River channels are dynamic systems shaped by water flow and . They constantly evolve, influenced by factors like , , and . Understanding these processes is crucial for grasping how rivers shape landscapes over time.
Sediment transport in rivers involves complex interactions between water flow and particles. From tiny clay particles to large boulders, rivers move sediment in various ways. This movement affects channel form, , and even long-term landscape evolution.
River Channel Dynamics and Morphology
Factors Influencing Channel Dynamics
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Channel Geometry and Flow Characteristics View original
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River channel dynamics result from interplay of water discharge, sediment supply, channel slope, and bed/bank resistance to erosion
(straight, , ) determined by , , and
Straight channels form in areas with low sediment load and resistant banks
Meandering channels develop in areas with moderate sediment load and erodible banks
Braided channels occur in areas with high sediment load and unstable banks
(grade) involves balance between erosion and , leading to stable longitudinal profile
Graded streams adjust their slope to efficiently transport their sediment load
Changes in base level can disrupt and trigger channel adjustments
Channel cross-sectional geometry shaped by relationship between discharge, sediment load, and bank material properties
Width-to-depth ratio increases with higher sediment loads and more erodible banks
Channels in cohesive materials tend to be narrower and deeper than those in non-cohesive sediments
Floodplain Development and Channel Migration
Floodplain development driven by lateral erosion, formation, and
Lateral erosion widens valley and creates space for floodplain development
Point bars form on inside of meander bends, gradually becoming part of the floodplain
Overbank deposition during floods adds fine-grained sediment to floodplain surface
occurs through processes of erosion and deposition
(neck and chute) can dramatically alter channel course
involves abrupt abandonment of existing channel for new path across floodplain
Anthropogenic activities significantly alter natural river channel dynamics and morphology
Dam construction reduces sediment supply and alters flow regime downstream
increases and reduces habitat diversity
disconnects river from floodplain, concentrating flow in main channel
impacts on precipitation patterns and land use changes lead to long-term adjustments in river channel form and behavior
Increased frequency of extreme events may accelerate erosion and channel instability
Changes in vegetation cover affect runoff patterns and sediment supply to rivers
Sediment Transport in Fluvial Systems
Sediment Entrainment and Transport Modes
occurs when (lift and drag) overcome gravitational force and friction holding particles in place
required for entrainment varies with particle size and density
used to determine critical shear stress based on particle characteristics
Transport modes include , , , and , depending on particle size and flow conditions
Rolling and sliding occur for larger particles close to the bed
Saltation involves particles bouncing along the bed in short hops
Suspension keeps finer particles aloft in the water column through
Sediment transport capacity influenced by flow velocity, turbulence, and
Higher velocities and turbulence increase transport capacity
Channel constrictions can locally increase transport capacity due to flow acceleration
Deposition and Sediment Sorting
Deposition occurs when flow velocity decreases below settling velocity of particles
Often happens in areas of reduced stream power (pools, channel expansions)
Settling velocity depends on particle size, shape, and density
illustrates relationship between particle size, flow velocity, and processes of erosion, transport, and deposition
Shows critical erosion velocity and settling velocity for different grain sizes
Demonstrates why clay particles are difficult to erode once deposited
Sediment sorting during transport and deposition leads to characteristic grain size distributions in different fluvial environments
occurs as larger particles are deposited first
in deposits can indicate changes in flow conditions over time
Stream Power and Sediment Transport
Stream Power Concepts and Calculations
Stream power defined as rate of per unit length of channel
Calculated as product of discharge, slope, and
Ω=γQS, where Ω is stream power, γ is specific weight of water, Q is discharge, and S is slope
Relationship between stream power and sediment transport capacity generally positive and non-linear
Higher stream power enables transport of larger particles and greater sediment volumes
Critical stream power threshold exists for initiation of sediment motion
Sediment size influences transport capacity through effect on particle entrainment thresholds and settling velocities
Larger particles require greater stream power for entrainment
Finer particles have lower settling velocities and can be transported at lower stream powers
Transport Capacity and Sediment Supply
describes maximum particle size a stream can transport at given flow condition
Related to stream power and local
Can be estimated using empirical equations or critical shear stress approaches
Transport capacity varies spatially within channel due to variations in local hydraulics and bed roughness
Higher in areas of flow convergence or increased slope
Lower in areas of flow divergence or decreased slope
quantify relationship between hydraulic parameters and sediment transport rates
Meyer-Peter and Müller equation commonly used for bedload transport:
qb=8(τ∗−τc∗)1.5(s−1)gD3
where qb is bedload transport rate, τ∗ is dimensionless shear stress, τc∗ is critical dimensionless shear stress, s is specific gravity of sediment, g is acceleration due to gravity, and D is particle diameter
Balance between sediment supply and transport capacity determines whether reach experiences , , or maintains equilibrium
Aggradation occurs when supply exceeds capacity
Degradation occurs when capacity exceeds supply
Equilibrium maintained when supply matches capacity
Fluvial Load Types
Suspended and Bed Load
consists of fine particles (typically silt and clay) carried within water column by turbulence
Concentration often increases with flow depth
Can constitute majority of total sediment load, especially during high flow events
includes coarser particles (sand and gravel) that move along or near channel bed by rolling, sliding, or saltation
Generally makes up smaller proportion of total load compared to suspended load
Transport is more episodic and strongly dependent on flow conditions
Ratio of suspended to bed load can influence channel morphology and sedimentary structures in depositional environments
High suspended load ratios associated with muddy floodplains and fine-grained channel deposits
High bed load ratios associated with gravel-bed rivers and coarse-grained deposits
Dissolved Load and Measurement Techniques
comprises ions and molecules in solution, primarily derived from chemical weathering of rocks and soils
Major ions include calcium, magnesium, sodium, potassium, bicarbonate, sulfate, and chloride
Concentration can vary seasonally and with discharge
Relative proportions of suspended, bed, and dissolved loads vary with lithology, climate, and watershed characteristics
Carbonate watersheds often have high dissolved loads
Arid regions may have higher proportion of bed load due to lack of vegetation and flashy runoff
differ for each load type
Water sampling used for suspended and dissolved loads
Depth-integrated samplers collect representative samples throughout water column
Automated samplers can capture temporal variations in load
Bedload samplers or tracers used for bed load
Helley-Smith sampler commonly used for sand and fine gravel
Painted or magnetic tracers can track movement of individual particles
Bed load transport often follows power-law relationship with discharge
Qb=aQb, where Qb is bed load transport rate, Q is water discharge, and a and b are empirical coefficients