- 22 - 



then tends to proceed down the eastern const of Grnnd Kpnnn v/here it 



is covered over or mixed with the other waters in thqt region. 



At a depth of 10 metres (figure 27) the rnnge in the distrihution 



o 

 of s"?.inity vories between 31.5 to prcter thqn 31.8 /oo. The 



waters nt this depth closely follow tVie movements at the surfnco, but 



they ore not en ''s large «^ sc"le. 



At 25 metres (figure 28) the outflow from the Saint John River is 

 not RS prominent ms Pt higher levels. Thus it moy be stated that the 

 freshet wter from, the S^- Int John River is carried away in the unper 

 25 metres and joins with the waters from Passamqquoddy Boy before 

 passing esist of Grand Mqnan «(t these depths. The wgter movements at 

 this depth nre approximately the s^me as those in the upper layers. 



The distribution of salinity <>t 50 metres (figure 29) is indica- 

 tive of a "dramr in" of waters to the Se int John and Pnssamaquoddy 



o 

 area, IVaters v/ith salinities as high as 32.20 /oo reach v/ell into 



the mouth of the Saint John River, and the entrance to Passamaquoddy 

 Bay. 



It has been shown that the movements from the Passamaquoddy and 

 Saint John areas take pl«ce in the upper 25 metres. The actual 

 physical nnd chemical conditions of the waters that make up this 

 outflow will vary, but the fact remains however, that the v/aters nro- 

 ceedlng from the drainage systems gradually become more saline as 

 they progress into the Boy^ which m^eans that salt v/ater from the 

 depths is being used up. Consequently, there must be a resultant 

 inflow to m^'U-e up for this consumrption of salt v/ater. As has been 

 demonstrated, this "inflov;" or "drav/ In" takes place at a depth of 



