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Merging of RVR Meander with CONCEPTS: Simplified 2D Model for Long-Term Meander Evolution

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Merging of RVR Meander with CONCEPTS: Simplified 2D Model for Long-Term Meander Evolution River, Coastal and Estuarine Morphodynamics: RCEM 2009 – Vionnet et al. (eds) © 2010 Taylor & Francis Group, London, ISBN 978-0-415-55426-8 Merging of RVR Meander with CONCEPTS: Simplified 2D model for long-term meander evolution Davide Motta Department of Civil and Environmental Engineering, University of Illinois, Urbana-Champaign, Urbana, IL, USA Jorge D. Abad Department of Civil and Environmental Engineering, University of Illinois, Urbana-Champaign, Urbana, IL, USA Department of Civil and Environmental Engineering, University of Pittsburgh, PA, USA Eddy J. Langendoen US Department of Agriculture, Agricultural Research Service, National Sedimentation Laboratory, Oxford, MS, USA Marcelo H. Garcia Department of Civil and Environmental Engineering, University of Illinois, Urbana-Champaign, Urbana, IL, USA ABSTRACT: RVR Meander is a simplified two-dimensional (2D) hydrodynamic and migration model (Abad and Garcia, 2006) while CONCEPTS (CONservational Channel Evolution and Pollutant Transport System) is a one-dimensional (1D) hydrodynamic and morphodynamic model (Langendoen and Alonso, 2008; Langendoen and Simon, 2008; Langendoen et al., 2009). Originally, RVR Meander reported only the use of Ikeda et al. (1981)’s hydrodynamic model, where the bank migration (ξ) was modeled by using the concept of near bank excess velocity (ue). In this regard, the bank migration was expressed as ξ = ueEo, where Eo is a bank migration coefficient, calibrated upon historical centerlines. The bed morphology was not modeled according to the sediment mass conservation (Exner equation), but instead it was assumed that the transversal bed slope was directly related to local curvature. On the other hand, CONCEPTS uses an advanced treatment of the bank retreat. However, since CONCEPTS is a 1D model, it does not incorporate corrections for secondary flow and transversal bed slope: therefore its applicability to meander bends might underestimate the shear stress along the stream banks and consequently underpredict the migration rate. This paper shows the preliminary results of an ongoing effort to merge both models, with the goal of implementing a hydrodynamic and morphodynamic model capable of reproducing the flow field and the river migration for predicting long-term evolution needed in engineering and geological applications. 1 INTRODUCTION near bank excess velocity (ue) and a calibrated bank migration coefficient (Eo). In the updated version, the Figure 1 shows a typical configuration of river bed morphodynamics can also be computed with the migration. Herein, intrinsic coordinates are used models advanced by Blondeaux and Seminara (1985) (s∗: streamwise coordinate, n∗: transverse coordi- and Zolezzi and Seminara (2001), which incorpo- nate). The angular amplitude is given by θ. The width, rate the sediment mass conservation equation (Exner depth, water surface and bed elevation of the channel equation). Moreover, the routines implemented in are defined as 2B∗, D∗, H ∗ and η∗ respectively. Orig- the 1D CONCEPTS model for the bank evolution inally, RVR Meander included Ikeda et al. (1981)’s processes, i.e. fluvial erosion, cantilever and planar hydrodynamic model where the bed morphology is failure (Langendoen and Simon, 2008), were extracted not calculated by using the sediment mass conser- and introduced into the new platform. The result- vation equation (Exner equation), but instead it is ing updated version RVR Meander + CONCEPTS computed by assuming that the transversal bed slope can be applied to non-straight channels for engineer- is related to the local curvature by St =−ADC(s), ing and geological time scales and the modules for where A is a transversal slope parameter (Zimmerman bank evolution allow for a physically-based represen- and Kennedy, 1978; Odgaard 1981), and C(s) = tation of the migration process replacing the use of −∂θ(s)/∂s is the local curvature. The bank migration an empirical formulation based on excess near-bank (ξ = ueEo) was modeled by using the concept of velocity. 