Measurements of tropospheric and stratospheric H<sub>2</sub>CO by an infrared high resolution technique

Barbe, A.; Marché, P.; Secroun, C.; Jouve, Pierre

doi:10.1029/gl006i006p00463

Cited by 37 publications

(15 citation statements)

References 6 publications

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“…Even in this instance, formaldehyde production from ethane is negligible above about 20 km in comparison with methane production. Ethane mixing ratios of 2 ppb give results at 5 kin, which compare favorably with the measured profile of Barbe et al [1979]. The deviation between Barbe's data and the predicted formaldehyde distribution above 20 km can probably be attributed to experimental difficulties in retrieving high altitude data.…”

Section: Ch30 + O2 '--> Ch20 + Ho2supporting

confidence: 59%

Atmospheric chemistry of ethane and ethylene

Aikin¹,

Herman²,

Maier³

et al. 1982

J. Geophys. Res.

117

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A detailed study of ethane and ethylene photochemistry is presented for the troposphere and stratosphere. It is demonstrated that the loss of ethane is controlled by OH in the troposphere and Cl in the stratosphere. Observations of ethane show a stratospheric behavior indicative of a free chlorine concentration below 30 km that is only 10% of the predicted value given by both our photochemical model calculations and those done by others. The inferred lower amount of chlorine cannot be explained by heterogeneous processes for concentrations of aerosols representing average background conditions, nor does current stratospheric photochemistry show agreement. Chemical destruction of ethane and ethylene within the atmosphere leads to the production of carbon monoxide, formaldehyde, and other products. Tropospheric concentrations of formaldehyde are enhanced by nearly a factor of 3 for an ethylene mixing ratio of 2 ppb. Simultaneous monitoring of formaldehyde and carbon monoxide, as well as other products, will greatly aid in determining the relative importance of different tropospheric CO sources. Peroxyacetyl nitrate (PAN) acts as a reservoir for odd‐nitrogen at the expense of HNO3, HO2NO2, NO, and NO2.

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Section: Ch30 + O2 '--> Ch20 + Ho2supporting

confidence: 59%

Atmospheric chemistry of ethane and ethylene

Aikin¹,

Herman²,

Maier³

et al. 1982

J. Geophys. Res.

117

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“…During January and February they measured total columns between 2.6 and 9.9 x 10 •5 molecules cm -2. Barbe et al [1979] The effective layer thickness of C2H 6 is seen to be higher than that of C2H 2 and shows much less variation. This is consistent with the fact that of the two species, C2H 6 has the longer chemical lifetime and is therefore allowed to be transported to somewhat higher levels.…”

Section: Resultsmentioning

confidence: 87%

Seasonal variations of atmospheric trace gases in the high Arctic at 79°N

Notholt¹,

Toon²,

Stordal³

et al. 1997

J. Geophys. Res.

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Abstract. Since March 1992 the total column abundances of several tropospheric and stratospheric trace gases have been monitored year-round from the Network for Detection of Stratospheric Change station in Ny/•desund, Spitsbergen (78.9øN, 11.9øE). A groundbased Fourier transform infrared (FTIR) spectrometer performed these measurements using the Sun as a light source during the summer, and the Moon during the winter. In situ measurements of C2H2, C2H6, and CC12F2, made from the top of a nearby mountain, were combined with the FTIR column data to infer additional information about the variation of the volume mixing ratio profiles with altitude and season. The short-lived tropospheric trace gases C2H2, C2H6, and CO exhibit large seasonal variations with a summer minimum, caused by reaction with OH. CH20 shows a second maximum during the summer, caused by its formation by methane oxidation. For the long-lived gases HF, N20 , and CH 4 the seasonal cycle is less pronounced and is forced mainly by wintertime stratospheric diabatic descent, which starts in early November and reaches a maximum in March. The total columns of the stratospheric trace gases indicate that the chemical repartitioning of HC1 into C1ONO2 starts in November, before the widespread production of polar stratospheric clouds. The total columns of the sum of HC1 plus C1ONO2 suggests that between December and March they are converted into their active counterparts. Photolysis of HNO 3 gives rise to its summer minimum, and its winter maximum, with no evidence for a strong winter denitrification.

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“…Further important questions can be addressed by the study of molecules important for the spectroscopy of the Earth's atmosphere [16][17][18][19][20][21][22][23][24]. In the past, much high resolution spectroscopic work has concentrated on relatively simple atmospheric trace gases such as ozone [18], methane [20][21][22][23][24] or some of the simpler fluoro-chloro-hydrocarbons [25], to name just a few selected examples from a very large body of work usually based on FTIR spectroscopy with conventional light sources.…”

Section: Introductionmentioning

confidence: 99%