74 PEOCEEDIXGS OF THE SAINT LOUIS MEETING 



origin of the bulk of the deposit. At such localities not uncommonly faunules 

 of laud gastropods are found in the loess, consisting of characteristically mois- 

 ture-loving, forest types which are in pronounced contrast to the typical loess 

 fauna which is generally considered to point to treeless, more or less steppe- 

 like, vegetation. That even under present climatic conditions the winds in 

 that portion of the Rhine Valley are competent to carry on the deposition of 

 loess is indicated by the fact that repeatedlj' during exceptional storms in 

 summer-time dust lodges in conspicuous quantity on the roof of the astro- 

 nomical observatory at Heidelberg, at an elevation of some 1,500 feet above 

 the plain, on top of the forest-covered slopes of the faultscarp. 



LATE PLEISTOCENE SHORELINE IN MAINE AND NEW HAMPSHIRE 

 BY FRANK J. KATZ 



(AJ)stract) 



In the coastal region of southwest Maine and southeast New Hampshire 

 there are uplifted beaches and deltas which lie higher than late Wisconsin 

 marine clay deposits in their immediate vicinity. The beach phenomena, in- 

 cluding wave-cut cliffs, wave-built terraces, and sand and cobble bars built on 

 what were evidently prominently exposed islands and headlands, are strongly 

 developed. A group of notable features of this character in Rockingham and 

 Strafford counties. Ncm^ Hampshire, and York County. Maine, and a second 

 group in Cumberland County, Maine, were examined and their elevations were 

 determined. Deltas in the valleys of Isinglass, Cocheco, Mousam, Ossippes, 

 Saco, and Little Androscoggin rivers were also examined and found to lie at 

 elevations accordant with those of the beaches. In height the beaches range 

 from 155 feet in Stratham. New Hampshire, to 300 feet in Pownal. Maine, and 

 the deltas from 20O feet in Dover, New Hampshire, to 300 feet in Paris. Maine, 

 and all are coincident with an approximately plane surface, sloping five to six 

 feet to the mile in a direction 40° east of south — in other words, the isobases 

 trend north 50° east, approximately parallel to the general trend of the north 

 shore of the Gulf of Maine. The 300-foot isobase passes through Milton, New 

 Hampshire, and the 200-foot isobase through Dover, New Hampshire, and 

 South Portland, Maine. If the slope is constant, the isobase zero is in the 

 vicinity of Salem, Massachusetts. In this territory many allied features have 

 been noted but not closely examined, nor have their elevations been reliably 

 determined. It is plain that some of the shoreline features in the region fall 

 below the surface indicated above, and it is also certain that none of them are 

 higher. 



The result here announced does not accord with the eastward extension of 

 the amount of uplift and the altitude of the uplift marine plane advocated to 

 explain the phenomena in- the Connecticut River valley and the Long Island 

 region. However, conclusions for the two regions are not irreconcilable, if it 

 can be established that the wave of uplift that followed the withdrawal of 

 the ice approximately parallel the continental border, or, what amounts to 

 the same thing, if there was a local center of uplift around Miiich the isobases 

 curve. 



Rear] by title in the absence of the autlior. 



