Property:Describe processes
From CSDMS
This is a property of type Text.
L
* Interception
* Evaporation of interceted water
* Snow melt
* Frost index
* Water available for infiltration and direct runoff
* Water uptake by roots & transpiration
* Evaporation from the soil surface
* Preferential bypass flow
* Infiltration capacity
* Actual infiltration and surface runoff
* Soil moisture redistribution
* Groundwater
* Surface runoff routing
* Sub-surface runoff routing
* Channel routing
* Irrigation
* Water use
+
S
*Fluvial/alluvial processes;
**Aggrading fluvial channels in one gridcell with crevasse. Subgrid sedimentation mimics alluvial ridge aggradation and overbank deposition. Avulsions are modelled one dimensionally by calculating the flow and sediment transport at prospective avulsion nodes. See also Dalman & Weltje (2008).
*Floodplain processes;
**Differential compaction, groundwater table, peat growth and overbank deposition
*Hypopycnal plume and marine currents:
**Rivers deliver sediment and water to the sea, where the river momentum spreads the suspended sediment in a plume. Multiple plumes and longshore current hydrodynamics are calculated using a potential flow routine. Subsequent sedimentation due to fallout uses the removal rate principle after Syvitski et al (1988).
*Wave resuspension and crosshore transport;
**Waves are modelled using linear Airy and Stokes wave theory. Deepwater wave height is derived from a Gaussian distribution to represent natural storm variability The asymmetric waves preferentially transport the sands (bedload fraction) shorewards and the fines (suspended load fraction) offshore. In combination with a littoral drift routine this allows waves to rework and transport sediments.
+
B
- Stochastically generated storm environment
- Dune growth and storm erosion
- Storm overwash
- Sea-level rise
- Shoreline change (ocean and back-barrier)
- Dynamic shoreface response to sea-level rise, overwash, and dune growth
- Interior shrub expansion and mortality +
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M
1. Bedrock and soil physical weathering;
2. Sediment transport by overland flow;
3. Soil Creep (diffusion);
4. Aeolian deposition. +
L
1D gradually varied channel flow, Total sediment transport of a river at a node, mass conservation, tectonic elevation changes, settling velocity +
S
H
2
C
2d multiple flow direction steady state flow model
Erosion and deposition over 9 separate grainsizes
Bedload and suspended load sediment transport
Slope processes (creep, enhanced creep and mass movement)
Vegetation growth
Aeolian transport (under development - slab dune model) +
A continuity equation, representing the conservation of sediment in the nearshore zone, relates gradients in alongshore sediment flux to horizontal shoreline changes, given a depth over which erosion or accretion are distributed—the depth of the shoreface. This treatment embodies the assumption that cross-shore sediment fluxes across base of the shoreface are small compared to gradients in alongshore flux. However, cross-shore sediment fluxes landward of the shoreline, associated with overwash, are treated, allowing barriers to migrate and maintain elevation relative to a rising sea level. See Ashton and Murray (2006a) for a full treatment of these model dynamics.
The material underlying the shoreline and shoreface converted to mobile sediment as it is exposed by shoreline erosion. The lithology is parameterized by two quantities that can vary across the model domain: the maximum weathering rate (which occurs when the shoreface is bare of sediment) and the composition of the resulting sediment (percentage coarse enough to stay in the nearshore system. See Valvo et al. (2006) for a full explanation of how underlying geology is treated.
Where beach nourishment is deemed by the user to be occurring, if the gradients in sediment flux would cause the shoreline to erode landward of a pre-determined location, sediment is added at the rate required to prevent such shoreline change. Hard structures are treated as if the lithology has a maximum weathering rate of 0. +
A
A set of biophysical modules that simulate biological and physical processes in farming systems.
A set of management modules that allow the user to specify the intended management rules that characterise the scenario being simulated and that control the simulation. +
O
Advection, Dispersion, Inflow, and Transient Storage. First-order loss/production, sorption. +
N
Advective transport and removal of nitrate and organic carbon via denitrification in lakes, wetlands, and channels. +
R
Aeolian sediment transport (snow or sand grains), granular motion, avalanches, snowfall, time-dependent cohesion +
W
C
A
Alpine3D is a model for high resolution simulation of alpine surface processes, in particular snow processes. The model can be driven by measurements from automatic weather stations or by meteorological model outputs. The core three-dimensional Alpine3D modules consist of a radiation balance model (which uses a view factor approach and includes shortwave scattering and longwave emission from terrain and tall vegetation) and a drifting snow model solving a diffusion equation for suspended snow and a saltation transport equation. The processes in the atmosphere are thus treated in three dimensions and coupled to a distributed one dimensional model of vegetation, snow and soil model (Snowpack) using the assumption that lateral exchange is small in these media. +
P
Any 3D ocean circulation, mixing, dispersion processes, etc +
T
Any density driven current including particle-laden flows produced by the lock-exchange (or continuous inflow) can be simulated. The flow can interact with any arbitrary topography on the bottom. +
G
Any type of turbidity (or gravity) currents could be modeled with this code. Is also handles the flows passing complex topographies, inflow/outflows too. +
S
Any type of turbidity (or gravity) currents could be modeled with this code. I also use it for modeling internal bores. +
C
As a crevasse splay evolves, the slope of its outflow should be no less than the slope of lower channel; and the bottom elevation of a crevasse splay should be no lower than the elevation of lowest point of channel bed, so the bottom elevation of the lowest point that a crevasse splay is able to cut down is max(hs, Zcsb).
A ratio of Q above the bottom of crevasse splay can be distributed to outflow of crevasse splay. After flow parameters for the outflow of crevasse splay are calculated, the erosion (deposition) rate of crevasse splay can be calculated, thus the morphology of crevasse splay can be updated.
When the crevasse splay has not yet cut down to the lowest point max(hs,Zcsb), it can be both widened and deepened. When the crevasse splay has cut down to the lowest point max(hs,Zcsb), it can only be widened or silted vertically. +
L
As of autumn 2013, the library of process components includes the following:
- diffusion (for conductive heat transport, soil transport over terrain, or other applications of diffusion theory)
- single-direction flow routing over topography
- detachment-limited stream erosion
- solar radiation input as a function of topography, latitude, and time
- evapotranspiration
- soil-moisture dynamics
- stochastic storm generation
- stochastic wildfire generation
- impact cratering
- overland flow / flood inundation +
B
BIT Model takes into consideration five different processes:
* reworking of the beach profile. The model assumes that the wave action reworks the beach profile towards an equilibrium configuration described by the Dean's equation;
* inner-shelf sediment redistribution, which is the redistribution of sediments beyond the beach toe determined by the bottom shear stresses produced by wind waves;
* overwas, which is the erosion of sediment along the beach profile and its corresponding deposition on the top of the barrier island or in the back-barrier area. Overwash is related to storm surges produced bt extreme atmospheric events;
* lagoonal deposition, which is the deposition of fine sediments in the accomodation space between the barrier island and the mainland;
* aeolian sediment reworking, which represents the wind action on the subaerial part of the island. +
C
Basic processes include runoff generation, water erosion and sediment transport, and gravitational erosion and sediment transport. Depending on the application, the user can apply a vegetation-growth module, various tectonic functions, and other options. +
B
Basin and Landscape Dynamics (Badlands) is a parallel TIN-based landscape evolution model, built to simulate topography development at various space and time scales. The model is presently capable of simulating hillslope processes (linear diffusion), fluvial incision ('modified' SPL: erosion/transport/deposition), spatially and temporally varying geodynamic (horizontal + vertical displacements) and climatic forces which can be used to simulate changes in base level, as well as effects of climate changes or sea-level fluctuations. +
C
Bay, marsh, and forest evolution on a coastline. Simulates marsh edge erosion, bay depth changes with wind waves, and marsh migration into coastal forests, and the carbon processes associated with these changes. +
S
Bed boundary layer for pure current, combined current and waves, and pure waves.
Transport of non-cohesive sediment.
Erosion, transport and deposition of cohesive sediment. +
R
Bed-material sediment transport and storage on a river network. +
M
Bedrock fluvial incision (shear stress or sediment flux dependency).
Mass wasting (creep and threshold-limited).
Bedload sediment transport & deposition in streams, fans, deltas.
Impact cratering, aeolian deposition, lava flows.
Flow routing with evaporation from depressions. +
H
O
Bottom orbital velocity is calculated from surface wave conditions using linear wave theory. A spectral approach is used. If input wave data are just wave height and period, a spectrum is estimated based on those as described in Wiberg and Sherwood 2008. Several spectral representations are available, and spectra can be estimated based on wind speed if surface wave conditions are unknown. +
C
CAM treats radiative transfer, tidal forcing from Saturn, a planetary boundary layer and surface interaction, thermal conduction in the soil and chemistry. The CARMA part of the code does the aerosol microphysics involving emission, coagulation and sedimentation. +
F
Calculate water depth from a flood extent polygon (e.g. from remote sensing analysis) based on an underlying DEM.
