waves crashing on sea cliff at Point Reyes Headlands
Fig. 10-10. Spilling breakers at Torrey Pines Beach, CA. Fig. 10-11. Plunging breaker (threatens a boat). Fig. 10-12. Surging breaker on a narrow Hawaii beach. Fig. 10-13. Surging wave crashing on seacliffs

Wave Trains

A wave train is a group of waves of equal or similar wavelengths traveling in the same direction. Individual waves move from the back to the front of a wave train, gradually building up, peaking, then declining as it moves to the front of the wave train (Figure 10-14). The result is that individual waves within a wave train are moving about twice as the wave train itself. Surfers watching advancing waves may notice that the first waves to arrive decline in intensity as they arrive as the following waves build higher. After the highest crest passes, the trailing waves decline in intensity as the wave train passes.
Waves moving through a wave train
Fig. 10-14. Waves moving through a wave train.

Origin of Wind Waves

Wind waves form from wind blowing on the ocean surface. The key factors influencing wave intensity include fetch, wind duration, wind strength, and proximity to wind source area. Wind energy is gradually transferred to the waves forming on a body of water, causing waves to absorb energy and grow in amplitude and period over distance and time (Figure 10-15). The transfer of wind energy to wave energy is not very efficient (only about 2% of the energy is actually transferred) but it is the size of the area that that the wind is impacting, as well as how strong the wind is blowing that matters.

Wind-Wave Input Factors:
Fetch is the "length" (distance) wind blows over open water. This is the uninterrupted distance over which the wind blows without significant change in direction.
Duration is how long the wind blows. Strong wind that does not blow for a long period will not generate large waves.
Wind strength: The stronger the wind, the bigger the waves. The wind must be moving faster than the wave crests for energy to be transferred.
Proximity: Separation of wave trains by period. Long-period waves move faster than shorter-period waves and will separate and advance before wave trains with shorter periods.

Wind-Wave Output Factors: (Waves!)
Wave height increases.
Wavelength increases.
Wave period increases.
• Direction - wave travel in the direction that the wind blows.

Wave Equation: Large Fetch + Long Duration + Strong Winds (wind speed) = Large, Long Period Waves

Fetch is important because the interrelationship between wind speed and duration, both functions of fetch, is predictive of wave conditions.

Fig. 10-15. Waves energy depends on wind speed, wind duration, and fetch.
Storm "sea" and "swell"
Figure 10-16. Sea and Swells illustrated. A storm generates winds that impact a region over open water. The area impacted by the wind is called a "sea." The waves generated by the storm will move out and away from sea are called "swell."

"Sea" and "Swell"

Sea: Area where wind waves are generated, mixed period and wavelengths. Seas are typically a chaotic jumble of waves of many different sizes (wave heights, wavelengths, and periods) (Figure 10-16).
Fully Developed Sea: Max size waves can grow given a certain fetch, wind speed and duration.

Ocean swell refers to series of ocean surface waves that were not generated by the local wind. Swell refers to an increase in wave height due to a distant storm. Ocean swell waves often have a long wavelength. Swell can develop on lakes and bays, but their size varies with the size of the water body and wave intensity. As waves move out and away from the storm center, they sort themselves out into groups of similar speeds and wavelengths. This produces the smooth undulating ocean surface called a swell. Swells may travel thousands of kilometers from the storm center until they strike shore. Swells are generated by storms over the open ocean, but many ocean swells originate in the oceans around Antarctica where there is high winds with nearly infinite duration and fetch (Figure 10-17).
Origin of ocean swells in the southern oceans
Fig. 10-17. Most ocean swells originate in the southern oceans where strong winds combine with unlimited fetch.

How Waves Form

When the wind starts to blow, the surface of a water body will go through a progression as waves form and intensify. When the wind starts to blow, the ocean surface will change from calm (mirror-like) conditions to form capillary waves (ripples), chop, wavelets, to waves (each with increasing wavelengths, wave heights, and wave periods). Smaller wave features can form on existing larger wave features, adding to the complexity of the water's surface.

Ripples (Capillary Waves)

Capillary waves are very small waves with wavelengths less than 1.7 cm or 0.68 inches (Figure 10-18). The formation of capillary waves is influenced by both the effects of surface tension and gravity. The ruffling of the water’s surface due to pressure variations of the wind on the water. This creates stress on the water and results in tiny short wavelength waves called ripples. Ripples are often called capillary waves. The motion of a ripple is governed by surface tension.They are the first waves to form when the wind blows over the surface of the water and are created by the friction of wind and the surface tension of the water. These tiny little waves increase the surface area of the sea surface and if the wind continues to blow, the size of the wave will increase in size and become a wind wave.


