|Origin of the sand
Sand is one of the components that make up soil (For a lengthy explanation, see the chapter on soil). The diagram shows how soil is made and sand. Every kind of rock weathers slowly by breaking apart into different substances. Whereas mechanical forces such as wind, rain, hail and ice may break the rock into smaller parts with identical chemical properties as the parent material, spontaneous and chemical weathering change its nature. It produces minerals and nutrients, oxides of iron and alumina, and silica, which combine into clay. The two other components are silt and sand (quartz). The combination of clay + silt + sand is called a loam.
When soil erodes, all of its components wash down into the sea. Here
the water movement sieves the loam into its components, each sedimenting
in different areas of the continental shelf and slope. Sand being the largest,
is transported by waves towards the coast where it may end up on a beach.
Silt and clay may remain in the coastal zone for a while but eventually
settle out in the calm waters of the deep ocean.
|At the end of the last ice age, the ocean's level was about 120m lower than today, due to the amount of water locked up in the polar and mountain ice caps. The beaches then were close to the edge of the continental shelf, and the flat land between there and where they are today, was covered in forest. Then the climate warmed, the sea level rose, and the beaches moved landwards, and with them, the sand that formed them. This sand is rather young, and its quantity has not changed very much since the end of the ice age. It took about 4000 years for the ocean to rise, and that process was completed some 6000 years ago.|
The diagram shows the extent of the beach sand into the sea. The top drawing shows a typical beach profile, first descending rapidly near the coast, then following the slope of the continental shelf to depths over 40m. The sand depth, shown in the bottom drawing, is about 2m near the shore, decreasing to about 20cm at 40m depth. This point may be 10km out in sea, depending on the width and slope of the continental shelf. Occasionally storms are large enough to stir the bottom this deep, and to sweep its sand towards the shore. It is here that the beach effectively ends.
|The beach and dunes
The beach shown in the diagram is typically found together with sand dunes. Not all beaches are like this (See types of beaches on this page). In the picture, the levels of high and low tide are shown and the wet beach is the area between them. The near shore zone extends to a depth of about 5m. In this zone much sand is moved because it is stirred easily by most waves. But the shore extends further down, to depths of 20m or more. At some time during a year or decade, the sand here is stirred by large storms and moved towards the beach.
Going from the wet beach inland, one encounters the dry beach, outside reach of the waves, but high waves during spring tide may deposit sand here. This part of the beach is partly formed by wave overwash and by the wind heaping the sand up. It can even be considered a fore-fore dune. Further back from here extends the back shore with its fore, mid and rear dunes.
|This diagram shows how the sand moves in the water, on the beach and behind the beach. Large waves occasionally move sand towards the beach and when they do, they move large quantities. Closer to the beach the sand movement is an every day affair and in the breaker zone huge quantities are moved almost every hour. As waves move sand towards the beach, gravity and back-wash move it back again at the same rate. Most of the movements cancel each other out and by and large, the sand remains in place.|
|The big difference comes once the sand remains on the beach, dries out during the low tide and is removed by the sea wind. This sand can no longer be reached by normal waves. As the wind brushes over the dried beach, it pushes sand up-hill in a jumping motion (saltation). The sand grains of which dunes are made, are too large to blow like dust clouds in the wind but they can saltate rapidly like a moving sheet over the ground. Once particles fall into the lee (wind shade) of the foredune, they stay there, making it appear as if the dune rolls backward to the next dune and so on. In this manner sand is pumped out of the sea. It is the mechanism by which a beach can repair (rebuild) storm damage. The wind transportation is much slower than that of water and it may take weeks to repair the damage a storm can do in one hour.|
The picture shows how a beach reshapes itself during a storm and how, afterwards, it rebuilds itself again. In the top picture the dotted line shows the beach profile before the storm and the solid profile during the storm. The two horizontal lines in the water correspond to high and low tide, the normal extent of the wet beach. Storms not only arrive with higher waves, but also with a storm surge that lifts the water level. During high tide the waves attack the beach above its normal level. The foredune is carved out and its sand creates a new beach at the level of attack. Sometimes lower down a bank is formed, which helps to break the waves. The storm brings new sand but borrows sand from the dunes.
After the storm (bottom picture), the forces of waves and wind gradually restore the damage wrought. Waves spread the increased amount of sand and sea winds gradually store it back onto the dunes where it came from.
A beach's ability to rebuild itself, makes it a formidable bastion against the sea. Whereas headlands and cliffs erode, beaches can hold their own against the anger of the sea.
The components of self repair are: 1) Beach sand being able to dry because of a receding tide and sunshine and wind; 2) Sea wind to blow the sand inland; 3) A sand storage in the dunes.