Program procedure:
1. Flood extent polygon to polyline
2. Polyline to Raster - DEM extent and resolution (Env)
3. Con - DEM values to Raster
4. Focal Statistics loop
5. Water depth calculation - difference between Focal Statistics output and DEM +
S
Centerline migration, Floodplain sediment, and channel profile evolution, depending upon choices in the parameter input files, as detailed in the model documentation. +
A
Channel migration and avulsion building stratigrpahy +
Channel planform geometry +
B
Cliff failure and retreat; hillslope evolution; river erosion; block release, transport, and weathering. +
W
Climate generation (CLIGEN), infiltration, percolation, evapotranspiration, plant growth, residue management and decomposition, runoff, hydralics of overland flow, soil detachment by raindrop impact and shallow flow (interrill), soil detachment by excess flow shear stress (rill, channel), sediment transport, sediment deposition, irrigation, winter processes (snow melt, frost, thaw), channel erosion processes, sedimentation in impoundments. +
C
I
Computation of drainage area, which, for a particular cell, is the sum of cells that drain through that cell. +
R
Computes wave refraction and diffraction processes over an arbitrary bathymetry constrained only to have mild bottom slopes. +
S
H
DEM resampling;
Depression filling;
Flow direction;
Flow accumulation; +
G
Discretizes a watershed into sub-catchments (for surface water) and a MODFLOW grid (for groundwater), and then uses these fundamental units to build input files for and execute GSFLOW and visualize it. +
L
Disturbance-driven soil creep (or other processes that can be represented by 2D diffusion). +
D
Erosion, transport and deposition of sediments (terrestrial -> deep-marine). Carbonate production. Complex tectonics (growth faults, salt deformation). +
W
Evolution of wind wave spectra under influence of wind, breaking, nonlinear interactions, bottom interaction (including shoalng and refraction), currents, water level changes and ice concentrsations. No diffraction. +
B
Explores ecogeomorphic couplings between adjacent and non-adjacent components of the entire coastal barrier system, from the ocean shoreface to the mainland forest. Processes include: Dune growth and storm erosion; storm overwash; shoreline change (ocean and back-barrier); dynamic shoreface response to sea-level rise, overwash, and dune growth; horizontal and vertical marsh dynamics; bay depth changes with wind waves; marsh migration into coastal forests; sediment exchange between barrier-marsh-bay-forest ecosystems; and carbon processes associated with ecogeomorphic changes. +
A
Extract c and alpha from:
Slope=cArea^alpha
For more details:
Cohen, S., G. Willgoose, and G. Hancock (2008), A methodology for calculating the spatial distribution of the area-slope equation and the hypsometric integral within a catchment, J. Geophys. Res., 113, F03027, doi:10.1029/2007JF000820. +
T
B
A
Fluvial erosion and depositions, lateral deposition across the floodplain, plume deposition in marine domain. +
C
Fluvial erosion, deposition and sedimentation, hillslope (diffusion) processes, flexure, orography +
E
Fluvial sediment entrainment and deposition +
S
Fluvial sediment erosion and deposition, fluvial bedrock erosion, the bedrock cover effect. +
P
Flux routing and sediment transport for the formation of river deltas. Resolves channel bifurcations, avulsion and migration. Can simulate subsidence (default basin-like shape, modify the Python code to customize). Can store stratigraphy (as sand fraction and thickness). +
C
For forward time integration, the simplest possible scheme, first-order forward Euler, is employed. +
B
Free surface flow of water. Conservation of heat, salinity, mass, turbulent kinetic energy, dissipation. +
S
Free surface, generalized s coordinate model. Classical representation of oceanic processes (tides, wind circulation, density driven circulation ...). Coupling with sediment transport and biogeochemistry +
G
Free-surface flow including wave action
Clastic erosion, transport, deposition
Compaction (load-based, vertical porous flow, full 3D porous flow)
Rudimentary carbonate growth +
GENESIS was designed to describe long-term trends of the beach plan shape in the course of its approach to an equilibrium form. The shoreline change model best calculates shoreline movement in transition from one equilibrium state to another. This change is usually caused by a notable pertubation, for example, jetty construction at a harbor or inlet, or placement of beach nourishment material. +
GSFLOW simulates flow within and among three regions. The first region is bounded on top by the plant canopy and on the bottom by the lower limit of the soil zone; the second region consists of all streams and lakes; and the third region is the subsurface zone beneath the soil zone. PRMS is used to simulate hydrologic responses in the first region and MODFLOW-2005 is used to simulate hydrologic processes in the second and third regions. +
W
General circulation model of early Earth. Particular detail is paid to chemistry, RT, and haze microphysics +
G
Groundwater flow and seepage +
T
H
HSPF assumes that the "Stanford Watershed Model" hydrologic model is
appropriate for the area being modeled. Further, the instream model assumes
the receiving water body is well-mixed with width and depth and is thus
limited to well-mixed rivers and reservoirs. Application of this methodology
generally requires a team effort because of its comprehensive nature. +
L
Heat conduction in permafrost, lake ice growth-decay, permafrost subsidence due to excess ice +
M
H
Hydrologic processes:
Precipitation, infiltration, evapotranspiration, overland flow, saturation-excess runoff, groundwater flow
Geomorphic processes:
Baselevel lowering, weathering, hillslope processes, erosion, sediment transport +
C
Hydrology: Spatially variable TOPMODEL
2d Hydrodynamic flow model: Using the Lisflood-FP (Bates et al., 2010) method
Fluvial erosion and deposition over 9 different grainsizes - through 10 active layers
Lateral erosion: Based on radius of curvature
Slope processes: Landslides and soil creep
Sand Dunes: Ability to couple sand dune sub model with fluvial processes. +
I
S
I
ILAMB takes a set of observational data encoded as CF-compliant netCDF files, extracts commensurate quantities from historical model results (ideally compliant with CMOR), and then subjects them to a gauntlet of statistical measures examining aspects of performance such as bias, RMSE, phase, interannual variability, and spatial distribution. This results in a hierarchical set of webpages which display and controls the flow of information. +
W
In WOFOST, crop growth is simulated on the basis of eco-physiological processes. The major processes are phenological development, light interception, CO2-assimilation, transpiration, respiration, partitioning of assimilates to the various organs, and dry matter formation. Further, the interaction with the soil is included in relation to soil moisture availability and (in more recent version) also soil N/P/K availability.
Potential and water-limited growth is simulated dynamically, with a time step of one day. Nutrient-limited production is calculated either statically based on the QUEFTS approach (on the basis of soil characteristics and the water-limited production output) or dynamically using nutrient demand/supply at daily time steps. +
L
Incision of a transport-limited river in an alluvial substrate. Initial geometry is that of a steep channel with sediment transport capacity exceeding that of the input flux from upstream.
The river randomly migrates left or right and needs to evacuate sediments mined from its bed and from the valley walls.
Product of wall erosion not evacuated by the river are deposited as taluses at the foot of the walls. +
W
It simulates rainfall runoff process as random storm events that fall on the initial topographic surface and flow downhill following steepest descent. +
K
Kudryavtsev's parametrization treats a permafrost environment as a system of individual layers, each with their own thermal properties.
