CMS-Flow:Non-equilibrium Sediment Transport: Difference between revisions

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= Transport Equation =
= Transport Equation =
Non-cohesive sediment transport is calculated with a non-equilibrium bed-material (total load) formulation. In this approach, the suspended- and bed-load transport equations are combined into a single equation and thus there is one less empirical parameter to estimate (adaptation length). The transport equation is derived by adding the suspended- and bed-load transport equations to obtain the general sediment mass balance equation and then substituting a non-equilibrium expression for the bed elevation change as suggested by Wu (2004):  
Non-cohesive sediment transport is calculated with a non-equilibrium bed-material (total load) formulation. In this approach, transport equation is derived by adding the suspended and bed load transport equations to obtain the general sediment mass balance equation and then substituting a non-equilibrium expression for the bed elevation change as suggested by Wu (2004):  
         {{Equation| <math> \frac{\partial}{\partial t} \biggl( \frac{ h C_{tk} }{\beta _{tk}} \biggr) + \frac{\partial (U_j h C_{tk})}{\partial x_j} = \frac{\partial }{\partial x_j} \biggl[ \nu _s h \frac{\partial (r_{sk} C_{tk})}{\partial x_j} \biggr] + \alpha _t \omega _{sk} (C_{t*k} - C_{tk}) </math>|2=1}}
         {{Equation| math \frac{\partial}{\partial t} \biggl( \frac{ h C_{tk} }{\beta _{tk}} \biggr) + \frac{\partial (U_j h C_{tk})}{\partial x_j} = \frac{\partial }{\partial x_j} \biggl[ \nu _s h \frac{\partial (r_{sk} C_{tk})}{\partial x_j} \biggr] + \alpha _t \omega _{sk} (C_{t*k} - C_{tk}) /math|2=1}}


where the subscript <math>k</math> indicates the sediment size class, <math>h</math> is the total water depth (<math> h = \zeta + \eta </math>), <math>C_{tk} </math> is the total load concentration, <math>C_{t*k} </math> is the sediment transport capacity, <math>\beta _{tk}</math> is the total load correction factor, <math> \nu _s </math> is the diffusion coefficient, <math>r_{sk}</math> is the fraction of suspended sediments, <math>\alpha_t</math> is the total load adaptation coefficient, and <math>\omega_{sk}</math> is the sediment fall velocity. Equation (1) is valid for both single and mixed sediments. However, only single-size sediment transport is available through the SMS interface. To access the nonuniform sediment transport, Advanced Cards must be used.  
where the subscript mathk/math indicates the sediment size class, mathh/math is the total water depth (math h = \zeta + \eta /math), mathC_{tk} /math is the total load concentration, mathC_{t*k} /math is the sediment transport capacity, math\beta _{tk}/math is the total load correction factor, math \nu _s /math is the diffusion coefficient, mathr_{sk}/math is the fraction of suspended sediments, math\alpha_t/math is the total load adaptation coefficient, and math\omega_{sk}/math is the sediment fall velocity. Equation (1) is valid for both single and mixed sediments. However, only single-size sediment transport is available through the SMS interface. To access the nonuniform sediment transport, Advanced Cards must be used.


= Hiding and Exposure =
= Hiding and Exposure =
== Single-Sized Sediment Transport ==
== Single-Sized Sediment Transport ==
At  many sites, the bed material can be characterized by a single sediment  size, with other sizes or materials (shell hash) which do not contribute  significantly to morphology change, but do modify the sediment  transport through hiding and exposure. By assuming that the spatial  distribution of the bed material composition is constant in time, a  hiding and exposure correction function can be introduced to correct the  critical shields parameter <math>\theta_{ck}^{he} = \xi_k  \theta_{ck}</math> where <math>\xi_k</math> is the  dimensionless hiding and exposure function and  <math>\theta_{ck}</math> is the critical shear stress of the  transport grain size. In CMS, a formula similar to that of Parker et  al. (1995) and others is implemented <math>\xi_k =  (d_k/d_{50})^{-m} </math> where is the grain size corresponding to  the 50th percentile, and <math> m </math> is an empirical  coefficient between 0.5-1.0 (default is 0.7).
At  many sites, the bed material can be characterized by a single sediment  size, with other sizes or materials (shell hash) which do not contribute  significantly to morphology change, but do modify the sediment  transport through hiding and exposure. By assuming that the spatial  distribution of the bed material composition is constant in time, a  hiding and exposure correction function can be introduced to correct the  critical shields parameter math\theta_{ck}^{he} = \xi_k  \theta_{ck}/math where math\xi_k/math is the  dimensionless hiding and exposure function and  math\theta_{ck}/math is the critical shear stress of the  transport grain size. In CMS, a formula similar to that of Parker et  al. (1995) and others is implemented math\xi_k =  (d_k/d_{50})^{-m} /math where is the grain size corresponding to  the 50th percentile, and math m /math is an empirical  coefficient between 0.5-1.0 (default is 0.7).


