An Observational and Numerical Investigation of Mesoscale Coastal Processes during Gale Iop 2

Details An Observational and Numerical Investigation of Mesoscale Coastal Processes during Gale Iop 2 An Observational and Numerical Investigation of Mesoscale Coastal Processes during Gale Iop 2

Feb 1991

adsabs.harvard.edu/cgi-bin/nph-data_query?bibcode=1991phdt........60d&link_type=abstract

Thesis (PH.D.)--THE PENNSYLVANIA STATE UNIVERSITY, 1991.Source: Dissertation Abstracts International, Volume: 52-04, Section: B,

Physics

Genesis Of Atlantic Lows Experiment, Coastal Processes

Scientific paper

A detailed analysis of the conventional and special observations taken during Intensive Observation Period 2 (IOP 2) of the Genesis of Atlantic Lows Experiment (GALE), and results from one- (1-D), two- (2-D), and three-dimensional (3-D) numerical model simulations using idealized and observed data are used to examine the structure, evolution, dynamics, and interactions of the coastal low-level jet (LLJ), marine atmospheric boundary layer (MABL), coastal front, and coastal cyclone, during a 72-h period between 23-26 January 1986. In one series of experiments, the Penn State/National Center for Atmospheric Research (PSU/NCAR) mesoscale model is initialized with idealized data to study the MABL near the Gulf Stream. Important contributors to the MABL response and frontal structure are the horizontal resolution of the sea surface temperature analysis, latent heat release in the lower troposphere, sea-surface fluxes of moisture, and high wind speeds near the MABL front. During GALE IOP 2, a diurnally varying, low-level northeasterly jet was observed along the Carolina Coastal Plain. Results from a 3-D real-data simulation and from a 1-D planetary boundary layer model show that the LLJ is a manifestation of strong low-level geostrophic forcing, with its strength and direction modulated by inertial accelerations. A large daytime speed reduction results from a rapid increase in the frictional stress at the jet level. Coastal frontogenesis takes place near the eastern edge of the Gulf Stream, coincident with a preexisting low-level coastal trough. Large sensible heat and moisture fluxes, present along the Gulf Stream, contribute directly to the trough formation. The ageostrophic deformation associated with the coastal trough formation may initiate the coastal frontogenesis. In the formative stage of the coastal front, the frontogenetical deformation over the Gulf Stream is opposed by the frontolytical differential diabatic effects. As the coastal front moves near the coastline, the deformation and differential diabatic terms act ln concert to intensify the baroclinic zone. Along the coastal front, a small-scale, shallow, warm-core cyclone develops in a region of weak quasi-geostrophic forcing. The baroclinic zone to the rear of the cyclone is substantially weakened and embedded in an environment less conducive for subsequent rapid cyclogenesis.

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