Air, snow, vegetation, soil each are separate layers and their thermal (insulatory effects) are quantified from layer thickness, their heat capacity and conductivity. +
D
Lagrangian particle transport. See also: https://passah2o.github.io/dorado/background/index.html +
V
Land Cover and Soil Snow Model
Meteorology (Inputs, Distributed Precip, and Snow/Elevation Bands)
Frozen Soil (including Permafrost)
Dynamic Lake/Wetland Model (new to 4.1.1)
Flow Routing +
C
Linearized RANS
Aeolian sediment transport
Shear stress reduction by vegetation
Plant growth (exponential relaxation) +
M
MARSSIM is a grid based, iterative framework that incorporates selectable modules, including: 1) flow routing, optionally including event-driven flow and evaporation from lakes in depression as a function of relative aridity (Matsubara et al., 2011). Runoff can be spatially uniform or variably distributed. Stream channel morphology (width and depth) is parameterized as a function of effective discharge; 2) bedrock weathering, following Equation 1; 3) spatially variable bedrock resistance to weathering and fluvial erosion, including 3-D stratigraphy and surficial coherent crusts; 4) erosion of bedrock channels using either a stream power relationship (Howard, 1994) or sediment load scour (Sklar and Dietrich, 2004; Chatanantavet and Parker, 2009); 5) sediment routing in alluvial channels including suspended/wash load and a single size of bedload. An optional sediment transport model simulates transport of multiple grain sizes of bedload with sorting and abrasion (Howard et al., 2016); 6) geometric impact cratering modeling optionally using a database of martian fresh crater morphology; 7) vapor sublimation from or condensation on the land surface, with options for rate control by the interaction between incident radiation, reflected light, and local topography; 8) mass wasting utilizing either the Howard (1994) or the Roering et al. (1999, 2001a) rate law. Bedrock can be optionally weathered and mass wasted assuming a critical slope angle steeper than the critical gradient for regolith-mantled slopes. Mass wasted debris is instantaneously routed across exposed bedrock, and the debris flux can be specified to erode the bedrock; 9) groundwater flow using the assumption of hydrostatic pressures and shallow flow relative to cell dimensions. Both recharge and seepage to the surface are modeled. Seepage discharge can be modeled to transport sediment (seepage erosion) or to weather exposed bedrock (groundwater sapping); 10) deep-seated mass flows using either Glen's law or Bingham rheology using a hydrostatic stress assumption; 11) eolian deposition and erosion in which the rate is determined by local topography; 12) lava flow and deposition from one or multiple vents. These model components vary in degree to which they are based on established theory or utilize heuristic
MODFLOW 6 presently contains two types of hydrologic models, the Groundwater Flow (GWF) Model and the Groundwater Transport (GWT) Model. The GWF Model for MODFLOW 6 is based on a generalized control-volume finite-difference (CVFD) approach in which a cell can be hydraulically connected to any number of surrounding cells. Users can define the model grid using
1. a regular MODFLOW grid consisting of layers, rows, and columns,
2. a layered grid defined by (x, y) vertex pairs, or
3. a general unstructured grid based on concepts developed for MODFLOW-USG.
For complex problems involving water-table conditions, an optional Newton-Raphson formulation, based on the formulations in MODFLOW-NWT and MODFLOW-USG, can be activated. The GWF Model is divided into "packages," as was done in previous MODFLOW versions. A package is the part of the model that deals with a single aspect of simulation. Packages included with the GWF Model include
- those related to internal calculations of groundwater flow (discretization, initial conditions, hydraulic conductance, and storage),
- stress packages (constant heads, wells, recharge, rivers, general head boundaries, drains, and evapotranspiration), and
- advanced stress packages (streamflow routing, lakes, multi-aquifer wells, and unsaturated zone flow).
An additional package is also available for moving water available in one package into the individual features of the advanced stress packages. The GWF Model also has packages for obtaining and controlling output from the model.
The GWT model for MODFLOW 6 simulates three-dimensional transport of a single solute species in flowing groundwater. The GWT Model solves the solute transport equation using numerical methods and a generalized CVFD approach, which can be used with regular MODFLOW grids or with unstructured grids. The GWT Model is designed to work with most of the new capabilities released with the GWF Model, including the Newton flow formulation, unstructured grids, advanced packages, and the movement of water between packages. The GWF and GWT Models operate simultaneously during a MODFLOW 6 simulation to represent coupled groundwater flow and solute transport. The GWT Model can also run separately from a GWF Model by reading the heads and flows saved by a previously run GWF Model. The GWT model is also capable of working with the flows from another groundwater flow model, as long as the flows from that model can be written in the correct form to flow and head files.
G
Main purpose of the model is to calculate subsurface temperature profile, active layer depth and freeze-up day. +
S
Many 2D flow situation with simple boundary conditions (ie no inflow or outflow). suitable for lock/exchange simulation of gravity/turbidity currents or to study stability properties of stratified flow. +
W
Marsh boundary erosion by waves
Marsh boundary progradation by accumulating sediments
Mudflat sediment erosion/deposition by wind waves
Sediment exchange between mudflat and open ocean
Sediment exchange between mudflat and marsh platform
Organogenic sediment production on marsh platform +
B
Mass flux per unit width, dry mass of grains moving over the unit bed area, calculates the suspendable amount present in the moving bed +
T
Modeled processes include:
*Channelized flow (kinematic, diffusive or dynamic wave, all 1D and D8-based)
*Overland flow
*Snowmelt (degree-day or energy balance)
*Icemelt (from valley glaciers using GC2D)
*Meteorology (including precipitation, air temperature, shortwave and longwave radiation, etc.)
*Evaporation (Priestley-Taylor or energy balance)
*Infiltration (Green-Ampt, Smith-Parlange or Richards' 1D, multi-layer), *Shallow subsurface flow (Darcy, up to 6 layers)
*Flow diversions (sinks, sources or canals) +
S
G
Natural, agricultural, atmospheric, and direct human (sewage and P detergents) inputs; effect of hydrological functioning; generalized loss of nutrients in soils and groundwater; loss in rivers, reservoirs, and through consumptive water withdrawals (irrigation). +
N
NearCoM predicts surface waves and wave-induced nearshore processes such as nearshore circulation, sediment transport and morphological changes. +
S
O
None, the module analyses strata produced by all depositional processes +
None. Code tests for the presence of order in strata that could arise from allocyclic or autocyclic processes +
G
Note: See also the GEOMBEST++Seagrass Users Guide, section 4
Seagrass wave attenuation and bay depth effects
Equilibrium profile & barrier transgression
Sea level rise
Back-barrier deposition
Marsh expansion/contraction
Marsh wave erosion +
M
Organic accretion
Inorganic accretion (function of elevation and distance from channels)
Pond formation
Pond expansion
Pond deepening
Pond drainage
Bank slumping (soil diffusion)
Subsidence due to ditches +
1
Overall, the module simulates a particle-based model of hillslope evolution in 1D.
The module contains several scripts and functions, the most important of which are the following.
(1) zrp.m is the script wherein the parameters are set and from which the following functions are called.
(2) init_x.m is the function which generates an initial profile for the hillslope.
(3) make_moves.m is the function which samples the probabilistic dynamics.
(4) calc_rates.m is the function which determines the rates at which the particles are moving.
In addition to these, there are the following.
(5) perturb.m is the function which implements the hillslope perturbation and is called by the main script.
(6) calc_flux.m and calc_fluxes.m are the functions which infer fluxes along the hillslope. +
O
Physical transport: Advection, Dispersion, Inflow, Transient Storage, and Settling.
Chemistry: Precipitation/Dissolution, Sorption/Desorption, Oxidation/Reduction, aqueous complexation, and acid-base reactions +
G
Please have a look at: http://www.slideshare.net/GEOFRAMEcafe/geotop-2008?type=powerpoint. +
C
Population ecology represented by diffuse competition Lotke-Volterra calculus, cellular automaton, cellular stochastic models.
Sediment transport arbitrated by slopes and wave energy pickup
Bioerosion scaled to the seafloor presence of skeletal material +
D
Precipitation enters the snowpack, if present, and is then available as snowmelt, depending mainly on air temperature and solar radiation. Snowmelt and rainfall partly infiltrate infiltrate into the soil and partly run off directly to surface storage, depending upon the moisture content of the soil. Infiltration is high if the soil is dry, and surface runoff is high if the soil is saturated. Soil moisture evaporates or is transpired by vegetation, depending on the types of vegetation, the season, solar radiation, air temperature, humidity, and wind speed. The remainder percolates into deeper basin storages that feed surface storage through interflows and groundwater flows. Generally, these supplies are high if the soil and groundwater storages are large. Finally, there is a flow into surface storage from the upstream cell, which is routed, along with all the other flows into surface storage, through the cell into the next downstream cell. +
H
Precipitation is generated by a climate routine within the model. Snow accumulation and melt,glacier growth and ablation, surface runoff, and groundwater evaporation, retention and recharge.
Long and short term sediment discharge is solved by an empirical relation. +
T
Priestley-Taylor method of estimating losses due to evaporation +
F
Process:
# carbonate productivity and deposition
# winnowing
# reef development
# carbonate depositional facies
Model determines these through five deterministic and fuzzy steps:
# data input
# data fuzzification
# fuzzy rule analysis
# aggregation of results
# defuzzification +
P
Processes like:
*Saturated subsurface flow.
*Variably-saturated subsurface flow.
*Integrated overland flow.
*Land-energy budget.
*Shallow heat transport.
*Bio-geochemistry (plant/water interactions).
