Antarctic Research Series Antarctic Oceanology I Vol. 15 OCEANOGRAPHY OF ANTARCTIC WATERS ARNOLD L. GORDON Lamont-Doherty Geological Observatory of Columbia University, Palisades, New York 10964 Abstract. The physical oceanography for the southwest Atlantic and Pacific sectors of antarctic waters is investigated with particular reference to the water structure and meridional circula­ tion. The cyclonic gyres of the Weddell Sea and area to the north and northeast of the Ross Sea are regions of intense deep water upwelling. Water at 400 meters within these gyres occurs at depths below 2000 meters before entering the gyral circulation. The northern boundary for the Weddell gyre is the Weddell-Scotia Confluence, and that for the gyre near the Ross Sea is the secondary polar front zone. The major region for production of Antarctic Bottom Water is the Weddell Sea, whereas minor sources are found in the Ross Sea region and perhaps in the Indian Ocean sector in the vicinity of the Amery Ice Shelf. The Ross Sea Shelf Water contains, in part, water related to a freezing process at the base of the Ross Ice Shelf. The mechanism may be of local importance in bottom water production. The salt balance within the Antarctic Surface Water indicates approximately 60 X 106 m3/sec of deep water upwells into the surface layer during the summer. This value is also found from Ekman divergence calculation. In winter, only one half of this value remains with the surface water; the other half sinks in the production of bottom water. An equal part of deep water is entrained by the sinking water, making the total southward migration of deep water 108 m3/sec during the winter. On averaging over a period of a year, it is found that the deep water merid­ ional transport is approximately 77 X 106 m3/sec. The ratio of zonal to meridional transport is, therefore, between 3:1 to 2:1. The recirculation of water between the antarctic water masses and Circumpolar Deep Water is large. The volume of water introduced by the inflow of North Atlantic Deep Water is only a fraction of the recirculation transport but is essential in that its high salinity maintains the steady state salinity condition of antarctic waters. I N T R O D U C T I O N For the purpose of this study, it is sufficient simply The three oceans are the Atlantic, Pacific, and In­ to call the waters within this zone the antarctic dian [Fleurieu, 1798-1800; Krilmmel, 1879]. The waters. This general term is used to denote the waters north polar extremity of the Atlantic is occasionally from the coast of Antarctica northward to the Antarc­ considered to be a separate ocean, the Arctic Ocean, tic Convergence. The water within the zone between but more often it is recognized as a marginal sea of this convergence and the Subtropical Convergence is the Atlantic, in much the same manner as are the sub antarctic water. This term is best applied only Caribbean and Mediterranean seas. The major oceans to the surface layers of this zone, since the intermedi­ are bounded on the south by the shores of Antarctica. ate, deep, and bottom layers are more or less continu­ The zone between Antarctica and the southern coasts ous across the Antarctic Convergence. of Australia, South America, and Africa permits free REVIEW OF ANTARCTIC OCEANOGRAPHY interocean circulation. Such a zone allows processes that equalize the characteristics of the major oceans. The basic structure and circulation of antarctic and Because of the importance of these processes and the subantarctic waters have been extensively studied by obviously similar climatic conditions of this circum­ Dean [1937] and other members of the Discovery polar zone, it is often given a separate name: the Expeditions. Table 1 lists the major general antarctic 'Antarctic Ocean,' 'Antarctic Seas,' or 'Southern Ocean oceanographic references. The purpose of the present (or Oceans).' However, this 'ocean' lacks a northern study is to: (1) elucidate the characteristics of water boundary in the classical sense, and so it is usually set masses and transition zones making up antarctic at an arbitrary latitude or some oceanographic bound­ waters; (2) further investigate bottom water forma­ ary as a convergence or divergence. tion and possible regions of formation; and (3) esti- 169 Copyright American Geophysical Union Antarctic Research Series Antarctic Oceanology I Vol. 15 170 ARNOLD L. GORDON TABLE 1. General Antarctic Oceanographic Studies ANTARCTIC CONVERGENCE (POLAR FRONT ZONE) The Antarctic Convergence, which can be considered Date of Antarctic Author Publication Area as an oceanic polar front zone, is the region separating the antarctic and subantarctic water masses. It has Brennecke 1921 Atlantic characteristics that alternately suggest convergence, Drygalski 1926 Atlantic divergence, or a combination of both [Wexler, 1959]. Deacon 1933 Atlantic The positions of the polar front found by the Eltanin Sverdrup 1933 Atlantic Wiist 1933 Atlantic and those determined by Mackintosh [1946] and Mosby 1934 Atlantic Houtman [1964] are shown in Gordon [1967a, pi. 13]. Wiist 1935-1936 