Model help:Sedflux
Sedflux
SEDFLUX is a basin-fill model, written in ANSI-standard C, able to simulate the delivery of sediment and their accumulation over time scales of tens of thousands of years. It simulates the dynamics of strata formation of continental margins fuse information from the atmosphere, ocean and regional geology, and it can provide information for areas and times for which actual measurements are not available, or for when purely statistical estimates are not adequate by themselves.
Model introduction
Sedflux combines individual process-response models into one fully interactive model, delivering a multi-sized sediment load onto and across a continental margin. The model allows for the deposit to compact, to undergo tectonic processes and isostatic subsidence from the sediment load. The new version, Sedflux 2.0 introduces a series of new process models, and is able to operate in one of two models to track the evolution of stratigraphy in either 2D or 3D. Additions to the 2D mode include the addition of models that simulate (1) erosion and deposition of sediment along a riverbed, (2) cross-shore transport due to ocean waves, and (3) turbidity currents and hyperpycnal flows. New processes in the 3D mode include (1) river channel avulsion, (2) two-dimensional diffusion due to ocean storms, and (3) two-dimensional flexure due to sediment loading. The spatial resolution of the architecture is typically 1–25 cm in the vertical and 10–100 m in the horizontal when operating in 2D mode. In 3D mode, the horizontal resolution usually extends to kilometers. In addition to fixed time steps (from days to hundreds of years), Sedflux 2.0 offers event-based time stepping as a way to conduct long-term simulations while still modeling low-frequency but high-energy events.
Model parameters
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Main equations
- River dynamics (using HydroTrend model)
1) Water discharge
[math]\displaystyle{ Q_{0}=u_{0}b_{0}h_{0} }[/math] (1)
2) Mean suspended load entering the ocean basin
[math]\displaystyle{ Q_{s0}= Q_{0} \sum\limits_{i=1}^N Cs_{i} }[/math] (2)
3) Bedload equation by Bagnold (1966)
[math]\displaystyle{ Q_{b}={\frac{\rho _{s}}{\rho _{s} - \rho}}{\frac{\rho g Q_{0}^ \beta s e_{b}}{g tan f}} }[/math] (3)
- Channel avulsion (using Avulsion model)
[math]\displaystyle{ \Theta _{n+1}=\Theta_{n} + X_{n} }[/math] (4)
- Bedload dumping (not hyperpycnal flow)
[math]\displaystyle{ D={\frac{Q_{b}}{W_{d}L \rho}} }[/math] (5)
- River plumes
1) Advection-diffusion equation
[math]\displaystyle{ {\frac{\partial u I}{\partial x}} + {\frac{\partial v I}{\partial y}} + \lambda I = {\frac{\partial}{\partial y}} \left ( K {\frac{\partial I}{\partial y}}\right ) + {\frac{\partial}{\partial x}} \left (K {\frac{\partial I}{\partial x}}\right ) }[/math] (6)
2) Froude number
[math]\displaystyle{ Fr = {\frac{u_{0}}{\sqrt{g h_{0}}}} }[/math] (7)
3) Plume's centerline
[math]\displaystyle{ {\frac{x}{b_{0}}}=1.53 + 0.90 \left ({\frac{u_{0}}{v_{0}}}\right ) \left ({\frac{y}{b_{0}}}\right )^\left (0.37\right ) }[/math] (8)
4) Non-conservative concentration along and surrounding the centerline position
[math]\displaystyle{ C\left (x,y\right ) = C_{0}exp\left (-\lambda t \right ) \sqrt{{\frac{b_{0}}{\sqrt{\pi}C_{1} x}}} exp [-\left ({\frac{y}{\sqrt{2} C_{1} x}}\right )^2] }[/math] (9)