The  transport grain size is specified in the Advanced Card  TRANSPORT_GRAIN_SIZE. The transport grain size should be the dominant  grain size in the area of interest.  
The  transport grain size is specified in the Advanced Card  TRANSPORT_GRAIN_SIZE. The transport grain size should be the dominant  grain size in the area of interest.  
To change the value of  <math> m </math> another Advanced Card  HIDING_EXPOSURE_COEFFICIENT. If it is desired to test the model with a  constant grain size and ignore the information in the D50_DATASET, the  Advanced Card CONSTANT_GRAIN_SIZE.
To change the value of  math m /math another Advanced Card  HIDING_EXPOSURE_COEFFICIENT. If it is desired to test the model with a  constant grain size and ignore the information in the D50_DATASET, the  Advanced Card CONSTANT_GRAIN_SIZE.


== Multiple-Sized  Sediment Transport==
== Multiple-Sized  Sediment Transport==
For nonuniform sediments, the hiding and  exposure is considered using a slightly modified form of the method  proposed by Wu et al. (2000) which accounts information on the whole  grain size distribution.
For nonuniform sediments, the hiding and  exposure is considered using a slightly modified form of the method  proposed by Wu et al. (2000) which accounts information on the whole  grain size distribution.
     {{Equation|<math> \xi_k =  (p_{ek}/p_{hk})^{-m} </math>|2=5}}
     {{Equation|math \xi_k =  (p_{ek}/p_{hk})^{-m} /math|2=5}}


where  <math>p_{ek}</math> and <math>p_{hk}</math> are  the exposure and hiding probabilities calculated as  
where  mathp_{ek}/math and mathp_{hk}/math are  the exposure and hiding probabilities calculated as  
       {{Equation|<math> p_{ek} = \sum_{j=1}^N p_{bj}  \frac{d_j}{d_k+d_j},  p_{hk} = \sum_{j=1}^N p_{bj} \frac{d_k}{d_k+d_j},  </math>|2=6}}
       {{Equation|math p_{ek} = \sum_{j=1}^N p_{bj}  \frac{d_j}{d_k+d_j},  p_{hk} = \sum_{j=1}^N p_{bj} \frac{d_k}{d_k+d_j},  /math|2=6}}


== Total load correction factor ==
== Total load correction factor ==
The total-load correction factor accounts for the time lag (hysteresis) between flow and sediment transport and is given by
The total-load correction factor accounts for the time lag (hysteresis) between flow and sediment transport and is given by
     {{Equation| <math>\beta_{tk} = \frac{1}{r_{sk} / \beta_{sk} + (1-r_{sk})U/u_{bk}}</math>|2=2}}
     {{Equation| math\beta_{tk} = \frac{1}{r_{sk} / \beta_{sk} + (1-r_{sk})U/u_{bk}}/math|2=2}}


where <math>U</math> is the current depth-averaged current magnitude, <math>u_b</math> is the bed-load transport velocity,  and <math>\beta_{sk}</math> is the suspended-load correction factor defined by  
where mathU/math is the current depth-averaged current magnitude, mathu_b/math is the bed-load transport velocity,  and math\beta_{sk}/math is the suspended-load correction factor defined by  
     {{Equation|<math>\beta_s = \frac{\int_{a}^{h} u_s c dz } { U \int_{a}^{h} c dz} </math>|2=3}}
     {{Equation|math\beta_s = \frac{\int_{a}^{h} u_s c dz } { U \int_{a}^{h} c dz} /math|2=3}}


