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Water Mass Distribution in Fram Strait and Over the Yermak Plateau in Summer 1997

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Water Mass Distribution in Fram Strait and Over the Yermak Plateau in Summer 1997 Ann. Geophysicae 18, 687±705 (2000) Ó EGS ± Springer-Verlag 2000 Water mass distribution in Fram Strait and over the Yermak Plateau in summer 1997 B. Rudels1, R. Meyer2, E. Fahrbach2, V. V. Ivanov3, S. ésterhus4, D. Quadfasel5 U. Schauer2, V. Tverberg6, R. A. Woodgate7 1 Finnish Institute of Marine Research, Lyypekinkuja 3A, P.O. PL33, FIN-00931 Helsinki, Finland e-mail: rudels@®mr.® 2 Alfred-Wegener-Institut fuÈ r Polar und Meeresforschung, Columbus straûe, Postfach 120161, D-27515 Bremerhaven, Germany 3 Arctic and Antarctic Research Institute, Ocean/Atmosphere Department, 38, Bering Street, 199397 St. Petersburg, Russia 4 Geophysical Institute, University of Bergen, Alle gaten 70, N-5007 Bergen, Norway 5 Niels Bohr Institute for Astronomy, Physics and Geophysics, University of Copenhagen, Juliane Maries Vej 30 DK-2100 Copenhagen é, Denmark 6 University Courses of Svalbard, Geophysics Marine Research, Postboks 156/157, N-9170 Longyearbyen, Norway 7 Applied Physics Laboratory, University of Washington, 1013 NE 40th Street, Seattle, Washington 98105-6698, USA Received: 26 May 1999 / Revised: 23 February 2000 / Accepted: 2 March 2000 Abstract. The water mass distribution in northern Fram Key words: Oceanography: general (Arctic and Strait and over the Yermak Plateau in summer 1997 is Antarctic oceanography; water masses) ± described using CTD data from two cruises in the area. Oceanography: physical (general circulation) The West Spitsbergen Current was found to split, one part recirculated towards the west, while the other part, on entering the Arctic Ocean separated into two branches. The main in¯ow of Atlantic Water followed the Svalbard continental slope eastward, while a second, narrower, branch stayed west and north of the Yermak 1 Introduction Plateau. The water column above the southeastern ¯ank of the Yermak Plateau was distinctly colder and less Fram Strait has long been considered the most impor- saline than the two in¯ow branches. Immediately west of tant communication link between the Arctic Ocean and the outer in¯ow branch comparatively high tempera- the Nordic Seas. At the turn of the century, it was tures in the Atlantic Layer suggested that a part of the known that an out¯ow of cold polar water and sea ice extraordinarily warm Atlantic Water, observed in the took place through the strait, and that a warm boundary current in the Eurasian Basin in the early subsurface layer, originating from an in¯ow of warm 1990s, was now returning, within the Eurasian Basin, Atlantic Water (AW) through Fram Strait, was present toward Fram Strait. The upper layer west of the Yermak in the interior of the Arctic Ocean (Nansen, 1902). It Plateau was cold, deep and comparably saline, similar to was, however, believed that the export of Polar Surface what has recently been observed in the interior Eurasian Water (PSW) dominated the exchanges, and that the Basin. Closer to the Greenland continental slope the main in¯ow from the Nordic Seas to the Arctic Ocean salinity of the upper layer became much lower, and the passed over the Barents Sea (Helland-Hansen and temperature maximum of the Atlantic Layer was Nansen, 1909). The Barents Sea in¯ow, after interacting occasionally below 0.5 °C, indicating water masses with run-o from the Siberian rivers, would then supply mainly derived from the Canadian Basin. This implies most of the PSW, and, because of freezing, brine that the warm pulse of Atlantic Water had not yet made rejection, and the formation of dense water over the a complete circuit around the Arctic Ocean. The shallow shelves, perhaps partly ventilate the deeper Atlantic Water of the West Spitsbergen Current recir- layers of the Arctic Ocean (Nansen, 1906). Nansen, culating within the strait did not extend as far towards however, later came to believe that the deep water in the Greenland as in the 1980s, leaving a broader passage for Arctic Ocean derived from the Greenland Sea and waters from the Atlantic and intermediate layers, exiting entered through Fram Strait (Nansen, 1915). Almost all the Arctic Ocean. A possible interpretation is that the of these conjectures have been found to be valid. Even circulation pattern alternates between a strong recircu- Nansen's initial suggestion (1902, 1906) that the Arctic lation of the West Spitsbergen Current in the strait, and Ocean deep waters were formed by slope convection, a larger exchange of Atlantic Water between the Nordic bringing brine-enriched shelf water into the deep Arctic Seas and the inner parts of the Arctic Ocean. Ocean basins, is now considered a more important process for the ventilation of the deep Arctic Ocean than an in¯ow of deep water from the Nordic Seas. (Aagaard Correspondence to: B. Rudels et al., 1985; Jones et al., 1995). 