[math]\displaystyle{ t\left (x,y\right ) = {\frac{u_{0} + u_{c}\left (x\right ) + 7u\left (x,y\right )}{9}} }[/math] (10)
[math]\displaystyle{ u_{c}\left (x\right ) = u_{0} \sqrt{{\frac{b_{0}}{\sqrt{\pi} C_{1} x}}} }[/math] (11)
[math]\displaystyle{ u\left (x,y\right ) = u_{0} \sqrt{{\frac{b_{0}}{\sqrt{\pi} C_{1} x }}} exp [-\left ({\frac{y}{\sqrt{2} C_{1} x}}\right )^2] }[/math] (12)
- Diffusion of seafloor sediments
1) Amount of bottom sediments that can be reworked by resuspension and diffusion
[math]\displaystyle{ q_{s} = k\left (t,z,D\right ) \bigtriangledown z = k \left ( {\frac{\partial z}{\partial x}}\hat{i} + {\frac{\partial z}{\partial y}} \hat{j} \right ) }[/math] (13)
2) Amount and direction of transport of the ith grain size
[math]\displaystyle{ q_{si} = \beta _{i} q_{s} }[/math] (14)
- Sediment failure
1) Stability of a possible failure plane
[math]\displaystyle{ F_{total} = {\frac{ \sum\limits_{i=0}^N[b_{i}\left ( c_{i} + \left ( {\frac{W_{i}}{b_{i}}} - u_{i} \right ) tan \phi _{i} \right ) {\frac{sec \alpha _{i}}{1 + {\frac{tan \alpha _{i} tan \phi _{i}}{F_{total}}}}}]}{\sum\limits_{i=0}^N W_{i} sin \alpha _{i}}} }[/math] (15)
2) excess pore pressure using Gibson's graphical approximation (1958)
[math]\displaystyle{ u_{i} = {\frac{\gamma' z_{i}}{a_{i}}} }[/math] (16)
[math]\displaystyle{ a \equiv 6.4 \left ( 1 - {\frac{T}{16}} \right )^\left (17\right ) + 1 }[/math] (17)
[math]\displaystyle{ T \equiv {\frac{m^2 t}{c_{v}}} }[/math] (18)
- River mouth turbidity currents
[math]\displaystyle{ {\frac{\partial u}{\partial t}} = g_{0} sin \alpha C - {\frac{E + C_{d}}{h}}u^2 - g_{0} \left ({\frac{e^C - 1}{e - 1}}\right ) cos \alpha C tan \gamma }[/math] (19)
[math]\displaystyle{ C = \sum\limits_{i=1}^N C_{i} = {\frac{\rho _{f} - \rho}{\rho _{s} - \rho}} }[/math] (20)
Fluid continuity equation 1) one dimensional steady-state turbidity current model INFLO
[math]\displaystyle{ {\frac{\partial Q}{\partial x}} = E u W }[/math] (21)
Continuity equation for the ith grain size of the flow's suspeneded load
[math]\displaystyle{ {\frac{\partial J_{i}}{\partial x}} = E_{Ri} - D_{Ri} }[/math] (22)
The rate of erosion of the ith grain size of the seafloor by the current
[math]\displaystyle{ E_{R} = \left ({\frac{C_{D} \rho _{f} u^2 - \delta _{b}}{\delta _{a}}} \right ) {\frac{\varphi _{i} W}{day}} }[/math] (23)
Rate of deposition of the ith grain size in the flow
[math]\displaystyle{ D_{Ri} = \left\{\begin{matrix} 0 & if u \gt u_{cr} \\ {\frac{\lambda _{i} J_{i}}{u}} \left ( 1 - {\frac{u^2}{u_{cr}^2}}\right ) & if u \lt = u_{cr} \end{matrix}\right. }[/math] (24)
Critical velocity for deposition
[math]\displaystyle{ u_{cr} = {\frac{w_{s}}{\sqrt{C_{D}}}} }[/math] (25)
2) turbidity current model Sakura Governing equation
[math]\displaystyle{ {\frac{\partial h}{\partial t}} + {\frac{\partial}{\partial x}} \left (u h_{f} \right ) = E_{w} u }[/math] (26)
[math]\displaystyle{ {\frac{\partial}{\partial t}} \left (u h_{f} \right ) + {\frac{\partial}{\partial x}}\left (u^2 h_{f}\right ) = -{\frac{\left ( \rho _{s} - \rho _{w} \right ) g}{2 \rho_{w}}}{\frac{\partial}{\partial x}} \left (Ch_{f}^2 \right ) + {\frac{\left (\rho _{s} - \rho _{w} \right ) g h_{f} C S}{\rho_{w}}} - C_{d} \left ( 1 + \alpha \right ) u^2 }[/math] (27)