Chop refers to small waves causing the ocean surface to be rough. Ripples and small wavelets form and move independently of large waves moving through an area, creating rough and irregular wave patterns (Figure 10-19).

capillary ripples forming around calm patches on Lake Hodges
Fig. 10-18. Capillary wave (ripples) forming next to a calm area (Lake Hodges, CA)
Ripples merge into wavelets in choppy water
Fig. 10-19. With increasing fetch, ripples merge to become wavelets in choppy surface water conditions.

Cat's Paws

A "cat's paw" is the imprint that a light breeze that ruffles small areas of a water surface. When generated by light wind in open water, a nautical name for them is "cat's paw" waves, since they may resemble paw prints (Figure 10-20). Light breezes which stir up such small ripples are also sometimes referred to as cat's paws. On the open ocean, much larger ocean surface waves (seas and swells) may result from coalescence of smaller wind-caused ripple-waves.

A squall is a a sudden violent gust of wind or a localized storm. A squall line is a line of thunderstorms that can form along or ahead of a cold front. It contains heavy precipitation, hail, frequent lightning, strong straight-line winds, and possibly tornadoes and waterspouts. At sea, a squall is used to describe a relatively rapid change in weather from calm or mild weather to sudden strong winds and intense precipitation, usually associated with passing a cold front.

"Cat paws" (ripple patches) on Lake Hodges
Fig. 10-20. Wind gusts creating "cat paws" capillary ripple patterns on the lake surface.

Beaufort Wind Force Scale (Wind Velocity, Wave Height, and Sea Conditions)

The Beaufort wind force scale relates wind speed (velocity) to observed conditions at sea (including wave height) or impact of features on land. It is a numbered scale from 0 to 12 to describe sea conditions and wave size. The Beaufort Scale was developed by Rear Admiral Sir Francis Beaufort 1774-1857, an officer in Britain's Royal Navy). Zero 0 on the Beaufort scale represents the calmest of seas (the water is so smooth that it looks like glass). A 12 on the Beaufort scale represents hurricane force waves (Figure 10-21).
Beaufort scale
Figure 10-21. Beaufort Wind Force Scale for sea conditions (and on land).

Wave Interference Patterns

Wave interference occurs where waves from different sources collide (Figures 10-22 and 10-23).

Constructive wave interference occurs where waves come together in phase or crest meets another crest (or trough meets another trough) .

Destructive wave interference: Waves come together out of phase or crest meets a trough.
Wave interference Ripples merge into wavelets in choppy water
Fig. 10-22. Examples of constructive and destructive wave interference patterns. Fig. 10-23. Interference patterns created by winds gusts blowing from different directions.

Rouge Waves

Rouge waves are large, unpredictable, and dangerous. Rouge waves (also called 'extreme storm waves') are those waves which are greater than twice the size of surrounding waves. They often come unexpectedly from directions other than prevailing wind and waves. Many reports of extreme storm waves describe them sudden "walls of water." They are often steep-sided and associated with unusually deep troughs. Some rouge waves are a result of constructive interference of swells traveling at different speeds and directions. As these swells pass through one another, their crests, troughs, and wavelengths sometimes coincide and reinforce each other. This process produces large, towering waves that quickly form and disappear. If the swells are traveling roughly in the same direction, these massive waves may last for several minutes before subsiding. Rouge waves can also form when storm swells move against a strong current, resulting in a shortening of the wavelength and increasing it’s amplitude. Large rouge wave of this kind are frequently experienced in the Gulf Stream and Agulhas currents (Figure 10-24).
Rouge wate
Fig. 10-24. This 60 foot rouge wave threatened a ship in the Gulf Stream near Charleston, South Carolina.

Behavior of Waves

Waves can bend when they encounter obstacles or changes on the sea floor.

Refraction involves bending. Wave refraction starts when wave base starts to interact with the sea bed and slow the waves down, causing them to bend toward shore. Refraction occurs when wave swells approach the beach at an angle (Figure 10-25).

