SOLUTION OF THE HYDROSTATIC PROBLEM FOR THE SEA. 131 



The soundings are as seen to have been taken with increasing intervals down- 

 wards, corresponding to the decreasing variations of temperature and salinity in the 

 greater depths. This inconstancy of intervals, though unavoidable practically, is 

 irrational from a theoretical point of view. Therefore the final results are interpo- 

 lated for two sets of constant intervals given in column 11 of each scheme. These 

 intervals are 10 dynamic meters or 10 decibars in the upper sheets, and 100 deci- 

 bars or 100 dynamic meters in the greater depths. 



The data tor each sounding are treated according to the two diflerent methods, 

 that of depth corresponding to a given pressure (tables U and W), and that of pres- 

 sure at a given depth (tables V and X). 



79. Graphic Representation. The results worked out in these examples are 

 represented graphically in figs. 25 and 26. The first vertical in each figure gives 

 the depth of the isobaric surfaces exactly as the first of fig. 1 (p. 45) gives these 

 depths for sea-water of 35 /oo salinity and temperature o C. The comparison shows 

 perspicuously a greater depth of the isobaric surfaces in the brackish water of the 

 Baltic than in that oi the Atlantic, while the Atlantic vertical would have shown 

 only microscopical differences from that of the normal sea-water (fig. 1), both 

 figures being reduced to the same scale. 



On the second vertical of figs. 25 and 26 the first division gives the situation of 

 the isobaric surfaces, transferred from the first vertical. The second division does 

 not, however, give the true specific volume as in fig. 1, but the anomaly of the 

 specific volume taken from column 10 of the schemes (pp. 126, 128). In this way 

 the difference from one vertical to another is made much more perspicuous. A 

 vertical would have no anomalous divisions if the water had the "normal" salinity 

 f 35 /oo an d the " normal " temperature of o C. The anomalous divisions 

 therefore show the deviation from this normal state. As is seen, these anomalies 

 are of relatively great numerical value in the brackish water of the Baltic, but oi 

 much smaller value in the Atlantic. Otherwise the anomaly varies rapidly near 

 the surface and slower as we proceed downward, the variations with the depth 

 being of the same order of magnitude along the vertical in the Baltic as along that 

 in the Atlantic. 



The third vertical in figs. 25 and 26 gives in exactly the same way the anomaly 

 of density in different dynamic depths. 