where <math>c</math> is the local sediment concentration, <math>a</math> is the thickness of the bed-load layer, and <math>u_s</math> is the stream-wise local current velocity. Assuming a logarithmic velocity distribution in non-dimensional form (shape function)
where mathc/math is the local sediment concentration, matha/math is the thickness of the bed-load layer, and mathu_s/math is the stream-wise local current velocity. Assuming a logarithmic velocity distribution in non-dimensional form (shape function)
     {{Equation|<math> u'_s(z) = \frac{u_s(z)}{U} = \frac{\ln{(z'/z'_0)}}{ \ln{(1/z'_0)} - 1} </math>|2=4}}
     {{Equation|math u'_s(z) = \frac{u_s(z)}{U} = \frac{\ln{(z'/z'_0)}}{ \ln{(1/z'_0)} - 1} /math|2=4}}


and an exponential concentration profile also in non-dimensional form
and an exponential concentration profile also in non-dimensional form
     {{Equation|<math> c'(z') = \frac{c(z)}{c_a} = \exp{ (-\phi'(z'-a')) } </math>|2=5}}
     {{Equation|math  c'(z') = \frac{c(z)}{c_a} = \exp{ (-\phi'(z'-a')) } /math|2=5}}


where <math>c</math> is the local concentration,  <math>c_a</math> is a near-bottom concentration specified at a reference height <math>a</math>, <math> \phi = w_s/ \epsilon_s </math>, <math>\phi'=\phi h</math>, <math>z'=z/h</math>, and <math>a'=a/h</math>. Using (4) and (5) he analytical solution to (3) is
where mathc/math is the local concentration,  mathc_a/math is a near-bottom concentration specified at a reference height matha/math, math \phi = w_s/ \epsilon_s /math, math\phi'=\phi h/math, mathz'=z/h/math, and matha'=a/h/math. Using (4) and (5) he analytical solution to (3) is
     {{Equation|<math> \beta_s = \frac{E_1(\phi' a') - E_1(\phi') + \ln{(a'/z'_0)} e^{-\phi' a'} - \ln{(1/z'_0)}e^{-\phi'}} {e^{- \phi' a'} [ \ln(1/z'_0)-1][1-e^{-\phi'(1-a')}]} </math>|2=6}}
     {{Equation|math \beta_s = \frac{E_1(\phi' a') - E_1(\phi') + \ln{(a'/z'_0)} e^{-\phi' a'} - \ln{(1/z'_0)}e^{-\phi'}} {e^{- \phi' a'} [ \ln(1/z'_0)-1][1-e^{-\phi'(1-a')}]} /math|2=6}}


where <math>E_1(x)=\int_{x}^{\infty}\frac{e^{-t}}{t}\, dt </math> is the exponential integral. Because the exponential integral requires and series expansion to solve it is more efficient to create a look up table and interpolate the values during the simulation which is what is done in CMS. A look up table is also created for when using the Rouse sediment concentration profile. Figure 1 and 2 compare the suspended load correction factor for exponential and Rouse sediment concentration profiles
where mathE_1(x)=\int_{x}^{\infty}\frac{e^{-t}}{t}\, dt /math is the exponential integral. Because the exponential integral requires and series expansion to solve it is more efficient to create a look up table and interpolate the values during the simulation which is what is done in CMS. A look up table is also created for when using the Rouse sediment concentration profile. Figure 1 and 2 compare the suspended load correction factor for exponential and Rouse sediment concentration profiles


[[File:Betas_LogExp.jpg|thumb|left|400px|Figure 1. Suspended load correction factor based on logarithmic velocity and exponential concentration profiles.]]
[[File:Betas_LogExp.jpg|thumb|left|400px|Figure 1. Suspended load correction factor based on logarithmic velocity and exponential concentration profiles.]]
Line 46: Line 46:
[[File:Betas_LogRouse.jpg|thumb|none|400px|Figure 2. Suspended load correction factor based on logarithmic velocity and Rouse concentration profiles.]]
[[File:Betas_LogRouse.jpg|thumb|none|400px|Figure 2. Suspended load correction factor based on logarithmic velocity and Rouse concentration profiles.]]


