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A list of all pages that have property "Describe key physical parameters" with value "2D advection-diffusion equation". Since there have been only a few results, also nearby values are displayed.

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List of results

  • Model:SIMSAFADIM  + (2D fluid flow potential, 2D dispersive/diffusive/advective transport, Lotka/Volterra polulation dynamics equations for carbonate producing organisms, deposition calculation based on equations of settling rates)
  • Model:WAVEREF  + (Airy wave theory)
  • Model:QDSSM  + (Basin digital elevation model.)
  • Model:CarboLOT  + (Bathymetry, seawater temperatures, ocean wave climate, benthic irradiance, seafloor hardness)
  • Model:MARSSIM  + (Bedrock erodibility, mass wasting diffusivity, bed material grain size, flow hydrologic parameters, relative evaporation rate, cratering size distribution and rate, eolian deposition parameters, etc.)
  • Model:GroundwaterDupuitPercolator  + (Boussinesq aquifer equation, Darcy's law.)
  • Model:GENESIS  + (Breaking wave conditions are estimated fro … Breaking wave conditions are estimated from input wave information using linear wave theory. Longshore sand transport rates are estimated using a modified version of the CERC equation and the equation governing shoreline change is formulated by conservation of sand volume.formulated by conservation of sand volume.)
  • Model:BEDLOAD  + (Bridge function, see Bridge and Dominic (1984) or Einstein's equation)
  • Model:Bing  + (Bulk density, viscosity, shear/yield strength)
  • Model:Shoreline  + (CERC formula for sediment transport rate (see Komar) Kamphuis formula for sediment transport rate. Conservation of sediment mass.)
  • Model:CruAKTemp  + (CRU-NCEP SNAP)
  • Model:PsHIC  + (Calculate the hypsometric integral by HI … Calculate the hypsometric integral by </br>HI = (Zbar-Zo)/(Zmax-Zo)</br>where Zbar is the average elevation of the contributing area to a pixel</br>Zo is the local elevation (the elevation of a pixel)</br>Zmax is the maximum elevation of a pixel contributing area.</br>For more details read: </br>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 mud</br>Creep coefficient for marsh peat</br>Tidal dispersion coefficient</br>Erosion coefficient</br>Critical shear stress for vegetated areas</br>Critical shear stress for unvegetated areas</br>Increase in τcr with depth below MLW</br>Settling velocity in unvegetated areas</br>Settling velocity in vegetated areas</br>Tidal range</br>Tidal period</br>External sediment supply</br>Rate of relative sea level rise</br>Manning coefficient for unvegetated mud</br>Manning coefficient for vegetated areas</br>Maximum organic accretion rate</br>Sediment dry bulk density</br>Morphological time step</br>Spatial resolution</br></br>v2.0 also includes:</br></br>Time series of wind speed and direction</br>Edge erodibility</br>Fraction of eroded edge material that is oxidized (i.e., removed from the mass balance)</br>Rate of pond deepening</br>Rate of pond expansion</br>Elevation 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</br> v = K * (1 - ψ_z) = Darcy's Law for vertical flow rate (m / s)</br> v_z = J - θ_t = conservation of mass, with source/sink term J</br> Θ_e = (θ - θ_r) / (θ_s - θ_r) = effective saturation or scaled water content (unitless)</br> θ_r = θ_s ( abs(ψ_B) / 10000)^λ = residual water content (unitless)</br> K = K_s * Θ_e^η/λ = hydraulic conductivity (m / s) (see Notes below)</br> ψ = ψ_B (Θ_e^-c/λ - 1)^1/c - ψ_A = pressure head (meters) (see Notes below)</br>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</br></br> M = (c_0 / 86400) * (T_air - T_0) = meltrate (mm / sec)</br> M_max = (1000 * h_snow / dt) * (ρ_water / ρ_snow) = max possible meltrate (mm / sec)</br> dh_snow = M * (ρ_water / ρ_snow) * dt = change in snow depth (m)/ ρ_snow) * dt = change in snow depth (m))
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