Raw CTD data were recorded on the computer' s hard disk 

 drive and archived on Iomega Bernoulli 20- Megabyte removable 

 disk cartridges. One-meter average values for each station 

 were created using Sea-Bird supplied software. A data report 

 gives standard-level listings for all CTD data from the cruise 

 (Amos. 1990). 



Results 



water depths in the Gulf of Anadyr are less than 1 50 m, and 

 mostly less than 100 m. In the Chirikov basin and southern 

 Chukchi Sea, water depths are even less — almost everywhere 

 30 m or less. The north-south size of this shallow shelf sea is 

 enormous, subtending about 1,200 km from the shelfbreak in 

 the northern Bering Sea to the shelfbreak in the Arctic Ocean. 

 In this shelf sea, diverse water properties are encountered. 

 Based on AK-47 data, in summer temperatures range from 

 nearly 12°C at the surface near the Alaskan coast in the 

 Chirikov basin, to -1.6°C at the bottom in the central Anadyr 

 Gulf, southwest of St. Lawrence. Salinities range from 24 ppt 

 at the surface near the Chukchi coast off Kolyuchin Bay to 

 33.6 ppt at the bottom in the same location (Station 45). 



A T/S diagram of all stations from AK-47 is shown in 

 Fig. 1 . Surface values of each station are marked by "T" and 

 bottom values by "B." and the dots are 1-m average values. 

 This diagram includes not only the shelf stations but the 1 1 

 stations taken in the deep Bering Sea. These latter form a tight 

 grouping: surface values are all >32 ppt up to about 33.4 ppt; 

 there is a temperature minimum in the S band 33.2-33.4 

 (forming a marked ""V" shape in the diagram); deeper, there is 

 a temperature maximum of 3.6<T<4.0°C, and below this, the 

 bottom values merge to a water type ~ 1 .8°C. 34.6 ppt. 



us/USSR BERING ' BB 



ALL STATIONS (in Fig 1) 



a. 



D 



I- 

 < 



cr 



LU 



a 

 z 



LU 



26 2B 30 



SALINITY (ppt) 



32 



34 



36 



Fig. I . Temperature-salinity diagram of all Korolev stations, from the shallow 

 northern region (Frontispiece) and 1 1 stations from the deep Bering Sea 

 basin. Bats are 1-m average values; for each station the surface value 

 is marked by a "T" and deepest value by a "B". 



The T/S values from shelf stations are massed, with few 

 exceptions almost all associated with surface layer values, in 

 the salinity range 31-33 ppt. There is one group with bottom 

 water temperatures <0"^C and another concentration of data 

 points between -0.5 and 3°C. Surface T's are spread mostly 

 between 3 and 10°C. There is a further scattering of surface 

 values, with T's >4°C, toward low salinities. A few stations 

 with bottom water temperatures ~()°C and S's >33 ppt deviate 

 from the mass of points. It has long been known that the main 

 flow in the northern Bering Sea is northward through Bering 

 Strait into the Arctic Ocean. Coachman and Shigaev (Subchapter 

 2.1, this volume) trace a primary pathway of this flow. Water 

 from the Bering Slope Current, which tlows northwestward 

 along the continental shelf edge of the eastern Bering Sea Shelf 

 ( Kinder t'/ «/.. 1975), crosses the continental shelf southwest of 

 St. Lawrence Island in the Gulf of Anadyr. The How maintains 

 itselfas a current (transport -0.5 to 1 Sv) circumnavigating the 

 gulf because its dynamics are analogous with tho.se of a western 

 boundary current (Kinder et ciL. 1986). From the Strait of 

 Anadyr, the flow follows the western side of Chirikov basin, 

 transits Bering Strait, then curves northeastward into Kotzebue 

 Sound before being steered by the topography to the north and 

 west. 



The second main regional flow is that of coastal water on 

 the east, entering through Shpanberg Strait east of St. Lawrence 

 and hugging the Alaskan coast northward through Bering 

 Strait, around Kotzebue Sound, and then northwest passed 

 Pt. Hope and Cape Lisburne. Between these flows is advected 

 a third water mass of shelf water; because this water mass is 

 made on the large Bering Sea Shelf south of St. Lawrence 

 through mixing of dilute coastal water with the more saline 

 Bering Sea continental slope water, it is identifiable as a 

 separate water mass by its intermediate values of salinity; it is 

 also the coldest of the water masses in summer south of Bering 

 Strait (cf. Coachman etal., 1975). 



The Korolev data provide the first quasi-synoptic coverage 

 of all these water masses within the region, thus allowing 

 quantitative as.sessment of the changes in temperature and 

 salinity as they are advected northward from the Bering Sea 

 into the Chukchi Sea. We now examine the water mass 

 modifications basin by basin. 



GiilfofAiuutyr 



All CTD stations from the Gulf of Anadyr, together with 

 Station 6 from the continental slope south of the gulf, are 

 plotted in Fig. 2a. The latter is in the Bering Slope Current and 

 thus shows the characteristics of this source water to the gulf. 

 It has a water mass curve typical of the current; that is, a 

 temperature minimum of ~2°C at S ~ 33.2 ppt, forming a "V" 

 in T/S space, below which is a T maximum (T ~ 3.8°C at 

 S ~ 33.7 ppt) followed by a T decrease and S increase to the 

 deep basin bottom water type (T ~ 1.6°C; S ~ 34.7 ppt). 



Surface temperatures in the gulf are typically 6 to 8°C at 

 this time of year, with salinities spread over the range 31.5 to 

 33 ppt. The spread in values reflects the nonconservative 

 nature of properties in the upper layer with exchange across the 

 sea surface, true in particular for temperature. 



29 