[math]\displaystyle{ {\frac{\partial}{\partial t}} \left ( Ch_{f} \right ) + {\frac{\partial}{\partial x}}\left ( u Ch_{f}\right ) = - F_{d} + F }[/math] (28)
[math]\displaystyle{ E_{w} = {\frac{0.00153}{0.0204 + Ri}} }[/math] (29)
[math]\displaystyle{ Ri = {\frac{\left (\rho_{s} - \rho_{w}\right ) g h_{f}C}{\rho_{w}u^2}} }[/math] (30)
[math]\displaystyle{ F_{d} = \left\{\begin{matrix} w_{s} C \left (2 - 1/p_{z} \right ) & p_{z} \lt 0.5 // 0 & p_{z} \gt = 0.5 \end{matrix}\right. }[/math] (31)
[math]\displaystyle{ F_{e} = \left ( \left (C_{d} \rho_{f} u^2 - b \right ) / \left ( a 86400 \right ) \right ) }[/math] (32)
[math]\displaystyle{ |log p_{z}|^\left (1/4 \right ) \cong 0.124 log_{2} Z_{0} + 1.2 }[/math] (33)
[math]\displaystyle{ Z_{0} \equiv w_{s}/ \left (\kappa u_{*} \right ) }[/math] (34)
- Debris flows
1) Depth-averaged debris flow equations (Continuity)
[math]\displaystyle{ {\frac{\partial D}{\partial t}} + {\frac{\partial}{\partial x}} [U_{p}D_{p} + {\frac{2}{3}}U_{p}D_{s}] = 0 }[/math] (35)
2) Depth-averaged debris flow equations (Momentum (shear layer))
[math]\displaystyle{ {\frac{2}{3}} {\frac{\partial}{\partial t}} \left (U_{p}U_{s} \right ) - U_{p} {\frac{\partial D_{s}}{\partial t}} + {\frac{8}{15}}{\frac{\partial}{\partial x}} \left ( U_{p}^2 D_{s} \right ) {\frac{2}{3}} U_{p} {\frac{\partial}{\partial x}} \left (U_{p} D_{s} \right ) = D_{s} g \left ( 1 - {\frac{\rho_{w}}{\rho_{\rho_{m}}}}\right ) S - D_{s} g {\frac{\partial D}{\partial x}} - 2 {\frac{\mu U_{p}}{\rho_{m} D_{s}}} }[/math] (36)
3) Depth-averaged debris flow equations (Momentum (plug flow layer))
[math]\displaystyle{ {\frac{\partial}{\partial t}} \left ( U_{p} D_{p}\right ) + {\frac{\partial}{\partial x}} \left (U_{p}^2 D_{p} \right ) + U_{p}{\frac{\partial D_{s}}{\partial t}} + {\frac{2}{3}}U_{p}{\frac{\partial}{\partial x}} \left (U_{p} D_{s} \right ) = D_{p} g \left ( 1 - {\frac{\rho_{w}}{\rho_{m}}} \right ) S - D_{p} g {\frac{\partial D}{\partial x}} - {\frac{\tau_{y}}{\rho_{m}}} }[/math] (37)
- Subsidence
1) Isostatic subsidence
[math]\displaystyle{ w \left (x\right ) = {\frac{p\left (x\right ) \alpha ^3}{8D}}exp \left( -{\frac{|x|}{\alpha}}\right ) + sin \left ({\frac{|x|}{\alpha}}\right ) }[/math] (38)
[math]\displaystyle{ \alpha \equiv ^4 \sqrt{{\frac{4D}{\rho_{m}g}}} }[/math] (39)
[math]\displaystyle{ W \left (x\right ) = \sum\limits_{i=-\propto}^\left (\propto\right ) w \left ( x - x_{i} \right ) }[/math] (40)
- Compaction
[math]\displaystyle{ {\frac{\partial \phi}{\partial \delta}} = - c \left ( \phi - \phi_{0}\right ) }[/math] (41)
- Subaerial erosion and deposition by river
[math]\displaystyle{ {\frac{\partial \eta}{\partial t}} = \nu {\frac{\partial ^2 \eta}{\partial x^2}} }[/math] (42)
Diffusion coefficient
[math]\displaystyle{ \nu \equiv {\frac{-8 \lt q\gt A \sqrt{c_{f}}}{C_{0}\left ( s - 1 \right )}} }[/math] (43)
- Cross-shore transport due to ocean storms
1) Closure depth
[math]\displaystyle{ h_{c} = 2.28 H_{ss} - 6.85 \left ({\frac{H_{ss}^2}{g T^2}}\right ) }[/math] (44)
2) Sediment flux for the outer shelf (depth greater than h_{c})
[math]\displaystyle{ q_{s} = {\frac{16}{3\pi}}{\frac{\rho}{\rho_{s} - \rho}}{\frac{C_{fs}\varepsilon _{ss}}{g}}I_{s}{\frac{U_{om}^3}{w_{s}}}\left ( v_{0} + {\frac{U_{om}^2}{5 w_{s}}}{\frac{\partial h}{\partial x}}\right ) }[/math] (45)
