Alkalinity and Strontium Profiles in Antarctic Waters
TEMP (°C)
SAL.(PERCENT)
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On Cruises 23 and 24, the Antarctic and Subtropical Convergences, respectively, were investigated. While the determination of temperature changes was the most important factor in defining the Antarctic Convergence, the observation of salinity variations was more significant to the definition of the Subtropical Convergence. On Cruise 26, activity was confined to the Tasman Sea, where hydrographic stations were occupied mainly in support of the biological program.
4(
5( 6(
7(
8( 9( 10 DEPTH (M) STD analog record at Eltanin station 607
from the ship, were placed around the STD sensors. Such calibration indicates that the observed microstructure is real. The figure shows the salinity and temperature analog trace of the upper 1,000 m for station 607 (59°S. 127°W.). Note the differences between the up and down traces. This may be due to shifting of the secondary inversions, which are probably of small horizontal extent. The inversions are of greatest magnitude within the T,1111, layer. An STD profile along 127°30'W. clearly shows the sinking and gradual deterioration of the T 111, layer (along with the secondary inversions) in the vicinity of the Antarctic Convergence. A similar structure is observed in the salinity values. The STD data promise to open a new dimension to the physical oceanographer. The bathythermograph (BT) program was continued throughout 1966. Analyses of the BT data for Cruises 25 and 27 (the latter one taking place during the first two months of 1967) indicate that a double Antarctic Convergence zone (primary and secondary components) occurs west of the Albatross Cordillera; such a zone had been found previously in the western part of the Southeast Pacific Basin. The eventual digitization of all of the BT data will enable them to be used more efficiently. 186
Alkalinity and Strontium Profiles in Antarctic Waters KARL K. TUREKIAN, DONALD F. SCHUTZ, PETER BOWER, and DAVID G. JOHNSON Department of Geology Yale University In continuation of our work on the distribution of the alkaline-earth metals in antarctic and adjacent waters as possible indicators of oceanic mixing processes, we have analyzed samples of seawater from the antarctic seas for strontium and alkalinity. Two profiles in the eastern Pacific sector of Antarctica (Eltanin Cruise 11) have been analyzed for strontium (Turekian and Schutz, 1965), and these two profiles as well as two profiles from the western Atlantic sector of Antarctica (Eltanin Cruise 22) have been analyzed for specific alkalinity. Analyses by X-ray fluorescence of the amounts of strontium in seawater are subject to an error of 2.2 percent coefficient of variation. The range of values obtained for water samples from antarctic seas exceeds this analytical error, whereas the range for samples from the rest of the world's oceans can be explained in terms of the error. The contour intervals of Fig. I are drawn with the analytical error in mind, and the resulting pattern shows the general features of distribution of strontium concentration with longitude. Clearly, the profile at 115'W. reveals a higher average strontium level (normalized to a constant chlorinity) than the profile at about 90°W. Alkalinity, as determined by the method of Anderson and Robinson (1946), was converted to specific alkalinity on the basis of salinity data obtained by the Lamont Geological Observatory at the time of collection. The results are presented in Fig. 2. ANTARCTIC JOURNAL
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It is evident that the two profiles in the Pacific sector (115° and 90°W.) and the one in the westernmost Atlantic sector show highly convoluted patterns with values ranging from 0.1026 to 0.1318—a difference of 30 percent. On the other hand, the profile at 15°W. is almost homogeneous in specific alkalinity. Along the 115'W. profile, a marked change in specific alkalinity appears to occur at the southern extension of the Albatross Cordillera between antarctic and Pacific waters. This discontinuity is seen not only in the level of strontium but also in that of the trace elements silver, cobalt, and nickel (Schutz and Turekian, 1965). Any interpretations we make at the present time are tenuous, but they do show the desirable paths for future studies: (1) On the basis that the water mass surrounding Antarctica has a net westward movement, it appears that it becomes highly textured with respect to specific alkalinity as the result of biological removal of calcium carbonate from the surface waters and its resolution at depth. (2) Where prominent physical barriers exist, such as the southern portion of the Albatross Cordillera, the chemical properties of the antarctic waters are distinct from those north of the barriers. This is true with respect to specific alkalinity and concentrations of strontium, silver, cobalt, and nickel. (3) The concentration of strontium in the eastern Pacific sector of Antarctica varies—notably, the average concentration is lower along the 90°W. profile than along the 115°W. profile. (4) There is no clear correlation between the amounts of barium (Turekian and Johnson, 1966) and strontium and specific alkalinity. (5) Data on specific alkalinity and strontium levels might be useful as indicators of the history of the antarctic water masses.
BIOLOGY
Zoogeography of Antarctic and Subantarctic Planktonic Foraminifera in the Atlantic and Pacific Ocean Sectors ALLAN W. H. BIE Lamont Geological Observatory Columbia University
1964, p. 41-89.
