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Stream power is the rate of potential energy loss per unit of channel length. [7] This potential energy is lost moving particles along the stream bed. = where is the stream power, is the density of water, is the gravitational acceleration, is the channel slope, and is the discharge of the stream.
For particle sizes where friction is the dominating force preventing erosion, the curves follow each other closely and the required velocity increases with particle size. However, for cohesive sediment, mostly clay but also silt , the erosion velocity increases with decreasing grain size , as the cohesive forces are relatively more important ...
The settling velocity (also called the "fall velocity" or "terminal velocity") is a function of the particle Reynolds number. Generally, for small particles (laminar approximation), it can be calculated with Stokes' Law. For larger particles (turbulent particle Reynolds numbers), fall velocity is calculated with the turbulent drag law.
Particle velocity (denoted v or SVL) is the velocity of a particle (real or imagined) in a medium as it transmits a wave. The SI unit of particle velocity is the metre per second (m/s). In many cases this is a longitudinal wave of pressure as with sound , but it can also be a transverse wave as with the vibration of a taut string.
Particle motion in an ocean wave at deep (A) and shallow (B) depths. 1) Propagation direction. 2) Wave crest. 3) Wave trough. Underneath the surface, there is a fluid motion associated with the free surface motion. While the surface elevation shows a propagating wave, the fluid particles are in an orbital motion.
Terminal velocity is the maximum speed attainable by an object as it falls through a fluid (air is the most common example). It is reached when the sum of the drag force ( F d ) and the buoyancy is equal to the downward force of gravity ( F G ) acting on the object.
Since the force is directed at right angles to the motion of the particle, it moves with a constant speed around a circle whose radius is given by: R = v f {\displaystyle R={\frac {v}{f}}} where f {\displaystyle f} is the Coriolis parameter 2 Ω sin φ {\displaystyle 2\Omega \sin \varphi } , introduced above (where φ {\displaystyle \varphi ...
If the particle's velocity is small enough, then the geodesic equation reduces to this: =. Here the Latin index n takes the values [1,2,3]. This equation simply means that all test particles at a particular place and time will have the same acceleration, which is a well-known feature of Newtonian gravity.