Currents » Calculated current results are giTsn in Table IV. Two 

 diagrams have been constructed, the first of wMch (Figure 4) diows the 

 dynamic topography of the surface referred to tho 1000 decibar level for 

 tho region of deep v/ater between tho Aleutian Ridge and the Pribilof Islands. 

 The second diagram (Figure 5) shoY/s the dynamic topography of tho surface 

 referred to tho 50 decibar level for tho region between St. Paul Island 

 and the Arctic Ocean. Contour lines foro drawn for intervals of tvo dynamic 

 centimeters. Arrows show the direction of the currjnt. Numbers adjacent 

 to the arroY/s give the water velocities in knots. Not all stations in dcop 

 witor region were sampled to depths of 1000 motors. In such cases the 

 dyncjnic hcigjits were obtcinod hj extrapolation, using 1000-motor_ stations as 

 a br.sis. The seme procedure was follov/ed for northern Bering Sea at st'-tions 

 loss than 50 nnters in depth. The diagrcjns are not exact o.t all points duo 

 to these extrapolations but are essentially correct as shown by chocking the 

 extrapolations using different reference stations. The small temperature and . 

 chlorinity variations' at depths of 1000 meters (Table VI) indicate alraost 

 constant conditions with little current at that depth. Thus Figure 4, based 

 on relative values, also gives quite accurately the picture of tho absolute 

 current field for the deeper region. 



North of the Aleutian Ridge near Bogoslof Island, tho currents paral-^ 

 Iclcd the ridgo toward the oast, swung north in tho vicinity of Unalaska 

 Island as tho water mot the continental sholf , and then doubled back along 

 the sholf as it headed to the northwest soutli of the Pribilof Islands. 

 Current magnitudes in this area were 0.3 knot or loss. Between Unimak and 

 Unalaska Islands, the Pacific water set noi^th into the Bering at relocities up 

 to 0,4 knot. West of Unalaska Island, tho velocity component towards the 

 north was loss, but tho general transfer of water from the Pacific to tho 

 Boring was still present. Water volocitics docroasod with increasing depth, 

 becoming small at depths of 800 to 1000 irBtors as compared to those at tho 

 surface. 



In tho northern portion of Boring Sea, v/ator from Bristol Bay and tho 

 Yukon Delta moved north along the Alaskan coast and passed into tho Arctic 

 through tho eastern portion of Bering Strait, Cold water from the G-ulf of 

 Anadir and perhaps some surface water from the doupor region of tho Boring, 

 moved north along tho Asiatic coast and into the Arctic on tho western side . 

 of the Strait. Small eddy currents Vifere found between St. Lawrence and the 

 Dionede Islands, Currents calculated by the Bjerknes method for the shallo¥\? 

 waters of North Bering Sea are low, as this method gives only the relative 

 velocities referred to the lowest observed lovel, and water at this level 

 was shown by direct current noasuroments to bo in motion. Surface currents 

 depicted in Figure 5 and given in roforonco to the 50-dociber level accord- 

 ingly do not givo tho obsolute currents for that region. Tho diagram, how- 

 ever, shows satisfactorily the lines of flow and rolativo current s. 



Calculated currents shoY/od that in general the v/ator in Boring Sea 

 moved in a diroction paralleling the coast linos and tho bottom contours. 

 This can bo readily seen by comparing figures 4 and 5 showing the currents 

 v/ith Figuro 2 showing tho bottom topography. 



Direct currents as obtained by observations from tho anchored ship 

 by riC-ons of ;ji Ekr:ian current motor (Table IV) are shown for several st-.tims 

 in Figuro 6, In this diagrara the .lengths of the arrows aro proportional to 

 the velocity of tho water masses and "their directions' sliow tho direction of 

 the flow. In most cases tho v/atcr v;as found to bo in i.ioti on from top to 



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