Search by property

This page provides a simple browsing interface for finding entities described by a property and a named value. Other available search interfaces include the page property search, and the ask query builder.

List of results

Model:CruAKTemp + (CRU-NCEP SNAP)
Model:PsHIC + (Calculate the hypsometric integral by HI … Calculate the hypsometric integral by HI = (Zbar-Zo)/(Zmax-Zo)where Zbar is the average elevation of the contributing area to a pixelZo is the local elevation (the elevation of a pixel)Zmax is the maximum elevation of a pixel contributing area.For more details read: 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, Journal of Geophysical Research, 113, F03027.rnal of Geophysical Research, 113, F03027.)
Model:CosmoLand + (Cosmogenic nuclide production decay with depth. Power-law distribution of landslide size. Calculates a fluvial storage reservoir.)
Model:MarshMorpho2D + (Creep coefficient for mud Creep coefficien … Creep coefficient for mudCreep coefficient for marsh peatTidal dispersion coefficientErosion coefficientCritical shear stress for vegetated areasCritical shear stress for unvegetated areasIncrease in τcr with depth below MLWSettling velocity in unvegetated areasSettling velocity in vegetated areasTidal rangeTidal periodExternal sediment supplyRate of relative sea level riseManning coefficient for unvegetated mudManning coefficient for vegetated areasMaximum organic accretion rateSediment dry bulk densityMorphological time stepSpatial resolutionv2.0 also includes:Time series of wind speed and directionEdge erodibilityFraction of eroded edge material that is oxidized (i.e., removed from the mass balance)Rate of pond deepeningRate of pond expansionElevation thresholds for pond formationon Elevation thresholds for pond formation)
Model:DLBRM + (Croley, T. E., II, and He, C. (2005). “Distributed-parameter large basin runoff model. I: Model development.” J. Hydrol. Eng., 10(3), 173–181.)
Model:BOM + (Current speed, temperature, salinity, sea surface elevation, wind speed, river fluxes. Based on Navier Stokes equations, Boussinesq approximation, terrain following coordinates (sigma))
Model:SETTLE + (Dietrich's equation)
Model:Avulsion + (Distribution of avulsion angles)
Model:Drainage Density + (Drainage density is calculated as the inverse of the minimum distance to channel averaged over all nodes in the Landlab domain.)
Model:SVELA + (Einstein's Method of partitioning grain and form friction)
Model:TauDEM + (Elevation, slope and contributing area related quantities)
Model:STORM + (Empirical functions from CERC, U.S. Army Corps of Engineers)
Model:WINDSEA + (Empirical functions from CERC, U.S. Army Corps of Engineers)
Model:TopoFlow-Infiltration-Richards 1D + (Equations Used by the 1D Richards' Equatio … Equations Used by the 1D Richards' Equation Method v = K * (1 - ψ_z) = Darcy's Law for vertical flow rate (m / s) v_z = J - θ_t = conservation of mass, with source/sink term J Θ_e = (θ - θ_r) / (θ_s - θ_r) = effective saturation or scaled water content (unitless) θ_r = θ_s ( abs(ψ_B) / 10000)^λ = residual water content (unitless) K = K_s * Θ_e^η/λ = hydraulic conductivity (m / s) (see Notes below) ψ = ψ_B (Θ_e^-c/λ - 1)^1/c - ψ_A = pressure head (meters) (see Notes below)These equations are used to compute the time evolution of 1D (vertical, subsurface) profiles for (1) soil moisture, θ, (2) pressure head, ψ, (3) hydraulic conductivity, K and (4) vertical flow rate, v. TopoFlow solves these equations separately to get time-evolving profiles for every grid cell in a DEM. The result is a 3D grid for each of these four variables that spans the unsaturated zone. The third equation above just defines a variable that is used in the 4th and 5th equations, so the coupled set constitutes 4 equations to be solved for 4 unknowns. These equations can be combined into one nonlinear, parabolic, second-order PDE (partial differential equation) known as the one-dimensional Richards' equation.as the one-dimensional Richards' equation.)