*Correlated, Gaussian random field generators. +
C
Processes represented by CREST are: Canopy interception, excess rain and infiltration water, runoff, evapotranspiration +
G
Processes represented:
''Note: See also the GEOMBEST+ Users Guide'', section 4<br>
'''4.1 Equilibrium profile'''<br>
'''4.2: Sea Level Change'''<br>
'''4.3: Initial Morphology/Stratigraphy'''<br>
'''4.4: Depth-Dependant Shoreface Response Rate'''<br>
'''4.5: Backbarrier Deposition'''<br>
'''4.6: Bay and Marsh Infilling'''<br> +
S
Processes:
# Wave properties derived from wind speed, wind angle and equations that describe a "fully-developed" sea state.
# Longshore sediment transport as modeled by the CERC or Kamphuis formulas.
# Conservation of mass for sediment.
# Simple methods to model cross-shore sediment transport. +
G
Processes:
*Rainfall: gage with nearest neighbor or inverse distance-squared weighting, radar.
*Interception: empirical model.
*Infiltration: Green & Ampt, Green & Ampt with redistribution, three-layer Green & Ampt, or Richard's equation.
*Overland runoff: 2-D finite volume diffusive wave with overland flow dykes and pothole lakes.
*Channel routing: 1-D dendritic finite-volume diffusive wave with culverts, on-channel lakes, rule curves, rating curves, scheduled releases.
*Groundwater: 2-D finite-difference with wells and various boundary conditions.
*Overland erosion: three alternative source equations, raindrop impact, erosion limits, deposition, arbitrary size classes.
*Channel sediment transport: advection-diffusion for fines, stream power for sands.
*Fate and transport of conservative and non-conservative
constituents in soil, overland, and channels +
R
ROMS resolved fast (gravity waves) and slow (Rossby waves) dynamics. Hydrostatic approximation but there is a nonhydrostatic version of ROMS. +
C
ROMS resolved fast (gravity waves) and slow (Rossby waves) dynamics. Hydrostatic approximation but there is a nonhydrostatic version of ROMS. +
ROMS resolved fast (gravity waves) and slow (Rossby waves) dynamics. Hydrostatic approximation but there is a nonhydrostatic version of ROMS. +
U
ROMS resolved fast (gravity waves) and slow (Rossby waves) dynamics. Hydrostatic approximation but there is a nonhydrostatic version of ROMS. +
S
G
Regolith disturbance; rock weathering; rock dissolution; baselevel lowering; fault slip +
Regression based interpolation. Different regression equation type can be used.
Land use area in each grid cell is the dependent variable and global population is the independent variable. +
Represented processes:
* Ice Thickness Evolution
* Temperature Solver
* Basal Boundary Condition
* Isostatic Adjustment +
Response of a lithospheric plate of nonuniform elastic thickness to an applied surface load +
O
Routes a hydrograph (changing water discharges through time) across a gridded model terrain. At each location, water discharge is calculated at each time step as a function of surface roughness, local water depths and water surface slopes. +
G
S
SBEACH is an empirically based numerical model for estimating beach and dune erosion due to storm waves and water levels. The magnitude of cross-shore sand transport is empirically related wave energy dissipation per unit water volume in the main portion of the surf zone. Direction of transport is dependent on deep water wave steepness and sediment fall speed. +
STWAVE simulates depth-induced wave refraction and shoaling, current-
induced refraction and shoaling, depth- and steepness-induced wave breaking,
diffraction, wind-wave growth, and wave-wave interaction and whitecapping that
redistribute and dissipate energy in a growing wave field. +
SWAN accounts for the following physics:
* Wave propagation in time and space, shoaling, refraction due to current and depth, frequency shifting due to currents and non-stationary depth.
* Wave generation by wind.
* Three- and four-wave interactions.
* Whitecapping, bottom friction and depth-induced breaking.
* Wave-induced set-up.
* Propagation from laboratory up to global scales.
* Transmission through and reflection (specular and diffuse) against obstacles.
* Diffraction. +
SWMM accounts for various hydrologic processes that produce runoff from urban areas. These include:
* time-varying rainfall
* evaporation of standing surface water
* snow accumulation and melting
* rainfall interception from depression storage
* infiltration of rainfall into unsaturated soil layers
* percolation of infiltrated water into groundwater layers
* interflow between groundwater and the drainage system
* nonlinear reservoir routing of overland flow. +
A
Salt marsh erosion by wind waves.
The presence of natural heterogeneities is an integral characteristic of salt marshes and needs to be account for, as local feedbacks could influence the large scale morphodynamic evolution of these wetlands. Herein, we use field data and a cellular automata model to investigate salt marsh response to wave action under different wave energy conditions and frequency of extreme events. +
B
Sea-level rise, alongshore sediment transport, and tidal-driven sediment transport on barrier islands, resulting in storm-overwash, tidal inlet formation, migration, and closure, and barrier transgression +
M
Sediment advection/diffusion
Sediment settling
Bed erosion
Soil creep
Organic sediment production
Increase in effective settling due to vegetation
Increase in drag due to vegetation +
S
Sediment routing in alluvial channels, deposition, erosion, avulsion +
E
Sediment transport (parameterized with slope and contributing area grids), rainfall, uplift, base-level lowering. +
T
Sediment transport under steady channel flow, oscillatory flow (sinusoidal and Stokes 2nd order waves) +
R
Sediment transport, channel bed aggradation/degradation, fluvial bank erosion (excess shear stress) and bank failure (mass wasting). See Lammers and Bledsoe (2018) and Lammers and Bledsoe (2019) for more information: https://www.sciencedirect.com/science/article/pii/S0022169418307303
https://www.sciencedirect.com/science/article/pii/S0301479718314968 +
M
Sedimentation, compaction, root growth and death, carbon deposition, carbon decay +
P
See See 'Description of Input and Examples for PHREEQC Version 3 - A computer program for speciation, batch-reaction, one-dimensional transport, and inverse geochemical calculations'. +
F
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See the GEOMBEST++ Users Guide, section 4.
Equilibrium profile
Sea Level Change
Depth-Dependant Shoreface Response Rate
Backbarrier Deposition
Bay and Marsh Infilling (including wave edge erosion) +
W
See the WRF-Hydro Technical Description https://ral.ucar.edu/projects/wrf_hydro/technical-description-user-guide
"First the 1-dimensional (1D) column land surface model calculates the vertical fluxes of energy (sensible and latent heat, net radiation) and moisture (canopy interception, infiltration, infiltration-excess, deep percolation) and soil thermal and moisture states. Infiltration excess, ponded water depth and soil moisture are subsequently disaggregated from the 1D LSM grid, typically of 1–4 km spatial resolution, to a highresolution, typically 30–100 m, routing grid using a time-step weighted method (Gochis and Chen, 2003) and are passed to the subsurface and overland flow terrain-routing modules. In typical U.S. applications, land cover classifications for the 1D LSMs are provided by the USGS 24-type Land Use Land Cover product or MODIS Modified IGBP 20-category land cover product (see WRF/WPS documentation); soil classifications are provided by the 1-km STATSGO database (Miller and White, 1998); and soil hydraulic parameters that are mapped to the STATSGO soil classes are specified by the soil analysis of Cosby et al. 20 (1984). Other land cover and soil type classification datasets can be used with WRF-Hydro but users are responsible for mapping those categories back to the same categories as used in the USGS or MODIS land cover and STATSGO soil type datasets. The WRF model pre-processing system (WPS) also provides a fairly comprehensive database of land surface data that can be used to set up the Noah and Noah-MP land surface models. It is possible to use other land cover and soils datasets.
Then subsurface lateral flow in WRF-Hydro is calculated prior to the routing of overland flow to allow exfiltration from fully saturated grid cells to be added to the infiltration excess calculated by the LSM. The method used to calculate the lateral flux of the saturated portion of the soil column is that of Wigmosta et al. (1994) and Wigmosta and Lettenmaier (1999), implemented in the Distributed Hydrology Soil Vegetation Model (DHSVM). It calculates a quasi-3D flow, which includes the effects of topography,
saturated soil depth, and depth-varying saturated hydraulic conductivity values. Hydraulic gradients are approximated as the slope of the water table between adjacent grid cells in either the steepest descent or in both x- and y-directions. The flux of water from one cell to its down-gradient neighbor on each timestep is approximated as a steady-state solution. The subsurface flux occurs on the coarse grid of the LSM while overland flow occurs on the fine grid.
Next, WRF-Hydro calcuates the water table depth according to the depth of the top of the saturated soil layer that is nearest to the surface. Typically, a minimum of four soil layers are used in a 2-meter soil column used in WRF-Hydro but this is not a strict requirement. Additional discretization permits improved resolution of a time-varying water table height and users may vary the number and thickness of soil layers in the model namelist described in the Appendices A3, A4, and A5.
