C. Priscu. Kate T. Wing was supported by a National Science covered antarctic lakes. Limnology and Oceanography, 32(1), Foundation REU grant to John C. Priscu. 260-270. Spigel, R.H., I. Fourne, and I. Sheppard. 1991. Difference in tempera- ture and conductivity between the east and west lobes of Lake References Bonney: Evidence for circulation within and between lobes. Antarctic Journal of the U.S., 26(5), 221-222. Vincent, W.F. 1981. Production strategies in antarctic inland waters: Priscu, J.C., L.R. Priscu, W.F. Vincent, and C. Howard-Williams. 1987. Eco-physiology in a permanently ice-covered lake. Ecology, 62(5), Photosynthate partitioning by microplankton in permanently ice- 1215-1224.
Potential hydrologic and geochemical consequences of the 1992 merging of Lake Chad with Lake Hoare in Taylor Valley DIANE M. MCKNIGHT and EDMUND D. ANDREWS, U.S. Geological Survey, Boulder, Colorado 80303
ake levels have been increasing throughout the McMurdo In late January 1992, we observed from a helicopter fly- LDry Valleys since detailed records began in 1960 (Chinn over that Lake Chad appeared to have merged with Lake 1993). Further, there is also evidence that the level of Lake Hoare. On 30 January and 1 February 1992, we studied the Bonney has been rising since the dry valley lakes were first narrows area between the two lakes by making water-level discovered by Scott s party in 1903 (Chinn 1993). Lakes in the measurements and collecting samples for analysis of major dry valleys are fed by glacial meltwater streams that flow for 6 ions. A sample was also obtained above the lake bottom from to 9 weeks during the austral summer, typically during a slush zone at a depth of 6.5 m at a site near the center of December and January. The rising lake levels, therefore, are Lake Chad. The water samples were filtered through 0.4- caused by increased streamfiow associated with longer peri- micrometer (p.m) Nuclepore filters using an Antlia filtration ods of temperatures above freezing and other climatic factors unit; samples for cation analysis were acidified with Ultrex (Chinn 1993). The ultimate cause of the warming trend in cli- nitric acid. Cations were analyzed by inductively coupled plas- mate in the dry valleys is not known. ma spectroscopy and anion analysis by ion chromatography. In addition to being the main source of water to the lakes, On 30 January 1992, we surveyed the water level in the glacial meltwater streams are also important sources of inor- moat areas from the north shore of both Lake Hoare and Lake ganic solutes to the lakes (Green et al. 1989). Solutes in the Chad relative to the New Zealand benchmark NZARPBMT15 streams come from leaching of marine aerosols and calcite, as (76.95 m above mean sea level) located between the two well as from primary weathering reactions occurring within lakes. The water level for both lakes was 74.21 m above mean the streambed alluvium (Green et al. 1989; McKnight and sea level. We interpret these measurements as showing that Andrews in press). Calcite is abundant in the dry valleys Lake Hoare has risen sufficiently such that it is now at the because of calcite deposition in Lake Washburn, which filled same level as Lake Chad. Depending on the inflow from melt- most of the Taylor Valley until about 10,000 years before pre- water streams to either lake in the future, the hydrologic con- sent. The abundance of marine aerosol is dependent upon nection between the two lakes could go in either direction. the proximity to the coast. Therefore, the relative ratio of sodi- Whereas, in the past when the surface of Lake Chad was high- um (Na) to calcium (Ca) as major cations is expected to er than Lake Hoare, the hydrologic connection, when it decrease with increasing distance from the coast. occurred, was always from Lake Chad to Lake Hoare. Lake Hoare is a closed-basin lake located in Taylor Valley The results of water sample analyses are presented in the with its eastern boundary determined by the Canada Glacier table. The results show significant variation in chemistry. (figure); it has been rising since records began in 1972 with a First, the sample of the bottom water of Lake Chad had rela- net rise of 1.35 meters (m) (Wharton et al. 1992; Chinn 1993). tively high solute concentrations, with Na and sulfate (SO4) The major streams flowing into Lake Hoare receive drainage much greater than Ca and chloride (Cl). The results for the from the Canada Glacier. Lake Chad is located west of Lake Lake Chad outlet and the two sites in the narrows are all sim- Hoare and has a surface area about a tenth of that of Lake ilar and had Ca:Na atomic ratios between 1.3 and 1.0. At the Hoare. Lake Chad receives drainage from the Suess Glacier Lake Hoare inlet, the Na concentrations were comparable to and can, in turn, drain into Lake Hoare. Since 1956, flow from those in the narrows, but the Ca concentration was about Lake Chad to Lake Hoare has been seen on aerial pho- half resulting in a lesser Ca:Na ratio of 0.6. The other major tographs of the area, specifically on 5 December 1956, 1 Janu- divalent cations, magnesium (Mg) and strontium (Sr), and ary 1958, 12 January 1975, 18 January 1981, and 20 December the anions SO4 and Cl showed the same pattern as Ca, being 1982 (Wharton personal communication). greater in the narrows than in the Lake Hoare inlet. The
ANTARCTIC JOURNAL - REVIEW 1993 249 102 1h