Thus a beach can store sand and grow during years of good sea winds, few rains or storms and much sunshine. As the sand pump pumps sand from the wet beach, it causes the beach to lie steeper. During years with opposite conditions, the beach can erode and lie flatter.
that beach erosion occurs mainly during large storms. These storms also
bring new sand from deeper down towards the beach. Note also that healthy
beaches, having sand pumps with over capacity, may still be capable
of repairing themselves during bad years. But once this self repair mechanism
becomes impaired, beaches become more sensitive to weather conditions and
climate cycles. The diagram shows actual beach erosion of Westhampton Beach
(USA), over a period of 40 years. The situation is typical for many beaches,
all over the world.
A twenty year cycle appears to overlay the general trend of 50 ft (15m) in 40 years.
Note that the rapid oscillations are depicted as growth during one year, followed by shrinking during the next year. What the author intended to show was growth during summer and shrinkage during winter, an oscillation twice as fast.
This rather complicated looking sand balance or sand budget diagram attempts to depict how sand moves in a dune/beach system. It is a model to sharpen our understanding. Scientists use such models to study the transport of sediment near beaches. From left to right, traversing the four boxes (compartments), runs the profile of a beach. The size of the boxes could be a part of the beach or the entire beach, and it is called a 'beach cell'. Sand can move out or into the beach cell by coastal drift parallel to the coast (sea currents). Sand moves towards the beach by wave action and away from the beach by gravity down its gradual slope.
The yellow part depicts the dry sand: the dry beach and the dunes. In
the lower left corner the origin of the sand is shown. Sand arises from
coastal erosion and is transported by rivers towards the sea.
The blue part comprises the wet sand: the wet beach, the nearshore with possible sand bank and the offshore deep sand compartments.
As rivers deposit sand nearshore and offshore, it enters the corresponding compartments. The land area that drains directly into the beach cell (catchment area) erodes at a rate depending on land use and rock type.
Following the boxes from right to left, the sand in the deep sand compartment
is stirred only by large waves that may pull sand towards the beach or
allow it to drift deeper down by the force of gravity.
Sand moving out of the deep sand compartment towards the beach, enters the sand bar or nearshore compartment which is subject to much more wave action and corresponding sand movement. From there, the sand is moved to the intertidal zone, the actual beach. Sea winds move it further onto the dunes but large waves can do so too by washing over the dry beach and dunes. Sand can also be lost this way, ending up further inland or back into rivers or estuaries. The breaker zone is the area with the highest transport of sand. Waves keep large volumes of sand in suspension, allowing it to be moved by ocean currents, tidal currents or wind induced currents. Some beaches are claimed to move half a million cubic metres of sand one way only, each year, the equivalent of 70,000 large truck loads or 200 trucks every day of the year!
As can be seen from the above, sediment transport along the coast is
a complicated process, which is difficult or even impossible, to measure.
The diagram shown here is of utmost importance in understanding how material is transported by water (and wind). Theoretical work was done by the British mathematician Sir George Gabriel Stokes (1819-1903), who formulated that drag experienced by a perfectly round sphere falling through a medium (straight line above) is proportional to diameter and speed. For the sake of simplicity, he assumed that the flow of the medium was laminar, thus without eddies that would increase friction. In practice, this is not so, hence the left and right-hand curves, which have been established experimentally. The diagram spans enormous scales: vertically soil particles from 1 micron to 10mm and horizontally water velocities from 0.1mm/s to 10m/s (36km/h). The right-hand curve shows what water speeds are necessary to erode a cohesive bed, whereas the left-hand curve shows at which speeds the moving particles start settling out again.
The graph shows that pebbles (grey size zone) are dislodged at about 100cm/s (1m/s), but settle down at about 20 cm/s. Sand (yellow zone) moves more easily, but silt and clay (brown zones) are hard to dislodged, once clumped together, whereas they need almost stagnant water to settle out again.
It shows how a beach is formed by a wave's forward wash, as long as the particles can resist its back wash. It also shows that mud flats cannot form where wind blows, and it illustrates that mud cakes, deposited by cyclonic rain storms, may take a decade of lesser storms to be worn away.
Reader, please note that a similar diagram is required to explain erosion and deposition by wind, but this important work has not been done. Since particles that are moved by air follow the same logic, and air being 800 times lighter than water, the wind transportation and sedimentation diagram can be approximated by shifting the horizontal scale by an unknown quantity to the right (for instance, 100cm/s may read 100km/h). Winds strong enough to shift pebbles are uncommon, whereas silt and mud stay air-borne. As a result, a narrow range of particles forms dunes (sand of 0.2-1.0 mm).
is sand deposited on a beach?
Why does sand stay put as the water draws back from a beach? Scientists say that the water that pushes sand up the beach, partly flows back through the sand bed. Thus the amount of water flowing back over the sand bed is less than which arrived there, and the sand stays. This is a myth because the amount of water draining back through the beach sand is negligible compared to what flows back over the sand, and there is a much better explanation.
Sand is transported over the sea bed towards the beach when waves 'stumble' such that their crests become narrower than their troughs. This produces a swift forward flow followed by a slower backward flow.