3) Equation for shoaling waves
[math]\displaystyle{ U_{om} \left (h\right ) = {\frac{\gamma b}{2}} \sqrt{g b_{b}} \left ({\frac{h}{h_{b}}}\right )^\left ({\frac{-3}{4}}\right ) }[/math] (46)
4) Komar's (1998) equation for the threshold of sediment motion
[math]\displaystyle{ {\frac{\rho u_{t}^2}{\left ( \rho_{s} - \rho \right ) g d}} = \left\{\begin{matrix} 0.21 \left ({\frac{d_{0}}{d}}\right )^ \left ({\frac{1}{2}}\right ) & for D \lt = 0.5 mm \\ 0.46 \pi \left ({\frac{d_{0}}{d}}\right )^\left ({\frac{1}{4}}\right ) & for D \gt 0.5 mm \end{matrix}\right. }[/math] (47)
5) Near-bottom threshold velocity
[math]\displaystyle{ u_{t} = {\frac{\pi d_{0}}{T}} = {\frac{\pi H}{T sinh \left (2 \pi h / L \right )}} }[/math] (48)
6) Sediment flux within the near-shore zone (depth less than h_{c})
[math]\displaystyle{ q_{s} = k_{c} \underline{x}^ \left ( 1 - m \right ) {\frac{dh}{dx}} }[/math] (49)
- Flexure of the lithosphere
1) Deflection of Earth's crust
[math]\displaystyle{ w \left (\lambda r \right ) = {\frac{q \lambda}{2 \pi \rho_{d}g}} Kei \left (\lambda r \right ) }[/math] (50)
2) Flexural parameter
[math]\displaystyle{ \lambda = \left ({\frac{D}{\rho_{d}g}}\right )^ \left ({\frac{-1}{4}}\right ) }[/math] (51)
3) Time delay between the addition of load and the lithosphere's response
[math]\displaystyle{ w \left (t \right ) = w_{0} \left ( 1 - exp \left (- t / t_{0} \right ) \right ) }[/math] (52)
Symbol | Description | Unit |
---|---|---|
Q_{0} (in River dynamics) | water discharge from the river | L^{3} / T |
u_{0} (in River dynamics) | mean river mouth flow velocity | L / T |
b_{0} (in River dynamics) | channel width | L |
h_{0} (in River dynamics) | channel depth | L |
Q_{s0} (in River dynamics) | mean suspended suspended load leaving the river | M / L |
Cs_{i} (in River dynamics) | concentration of the ith grain size size | M / L^{3} |
Q_{b} (in River dynamics) | bedload flux from river mouth | M / T |
Q_{c} (in River dynamics) | critical discharge below which no bedload transport occurs | M / T |
ρ_{s} (in River dynamics) | grain density | M / L^{3} |
ρ | fluid density (in River dynamics) | M / L^{3} |
g | acceleration due to gravity | l / t^{2} |
β (in River dynamics) | bedload rating term | - |
s (in River dynamics) | slope of the riverbed | - |
e_{b} (in River dynamics) | bedload efficiency | - |
f (in River dynamics) | angle of repose of river bed sediment | - |
X (In avulsion) | river distributary | - |
Θ (In avulsion) | anglar position of X distributary | - |
D (in bedload dumping) | depth of bedload dumped at river mouth | L |
x | longitudinal or axial direction | - |
y | lateral direction | - |
u (in river plumes) | longitudinal velocity (in the x direction) | L / T |
v (in river plumes) | lateral velocity (in the y direction) | L / T |
I (in river plumes) | sediment inventory of the plume | - |
λ (in river plumes) | removal rate constant for a grain size (take marine flocculation into account) | 1 / T |
K (in river plumes) | sediment diffusivity driven by turbulence (assumed equal to the turbulent diffusivity and the eddy viscosity) | L^{2} / T |
Fr | Froude number | - |
v_{0} (in river plumes) | ambient coastal current velocity | L / T |
C_{1} (in river plumes) | empirically derived constant and found to be 0.109 | - |
