Comprehensive coastal circulation model with application to the Gulf of Maine

Lynch, Daniel R.; Ip, J.T.C.; Naimie, Christopher E.; Werner, Francisco E.

doi:10.1016/0278-4343(95)00028-3

Cited by 242 publications

(177 citation statements)

References 64 publications

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“…[13] The finite element model of Janeković and Kuzmić [2005] is based on the 3-D, nonlinear, shallow water equations [Lynch et al, 1996] with no stratification. The Figure 1.…”

Section: Numerical Modelmentioning

confidence: 99%

Tidal currents in the northwestern Adriatic: High‐frequency radio observations and numerical model predictions

et al. 2007

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[1] A 2-year deployment of high-frequency radio current meters along the Italian coast of the northwestern Adriatic is used to characterize the surface tidal currents. In the middle of the basin, the M 2 and K 1 currents oscillate along the basin axis, but become more circular toward the Italian coast. Comparisons with a 3-D finite-element nonlinear numerical model of the tides show a good agreement for phases in the middle of the basin, although modeled currents amplitudes are overestimated. However, modeled phases lag observed phases by up to 50°(1.7 hours) for M 2 and 100°(6.7 hours) for K 1 , and modeled amplitudes are underestimated, in a 10-20 km wide strip along the Italian coast. This shallow (< 30 m deep) region is stratified by low-salinity surface water from the Po, and laterally sheared by the Western Adriatic Current, both absent from the model but possibly affecting tidal propagation. The model may also incompletely parameterize the combined effects of bottom friction and vertical mixing of momentum.

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“…[13] The finite element model of Janeković and Kuzmić [2005] is based on the 3-D, nonlinear, shallow water equations [Lynch et al, 1996] with no stratification. The Figure 1.…”

Section: Numerical Modelmentioning

confidence: 99%

Tidal currents in the northwestern Adriatic: High‐frequency radio observations and numerical model predictions

et al. 2007

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“…Few applications of the FEM to steady-state ocean inverse problems (Brasseur, 1991;Schlichtholz and Houssais, 1999;Dobrindt and Schr€ o oter, 2002a,b;Nechaev et al, 2003) appeared. Some existing two-dimensional (2D) FE shallow water tide models have been generalized by accounting for the dependence on the vertical coordinates with the FDM (Westerink et al, 1992;Lynch and Naimie, 1993) and by including heat and salt advection (Lynch et al, 1996). But they are exclusively used in modelling the coastal dynamics for relatively short time periods (up to few months).…”

Section: Introductionmentioning

confidence: 99%

A finite-element ocean model: principles and evaluation

2004

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We describe a three-dimensional (3D) finite-element ocean model designed for investigating the largescale ocean circulation on time scales from years to decades. The model solves the primitive equations in the dynamical part and the advection-diffusion equations for temperature and salinity in the thermodynamical part. The time-stepping is implicit. The 3D mesh is composed of tetrahedra and has a variable resolution. It is based on an unstructured 2D surface mesh and is stratified in the vertical direction. The model uses linear functions for horizontal velocity and tracers on tetrahedra, and for surface elevation on surface triangles. The vertical velocity field is elementwise constant. An important ingredient of the model is the Galerkin least-squares stabilization used to minimize effects of unresolved boundary layers and make the matrices to be inverted in time-stepping better conditioned. The model performance was tested in a 16-year simulation of the North Atlantic using a mesh covering the area between 7°and 80°N and providing variable horizontal resolution from 0.3°to 1.5°.

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“…The along-front component, dominated by the thermal-wind shear and tidal rectification, has well been studied by theoretical and modeling studies [Loder, 1980;Garrett and Loder, 1981;Loder and Wright, 1985;Naimie et al, 1994;Naimie, 1996;Lynch et al, 1996;Chen and Beardsley, 1998;Ou, 1999Ou, , 2000Chen et al, 2003] and field observations [Butman and Beardsley, 1987;Loder and Brickman, 1992;Loder et al, 1993;Limeburner and Beardsley, 1996]. In contrast, due in part to its much weaker magnitude (1 -3 cm/s, one order smaller than the along-shore flow), the cross-front component is less well understood and more complicated.…”

Section: Introductionmentioning

confidence: 99%

Numerical study of the diapycnal flow through a tidal front with passive tracers

Houghton

Chen

et al. 2004

J. Geophys. Res.

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[1] A two-dimensional numerical model is used to study the diapycnal flow through a tidal front with passive tracers. In a basic numerical experiment a passive tracer is released into the bottom water at the offshore edge of a tidal front, and it subsequently moves on-bank with a velocity that decreases with time. This qualitatively agrees with a recent field experiment using a dye tracer on Georges Bank. Additional experiments are performed to investigate the sensitivity of the tracer dispersion to the tidal phase and the location of tracer release within the front. As the release point is moved on-bank across the front, the tracer velocity decreases until it weakly reverses on the on-bank edge of the front. This trend can be understood by considering the structure of the Lagrangian velocity field in the tidal front, the degree of vertical mixing of the tracer, and the concentrationweighted mean patch velocity. The tidal phase at the time of tracer release does not significantly affect the tracer dispersion.

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Comprehensive coastal circulation model with application to the Gulf of Maine

Cited by 242 publications

References 64 publications

Tidal currents in the northwestern Adriatic: High‐frequency radio observations and numerical model predictions

Tidal currents in the northwestern Adriatic: High‐frequency radio observations and numerical model predictions

A finite-element ocean model: principles and evaluation

Numerical study of the diapycnal flow through a tidal front with passive tracers

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