Showing papers by "Kenneth H. Brink published in 1998"

The global coastal ocean : regional studies and syntheses

Abstract: Partial table of contents: PANREGIONAL OVERVIEWS Western Ocean Boundary Shelves (J. Loder, et al.) Polar Ocean Boundaries (T. Royer & P. Stabeno) REGIONAL OCEANOGRAPHY Intra-Americas Sea Circulation (3,W) (C. Mooers & G. Maul) Coastal Ocean Circulation Off Western South America (6,E) (P. Strub, et al.) Coastal Oceanography of Western North America from the Tip of Baja California to Vancouver Island (8,E) (B, Hickey) Coastal Processes in the Northern North Pacific (9,P) (T. Royer) The Celtic Seas (19,E) (J. Simpson) Continental Shelf of the Bering Sea (24,P) (J. Schumacher & P. Stabeno) The Black Sea (28,S) (E. Vzsoy & \. l ata) Seas of the Arabian Region (29,S) (C. Sheppard & D. Dixon) Index.

Variability of the near-surface eddy kinetic energy in the California Current based on altimetric, drifter, and moored current data

Abstract: Low-pass-filtered velocities obtained from World Ocean Circulation Experiment (WOCE) surface drifters deployed in the California Current off northern California during 1993-1995 have been compared with surface geostrophic velocity estimates made along subtracks of the TOPEX/POSEIDON altimeter and with moored acoustic Doppler current profiler (ADCP) data. To obtain absolute geostrophic velocities, a mean sea surface height (SSH) field was estimated using the mean drifter velocities and historical hydrographic data and was added to the altimetric SSH anomalies. The correlation between collocated drifter and altimetric velocities is 0.73, significant at the 95% level. The component of the drifter velocity which was uncorrelated with the altimetric velocity was correlated with the wind in the Ekman transport sense. Monthly averages of eddy kinetic energy (EKE), estimated using all drifter and altimeter data within the domain (124°-132°W, 33°-40.5°N), show energy levels for the drifters that are about 13% greater than those for the altimeter. Drifter, altimeter, and ADCP measurements all exhibit similar seasonal cycles in EKE, with the altimeter data reaching maximum values of about 0.03 m 2 s -2 in late summer/fall. Wavenumber spectra of the altimeter velocity indicate that the velocity fluctuations were dominated by features with wavelengths of 240-370 km, while the ADCP data suggest that the temporal scales of these fluctuations are at least several months. Between 36° and 40.5°N, the region of monthly maximum EKE migrates westward to about 128°W on a seasonal timescale. This region of maximum EKE coincides with the maximum zonal SSH gradient, with increased EKE associated with increased southward flow. A simple model shows that much of the seasonal cycle of the SSH anomalies can be produced by linear processes forced by the curl of the wind stress, although the model cannot explain the offshore movement of the front.

Monsoons boost biological productivity in Arabian Sea

Abstract: Monsoons over the Arabian Sea—the oceanic basin that separates the Arabian peninsula from the Indian subcontinent—follow seasonal cycles, reversing directions twice a year, in summer and winter. Rather than spreading across the expanse of the sea, the southwest (summer) monsoon is often concentrated into a jet over the central Arabian Sea. Evidence suggests that variations in wind stress force substantial upwelling in the ocean to the west of the jet, and weaker upwelling or even downwelling to the east. This upwelling provides nutrients to the euphotic zone and enhances biological productivity.

The global coastal ocean : processes and methods

Abstract: PHYSICAL AND DYNAMICAL PROCESSES Wind-Driven Currents Over the Continental Shelf (K. Brink) Buoyancy Effects in Coastal and Shelf Seas (A. Hill) Topographic Effects, Straits and The Bottom Boundary Layer (J. Trowbridge, et al.) Air Sea Interaction in the Coastal Zone (G. Geernaert & S. Larsen) Tidal Processes in Shelf Seas (J. Simpson) Deep-Sea Forcing and Exchange Processes (K. Brink) GLOBAL AND INTERDISCIPLINARY PROCESSES Sea Ice Processes and Water Mass Modification and Transport over Arctic Shelves (G. Gawarkiewicz, et al.) Sea Level Change (R. Stewart, et al.) Evaluation and Comparison of the Global Carbon Cycle in the Coastal Zone and in the Open Ocean (R. Wollast) Sediment Transport and Terrigenous Fluxes (Y. Wang, et al.) Recruitment and the Population Dynamics Process (B. Rothschild & M. Fogarty) MODELS AND DATA Remote Sensing (J. Nihoul, et al.) Hydrographic Observations in the Coastal Ocean (K. Brink) Current and Water Property Measurements in the Coastal Ocean (T. Dickey, et al.) Boundary Flux Measurements in the Coastal Ocean (W. Brown) Empirical Modal Decomposition in Coastal Oceanography (H. von Storch & C. Frankignoul) Numerical Models of the Coastal Ocean (D. Haidvogel & A. Beckmann) Coupled Physical, Chemical and Biological Models (J. Nihoul & S. Djenidi) Overview of Interdisciplinary Modeling for Marine Ecosystems (E. Hofmann & C. Lascara) Index.

Comments on "The non-wavelike response of a continental shelf to wind" by G. T. Csanady

Abstract: 2. Offshore boundary condition There is nothing arbitrary about the appropriate choice of boundary condition at x 5 l (where the topography meets the  at-bottom deep ocean). This point was dealt with clearly by Buchwald and Adams (1968), Gill and Schumann (1974), and Allen (1976b), for example. The cross-shelf transport and the pressure must be continuous at x 5 l. This implies that cross-shelf velocity must be continuous if depth h and wind stress G are continuous. Hence, from Csanady’s equation (1), both components of the pressure gradient, z x and z y must be continuous at x 5 l. This in turn implies that pressure and its derivative normal to the boundary, z and z x must be continuous at x 5 l. Csanady’s condition 1 ( z deŽ ned as zero offshore) allows z to be continuous, but not z x. His second (channel) condition causes pressure to be discontinuous at x 5 l, another unsatisfactory property. His third condition is the traditional z x 5 0 at x 5 l, which allows both z and z x to be continuous. Csanady (1998) advocates that pressure approach zero far from shore in the ‘‘boundary layer’’ or ‘‘long wave’’ approximation.This is equivalent to taking limits—far offshore vs. long wave—in the wrong order, as we now demonstrate. Once the long-wave approximation is made, Csanady’s (4) reduces to