Then overland flow is defined. The fully unsteady, spatially explicit, diffusive wave formulation of Julien et al. (1995-CASC2D) with later modification by Ogden (1997) is the current option for representing overland flow, which is calculated when the depth of water on a model grid cell exceeds a specified retention depth. The diffusive wave equation accounts for backwater effects and allows for flow on adverse slopes (Ogden, 1997). As in Julien et al. (1995), the continuity equation for an overland flood wave is combined with the diffusive wave formulation of the momentum equation. Manning’s equation is used as the resistance formulation for momentum and requires specification of an overland flow roughness parameter. Values of the overland flow roughness coefficient used in WRF-Hydro were obtained from Vieux (2001) and were mapped to the existing land cover classifications provided by the USGS 24-type land-cover product of Loveland et al. (1995) and the MODIS 20-type land cover product, which are the same land cover classification datasets used in the 1D Noah/Noah-MP LSMs.
Additional modules have also been implemented to represent stream channel flow processes, lakes and reservoirs, and stream baseflow. In WRF-Hydro v5.0 inflow into the stream network and lake and reservoir objects is a one-way process. Overland flow reaching grid cells identified as ‘channel’ grid cells pass a portion of the surface water in excess of the local ponded water retention depth to the channel model. This current formulation implies that stream and lake inflow from the land surface is always positive to the stream or lake element. There currently are no channel or lake loss functions where water can move from channels or lakes back to the landscape. Channel flow in WRF-Hydro is represented by one of a few different user-selected methodologies described below. Water passing into and through lakes and reservoirs is routed using a simple level pool routing scheme. Baseflow to the stream network is represented using a conceptual catchment storage-discharge bucket model formulation (discussed below) which obtains “drainage” flow from the spatially-distributed landscape. Discharge from buckets is input directly into the stream using an empirically-derived storage-discharge relationship. If overland flow is active, the only water flowing into the buckets comes from soil drainage. This is because the 21 overland flow scheme will pass water directly to the channel model. If overland flow is switched off and channel routing is still active, then surface infiltration excess water from the land model is collected over the pre-defined catchment and passed into the bucket as well. Each of these process options are enabled through the specification of options in the model namelist file."
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M
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Soil infiltration, as calculated using the Green-Ampt equation. +
H
Soil production from to different lithologies; weathering and transport of discrete rock blocks; transport of soil using linear diffusion; boundary incision +
A
Spatiotemporal varying sediment availability through simulation of the process of beach armoring.
A 1-D advection scheme.
Multifraction Erosion and Deposition.
Hydraulic Mixing, Infiltration, and Evaporation. +
P
A
B
C
Subsidence
Depth dependent carbonate production
Lithofacies spatial distribution based on number of neighoubrs of same facies type +
Subsidence and uplift
Eustatic oscillations
Water depth dependent in-situ carbonate production
Spatial variations in sediment production rate
Depth dependent sediment transport
Diffusional sediment transport +
T
TISC is a geodynamic numerical model combining computer modeling techniques to investigate the interplay between lithospheric-scale tectonics and erosion/sedimentation at the Earth's surface. TISC is a code that integrates the calculation of lithospheric flexure, kinematic fault deformation, and surface mass transport (erosion/transport/sedimentation) along drainage networks. In other words, TISC is a software that simulates the evolution of 3D large-scale sediment transport together with tectonic deformation and lithospheric isostatic movements on geological time scales. TISC stands for Tectonics, Isostasy, Surface transport, and Climate.
Take a look at the documentation wiki and download TISC at GitHub. TISC is available for Linux / OS X platforms only.
Download TISC from the github repository
See also the Open Forum.
The Landscape Evolution Model (LEM) component of TISC can deal with closed (internally-drained, endorheic) basins and finds the equilibrium between precipitation in drainage basins and evaporation in terminal lakes. Orographic precipitation is also calculated. Relative to other existing LEMs (Child, Cascade, Eros, ...), TISC explicitly handles lakes forming in local topographic minima, finding the outlet of such water bodies, and accounting for their role as hydrological and sedimentary sinks. It also accounts for internal drainage (endorheism) depending on the collected runoff and the lake's surface evaporation, explicitly calculating the extension of the resulting closed-drainage lakes. It also tracks sediment horizons in the sedimentary basins. TISC uses a fixed rectangular mesh for the finite-difference method. Water flow is at steady state.
Particular attention is given to the formation of sedimentary basins, with a full track of the source-to-sink balance between erosion and sedimentation. Further information in these papers (G-C, 2002, Basin Res., G-C et al., 2003) showing first results of this numerical model. +
TOPMODEL is defined as a variable contributing area conceptual model in which the dynamics of surface and subsurface saturated areas is estimated on the basis of storage discharge relationships established from a simplified steady state theory for downslope saturated zone flows. The theory assumes that the local hydraulic gradient is equal to the local surface slope and implies that all points with the same value of the topographic index, a/tan B will respond in a hydrologically similar way. This index is derived from the basin topography, where a is the drained area per unit contour length and tan B is the slope of the ground surface at the location. Thus the model need make calculations only for representative values of the index. The results may then be mapped back into space by knowledge of the pattern of the index derived from a topographic analysis. +
ThawLake1D Model couples a permafrost thermal model, a lake ice model and a subsidence model. It models heat conductio through a lake-permafrost system, evaluating temperature with depth. +
The Degree-Day method for modeling Snowmelt. +
The Energy Balance method for modeling snowmelt. +
The Energy Balance method of estimating losses due to evaporation. +
The Green-Ampt method for modeling infiltration. +
P
The Penn State Integrated Hydrologic Model (PIHM) is a fully coupled multiprocess hydrologic model. Instead of coupling through artificial boundary conditions, major hydrological processes are fully coupled by the semi-discrete finite volume approach. For those processes whose governing equations are partial differential equations (PDE), we first discretize in space via the finite volume method. This results in a system of ordinary differential equations (ODE) representing those procesess within the control volume. Within the same control volume, combining other processes whose governing equations are ODE’s, (e.g. the snow accumulation and melt process), a local ODE system is formed for the complete dynamics of the finite volume. +
Q
The QUAL2K framework includes the following new elements:
*Software Environment and Interface. Q2K is implemented within the Microsoft Windows environment. Numerical computations are programmed in Fortran 90. Excel is used as the graphical user interface. All interface operations are programmed in the Microsoft Office macro language: Visual Basic for Applications (VBA).
*Model segmentation. Q2E segments the system into river reaches comprised of equally spaced elements. Q2K also divides the system into reaches and elements. However, in contrast to Q2E, the element size for Q2K can vary from reach to reach. In addition, multiple loadings and withdrawals can be input to any element.
*Carbonaceous BOD speciation. Q2K uses two forms of carbonaceous BOD to represent organic carbon. These forms are a slowly oxidizing form (slow CBOD) and a rapidly oxidizing form (fast CBOD).
*Anoxia. Q2K accommodates anoxia by reducing oxidation reactions to zero at low oxygen levels. In addition, denitrification is modeled as a first-order reaction that becomes pronounced at low oxygen concentrations.
*Sediment-water interactions. Sediment-water fluxes of dissolved oxygen and nutrients can be simulated internally rather than being prescribed. That is, oxygen (SOD) and nutrient fluxes are simulated as a function of settling particulate organic matter, reactions within the sediments, and the concentrations of soluble forms in the overlying waters.
*Bottom algae. The model explicitly simulates attached bottom algae. These algae have variable stoichiometry.
*Light extinction. Light extinction is calculated as a function of algae, detritus and inorganic solids.
*pH. Both alkalinity and total inorganic carbon are simulated. The river’s pH is then computed based on these two quantities.
*Pathogens. A generic pathogen is simulated. Pathogen removal is determined as a function of temperature, light, and settling.
*Reach specific kinetic parameters. Q2K allows you to specify many of the *Weirs and waterfalls. The hydraulics of weirs as well as the effect of weirs and waterfalls on gas transfer are explicitly included.
T
The Richards 1D method for modeling infiltration. +
The Smith-Parlange 3-parameter method for modeling infilteration. +
The TopoToolbox 2 is a Matlab based software for Digital Elevation Model (DEM) analysis. It uses an object oriented programming (OOP) approach to represent and work with geoferenced raster data, flow directions, stream networks and swath profiles in Matlab. TopoToolbox offers a wide range of tools to analyse DEMs, flow and stream networks, that allow for interactive and automated workflows. +
M
The bed is represented by a 2-D matrix. At this time the bed is 250 x 250. Each block (i,j) is taken to be a slab of sediment 10cm x 10cm x 1cm deep.
A second matrix represents the flow. This is the same everywhere in the domain at each time point, except for a random spatial fluctuation representing turbulence.