C_{0} (in river plumes) | plume concentration at the river mouth | M / L^{3} |
q_{s} (in diffusion of seafloor sediments) | amount of bottom sediments that can be reworked by resuspension and diffusion (resuspended sediment) | M / L |
k (in diffusion of seafloor sediments) | diffusion coefficient | - |
t | time | T |
z (in diffusion of seafloor sediments) | water depth | L |
D (in diffusion of seafloor sediments) | grain size | L |
β_{i} (in diffusion of seafloor sediments) | user-defined index (between 0 and 1), reflect the ability of resuspension to move the ith grain size | - |
b (in Sediment failure) | width of a slice in a failure | L |
c (in Sediment failure) | sediment cohesion | M / T^{2} |
W (in Sediment failure) | linear weight of the sediment | M / T^{2} |
u (in Sediment failure) | excess pore pressure | M / (L T^{2}) |
φ (in Sediment failure) | sediment friction angle | - |
α (slope of failure surface) | slope of the failure surface | - |
F_{total} (slope of failure surface) | factor of safety for a sediment failure | - |
γ' (slope of failure surface) | submerged density of sediment, equals to (γ - γ_{f})g | M / L^{3} |
z | depth of the failure plane with respect to the seafloor | L |
l | sedimentation rate | M / T |
C_{v} (in River mouth turbidity currents ) | consolidation coefficient for the sediment | - |
g_{0} (in River mouth turbidity currents ) | reduced gravity | L / T^{2} |
u (in River mouth turbidity currents) | downslope velocity | L / T |
α (in River mouth turbidity currents) | seafloor slope | - |
E (in River mouth turbidity currents) | entrainment coefficient that controls the rate seawater dilutes the gravity flow | - |
C_{D} (in River mouth turbidity currents) | drag coefficient | - |
h (in River mouth turbidity currents) | height of the flow | L |
ρ (in River mouth turbidity currents) | ambient fluid density | M / L^{3} |
ρ_{f} (in River mouth turbidity currents) | density of the flow | M / L^{3} |
ρ_{s} (in River mouth turbidity currents) | grain density | M / L^{3} |
C (in River mouth turbidity currents) | vertically averaged flow concentration | - |
C_{i} (in River mouth turbidity currents) | volume concentration of the ith grain size in the flow | M / L^{3} |
n (in River mouth turbidity currents) | number of discrete grain sizes carried by the flow | - |
W (in River mouth turbidity currents) | flow width | L |
Q (in River mouth turbidity currents) | volume discharge between flow elements | L^{3} / T |
J_{i} (in River mouth turbidity currents) | flux of ith grain size between elements | L^{3} / T |
E_{Ri} (in River mouth turbidity currents) | rate of erosion of the ith grain size | L / T |
day (in River mouth turbidity currents) | 86400 s | T |
δ_{a} (in River mouth turbidity currents) | gradient of shear strength in seafloor sediment | M / (LT^{2}) |
δ_{b} (in River mouth turbidity currents) | shear strength of the sediment at the seafloor | M / (L^{1} T^{2}) |
D_{Ri} (in River mouth turbidity currents) | rate of deposition of the ith grain size | L / T |
u_{cr} (in River mouth turbidity currents) | critical velocity for deposition | L / T |
h_{f} (in River mouth turbidity currents) | flow thickness | L |
E_{w} (in River mouth turbidity currents) | water entrainment coefficient | - |
S (in River mouth turbidity currents) | bottom slope gradient | - |