Model:TopoFlow-Snowmelt-Degree-Day + (Equations Used by the Degree-Day Method … Equations Used by the Degree-Day Method M = (c_0 / 86400) * (T_air - T_0) = meltrate (mm / sec) M_max = (1000 * h_snow / dt) * (ρ_water / ρ_snow) = max possible meltrate (mm / sec) dh_snow = M * (ρ_water / ρ_snow) * dt = change in snow depth (m)/ ρ_snow) * dt = change in snow depth (m))
Model:TopoFlow-Snowmelt-Energy Balance + (Equations Used by the Energy-Balance Metho … Equations Used by the Energy-Balance Method M = (1000 * Q_m) / (ρ_water * L_f) = meltrate (mm / sec) M_max = (1000 * h_snow / dt) * (ρ_water / ρ_snow) = max possible meltrate (mm / sec) dh_snow = M * (ρ_water / ρ_snow) * dt = change in snow depth (m) Q_m = Q_SW + Q_LW + Q_h + Q_e - Q_cc = energy flux used to melt snow (W / m^2) Q_h = ρ_air * c_air * D_h * (T_air - T_surf) = sensible heat flux (W / m^2) Q_e = ρ_air * L_v * D_e * (0.662 / p_0) * (e_air - e_surf) = latent heat flux (W / m^2) D_n = κ^2 * u_z / LN((z - h_snow) / z0_air)^2 = bulk exchange coefficient (neutrally stable conditions) (m / s) D_h = D_n / (1 + (10 * Ri)), (T_air > T_surf) = bulk exchange coefficient for heat (m / s) (stable) = D_n * (1 - (10 * Ri)), (Tair < Tsurf) = bulk exchange coefficient for heat (m / s) (unstable) D_e = D_h = bulk exchange coefficient for vapor (m / s) Ri = g * z * (T_air - T_surf) / (u_z^2 (T_air + 273.15)) = Richardson's number (unitless) Q_cc = (see note below) = cold content flux (W / m^2) E_cc(0) = h0_snow * ρ_snow * c_snow * (T_0 - T_snow) = initial cold content (J / m^2) (T0 = 0 now) e_air = e_sat(T_air) * RH = vapor pressure of air (mbar) e_surf = e_sat(T_surf) = vapor pressure at surface (mbar) e_sat = 6.11 * exp((17.3 * T) / (T + 237.3)) = saturation vapor pressure (mbar, not KPa), Brutsaert (1975)vapor pressure (mbar, not KPa), Brutsaert (1975))
Model:TopoFlow-Infiltration-Green-Ampt + (Equations Used by the Green-Ampt Method f … Equations Used by the Green-Ampt Method f_c = K_i + ((K_s - K_i) * (F + J) / F) = infiltrability (m / sec) (max infiltration rate) = K_s + (J / F) * (K_s - K_i) = infiltrability (m / sec) (max infiltration rate) J = G * (θ_s - θ_i) = a quantity used in previous equation (meters) v_0 = min((P + M), f_c) = infiltration rate at surface (mm / sec) (K_s < (P + M)) = (P + M) = infiltration rate at surface (mm / sec) (K_s > (P + M)) F = ∫ v_0(t) d_t, (from times 0 to t) = cumulative infiltration depth (meters) (vs. I' in Smith (2002)iltration depth (meters) (vs. I' in Smith (2002))
Model:TopoFlow-Infiltration-Smith-Parlange + (Equations Used by the Smith-Parlange 3-Par … Equations Used by the Smith-Parlange 3-Parameter Method f_c = K_s + γ * (K_s - K_i) / (exp(γ * F / J) - 1) = infiltrability (m / sec) (max infiltration rate) J = G * (θ_s - θ_i) = a quantity used in previous equation (meters) v_0 = min((P + M), f_c) = infiltration rate at surface (mm / sec) (K_s < (P + M)) = (P + M) = infiltration rate at surface (mm / sec) (K_s > (P + M)) F = ∫ v_0(t) dt, (from times 0 to t) = cumulative infiltration depth (meters) to t) = cumulative infiltration depth (meters))
Model:WACCM-EE + (Equations focused on are the radiative transfer equations, and equations governing haze microphysics)
Model:Caesar + (Flow depths calculated using version of ma … Flow depths calculated using version of mannings implemented across a cellular grid using a scanning algorithm.Sediment tranport using either Einstein or Wilcock and Crowe functionsSlope model using simple slab failure and psuedo USLE implementationDune model adaption of DECAL and Werner slab modelel adaption of DECAL and Werner slab model)
Model:IDA + (Flow direction: the direction to the immediately neighboring cell (N,NE,E,...) to which flow from a cell is directed. Drainage area: The size of the total number of cells that drain through a cell.)
