Natural Disasters

Prof. Stephen A. Nelson

Coastal Zones

Oceans and Coastal Zones

The oceans play a major role in weather and climate because over 70% of the Earth's surface is covered by oceans.  The atmosphere picks up most of its moisture and heat from the oceans and thus weather patterns and climate are controlled by the oceans.

The oceans vary considerably in their depth.  The deepest part of the ocean is called the abyssal plain.  As the seafloor starts to rise toward continental margins it is called the continental rise. The continental slope is the steep slope rising toward continual margins.  The gently sloping area along the margin of a continent is called the continental shelf.  In addition, deep trenches that occur along zones where oceanic lithosphere descends back into the mantle are called oceanic trenches. And,   ridges in the deep oceans that rise above the abyssal plains and where new oceanic lithosphere is created are called oceanic ridges.  These features all effect the circulation of the oceans and the ecosystems that inhabit the oceans.

Coastal Zones

A coastal zone is the interface between the land and water. These zones are important because a majority of the world's population inhabit such zones. Coastal zones are continually changing because of the dynamic interaction between the oceans and the land. Waves and winds along the coast are both eroding rock and depositing sediment on a continuous basis, and rates of erosion and deposition vary considerably from day to day along such zones. The energy reaching the coast can become high during storms, and such high energies make coastal zones areas of high vulnerability to natural hazards.  Thus, an understanding of the interactions of the oceans and the land is essential in understanding the hazards associated with coastal zones.  Tides, currents, and waves bring the energy to the coast, and thus we start with these three factors.

Tides are due to the gravitational attraction of Moon and to a lesser extent, the Sun on the Earth. Because the Moon is closer to the Earth than the Sun, it has a larger effect and causes the Earth to bulge toward the moon.

• The tidal bulges result in a rhythmic rise and fall of ocean surface, which is not noticeable to someone on a boat at sea, but is magnified along the coasts. Usually there are two high tides and two low tides each day, and thus a variation in sea level as the tidal bulge passes through each point on the Earth's surface.
  
  
• Along most coasts the range is about 2 m, but in narrow inlets tidal currents can be strong and fast and cause variations in sea level up to 16 m.
  

• Because the Sun also exerts a gravitational attraction on the Earth, there are also monthly tidal cycles that are controlled by the relative position of the Sun and Moon. The highest high tides occur when the Sun and the Moon are on the same side of the Earth (new Moon) or on opposite sides of the Earth (full Moon). The lowest high tides occur when the Sun and the Moon are not opposed relative to the Earth (quarter Moons).
  

These highest high tides become important to coastal areas during hurricane season and you always hear dire predications of what might happen if the storm surge created by the tropical cyclone arrives at the same time as the highest high tides.

The surface of the oceans move in response to winds blowing over the surface. The winds, in effect, drag the surface of oceans creating a current of water that is usually no more than about 50 meters deep.  Thus, surface ocean currents tend to flow in patterns similar to the winds as discussed above, and are reinforced by the Coriolis Effect.  But, unlike winds, the ocean currents are diverted when they encounter a continental land mass. 

Waves are generated by winds that blow over the surface of oceans. In a wave, water travels in loops. But since the surface is the area affected, the diameter of the loops decreases with depth. The diameters of loops at the surface is equal to wave height (h).

Wavelength (L) = distance to complete one cycle

Wave Period (P) = time required to complete on cycle.

Wave Velocity (V) = wavelength/wave period (L/P).

• Wave Base - Motion of waves is only effective at moving water to depth equal to one half of the Wavelength (L/2). Water deeper than L/2 does not move. Thus, waves cannot erode the bottom or move sediment in water deeper than L/2. This depth is called wave base. In the Pacific Ocean, wavelengths up to 600 m have been observed, thus water deeper than 300m will not feel passage of wave. But outer parts of continental shelves average 200 m depth, so considerable erosion can take place out to the edge of the continental shelf with such long wavelength waves.
  
  When waves approach shore, the water depth decreases and the wave will start feeling bottom. Because of friction, the wave velocity (= L/P) decreases, but its period (P) remains the same Thus, the wavelength (L) will decrease. Furthermore, as the wave "feels the bottom", the circular loops of water motion change to elliptical shapes, as loops are deformed by the bottom. As the wavelength (L) shortens, the wave height (h) increases. Eventually the steep front portion of wave cannot support the water as the rear part moves over, and the wave breaks. This results in turbulent water of the surf, where incoming waves meet back flowing water.

Rip currents form where water is channeled back into ocean.

• Wave Erosion - Rigorous erosion of sea floor takes place in the surf zone, i.e. between shoreline and breakers. Waves break at depths between 1 and 1.5 times wave height. Thus for 6 m tall waves, rigorous erosion of sea floor can take place in up to 9 m of water.
  
  Waves can also erode by abrasion and flinging rock particles against one another or against rocks along the coastline.
  
  

• Wave refraction - Waves generally do not approach shoreline parallel to shore. Instead some parts of waves feel the bottom before other parts, resulting in wave refraction or bending.

