A sediment cell is a largely self-contained stretch of coastline. They are regarded as closed systems as sediment is not usually transferred from one to the other. In reality, some sediment does get transferred between neighbouring cells.

As a wave approaches land it usually changes direction due to the way the wave drags on the bottom. When these waves change direction they can create a headland. A headland is a part of the shore that sticks out into the ocean.

On some beaches, sand grain size composition varies with distance from the water. A greater proportion of finer, smaller sand grains may be pushed higher up the beach by waves or by wind, whereas larger, coarser grains are deposited closer to the water.

A sediment cell operates as a closed system, with virtually no inputs or outputs of sediment from the cell. This system contains inputs, transfers and outputs. Sources are places where sediment is generated, such as cliffs or eroding sand dunes.

The key characteristics of sediment cells are as follows. Cells are discreet and function separately from each other. The sediment cells are geographically bounded by significant disruptions to the coastline, such as headlands, estuaries or a convergence of currents or longshore drift direction.

Sediment cells are areas along the coastline and in the nearshore area where the movement of material is largely self-contained. They can be considered as a closed coastal sub-system as far as sediment is concerned.

Sediment deposition is an extremely important part of the overall coastal system and, more specifically, the sediment cell. Areas of deposition – beaches, spits, mudflats, sand dunes and offshore bar – are all sediment stores or ‘sinks’ (Figure 7).

The main sources of sediment along coasts are: (1) the coastal landforms themselves, including cliffs and beaches; (2) the nearshore zone; and (3) the offshore zone and beyond.

Factors that influence sediment yield The quantity and type of sediment moving through a stream channel are intimately related to the geology, topographic character, climate, vegetational type and density, and land use within the drainage basin.

Geologists refer to all channelized water as “stream” regardless of size. The Longitudinal profile depicts the shape of a stream from head to mouth. Gradient: slope of the stream, determines the velocity of the stream. Divide: the higher topography that separates one drainage basin from another.

Parallel drainage. drainage pattern associated with steep slopes.

There are two types of base level- ultimate base level and local base level. The ultimate base level is sea level where the majority of water stream loses their mightiness. The local base level at which the river can erode its bed locally.

suspension