appear to coincide with increased northward surface flow. Monthly mean 

 Sverdrup transport was computed across the North Atlantic between 15°N and 

 35°N. When compared at the same latitude, residual sea- level and Sverdrup 

 transport, both interpreted as indices of Gulf Stream transport, generally 

 disagree in phase during summer. However north of the Florida Channel they 

 are consistent during winter, assuming that lower sea- level at this time 

 reflects increased flow in the stream. (Author). 



022 BLAHA, J., and STURGES , W. 1987. "Slope of Sea-Level from Miami to 

 Atlantic City," Journal of Physical Oceanography . Vol 17, pp 177-184. 



Results of land leveling do not agree with oceanographers ' expectations 

 concerning coastal slopes of sea- level. Recent studies have shown that along 

 the west coast of the United States this discrepancy can be explained by the 

 vertical movement of leveling benchmarks. On the east coast, where the 

 movement of benchmarks is not expected, land leveling suggests that sea- level 

 should rise as much as 30 cm from Miami, Florida, to Charleston, South 

 Carolina. However, oceanographers find that sea- level falls, from south to 

 north, approximately 15 cm along the shoreward edge of the Gulf Stream. The 

 discrepancy between these findings could be explained if oceanographic effects 

 that support large alongshore slopes, and that arise primarily on the 

 continental shelf, could be identified. We examine coastal wind stress and 

 runoff as two such forcing mechanisms. To do this, we derive a statistical 

 model of the alongshore change of sea-level between tide gages, based on the 

 alongshore momentum equation. The computed mean sea- level differences are 

 only 1-2 cm between pairs of tide gages, and the signs change from one pair of 

 stations to the next. The conclusion is that the forcing mechanisms that we 

 have studied cannot explain the slopes found by land leveling. 



The model is able to predict the seasonal variation of slope between 

 Charleston and Fernandina and between Atlantic City and Norfolk. The observed 

 differences (-8 cm) compare well with the model -computed differences between 

 these sites. Thus, along these sections of coastline, close to shore, we 

 conclude that the seasonal variations of slope seem to be forced largely by 

 coastal winds. On the other hand, only half of the seasonal range observed 

 between Fernandina and Miami and between Norfolk and Charleston could be 

 modeled as effects of wind stress and runoff. The effects of other forcing 

 mechanisms may be more important in these areas. (Authors). 



023 BLOOM, A. L. 1959. "Late Pleistocene Changes of Sea-Level in 

 Southwestern Maine," Office of Navel Research, Project No. NR 388-040, pp 143. 



The evidence of late Pleistocene marine submergence of the coastal plain 

 of southwestern Maine consists primarily of a sheet of gray, silty clay, 

 containing a cold-water marine fossil fauna. The name "Presumpscot Formation" 

 is proposed for this sediment, from exposures in the Presumpscot River Valley 

 near Portland, Maine. In the eastern one-third of the area, the Presumpscot 

 Formation unconf ormably overlies glacial drift, and is known from well logs to 

 overlie drift at depths of at least 60 ft below present sealevel; an interval 

 of subaerial exposure of the deglaciated landscape prior to submergence is 

 indicated. This area of postglacial marine submergence coincides with an area 

 of inferred southward flow of glacier ice. 



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