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Pond 77"40 . Base from U.S. Geological Survey, 0 1 Lake Bonney, Lake Fryxel!, 2 MILES Contour niervdl 50 neters,wUh Antarctica, 1977 Supplementary Contours at 25 meter intervals 0 1 2 KILOMETERS f)t I Map showing location of Lake Hoare and Lake Chad in Taylor Valley. observation that the water in the narrows, the transition zone Both hydrologic and geochemical changes can be envisioned. between the lakes, is most like Lake Chad water suggests that First, the more direct hydrologic transport from the "Lake the average direction of flow is from Lake Chad to Lake Chad" lobe could influence the circulation in the main lake, Hoare. During January 1992, there were other indications of possibly causing a west-to-east flowpattern in the zone just substantial rise in the level of Lake Hoare such as the below the ice cover. Such a flow from the west lobe to the east encroachment of the lake waters near a field camp estab- lobe has been observed in Lake Bonney (Priscu personal com- lished in 1987. munication). Greater velocities under the ice could have sev- The water chemistry in the open water "moat" areas of eral consequences. For example, the major cation composi- the lakes at the end of the streamfiow period is probably con- tion could shift in the zone just below the ice. Also transport trolled by the chemistry of the streamfiow and mixing with of algal and bacterial species from Lake Chad to Lake Hoare the lakewater. The ice cover is about 3.5 to 4 m in Lake Hoare could occur. Another biological consequence may be whereas in Lake Chad, the ice appeared to extend to 6.5 m, enhancement of growth for diatoms, which require some close to the lake bottom. Therefore, mixing with lake water mixing to avoid sinking. In 1987, we found very low abun- may be more significant for meltwater coming into either of dance of several diatoms (for example, Cyclotella sp. and Nay- the two basins in Lake Hoare. The greater Na:Ca ratio in the icula muticopsis) just below the ice cover (depths of 4.1 and Lake Hoare inlet area may possibly reflect differences in the 5.0 m), and no diatoms were found below 7.5 m. Greater relative importance of sources of solutes, such as leaching of abundances and diversity of diatoms may occur if there were marine aerosols, dissolution of calcite, and primary weather- a layer below the ice with flow going from the "Lake Chad" ing reactions. lobe to Lake Hoare. The merging of the two lakes will cause the meltwater It is possible that the changes associated with the merg- from the Suess Glacier to interact more directly and rapidly ing of the two lakes would leave a record of an "abrupt" with the water in upper layer just below the ice in Lake Hoare. change of some kind in the lake sediments, such as the
ANTARCTIC JOURNAL REVIEW 1993 250 - q1y
Major ion chemistry in Lake Chad and Lake Hoare on 1 February 1992
Lake Chad bottom 793 97 527 1.6 5.8 12.2 161 40 0.07 Lake Chad outlet 5.8 13.6 3.5 0.09 3.2 8.0 8.0 12.0 1.3 Narrows 6.3 13.3 3.4 0.1 3.9 1.9 8.0 11.9 1.2 End of Narrows 8.2 14.4 3.9 0.1 4.04 3.7 8.5 12.7 1.0 Lake Hoare inlet 7.2 7.4 2.2 .06 3.7 1.70 5.4 9.0 0.6 aln milligrams per liter. bSj02 denotes silica.
appearance of particular diatom species in the sedimentary in antarctic lakes. (Antarctic Research Series, Vol. 39.) Washington, record. These observations point out that distinct or abrupt D.C.: American Geophysical Union. events affecting the physical system can occur during the 10- Green, W.J. T.J. Gardner, T.G. Ferdelman, M.P. Angle, L.C. Varner, and P. Nixon. 1989. Geochemical processes in the Lake Fryxell to 100-year periods of gradual, but steady, climatic change. basin (Victoria Land, Antarctica). Hydrobiologia, 172, 129-148. The possibility of such physical events might be considered in McKnight, D.M., Aiken, G.R., Andrews, E.D., Bowles, E.G., and Har- the paleolimnological study of lake sediments to elucidate nish, R.A. 1993. Dissolved organic material in Dry Valley lakes: A conditions in the past. comparison of Lake Fryxell, Lake Hoare, and Lake Vanda. In W.J. We thank R. Harnish and V.C. Stephens for their assis- Green, E.I. Friedman (Eds.), Physical and biogeochemical processes in antarctic lakes. tance in the analysis of major ions. This research was support- (Antarctic Research Series, Vol. 39.) Washington, D.C.: American Geophysical Union. ed by the National Science Foundation grant OPP 88-17113. McKnight, D.M., and E.D. Andrews. In press. Hydrologic and geo- chemical processes at the stream-lake interface in a permanently References ice-covered lake in the McMurdo Dry Valleys, Antarctica. Ver- handlungen International Verein Limnologie. Aiken, G.R., D.M. McKnight, R.L. Wershaw, and L. Miller. 1991. Evi- Priscu, J.C. 1993. Personal communication. dence for the diffusion of aquatic fulvic acids from the sediments Wharton, R.A., Jr. 1993. Personal communication. of Lake Fryxell, Antarctica. In R.A. Baker (Ed.), Organic substances Wharton, R.A. Jr., G.P. McKay, G.D. Glow, D.T. Andersen, G.M. Sim- and sediments in water. Ann Arbor: Lewis Publishers. mons Jr., and F.G. Love. 1992. Changes in ice cover thickness and Chinn, T.J. 1993. Physical hydrology of the dry valley lakes. In W.J. lake level of Lake Hoare, Antarctica: Implications for local climatic Green, E.I. Friedman (Eds.), Physical and biogeochemical processes change. Journal of Geophysical Research, 97(C3), 3503-3513.
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