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Global Climate Change Digest
A Guide to Information on Greenhouse Gases and Ozone Depletion
Published July 1988 through June 1999
FROM VOLUME 1, NUMBER 4, OCTOBER 1988
PROFESSIONAL PUBLICATIONS...
ATMOSPHERIC CHEMISTRY
Item #d88oct62
 "Contribution of Cl- and F-bearing Gases to the Atmosphere by
Volcanoes," R.B. Symonds (Dept. Geolog. Eng., Michigan Tech. Univ.,
Houghton MN 49931), Nature, 334(6181), 415-418, Aug. 4, 1988.
Uses equilibrium thermodynamics to predict the speciation of Cl and F in
volcanic gases and provide new estimates of the global emission rates to the
atmosphere. Calculations show that HCl and HF are the dominant species of Cl and
F in volcanic gases, at least several orders of magnitude more abundant than all
other species. Although large explosive eruptions are infrequent, they may
inject significant amounts of HCl and HF into the stratosphere.
Item #d88oct63
"Phosgene Measurements in the Upper Troposphere and Lower
Stratosphere," S.R. Wilson (Max-Planck Inst. Chemistry, POB 3060, D-6500
Mainz, FRG), P.J. Crutzen et al., Nature, 334(6184), 689-691,
Aug. 25, 1988.
Phosgene is one possible product from the oxidation of natural and
industrial chlorinated hydrocarbons which can further oxidize to form ClOx,
which destroys ozone. Measurements of phosgene show a mixing ratio of 17 pptv in
the upper troposphere and an average of 22 pptv in the lower stratosphere. These
values are substantially greater than those estimated with a model that only
considers the photochemical breakdown of CCl4, indicating the possible
significance of more reactive chlorocarbon compounds, especially CHCl3, CH3CCl3,
C2HCl3 and C2Cl4 and their oxidation products in supplying chlorine to
the lower stratosphere.
Item #d88oct64
"Chlorine, Bromine and Iodine in Arctic Aerosols," W.T. Sturges
(Inst. Aerosol Sci., Univ. Essex, Wivenhoe Park, Colchester, Essex C04 3SQ, UK),
L.A. Barrie, Atmos. Environ., 22(6), 1179-1194, 1988.
Suspended particulate samples were collected weekly at three stations in the
Canadian Arctic between 1979 and 1984. Br concentrations peaked every year just
after the arctic dawn two orders of magnitude greater than could be explained by
marine, automotive, and crustal sources. Chlorine concentrations appeared to be
of marine origin. Iodine was found to be enriched relative to seawater by a
factor of 1000-10,000.
Item #d88oct65
"Radical Variability Determined from LIMS and SAMS Satellite Data,"
J.A. Pyle (Dept. Phys. Chem., Univ. Cambridge, Lensfield Rd., Cambridge CB2 1EP,
UK), A.M. Zavody, J. Atmos. Chem., 6, 201-220, Apr. 1988.
Global coverage by satellites of stratospheric trace constituents over long
time periods allows derivation of monthly zonal mean profiles. This has been
done for H, OH, HO2, H2O2, Cl, ClO, HCl, HOCl, ClONO2, NO and O. The standard
deviation of these quantities is a measure of their variability. Claims that
comparing theoretical variability estimates with measurements is a better test
of a photochemical theory than simply the comparison of single modeled and
observed profiles.
Item #d88oct66
"Responses of the Tropospheric Ozone and Odd Hydrogen Radicals to
Column Ozone Change," S.C. Liu (Aeronomy Lab., ERL/NOAA, 325 Broadway,
Boulder CO 80303), M. Trainer, ibid., 221-233.
