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Modelling of Sediment Transport and Morphological Evolution Under the Combined Action of Waves and Currents

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Modelling of Sediment Transport and Morphological Evolution Under the Combined Action of Waves and Currents Ocean Sci., 13, 673–690, 2017 https://doi.org/10.5194/os-13-673-2017 © Author(s) 2017. This work is distributed under the Creative Commons Attribution 3.0 License. Modelling of sediment transport and morphological evolution under the combined action of waves and currents Guilherme Franz1, Matthias T. Delpey2, David Brito3, Lígia Pinto1, Paulo Leitão4, and Ramiro Neves1 1MARETEC, Instituto Superior Técnico, Universidade de Lisboa, Av. Rovisco Pais, 1049-001, Lisboa, Portugal 2Centre Rivages Pro Tech, SUEZ, 2 allée Théodore Monod, Bidart, France 3ACTION MODULERS, Estrada Principal, no. 29, Paz, 2640-583 Mafra, Portugal 4HIDROMOD, Rua Rui Teles Palhinha, no. 4, Leião, 2740-278 Porto Salvo, Portugal Correspondence to: Guilherme Franz ([email protected]) Received: 24 February 2017 – Discussion started: 21 March 2017 Revised: 17 July 2017 – Accepted: 25 July 2017 – Published: 7 September 2017 Abstract. Coastal defence structures are often constructed ter conditions and during events of highly energetic waves. to prevent beach erosion. However, poorly designed struc- The MOHID code is available in the GitHub repository. tures may cause serious erosion problems in the downdrift direction. Morphological models are useful tools to predict such impacts and assess the efficiency of defence structures 1 Introduction for different scenarios. Nevertheless, morphological mod- elling is still a topic under intense research effort. The pro- The morphological features of the coastal zone depend on the cesses simulated by a morphological model depend on model sediment characteristics and the combined action of waves complexity. For instance, undertow currents are neglected in and currents. Wind waves are the main energy source for coastal area models (2DH), which is a limitation for simulat- most beaches. Particularly in the surf zone, waves may in- ing the evolution of beach profiles for long periods. Model duce considerable changes in mean sea level and strong cur- limitations are generally overcome by predefining invariant rents (Longuet-Higgins, 1970a, b, 1983). The pattern of surf equilibrium profiles that are allowed to shift offshore or on- zone currents varies with the angle of waves approaching shore. A more flexible approach is described in this paper, the shore as well as with bathymetric heterogeneities, lead- which can be generalised to 3-D models. The present work ing to longshore and rip currents. Sediment is usually car- is based on the coupling of the MOHID modelling system ried shoreward during low wave conditions, mainly due to and the SWAN wave model. The impacts of different de- the asymmetry of waves in shallow waters (Myrhaug et al., signs of detached breakwaters and groynes were simulated in 2004). The sediment accumulated during these periods may a schematic beach configuration following a 2DH approach. be eroded very rapidly under high wave conditions during a The results of bathymetry evolution are in agreement with the major storm. Following these energetic events, the bottom patterns found in the literature for several existing structures. profile may recover its initial shape only if the longshore The model was also tested in a 3-D test case to simulate the transport of sediment during the storm is low. Different struc- formation of sandbars by undertow currents. The findings of tures such as breakwaters and groynes can prevent the along- this work confirmed the applicability of the MOHID mod- shore movement of sediment (e.g. Dally and Pope, 1986). elling system to study sediment transport and morphological Consequently, serious erosion problems in the downdrift di- changes in coastal zones under the combined action of waves rection may arise from the construction of these structures. and currents. The same modelling methodology was applied Morphological models are useful tools to assess the impact of to a coastal zone (Costa da Caparica) located at the mouth protection structures, enabling us to consider different wave of a mesotidal estuary (Tagus Estuary, Portugal) to evaluate conditions and structure designs. the hydrodynamics and sediment transport both in calm wa- Published by Copernicus Publications on behalf of the European Geosciences Union. 