Model:SINUOUS + (Flow modeling is based on the Ikeda, Parke … Flow modeling is based on the Ikeda, Parker, and Sawaii (1984) and Johannesson and Parker (1989) linearized flow models. See the model documentation and published papers documented therein. Floodplain sedimentation is modeled as described in the documentation and in Howard(1992, 1996). Backwater flow routing and bed sediment routing is based upon Gary Parker's ebook spreadsheet RTe-bookAgDegBW.xls:. See the program documentation for further details.program documentation for further details.)
Model:ParFlow + (Fully described in manual.)
Model:GLUDM + (Global population values is assumed to be the most important controlling factor on the area of a specific agricultural land use area.)
Model:Lake-Permafrost with Subsidence + (Heat conduction equations, lake ice growth-decay equations)

Model:Icepack + (Ice thickness and velocity, mass continuity, Stokes equations)

Model:CMFT + (In each cell and at each time step the following are computed: bottom elevation, above-ground vegetation, water level, wave height, tidal current velocity, bottom shear stress, and suspended sediment concentration.)
Model:Pllcart3d + (Incompressible Navier-Stokes equations coupled to a convective-diffusive equation to describe the concentration field of the particles.)
Model:Spbgc + (Incompressible flow equations: Navier-Stokes with or without Boussinesq approximation. Transport equation to describe the motion of particles (or Salanity or Temperature).)
Model:Gvg3Dp + (Incompressible flow equations: Navier-Stokes with Boussinesq approximations. Transport equation to describe the motion of particles (or Salanity or Temperature).)
Model:SISV + (Incompressible flow equations: Navier-Stokes with Boussinesq approximations. Transport equation to describe the motion of particles (or Salanity or Temperature).)
Model:HEBEM + (Infiltration capacity, water balance equation Hydraulic conductivity, 2-D Dupuit groundwater movement equation)
Model:OTIS + (Instream mass transport based on the Advection-Dispersion equation with additional terms to consider inflow, transient storage, and chemical transformation.)
Model:KWAVE + (Key parameters include soil hydraulic properties, parameters related to vegetation cover (needed to compute interception), and hydraulic roughness.)
Model:Kirwan marsh model + (Key parameters include the rate of sea lev … Key parameters include the rate of sea level rise, suspended sediment concentration, tidal range (which controls vegetation distribution), critical shear stress for sediment erosion, and the period of time that erosion takes place during each tidal cycle. Parameters controlling the growth pattern of vegetation can easily be modified.tern of vegetation can easily be modified.)
Model:WASH123D + (Key physical parameters are: # flows rive … Key physical parameters are:# flows rivers/stream/canal/open channel networks - 1D St Venant Equations for River Networks with kinematic, diffusive, and fully dynamic wave options,# flows in overland regime - 2D St Venant Equations with: kinematic, diffusive, and fully dynamic wave options,# flow in subsurface media - 3D Richard Equation for both vadose and saturated zones,# salinity, thermal, and sediment transport in river networks and overland regime - modified ddvection-dispersion equations with phenomenological approaches for erosion and deposition, and# water quality transport for all media - advection-dispersion-reaction equations with reaction-based mechanistic approaches to water quality modeling using a general paradigm.For details refer to Yeh et al., 2005 Technical Report on WASH123D et al., 2005 Technical Report on WASH123D)
Model:Sun fan-delta model + (Key physical parameters include sediment g … Key physical parameters include sediment grain size, sediment, density, water and sediment discharge, run time, the initial surface slope, the threshold sediment flux to propagate a new channel, and the allowed channel superelevation above the surrounding topography before avulsion. These parameters and the governing equations for the model are fully described in Limaye et al. (2023), Effect of standing water on formation of fan-shaped sedimentary deposits at Hypanis Valles, Mars, https://dx.doi.org/10.1029/2022GL102367s, https://dx.doi.org/10.1029/2022GL102367)