<br style="clear:both" />
br style=clear:both /


In CMS, the bed load velocity is determined using the Van Rijn formula (1984)
In CMS, the bed load velocity is determined using the Van Rijn formula (1984)
     {{Equation|<math> \frac{u_b}{\sqrt{(\rho_s/\rho-1)gd_k}} = aT^b </math>|2=4}}
     {{Equation|math \frac{u_b}{\sqrt{(\rho_s/\rho-1)gd_k}} = aT^b /math|2=4}}


where and <math>T</math> is the non-dimensional transport stage number given by <math>T=\tau'_b/\tau_{cr} -1</math>, and <math>a,b</math> are empirical coefficients equal to 1.64 and 0.5 (Wu et al. 2006).
where and mathT/math is the non-dimensional transport stage number given by mathT=\tau'_b/\tau_{cr} -1/math, and matha,b/math are empirical coefficients equal to 1.64 and 0.5 (Wu et al. 2006).


= Bed Change Equation =
= Bed Change Equation =
The change in the water depth is calculated by  
The change in the water depth is calculated by  
       {{Equation| <math> (1 - p'_m) \biggl( \frac{\partial \zeta}{\partial t} \biggr)_k = \alpha _t \omega _s (C_{tk*} - C_{tk}) + \frac{\partial }{\partial x_j} \biggl[ D_s |Q_{bk}| \frac{\partial \zeta}{\partial x_j} \biggr] </math>|2=4}}
       {{Equation| math (1 - p'_m) \biggl( \frac{\partial \zeta}{\partial t} \biggr)_k = \alpha _t \omega _s (C_{tk*} - C_{tk}) + \frac{\partial }{\partial x_j} \biggl[ D_s |Q_{bk}| \frac{\partial \zeta}{\partial x_j} \biggr] /math|2=4}}


where <math> p'_m </math> is the sediment porosity, <math>Q_{bk}</math> is the bed load transport, and <math> D_s </math> is a bedslope coefficient.
where math p'_m /math is the sediment porosity, mathQ_{bk}/math is the bed load transport, and math D_s /math is a bedslope coefficient.


= Bed Sorting and Gradation (nonuniform sediments) =
= Bed Sorting and Gradation (nonuniform sediments) =
When simulating nonuniform sediments it is necessary to keep track of the vertical variation in bed composition. In order to do this, the bed is divided into discrete layers. The top layer is the mixing or active layer and is the layer of sediment which is actively being exchanged with the bed and suspended loads. The temporal variation of the bed-material in the mixing and second layers is calculated as (Wu 2004)
When simulating nonuniform sediments it is necessary to keep track of the vertical variation in bed composition. In order to do this, the bed is divided into discrete layers. The top layer is the mixing or active layer and is the layer of sediment which is actively being exchanged with the bed and suspended loads. The temporal variation of the bed-material in the mixing and second layers is calculated as (Wu 2004)
     {{Equation|<math> \frac{\partial (\delta_m p_{bk}) }{\partial t} + \biggl( \frac{\partial \zeta}{\partial t}  \biggr)_k = -\frac{\partial (\delta_m p_{bk}) }{\partial t} = p^*_{bk} \biggl(\frac{\partial \delta_m }{\partial t}  + \frac{\partial \zeta }{\partial t} \biggr) </math>|2=7}}
     {{Equation|math \frac{\partial (\delta_m p_{bk}) }{\partial t} + \biggl( \frac{\partial \zeta}{\partial t}  \biggr)_k = -\frac{\partial (\delta_m p_{bk}) }{\partial t} = p^*_{bk} \biggl(\frac{\partial \delta_m }{\partial t}  + \frac{\partial \zeta }{\partial t} \biggr) /math|2=7}}


where <math> \delta_m </math> and <math> \delta_s </math> are the thicknesses of the mixing and second layers respectively. <math> p^*_{bk} = p_{bk} </math> for <math> \partial \zeta / \partial t + \partial \delta_m / \partial t \le 0 </math> or <math> p^*_{bk} = p_{sk} </math> otherwise. Figure 3 shows an example of the bed layer evolution over time for varying bed deposition and erosion.
where math \delta_m /math and math \delta_s /math are the thicknesses of the mixing and second layers respectively. math p^*_{bk} = p_{bk} /math for math \partial \zeta / \partial t + \partial \delta_m / \partial t \le 0 /math or math p^*_{bk} = p_{sk} /math otherwise. Figure 3 shows an example of the bed layer evolution over time for varying bed deposition and erosion.


