Sedimentation by unidirectional traction currents is one of the most important processes for the transport and deposit of sediments. This is explained as the variation of the shape of the bed as the velocity of the fluid increases, through the Froude number, making it easy to identify it by the way in which the tissue and structure of the sediments are deposited; These traction currents can be generated by the effect of gravity (rivers), by the wind or by the forces of the tides. This process has been explained through essays, where it begins with a channel at rest. The sand on the channel floor is flat, the current velocity is zero. The water is allowed to move through the channel at a gradually increasing velocity. Sand grains begin to roll and jump when the critical velocity threshold is crossed.

A significant percentage of the world's sedimentary cover is deposited by turbidity currents, the behavior of a turbid flow is governed by the difference in density between it and the ambient fluid, by the shear stresses of its upper and lower limit, by its height and the angle of slope through which it flows.
urbidity currents operate in very diverse sedimentary contexts, but they are particularly effective in submarine canyons and constitute the most important mechanism for mobilizing and transferring sediment from shallow marine areas (shelfs) to deeper marine ones (ocean basins). ver time, the test of these types of currents have been tested in laboratories, since they are very difficult to experiment in the natural environment, from these experiments it is known that they show a characteristic geometry as they move, a part frontal or “head”, where the coarse sediment (from microconglomerate to coarse sand) is concentrated; an intermediate part or "body", the sediment that is dragged is medium-fine grain sand and a distal part or "tail", where clay silt is found. The flow of detail in the head is forward and upward, which initially causes strong erosion on the top of the bed on which they travel. In the body and tail the flow is parallel to the slope. This type of currents sediments turbidite sands, these are generally thick sequences of sandstones and periodic intercalated shale, in which a series of sections or "intervals" are differentiated. t is what is known as the “Bouma sequence”, since said author was the first to describe it in 1962. These intervals, from the wall (base) to the top of the turbiditic layer are the following: • Interval A: massive or granuloclassified (direct granuloclassification; with a decrease in the grain size of the sediment towards the top) (from microconglomerate to coarse sand). • Interval B: with parallel lamination (in coarse to medium sand). • Interval C: with “ripples” (current ripples) (in medium to fine/very fine sand). • Interval D: with parallel lamination (in silt/clay).
• Interval E: non-turbiditic (with diverse lithology; marl, silt/clay,
fine-grained limestone, etc.). As each interval is deposited, the energy in the fluid is lost, that is, the minerals in the E interval deposit with very little energy.

In low-density turbidity currents, the main mechanism is suspension drop, with traction from the subordinate bed load and the development of typical normal-graded layers.

Wind fluids tend to have a very similar glide to that of fluids, these particles move by rolling or jumping and therefore their bed shape is also similar. These carry the particles in suspension (cloud of dust). Threshold studies describe wind fluids as currents that carry low-density particles such as silts and clays. Although they have shapes similar to fluids, dunes are the most common type of this type of fluid, many studies have tried to understand the factors that control the morphology of wind dunes and their elusive internal structure. Special attention has been paid to the geometry and genesis of sand dunes, in order to better describe how these fluids were deposited. Four main morphological types can be defined: 1. Barchan dune (Form where sand is scarce. These are forms of bed transport, not net deposition. It is unlikely that they are often preserved in the geologic record). 2. Duna estrellada. 3. Dune seif (sand deposit)

Wind deposition occurs when the wind does not have enough energy to transport sand and other particles and deposits them.
The most characteristic sedimentary form of wind modeling are the wavy accumulations of sand grains of different sizes, such as ripples (up to 20 cm high), dunes or megadunes. Desert dune fields can occupy large areas, although loess, accumulations of fine materials (silts and clayey silts) can travel much further when transported in suspension.