Diffraction involves spreading (or dispersion) of wave energy. Wave diffraction refers to various phenomena which occur when a wave encounters an obstacle or change in geometry of the seabed. For example waves are diffracted when they when they pass an island, or when they pass a point or other structure, such as a jetty at the mouth of a harbor (Figure 10-26).

Reflection (bouncing) involves crashing into a solid surface (such as a seawall or cliff) and reflecting back to sea. Reflection can result in standing waves—waves that move back and forth (oscillate) in a vertical position waves strike an obstruction head-on and then are reflected backwards in the direction they came from.
Wave refraction near the seashore
Fig. 10-25. Wave refraction as waves approach the beach at an angle.
Wave diffraction
Fig. 10-26. Wave diffraction around offshore obstruction on waves nearshore

Surfer's Guide to Wave Forecasting for San Diego County

San Diego County "Swell Window"

• The compass bearing window that we can receive swell from is between 180° and 340° (Figure 10-27). Waves are weak on the “edges” of this window. The best part of our window is really between 200° and 300° degrees because the waves simply have to bend too much to be received on our coastline if they are outside of that range.

• North San Diego County is better for S + SW Swells
• South San Diego County is better for N + NW Swells
• Everyone loves a West Swell!

Swells affection San Diego region
Fig. 10-27. The "swell window" for San Diego County is roughly between 180° and 340° (with North being 360°).

Getting Swell Information Data Real-Time

Casual surfers in San Diego County can get "forecasts" of waves from a number of website (listed below). However,
professional "surfers" (and swell wave forecasters for navigation and other purposes) use real-time buoy information available from the National Data Buoy Center (NOAA) network to evaluate swell period and height in different parts of the Pacific Ocean basin and around the world. Data from this system is incorporated into many government weather and commercial shipping navigation websites and several surfing organization websites.

For example: check this "maximum wave energy" animation:

Surfers check at distant buoy locations to look for increases in "wave period," but not so much in wave height. (Why?)
Bouys throughout the world oceans
Fig. 10-28. Location of buoys associated with the National Data Buoy Center (NOAA)

Summer Swells Affecting San Diego County

• Large Storms (Largest on Earth) generate swell between Antarctica and New Zealand (Figure 10-29).
• Storm track is always West to East.
• Initial angle is 210 degrees, then moves towards 180 degrees and out of our swell window.

(Look at example: Buoy Station 51002)

• Timing is 9-10 days to San Diego from storms position. Equatorial Buoy is about ½ way in between.

• ??? What determines whether a swell is received in 9 or 10 days??? Wave speed/period!
• The Largest surf is in northern San Diego County comes from the south.

Winter Swells

• Largest swells on average
• Generated in the Gulf of Alaska, most begin off of the Kuril Islands
• Storm track is generally from West to East
• Early season swell is usually more Northerly, N or NNW direction or about 320 to 340 degrees.
• Later season storms drop farther south and give us a more westerly swell direction from about 280 to 300 degrees. We also get more rain from these storms.

• Timing is about 1 day from the offshore (way) California or Oregon Buoy. From Point Conception (Harvest Buoy) its about 6 hours. Harvest Buoy is best to get swell direction.

• Partial swell blockage occurs in the Southern California Bight from wave shadows created from the Channel Islands.
• Surf largest in Southern San Diego County and Northern Baja. We also can get colder water and upwelling conditions.
Circumpolar current around Antarctica
Fig. 10-29. The Antarctic Circumpolar wind belt is the source of most swells. Why?
NOAA bouy 51002
Fig. 10-30. The Antarctic Circumpolar wind belt is the source of most swells. Why?

Locally Generated Swell

We have a number of locally generated swells that come from smaller storms in the Pacific Northwest.
• These storms produce surf that has a shorter period (between 6 and 10 seconds) because the storms are not very large.
• The swell angle is very steep from the NNW around 320 to 340 degrees.
• We often get upwelling associated with these storms as well.

Hurricane Swell

During the late summer and early fall we can get swell from hurricanes that form off of the coast of mainland mexico.
• The wave periods generated from these storms is usually between 10 and 14 seconds.
• The key identifying waves from these storms is the angle. The swell angle begins from the S or SSE between 160 and 180 degrees. The angle increases with time as the storm moves up the coast and either onshore or out to sea towards Hawaii.
Beacons_Beach looking south
Fig. 10-31. A southwest swell coming in from the southwest at Beacons Beach, Encinitas, San Diego Co.