[[File:Bed_layering_V2.jpg|thumb|left|500px|Figure 3. Example of bed layer variation for varying deposition and erosion.]]
[[File:Bed_layering_V2.jpg|thumb|left|500px|Figure 3. Example of bed layer variation for varying deposition and erosion.]]


<br style="clear:both" />
br style=clear:both /


= Avalanching =
= Avalanching =
The process of avalanching is simulated by enforcing the angle of repose while maintaining mass continuity between adjacent cells. The presented approach adopts a relaxation method between adjacent cells and is stable and efficient. The equation for bed change due to avalanching is obtained by combining the equation of angle of repose and the continuity equation to obtain
The process of avalanching is simulated by enforcing the angle of repose while maintaining mass continuity between adjacent cells. The presented approach adopts a relaxation method between adjacent cells and is stable and efficient. The equation for bed change due to avalanching is obtained by combining the equation of angle of repose and the continuity equation to obtain
       {{Equation|<math> \Delta \zeta ^a _p =  R \sum_i \frac{ A_i \delta x_i }{A_p + A_i} ( \tan{ \phi^n_i } - \textrm{ sgn } \phi _i \tan{\phi_r }) \textrm{ H } ( | \phi^n _i | - \phi _r ) </math>|2=8}}
       {{Equation|math \Delta \zeta ^a _p =  R \sum_i \frac{ A_i \delta x_i }{A_p + A_i} ( \tan{ \phi^n_i } - \textrm{ sgn } \phi _i \tan{\phi_r }) \textrm{ H } ( | \phi^n _i | - \phi _r ) /math|2=8}}


where the subscripts p and i indicate the center and neighboring cells respectively, <math>\delta x</math> is the cell center distance between cells p and i, <math> \Delta \zeta ^a _p </math> is the bed change due to avalanching, A is the cell area, <math>\phi</math> is the bed slope, <math>\phi _r</math> is the sediment repose angle, R is an under-relaxation factor (approximately 0.25-0.5), and <math>\textrm{H}</math> and <math>\textrm{ sgn}</math> are the Heaviside and sign functions. The equation is applied every morphologic time step by sweeping through all of the computational cells to calculate <math> \Delta \zeta </math> and then modifying the bathymetry as <math>\zeta^{n+1}=\zeta^n + \Delta \zeta^a  </math>.
where the subscripts p and i indicate the center and neighboring cells respectively, math\delta x/math  is the cell center distance between cells p and i, math  \Delta \zeta ^a _p /math is the bed change due to avalanching, A is the cell area, math\phi/math is the bed slope, math\phi _r/math is the sediment repose angle, R is an under-relaxation factor (approximately 0.25-0.5), and math\textrm{H}/math and math\textrm{ sgn}/math are the Heaviside and sign functions. The equation is applied every morphologic time step by sweeping through all of the computational cells to calculate math \Delta \zeta /math and then modifying the bathymetry as math\zeta^{n+1}=\zeta^n + \Delta \zeta^a  /math.