The user-defined flow picks up (or puts down) sediment according to a transport law. Three transport laws have been tested: Bailard (1981), Ribberink (1998) or simple rules. The simple rules are simply thresholds: (if flow greater than 70cm/sec pick up one block).
Once sand block have been picked up, they are moved forward with the flow. Generally, I have used a fraction of the distance that the water would travel (jump_frac). So, with a flow of 100cm/sec, in one second that water goes 100 cm. The sand in this case would go 50 cm (half the distance). At the extremes, the model is sensitive to this parameter, but at intermediate values, it is not.
Tested flows have consisted of combined sinusoidal flow+steady flow, purely osc, purely steady, and natural flow time series taken from current meter measurements. All flows have a random spatial fluctuation added at each time point.
Once bedforms are generated, feedback rules are employed by altering the flow over the bedform. Once a bedform gets tall, the flow over the top accelerates, increasing transport at that location. In the steep lee of a bedform, a shadow zone forms where flow goes to ~zero, therefore transport goes to zero. These mechanisms destroy or build bedforms. +
P
The code models the evolution of a diffusive interface and the instabilities that arises when a less viscous fluid pushes a more viscous one in a confined rectangular geometry. +
T
The diffusive wave method for flow routing in the channels of a D8-based river network. +
The dynamic wave method for flow routing in the channels of a D8-based river network. +
C
The effects of individual storm events and SLR on shoreface evolution; dune dynamics, including dune growth, erosion, and migration; overwash deposition by individual storms; large-scale coastline evolution arising from alongshore sediment transport processes; and human management activities. +
The four primary components of our multi-physics code include geomechanical, hydrologic, solute transport and heat transfer modules. The geomechanical module calculates displacement of an elastic lithosphere disturbed by an ice sheet load. Transient geomechanical deformation is represented by one-dimensional (lateral) viscous asthenosphere flow. Our geomechanical module is partially coupled to the hydrologic module by providing the rate of change in the mean normal stress. Mean normal stress change rate is included as a source term in the groundwater flow equation driving flow. Flow is also influenced by changes in the top specified hydraulic head boundary condition. We implement two-way coupling between fluid flow, solute transport and heat transfer module via density and viscosity equations of state.
Three additional modules in our multi-physics code calculate changes to the upper hydraulic and thermal boundary conditions or alter the hydraulic transport properties (permeability) due to hydrogeomechanical failure. These include ice sheet evolution, permafrost, and failure analysis modules. Ice sheet thickness determines both the vertical load in the geomechanical module as well as the hydraulic head boundary condition at the land surface in the hydrologic module. In this study we adopted a simple parabolic polynomial equation to represent the idealized geometry of an ice sheet’s cross section in the ice sheet evolution module. We solved for permafrost
formation at and below the land surface using a suite of one-dimensional heat transfer models. We allowed for grid growth within the permafrost module to account for changes in ice sheet thickness. A failure analysis module was used to modify permeability due to hydromechanical failure. We adopted the effective Coulomb’s Failure Stress change criterion from Ge et al.(2009) to assess regions of failure during glaciations. +
M
The ground-water flow equation is solved using the finite-difference approximation. The flow region is subdivided into blocks in which the medium properties are assumed to be uniform. In plan view the blocks are made from a grid of mutually perpendicular lines that may be variably spaced. Model layers can have varying thickness. A flow equation is written for each block, called a cell. Several solvers are provided for solving the resulting matrix problem; the user can choose the best solver for the particular problem. Flow-rate and cumulative-volume balances from each type of inflow and outflow are computed for each time step. +
W
The integrated multi-processes include:
# hydrological cycles (evaporation, evapotranspiration, infiltration, and recharges);
# fluid flow (surface runoff in land surface, hydraulics and yydrodynamics in river/stream/canal networks;
# interflow in vadose zones, and groundwater flow in saturated zones);
# salinity transport and thermal transport (in surface waters and groundwater);
# sediment transport (in surface waters);
# water quality transport (any number of reactive constituents);
# biogeochemical cycles (nitrogen, phosphorous, carbon, oxygen, etc.); and
# biota kinetics (algae, phyotoplankton, zooplakton, caliform, bacteria, plants, etc.). +
C
The key processes are 1) topographically-driven overland flow and 2) bedload transport by this flow. Through these processes the model self-organizes channels which incise, back-fill, and avulse. Processes are similar to alluvial fans. There are no marine processes besides bedload dumping. +
T
The kinematic wave method for flow routing in the channels of a D8-based river network. +
R
The main source code calls sub-modules that simulate the following processes:
- Vegetation community colonization as a function of local water depth. Colonization is deterministic over some ranges and stochastic in others.
- Solution of flow field in two dimensions using a cellular automata algorithm (see Larsen and Harvey, 2010, Geomorphology, and Larsen and Harvey, 2010 in press, American Naturalist). The flow field is only simulated during high-flow events that entrain sediment.
- Sediment transport by flow according to an advection-dispersion equation. Within each high-flow pulse, steady conditions are assumed.
- Evolution of the topography through sediment transport, peat accretion (which is based on Larsen et al., Ecological Monographs, 2007), diffusive erosion of topographic gradients, vegetative propagation, and below-ground biomass expansion.
- Adjustment of water levels and high-flow discharge to satisfy a water balance and compensate for the growth of vegetation patches. +
F
The mean annual temperature of the warmest and coldest months at a given location gives a first-order estimate of distribution of permafrost. +
K
The model calculates changes in elevation and vegetation growth for a hypothetical salt marsh. In each cell, elevation change is calculated as the difference between accretion and erosion. Accretion rates are a function of inundation depth, vegetation growth, and suspended sediment concentration. Water routed according to Rinaldo et al. (1999) scheme. Erosion rates calculated according to excess sheer stress. Channels widen according to a diffusion-like routine where downslope transport is inversely proportional to vegetation. Vegetation grows according to Morris et al. (2002) where biomass is proportional to inundation depth up until an optimum depth. Episodic vegetation disturbance is simulated by removing vegetation from randomly selected cells (Kirwan et al., 2008). Another version of the model treats wave erosion in a simplistic manner (Kirwan and Murray, 2008). +
E
The model computes flow accumulation using multiple flow direction over unstructured grids based on + an adaptation of the implicit approach proposed by Richardson & Perron (Richardson, Hill, & Perron, 2014).
+ an extension of the parallel priority-flood depression-filling algorithm from (Barnes, 2016) to unstructured mesh is used to simulate sedimentation in upland areas and internally drained basins.
+ marine sedimentation is based on a diffusion algorithm similar to the technique proposed in pybadlands (Salles, Ding, & Brocard, 2018). +
H
The model consists of subroutines for meteorological interpolation, snow accumulation and melt, evapotranspiration estimation, a soil moisture accounting procedure, routines for runoff generation and finally, a simple routing procedure between subbasins and in lakes. It is possible to run the model separately for several subbasins and then add the contributions from all subbasins. Calibration as well as forecasts can be made for each subbasin. +
D
The model describes the tidal-network initiation and development, and the vertical accretion of the adjacent marsh platform. Tidal network development is driven by the exceedance of a local hydrodynamic bottom shear stress, controlled by water surface gradients. Marsh vertical growth is modeled by using a sediment balance equation acconting for erosion and deposition terms. The deposition terms account for sediment settling, trapping and organic production. +
F
The model is forced by tidal or other barotropic boundary conditions, wind, and/or fixed baroclinic pressure gradient, all acting at a single frequency (including zero) and specified by the user. +
E
The model predicts bankfull geometry of single-thread, sand-bed rivers from first principles, i.e. conservation of channel bed and floodplain sediment, which does not require the a-priori knowledge of the bankfull discharge. Building on previous work on the equilibrium of engineered rivers, i.e. rivers with fixed banks and sinuosity (Blom et al., 2016, 2017, Arkesteijn et al., 2019), as well as formulations for floodplain morphodynamics (Lauer & Parker, 2008, Viparelli et al., 2013, Lauer et al., 2016) and bank migration (Parker et al., 2011, Eke et al., 2014, Davidson & Eaton, 2018, De Rego et al., 2020), we derive equilibrium solutions for channel geometry (width, depth, slope), floodplain sediment size distribution, bankfull discharge, channel migration and overbank deposition rates.
References
Arkesteijn, L., Blom, A., Czapiga, M. J., Chavarrias, V. & Labeur, R. J. (2019). The quasi-equilibrium longitudinal profile in backwater reaches if the engineered alluvial river: A space-marching method, Journal of Geophysical Research: Earth Surface 124, 2542-2560.
Blom, A., Viparelli, E. & Chavarrias, V. (2016). The graded alluvial river: Profile concavity and downstream fining, Geophysical Research Letters 43 (12), 6285-6293.
