Mid-Atlantic Bight. Transport over a Long Shallow Shelf. The Shelf. ~ 25m depth at the inner shelf ~ 50m at midshelf ~ 200m at the shelf break, where it then drops rapidly to deep ocean (1 Degree Longitude ~ 85.4km @ 40N) The distance shore to shelf break ranges from 60-200km.
Transport over a Long Shallow Shelf
~ 25m depth at the inner shelf
~ 50m at midshelf
~ 200m at the shelf break, where it then drops rapidly to deep ocean
(1 Degree Longitude ~ 85.4km @ 40N)
The distance shore to shelf break ranges from 60-200km
Chesapeake Bay system
K_M - vertical eddy viscosity
K_H - vertical eddy diffusivity
Density taken from the Equation of State
Salinity is constant
Horizontal eddy viscosity and diffusivity are constant
K_M terms calculated for surface wind stress and bottom stress given by D
L= 65km (width of shelf)
Wind Stress is the primary mechanism for transport.
Integrated continuity equation can be used to demonstrate the surface and bottom stress is directly related to across shore transport while inversely related to along shore divergence.
Shallow Shelf allows for fresh water intrusions to reach the bottom instead of forming a lens.
Supports geostrophic, cyclonic flow of high downshelf velocity.
High shear across shore.
These intrusions become displaced offshore and mix while the region experiences upwelling at the coast.
The buoyancy intrusion's flow is driven by stratification gradients (dN^2/dy) creating velocity gradients along shore.
Negative gradient indicates convergence with the intrusion upshelf.
Positive gradient indicates divergence with the intrusion downshelf.
While wind dominates the buoyancy intrusion under strong wind conditions, divergence may still be strong under light wind conditions.
Across-Shelf Transport on a Continental Shelf: Do Across-Shelf Winds Matter?
Three-Dimensional Flow in a Shallow Coastal Upwelling Zone: Alongshore
Convergence and Divergence on the New Jersey Shelf
Tilburg and Garvine 2003
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