= Boundary Conditions =
= Boundary Conditions =
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* Camenen, B., and Larson, M. (2007). “A unified sediment transport formulation for coastal inlet application”. Technical Report ERDC-CHL CR-07-01.  Vicksburg, MS: U.S. Army Engineer Research and Development Center, U.S.A
* Camenen, B., and Larson, M. (2007). “A unified sediment transport formulation for coastal inlet application”. Technical Report ERDC-CHL CR-07-01.  Vicksburg, MS: U.S. Army Engineer Research and Development Center, U.S.A
* Parker, G., Kilingeman, P. C., and McLean, D. G. (1982). “Bed load and size distribution in paved gravel-bed streams.” J. Hydr. Div., ASCE, 108(4), 544-571.   
* Parker, G., Kilingeman, P. C., and McLean, D. G. (1982). “Bed load and size distribution in paved gravel-bed streams.” J. Hydr. Div., ASCE, 108(4), 544-571.   
* Soulsby, R. L. (1997). "Dynamics of marine sands, a manual for practical applications". H. R. Wallingford, UK: Thomas Telford.
* Soulsby, R. L. (1997). Dynamics of marine sands, a manual for practical applications. H. R. Wallingford, UK: Thomas Telford.
* Watanabe, A. (1987). “3-dimensional numerical model of beach evolution”. Proc. Coastal Sediments ’87, ASCE, 802-817.  
* Watanabe, A. (1987). “3-dimensional numerical model of beach evolution”. Proc. Coastal Sediments ’87, ASCE, 802-817.  
* Wu, W. (2004).“Depth-averaged 2-D numerical modeling of unsteady flow and nonuniform sediment transport in open channels”. J. Hydraulic Eng., ASCE, 135(10), 1013–1024.
* Wu, W. (2004).“Depth-averaged 2-D numerical modeling of unsteady flow and nonuniform sediment transport in open channels”. J. Hydraulic Eng., ASCE, 135(10), 1013–1024.

Revision as of 19:25, 22 June 2011

UNDER CONSTRUCTION

written by Alejandro Sanchez Last date modified: December 8, 2010

Transport Equation

Non-cohesive sediment transport is calculated with a non-equilibrium bed-material (total load) formulation. In this approach, transport equation is derived by adding the suspended and bed load transport equations to obtain the general sediment mass balance equation and then substituting a non-equilibrium expression for the bed elevation change as suggested by Wu (2004):

  math \frac{\partial}{\partial t} \biggl( \frac{ h C_{tk} }{\beta _{tk ({{{2}}})

\biggr) + \frac{\partial (U_j h C_{tk})}{\partial x_j} = \frac{\partial }{\partial x_j} \biggl[ \nu _s h \frac{\partial (r_{sk} C_{tk})}{\partial x_j} \biggr] + \alpha _t \omega _{sk} (C_{t*k} - C_{tk}) /math|2=1}}

where the subscript mathk/math indicates the sediment size class, mathh/math is the total water depth (math h = \zeta + \eta /math), mathC_{tk} /math is the total load concentration, mathC_{t*k} /math is the sediment transport capacity, math\beta _{tk}/math is the total load correction factor, math \nu _s /math is the diffusion coefficient, mathr_{sk}/math is the fraction of suspended sediments, math\alpha_t/math is the total load adaptation coefficient, and math\omega_{sk}/math is the sediment fall velocity. Equation (1) is valid for both single and mixed sediments. However, only single-size sediment transport is available through the SMS interface. To access the nonuniform sediment transport, Advanced Cards must be used.

Hiding and Exposure

Single-Sized Sediment Transport

At many sites, the bed material can be characterized by a single sediment size, with other sizes or materials (shell hash) which do not contribute significantly to morphology change, but do modify the sediment transport through hiding and exposure. By assuming that the spatial distribution of the bed material composition is constant in time, a hiding and exposure correction function can be introduced to correct the critical shields parameter math\theta_{ck}^{he} = \xi_k \theta_{ck}/math where math\xi_k/math is the dimensionless hiding and exposure function and math\theta_{ck}/math is the critical shear stress of the transport grain size. In CMS, a formula similar to that of Parker et al. (1995) and others is implemented math\xi_k = (d_k/d_{50})^{-m} /math where is the grain size corresponding to the 50th percentile, and math m /math is an empirical coefficient between 0.5-1.0 (default is 0.7).

The transport grain size is specified in the Advanced Card TRANSPORT_GRAIN_SIZE. The transport grain size should be the dominant grain size in the area of interest. To change the value of math m /math another Advanced Card HIDING_EXPOSURE_COEFFICIENT. If it is desired to test the model with a constant grain size and ignore the information in the D50_DATASET, the Advanced Card CONSTANT_GRAIN_SIZE.

Multiple-Sized Sediment Transport

For nonuniform sediments, the hiding and exposure is considered using a slightly modified form of the method proposed by Wu et al. (2000) which accounts information on the whole grain size distribution.

