306 ANNU.VL EEPORd? SMITHSONIAN INSTITUTION, 19 3 



straw, also appear diagramed and described in his report as graphs 

 labeled New Haven, C2, C3, Plate II. 



In Figure 2 appears an example of the correlation which Reeds 

 has made of the varves occurring in five separate clay pits at Haver- 

 straw, N. Y. Seventy varves, with field numbers +20 to +90, serial 

 numbers 231-301, appear on this diagram. The thickness of the 

 " summer " and " winter " layers in each varve has been differen- 

 tiated, the " winter " band being represented by a black shading, 

 the " summer " layer by the ruled vertical line extending from the 

 base line upward to the beginning of the winter layer in each sec- 

 tion. Five such graphs, one for each pit, appear on the diagram. 

 As the curves closely simulate one another in their oscillations, the 

 correlation may be said to be firmly established. The thickness of 

 the varves in each graph has been averaged and the mean for each 

 determined, as follows: Hornbecker pit, 14.8 mm.; Dunnegan pit, 

 15.1 mm.; Washburn-Fowler pit, 23.9 mm.; Morrisey pit, 26.0 

 mm.; Renn and Archer pits, 27.4 mm. This variation in thickness 

 of the deposits is attributed primarily to their location and elevation, 

 during the deposition of the clay. The Hornbecker and Dunnegan 

 pits, which are a quarter of a mile apart in west Haverstraw, have 

 been cut into the 60-foot escarpment, which is one-half mile distant 

 from the Hudson River. The Washburn-Fowler pit, a quarter of a 

 mile long, stretches lengthwise from near the floor of the Dunnegan 

 pit eastward on the flood plain of the Hudson River. The Morrisey 

 and Renn-Archer pits are deep ones, appearing south of Jones Point, 

 near the Hudson River front, in Haverstraw. They are fully a mile 

 southeast of the Hornbecker, Dunnegan, and Washburn-Fowler pits, 

 in West Haverstraw. The Haverstraw deposits, when contrasted 

 with those in West Haverstraw, show not only a greater average 

 thickness, but particularly so for the corresponding winter layers. 

 These variations are due, no doubt, to a greater depth of water and 

 volume of sediments over the Jones Point area in Haverstraw, al- 

 though farther from the ice front, than the terrace banks in West 

 Haverstraw, which were f artheest removed from the main channel of 

 the glacio-fluvial river, the Hudson. With a greater depth of water 

 and a larger volume of sediments in the main channel than near the 

 margins of the lake, it is not surprising that during the winter 

 months more clay particles settled down through the cold milky 

 waters to form the thicker " winter " layer at Jones Point than that 

 on the sites of the Hornbecker and Dunnegan pits. Each of the five 

 curves has been smoothed by taking the average of each four succes- 

 sive varves. The smoothed curves have been entered as single-line 

 graphs above the other curves by using the mean of each section as 

 a base line. A comparison of these smoothed curves shows a close 

 agreement in all of the pits. These smoothed graphs represent a 



