Antarctic aerosol research
References
Brost, R. A., and Wyngaard, J . C. 1978. A model study of the stably stratified planetary boundary layer. Journal of Atmospheric
Science, 35, 1427-1440.
Carroll, J . J. 1979. Long-term means and short-term variability of the surface energy balance components at the South Pole. Presented at Symposium on Antarctic Meteorology (17th General
Antarctic aerosol research S. BARNARD, R. HENRY, A. HoGAN, and J. SAMPSON
Atmospheric Sciences Research Center State University of New York-Albany Albany, New York 12203 S. Barnard departed for Antarctica in October, arrived at Pole just after the station opening, and remained there through the austral summer 1979-80. J. Samson arrived at Pole in mid-December. They continued a series of aerosol observations and investigations of basic meteorological transport processes and began a new series of experiments to estimate the flux of aerosol particles from the antarctic atmosphere to the surface snow and firn. R. Henry arrived at McMurdo Station in early January. He began a new series of observations of ozone, small ions, aerosol particles, and water vapor near the surface. This program will attempt to (1) determine the frequency of intrusions of stratospheric air to the surface about the periphery of Antarctica, (2) evaluate the transport of marine moisture across the Ross Ice Shelf, and (3) establish the characteristics of small ion concentrations in the extremely clear air arriving at McMurdo from the ice cap. A. Hogan joined usccc Northwind in Wellington, New Zealand, on 19 December 1979 and made aerosol, solar, and other meteorological observations along a track from Wellington to Campbell Island to the Ross Sea (figure). These observations were continued at McMurdo and Vanda Stations. The 1979-80 austral summer was unusual in that a persistent flow was established, bringing relatively warm air to Antarctica through most of the season. Relatively weak (for the southern ocean) northerly winds followed the Northwind almost to Antarctica, finally yielding to the polar easterlies over the Ross Sea. During early January this flow became strong enough to cause persistent "southerly" winds (along the international dateline, rather than from the usual direction along the Greenwich meridian) at the surface at the South Pole. As such flow may transport material from the Ross Sea area to the South Pole, which might 182
Assembly of International Union of Geodesy and Geophysics, Canberra, Australia). Carroll, J . J. , and Fitch, B. W. 1980. Dependence of snow albedos on solar elevation and cloudiness at the South Pole. Manuscript submitted for publication. Carroll, J. J., and Fitzjarrald, D. E. 1979. Atmosphere-surface interactions in the unsteady, stable planetary boundary layer. Presented at Symposium on Antarctic Meteorology, (17th General Assembly of International Union of Geodesy and Geophysics, Canberra, Australia).
later be found in firn strata, we are now analyzing the 20-year Pole Station record to determine the frequency of such transport. Aerosol observations indicate that surface aerosol concentrations in the South Pacific are similar to those measured in the past over the North Pacific and the Icelandic low pressure area of the North Atlantic (Hogan 1976). Aerosol concentrations over the Ross Sea were comparable to those measured by Meszaros and Vissy (1974) over the Weddell Sea. Solar observations show the total atmosphere to be quite clear and low in aerosol concentration from 40° to 50°S but quite turbid in the vicinity of the Antarctic Convergence. The air of the polar easterlies over the Ross Sea was also quite low in total aerosol content, but not nearly as low as antarctic continental air measured over McMurdo and Vanda Stations. The Angstrom (1961) turbidity (total attenuation of sunlight by aerosol particles) measured at McMurdo and Vanda Stations showed no change from similar measurements made near there by Fischer in 1967 and at Mandheim in 1949 (Liljequist 1956). This research was supported by National Science Foundation grants DPP 76-23110 and DPP 76-23115 and by National Oceanic and Atmospheric Administration grant 047 022 44025. The authors offer special thanks to Captain Garrett and the officers and men of Northwind for their enthusiastic support, and to the New Zealand Antarctic Research Program, Gary Lewis, and Brian Leech for their assistance at Vanda Station.
References
Angstrom, A. Techniques of determining the turbidity of the atmosphere. Tellus, 13, 214-223. Fischer, W. H. 1967. Some atmospheric turbidity measurements in Antarctica. Journal of Applied Meteorology, 6, 958-959. Hogan, A. 1976. Physical properties of the atmospheric aerosol (Final report NSF grant GA 32502, ASRC Report 408). Liljequist, G. H. 1956. Energy exchange of an antarctic snowfield. In
Norwegian British Swedish Antaittic Expedition 1949-52, Scientific Results (Vol. 2, Part 1). Oslo: Norsk Polarinstitutt. Meszaros, A. and Vissy, K. 1974. Concentrations, size distribution
and chemical nature of atmospheric aerosol particles in remote oceanic areas. Aerosol Sciences, 5, 101-109. ANTARCTIC JOURNAL
I NORTHWINO CRUISE WINO (TIME)
6 12 18
- I I I
TEMPERATURE AIR SEA C C 0 10 0 10
AEROSOL SUN CN V/M Afl NIP 102CM3 10-6 CM 3 LY/MIN 0 100 100 10 1
50
lN
— 6O
'J)L. 4'
-
F p—. 70
L
I I
=-
11111111
III III II III
Aerosol concentrations, solar intensity, atmospheric turbidity, and meteorological conditions encountered along the cruise route of uscoc Northwlnd from Wellington, New Zealand, to Campbell Island to McMurdo Sound, 19 December 1979-6 January 1980.