C_{d} (in River mouth turbidity currents) | drag coefficient, equals to 0.004 | - |
α(in River mouth turbidity currents) | ratio of the drag force at the upper flow surface to that at the bed, equals to 0.43 | - |
F_{d}(in River mouth turbidity currents) | flux of sediment deposition | - |
F_{d}(in River mouth turbidity currents) | flux of sediment erosion | - |
Ri(in River mouth turbidity currents) | Richardson number from Fukishima et al. (1985) | - |
w_{s}(in River mouth turbidity currents) | particle settling velocity | L / T |
ρ_{f}(in River mouth turbidity currents) | flow density | M / L^{3} |
a(in River mouth turbidity currents) | increasing rate of shear strength with burial depth, equals to 3.5 | - |
b(in River mouth turbidity currents) | shear strength at the bed, equals to 0.2 | - |
Z_{0}(in River mouth turbidity currents) | Rouse number | - |
κ (in River mouth turbidity currents) | von Karman constant, equals to 0.4 | - |
u_{*} (in River mouth turbidity currents) | shear velocity of the flow | l / t |
D (in Debris flows) | total depth of the debris flow (D_{p} + D_{s}) | L |
D_{p} (in Debris flows) | depth of the upper plug zone | L |
U_{p} (in Debris flows) | layer-averaged velocity of the upper plug zone | L / T |
D_{s} (in Debris flows) | depth of the lower shear layer | L |
U_{s} (in Debris flows) | layer-averaged veolocity of the lower shear layer | L / T |
ρ_{m} (in Debris flows) | density of the mud flow | M / L^{3} |
τ_{y} (in Debris flows) | yield strength | - |
μ (in Debris flows) | kinematic viscosity | - |
w (in Subsidence) | displacement of crust due to sediment loading | L |
D (in Subsidence) | flexural rigidity of the earth's crust | M L^{2} / T^{2} |
ρ_{m} (in Subsidence) | density of the overlying sediment | M / L^{3} |
φ (in Compaction) | porosity of sediment | - |
φ_{0} (in Compaction) | porosity of sediment in its closest packed arrangement (due only to mechanical compaction) | - |
δ (in Compaction) | sediment load | - |
c (in Compaction) | empirical constant for compaction | L T^{2} / M |
η (in Subaerial erosion and deposition by rivers) | height of the bed | L |
ν (in Subaerial erosion and deposition by rivers) | diffusion coefficient | - |
(in Subaerial erosion and deposition by rivers) |
long-term average water discharge | L^{3} / T |
c_{f} (in Subaerial erosion and deposition by rivers) | drag coefficient | - |
C_{0} (in Subaerial erosion and deposition by rivers) | sediment concentration of the bed | M / L^{3} |
s (in Subaerial erosion and deposition by rivers) | sediment specific gravity | - |
A (in Subaerial erosion and deposition by rivers) | river-type dependent constant (user-defined and takes on one of the two values depending on the river type: 1 for meandering river, (ε/(1+ε))^{3/2} for braided river) | - |
ε (in Subaerial erosion and deposition by rivers) | typically about 0.4 for gravel bed rivers (Parker, 1978) | - |
τ (in Subaerial erosion and deposition by rivers) | shear stress in the center of a braided channel, equals to (1+ε)τ_{c} | - |
τ_{c} (in Subaerial erosion and deposition by rivers) | critical shear stress needed for band erosion | - |
h_{c} (in Cross-shore transport due to ocean storms) | closure depth | L |