A tsunami
is a very long and/or high sea wave or coastal serge of water caused by an earthquake or other disturbance. Tsunamis get their name from Japan (where they are fairly common): "Tsu"[ harbor], "nami" [wave].

Tsunamis are caused by displacement of the earth's crust under an ocean or body of water of any size. They can also be generated by earthquakes, volcanic explosions, underwater landslides, even asteroid impacts. When the solid earth moves, the water above it also moves with it (Figures 10-32 and 10-33). Tsunamis are the result of both the initial shock waves and the following motion of the water readjusting to a stable pool (sea level). Tsunamis can travel great distances throughout the world's ocean. Their energy is dissipated when they approach shorelines where they come onshore as a great surge of water, with or without a massive "tidal wave" crashing onshore. Although most tsunamis are small (barely detectible), some modern tsunamis have reached inland elevations many hundreds of feet above sealevel.

Tsunami Characteristics:
• Tsunamis are usually less than 2 feet in the open ocean.
• In deep ocean, tsunami wavelengths are long, commonly 100’s of miles.
• Tsunamis always behave like shallow water waves ( d < L/20) because no ocean deep enough!
• Undetectable by ships in open ocean because wavelengths are so long (slow rise and fall as wave passes).
• Open ocean tsunami velocity is 400 – 500 mph. So about 4 – 5 hours from Alaska to San Diego (or Hawaii).
• Wave stacks up on continental shelf, about ½ of the time a trough arrives first (sea recedes from shore).
• Waves 30 – 100 ft are common – locally run-up can be higher.
• Highest is thought to be +300 ft., 66 million years ago from asteroid collision in the Gulf of Mexico.

Tsunami diagram
Fig. 10-32. How a tsunami is generated by an earthquake.
Tsunami surge
Fig. 10-33. Tsunamis move onshore more as a surge than just a wave.
Major Tsunami Events Cause and Effects Damages
Sumatra, Indonesia,
26 December 2004
The 9.1 magnitude earthquake offshore of Sumatra. The fault zone that caused the tsunami was roughly 1300 km long, vertically displacing the sea floor by several meters. Tsunami was as tall as 50 m, reaching 5 km inland. Many billions in damage, estimated 230,000 people killed.
North Pacific Coast, Japan,
11 March 2011
Tsunami was spawned by an 9.0 magnitude earthquake. Many coastal communities were destroyed and the Fukushima Daiichi nuclear power plant was damaged, releasing radiation 10m-high waves swept over the east coast of Japan, killing more than 18,000 people, Most expensive disaster in history: ~$235 billion.
Lisbon, Portugal,
1 November 1755
A magnitude 8.5 earthquake produced a series of three huge waves that struck various towns along the west coast of Portugal and Spain. Tsunami was up to 30 m high in some places The earthquake and tsunami killed an estimated 60,000 people in the Portugal, Spain, and Morocco.
Krakatoa, Indonesia,
27 August 1883
This tsunami event was caused by explosive eruptions of the Krakatoa caldera volcano in the Sunda Strait between the islands of Java and Sumatra. Multiple waves as high as 37 m. The event killed about 40,000 people in total; however, about 2,000 deaths were from the volcanic eruptions.
Enshunada Sea, Japan, 20 September 1498 An earthquake estimated about magnitude 8.3, caused tsunami waves along the coasts of Izu, Kii, Mikawa, Sagami, and Surugu (Japan). Coastal communities were washed away; estimated 31,000 people were killed.
Nankaido, Japan,
28 October 1707
A magnitude 8.4 earthquake caused tsunamis as high as 25 m that swept onto the Pacific coasts of Kyushyu, Shikoku and Honshin. About 30,000 buildings were damaged and about 30,000 people were killed.

Sanriku, Japan,
15 June 1896

An estimated magnitude 7.6 earthquake off the coast of Sanriku, Japan generated a tsunami reported to have reached a height of 38.2 m. 11,000 homes destroyed and 22,000 people killed in Japan; 4,000 also killed in China.
Northern Chile,
13 August 1868
Earthquakes estimated at magnitude 8.5, off the coast of Africa, Peru (now Chile). Tsunamis affected entire Pacific Rim; waves reported up to 21 m high over two and three days. Estimated 25,000 deaths and an $300 million in damages caused by the tsunamis and earthquakes along Peru-Chile coasts.
Ryuku Islands, Japan,
24 April 1771
A magnitude 7.4 earthquake produced a tsunami that damaged coastal communities on Ishigaki and Miyako Islands and others in the region. Tsunamis were 11 to 15 m high. Tsunami destroyed 3,137 homes and about12,000 people were killed.
Ise Bay, Japan,
18 January 1586
An earthquake that caused a tsunami estimated to be about magnitude 8.2. The tsunamis rose to a height of 6 m. Earthquake and following fired destroyed most of a city. 8000 people were killed.

