J. D. Dana—The flood from the melting Glacier.* 178 
hence prove that, throughout the New Haven estuary—then six 
miles in depth if we reckon only to Pine and Mill Rocks, and 
over half that in width and opening (as now) to the southward 
—the deposition took place under the pushing and plungin 
action of the incoming tide, the tidal waters having been forced 
into heavier plunging than usual owing to the violent resisting 
flood of fresh waters in front. 
This rise to the northward in the oblique lamination (or dip 
to the southward) prevails except at the mouths of the valleys. 
he beds at the lower extremity of the Quinnipiac valley, just 
southeast of Hast Rock (K), afford one of these exceptions. 
At this place, along the cut of the Air-Line railroad between 
Mill River and the Quinnipiac, the stratified drift-deposits, which 
here have their full height or 42 feet above high tide level, are 
exposed to view toa depth of about 25 feet. Through the 
northeast half of the cut (near C) where it is within the range 
of the Quinnipiac valley, the beds of the upper 20 feet have 
the oblique lamination rising to the southward, that is, in a diree- 
tion the opposite to that in the underlying beds, and the oppo- 
site to that which characterizes the whole thickness of the 
deposit over the New Haven region except at the mouths of 
the valleys. The following cut represents a part, six feet in 
—. 
height, of a vertical section, and shows the race of junction 
NS between the upper and lower portions; above NS oblique 
lamination rises to the southward, and below NS t the northward. 
In addition to this difference of direction, the beds below are 
brownish-red, and those above rusty brownish-yellow. 
The deposits present this difference above and below for half a 
mile along the cut. But passing beyond this westward, or toward 
Mill River, out of the Quinnipiac Valley, the upper stratum 
gradually loses its distinctive ch rand becomes like that of 
the plain deposits elsewhere. This change on passing out of 
the range of the Quinnipiac proves that the existence of such 
an upper stratum was re cee on the flow of the river and 
not on any variation in level or depth, or on any subsequ 
action of currents. The drift deposits have a uniform level 