Model:CrevasseFlow + (Key physical parameters: *Q: water dischar … Key physical parameters:*Q: water discharge upstream crevasse splay;*Qcs: outflow discharge of crevasse splay;*Qabove: the water discharge above the bottom of crevasse splay; *rq: the discharge ratio of Qcs and Qabove;*hs: channel belt's super-elevation (the elevation of lowest point of channel bed);*Zcs: bottom elevation of crevasse splay;*Bcs: width of crevasse splay;*Hcs: flow depth of crevasse splay;*Vcs: flow velocity of crevasse splay;*jcs: slope of the outflow of crevasse splay;*Zcsb: bottom elevation of a crevasse splay whose flow slope is equal to the channel slope j;Key physical equations:*Zcs<=max(hs,Zcsb); *rq=(1.55-1.45*Fi)*Bcs/wc+0.16*(1-2*Fi), in which Fi is the Fraud number for flow in the trunk channel, wc is width of the trunk channel;*Hcs=(nc*Qcs/sqrt(jcs)/Bcs)^(3/5);*Vcs=Qcs/Hcs/Bcs;*dE=M*(Vcs^2-ucre^2)/ucre^2*dt, where M is M-coefficient for erosion rate for crevasse slpay, ucre is critical velocity for erosion, dt is time step;*dD=Sv*(1-Vcs^2/ucrd^2)*ws/0.6*dt, where Sv is volume sediment concentration, ucrd is critical velocity for deposition, ws is settling velocity of suspended load, dt is time step. velocity of suspended load, dt is time step.)
Model:GOLEM + (Key state variables include surface elevation, soil thickness, and discharge.)
Model:VIC + (Land Cover can subdivide each grid cell's … Land Cover can subdivide each grid cell's land cover into arbitrary number of "tiles", each corresponding to the fraction of the cell covered by that particular land cover (e.g. coniferous evergreen forest, grassland, etc.)geographic locations or configurations of land cover types are not considered; VIC lumps all patches of same cover type into 1 tileSnow ModelVIC considers snow in several forms: ground snow pack, snow in the vegetation canopy, and snow on top of lake ice. Main features:Ground snow pack is quasi 2-layer; the topmost portion of the pack is considered separately for solving energy balance at pack surfaceMeteorological Input DataCan use sub-daily met data (prcp, tair, wind) at intervals matching simulation time stepCan use daily met data (prcp, tmax, tmin, wind) for daily or sub-daily simulationsDisaggregates daily met data to sub-daily via Thornton & Running algorithm and others (computes incoming sw and lw rad, pressure, density, vp)VIC can consider spatial heterogeneity in precipitation, arising from either storm fronts/local convection or topographic heterogeneity. Here we consider the influence of storm fronts and local convective activity. This functionality is controlled by the DIST_PRCP option in the global parameter file. Main features:Can subdivide the grid cell into a time-varying wet fraction (where precipitation falls) and dry fraction (where no precipitation falls).The wet fraction depends on the intensity of the precipitation; the user can control this function.Fluxes and storages from the wet and dry fractions are averaged together (weighted by area fraction) to give grid-cell average for writing to output files.Elevation BandsVIC can consider spatial heterogeneity in precipitation, arising from either storm fronts/local convection or topographic heterogeneity. Here we consider the influence of topography, via elevation bands. This is primarily used to produce more accurate estimates of mountain snow pack. This functionality is controlled by the SNOW_BAND option in the global parameter file. Main features:Can subdivide the grid cell into arbitrary number of elevation bands, to account for variation of topography within cellWithin each band, meteorologic forcings are lapsed from grid cell average elevation to band's elevationGeographic locations or configurations of elevation bands are not considered; VIC lumps all areas of same elevation range into 1 bandFluxes and storages from the bands are averaged together (weighted by area fraction) to give grid-cell average for writing to output filesHowever, the band-specific values of some variables can be written separately in the output filesLiang et al. (1999): set QUICK_FLUX to TRUE in global parameter file; this is the default for FULL_ENERGY = TRUE and FROZEN_SOIL = FALSE.Cherkauer et al. (1999): set QUICK_FLUX to FALSE in global parameter file; this is the default for FROZEN_SOIL = TRUE.By default, the finite difference formulation is an explicit method.By default, the nodes of the finite difference formulation are spaced linearly.These apply to the case QUICK_FLUX = FALSE and FROZEN_SOIL = TRUE, i.e. the formulation of Cherkauer et al. (1999).e. the formulation of Cherkauer et al. (1999).)