Atlantic Two expressions of the front are defined: the surface Deacon 1937 Circumpolar expression (large surface temperature gradients) and Mackintosh 1946 Circumpolar Midttun and Natvig 1957 Pacific a subsurface frontal expression (the location where Model 1957-1958 Atlantic the temperature minimum begins to increase in depth Burling 1961 SW Pacific toward the north at a relatively rapid rate). The polar Deacon 1963 Circumpolar front zone is found to be 2°-4° of latitude in width. Ishino 1963 Circumpolar The surface and subsurface expressions are many Kort 1964 Circumpolar Brodie 1965 Circumpolar times separated by a number of kilometers; the more Tolstikov 1966 Circumpolar common case is a more southerly surface expression. Gordon 1967a SW Atlantic; In the western Southeast Pacific Basin, a double fron­ SE Pacific tal system is found. In this region, the fairly stable ^min layer extends from Antarctica to the secondary frontal zone. Between the secondary and the more northern primary zone is a region of a weak and mate the meridional water transport. The following broken T\n layer and suggestions of divergences. Oc­ is a very brief account of the oceanography of antarc­ m casionally the Tmin layer descends slightly at the sec­ tic waters. The reader is referred to Deacon [1937, ondary front, but the major descent occurs at the pri­ 1963], Gordon [1967a], and other authors shown in mary front. Eltanin BT data from cruises 25 and 27 Table 1 for a more complete description. (along longitudes 127° and 157°W) indicate that Figure 1 is a schematic representation of the water such a double structure also exists to the west of mass structure, core layers, and meridional compo­ the Mid-Oceanic Ridge (see 'Antarctic Polar Front nents of motion. The main flow is zonal, westward Zone,' this volume). Houtman [1967] shows a simi­ south of the Antarctic Divergence and eastward north lar structure south of New Zealand. The occurrence of the divergence. The surface and bottom water of a double frontal system with combination of con­ masses are antarctic in origin, in that their charac­ vergence and divergence may be fairly common. teristics are acquired south of the Antarctic Conver­ Some of the Antarctic Surface Water sinking in the gence. Their northward and downward component of region of the frontal zone contributes to the formation motion is compensated by a southward and upward flowing deep water mass. The results of this important of the low saline intermediate water of the world meridional exchange are that heat and nutrients are oceans. The rest mixes into the Subantarctic Surface supplied to the surface of antarctic waters from lower Water contributing to the warm water sphere of the latitudes, and the oxygen content of the deep water of world ocean. The descent of the Antarctic Surface the world is replenished. Such a process allows a Water begins when the Tmin layer is between 200 to steady heat flux from ocean to atmosphere and a high 300 meters (see Gordon [1967a, pi. 3]). Although biological productivity rate in the photic zone, main­ the Ti is quickly destroyed by mixing, the low salin­ mn taining the proper environment for life in the deep ity is maintained and is used as the identifying char­ water and the low temperatures of the deep ocean. The acteristic of the intermediate water masses of the world ratio of meridional zonal flow is discussed in a later ocean. Ostapoff [1962] shows surface water cutting section. The structure shown in Figure 1 is found across the 200-meter level as a band of low salinity around Antarctica. However, important variations water. Figure 2 is the salinity at 200 meters con­ with longitude occur within the water column. These structed from Eltanin stations. The low salinity band variations can be correlated with the asymmetry of shows some more detail than that of Ostapoff; it sug­ Antarctica and submarine ridges and basins. gests that sinking is not uniform throughout the area. Copyright American Geophysical Union Antarctic Research Series Antarctic Oceanology I Vol. 15 OCEANOGRAPHY OF ANTARCTIC WATERS 171 Copyright American Geophysical Union Antarctic Research Series Antarctic Oceanology I Vol. 15 Copyright American Geophysical Union Antarctic Research Series Antarctic Oceanology I Vol. 15 OCEANOGRAPHY OF ANTARCTIC WATERS 173 On comparing it with Gordon [19677 a, pi. 14], it tion and character from 400 to 4000 meters suggests is found that the surface water descent compares only minor amounts of convergence at the Weddell- well with the primary frontal zone. The temperature Scotia Confluence. In the surface layer, large horizon­ at 200 meters is shown in Figure 3. The isotherm tal variations are found. Here the boundary of the distribution is extended to the continent by using the Weddell and Southeast Pacific surface water is much data in Tolstikov [1966]. The warmer band of water more turbulent than the deep water boundary. How­ in the southern Southeast Pacific Basin and Weddell ever, the separation is obvious on the T/S diagram Sea shows the position of the Antarctic Divergence. of the area (Figure 4). The colder band just to its north is the Antarctic Sur­ face Water. The convergence occurs in the large tem­ W A T E R M A S S E S perature gradient region. The mean position can be TEMPERATURE-SALINITY RELATION approximated by the 2° isotherm. Botnikov [1964] Water masses can be conveniently defined by their used the 2°C isotherm of the temperature minimum particular relationship of temperature and salinity. layer to define the summer position of the convergence. For this purpose, a plot of temperature against salinity ANTARCTIC DIVERGENCE of all data points is made. Such a plot, the T/S dia­ gram, was introduced to oceanography by Helland- The Antarctic Divergence (average latitude of 65°S) Hansen [1916]. is essentially a wind-produced feature. The wester­ To construct a T/S diagram for the region investi­ lies north of the divergence transport surface water gated by Eltanin, the hydrographic data from most eastward with a small component to the north, whereas of cruises 7 to 27 were used. Figure 4 is the group the coastal easterlies cause a westerly flow with a south­ T/S plot for Eltanin cruises 7, 8, 9, 12, and 22, which ward component to the surface water. The resulting represent the Drake Passage, the Scotia and Weddell divergence and deep water upwelling, which may be of seas, and the areas immediately north and east of a diffusive nature or perhaps occur within limited re­ these seas. gions over short time periods, are the most important The water masses were identified in the following oceanographic processes of antarctic waters. They manner: The Antarctic Surface Water includes the allow the deep water contact with the antarctic atmos­ water within and above the temperature minimum phere and the associated sea-air interaction. The up- layer (100-300 meters). The upper and lower deep welling necessitates a southward flow of the deep water. water are identified by a temperature maximum and This flow on conserving its angular momentum may salinity maximum, respectively. The Weddell Deep help create the zonal currents of antarctic waters and Water (WDW) is that deep water south of the the small amount of attenuation of the current with Weddell-Scotia Confluence. The deep water found in depth. the Pacific sector and north of the Weddell-Scotia Along the antarctic coasts, cold, relatively saline Confluence in the Scotia Sea is called the Southeast shelf water forms, owing to the intense cold and freez­ Pacific Deep Water (SPDW). The water between the ing of sea water. Shelf water on mixing with roughly Antarctic Surface Water and Circumpolar Deep Water equal proportions of deep water forms Antarctic Bot­ and the water between the Circumpolar Deep Water tom Water, which flows northward. This northward and Antarctic Bottom Water constitute transitional motion initiates a westward component of motion zones. Within each of these zones, a layer of zero along the continental rise of Antarctica and accumula­ meridional motion exists. The bottom water boundary tion of bottom water to the east of the main submarine with the deep water is not well defined and is arbitrar­ ridges. ily set at slightly below the 0°C isotherm in the WEDDELL-SCOTIA CONFLUENCE Weddell Sea and +0.5 °C in the Pacific sector. The Subantarctic Surface Water is the thick isohaline layer The Weddell-Scotia Confluence [Gordon, 1967a] or north of the polar front zone. At its base is the Ant­ Bellingshausen Front [Model, 1957, 1958] is the line arctic or Subantarctic Intermediate Water, defined by separating the water derived from the Weddell Sea a weak salinity minimum (it is much more obvious and that derived from the Pacific Ocean. It is a line north of the Subtropical Convergence). A transitional extending from the Bransfield Strait through the cen­ zone between the Subantarctic Surface Water and the tral Scotia Sea and north of the South Sandwich deep water is the relatively isothermal layer between Islands. It is most pronounced and stationary in the these two water masses. Circumpolar Deep Water. The small change in posi­ Copyright American Geophysical Union Antarctic Research Series Antarctic Oceanology I Vol. 15 Copyright American Geophysical Union Antarctic Research Series Antarctic Oceanology I Vol. 15 OCEANOGRAPHY OF ANTARCTIC WATERS 175 Besides the general usefulness of such a diagram face and Subantarctic Surface Water, in these cases, in identifying water masses and defining their T/S are found only by a change in salinity. The water to region, three important facts are found: the south is slightly less dense than the Subantarctic Water. In such a case, some Subantarctic Surface 1. The deep water of the Weddell Sea is in the Water may sink at the front to join with water of the same T/S region as the bottom water of the Southeast temperature minimum layer. Pacific Basin. Therefore, it is reasonable to conclude 3. The Antarctic Surface Water can be subdivided that the WDW at 400 meters is derived from that bot­ into the surface water of the Weddell Sea and that of tom water which occurs below 3000 meters in the the Scotia Sea. The line of