ographic Office Publication No. 607 (1968). 

 Paired protected thermometers were used on 

 each bottle with unprotected reversing thermom- 

 eters added on the deeper bottles. Sampling 

 depths were determined from L-Z curves based 

 on thermometric depth and wire angle. All cal- 

 culations were performed on a PDP-5 digital 

 computer utilizing programs described by 

 O'Hagan (1964). \'olume transports were com- 

 puted using the method of subdividing each 

 oceanographic section into solenoids for com- 

 putations as described by Kollmeyer (1967). 



Data were also obtained on 10 stations using 

 a Bissett-Berman Mode! 9060 self-contained 

 salinity-temperature-depth (STD) recorder. 

 The STD data were quality controlled l)y com- 

 parison with temperatures and salinities ob- 

 tained from deep-sea reversing thermometers 

 and water samples collected at the surface and 

 just above the STD at the bottom of the cast. 

 An average quality control correction for the 

 STD stations was determined from the differ- 

 ences between the STD data and the associated 

 quality control samjiles and was applied to the 

 raw data from the recorder. 



The data presented in the Tables of Ocean- 



ographic Data (app. A) are reproduced from 

 computer listings from the National Ocean- 

 ographic Data Center (NODC Cruise Numbers 

 :51-8184 and 31-1705). Anomalies of dynamic 

 height in the listings were computed by NODC, 

 but all discussion of dynamic heights in this 

 text is based on computations made at the 

 Coast Guard Oceanographic Unit. Dynamic 

 heights in water shallower than the reference 

 level were computed in a manner similar to 

 that of Helland-Hansen (1934), as described 

 in detail by Kollmeyer (1967). 



The survey and glaciological data from 27 

 glaciers will he published in a separate Coast 

 Guard publication after the analysis is com- 

 pleted. Glacier fronLs were charted, and bench- 

 marks were established at survey stations 

 wherever possible for reference during future 

 surveys. Records were kept on ice movement 

 and calving and on iceberg distribution ai'ound 

 the glaciers and in the fjords and bays. Photo- 

 grai)hic overflights of the major glacier fronts 

 were conducted by a Coast Guard HC-130 air- 

 craft equi]iped with a T-11 aerial camera. 

 Ship's helicopters were used to obtain oblique 

 and vertical photographs of all glacier fronts. 



DISCUSSION 



The interchange of water between the Arctic 

 Ocean and Baffin Bay takes place through 

 Nares Strait, Jones Sound, and Lancaster 

 Sound (fig. 1), but this flow is re.stricted due 

 to limiting sill depths of 250, 175, and 180 

 meters respectively (Bailey, 1956). Nares 

 Strait is the deepest and most direct path for 

 this interchange and is of major importance 

 in determining the water and heat budgets of 

 the Aictic Ocean and Baffin Bay. The general 

 bathymetiy of Nares Strait consists of a nar- 

 row, deep channel running along the western 

 .side of the strait with a sill at 250 meters in 

 central Kane Basin (fig. 4). 



Previous investigators of the eastern Arctic 

 have noted that waters at about 250 meters 

 have characteristics (-0.3" C, 34.4%,,) similar 

 to deep water found in Baffin Bay and have 

 hypothesized that this water flows over the 

 sill in Kane Basin and sinks to the bottom in 

 Baffin Bay. Bailey (1957) and Collin (1965) 

 concluded that this is not a continuous process 



but probably takes place as an intermittent 

 pulsing. Muench (1971a) suggests that this 

 method is less common than previously indi- 

 cated, and he upholds the theory of Sverdrup, 

 Johnson, and Fleming (1942) that Baffin Bay 

 Deep Water is formed by a mixture of Labra- 

 dor Sea Deep Water and Baffin Bay Surface 

 Water whose salinity had been increased suffi- 

 ciently by freezing to cause the water to sink. 

 Examination of the water characteristics 

 observed in Nares Strait in 1970 (figs. 17 and 

 18) shows water with the proper temperature- 

 salinity relationship (<-0.3- C, >34.4"„„) at 

 200 meters at station 20 over the sill in Kane 

 Basin and at 300 meters at station 19 just 

 south of the sill. However, water of proper 

 salinity for deep water formation was not pres- 

 ent in the passage between Kane Basin and 

 Smith Sound. The distribution of salinity and 

 density through Nares Strait (figs. 18 and 19) 

 suggests the presence of an isopycnal wave of 

 denser water overflowing the sill in Kane 