The response of tropospheric ozone to a change in solar UV penetration due
to perturbation of column ozone depends critically on the tropospheric NOx (NO +
NO2) concentration. At high NOx or a polluted area where there is a net ozone
production, a decrease in column ozone will increase the solar UV penetration to
the troposphere and thus increase the tropospheric ozone concentration. The
opposite would occur at remote oceanic areas where NOx is low. This may have
important implications for the interpretation of the long-term trend of
tropospheric ozone. Model calculations show that the change in OH, HO2 and H2O2
concentrations are independent of the NOx concentration.
Item #d88oct67
"Tropospheric Ozone and Oxides of Nitrogen over the North-Western
Pacific in Summer," Y. Kondo (Res. Inst. Atmos., Nagoya Univ., Toyokawa,
Japan), ibid., 235-250.
In summer, atmospheric ozone was measured from an aircraft platform
simultaneously with nitric oxide (NO), oxides of nitrogen (NOy), and water vapor
over the Pacific Ocean in east Asia from 34° N to 19° N along the
longitude of 138 + or - 3° E. A good correlation in the smoothed meridional
distributions between ozone and NOy was seen. In particular, north of 25° N,
ozone and NOy mixing ratios were considerably higher than those observed in
tropical marine air south of 25° N.
Item #d88oct68
"Spectroscopic Evidence for the Presence of the gamma 4-Q
Branch of Chlorine Nitrate (ClONO2) in Ground-Based Infrared Solar Spectra,"
R. Zander (Inst. Astrophys., Univ. Liège, B-4200 Liège-Ougrée,
Belgium), Ph. Demoulin, ibid., 191-200.
Analysis of measurements leads to good agreement with recently published
results from the ATMOS/SL3 mission at 30° N latitude. The present research
represents an important step towards assessing the possibility of monitoring the
telluric ClONO2 column density from high mountain based stations.
Item #d88oct69
"Chemistry of Organic Traces in Air," Th. Class (Dept.
Analytical Chem., Univ. Ulm, D-7900 Ulm, FRG), K. Ballschmiter, ibid.,
35-46.
The occurrence of bromo- and bromochloromethanes in marine air and seawater
of the Atlantic Ocean were measured and evaluated. A correlation exists between
high concentrations of these compounds in air and in water and the presence of
algae at the coastlines of various islands and high bioactivity in the Atlantic
Ocean near the West African coast.
Item #d88oct70
"Emission of Nitrous Oxide from Temperate Forest Soils into the
Atmosphere," J. Schmidt (Max-Planck-Inst. Chem., Saarstr. 23, D-6500 Mainz,
FRG), W. Seiler, R. Conrad, ibid., 95-115.
N2O emission rates were measured during a 13-month period from July 1981 to
August 1982 at six different forest sites in Germany. The N2O emission rates
followed a general seasonal trend, with relatively high values during spring and
fall. There was a brief episode of relatively high N2O emission rates
immediately after thawing of the winter snow.
Item #d88oct71
"Influence of the Surface Microlayer on the Flux of Nonconservative
Trace Gases (CO, H2, CH4, N2O) Across the Ocean-Atmosphere Interface," R.
Conrad (Univ. Konstanz, POB 5560, D-7750 Konstanz 1, FRG), W. Seiler, ibid.,
83-94.
When the water was supersaturated with respect to atmospheric CO, H2, CH4,
and N2O, the transfer velocities of the emission process were smaller than those
determined for the deposition process. The results are interpreted by
destruction processes active within the surface microlayer.
Item #d88oct72
"Ozone Over McMurdo Station, Austral Spring 1986: Altitude Profiles
for the Middle and Upper Stratosphere," B.J. Connor (Sci. & Tech.
Corp., Hampton, Virginia), J.W. Barrett et al., J.Geophys. Res., 92(D11),
13,211-13,230, Nov. 20, 1987.
The ozone profile was measured between 25 and 55 km by ground-based
millimeter-wave spectrometry from September 12 to October 29. Mixing ratio at 25
km decreased by 15% during the period, with no decrease observed at higher
altitudes, but considerable variability was found at all altitudes. The
observation that ozone depletion was confined to the lower stratosphere is
consistent with theories using heterogenous chemistry associated with polar
stratospheric clouds. This data did not support theories predicting depletion in
the upper stratosphere.
