were used for all oxygen sampling. The samples 

 were chemically treated and stored until analysis 

 (storage time never exceeded 2 hours) in 150- 

 milliliter glass bottle with ground and lapped 

 glass stoppers. The sodium thiosulfate solution 

 was standardized daily with a previously prepared 

 potassium bi-iodate solution. Aliquot samples of 

 the treated sea water were withdraw by a 50 ml 

 micro-burette. The precision of the method is con- 

 sidered to be ±.03 ml/liter. 



Programs in FORTAN for use on the digital 

 computer of the Woods Hole Oceanographic Insti- 

 tution were prepared for the correction of revers- 

 ing thermometers and determination of thermo- 

 metric depths, the computation of sigma-t and 

 specific volume anomaly, the determination of the 

 amount of dissolved oxygen in milliliters per liter 

 and the computation of percent oxygen saturation 

 based on Fox ( 1909) . Each of the above programs 

 was used for processing the data from Kennedy 

 Channel, Kane Basin, Smith Sound, and upper 

 Baffin Bay used in preparing the illustrations. 

 The raw data was reprocessed by the National 

 Oceanographic Data Center for inclusion in the 

 Table of Oceanographic Data (table V) at the end 

 of this publication. A careful check was made of 

 the processed data from both computers and it was 

 found to be in perfect agreement. 



The Richardson current meter data is presently 

 in the possession of the Coast Guard Oceano- 

 graphic Unit, Washington, D.C. Difficulties were 

 encountered with the machine processing of the 

 data causing the program to be temporarily halted. 

 It is hoped that the difficulties can be solved and 

 the program completed in the near future. When 

 this is accomplished, the current data will be pub- 

 lished as a separate report in this series. 



The ice chart of 2 July showed the ice island 

 straddling Kennedy Channel from the Canadian 

 shore to Hans Island and the little ice that had 

 moved past between Hans Island and Greenland 

 was stopped 5 miles further south by Franklin 

 Island. It appeared from reports that the ice 

 island had been in this position for quite some 

 time. An ice reconnaissance flight on 24 July 

 showed that the ice island had shifted to the east 

 side of the channel lodging against the north 

 shore of Franklin Island allowing the polar ice to 

 move south. A flight on 26 July showed the ice 

 island in the middle of Kennedy Channel broken 

 in three pieces, the largest of which was 4 by 7 

 miles and moving southward with the pack ice 



that had been backing up into the Arctic Ocean. 

 The positions determined from the reconnaissance 

 flights and later positions furnished by the CGC 

 Westiolnd (which was in Kane Basin conducting 

 hull strength tests), showed a drift of about 13 

 miles per day for the ice island and 15 miles per 

 day for the pack ice. This difference in drift af- 

 forded a lee (in the pack ice) south of the ice 

 island fragments allowing Evergreen to occupy 

 the last station of the Kennedy Channel section 

 fairly close to shore. 



The Evergreen found ice conditions unusually 

 light throughout the survey due to the blocking 

 action of the ice island across Kennedy Channel. 

 Smith Sound was ice free and normally ice-choked 

 Kane Basin was free of ice on the west side before 

 the arrival of the polar pack. Peabody Bay, 

 which constitutes the entire east side of Kane 

 Basin, was still ice covered but some of the fast 

 ice had broken loose and had begun drifting south 

 to Smith Sound. Some remnants of fast ice from 

 the bays on the west side of the basin had moved 

 south but the concentration was low and it was 

 easily avoided. The polar ice which had been held 

 back by the ice island had moved halfway down 

 the west side of Kane Basin. 



Figure 2a shows the vertical temperature dis- 

 tribution between Cape Collinson, Ellesmere Is- 

 land, and Cape Jefferson, Greenland, on a trans- 

 verse section which for purposes of simplicity 

 will be known as lower Kennedy Channel. It is 

 interesting to note that the water below 200 meters 

 in the central and eastern part of the channel is 

 above 0° C and shows a slight and gradual warm- 

 ing to the bottom. The coldest water is found on 

 the western or Ellesmere side of the channel above 

 100 meters with a narrow pocket at 80 meters that 

 reaches to the center of the channel. This cold 

 water appears closer to the surface further west. 

 In figure 2b, the Kane Basin section from Cape 

 Louis Napoleon to Cape Russell, the temperature 

 minimum appears centered over the deepest part 

 of the channel which is closer to the Greenland 

 shore and with its core located at a depth of about 

 75 meters. The temperature minimum along the 

 western shore is no longer in evidence although 

 there still is some cold water following the western 

 shore. Temperatures again rise gradually to the 

 bottom in the western-central part of the channel. 

 In figure 2c, the Smith Sound section shows a 

 complete disappearance of the temperature mini- 

 mum found further north. It is possible that the 