Balloon-borne measurements of trace gases and aerosols over the South Pole D. J. HOFMANN, J. M. Ros, A. F. Fui, J. W. HARD ER , N. T. Kio, and C. L. OlsoN Department of Physics and Astronomy University of Wyoming Laramie, Wyoming 82077
D. L. ALBRrrrON, A. L. SCHMELTEKOPF and P. D. GOLDAN Aeronomy Laboratory National Oceanic and Atmospheric Administration Boulder, Colorado 80303
In January 1980, nine balloon soundings were conducted from South Pole Station. This campaign marked the ninth and final summer of stratospheric research in Antarctica by 1980 REVIEW
the Department of Physics and Astronomy at the University of Wyoming. Measurements conducted included two sets of five trace gas samples to a height of 31 kilometers, aerosol particles (radius ^!t0.15 micrometers) and condensation nuclei (radius 2:0.01 micrometers) to 28 kilometers, and five short soundings of condensation nuclei to about 4 kilometers to study the surface condensation nuclei features. As in the past, the air samples were analyzed by the National Oceanic and Atmospheric Administration (No) Aeronomy Laboratory in Boulder, Colorado; the results for the two soundings are shown in figure 1. For the first time large plastic balloons were employed at South Pole. This allowed samples to be obtained above 30 kilometers. Samples of methyl chloroform (CH3CC13) were obtained in addition to nitrous oxide (N 20), and the fluorocarbons F-12 (CF2 0 2), and F-il (CFC1 3). This marks the fourth measurement of the latter three gases, each a year apart. While stratospheric levels do not show a consistent time dependence, probably because of transport effects, which require averaging over a much larger data set, the upper tropospheric (6 to 7 kilometers) samples apparently do. Figure 2 shows the time history of these gases at this level. 183
Brost, R. A., and Wyngaard, J . C. 1978. A model study of the stably stratified planetary boundary layer. Journal of Atmospheric
Science, 35, 1427-1440.
Carroll, J . J. 1979. Long-term means and short-term variability of the surface energy balance components at the South Pole. Presented at Symposium on Antarctic Meteorology (17th General
Antarctic aerosol research S. BARNARD, R. HENRY, A. HoGAN, and J. SAMPSON
Atmospheric Sciences Research Center State University of New York-Albany Albany, New York 12203 S. Barnard departed for Antarctica in October, arrived at Pole just after the station opening, and remained there through the austral summer 1979-80. J. Samson arrived at Pole in mid-December. They continued a series of aerosol observations and investigations of basic meteorological transport processes and began a new series of experiments to estimate the flux of aerosol particles from the antarctic atmosphere to the surface snow and firn. R. Henry arrived at McMurdo Station in early January. He began a new series of observations of ozone, small ions, aerosol particles, and water vapor near the surface. This program will attempt to (1) determine the frequency of intrusions of stratospheric air to the surface about the periphery of Antarctica, (2) evaluate the transport of marine moisture across the Ross Ice Shelf, and (3) establish the characteristics of small ion concentrations in the extremely clear air arriving at McMurdo from the ice cap. A. Hogan joined usccc Northwind in Wellington, New Zealand, on 19 December 1979 and made aerosol, solar, and other meteorological observations along a track from Wellington to Campbell Island to the Ross Sea (figure). These observations were continued at McMurdo and Vanda Stations. The 1979-80 austral summer was unusual in that a persistent flow was established, bringing relatively warm air to Antarctica through most of the season. Relatively weak (for the southern ocean) northerly winds followed the Northwind almost to Antarctica, finally yielding to the polar easterlies over the Ross Sea. During early January this flow became strong enough to cause persistent "southerly" winds (along the international dateline, rather than from the usual direction along the Greenwich meridian) at the surface at the South Pole. As such flow may transport material from the Ross Sea area to the South Pole, which might 182
Assembly of International Union of Geodesy and Geophysics, Canberra, Australia). Carroll, J . J. , and Fitch, B. W. 1980. Dependence of snow albedos on solar elevation and cloudiness at the South Pole. Manuscript submitted for publication. Carroll, J. J., and Fitzjarrald, D. E. 1979. Atmosphere-surface interactions in the unsteady, stable planetary boundary layer. Presented at Symposium on Antarctic Meteorology, (17th General Assembly of International Union of Geodesy and Geophysics, Canberra, Australia).