separation is the Weddell- northern Drake Passage. The Southeast Pacific Bot­ tom Water leaves the sea floor in the northern Scotia Scotia Confluence. The surface water of the Weddell Sea and the area to the northwest of South Georgia Sea is colder and spans a greater salinity range. [Gordon, 1966, 1967a]. Therefore, great amounts of The T/S distribution of the Eltanin stations of the upwelling are associated with the transfer of water South Pacific sector of the antarctic waters is shown into the cyclonic Weddell gyre. The oxygen of the in Figure 5. The following cruises are included: 10, WDW is between 4.5^1.7 ml/1 compared to the 4.7- 11, 13, 14, 15, 17, 19, 20, 23, 27. The excluded cruises 4.9 ml/1 range of the bottom water passing through were either in the Tasman Sea, or mainly north of the northern Drake Passage, indicating some oxygen 50 °S. consumption in transit from the Drake Passage to the Basically, the same water masses shown in Figure 4 Weddell Sea. It is interesting to point out that the are found in Figure 5. It is possible to divide the bottom water formed in the Weddell Sea includes some Antarctic Surface Water and the underlying transition of the warmer bottom water of the Southeast Pacific zone into two sections, as is done in the Weddell and Basin, which may be derived from the area of the Scotia seas. The division is the secondary polar front Ross Sea. The volume transport of the water below zone. Besides the sharp difference in the surface T/S 3000 meters in the northern Drake Passage is 25 X points north and south of the secondary front, some 106 m3/sec (calculated from Gordon [19676, fig. 3]). difference is found in the deep water. The upper deep The probable transfer is in the vicinity of 30 °E water south of the secondary front (that is, in the [Model, 1957], where a broad southward penetration southwestern Southeast Pacific Basin and the area im­ of warm water occurs. mediately northeast of the Ross Sea) is in the same The WDW is, in part, converted to surface water by T/S region as the lower SPDW and transition into the sea-air exchange and, in part, entrained with the sink­ Southeast Pacific bottom water, indicating a return ing shelf water in the production to AABW. In addi­ flow of the deep water to the southwest in the same tion, some WDW may exit from the gyre directly. manner as the flow into the Weddell Sea. From the Therefore, it is not possible to arrive at a rate of core layer maps of Gordon [1967a] this return occurs AABW production; however, if all the WDW exits as between 130° to 140 °W. Similar to the WDW, it a 50% component of the AABW, implying that the represents an upwelling of deep water from between surface water of the Weddell gyre is derived from out­ 2000 and 3000 meters to about 400 meters. The gra­ side the Weddell Sea, an upper limit of 50 sv is placed dients across the secondary front zone in the deep on the AABW outflow. The actual value is probably water are not as intense as they are across the Weddell- much less than this value. Scotia Confluence. 2. The warm water occasionally found to over­ The phenomenon suggested by the T/S diagrams ride the temperature minimum layer south of the sub­ of intense upwelling in the cyclonic gyres of the Wed­ surface expression of the polar front [Gordon, 1967a] dell Sea and southwestern Southeast Pacific Basin may is either Subantarctic Surface Water, as in the case of be the primary method in which deep water is carried Eltanin cruise 8, or warmed (modified) Antarctic upward. Similar conditions may exist near the Ker- Surface Water, cruises 7 and 22, which represent guelen Plateau. January and February conditions. The warmed Ant­ The Subantarctic Intermediate Water is much more arctic Surface Water has salinities similar to the Ant­ pronounced in the Pacific sector, covering a T/S re­ arctic Surface Water, that is, 0.2 to 0.3%c lower than gion of slightly lower salinity, perhaps due to the lower the Subantarctic Surface Water. The warming ob­ salinity of the Antarctic or Subantarctic Surface Water. scures the temperature surface expression of the polar Warmed or modified Antarctic Surface Water is found front, and the surface boundaries of the Antarctic Sur­ on cruises 19 and 23, again indicating that the more Copyright American Geophysical Union Antarctic Research Series Antarctic Oceanology I Vol. 15 176 ARNOLD L. GORDON Fig. 4. Temperature-salinity diagram for Drake Passage, Scotia Sea, and Weddell Sea. SPDW = deep water of the Southeast Pacific Basin; SP Bottom = bottom water of the Southeast Pacific Basin; WDW = deep water of the Weddell Sea; NADW = North Atlantic Deep Water. Copyright American Geophysical Union Antarctic Research Series Antarctic Oceanology I Vol. 15 OCEANOGRAPHY OF ANTARCTIC WATERS 177 337 339 34.1 34-3 34-5 34.7 34-9 SALINITY (%o) Fig. 5. Temperature-salinity diagram for Pacific Ocean sector of antarctic waters. Abbreviations as in Figure 4 caption; RSDW = deep water in the ocean region north and northeast of the Ross Sea, but south of the secondary polar front zone. Copyright American Geophysical Union Antarctic