Clastic transport and fluid flow
Transport: Weathered rock is transported from source areas to depositional sites by three kinds of processes:
 Direct fluid flows of air, water, and glacial ice
 Wet, gravitydriven mass wasting,
 Dry, gravitydriven mass wasting,
Fluiddriven Transport:
Hydraulics  the properties of fluid flow
Fluid plays an important role in most models of sediment transport. Thus knowledge of hydraulics, the science of fluid flow, is essential to sedimentation and stratigraphy. Fluids resist forces that tend to change their volume, but readily alter their shape in response to external forces. The ability of a fluid to entrain particles is dependent on:
 Density
 Velocity
 Viscosity (resistance to shearing)
 Grain size
Density: Mass per unit volume. Typically measured in Kg/m^{3} or the equivalent g/cm^{3}. Examples:
 seawater = 1.03 g/cm^{3}
 freshwater = 1.0 g/cm^{3}
 glacial ice = 0.9 g/cm^{3}
 air < 0.001 g/cm^{3}
Velocity: Distance traveled per unit time.
Viscosity: the constant of proportionality between shear stress and shear rate. Stated simply, a more viscous fluid resists deformation more strongly than a less viscous. All fluids will deform when stressed. The more they are stressed, the more they are deformed. For most fluids, this relationship is directly proportional and can be written as follows:
τ = μ*du/dy
Where τ is shear stress, du/dy is shear rate, and μ is viscosity. Fluids of this type are called Newtonian fluids. Viscosity can be described as internal friction. Units of this force are in Poise (P) (=1 g * cm^{1} * s^{1}). The names Poiseuille and the shortened Poise are from the French physician, Jean Louis Poiseuille (1799  1869).
Examples of the viscosities of common substances at 20 deg. C:
Water  1.002 x 10^{2} Poise 
Air  ~1.7 x 10^{5} P 
Natural gas  1.0 x 10^{5} P 
Glacial ice  1.0 x 10^{11} P 
Mantle rock  1.0 x 10^{20} P 
Viscosity is temperature dependent (compare honey that has been heated on a stove with honey coming from a refrigerator.) This table demonstrates the change of water viscosity with temperature:
Temperature (deg. C)  Viscosity cP 
0  1.792 
20  1.002 
40  0.656 
60  0.469 
80  0.357 
100  0.284 
Scaling issue  boundary layers:
When a fluid flows around an object (or an object moves through a fluid) the region directly adjacent to the object  the boundary layer  is dominated by viscous and electrostatic forces that make it tend to adhere to the object. The thickness of this layer varies with: Viscosity
 Veocity
Flow conditions: Although fluid flow is describable by the continuous variables given above, it typically falls into one of two discrete states:
 Laminar flow: Fluid particles move uniformly in subparallel sheets or filaments. Characteristic of slow moving or very viscous material (E.G. glacial ice)
 Turbulent flow: Fluid particles move in random haphazard pattern. Characteristic of high velocity material. High erosive effect (E.G. surface winds)
The image of cigarette smoke (right) shows the abrupt transition between these states.
Numeric descriptors of flow:
Relationships of velocity, density, viscosity and flow state are numerically described using two dimensionless numbers: Reynolds Number
 Froude Number
 Velocity (higher velocity > turbulent)
 Viscosity (higher viscosity > laminar)
 The roughness of the flow boundary (rougher > turbulent)
 the confinement of the flow (more confined > turbulent)
 r is the hydraulic radius ((2A/P) where A = crosssectional area and P = wetted perimeter)
 V is the flow velocity (m/s)
 ρ is the fluid density (kg/m^{3})
 μ is viscocity (kg/(m^{.}s)).
 At low speed, raindrops roll downhill on the windshield under the influence of gravity. They can do this because the vehicle is operating at a low Reynolds number so its boundary layer is thick enough completely to encompass the raindrops.
 At higher speeds (and higher Reynolds numbers), the raindrops begin to move upward because the boundary layer has become thin enough that the drops are poking out of it and being blown by the surrounding medium.
 At very high speeds (don't try this at home) the drops move in random directions because the bondary layer is now so thin that the currents of the surrounding medium are channelled through minor irregularities of the windshield's topography (scratches, halfcleaned birdshit stains, etc.)
 V=velocity
 D=depth of flow
 g=gravitational constant.
 F_{r} < 1 results in tranquil flow. The velocity of gravity waves is greater than the flow velocity (i.e. waves can move upstream).
 F_{r} > 1 results in rapid flow. The velocity of gravity waves is less than the flow velocity,so no waves propagate upstream.