later be found in firn strata, we are now analyzing the 20-year Pole Station record to determine the frequency of such transport. Aerosol observations indicate that surface aerosol concentrations in the South Pacific are similar to those measured in the past over the North Pacific and the Icelandic low pressure area of the North Atlantic (Hogan 1976). Aerosol concentrations over the Ross Sea were comparable to those measured by Meszaros and Vissy (1974) over the Weddell Sea. Solar observations show the total atmosphere to be quite clear and low in aerosol concentration from 40° to 50°S but quite turbid in the vicinity of the Antarctic Convergence. The air of the polar easterlies over the Ross Sea was also quite low in total aerosol content, but not nearly as low as antarctic continental air measured over McMurdo and Vanda Stations. The Angstrom (1961) turbidity (total attenuation of sunlight by aerosol particles) measured at McMurdo and Vanda Stations showed no change from similar measurements made near there by Fischer in 1967 and at Mandheim in 1949 (Liljequist 1956). This research was supported by National Science Foundation grants DPP 76-23110 and DPP 76-23115 and by National Oceanic and Atmospheric Administration grant 047 022 44025. The authors offer special thanks to Captain Garrett and the officers and men of Northwind for their enthusiastic support, and to the New Zealand Antarctic Research Program, Gary Lewis, and Brian Leech for their assistance at Vanda Station.
References
Angstrom, A. Techniques of determining the turbidity of the atmosphere. Tellus, 13, 214-223. Fischer, W. H. 1967. Some atmospheric turbidity measurements in Antarctica. Journal of Applied Meteorology, 6, 958-959. Hogan, A. 1976. Physical properties of the atmospheric aerosol (Final report NSF grant GA 32502, ASRC Report 408). Liljequist, G. H. 1956. Energy exchange of an antarctic snowfield. In
Norwegian British Swedish Antaittic Expedition 1949-52, Scientific Results (Vol. 2, Part 1). Oslo: Norsk Polarinstitutt. Meszaros, A. and Vissy, K. 1974. Concentrations, size distribution
and chemical nature of atmospheric aerosol particles in remote oceanic areas. Aerosol Sciences, 5, 101-109. ANTARCTIC JOURNAL
I NORTHWINO CRUISE WINO (TIME)
6 12 18
- I I I
TEMPERATURE AIR SEA C C 0 10 0 10
AEROSOL SUN CN V/M Afl NIP 102CM3 10-6 CM 3 LY/MIN 0 100 100 10 1
50
lN
— 6O
'J)L. 4'
-
F p—. 70
L
I I
=-
11111111
III III II III
Aerosol concentrations, solar intensity, atmospheric turbidity, and meteorological conditions encountered along the cruise route of uscoc Northwlnd from Wellington, New Zealand, to Campbell Island to McMurdo Sound, 19 December 1979-6 January 1980.
Balloon-borne measurements of trace gases and aerosols over the South Pole D. J. HOFMANN, J. M. Ros, A. F. Fui, J. W. HARD ER , N. T. Kio, and C. L. OlsoN Department of Physics and Astronomy University of Wyoming Laramie, Wyoming 82077
D. L. ALBRrrrON, A. L. SCHMELTEKOPF and P. D. GOLDAN Aeronomy Laboratory National Oceanic and Atmospheric Administration Boulder, Colorado 80303
In January 1980, nine balloon soundings were conducted from South Pole Station. This campaign marked the ninth and final summer of stratospheric research in Antarctica by 1980 REVIEW
the Department of Physics and Astronomy at the University of Wyoming. Measurements conducted included two sets of five trace gas samples to a height of 31 kilometers, aerosol particles (radius ^!t0.15 micrometers) and condensation nuclei (radius 2:0.01 micrometers) to 28 kilometers, and five short soundings of condensation nuclei to about 4 kilometers to study the surface condensation nuclei features. As in the past, the air samples were analyzed by the National Oceanic and Atmospheric Administration (No) Aeronomy Laboratory in Boulder, Colorado; the results for the two soundings are shown in figure 1. For the first time large plastic balloons were employed at South Pole. This allowed samples to be obtained above 30 kilometers. Samples of methyl chloroform (CH3CC13) were obtained in addition to nitrous oxide (N 20), and the fluorocarbons F-12 (CF2 0 2), and F-il (CFC1 3). This marks the fourth measurement of the latter three gases, each a year apart. While stratospheric levels do not show a consistent time dependence, probably because of transport effects, which require averaging over a much larger data set, the upper tropospheric (6 to 7 kilometers) samples apparently do. Figure 2 shows the time history of these gases at this level. 183