Wave energy can thus be concentrated on headlands, to form cliffs. Headlands erode faster than bays because the wave energy gets concentrated at headlands.

Coastal Erosion and Sediment Transport

Coastlines are zones along which water is continually making changes. Waves can both erode rock and deposit sediment. Because of the continuous nature of ocean currents and waves, energy is constantly being expended along coastlines and they are thus dynamically changing systems, even over short (human) time scales.

Erosion by Waves

As we discussed previously, the motion of waves is only felt to a depth of 1/2 times the wavelength.  Thus, waves can only erode if the water along a coastline is shallower than 1/2 times the wavelength.  But, when the wave breaks as it approaches the shoreline, vigorous erosion is possible due to the sudden release of energy as the wave flings itself onto the shore.  In the breaker zone rock particles carried in suspension by the waves are hurled at other rock particles. As these particles collide, they are abraded and reduced in size.  Smaller particles are carried more easily by the waves, and thus the depth to the bottom is increased as these smaller particles are carried away by the retreating surf.  Furthermore, waves can undercut rocky coastlines resulting in mass wasting processes wherein material slides, falls, slumps, or flows into the water to be carried away by further wave action.

Transport of Sediment by Waves and Currents

Sediment that is created by the abrasive action of the waves or sediment brought to the shoreline by streams is then picked up by the waves and transported.  The finer grained sediment is carried offshore to be deposited on the continental shelf or in offshore bars, the coarser grained sediment can be transported by longshore currents and beach drift.

• Longshore currents - Most waves arrive at the shoreline at an angle, even after refraction. Such waves have a velocity oriented in the direction perpendicular to the wave crests, but this velocity can be resolved into a component perpendicular to the shore (Vp) and a component parallel to the shore (V_L). The component parallel to the shore can move sediment and is called the longshore current.

• Beach drift - is due to waves approaching at angles to beach, but retreating perpendicular to the shore line. This results in the swash of the incoming wave moving the sand up the beach in a direction perpendicular to the incoming wave crests and the backwash moving the sand down the beach perpendicular to the shoreline. Thus, with successive waves, the sand will move along a zigzag path along the beach.

High winds blowing over the surface of the water during storms bring more energy to the coastline and can cause more rapid rates of erosion.  Erosion rates are higher because:

• During storms wave velocities are higher and thus larger particles can be carried in suspension.  This causes sand on beaches to be picked up and moved offshore, leaving behind coarser grained particles like pebbles and cobbles, and reducing the width of the beach.
  
  
• During storms waves reach higher levels onto the shoreline and can thus remove structures and sediment from areas not normally reached by the incoming waves.
  

• Because wave heights increase during a storm, waves crash higher onto cliff faces and rocky coasts.  Larger particles are flung against the rock causing rapid rates of erosion.
  
  
• As the waves crash into rocks, air occupying fractures in the rock becomes compressed and thus the air pressure in the fractures is increased.  Such pressure increases can cause further fracture of the rock.
  

• Rocky Coasts - In general, coastlines that have experienced recent tectonic uplift as a result of either active tectonic processes (such as the west coast of the United States) or isostatic adjustment after melting of glacial ice (such as the northern part of the east coast of the United States) form rocky coasts with cliffs along the shoreline.  Anywhere wave action has not had time to lower the coastline to sea level, a rocky coast may occur. Because of the resistance to erosion, a wave cut bench and wave cut cliff develops. The cliff may retreat by undercutting and resulting mass-wasting processes.

If subsequent uplift of the wave-cut bench occurs, it may be preserved above sea level as a marine terrace.

Because cliffed shorelines are continually attacked by the erosive and undercutting action of waves, they are susceptible to frequent mass-wasting processes which make the tops of these cliffs unstable areas for construction as you noted in your homework on mass-wasting processes.

Along coasts where streams entering the ocean have cut through the rocky cliffs, wave action is concentrated on the rocky headlands as a result of wave refraction, as discussed previously.

• Beaches - A beach is the wave washed sediment along a coast. Beaches occur where sand is deposited along the shoreline. A beach can be divided into a foreshore zone, which is equivalent to the swash zone, and backshore zone, which is commonly separated from the foreshore by a distinct ridge, called a berm. Behind the backshore may be a zone of cliffs, marshes, or sand dunes.

• Barrier Islands - A barrier island is a long narrow ridge of sand just offshore running parallel to the coast. Separating the island and coast is a narrow channel of water called a lagoon. Most barrier islands were built during after the last glaciation as a result of sea level rise. Barrier islands are constantly changing. They grow parallel to the coast by beach drift and longshore drift, and they are eroded by storm surges that often cut them into smaller islands.  Barrier islands are common along the east and Gulf coasts of the United States.
  

• Coral Reefs  - Reefs consist of colonies of organisms, like corals, which secrete calcium carbonate. Since these organisms can only live in warm waters and need sunlight to survive, reefs only form in shallow tropical seas. Fringing reefs form along coastlines close to the sea shore, whereas barrier reefs form offshore, separated from the land by a lagoon.  Both types of reefs form shallow water and thus protect the coastline from waves. However, reefs are high susceptible to human activity and the high energy waves of storms.
  