H_{ss} (in Cross-shore transport due to ocean storms) | height of the storm wave that is exceeded only 12h each year | L |
T (in Cross-shore transport due to ocean storms) | period of the storm wave that is exceeded only 12h each year | T |
q_{s} (in Cross-shore transport due to ocean storms) | sediment flux at each position along the outer shelf profile | M / T |
C_{fs} (in Cross-shore transport due to ocean storms) | constant drag coefficient | - |
ε_{ss} (in Cross-shore transport due to ocean storms) | efficiency of suspended sediment transport | - |
I_{s} (in Cross-shore transport due to ocean storms) | time fraction (intermittency) of ocean storms | - |
U_{om} (in Cross-shore transport due to ocean storms) | near-bed velocity due to waves | L / T |
h (in Cross-shore transport due to ocean storms) | local water depth | L |
γ_{b} (in Cross-shore transport due to ocean storms) | ratio of wave height to water depth where wave will break, assumed to be 0.6 | - |
h_{b} (in Cross-shore transport due to ocean storms) | water depth where wave will break | L |
D (in Cross-shore transport due to ocean storms) | grain size | L |
u_{t} (in Cross-shore transport due to ocean storms) | near-bottom threshold velocity | L / T |
d_{0} (in Cross-shore transport due to ocean storms) | orbital diameter of the wave motion | L |
H (in Cross-shore transport due to ocean storms) | wave height | L |
T (in Cross-shore transport due to ocean storms) | wave period | T |
L (in Cross-shore transport due to ocean storms) | wave length | L |
x (in Cross-shore transport due to ocean storms) | offshore position normalized by the position of near-shore boundary | - |
m (in Cross-shore transport due to ocean storms) | diffusion coefficient within this specific x-dependence to ensure the equilibrim profile will be a Bruun profile, m equals to 2/3 | - |
w (in Flexure of the lithosphere) | deflection of earth's crust | - |
λ (in Flexure of the lithosphere) | flexural parameter | - |
r (in Flexure of the lithosphere) | distance from the point load | - |
q (in Flexure of the lithosphere) | point load | - |
Kei (in Flexure of the lithosphere) | Kelvin function | - |
ρ_{d} (in Flexure of the lithosphere) | density of the asthenosphere | M / L^{3} |
D (in Flexure of the lithosphere) | flexural rigidity of the earth's crust | - |
w_{0} (in Flexure of the lithosphere) | equilibrium deflection | - |
t_{0} (in Flexure of the lithosphere) | response time associated with mantle viscosity | - |
Notes
See the reference Syvitski and Hutton (2001) and Hutton and Syvitski (2008).
Examples
An example run with input parameters, BLD files, as well as a figure / movie of the output
Follow the next steps to include images / movies of simulations:
- Upload file: https://csdms.colorado.edu/wiki/Special:Upload
- Create link to the file on your page: [[Image:<file name>]].
See also: Help:Images or Help:Movies
Developer(s)
References
- Hutton, E. W. H. and Syvitski, J. P. M., 2008. Sedflux 2.0: An advanced process-response model that generates three-dimensional stratigraphy. Computer & Geosciences, 34, 1319~1337, Doi: [10.1016/j.cageo.2008.02.013].
- Syvitski, J. P. M. and Hutton, E. W. H., 2001. 2D SEDFLUX 1.0C: an advanced process-response numerical model for the fill of marine sedimentary basins. Computer & Geosciences, 27, 731~753, Doi: [10.1016/S0098-3004(00)00139-4].