The circulation in the Gulf of Maine has an important baroclinic component. It appears to be driven mostly by the density contrast between high‐salinity slope water which enters from the Atlantic and fresher waters which are formed in the Gulf or which enter from the Scotian shelf. Hydrographie surveys in three successive spring seasons suggest that slope water accumulates in Georges Basin, driving a counterclockwise surface circulation which brings Scotian shelf water westward into the Gulf and contributes to the eastward jet along the inner edge of Georges Bank. The slope water also crosses a sill and enters Jordan Basin, where it provides a potential energy source which may enhance a counterclockwise gyre partly driven by nearshore buoyancy sources and perhaps the wind. The coastal limb of the gyre turns offshore east of Penobscot Bay. Part of the separated coastal current recirculates in Jordan Basin, and part of it continues into Wilkinson Basin, generating a clockwise eddy as it passes over Jeffreys Bank. There is little evidence for recirculating surface flow in Wilkinson Basin. Instead, the surface water appears to split into branches feeding the Jordan Basin gyre, the Georges Bank jet, and an export path to Nantucket Shoals. The Jordan and Georges branches seem to be divided by the denser slope water in Georges Basin, and this may be the central process controlling the vernal intensification of the circulation in the Gulf. A more complete dynamical understanding awaits models which include the baroclinic influence of boundary waters.
Simultaneously measured Eulerian currents and spatially extensive subsurface temperatures have provided a time series of eight synoptic, three‐dimensional views of the Gulf Stream frontal zone along the Carolina continental margin. Two large‐amplitude meanders were observed to progress through the study area between Charleston and Cape Hatteras during February 1979. Each meander had a vertically coherent, skewed wave‐like subsurface structure. The Eulerian velocity and temperature signatures produced by the meanders at the 250‐m level over the 390‐m isobath reflect this skewness. At a particular instrument, the in‐phase increases in temperature and downstream velocity associated with an approaching meander crest occurred during a longer time interval than did the more rapid decreases in these quantities following the crest's passage. Typically, the downstream velocity component at this level fluctuated from about −20 cm s−1 to near 100 cm s−1, while the cross‐stream component varied approximately ±25 cm s−1 about a near‐zero mean. For a particular meander, the maximum in the offshore velocity component led the downstream maximum in time in a manner typical of progressive wave motions; however, the lead time was always less than one quarter of a meander period implying that u and υ were not in quadrature, as would have been the case for stable waves. The two meanders were observed downstream of the area off Charleston where a seaward deflection of the stream is often found. Subsurface temperature data from February 10, 1979, show that on that date the degree of deflection was greatest near the surface, and that almost no deflection existed within the deeper reaches of the water column. According to later data, the deflection decreased as the meanders progressed alongshore away from the area, suggesting that the vertical structure of the deflection observed on the tenth may have been associated with the late stages of a meander passage. Filaments of warm Gulf Stream water extended southwestward ‘behind’ the crests of the two meanders. The filaments were relatively shallow features, extending from the surface to a depth of a few tens of meters. They were oriented essentially parallel to the bottom contours over the outer shelf and upper slope, and were separated from the main body of the Gulf Stream by cool water. The presence of the cool water between the stream and the filaments at the surface was due to upwelling of water from deep within or below the main stream. Peaks in the time series of vorticity components indicate that maximum cyclonic relative vorticity occurred behind the meander crests, in the leading portion of the trough near where a warm filament joined a meander crest. The meanders may have been initiated upstream of our study area, and then ‘amplified’ by the deflection process off Charleston. Energy flux calculations for the region off Onslow Bay indicate that meander kinetic energy was being converted to mean energy there. It seems likely that the deflection produces meander growth within the 100...
The eastern Maine coastal current flows southwestward, carrying cold and nutrient-rich waters along the coast from the tidally stirred eastern gulf toward the central and western gulf, where in summer the~aters are warmer and more stratified. The current typically turns offshore before reaching Penobscot Bay, near the central coast, at a location determined largely by the distribution of dense slope water in Jordan Basin. The slope water, which enters the gulf as a deep inflow from the Atlantic Ocean, thus plays a major role in determining the intensity, direction and timing of the delivery of nutrients to the interior gulf. In this paper, we use data from two cruises in August 1987 to examine the variability and nutrient transport of the coastal current, especially to show the important physical linkages between the deep slope water, the structure of the coastal current, and its likely significant effect on biological productivity in the gulf.
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