me) at Cape Columbia than at Cape Sheridan.
The Cape Columbia tides are even earlier than the tides along the
northern coast of the Spitzbergen Islands. These facts prove that the
tide at Cape Columbia comes from the west. It is the Baffin Bay tide
transmitted, first, northwesterly through the eastern portion of the
Arctic Archipelago to the Arctic Ocean, and then easterly along the
northern coast of Grant Land to Cape Columbia. That the tide wave should
be felt after a passage of this kind, instead of practically
disappearing after entering the Arctic Ocean, is one argument for the
existence of a waterway of limited width to the northwest of Grant Land.
This suggests that Crocker Land, first seen by Peary on June 24, 1906,
from an altitude of about 2000 feet, may form a portion of the northern
boundary of this channel or waterway.

The tides along the northern coast of Greenland are due mainly to the
large rise-and-fall occurring at the head of Baffin Bay. The Arctic
Ocean being of itself a nearly tideless body so far as semidaily tides
are concerned, it follows that the time of tide varies but little as one
goes through Smith Sound, Kane Basin, Kennedy Channel, and Robeson
Channel; in other words there exists a stationary oscillation in this
waterway. The northeasterly trend of the shore line of Peary Land beyond
Robeson Channel and the deflecting force due to the earth's rotation
tend to preserve, far to the northeastward and partly in the form of a
free wave of transmission, the disturbance resulting from the stationary
oscillation in the straits. The tide observations indicate that this
disturbance is felt as far as Cape Morris Jesup, where the semidaily
range of tide is only 0.38 foot. At Cape Bryant, northeast of Robeson
Channel, the range is 1.07 feet. These values, taken in connection with
the Robeson Channel disturbance, indicate that the time of tide along
the coast of Peary Land becomes later as one travels eastward from Cape
Bryant.

Owing to the comparatively short distance between Cape Bryant and Cape
Morris Jesup, it is probable that at the latter point the crest of the
wave transmitted from the southwest will appear to arrive much earlier
than will the crest of the wave passing between Spitzbergen Islands and
Greenland. In this way the small size of the semidaily tide at Cape
Morris Jesup, as well as its time of occurrence, can be partially
explained.

A no-tide point doubtless exists in Lincoln Sea,