IOS HYDROGRAPHY. 



of o - 2 centimetres. The water was running out over the edges of the vessel no matter where. Motes 

 in the water proved by their motion that there was a real eddy-like formation with a horizontal axis 

 above the place where the boundary-plane was in its lowest position. In the experiment, the boundary- 

 plane between the solution of the chloride of calcium and the pure water is a visible isohaline, and 

 it has, as may be seen, the same shape as the isotherms in the afore-mentioned sections. With a more 

 rapid outflow of the water, the deepest place of the boundary-plane B is advancing farther from the 

 orifice of eduction. 



In consequence of the Atlantic water taking a sideward motion when it comes up under Iceland, 

 rather complicated motions may be the result, and the form which is found for isotherms and isohalines 

 may possibly be due to other causes than those mentioned here. But for all that we can hardly make 

 the assumption that the said depression in the isotherms can be caused by thermical effects only. 



SECTION VI. 



From station 8 (abreast of Faxe Bay in a south-westerly direction). 



From the south-western point of Iceland, a submarine ridge is extending in a south-westerly 

 direction. Respectively on the southern and northern side of this latter, the two sections V and VI 

 are lying. Looking at these sections, it will appear that the ridge stands as a partition be- 

 tween water of different properties. North of the ridge, the water at the bottom has at the 

 same depth a lower temperature and less salinity than that south of the ridge. This latter is thus a 

 natural line of demarcation between the Denmark Strait and the Atlantic. 



It is not, however, only in the case of the bottom-water that this submarine ridge, which in 

 connection with the Iceland & Greenland ridge encloses a whole basin in the Denmark Strait, becomes 

 a boundary. Also the higher strata on each side of the ridge show differences, though 

 less distinctive than those found for water from the sides of the Faroe-Iceland ridge. While thus 

 the isotherms in section VI approach the surface more and more, successively as we advance in a 

 south-westerly direction, the contrary will be the case with the isotherms in section V, that is to say, 

 only in the outermost part of the section (from station 74 to station 78). The nearer we come to 

 Iceland, the smaller will be the difference between the 2 sections. 



This can naturally be accounted for thereby, that the water in the Irminger Current 

 along the westcoast of Iceland passes right across the two sections near the coast, 

 and by this makes up for the differences. Farther to the south-westward, the motion must 

 have another direction than the perpendicular one on the ridge. For a current running 

 in this direction, would also here tend to effect an adjustment of the differences on the two sides of 

 the ridge; the observations prove now that such an equalization does not take place. There is in 

 consequence of this every reason to believe that the motion goes in the same direction 

 as the ridge, that istosay towards/^wrf. Very likely it is caused thereby, that the current setting 

 north in the western part of the Atlantic, is turning off in a north-easterly direction when it falls in 

 with the eastern Greenland Polar Current, at the same time carrying with it part of the water of 

 the Polar Current At the southwest coast o f Iceland, the Atlantic Current is divided into 

 two currents: one that runs to the eastward, and another that runs North and forms 