Blom, A., Arkesteijn, L., Chavarrias, V. & Viparelli, E. (2017). The equilibrium alluvial river under variable flow and its channel-forming discharge, Journal of Geophysical Research: Earth Surface 122, 1924-1948.
Davidson, S.L. & Eaton, B. C. (2018). Beyond Regime: A stochastic model of floods, bank erosion, and channel migration. Water Resources Research, 54, 6282-6298.
De Rego, K., Lauer, J. W., Eaton, B. & Hassan, M. (2020). A decadal-scale numerical model for wandering, cobble-bedded rivers subject to disturbance, Earth Surface Processes and Landforms 45, 912-927.
Eke, E., Parker, G. & Shimizu, Y. (2014). Numerical modeling of erosional and depositional bank processes in migrating river bends with self-formed width: Morphodynamics of bar push and bank pull, Journal of Geophysical Research: Earth Surface 119, 1455-1483.
Lauer, J. W. & Parker, G. (2008). Modeling framework for sediment deposition, storage, and evacuation in the floodplain of a meandering river: Theory, Water Resources Research 44, W04425, doi: 10.1029/2006WR005528.
Lauer, J. W., Viparelli, E. & Piegay, H. (2016). Morphodynamics and sediment tracers in 1-D (MAST-1D): 1-D sediment transport that includes exchange with an off-channel sediment reservoir, Advances in Water Resources 93, 135-149.
Parker, G., Shimizu, Y., Wilkerson, G. V., Eke, E. C., Abad, J. D., Lauer, J. W., Paola, C., Dietrich, W. E. & Voller, V. R. (2011). A new framework for modeling the migration of meandering rivers, Earth Surface Processes and Landforms 36, 70-86.
Viparelli, E., Lauer, J. W., Belmont, P. & Parker, G. (2013). A numerical model to develop long-term sediment budgets using isotopic sediment fingerprints, Computers & Geosciences 53, 114-122.
T
The model represent the streamwise and vertical dispersal of a patch of tracer stones in an equilibrium gravel bed. +
S
The model simulates infiltration, fluid flow, and sediment transport. Fluid behavior is influenced by sediment concentration. +
M
The model simulates the lateral migration of a meandering rivers, allowing the formation of oxbow lakes and scroll bars which may have a different erosional resistance with respect to the pristine floodplain. +
P
The model simulates transport and deposition from the dense endmember of a pyroclastic density currents generated either by impulsive column collapse or sustained fountaining eruptions. +
1
The model solves both Gary Parker's three and four equation models for sediment mixtures. A condition was incorporated in the model to solve the equation of conservation of turbulent kinetic energy (fourth equation) and to decide how to estimate the friction coefficients. <br><br>See also: Eke, E., Viparelli, E., and Parker, G., 2011. Field-scale numerical modeling of breaching as a mechanism for generating continuous turbidity currents. Geosphere, 7, 1063-1076. Doi: 10.1130/GES00607.1 +
U
The model uses physically-based calculations of radiative, sensible, latent and advective heat exchanges. +
H
The module generates hillslope profiles by routing flow from every point on a drainage divide into a channel. +
C
The module performs topographic analysis but the analysis is based on the assumption that the stream power incision model is a good approximation for channel incision. +
F
The numerical model solves the two-dimensional shallow water equations with different modes of sediment transport. Moreover are presently implemented the Savage-Hutter type model describing avalanches of granular materials (not tested yet) and the equations governing the motion of two layers of immiscible fluid. +
R
The original process models include the following:
* The MTN-Clim model (Running et al, 1987) uses topography and user supplied base station information to derive spatially variable climate variables such as radiation and to extrapolate input climate variables over topographically varying terrain.
* An ecophysiological model is adapted from BIOME-BGC (Running and Coughlan, 1988; Running and Hunt, 1993) to estimate carbon, water and potentially nitrogen fluxes from different canopy cover types.
* Distributed hydrologic models – The original RHESSys utilized a single approach, TOPMODEL, to model soil moisture redistribution and runoff production. We now include two approaches:
** TOPMODEL (Beven and Kirkby, 1979) is a quasi distributed model. TOPMODEL distributes hillslope soil moisture based on a distribution of a topograhically defined wetness index.
** An explicit routing model is adapted from DHSVM (Wigmosta et al., 1994) which models saturated subsurface throughflow and overland flow via explicit connectivity. An important modification from the grid-based routing in DHSVM is the ability to route w ater between arbitrarily shaped surface elements. This allows greater flexibility in defining surface patches and varying shape and density of surface tesselation. +
F
The present version of FVCOM includes a number of options and components as shown in Figure above. These include:
# choice of Cartesian or spherical coordinate system,
# a mass-conservative wet/dry point treatment for the flooding/drying process simulation,
# the General Ocean Turbulent Model (GOTM) modules (Burchard et al., 1999; Burchard, 2002) for optional vertical turbulent mixing schemes,
# a water quality module to simulate dissolved oxygen and other environmental indicators,
# 4-D nudging and Reduced/Ensemble Kalman Filters (implemented in collaboration with P. Rizzoli at MIT) for data assimilation,
# fully-nonlinear ice models (implemented by F. Dupont),
# a 3-D sediment transport module (based on the U.S.G.S. national sediment transport model) for estuarine and near-shore applications, and
# a flexible biological module (FBM) for food web dynamics study.
FBM includes seven groups: nutrients, autotrophy, heterotrophy, detritus, dissolved organic matter, bacteria, and other. With various pre-built functions and parameters for these groups, GBM allows users to either select a pre-built biological model (such as NPZ, NPZD, etc.) or to build their own biological model using the pre-defined pool of biological variables and parameterization functions. +
P
The primary objectives are: (1) simulation of hydrologic processes including evaporation, transpiration, runoff, infiltration, and interflow as determined by the energy and water budgets of the plant canopy, snowpack, and soil zone on the basis of distributed climate information (temperature, precipitation, and solar radiation); (2) simulation of hydrologic water budgets at the watershed scale for temporal scales ranging from days to centuries; (3) integration of PRMS with other models used for
natural-resource management or with models from other scientific disciplines; and (4) providing a modular design that allows for selection of alternative hydrologic-process algorithms from the standard PRMS module library. +
C
D
The rainfall-excess components include soil-moisture accounting, pervious-area rainfall excess, impervious-area rainfall excess, and parameter optimization. The Green-Ampt equation is used in the calculations of infiltration and pervious area rainfall excess. A Rosenbrock optimization procedure may be used to aid in calibrating several of the infiltration and soil-moisture accounting parameters. Kinematic wave theory is used for both overland-flow and channel routing. There are three solution techniques available: method of characteristics, implicit finite difference method, and explicit finite difference method. Two soil types may be defined. Overland flow may be defined as turbulent or laminar. Detention reservoirs may be simulated as linear storage or using a modified-Puls method. Channel segments may be defined as gutter, pipe, triangular cross section, or by explicitly specifying the kinematic channel parameters alpha and m. +
T
The two key elements of TUGS model are a surface-based bedload transport equation that allows for calculation of transport rate and grain size distribution of both gravel and sand (Wilcoco and Crowe 2003), and functions that link bedload grain size distributions with surface and subsurface grain size distributions (Hoey and Ferguson 1994; Toro-Escobar et al. 1996; Cui 2007a). +
G
This code will erode cells according to a shear stress and also deposit sediment based on the concentration of sediment in a modeled water column. Additionally it has a headcut that migrates upstream and as the headcut erodes it deposits sediment downstream that the model must erode. +
D
This component calculates the flux of soil on a hillslope according to a soil depth-dependent linear diffusion rule. +
This driver program solves the equations describing horizontal velocities in a buoyant, turbulent, plane jet issuing in a normal direction from a coast into a large volume of still fluid. Sedimentation under the jet is modelled using a hemipelagic rain formulation, bedload dumping, and downslope diffusion due to slides, slumps and turbidity currents. +
K
This model is designed to represent infiltration (Green-Ampt), rainfall interception, and runoff (kinematic wave). Hydraulic roughness is accounted for using a depth-dependent Manning-type flow resistance equation.
For details on the model equations and numerical solution, see the following references:
Rengers, F.K., McGuire, L.A., Kean, J.W., Staley, D.M. and Hobley, D.E.J., 2016.
Model simulations of flood and debris flow timing in steep catchments after wildfire.
Water Resources Research, 52(8), pp.6041-6061.