Reynolds Number:

Named for British physicist Sir Osborne Reynolds, describes the relative strength of inertial and viscous forces in a moving fluid by giving their dimensionless ratio:
inertial forces/viscous forces
As it happens, this relationship also describes the relationships between the transition from laminar to turbulent flow such that:
Reynolds Number = R_{e} = 2rVρ/μ
Where:
Note: The numerator shows inertial forces, or the tendency of discrete particles of fluid to resist changes in velocity and continue to move uniformly in the same direction. The denominator  viscosity, or resistivity to shearing or deformation. The transition from laminar to turbulent flow occurs between R_{e} of 500 and 2000. Typically, we see:
Environment:  R_{e}:  Flow: 
Slow flow and unconfined fluids moving across open surfaces (surface runoff sheet flow, slow streams, continental ice sheets)  <500  laminar 
5002000  transitional  
Rapid constricted flow (Fast streams, turbidity currents)  >2000  turbulent 
Rain on windshield from BetterPhoto.com
Viscous forces tend to resist fluid motion, keeping flow smooth, while inertial forces generate disordered (turbulent) motions. As such high inertial flows (R_{e}> 5000) tend to be turbulent, and viscous flows (R_{e}< 500) tend to be laminar. Unconfined fluids moving across open surfaces (windstorms, surface runoff sheet flow, very slowmoving streams, and continental ice sheets) have R_{e}<5002000 and exhibit laminar flow. Fastmoving streams and turbidity currents have R_{e} >2000.
Why does a sedimentologist care? Because turbulent flow carries much greater erosive force than laminar flow.
Raft caught on standing wave from AbsoluteAstronomy.com
Froude Number:

Elucidated by British physicist William Froude, a mathematical representation of the ratio between fluid inertial forces and fluid gravitational forces. This describes the tendency of a moving fluid to continue moving despite the gravitational forces that act to stop its motion.
F_{r} = flow velocity/(acceleration of gravity * force of inertia)
F_{r} = V/√(gD)
Where:
Consequences:
Gravity waves? Throw a stone into a standing body of water and watch the waves move out in concentric paths. This is a gravity wave; now throw a stone into moving water. if you can see the gravity wave move upstream then it is faster than the velocity of the stream. Thus F_{r} <1 otherwise known as tranquil flow, which is typical of most bodies of flowing water. If, however, F_{r} >1 then the velocity of the stream is faster than the gravity wave and rapid flow occurs.
Why does a sedimentologist care? Because Froude numbers are important to understanding the ripples and other sedimentary structures that form at the base of rapidly moving streams.
Particle Transport
Particle motion in flowing fluid: We care about hydraulics because of flowing fluids' ability to transport sediment. Why, however, does this actually happen?
Whereas ions in solution are simply part of the fluid, clasts must be moved by mechanical forces. This involves three distinct processes:
 Entrainment: Particles picked up into the transport medium (water, air, etc.)
 Transport: Movement within the transport medium
 Deposition: Settling out of the transport medium
 fluid drag (F_{D})
 fluid lift (F_{L})
In flowing streams, F_{D} and F_{L} combine to yield a composite fluid force, F_{F}.
 Dissolved load: The fraction in solution as ions.
 Suspended load: That fine portion that is kept in constant suspension by electrostatic and viscous interactions with the surrounding water. Generally clay or silt sized particles.
 Bed load: That portion that cannot be kept in constant suspension. Generally sand sized and larger. The bed load moves in two manners:
 saltation: bouncing along the stream bed, or being repeatedly picked up and put down by F_{F}.
 Traction: The remainder that rolls or slides in constant contact with the bed.
 No surprise that the smallest grains are deposited at the lowest flow velocities.
 But why are sand sized particles entrained before clay particles? (See if you can figure it out.)
Above all, larger clasts are entrained at higher velocities. Why?
Stokes' Law:
Developed by Sir George Gabriel Stokes, An object falling through a fluid experiences three forces: The force of gravity (F_{g}), accelerating it downward
 Bouyancy (F_{up})
 Drag (F_{d}), pushing it upward.
Terminal fall velocity: The speed with which it falls is the balance of these forces. Gravity tends to accelerate it downward, however, the laws of fluid dynamics tell us that the faster the object falls, the more drag it experiences, slowing it down. Eventually it reaches a settling rate, a point at which drag and bouyancy balance gravitational acceleration, the terminal fall velocity (F_{d}).
Essentially, this is expressed as F_{d} = F_{g}  F_{up}
Stokes calculated the fall velocity for small particles, < 0.1 mm diameter. First, consider the frictional resistance that the fluid offers to movement of a settling sphere:
where:
 Fd = resistance (frictional drag)
 C_{d} = Cd=drag coefficient (constant)
 d = particle diameter
 ρ_{f} is fluid density
 V = settling velocity of sphere.
Then consider the force of gravity pulling the sphere downward:
where ρ_{s} = density of the sphere and g = acceleration due to gravity.
The bouyant force of the liquid is given by:
where ρ_{f} = density of the fluid
Substituting these details into the original equation gives us:
This can be simplified into:
If the temperature and fluid density are constant and the sphere and fluid densities known then this equation can be simplified significantly using the Reynolds number relationship to:
where C is a constant given by (ρ_{s}  ρ_{f})g/18μ. At 20 deg C, in water, with a sphere density of 2.65 g/cc, C = 3.59 x 10^{4}
The punchline: In words, with density and viscosity constant, velocity increases as the square of grain diameter.
If we rotate the arrangement 90 degrees: With density and viscosity constant, the velocity required to move a clast through drag increases as the square of grain diameter.