912 
BULLETIN OF THE BUREAU OF FISHERIES 
more closely as far as the cape, or perhaps to Massachusetts Bay, such as were actu- 
ally followed by bottles set out in the Bay of Fundy during the summer of 1919 
(p. 870) and off Cape Neddick (series O) in July, 1926. The locations of the isohalines 
at the surface are thus entirely reconcilable, both with the drifts assumed for the 
bottles and with the annual difference indicated by the sets put out in the summers of 
1919, 1922, 1923, and 1926. 
Mavor (1923), in his discussion of the distribution of salinities and temperatures 
in the Bay of Fundy for August, 1919, has shown that these are best explained as 
due to a movement of water into the bay on the Nova Scotian side, recognizable 
from the surface down to a depth of 100 meters, crossing northward toward New 
Brunswick about midway up the bay, with a counterbalancing outflow of water 
of low salinity southward and westward along the northern (New Brunswick) 
side. Here, again, temperature and salinity corroborate the evidence of drift 
bottles (p. 870). 
The high surface salinities recorded in the northeastern corner of the gulf on the 
August cruises of 1912 and 1913 suggested a continuous tongue of highly saline water 
flowing into the eastern side of the gulf at the surface from the Atlantic Basin. 
However, subsequent discovery that the high surface values encountered in the basin 
between Maine and Nova Scotia in successive summers actually represent an isolated 
pool, resulting from local upwelling combined with tidal stirring (p. 768), and sur- 
rounded by less saline water on all sides, has lead to the appreciation that the gulf 
receives its saline water chiefly in the deeper strata (p. 842), not on the surface. 
The rather abrupt west-east transition in surface salinity registered in the offing 
of Cape Sable in the summers of 1914 and 1915, added to the retreat of the critical 
isohalines (32 to 31.5 per mille) from the eastern side of the gulf, eastward, with the 
advance of the spring (p. 755), argues against any notable current from the east past 
the cape as characteristic of summer. Here, however, the effect which the active 
tidal mixing southwest and west of the cape would have in increasing the salinity of 
the surface, moving westward, must be taken into account. 
If the evidence of salinity does not make clear the dominant set, if any, past 
Cape Sable for the summer months, the tongue of low salinity and low temperature 
found extending along the southeastern face of Georges Bank from northeast to 
southwest in July, 1914 (p. 770), is “hard to explain, except as an outflowing current 
from the gulf” (Bigelow, 1917, p. 241); and though this may not be a regular feature 
of the summer circulation (p. 608), the fact that several bottles from the Cape Cod and 
Cape Ann series of 1922 and 1923 seem to have drifted out of the gulf via this same 
route across the eastern end of Georges Bank (figs. 174 and 176) is certainly sug- 
gestive of its permanency. A tendency for water of low salinity to spread from the 
vicinity of Cape Cod southeastward to the neighboring part of Georges Bank is also 
indicated by the contrast in salinity between the western and eastern ends of the 
latter on the summer chart for 1914 (fig. 136, isohaline for 32.2 per mille). Here, 
again, a close parallel appears from the set, as indicated by the salinity of the surface 
water and the probable drift tracks of bottles that went in that direction from the Cape 
Cod series of 1922 (series B, p. 880, fig. 174). Farther south, in the southwestern 
part of the area, successive isohalines for 32.5 to 33.5 or 34 per mille, closely crowded 
and roughly paralleling the edge of the continent, prove that the dominant set here 
