In some coastal areas, the hydrodynamic conditions involving wave-current interaction are extremely complex. Strong tidal currents affect wave transformation. Normally, tidal and wind-driven circulation and wind wave generation and transfor- mation are modeled in separate process models. The independent modeling of wave transformation and circulation can not predict the complicated coastal process very well in lack of considering the interaction between the two processes. In order to
take into account the interaction between the waves and currents, the coupling of ROMS and SWAN models is developed.
4.2.1 Shelf Circulation Model ROMS
The Regional Ocean Model System (ROMS) is a three-dimensional numer- ical ocean model, which simulates currents, ecosystems, biogeochemical cycles and sediment movement in various coastal regions. ROMS solves the primitive equations in an Earth-centered rotating environment with the Boussinesq approximation and hydrostatic vertical momentum balance. It uses stretched, terrain-following coordi- nates in the vertical and orthogonal curvilinear coordinates in the horizontal. Ini- tially, the S-coordinate Rutgers University Model (SCRUM) was developed by Song and Haidvogel (1994). Later, ROMS was completely rewritten to include high- order advection schemes, accurate pressure gradient algorithms, several subgrid- scale parameterizations, atmospheric, oceanic, and benthic boundary layers, bio- logical modules, radiation boundary conditions and data assimilation (Shchepetkin and McWilliams, 2005).
In the model domain of Delaware Bay and its adjacent ocean region, ROMS is driven by M2, N2, S2, K2, O1, K1 and Q1 tides at the offshore boundary (Personal communication with Long Xu). The solid line in Figure 4.29 shows water depth- averaged tidal current velocities calculated by ROMS in east-west and north-south components at the measuring station during October 27 through October 29, 2003, which is compared to the measured data from ADCP (circles). The simulated results agree well with the measured data except a little overestimation in east-west component. Since the M2 tide dominates in this process, the period of the current velocity is about twelve hours.
4.2.2 Coupling the Model Systems
In this study, the traditional file I/O method is used to couple ROMS and SWAN. First, ROMS is driven by the tide at the offshore boundary. The water depth-averaged current velocities calculated by ROMS are stored in files for the desired periods, which are used as input files for SWAN.
The tidal current at 20:00 October 27 in the whole model domain is shown in the right panel of Figure 4.30. This current field is applied to SWAN simulation. The left panel of Figure 4.30 is the spatially variable wind field at this time. Figure 4.31 shows the Hs with (right panel) and without (left panel) currents based on this
wind field. Since the current is very small on the ocean shelf, it does not affect Hs
much. In the upper bay, current and wind are almost perpendicular each other, so there is not much change due to the current. In the middle of the bay, the current has the similar direction as wind, which makes the Hs decrease in the bay. The %
difference in Figure 4.32 also shows this trend. The Tp distributions in the model
domain with and without current field are presented in Figure 4.33. According to the % difference shown in Figure 4.34, the current affects theTp much near shore. In
Figure 4.35, blue diamond stands for the results with tidal current field on spatially variable wind field, and the red cross stands for the ones without current field. The data measured by waverider buoy at the measuring station is represented by black circle. Both of the Hs andTp decrease due to the current. Hs with current is closer
to the measurement, but Tp deviates more.
Another current field at 03:00 October 28 is presented at the right panel of Figure 4.36. The current is still small on the ocean shelf. At the mouth of the bay, the current is bigger and opposite to wind, which increases Hs. In the upper and
middle of the bay, the current has the same direction as the wind, which makes Hs
decrease. The details of the change of Hs between the left panel and right panel
are presented in Figure 4.39 and the % difference is shown in Figure 4.40. As for the measuring station in Figure 4.35, Hs does not change and matches well with
the measurement. While the Tp with current deviates more than the one without
current.
Finally, the current field at 00:00 October 29 is chosen in the right panel of Figure 4.41. Most of the currents are offshore. Again, the currents on ocean shelf are too small to affect the wind-generated waves much. In Figure 4.43, the % difference of the two distributions in Figure 4.42 shows Hs increases much in the middle and
the mouth of the bay due to the current existance. Tp only changes a little on the
boundary in the middle of the bay as shown in Figure 4.44 and Figure 4.45. These trends are also shown in Figure 4.35.