Model:LOGDIST + (Law of the Wall)
Model:RCPWAVE + (Linear nearshore wave transformation numer … Linear nearshore wave transformation numerical model for estimating wave transformation over an arbitrary bathymetry constrained to have mild bottom slopes. The model is based on the numerical solution of the parabolic approximation of the velocity potential of the forward scattered wave field.ntial of the forward scattered wave field.)
Model:Coastal Dune Model + (Linearized RANS for turbulent boundary layer over smooth terrain Shear stress partitioning model (work of Raupach et al 1993) Vegetation growth parameters (timescale, vegetation height, ratio of frontal to basal area))
Model:TopoFlow-Channels-Dynamic Wave + (Main equations used by this component: ΔV … Main equations used by this component: ΔV(i,t) = Δt * ( R(i,t) Δx Δy - Q(i,t) + Σ_k Q(k,t) ) = change in water volume (m^3) (mass cons.) d = {( w^2 + 4 tan(θ) V / L)^1/2 - w } / (2 tan(θ)) = mean water depth in channel segment (m) (if θ > 0) d = V / (w * L) = mean water depth in channel segment (m) (if θ = 0) Δv(i,t) = Δt * (T_1 + T_2 + T_3 + T_4 + T_5) / ( d(i,t) * A_w )= change in mean velocity (m / s) (mom. cons.) T_1 = v(i,t) * Q(i,t) * (C - 1) = efflux term in equation for Δv T_2 = Σ_k (v(k,t) - v(i,t) * C) * Q(k,t) = influx term in equation for Δv T_3 = -v(i,t) * C * R(i,t) * Δx * Δy = "new mass" momentum term in equation for Δv T_4 = A_w * (g * d(i,t) * S(i,t)) = gravity term in equation for Δv T_5 = -A_w * (f(i,t) * v(i,t)^2) = friction term in equation for Δv Q = v * A_w = discharge of water (m^3 / s) f(i,t) = ( κ / LN ( a * d(i,t) / z_0) )^2 = friction factor (unitless) (for law of the wall) f(i,t) = g * n^2 / Rh(i,t)^1/3 = friction factor (unitless) (for Manning's equation) C = A_w / A_t = area ratio appearing in equation for Δv A_t = w_t * L = top surface area of a channel segment (m2) (L = length) w_t = w + ( 2 * d * tan(θ) ) = top width of a wetted trapezoidal cross-section (m) R_h = A_w / P_w = hydraulic radius (m) A_w = d * (w + (d * tan(θ))) = wetted cross-sectional area of a trapezoid (m2) P_w = w + (2 * d / cos(θ)) = wetted perimeter of a trapezoid (m) V_w = d^2 * ( L * tan(θ) ) + d * (L * w) = wetted volume of a trapezoidal channel (m)(Source: TopoFlow HTML Help System)nnel (m) (Source: TopoFlow HTML Help System))
Model:TopoFlow-Evaporation-Energy Balance + (Main equations used by this component: ET … Main equations used by this component: ET = (1000 * Q_et) / (ρ_water * L_v) = evaporation rate (mm / sec) Q_et = (Q_SW + Q_LW + Q_c + Q_h) = energy flux used to evaporate water (W / m^2) Q_c = K_soil * (T_soil_x - T_surf) * (100 / x)= conduction energy flux (W / m^2) (between surf. and subsurf.) Q_h = ρ_air * c_air * D_h * (T_air - T_surf) = sensible heat flux (W / m^2) D_n = u_z * κ^2 / LN((z - h_snow) / z0_air)^2 = bulk exchange coeff. (neutrally stable conditions) (m / s) D_h = D_n / (1 + (10 * Ri)), (T_air > T_surf) = bulk exchange coeff. for heat (m / s) (stable) = D_n * (1 - (10 * Ri)), (T_air < T_surf) = bulk exchange coeff. for heat (m / s) (unstable) Ri = g * z * (T_air - T_surf) / (u_z^2 (T_air + 273.15)) = Richardson's number (unitless)air + 273.15)) = Richardson's number (unitless))
