decrease in the percentage of the vohinie transport following the 

 eastern branch. 



Figure 22 shows the localioii of llic section across the Lahi-.-idoi- 

 Sea occupied during (he postseason siu-vey and gives the dyiuiniic 

 topography of the sea surface in tlie vicinity of the section. Figures 

 23 and 24 show the distribution of temperature and salinity, respec- 

 tively, along this section. The (Hstribution of dissolved oxygen is 

 given in jnilliliters per liter in figure 25 and in percentage saturation 

 in figure 26. 



In considering figure 22, it nuist be kept in mind that the frag- 

 mentary dynamic topography shown is not the result of a network 

 survey and while having some support from GEK observations, it is 

 principally useful in showing the location of the steeper gradients. 



The Labrador Current shows characteristic temperature distribu- 

 tion in figure 23, with a core of negative temperatures over the Labra- 

 dor shelf, a steep horizontal temperature gra(hent over the continental 

 slope, and warm water ofi'shore, witli a temperature maxinnim intersect- 

 ing bottom at about 600 meters. A slight temperature maximum, as 

 defined by the isotherm of 3.4°, extends northeastward from the 

 Labrador side at a depth of about 1,500 meters as far as station 7943. 

 On the Greenland side the cold inshore component of the West 

 Greenland Current is delineated by the 2° isotherm while the effect 

 of the L'minger Current component is evident in water w^armer than 

 5°. 



The salinity distril)ution shown in figure 24 shows a characteristic 

 slope of the isohalines over the Labrador shelf with a gradation from 

 low salinity coastal water to salinities greater than 34.80%o over the 

 continental slope. A downward bulge of the isohaline of 34.85 

 between stations 7938 and 7939 roughly coincides with a sunilar 

 bulge in the isotherm of 3.4° seen in figure 23. This warmer fresher 

 water is considered to be associated with the noi'thward flow just 

 seaward of the Labrador Current. On tJie Greenland side, the 

 salinity maximum of greater than 35°/oo outlines the coi-e of tlie 

 Irminger Current com]Jonent of the West Greenland Current. Be- 

 neath this there is a salinity maximum extending downward and 

 southwestward at depths between 2,000 and 3,000 meters, as indicated 

 by the isohaline of 34.9°/oo- C^omparison of figures 23 and 24 shows 

 this deep salinity maximum to be deeper than the temperature 

 maximum. 



An analysis of the temperature and velocity structure of the West 

 Greenland Current showed a volume transport of 5.98X10** ju^sec 

 compared to a seasonal normal of 4.73. The mean temperature 

 found in 1961 was 4.69° compared wnth a seasonal normal of 4.46°. 

 Tims the heat transport was 28.07X10** nr^ °C/sec compared with 

 a seasonal normal of 21 .09. If tlie East Greenland Current component 

 is assumed to liave a constant mean temperature of 3.2° and the 



33 