McGuire, L.A. and Youberg, A.M., 2019. Impacts of successive wildfire on soil hydraulic properties:
Implications for debris flow hazards and system resilience. Earth Surface Processes and Landforms,
44(11), pp.2236-2250. +
G
This tool is used to identify knickpoints using a drainage area threshold and a curvature threshold value +
S
This tool maps out local surface roughness based on the neighborhood distribution of surface normal vectors. As sediment transport processes in soil mantled landscapes tend to be diffusive, the emergence of bedrock drives an increase in surface roughness that is mapped out by this algorithm. +
D
This tool works under the assumption that the channels incise approximately based on the stream power law. It identifies the channel head as the upstream limit of fluvial incision based on the chi profile of the channel. +
P
Thus the model yields not only compressional wave speeds, but also shear wave speeds and compressional and shear wave attenuation coefficients. +
C
Tidal currents
Sea waves
Swell waves
Storm surges
Tidal dispersion transport
Along-wave transport
Downslope transport by currents, swell waves, breaking waves, and sea waves
Edge erosion
Marsh processes
Along-shore transport by radiation stresses +
M
Tide-averaged flow (by tidal dispersion)
Flow erosion (assuming quasi-static propagation)
Sediment deposition
Sediment transport
Soil diffusion (aka creep)
Organic sediment production
Vegetation effect on drag, settling velocity, soil creep
Sea level rise
v.20 also includes:
Wind waves (empirical function of speed, water depth, and fetch)
Edge erosion
Identification of impounded areas
Active pond deepening
Active pond expansion +
C
Time- and length-averaged sediment transport in shelf, shoreface and surf zone environments combined with morphodynamic-driven sediment flux through inlet, along ebb tide delta and with the bay or estuar. +
Q
Time-averaged sediment transport by long-range river transport based on discharge and gradient and on short range diffusive transport based on gradient and diffusion coefficients. Thresholds for slope and discharge can be set and act as a means to keep the flow from spreading over every adjacent grid cell allowing avulsion and bifurcation processes to be modeled. +
A
W
To simulate real weather and to do simulations with coarse resolutions, a minimum set of physics components is required, namely radiation, boundary layer and land-surface parameterization, convective parameterization, subgrid eddy diffusion, and microphysics. Since the model is developed for both research and operational groups, sophisticated physics schemes and simple physics schemes are needed in the model. The objectives of the WRF physics development are to implement a basic set of physics into the WRF model and to design a user friendly physics interface. Since the WRF model is targeted at resolutions of 1-10 km, some of physics schemes might not work properly in this high resolution (e.g. cumulus parameterization). However, at this early stage of model development, only existing physics schemes are implemented, and most of them are taken from current mesoscale and cloud models. In the future, new physics schemes designed for resolutions of 1-10 km should be developed and implemented. See http://www.mmm.ucar.edu/wrf/users/docs/wrf-phy.html#physics_scheme for more information +
S
D
Tool is used to regionalize a study area into zones with 'common physical characteristics' with the underlying aim of differentiating areas of influence of various physical processes. Regionalization attempts to aggregate spatial units or observations into clusters based on spatial continuity as well as attribute similarity.
Geometry metrics are derived from satellite data analysis and include a.o. island area, island aspect ratio, island fractal dimension, and surrounding channel metric, channel width, channel sinousity, number of outflow channels, convexity. +
C
Tracking of cosmogenic nuclides on surface and in fluvial system of a landslide dominated drainage basin +
G
C
L
G
Two-dimensional depth-averaged flows, particularly suitable for tsunami and storm surge modeling, and has also bee used for dam breaks and flooding of river valleys. +
N
Uses a non-local means filter image processing technique to perform filtering/smoothing of a DEM. +
Uses the Python NetCDF toolkit (see python-netcdf on apt) to pull the desired information out of NetCDF files generated from NEXRAD (WSR-88D) outputs +
C
Using energetics-based formulations for wave-driven sediment transport, we develop a robust methodology for estimating the morphodynamic evolution of a cross-shore sandy coastal profile. The wave-driven cross-shore
sediment flux depends on three components: two onshore-directed terms (wave asymmetry and wave streaming) and an offshore-directed slope term. The cross-shore sediment transport formulation defines a dynamic equilibrium profile and, by perturbing about this steady-state profile, we present an advection-diffusion formula for profile evolution. Morphodynamic Péclet analysis suggests that the shoreface is diffusionally dominated. Using this depth-dependent characteristic diffusivity timescale, we distinguish a morphodynamic depth of closure for a given time envelope. Even though wave-driven sediment transport can (and will) occur at deeper depths, the rate of morphologic bed changes in response to shoreline change becomes increasingly slow below this morphodynamic closure depth. +
D
Watershed erosion +
O
Wave generation, propagation, shoaling, diffraction, refraction, breaking. Nonlinear wave-wave and wave-current interaction. Surf and swash hydrodynamics. +
Q
We model sedimentation in a fluvio-deltaic system under base-level changes. Possible dynamics include: (1) river aggradation (i.e., a seawards migration of the alluvial-basement transition), (2) river degradation (i.e., a landwards migration of the alluvial-basement transition), (3) regression (i.e., a seawards migration of the shoreline), and (4) transgression (e.g., a landwards migration of the shoreline). +
B
Weathering and erosion of bedrock on a hillslope; vertical and horizontal displacement due to earthquakes. +
C
Wind waves are computed by wave action propagation, tidal current are computed with a quasi static approximation. Bottom shaer stress, computed from a combination ot the two, induces bottom erosion. Suspended sediment are advected / diffused by tidal current, and eventually sedimented back. A different erosional process are used where waves break on a vertical obstacle (the vertical scarp at the marsh boundary). Vegetation is computed as a function of the ground elevation respect to the mean tidal level. Vegetation change bottom erodability and the sediment trapping. +
S
Z
D
development of dune landscapes under the interaction between aeolian sand transport and vegetation growth and response +
drying/flooding, turbulence and large eddies, stratification, internal waves, density effects of salinity, temperature and sediment, free surface flow, wave-current interaction, wind forcing, precipitation and evaporation, sediment sorting, fluid mud, morphological change, biochemical reactions, algae modelling, nutrient cycling, atmosphere-water exchange, adsorption and desorption of substances, deposition and re-suspension of particles and adsorbed substances, bacterial , predation +
F
S
fluid flow (2D potential flow), clastic sediment transport and deposition, carbonate deposition and transport, evaporate deposition, sea level change and coastline movement +
T
G
global-scale forward models of landscape evolution, dual-lithology (coarse and fine) sediment routing and stratigraphic history forced with deforming plate tectonics, paleotopographies and paleoclimate reconstructions. +
I
ice stress balance, ice mass transport / free surface, ice thermal (cold- and enthalpy-based), dual continuum hydrology, SHAKTI hydrology, GlaDS hydrology, ice damage mechanics, transient (time-dependent projection), grounding line dynamics, glacial isostatic adjustment (GIA), solid earth elastic response, sea-level fingerprints, positive degree day (PDD), surface energy balance (snow densification and surface mass balance calculation with the GEMB model), basal melt parameterizations (PICO/PICOP), empirical scalar tertiary anisotropy regime (ESTAR), uncertainty quantification capabilities (Dakota) +
D
M
D
n/a +
R
C
S
B
quasi-normal flow (1D)
downstream and transverse sediment fluxes
mass conservation (Exner) +
S
sediment transport drive by turbulent/laminar flows +
A
G
W
see: Sagy Cohen, Albert J. Kettner, James P.M. Syvitski, Balazs M. Fekete, WBMsed, a distributed global-scale riverine sediment flux model: Model description and validation, Computers and Geosciences, ISSN 0098-3004, 10.1016/j.cageo.2011.08.011. +
X
short wave propagation, infragravity waves, shear waves, swash, overtopping, overwashing, breaching, longshore current, cross-shore current, suspended sediment transport, morphological changes, dune erosion +
H
snowmelt process, skin and canopy processes, soil processes, surface water and shallow groundwater processes, river routing +
S
surface plumes, hyperpycnal plumes, sediment slope failure that results in turbidity currents or debris flows, subsidence, compaction, sediment remobilization due to waves and currents, river avulsion +
T
tAo is an open-source software designed to model the interplay between lithosphere flexure and surface transport (erosion/sedimentation), particularly during the formation of orogens and foreland sedimentary basins (see details). This 2D (cross-section) numerical model calculates 1D lithospheric flexure with different rheologies, in combination with fault kinematics, other isostatic loads, and erosion/deposition. Erosion models include both constant-rate and climate-based approaches. The programs are developed in C for Linux platforms, graphic output is produced using GMT scripts, and standard PCs match the CPU and memory requirements. The software is available under a GPL license. +
M
Y
W
virtually all earth atmospheric processes +
M
water volume flux, water supply, reservoir operations +
W
F