Model:TopoFlow-Channels-Diffusive Wave + (Main equations used by this component: ΔV … Main equations used by this component: ΔV(i,t)= Δt * ( R(i,t) Δx Δy - Q(i,t) + Σk Q(k,t) ) = change in water volume (m^3), mass conservation d = {( w^2 + 4 tan(θ) V / L)^1/2 - w } / (2 tan(θ)) = mean water depth in channel segment (m) (if θ > 0) d = V / (w * L) = mean water depth in channel segment (m) (if θ = 0) Q = v * Aw = discharge of water (m^3 / s) v = n^(-1) * Rh^(2/3) * S^(1/2) = section-averaged velocity (m / s), Manning's formula v = ( g * Rh * S)^(1/2) * LN( a * d / z0) / κ = section-averaged velocity (m / s), Law of the Wall Rh = Aw / Pw = hydraulic radius (m) Aw = d * (w + (d * tan(θ))) = wetted cross-sectional area of a trapezoid (m^2) Pw = w + (2 * d / cos(θ)) = wetted perimeter of a trapezoid (m) Vw = d^2 * ( L * tan(θ) ) + d * (L * w) = wetted volume of a trapezoidal channel (m)(Source: TopoFlow HTML Help System)nnel (m) (Source: TopoFlow HTML Help System))
Model:TopoFlow-Evaporation-Priestley Taylor + (Main equations used by this component: ET … Main equations used by this component: ET = (1000 * Q_et) / (ρ_water * L_v) = evaporation rate (mm / sec) Q_et = α * (0.406 + (0.011 * T_air)) * (Q_SW + Q_LW - Q_c) = energy flux used to evaporate water (W / m^2) Q_c = K_soil * (T_soil_x - T_surf) * (100 / x) = conduction energy flux (W / m^2)0 / x) = conduction energy flux (W / m^2))
Model:TopoFlow-Channels-Kinematic Wave + (Main equations used by this component: ΔV … Main equations used by this component: ΔV(i,t) = Δt * ( R(i,t) Δx Δy - Q(i,t) + Σ_k Q(k,t) ) = change in water volume (m^3), mass conservation d = {( w^2 + 4 tan(θ) V / L)^1/2 - w } / (2 tan(θ)) = mean water depth in channel segment (m) (if θ > 0) d = V / (w * L) = mean water depth in channel segment (m) (if θ = 0) Q = v * A_w = discharge of water (m3 / s) v = n^-1 * R_h^2/3 * S^1/2 = section-averaged velocity (m / s), Manning's formula v = ( g * Rh * S)^1/2 * LN( a * d / z_0) / κ = section-averaged velocity (m / s), Law of the Wall R_h = A_w / P_w = hydraulic radius (m) A_w = d * (w + (d * tan(θ))) = wetted cross-sectional area of a trapezoid (m2) P_w = w + (2 * d / cos(θ)) = wetted perimeter of a trapezoid (m) V_w = d^2 * ( L * tan(θ) ) + d * (L * w) = wetted volume of a trapezoidal channel (m) = wetted volume of a trapezoidal channel (m))
Model:Marsh column model + (Many, see Mudd et al. (2009) ECSS v 82(3) 377-389)
Model:Equilibrium Calculator + (Model governing equations express the cons … Model governing equations express the conservation of sand and mud in the floodplain and in the channel. Water depth and shear stress are computed with a Chezy formulation for a composite rectangular cross section. Total ((bedload plus suspended load) sand transport capacity is computed with an Engelund and Hansen-type of bulk load relation (see Parker, 2004). The mean annual sand load is determined by averaging the sand transport capacities over the flow duration curve. Channel migration rate is computed as in Eke et al. (2014). Overbank deposition rates are computed with the approach presented in Parker et al. (1996). ReferencesEke, 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.Parker, G. (2004). 1D sediment transport morphodynamics with applications to rivers and turbidity currents e-book available at http://hydrolab.illinois.edu/people/parkerg/morphodynamics_e-book.htm .Parker, G., Cui, Y., Imran, J. & Dietrich, W. E. (1996). Flooding in the lower Ok Tedi, Papua New Guinea due to the disposal of mine tailings and it’s amelioration, International Seminar on Recent trends of floods and their preventive measures, 20-21 June, Sapporo, Japan.r preventive measures, 20-21 June, Sapporo, Japan.)
Model:FVshock + (Momentum and continuity differential equations are solved for each layer. Closure equations are solved for bed-load discharge and entrainment/deposition.)