674 G. Franz et al.: Modelling of sediment transport and morphological evolution The complexity of morphological models ranges from approach may be more appropriate in order to consider the coastal profile models to 2- or 3-D models. Actually, mor- effect of non-uniform grain-size distributions on the overall phological models are usually a set of different models or sediment transport, through morphological models that ac- modules, depending on the chosen approach. Here the focus count for multiple sediment fractions. Grain-size sorting is is on the coupling of a spectral wave model with a phase- generally observed along the cross-shore beach profile, as averaged hydrodynamic and sediment transport model. Spec- well as in the longshore beach direction (Komar, 1998). Fur- tral wave models offer a representation of the physical pro- thermore, the method can be generalised to 3-D models for cesses related to the generation, propagation, and dissipation a better representation of sandbar slopes and to update the of waves (e.g. Booij et al., 1999). The wave-induced forces shoreline position. computed by a wave model can be provided to a hydrody- This paper is divided into five sections. A brief descrip- namic model in order to simulate wave-related phenomena, tion of the effect of waves in the nearshore hydrodynamics such as wave set-up, wave-induced currents, and mixing. On and sediment transport is given in Sect. 2. The numerical the other hand, the hydrodynamic model can return water modelling approach is presented in Sect. 3. The methodol- levels and currents to the wave model (e.g. Warner et al., ogy was verified for different test cases (Sect. 4). Firstly, the 2008). Additional processes can be considered in the hy- morphological evolution of a schematic beach was evaluated drodynamic model, such as wind action, tidal motion, and for different designs of coastal defence structures (detached river discharges. The transport of suspended sediment may breakwaters and groynes) following a 2DH model configu- be simulated by an advection/diffusion model. The mech- ration. The model was applied later in a 3-D configuration anism of erosion/deposition of sediments is controlled by for the same schematic beach to verify the development of the bed shear stress induced by currents and waves. The sandbars. Finally, the numerical modelling methodology was bathymetry evolution resulting from the total sediment trans- applied to assess the hydrodynamics and sediment transport port (suspended load and bed load) affects the patterns of under extreme wave conditions in a coastal zone (Costa da currents and waves. Due to the interdependence of the phys- Caparica) located at the mouth of a mesotidal estuary (Tagus ical processes involved in sediment dynamics, all of these Estuary, Portugal). The main conclusions found from these models must be coupled. test cases are discussed in Sect. 5. The hydrodynamics inside the surf zone is influenced by important 3-D effects. Due to the absence of 3-D processes (e.g. undertow), coastal area models (2DH) fail to reproduce 2 Background a consistent evolution of beach profiles for long periods. This shortcoming can be overcome by predefining invariant equi- The effect of breaking waves on the mean sea level (wave librium profiles. In this case, the equilibrium profile only set-up) has been known since the laboratory measurements shifts offshore or onshore depending on the overall sediment performed by Saville (1961), confirmed further by Bowen et balance along the profile, similarly to a coastal profile model al. (1968). This tilt of the mean sea level is explained by the (e.g. Kriebel and Dean, 1985; Kristensen et al., 2013). As the horizontal flux of momentum carried by waves or, equiva- sediment transport in the swash zone is usually neglected in lently, by the radiation stress, a vertically integrated momen- large-scale 2DH models, this approach also has the advan- tum flux whose gradient balances the wave set-up (Longuet- tage of updating the shoreline position. However, limitations Higgins and Stewart 1962, 1964). In the surf zone, wave arise when a structure is present in the surf zone. Moreover, heights and orbital velocities decrease towards the shore due the processes responsible for sandbar evolution are not con- to wave breaking. As a consequence, the radiation stress also sidered. Attempts to simulate sandbar dynamics have been decreases, resulting in a force directed towards the shore. performed generally with cross-shore 2-D (2DV) and quasi- This force is balanced by a hydrostatic pressure gradient that 3-D models (e.g. Drønen and Deigaard, 2007; Ruessink et increases the mean sea level onshore. al., 2007). Nevertheless, the proper reproduction of sandbar Breaking waves can also drive strong currents in the surf migration is still an active topic of research (e.g. Dubarbier et zone, which are important for sediment transport and mor- al., 2015). Inaccuracies in the cross-shore sediment transport phological evolution in the coastal zone. The horizontal mass may degrade the coastal profile, which is a restriction for the transport associated with waves, or Stokes drift, is oriented simulation of long-term morphological evolution. shoreward and vertically sheared, being more intense at the In this work, we test a more flexible approach to overcom- surface (e.g. Ardhuin et al., 2008). As a result, mass conser- ing the 2DH model limitations in order to simulate morpho- vation in the nearshore is satisfied by a seaward transport in logical evolution for long periods. Instead of fixing an equi- the lower part of the water column, called undertow, which librium profile to update the bathymetry and shoreline posi- has an important role in sandbar formation. The undertow is tion, we defined a maximum slope that when surpassed gen- strongest in steep beaches and may be insignificant for mod- erates sediment transport in the downslope direction.
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