One antarctic, two antarctic-subantarctic, and six subantarctic species of planktonic Foraminifera have been observed in the two major faunistic regions that are separated by the Antarctic Convergence (Antarctic Polar Front). The only prolific antarctic species south of the Convergence is Globigerina pachyderma. Six species occur generally north of the Antarctic Convergence in subantarctic waters, namely Globigerina bulloides, Globorotalia inflata, Globorotalia truncatulinoides, Globorotalia scitula, Globigerinita glutinata, and a yet-unnamed new species of Globorotalia. Globigerina quinqueloba and Globigerinita uvula are found more frequently in the antarctic region than the other species referred to, but they are also commonly encountered in subantarctic waters. All species show widely overlapping distributions, but the centers of maximum concentration of each species are clearly delineated and are generally located either in antarctic or subantarctic waters. The subantarctic species can cross the Antarctic Convergence and exist over an average distance of 300 miles southward before they completely disappear. The preferred seasonal occurrence of G. truncatulinoides is between early May and late October, while G. inflata proliferates between early August and late December. In the austral winter (June-September), the upper 100 m of water around Antarctica is comparatively barren of plankton (including Foraminifera), as the bulk of the planktonic populations inhabit waters between 250 and 1,000 m during this period. In comparing the fossil assemblages in bottom sediments studied by Blair (1965) with living populations from the same regions, we have noted the following facts: The largest populations of fossil representatives of G. pachyderma (20 percent isopleth), G. bulloides (20 percent isopleth), G. truncatulinoides (5 percent isopleth), and G. in flata (10 percent isopleth) are all north of the
188
ANTARCTIC JOURNAL
References Anderson, D. H. and R. J. Robinson. 1946. Rapid electrometric determination of the alkalinity of seawater using a glass electrode. Analytical Chemistry, 18: 767-773. Schutz, D. F. and K. K. Turekian. 1965. The distribution of cobalt, nickel, and silver in ocean water profiles around Pacific Antarctica. Journal of Geophysical Research, 70 (22): 5519-5528. Turekian, K. K. and D. G. Johnson. 1966. The barium distribution in seawater. Geochimica et Cosmochimica Acta, 30: 1153-1174. Turekian, K. K. and D. F. Schutz. 1965. Trace element
economy in the oceans. Rhode Island. University. Narragansett Marine Laboratory. Occasional Publication No.
3, Marine Geochemistry, Proceedings of a Symposium held at The University of Rhode Island, October 29-30,
SAL.(PERCENT)
IC 2C 3C
On Cruises 23 and 24, the Antarctic and Subtropical Convergences, respectively, were investigated. While the determination of temperature changes was the most important factor in defining the Antarctic Convergence, the observation of salinity variations was more significant to the definition of the Subtropical Convergence. On Cruise 26, activity was confined to the Tasman Sea, where hydrographic stations were occupied mainly in support of the biological program.
4(
5( 6(
7(
8( 9( 10 DEPTH (M) STD analog record at Eltanin station 607
from the ship, were placed around the STD sensors. Such calibration indicates that the observed microstructure is real. The figure shows the salinity and temperature analog trace of the upper 1,000 m for station 607 (59°S. 127°W.). Note the differences between the up and down traces. This may be due to shifting of the secondary inversions, which are probably of small horizontal extent. The inversions are of greatest magnitude within the T,1111, layer. An STD profile along 127°30'W. clearly shows the sinking and gradual deterioration of the T 111, layer (along with the secondary inversions) in the vicinity of the Antarctic Convergence. A similar structure is observed in the salinity values. The STD data promise to open a new dimension to the physical oceanographer. The bathythermograph (BT) program was continued throughout 1966. Analyses of the BT data for Cruises 25 and 27 (the latter one taking place during the first two months of 1967) indicate that a double Antarctic Convergence zone (primary and secondary components) occurs west of the Albatross Cordillera; such a zone had been found previously in the western part of the Southeast Pacific Basin. The eventual digitization of all of the BT data will enable them to be used more efficiently. 186
Alkalinity and Strontium Profiles in Antarctic Waters KARL K. TUREKIAN, DONALD F. SCHUTZ, PETER BOWER, and DAVID G. JOHNSON Department of Geology Yale University In continuation of our work on the distribution of the alkaline-earth metals in antarctic and adjacent waters as possible indicators of oceanic mixing processes, we have analyzed samples of seawater from the antarctic seas for strontium and alkalinity. Two profiles in the eastern Pacific sector of Antarctica (Eltanin Cruise 11) have been analyzed for strontium (Turekian and Schutz, 1965), and these two profiles as well as two profiles from the western Atlantic sector of Antarctica (Eltanin Cruise 22) have been analyzed for specific alkalinity. Analyses by X-ray fluorescence of the amounts of strontium in seawater are subject to an error of 2.2 percent coefficient of variation. The range of values obtained for water samples from antarctic seas exceeds this analytical error, whereas the range for samples from the rest of the world's oceans can be explained in terms of the error. The contour intervals of Fig. I are drawn with the analytical error in mind, and the resulting pattern shows the general features of distribution of strontium concentration with longitude. Clearly, the profile at 115'W. reveals a higher average strontium level (normalized to a constant chlorinity) than the profile at about 90°W. Alkalinity, as determined by the method of Anderson and Robinson (1946), was converted to specific alkalinity on the basis of salinity data obtained by the Lamont Geological Observatory at the time of collection. The results are presented in Fig. 2. ANTARCTIC JOURNAL
