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A list of all pages that have property "Describe key physical parameters" with value "Einstein's Method of partitioning grain and form friction". Since there have been only a few results, also nearby values are displayed.

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List of results

  • Model:MizuRoute  + (---)
  • Model:MCPM  + (-Creep simulated as a linear diffusion process, with vegetation dependent diffusivity -Suspended sediment concentration variable in time and space throughout the cross section)
  • Model:SiStER  + (1) Conservation of mass and momentum 2) Non linear viscosity law + elasticity + plasticity 3) Conservation of energy)
  • Model:Subside  + (1D and 2D flexure equations)
  • Model:LONGPRO  + (1D channel flow: See Henderson (1966, p. 143), Total sediment transport: See Yang's (1973); mass conservation: See Slingerland (1986); Settling velocity: See Dietrich's equation)
  • Model:Plume  + (2D advection-diffusion equation)
  • 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))
  • Model:TopoFlow-Snowmelt-Energy Balance  + (Equations Used by the Energy-Balance Metho … Equations Used by the Energy-Balance Method</br></br> M = (1000 * Q_m) / (ρ_water * L_f) = 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)</br> Q_m = Q_SW + Q_LW + Q_h + Q_e - Q_cc = energy flux used to melt snow (W / m^2)</br> Q_h = ρ_air * c_air * D_h * (T_air - T_surf) = sensible heat flux (W / m^2)</br> Q_e = ρ_air * L_v * D_e * (0.662 / p_0) * (e_air - e_surf) = latent heat flux (W / m^2)</br> D_n = κ^2 * u_z / LN((z - h_snow) / z0_air)^2 = bulk exchange coefficient (neutrally stable conditions) (m / s)</br> D_h = D_n / (1 + (10 * Ri)), (T_air > T_surf) = bulk exchange coefficient for heat (m / s) (stable)</br> = D_n * (1 - (10 * Ri)), (Tair < Tsurf) = bulk exchange coefficient for heat (m / s) (unstable)</br> D_e = D_h = bulk exchange coefficient for vapor (m / s)</br> Ri = g * z * (T_air - T_surf) / (u_z^2 (T_air + 273.15)) = Richardson's number (unitless)</br> Q_cc = (see note below) = cold content flux (W / m^2)</br> E_cc(0) = h0_snow * ρ_snow * c_snow * (T_0 - T_snow) = initial cold content (J / m^2) (T0 = 0 now)</br> e_air = e_sat(T_air) * RH = vapor pressure of air (mbar)</br> e_surf = e_sat(T_surf) = vapor pressure at surface (mbar)</br> 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</br> f_c = K_i + ((K_s - K_i) * (F + J) / F) = infiltrability (m / sec) (max infiltration rate)</br> = K_s + (J / F) * (K_s - K_i) = infiltrability (m / sec) (max infiltration rate)</br> J = G * (θ_s - θ_i) = a quantity used in previous equation (meters)</br> v_0 = min((P + M), f_c) = infiltration rate at surface (mm / sec) (K_s < (P + M))</br> = (P + M) = infiltration rate at surface (mm / sec) (K_s > (P + M))</br> 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</br></br> f_c = K_s + γ * (K_s - K_i) / (exp(γ * F / J) - 1) = infiltrability (m / sec) (max infiltration rate)</br> J = G * (θ_s - θ_i) = a quantity used in previous equation (meters)</br> v_0 = min((P + M), f_c) = infiltration rate at surface (mm / sec) (K_s < (P + M))</br> = (P + M) = infiltration rate at surface (mm / sec) (K_s > (P + M))</br> 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.</br>Sediment tranport using either Einstein or Wilcock and Crowe functions</br>Slope model using simple slab failure and psuedo USLE implementation</br>Dune 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.)
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