Item #d88oct73
"Heavy Ozone Distribution in the Stratosphere From Far-Infrared
Observations," M.M. Abbas (Space Sci. Lab., NASA, Huntsville, Alabama), J.
Guo et al., ibid., 13,231-13,239.
Balloon-borne high resolution thermal emission spectral data indicate the
ratio of total heavy isotopic ozone 50O3 to normal 48O3 shows enhancements of
about 45% at 37 km, decreasing to a minimum of about 13% at about 29 km, and
increasing to about 18% at 25 km. There is no accepted explanation for an
enhancement of stratospheric heavy ozone at this time.
Item #d88oct74
"Infrared Measurements of Several Nitrogen Species Above the South
Pole in December 1980 and November-December 1986," F.J. Murcray (Phys.
Dept., Univ. Denver, Denver, Colorado), F.H. Murcray et al., ibid.,
13,373-13,376.
Total vertical column amounts of HNO3 were measured in 1980 and 1986; while
NO and NO2 were also measured in 1986. The latter measurement defines for the
first time the ambient levels of these N species immediately following the
breakup of the polar vortex.
Item #d88oct75
"The Gas-Phase Reaction of ClONO2 with Hydrogen Chloride," R.
Atkinson (Statewide Air Pollut. Res. Ctr., Univ. Calif., Riverside CA 92521), S.
Aschmann et al., J. Atmos. Chem., 5, 83-90, 1987.
Laboratory experiments indicate this homogenous gas-phase reaction can be
estimated to be of negligible importance as a ClONO2 loss process in the
stratosphere.
Item #d88oct76
"Atmospheric Trace Gas Analysis Using Matrix Isolation-Fourier
Transform Infrared Spectroscopy," D.W.T. Griffith (Dept. Chem., Univ.
Wollongong, POB 1144, Wollongong, NSW 2500, Australia), G. Schuster, ibid.,
59-81.
The method is described along with some measurements of N2O and CFCl3 from
samples collected at ground level and by aircraft at 9-14 km.
Item #d88oct77
"Feasibility of Observations of Stratospheric Trace Gases Using the
Hubble Space Telescope," M. Jaramillo (Dept. Phys., State Univ. of N.Y.,
Stony Brook NY 11794), R.L. De Zafra, ibid., 23-26.
Concludes that stratospheric observations with HST are not practical
primarily due to high opacity of stratospheric ozone over most of the bandpass.
Item #d88oct78
"Measurements of Solar Occultation: the Error in a Naive Retrieval
if the Constituent's Concentration Changes," H.K. Roscoe (Dept. Atmos.
Phys., Clarendon Lab., Parks Rd., Oxford 0X1 3P0, UK), J.A. Pyle, ibid.,
323-341.
Uses a model to calculate the error for NO, NO2, OH and ClO measured near
sunrise or sunset when concentrations are changing rapidly.
Item #d88oct79
"Nitrous Oxide Emission from Native and Reestablished Prairies in
Southern Wisconsin," R.L. Cates Jr., D.R. Keeney (Dept. Soil Sci., Univ.
Wisconsin, Madison WI 53706), Amer. Midland Naturalist, 117(1),
35-42, Jan. 1987.
Presettlement vegetation in southern Wisconsin included areas of oak savanna
that supported an understory of prairie vegetation, as well as open prairie.
Estimates of N2O production by such systems could provide a base level to which
relative contributions from managed lands might be compared. Emissions were
monitored by a static chamber at three dissimilar sites. Emissions were similar
among the sites and very low, were not affected by wet periods, and were highest
with high soil temperatures and at spring thaw. Emissions were more than an
order of magnitude lower than reported from N-fertilized fields and generally
lower than from replanted forests.
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