proposed here and suggest that the curve may be applicable for much of the 

 inner Continental Shelf off the northeastern United States. 



The proposed sea-level-rise curve indicates that relative sea-level was 

 about 70 m below its present level 12,000 year ago. From that time to about 

 10,000 year ago, sea-level rose at a rate of 1.7 m/100 year. Between 

 10,000 and 6,000 year ago, the rate of sea- level rise dropped gradually to 

 about 0.3 m/ 100 year and remained at that rate until about 2,000 year ago. 

 From then until now, the rate of sea- level rise has been about 

 0.01 m/100 year. (Authors). 



255 OLSSON, R. K. 1988. "Foraminiferal Modeling of Sea-Level Change in 

 the Late Cretaceous of New Jersey," Wilgus, C. K. , Hastings, B. S., Kendall, 

 C. G. , Posamentier, H. W. , Ross, C. A. , and Van Wagoner, J. C. , eds . , Sea- 

 Level Changes: An Integrated Approach . Special Publication No. 42, Society of 

 Economic Paleontologists and Mineralogists, Tulsa, OK, pp 289-298. 



Paleoslope models of foraminifera in the Upper Cretaceous of the New 

 Jersey coastal plain are utilized to estimate paleobathymetric change during 

 cycles of rising and falling sea-level. The paleoslope method estimates 

 change in sea- level from the distribution of foraminiferal assemblages and 

 species on a baseline parallel to the regional dip. The paleoslope is the 

 restoration of the original depositional slope. Application of the paleoslope 

 model to the Carapanian of New Jersey indicates a maximum rise of sea- level of 

 90 m and 80 m, respectively, during two cycles of sea-level change. By 

 extension, a paleodepth curve is derived for the other cycles in the Late 

 Cretaceous. Eight cycles are recognized in the Late Cretaceous section of New 

 Jersey. (Author). 



256 ORSON, R. , PANAGEOTOU, W. , and LEATHERMAN, S. 1985. "Response of Tidal 

 Salt Marshes of the U.S. Atlantic and Gulf Coasts to Rising Sea-Levels," 

 Journal of Coastal Research . Vol 1, No. 1, pp 29-37. 



A salt marsh responds in many diverse ways to a rising sea-level. A 

 major factor is its ability to maintain surface elevations with respect to the 

 mean high water level. Other influences include local submergence rates, 

 sedimentation rates, density and composition of the indigenous flora, and type 

 and intensity of cultural modifications. If sea-level rise accelerates, it 

 would be reasonable to assume that further stresses will be placed on these 

 systems, most likely resulting in increased losses. If the relative rate of 

 sea-level rise reaches catastrophic proportions (exceeding 10 mm year'), sub- 

 stantial reductions in wetland area and a corresponding increase in open water 

 habitats is projected. Due to the complex interrelationship of natural pro- 

 cesses and cultural alterations that have previously influenced marshes, it is 

 difficult at the present time to separate and identify responses. Thus, each 

 marsh must be assessed individually until we have a more thorough 

 understanding of these systems in general. (Authors). 



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