Research Series Antarctic Oceanology I Vol. 15 178 ARNOLD L. GORDON southern surface expression of the polar front zone between deep and surface water, indicates the recent relative to the subsurface expression is not always due contact with the sea surface of a substantial compo­ to overriding of Subantarctic Surface Water. nent. The ratio of shelf or surface water to deep water Water masses associated with the Ross Sea are within the Antarctic Bottom Water cannot be far shown in Figure 5. These are the Ross Sea Winter from unity for the bottom water leaving the Weddell Water and the dense Ross Sea Shelf Water, which is Sea; this agrees with the conclusions of Baranov and discussed below. Both of these water masses represent Botnikov [1964] and other considerations discussed a protrusion on the T/S diagram to colder, more saline later in this study. water and, therefore, must have an origin related to The upper boundary of the Antarctic Bottom Water ice formation: either sea ice or freezing beneath the can be seen by a rapid oxygen saturation increase Ross Ice Shelf. close to the sea floor. Figure 7 shows the saturation versus depth of selected regions of antarctic water OXYGEN SATURATION OF ANTARCTIC WATERS between 20 °W and 170°W. Sections a to d are along the path of flow of the bottom water from the The degree of saturation for all Eltanin oxygen data Weddell Sea [Gordon, 1966]. The rapid increase of was calculated based on the solubility of oxygen in oxygen saturation occurs approximately 1000 meters sea water given by Green and Carritt [1967]. The from the sea floor. Substantial amounts of bottom surface water has saturations between 95-100% with water are evident in sections a, c, and d, indicating occasional observation of saturations above 100%. that the main flow is east of the South Sandwich Surface values as high as 108% are found (station Trench. The bottom water of the trench first de­ 522). Supersaturated values may be caused by rapid creases in the degree of saturation by approximately surface heating, observed to occur under calm summer 10% before an increase is observed to the bottom. conditions, which decreases the solubility of the sur­ Adiabatic warming would increase the bottom oxygen face water, causing the initial 100% saturation level saturation level but not by the amount observed near to increase. the trench floor. Therefore some bottom water renewal The vertical convection within the Antarctic Surface occurs, but the trench floor appears not to be the Water causes a high degree of oxygen saturation to major avenue of AABW flow. the base of the surface water. The degree of satura­ Sections e to g are of stations located in the tion is fairly uniform from the surface to the 95% Scotia Sea. In the central Scotia Sea and northern level; a sharp drop in saturation occurs below this. Drake Passage where potential temperatures show The 90% saturation level occurs only meters below little Antarctic Bottom Water, the saturation of the the 95% level and can be taken as the base of free lower 1000 meters increases only slightly or decreases vertical convection. Figure 6 shows the depth of this with depth. In the southern areas of the Scotia Sea surface. The depth of the convective layer south of the which receive a fresh supply of bottom water from the polar front zone rarely exceeds 200 meters. Depths passage between the Bruce and South Orkney ridges, of less than 100 meters are found in the stable surface the bottom saturation shows a marked increase. This water of the southern section of the Southeast Pacific increase begins about 800 meters above the bottom, Basin and the northern Weddell Sea. which agrees well with the upper limits of the bottom The winter values tend to be slightly greater than water in the southern Drake Passage discussed by those found in summer. In the polar front zone, large Gordon [1966] and used in geostrophic calculations variations of depth of the 90% surface are found, [Gordon, 19676]. owing, no doubt, to the fluctuating convergence and Sections h to / in the Southeast Pacific Basin divergence within this zone. Within the Subantarctic show only small increases in bottom oxygen saturation Surface Water, the depths are greater than 300 meters, and, in the case of the southeastern region of the basin, with values as high as 740 meters. a marked decrease. Such a decrease indicates that The lowest degree of saturation (between 50 and 60%) occurs in the vicinity of the temperature maxi­ the bottom oxygen values are significantly influenced mum and oxygen minimum. Below this oxygen satura­ by organic decay and that renewal of highly oxygen­ tion minimum, the saturation increases to values above ated Antarctic Bottom Water is small. Section / in 60%. Where a high percentage of Antarctic Bottom the northern Southeast Pacific Basin shows a steady Water exists, the saturation reaches 80%. The high increase in saturation from the minimum to the bot­ saturation of the bottom water, roughly intermediate tom. A higher percentage of Antarctic Bottom Water Copyright American Geophysical Union