Hydrographical Observations from the Danmark Expedition. 359 



This supposition was first put forward by Ryder and was sup- 

 ported later, among others, by Fr. Nansen and B. Helland-Hansen; in 

 my opinion, it is the most probable explanation, until direct obser- 

 vations in the northernmost part of the Greenland Sea decide the 

 question once for all. 



We may believe, that the warm current comes in at a latitude 

 of ca. 80° and then follows the Polar Current southwards, whilst 

 through the submarine fjords in the Continental Shelf it flows in to- 

 wards land and fills up the deeper parts of the waters here and the 

 fjords. 



During this movement of the current towards land it must pass 

 over bars, where a slight mixing with Polar Current water may occur. 



As all the stations in the section were taken at intervals of a few 

 days, we may conclude, that the difference in temperature and sa- 

 linity, at the same depth at different stations, is for the most part 

 due to different geographical situation. 



The direction from St. LXXIII over LXXV to LXXVI points 

 somewhat out from land, whilst the direction between St. LXXVI 

 and St. LXXVII is nearly parallel with the line of the coast and the 

 direction of the Polar Current. 



Between the last two stations the direction of the curves is al- 

 most horizontal. The temperature and salinity, in other words, remain 

 almost unchanged, as we go parallel to the coast in the direction of 

 the Polar Current. As we approach the land, however, as, for example, 

 in Sect. II following the curves from St. LXXVI inwards, these are 

 slightly raised except the 33 p. m. isohaline, which lies deeper 

 owing to special conditions in under the land, where, as will be shown 

 later, mixing takes place between the water-layers at a depth of ca. 

 50 to 100 m. At the same time the 32.50 p. m. isohaline shows a 

 greater bend in towards land than the 33 p. m. This is due to a mixing 

 with fresh water from the rivers in the uppermost layers. 



At St. LXXIII in the mouth of Øresund the average salinity 

 of the layer — 50 m. was 32.55 p. m. in the middle of June. From 

 the middle of June to the middle of July this average salinity decreased, 

 owing to the outflow of water from the melting ice and snow, to 

 32.05 p. m. At the same time as this (middle of June) the average 

 salinity for the layer — 50 m. at St. LXXVI further from land was 

 32.30 p. m., thus considerably greater. 



Owing to the difference in the average density of the two layers 

 (26.02 at St. LXXVI against 25.80 at St. LXXIII) there must have been 

 an east-going movement in the uppermost 50 m. of the coastal water, 

 a movement which has helped to keep the drift-ice away from shore. 



Along with this movement in the upper layers there must have 

 been a reaction current in the deeper layers, which can also be traced 

 in the 34 p . m. isohaline, which rises up towards the land. In spite 