688 B. Rudels et al.: Water mass distribution in Fram Strait and over the Yermak Plateau in summer 1997 The severe climate and the presence of sea ice make ward-drifting sea ice and maintains the open water the observation conditions in Fram Strait harsh, and north of Svalbard, known as the Whalers' Bay (Aagaard the early transport estimates were derived, either from et al., 1987; Untersteiner, 1988). Fram Strait is the only geostrophic velocities calculated for the ice-free part of deep connection to the Arctic Ocean, and although the the strait, dominated by the West Spitsbergen Current, out¯ow of PSW through the Canadian Arctic Archipel- and/or from mass and salt conservation arguments ago is about as large as that leaving through Fram Strait (Timofeyev, 1961, 1963; Mosby, 1962; Vowinckel and (1 Sv) (Rudels, 1986; Steele et al., 1996), all denser Orvig, 1970). In the 1970s the ®rst year-long time series water masses must exit through Fram Strait. Further- from current meters moored in the West Spitsbergen more, >90% of the sea ice exported from the Arctic Current became available (Aagaard et al., 1973), and Ocean passes through Fram Strait (Vowinckel and the transport estimates for the West Spitsbergen Current Orvig, 1970). rose from 3±4 Sv to 7 Sv (1 Sv = 106 m3 s)1). Fram Recent studies have shown that the circulation in the Strait became regarded as the most important passage, Arctic Ocean comprises several loops and the waters not just for exiting polar waters, but also for the in¯ow passing along the separate loops, acquire dierent of Atlantic Water from the Nordic Seas. Aagaard and characteristics (Rudels et al., 1994; McLaughlin et al., Greisman (1975) worked out a mass budget for the 1996). Intensi®ed ®eld work in the interior of the Arctic Arctic Ocean, where the in¯ow and out¯ow through Ocean, from ice breakers as well as from submarines, Fram Strait were balanced and, in addition to an has also revealed substantial variations in the water out¯ow of 1.8 Sv of PSW, 5.3 Sv of cooled Modi®ed mass characteristics compared to the climatological (and Atlantic Water (MAW) were exported from the Arctic. previously assumed quasi-stationary) water mass prop- These results, and the importance of the meridional erties of the interior Arctic Ocean (Quadfasel et al., oceanic heat and freshwater transports for the climate of 1991; Carmack et al., 1995; Morison et al., 1998; Steele the Arctic, led to intensi®ed measuring activity in Fram and Boyd, 1998). These variations imply changes in the Strait. HMS Ymer made complete crossings in 1980 water mass transformations in the Nordic Seas, and in (Rudels, 1987). In 1983 and 1984 the Marginal Ice Zone the Arctic Ocean, that eventually could aect the global Experiment (MIZEX) studied atmosphere-ice-ocean thermohaline circulation through the over¯ow of dense interactions and mixing processes associated with the water across the Greenland-Scotland Ridge. The inter- meeting of the northward-¯owing West Spitsbergen national Arctic Ocean System Study (ACSYS) co- Current and polar water and ice, exiting the Arctic ordinated by the World Climate Research Programme Ocean in the East Greenland Current. Several complete (WCRP), and the European Commission programme on crossings of the strait were made during MIZEX and in the Variability of Exchanges in the Northern Seas the years after (Quadfasel et al., 1987; Bourke et al., Programme (VEINS), among others, are investigating 1988), and the current meter observations were extended this variability. VEINS involves a simultaneous study of westward to the East Greenland Current (Foldvik et al., the exchanges through the four main passages to the 1988). These studies showed that the recirculation of Nordic Seas: the Faeroe-Shetland Channel: the Barents AW in Fram Strait was considerable and that the in¯ow Sea; Fram Strait; and Denmark Strait. of AW to the Arctic Ocean was much smaller (0.6± 1.5 Sv, Aagaard and Carmack, 1989) than previously estimated. The measured out¯ow of 3 Sv in the East 2 Observations Greenland Current above 700 m (Foldvik et al., 1988) then suggested a stronger in¯ow to the Arctic Ocean Hydrographic observations were made on the ARK- over the Barents Sea than through Fram Strait, in XIII-2 cruise of RV Polarstern in July 1997 and included agreement with the earlier view (Helland-Hansen and two crossings (sections II and III) of the northern Fram Nansen, 1909). Strait and the Yermak Plateau, and a short meridional In contrast to Fram Strait proper, the area north of section (V) north of Spitsbergen (Fig. 1a) (Stein and the strait has been less systematically studied and mainly Fahl, 1997). One month later, during a cruise with RV by extensive, but shorter, ®eld campaigns: e.g., the Lance in Fram Strait proper, a zonal hydrographic airborne Eurasian Basin Experiment (EUBEX) in the section, along 78°50¢N in the eastern and along 79°Nin western Eurasian Basin (Perkin and Lewis, 1984), partly the western part of the strait, was added (section I, MIZEX, and the Co-ordinated Eastern Arctic Experi- Fig.
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