  {{{1}}} (5)

where mathp_{ek}/math and mathp_{hk}/math are the exposure and hiding probabilities calculated as

  {{{1}}} (6)

Total load correction factor

The total-load correction factor accounts for the time lag (hysteresis) between flow and sediment transport and is given by

  {{{1}}} ({{{2}}})

/math|2=2}}

where mathU/math is the current depth-averaged current magnitude, mathu_b/math is the bed-load transport velocity, and math\beta_{sk}/math is the suspended-load correction factor defined by

  {{{1}}} (3)

where mathc/math is the local sediment concentration, matha/math is the thickness of the bed-load layer, and mathu_s/math is the stream-wise local current velocity. Assuming a logarithmic velocity distribution in non-dimensional form (shape function)

  {{{1}}} ({{{2}}})

{ \ln{(1/z'_0)} - 1} /math|2=4}}

and an exponential concentration profile also in non-dimensional form

  {{{1}}} (5)

where mathc/math is the local concentration, mathc_a/math is a near-bottom concentration specified at a reference height matha/math, math \phi = w_s/ \epsilon_s /math, math\phi'=\phi h/math, mathz'=z/h/math, and matha'=a/h/math. Using (4) and (5) he analytical solution to (3) is

  {{{1}}} ({{{2}}})

{e^{- \phi' a'} [ \ln(1/z'_0)-1][1-e^{-\phi'(1-a')}]} /math|2=6}}

where mathE_1(x)=\int_{x}^{\infty}\frac{e^{-t}}{t}\, dt /math is the exponential integral. Because the exponential integral requires and series expansion to solve it is more efficient to create a look up table and interpolate the values during the simulation which is what is done in CMS. A look up table is also created for when using the Rouse sediment concentration profile. Figure 1 and 2 compare the suspended load correction factor for exponential and Rouse sediment concentration profiles

Figure 1. Suspended load correction factor based on logarithmic velocity and exponential concentration profiles.
Figure 2. Suspended load correction factor based on logarithmic velocity and Rouse concentration profiles.

br style=clear:both /

In CMS, the bed load velocity is determined using the Van Rijn formula (1984)

  math \frac{u_b}{\sqrt{(\rho_s/\rho-1)gd_k ({{{2}}})

= aT^b /math|2=4}}

where and mathT/math is the non-dimensional transport stage number given by mathT=\tau'_b/\tau_{cr} -1/math, and matha,b/math are empirical coefficients equal to 1.64 and 0.5 (Wu et al. 2006).

Bed Change Equation

The change in the water depth is calculated by

  Q_{bk} (4)

where math p'_m /math is the sediment porosity, mathQ_{bk}/math is the bed load transport, and math D_s /math is a bedslope coefficient.

Bed Sorting and Gradation (nonuniform sediments)

When simulating nonuniform sediments it is necessary to keep track of the vertical variation in bed composition. In order to do this, the bed is divided into discrete layers. The top layer is the mixing or active layer and is the layer of sediment which is actively being exchanged with the bed and suspended loads. The temporal variation of the bed-material in the mixing and second layers is calculated as (Wu 2004)

  {{{1}}} (7)

where math \delta_m /math and math \delta_s /math are the thicknesses of the mixing and second layers respectively. math p^*_{bk} = p_{bk} /math for math \partial \zeta / \partial t + \partial \delta_m / \partial t \le 0 /math or math p^*_{bk} = p_{sk} /math otherwise. Figure 3 shows an example of the bed layer evolution over time for varying bed deposition and erosion.

Figure 3. Example of bed layer variation for varying deposition and erosion.

br style=clear:both /

Avalanching

The process of avalanching is simulated by enforcing the angle of repose while maintaining mass continuity between adjacent cells. The presented approach adopts a relaxation method between adjacent cells and is stable and efficient. The equation for bed change due to avalanching is obtained by combining the equation of angle of repose and the continuity equation to obtain

  \phi^n _i (8)

where the subscripts p and i indicate the center and neighboring cells respectively, math\delta x/math is the cell center distance between cells p and i, math \Delta \zeta ^a _p /math is the bed change due to avalanching, A is the cell area, math\phi/math is the bed slope, math\phi _r/math is the sediment repose angle, R is an under-relaxation factor (approximately 0.25-0.5), and math\textrm{H}/math and math\textrm{ sgn}/math are the Heaviside and sign functions. The equation is applied every morphologic time step by sweeping through all of the computational cells to calculate math \Delta \zeta /math and then modifying the bathymetry as math\zeta^{n+1}=\zeta^n + \Delta \zeta^a /math.