37 τ τ 2B* slope and s and n are the local bed shear stresses in A the streamwise and transverse directions left bank at t*+dt* (a) dt* Rc* 2 2 left bank at t* τ = (τs, τn) = (U, V )Cf U + V (4) A Cf is the friction coefficient, ρ is the water density, ν0 ∗/ ∗ ∗ valley centerline is B Rc (Rc is a reference radius of curvature), and s* βτs ∂U n* f =−nC(s) + V − C(s)UV (5) 11 D ∂n ∂V ∂H βτ right bank at t*+dt* =− C( ) + + n + C( ) 2 g11 n s V ∂ ∂ s U right bank at t* n n D (6) (b) left bank at t* CL right bank at t* ∂(VD) )retuo( )renni( m =−C(s) VD + n (7) 11 ∂n Do* D* Following linearization, the perturbed variables are: H* transversal slope (St) −a2s U1(s, n) = a1e + n a3C(s) + 2B* reference level s −a2s a2s +a4e C(s)e ds (8) 0 Figure 1. (a) Planform migration, (b) cross-section config- a1 − uration. Variables are given in dimensioned values. V (s, n) = a e a2s(n − 1) 1 2 2 a a + 2 (nu(s, n) − u(s,1)) + 5 (n2 − 1) 2 HYDRODYNAMIC AND BED 2 2 MORPHODYNAMIC MODELS (9) As mentioned, RVR Meander + CONCEPTS incorpo- 2 2 A D1(s, n) = χ F + C(s)n (10) rates several simplified 2D hydrodynamic and mor- 0 χ phodynamic models: the Ikeda et al. (1981)’s model, η ( ) =−A C( ) the Blondeaux and Seminara (1985)’s model, and the 1 s, n χ s n (11) Zolezzi and Seminara (2001)’s model. For the pur- pose of this paper, only the Ikeda et al. (1981)’s model 2 = ∗2/ ∗ χ = ( / )1/3 is presented. Starting from the streamwise and trans- where F0 U0 gH , S S0 , S is the chan- verse momentum equations and the water conservation nel slope and S0 is the valley centerline. The final equation: results in dimensionless variables are given as: ∂U ∂U ∂H βτs ( ) = + ν ( ) U + V + + = ν f (1) U s, n 1 0U1 n (12) ∂s ∂n ∂s D 0 11 V (s, n) = ν0V1(n) (13) ∂V ∂V ∂H τ U + V + + β n = ν g (2) ( ) = + ν ( ) ∂s ∂n ∂n D 0 11 D s, n 1 0D1 n (14) ∂(DU) ∂(DV ) η(s, n) = F2H(s, n) − D(s, n) (15) + = ν m (3) 0 ∂s ∂n 0 11 The curvature can be calculated with different The previous equations are expressed in dimen- methods: parametric, numerical θ/ s backward or ∗ ∗ ∗ ∗ sionless values, with β = B /D , (U, V ) = (U , V )/ central scheme, fitting a local circle or with parametric ∗ ( ) = ( ∗ ∗)/ ∗ = ∗/ ∗ = ∗/ ∗2 Uo , s, n s , n B , D D D0, H gH U0 , cubic splines. Details of those and of some of the above (τ τ ) = (τ ∗ τ ∗)/ρ ∗2 ∗ ∗ s, n s , n Uo , where Uo and D0 are the equations and implementation can be found in Abad velocity and depth for bed slope equal to the valley et al. (2009). 38 3 PHYSICALLY-BASED BANK EVOLUTION The planar failure, i.e. the failure of blocks along a planar failure surface, is solved using a limit equilib- The processes of fluvial erosion and mass bank failure rium method, which invokes the search for the smallest (cantilever and planar) were included in RVR Mean- factor of safety, which is the ratio of available shear der + CONCEPTS, following Langendoen and Simon strength to mobilized shear strength. (2008) and Langendoen et al. (2009). The evolution Details of the physically-based bank evolution pro- of both right and left bank is computed considering cesses, equations and modeling can be found in Lan- a natural bank profile and the presence of horizontal gendoen and Simon (2008) and Abad et al. (2009). layers characterized by different properties. The fluvial erosion rate E, in the horizontal direc- tion, for each of the layers in the left and right bank 4 COUPLING RVR MEANDER is modeled using an excess shear stress relation as AND CONCEPTS follows The migration distance of the centerline is calculated, (τ − τ ) at each node (i.e., cross section), considering the dis- = c E M τ (16) placement of the toes of the left and right bank. It is c assumed that all the material eroded from the bank goes into suspension and does not deposit (purely where M is the erosion rate coefficient and τc is the erosional regime). As a consequence, the channels critical shear stress. Both are characteristic of each widens, and, after every time step, the new width layer material. τ is the shear stress on the layer. Several used to recompute the hydrodynamics is taken as the methodologies are used to calculate the shear stress minimum in the reach. at natural cross sections and implemented into 1D As other meander migration models, in order to models (Lundgren and Jonsson, 1964; Khodashenas avoid the propagation of numerical errors related to and Paquier, 1999). The effect of secondary currents the computation of the channel curvature, two different in the near-bank shear stress was studied for straight and alternative techniques were implemented in RVR channels with trapezoidal cross sections (Knight et al., Meander + CONCEPTS. The first one is based on the 2007) and cohesive river banks (Papanicolaou et al., filtering of the curvature (Crosato, 2007) 2007). These methodologies are mostly applied to straight channels, therefore, their validation to apply C − + 2C + C + C = i 1 i i 1 (17) them to meandering configurations is necessary. i 4 Depending on the planform configuration and bed morphodynamics, the distributions of near-bed and where i−1, i and i+1 are consecutive nodes. The near-bank shear stresses could differ dramatically second is a Savitzky-Golay filter applied to the coor- from straight channels. At field scale, there are some dinates of the migrated centerline, which is essentially detailed measurements of in situ shear stresses, how- a generalization of the moving window averaging, ever, most of the time, these values reflect particular with an underlying function within the moving win- cases with no generalized findings.
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