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It is evident that the two profiles in the Pacific sector (115° and 90°W.) and the one in the westernmost Atlantic sector show highly convoluted patterns with values ranging from 0.1026 to 0.1318—a difference of 30 percent. On the other hand, the profile at 15°W. is almost homogeneous in specific alkalinity. Along the 115'W. profile, a marked change in specific alkalinity appears to occur at the southern extension of the Albatross Cordillera between antarctic and Pacific waters. This discontinuity is seen not only in the level of strontium but also in that of the trace elements silver, cobalt, and nickel (Schutz and Turekian, 1965). Any interpretations we make at the present time are tenuous, but they do show the desirable paths for future studies: (1) On the basis that the water mass surrounding Antarctica has a net westward movement, it appears that it becomes highly textured with respect to specific alkalinity as the result of biological removal of calcium carbonate from the surface waters and its resolution at depth. (2) Where prominent physical barriers exist, such as the southern portion of the Albatross Cordillera, the chemical properties of the antarctic waters are distinct from those north of the barriers. This is true with respect to specific alkalinity and concentrations of strontium, silver, cobalt, and nickel. (3) The concentration of strontium in the eastern Pacific sector of Antarctica varies—notably, the average concentration is lower along the 90°W. profile than along the 115°W. profile. (4) There is no clear correlation between the amounts of barium (Turekian and Johnson, 1966) and strontium and specific alkalinity. (5) Data on specific alkalinity and strontium levels might be useful as indicators of the history of the antarctic water masses.
BIOLOGY
Zoogeography of Antarctic and Subantarctic Planktonic Foraminifera in the Atlantic and Pacific Ocean Sectors ALLAN W. H. BIE Lamont Geological Observatory Columbia University
1964, p. 41-89.
One antarctic, two antarctic-subantarctic, and six subantarctic species of planktonic Foraminifera have been observed in the two major faunistic regions that are separated by the Antarctic Convergence (Antarctic Polar Front). The only prolific antarctic species south of the Convergence is Globigerina pachyderma. Six species occur generally north of the Antarctic Convergence in subantarctic waters, namely Globigerina bulloides, Globorotalia inflata, Globorotalia truncatulinoides, Globorotalia scitula, Globigerinita glutinata, and a yet-unnamed new species of Globorotalia. Globigerina quinqueloba and Globigerinita uvula are found more frequently in the antarctic region than the other species referred to, but they are also commonly encountered in subantarctic waters. All species show widely overlapping distributions, but the centers of maximum concentration of each species are clearly delineated and are generally located either in antarctic or subantarctic waters. The subantarctic species can cross the Antarctic Convergence and exist over an average distance of 300 miles southward before they completely disappear. The preferred seasonal occurrence of G. truncatulinoides is between early May and late October, while G. inflata proliferates between early August and late December. In the austral winter (June-September), the upper 100 m of water around Antarctica is comparatively barren of plankton (including Foraminifera), as the bulk of the planktonic populations inhabit waters between 250 and 1,000 m during this period. In comparing the fossil assemblages in bottom sediments studied by Blair (1965) with living populations from the same regions, we have noted the following facts: The largest populations of fossil representatives of G. pachyderma (20 percent isopleth), G. bulloides (20 percent isopleth), G. truncatulinoides (5 percent isopleth), and G. in flata (10 percent isopleth) are all north of the
188
ANTARCTIC JOURNAL
References Anderson, D. H. and R. J. Robinson. 1946. Rapid electrometric determination of the alkalinity of seawater using a glass electrode. Analytical Chemistry, 18: 767-773. Schutz, D. F. and K. K. Turekian. 1965. The distribution of cobalt, nickel, and silver in ocean water profiles around Pacific Antarctica. Journal of Geophysical Research, 70 (22): 5519-5528. Turekian, K. K. and D. G. Johnson. 1966. The barium distribution in seawater. Geochimica et Cosmochimica Acta, 30: 1153-1174. Turekian, K. K. and D. F. Schutz. 1965. Trace element
economy in the oceans. Rhode Island. University. Narragansett Marine Laboratory. Occasional Publication No.
3, Marine Geochemistry, Proceedings of a Symposium held at The University of Rhode Island, October 29-30,
