Hydrographical Observations from the Danmark Expedition. 395 



This explains, why the ice everywhere melted more rapidly in 

 the summer of 1908 than in the summer of 1907, though the average 

 air temperature was nearly the same in both summers. 



To show the rapidity wth which the stratified snow-ice melted, 

 I may give the following measurements of the thickness of the ice 

 taken in four holes at 100, 200, 300 m. from the ship and close to 

 the latter. 



Hole I Hole II Hole III Hole IV 



close to ship 100 m. from ship 200 m. from ship 300 m. from ship. 



23/vi 08 130 cm. 136 cm. 138 cm. 115 cm. 



26/vi - 118 - 130 - 123 - 83 - 



1/vii - 41 - 42 - - - 



Simultaneous measurements of the thickness of ice, thickness of snow and 

 surface salinity in the fjords and inland lakes 1908. (Table 7 p. 396). 



Remarks: In the winter of 1906 — 07 it was found, that the thick- 

 ness of ice in the fjords was very different at stations which lay quite 

 close together. In March 1908, therefore, a series of measurements 

 was made of the thickness of ice at stations, which lay in a line across 

 the fjords and sounds; at the same time measurements were made 

 of the height of the snow above the ice and some measurements of 

 the surface temperature and salinity. 



At this time (March 1908) the ice in Danmarks Havn had reached 

 its maximum thickness and decreased thereafter but little in thick- 

 ness during the two following months. We may assume, therefore, 

 that the ice in the fjords had likewise nearly attained its maximum 

 thickness after the winter. 



It appears from the observations that the thickness of the ice 

 was on an average least in the eastern part (mouth) of the fjords and 

 increased in towards the inland ice, due in part presumably to the 

 fact, that the transport of heat from the deeper layers in the sea was 

 greatest in the neighbourhood of the sea. 



On the inland lakes the thickness of the ice was even greater 

 than in the western part of the fjords, which is probably to be ascribed 

 in part to the fact, that the cooling from the atmosphere in the course 

 of the winter did not give rise to convection currents in the fresh- 

 water lakes, when their temperature became -f 4° C. or less, whereas 

 these were produced in the sea and here, in the course of the winter, 

 constantly brought up deeper, warmer layers to the surface. 



Conversely, the surface salinity was greatest in the eastern part 

 and decreased westwards, in part probably because the transport of 

 chlorides to the surface from the deeper layers in the sea was great- 

 est in the eastern part, and in part owing to the downflow of melting 

 snow and ice water from the inland ice in the west. 