Simple tsunami origin animation (NOAA) - How tsunamis form from an earthquake.
Three Chile Tsunamis animation (PTWC) - Breakout animations of tsunamis of different intensities.
Drawback before arrival of 2004 tsunamis in Sri Lanka
Fig. 10-34. Drawback from tsunami in Sri Lanka exposed about 150 meters before the tsunamis arrived from 2004 earthquake.
tsunami 2010 Japan
Fig. 10-35. Tsunamis arriving on the coast of Japan, 2011
2004 Tsunami coming onshore in Thailand

Fig. 10-36. 2004 Tsunami coming onshore in Thailand

Whirlpool caused by tsunami in Japan, 2011
Fig. 10-37. Giant whirlpool caused by the Japan, 2011 tsunamis (note the boat for scale).
Tsunami sources Tsunami travel time from 1960 earthquake in Chili Tsunami travel time from 2011 earthquake in Japan Tsunami amplitude map of Japan earthquake, 2011
Fig. 10-38. Map showing locations of tsunami-generating earthquakes Fig. 10-39. Map of tsunami travel times generated by magnitude 9.5 earthquake Chili, 22 May, 1960. Fig. 10-40. Map of tsunami travel time from magnitude 9.0 earthquake in northern Japan, 11 March 2011 Fig. 10-41. Maximum wave amplitude of tsunami from northern Japan, 11 March 2011

Tsunami Damage from the 2004 Sumatra tsunami
Banda Aceh before 2004 tsunami Banda Aceh after 2004 earthquake Only a brick mosque survived tsunami damage in Banda Aceh, 2004 tsunami Tsunami 2004 runup
Fig. 10-42. Banda Aceh, Indonesia before 2004 tsunami

Fig. 10-43. Banda Aceh, Indonesia after 2004 tsunami

Fig. 10-44. Mosque survived 2004 tsunami in Banda Aceh, Sumatra

Fig. 10-45. Vegetation stripped from hillsides by run up: Banda Aceh, Sumatra tsunami 2004

Examples of Tsunami Damage
Tsunami damage on Sri Lanka, 2004 Damage from a 1993 tsunami in Japan Tsunami damage from the Alaska 1964 tsunami Tsunami damage from the 2011 earthquake in Japan
Fig. 10-46. The Sumatra 2004 earthquake caused damage in Sri Lanka 2,000 miles away. Fig. 10-47. Damage from the Tsunami of July 12, 1993, a magnitude 7.6 in the Sea of Japan near Hokkaido. The tsunami was 32 meters high on Okishuri, Island. Fig. 10-48. Tsunami damage in Kodiak, Alaska from the March 27,1964 earthquake (magnitude 9.2) Fig. 10-49. March 11, 2011 Tohoku Japan earthquake and tsunami

Tsunami Warning System
Tsunami Dart Alert System tsunami buoy Pacific Tsunami Warning_system Everything you ever wanted to know about tsunamis, and more:

Pacific Tsunami Warning Center website.

Learn about: Tsunami Paleogeohistory of San Diego County
Fig. 10-50 & 51. DART Buoy and DART tsunami warning system (left). Fig. 10-52. Location of tsunami warning system buoys around Pacific and Atlantic basins.

Tsunami videos

Indonesia Tsunami 2004 (NOAA): Tsunami waves "move out" animation of Indian Ocean
Thailand 2004: YouTube video

Japan Tsunami 2011
(NOAA): Tsunami waves "move out" animation of Pacific Basin
Japan 2011 Tsunami (overtops wall): YouTube video
Japanese 2011 Tsunami caught on CCTV: YouTube video
Helicopter view of Japan 2011 tsunamis: YouTube video

Tsunami surfing
Fig. 10-53. Surfing a tsunami wave? (Not recommended!)
Chapter 10 quiz questions 1/1/2016