A point bar is a depositional feature made of alluvium
that accumulates on the inside bend of streams
s below the slip-off slope
. Point bars are found in abundance in mature or meander
ing streams. They are crescent-shaped and located on the inside of a stream bend, being very similar to, though often smaller than, towheads
, or river islands.
Point bars are composed of sediment that is well sorted
and typically reflects the overall capacity of the stream. They also have a very gentle ''slope'' and an elevation
very close to water level. Since they are low-lying, they are often overtaken by floods
and can accumulate driftwood and other debris during times of high water levels. Due to their near flat topography
and the fact that the water speed is slow in the shallows of the point bar they are popular rest stops for boaters and rafters. However, camping on a point bar can be dangerous as a flash flood
that raises the stream level by as little as a few inches (centimetres) can overwhelm a campsite in moments.
A point bar is an area of deposition
whereas a cut bank
is an area of erosion
Point bars are formed as the secondary flow
of the stream sweeps and rolls sand, gravel and small stones laterally across the floor of the stream and up the shallow sloping floor of the point bar.
Any fluid, including water in a stream, can only flow around a bend in vortex
flow. In vortex flow the speed of the fluid is fastest where the radius of the flow is smallest, and slowest where the radius is greatest. (Tropical cyclones
es, and the spinning motion of water as it escapes down a drain are all visible examples of vortex flow.) In the case of water flowing around a bend in a stream the secondary flow
in the boundary layer
along the floor of the stream does not flow parallel to the banks of the stream but flows partly across the floor of the stream toward the inside of the stream (where the radius of curvature is smallest). This movement of the boundary layer is capable of sweeping and rolling loose particles including sand, gravel, small stones and other submerged objects along the floor of the stream toward the point bar.
This can be demonstrated at home. Partly fill a circular bowl or cup with water and sprinkle a little sand, rice or sugar into the water. Set the water in circular motion with a hand or spoon. The secondary flow
will quickly sweep the solid particles into a neat pile in the center of the bowl or cup. The primary flow (the vortex) might be expected to sweep the solid particles to the perimeter of the bowl or cup, but instead the secondary flow
along the floor of the bowl or cup sweeps the particles toward the center.
Where a stream is following a straight course the slower boundary layer along the floor of the stream is also following the same straight course. It sweeps and rolls sand, gravel and polished stones downstream, along the floor of the stream. However, as the stream enters a bend and vortex flow commences as the primary flow, a secondary flow also commences and flows partly across the floor of the stream toward the convex bank (the bank with the smaller radius). Sand, gravel and polished stones that have travelled with the stream for a great distance where the stream was following a straight course may finally come to rest in the point bar of the first stream bend.
Due to the circular path of a stream around a bend the surface of the water is slightly higher near the concave bank (the bank with the larger radius) than near the convex bank. This slight slope on the water surface of the stream causes a slightly greater water pressure on the floor of the stream near the concave bank than near the convex bank. This pressure gradient drives the slower boundary layer across the floor of the stream toward the convex bank. The pressure gradient is capable of driving the boundary layer up the shallow sloping floor of the point bar, causing sand, gravel and polished stones to be swept and rolled up-hill.
The concave bank is often a cut bank
and an area of erosion
. The eroded material is swept and rolled across the floor of the stream by the secondary flow
and may be deposited on the point bar only a small distance downstream from its original location in the concave bank.
The point bar typically has a gently sloping floor with shallow water. The shallow water is mostly the accumulated boundary layer and does not have a fast speed. However, in the deepest parts of the stream where the stream is flowing freely, vortex flow prevails and the stream is flowing fastest where the radius of the bend is smallest, and slowest where the radius is greatest. The shallows around the point bar can become treacherous when the stream is rising. As the water depth increases over the shallows of the point bar, the vortex flow can extend closer toward the convex bank and the water speed at any point can increase dramatically in response to only a small increase in water depth.
Fallacy regarding formation of point bars
An old fallacy exists regarding the formation of point bars and oxbow lake
s which suggests they are formed by the deposition
(dropping) of a watercourse's suspended load
claiming the velocity and energy of the stream ''decreases'' toward the inside of a bend. This fallacy relies on the erroneous notion that the momentum of the water is "always" slowest on the inside of the bend (where the radius is smallest) and fastest on the outside of the bend (where the radius is greatest), which ignores its increased angular momentum
Mass deposition of suspended solids rarely occurs on one bank save in tidal estuaries
; instead, vortex
flow being faster on the inner bank compensates for the greater height and therefore mass of water flowing downstream along the concave bank, and the rough, shallow bed usually provides per liter of water above more agitation to maintain any suspended particles
. Any relatively steady gradient open flow not met with complex interactions with contrary flows, such as tides, or major obstacles, flows around a bend in a simple model of vortex flow, with relatively few variables and coefficient
Point bars typically have a gently sloping floor with shallow water. Clearly a higher proportion of the water in very shallow water does much more work to overcome friction above and below (especially in a countervailing breeze) which lowers its speed, see Bernoulli's principle
. It is probably this close-quarters observation which led early geographers to believe in deposition by sedimentation of suspended matter rather than close-to-bed secondary currents.
In a steady-gradient section of a watercourse, sedimentation may occur where the water is saturated and the shallow bank has high flow resistance but does not agitate the suspension. Similarly, the fallacy has scant explanation as to why deposition occurs at a stream bend, and little or none occurs where the stream is following a straight course, with exception of a steep slope (river gradient) where the river has formed a natural cut
or waterfall and may then deposit some of its load at the point of meeting a less steep section e.g. great meander.
In the settled low-gradient parts of a meandering watercourse the water speed is slow, turbulence is low, and the water is not capable of holding coarse sand and gravel in suspension. In contrast, point bars comprise coarse sand, gravel, polished stones and other submerged objects. These materials have not been carried in suspension and then dropped on the point bar – they have been swept and rolled into place by the secondary flow that exists across the floor/bed in the vicinity of a stream bend, which will be intensified if there is reflection
particularly from an irregular, scoured opposing bank.
*Tarbuck, E. J. and F. K. Lutgens. ''Earth'', 7th Edition. Prentice Hall: Upper Saddle River, New Jersey, 2002. pp. 277, 279.