On the beach the top of the wave breaks and mingles with the foot of the wave, both dashing forward with a force driven by the energy from the height and speed of the collapsing wave. The resulting rush of water is fast and strong and moves sand effortlessly up the beach. The water then comes to a rest as the sand particles settle out. The water then begins flowing back down the beach, first slowly and then faster until it dislodges cohesive sand grains. But the forcing power is much less than that of the on-rushing waves. The particles that settled at the top of the forward rush, stay because of the hysteresis (lagging behind) between erosion speed and settling speed in the diagram above. Thus sand settles on the beach only when the tide recedes.
does sand move to deeper depths?
The common idea is that sand simply flows downhill, but this idea cannot work because the bottom gradient is so small (the sand bottom is nearly horizontal). We know that 'stumbling' waves move the sand towards the beach, so how can it flow away from the beach?
It happens by those waves that do not 'stumble' but do stir the bottom, such that the forward motion of the water over the sea bottom is about the same as the backward motion. Sand is then moved both towards and from the beach, but as it accidentally reaches deeper water, the water movement becomes less, allowing it to settle out. Sand that accidentally moved to shallower water, keeps moving until it is accidentally moved to deeper water. Eventually the bottom becomes so deep that even the deepest waves can no longer transport the sand towards the beach. From this boundary, the sand keeps moving towards the deep, and this is where the beach ends. See the chapter on mining the sea sand for more information.
Very light particles such as mud (silt + clay) move in this manner all the way to the edge of the continental shelf and clay moves even further down the continental slope.
It should be noticed that currents, such as tidal currents, play an important role at these depths in combination with deep (long) waves.
mystery of the pebble beaches
Many 'beaches' do not consist of sand but of pebbles or boulders, sometimes with sandy beaches in between. Why is this so, whereas there occurs so much sand in the sea, starting right at the foot of the pebble beach? The photo shows such a beach, having formed a tall and wide dyke. The answer must be found in the sedimentation/ transportation diagram above. First of all, the coarse material must be available, such as originating from a fast flowing river nearby. Since pebbles do not move as easily as sand, pebble beaches occur only close to the origin of their material (a river). Only fast water movements in excess of 1m/s are capable of moving pebbles, so pebble beaches form only along very exposed shores. The reason that they are not topped over by sand, is that pebbles are capable of staying put much better than sand, resisting the wave's back-wash much better. As a result, they form steep beaches with strong back wash, too strong for sand to settle out. So the sand remains at the foot of the pebble beach. However, in less exposed places, the process reverses, allowing sand to lay over a deeper bed of pebbles. As a result one may find sand and pebble beaches seemingly 'alternating'. Note that pebbles laying on top of the sand, prevent the formation of dunes. Note that all pebbles on the photo have the same flat shape which allows them to be transported easily in water, while also staying put outside the water.
Where a variety of coarse material exists, ranging from pebbles to large boulders, one finds the boulders cast high up the beach or along the sides of pocket beaches, out of reach of average storms. Underneath or more towards the middle of the beach, one finds successively smaller stones. With it the slope of the beach also becomes more gradual.
|Rips and cusps
Some beaches are notorious for their rips. Rips are unpredictable currents, flowing away from the beach. They pull swimmers into deeper water and are very focused and strong. Rips arise when breaker upon breaker pushes new water onto the beach, not allowing much time for it to flow back. Normally a wave that runs up a beach will flow back underneath the next one, causing an undertow current, familiar to swimmers. Where waves arrive in rapid succession, a rip may occur, allowing the piled-up water to flow back to the sea.
Because rips are narrowly focused currents, swimmers should swim out
of them in a direction parallel to the beach. Where rips occur, the water
level is lowest and so are the waves. Where water flows towards the beach,
both the water level and the waves are highest. A swimmer should swim to
such a place. Some beaches have irregularities such as under water reefs
where rips always form. Don't swim near reefs and groynes.
diagram provides an aerial view of rips and cusps. The left side shows
waves heading straight for the shore. If the shore is exactly the same
everywhere, a rip may form anywhere. It causes a current jet back to sea
and two corresponding deep eddies.
When the wind blows at an angle to the beach, a regular pattern of cusps (latin word for spear points) appears in the beach, particularly at high tide. The beach is lowest at a cusp and highest in between. Each cell produces a circulating current pattern. Along the beach, the cusps are synchronised by an edge wave running along the beach in the breaker zone. This wave dips at each cusp and rises in between.
Photo Van Dorn, 1974.
Photo Van Dorn, 1974.
|Types of beach
Beaches differ in shape, according to the forces that created them: waves, tides and wind. They also differ according to the material available: mud, sand, iron sand, shells, cobbles, boulders, etc. Using photographs of beaches in New Zealand, it can be shown that each beach has its own characteristics that make it unique. For more pictures of New Zealand beaches, see Our disappearing beaches. The detailed sand photographs of the sand are 21 by 14 mm.
|The sheltered crater lake Rotokawau near Rotorua, has no beaches because there is not enough wind to make waves large enough.||