The shape of coast is controlled mainly by tectonic forces and meteorological conditions. Examples:

• The west coast of the U.S. is a rugged coast with many sea cliffs and raised wave cut benches (marine terraces). This is what is called an emergent coastline and in this case is due to a recent episode of uplift of the land relative to the sea by tectonic forces. The coast of New England is also an emergent case, but in this case, the rise of the land surface has been due to removal of glacial ice which had depressed the land during the last glaciation which ended about 10,000 years ago.
  

• The rest of the east coast, on the other hand, is a submerged coast, and shows submerged valleys, barrier islands, and gentle shorelines, all due to rise of sea level since last glaciation age (during glacial ages, seawater is tied up in ice, and sea level is lower; when the ice melts sea level rises).

• Storms - great storms such as hurricanes or other winter storms can cause erosion of the coastline at much higher rate than normal. During such storms beaches can erode rapidly and heavy wave action can cause rapid undercutting and mass-wasting events of cliffs along the coast, as noted above.  Note that the El Niņo driven storms on the west coast caused extensive coastal erosion in 1998.
  
  
• Tsunamis - a tsunami is a giant sea wave generated by earthquakes, volcanic eruptions, or landslides, as we have discussed before. Such waves can have wave heights up to 30 m, and have great potential to wipe out coastal cities.
  

• Landslides - On coasts with cliffs, the main erosive force of the waves is concentrated at the base of the cliffs. As the waves undercut the cliffs, they may become unstable and mass-wasting processes like landslides will result. Massive landslides can also generate tsunamis.

Adapting to Coastal Erosion

Seacliffs, since they are susceptible to landslides due to undercutting, and barrier islands and beaches, since they are made of unconsolidated sand and gravel, are difficult to protect from the action of the waves. Human construction can attempt to prevent erosion, but cannot always protect against abnormal conditions.  Furthermore, other problems are sometimes caused by these engineering feats.

Protection of the Shoreline. Shoreline protection can be divided into two categories: hard stabilization in which structures are built to reduce the action of the waves and soft stabilization which mainly refers to adding sediment back to a beach as it erodes away.

• Hard Stabilization - Two types of hard stabilization are often used.  
  

  • One type interrupts the force of the waves. Seawalls are built parallel to the coastline to protect structures on the beach. A seawall is usually built of concrete or piles of large rocks.  Waves crash against the seawall and are prevented from running up the beach.  Breakwaters serve a similar purpose, but are built slightly offshore, again preventing the force of the waves from reaching the beach and any structures built on the beach.
    

  • The other type interrupts the flow of sediment along the beach.  These structures include groins and jetties, built at right angles to the beach to trap sand and widen the beach.
    

While hard stabilization does usually work for its intended purpose, it does cause sediment to be redistributed along the shoreline.  Breakwaters, for example cause wave refraction, and alters the flow of the longshore current.  Sediment is trapped by the breakwater, and the waves become focused on another part of the beach, not protected by the breakwater, where they can cause significant erosion. Similarly, because groins and jetties trap sediment, areas in the downdrift direction are not resupplied with sediment, and beaches become narrower in the downdrift direction.

• Soft stabilization is primarily accomplished by adding sediment to the coastline, usually by dredging sediment from offshore and pumping it onto the coastline. Adding sediment is necessary when erosion removes too much sediment. But, because the erosive forces are still operating, such addition of sediment will need to be periodically repeated. 

As noted above, hard stabilization usually affects areas in the downdrift direction of the longshore current.  The net result being that some areas of a coastline are protected while other areas are destroyed.  Nearly all human intervention with coastal processes interrupts natural processes and thus can have an adverse effect on coastlines. Three examples of human interference are discussed below.

• Barrier Islands along the North Carolina Coast show a noticeable difference among the islands that have been built upon and those that have not. The undeveloped islands have beaches 100 to 200 meters wide, while the developed islands have beaches with widths less than 30 m.
  

• In order to protect southern California cities from flooding caused by heavy rains, most of the streams draining into the ocean have been dammed. The dams trap sediment that would normally be carried to the ocean by stream flow. Since this sediment is not being supplied to the ocean, longshore currents cannot resupply the beaches with sediment, but do carry the existing sediment in the downdrift direction, resulting in significant erosion of the beaches.
  
  
• Most of the state of Louisiana has resulted from the deposition of sediments by the Mississippi River during floods over the last 10,000 years. Humans, however, have prevented the River from flooding by building a levee systems that extends to the mouth of the River.  As previously deposited sediments become compacted they tend to subside. But, since no new sediment is being supplied by Mississippi River flooding, the subsidence results in a relative rise in sea level.   This, coupled with a current rise in eustatic sea level, is causing coastal Louisiana to erode at an incredible rate, estimated at 25 square miles a year.  An excellent series of articles concerning the coastal erosion problem in Louisiana was published this semester by the Times-Picayune newspaper.  See the article and the accompanying flash animation at:
  
  http://www.nola.com/speced/lastchance/

From: http://marine.usgs.gov/fact-sheets/Barrier/barrier.html