Boundary Conditions

There are three types of boundary conditions in the sediment transport: Wet-dry, Outflow and Inflow.

1. Wet-dry interface.

The interface between wet and dry cells has a zero-flux boundary condition. Both the advective and diffusive fluxes are set to zero at the wet-dry interfaces. Note that avalanching may still occur between wet-dry cells.

2. Outflow Boundary Condition

Outflow boundaries are assigned a zero-gradient boundary condition and sediments are allowed to be transported freely out of the domain.

3. Inflow Boundary Condition

When flow is entering the domain, it is necessary to specify the sediment concentration. In CMS-Flow, the inflow sediment concentration is set to the equilibrium sediment concentation. For some cases, it is desired to reduce the amount of sediment entering from the boundary such as in locations where the sediment source is limited (i.e. coral reefs). The inflow equilibrium sediment concentration may be adjusted by multiplying by a loading scaling factor and is specified by the Advanced Card NET_LOADING_FACTOR or SEDIMENT_INFLOW_LOADING_FACTOR.

Numerical Methods

The governing equations are discretized using the Finite Volume Method on a staggered, non-uniform Cartesian grid. Time integration is calculated with a simple explicit forward Euler scheme. Diffusion terms are discretized with the standard central difference scheme. Advection terms are discretized with either the first order upwind scheme or the second order Hybrid Linear/Parabolic Approximation (HLPA) scheme of Zhu (1991). The default advection scheme is HLPA but may be changed with the Advanced Card ADVECTION_SCHEME.

References

  • Buttolph, A. M., C. W. Reed, N. C. Kraus, N. Ono, M. Larson, B. Camenen, H. Hanson, T. Wamsley, and A. K. Zundel. (2006). “Two-dimensional depth-averaged circulation model CMS-M2D: Version 3.0, Report 2: Sediment transport and morphology change.” Coastal and Hydraulics Laboratory Technical Report ERDC/CHL TR-06-9. Vicksburg, MS: U.S. Army Engineer Research and Development Center, U.S.A.
  • Camenen, B., and Larson, M. (2007). “A unified sediment transport formulation for coastal inlet application”. Technical Report ERDC-CHL CR-07-01. Vicksburg, MS: U.S. Army Engineer Research and Development Center, U.S.A
  • Parker, G., Kilingeman, P. C., and McLean, D. G. (1982). “Bed load and size distribution in paved gravel-bed streams.” J. Hydr. Div., ASCE, 108(4), 544-571.
  • Soulsby, R. L. (1997). Dynamics of marine sands, a manual for practical applications. H. R. Wallingford, UK: Thomas Telford.
  • Watanabe, A. (1987). “3-dimensional numerical model of beach evolution”. Proc. Coastal Sediments ’87, ASCE, 802-817.
  • Wu, W. (2004).“Depth-averaged 2-D numerical modeling of unsteady flow and nonuniform sediment transport in open channels”. J. Hydraulic Eng., ASCE, 135(10), 1013–1024.
  • van Rijn, L. C. (1985). “Flume experiments of sedimentation in channels by currents and waves.” Report S 347-II, Delft Hydraulics laboratory, Deflt, Netherlands.
  • Zhu, J. (1991). “A low diffusive and oscillation-free convection scheme”. Com. App. Num. Meth., 7, 225-232.
  • Zundel, A. K. (2000). “Surface-water modeling system reference manual”. Brigham Young University, Environmental Modeling Research Laboratory, Provo, UT.

External Links

  • Aug 2006 Two-Dimensional Depth-Averaged Circulation Model CMS-M2D: Version 3.0, Report 2, Sediment Transport and Morphology Change [1]
  • Aug 2008 CMS-Wave: A Nearshore Spectral Wave Processes Model for Coastal Inlets and Navigation Projects [2]

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