Stratospheric H2O

Ellsaesser, Hugh W.; Harries, J. E.; Kley, D.; Penndorf, R.

doi:10.1016/0032-0633(80)90081-1

Cited by 40 publications

(11 citation statements)

References 24 publications

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“…For example, Brewer first proposed that troposphere-to-stratosphere transport is limited to the tropics where tropopause temperatures are cold enough to "freeze-dry" tropospheric air as it enters the stratosphere [Brewer 1949]. In general agreement with this idea, the seasonal variation in water vapor mixing ratios in the lower stratosphere, inferred from balloon, satellite, and aircraft measurements [e.g., Mastenbrook 1968;Ellsaesser et al 1980;Remsberg et al 1984;McCormick et al 1993;Hintsa et al 1994], follows the seasonal trend in minimum tropical tropopause temperatures [e.g., Reed and Vlcek 1969; Newell and Gould-Stewart 1981]. Zonally-averaged monthly mean tropical tropopause temperatures, however, are too warm to produce the low H20 mixing ratios observed in the stratosphere [e.g., Ellsaesser 1974; Danielsen 1982; Newell and Gould-Stewart 1981], and the mechanism for transport across the tropopause remains unclear.…”

Section: Introductionmentioning

confidence: 94%

Measurements of stratospheric carbon dioxide and water vapor at northern midlatitudes: Implications for troposphere‐to‐stratosphere transport

Boering

Hintsa

Wofsy

et al. 1995

Geophysical Research Letters

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Simultaneous in situ measurements of CO2 and water vapor in the lower stratosphere were obtained in November 1992 and May 1993 up to 21 km at midlatitudes. Seasonal changes in both species were observed up to pressure‐altitudes of 19 km (∼440 K), a result of vertical propagation of seasonal oscillations in CO2 and H2O mixing ratios for air entering the stratosphere in the tropics followed by horizontal transport to midlatitudes. The inferred phase difference between their seasonal cycles at the tropical tropopause (2 months) remained coherent at midlatitudes, although the amplitudes were reduced, implying a mean transport time of 4–6 months from the tropical tropopause (∼16 km) to ∼18.5–19 km at midlatitudes in both November and May. The measurements indicate that air enters the stratosphere throughout the year and suggest that vertical propagation of the seasonal minimum in water vapor, rather than deep convective overshoot, is both sufficient and necessary to explain the minimum in water (“hygropause”) observed several kilometers above the tropopause.

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Section: Introductionmentioning

confidence: 94%

Measurements of stratospheric carbon dioxide and water vapor at northern midlatitudes: Implications for troposphere‐to‐stratosphere transport

Boering

Hintsa

Wofsy

et al. 1995

Geophysical Research Letters

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“…Ellsaesser, et al (1980) reviewed the status of stratospheric water vapor measurements including data obtained up until 1979.…”

Section: Bicmentioning

confidence: 99%

Intercomparison of stratospheric water vapor profiles obtained during the Balloon Intercomparison Campaign

et al. 1990

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The Balloon Intercomparison Campaign (BIC) was set up to intercompare remote sensing measurements of a number of compounds other than water vapor; however, water vapor has strong absorption features throughout the infrared and mm wave regions of the spectrum. Therefore many of the investigators involved in BIC have absorption or emission features due to water vapor in the data they obtained during the balloon flights made under the campaign.These features have been used by the investigators to determine the stratospheric water vapor profiles which are compared in this paper. The profiles allow comparison of a wide range of remote sensing techniques involving both emission and absorption in the mid-infrared and emission techniques in the far infrared.

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“…According to current theoretical understanding, air entering the stratosphere through the tropical tropopause in the upward portion of the Hadley cell circulation is freeze dried by the very low temperatures (•190øK) that exist in this region. This is believed to account for the extremely low stratospheric mixing ratios (<5 ppmv) for H20 [Ellsaesser et al, 1980]. Water vapor is produced chemically in the stratosphere as an end product of the methane oxidation sequence.…”

Section: H•omentioning

confidence: 99%

A two‐dimensional model of stratospheric chemistry and transport

Miller¹,

Filkin²,

Owens³

et al. 1981

J. Geophys. Res.

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A two‐dimensional chemical model of the atmosphere is described. The model includes the major features associated with advanced one‐dimensional models: 30 active chemical species and all the important chemical reactions connecting them, diurnal effects, and Rayleigh scattering. The species are transported and calculated separately, with the exception of the odd oxygen family [O3, O(3P), O(1D)] and H and N atoms. The transport scheme contains both diffusive and advective terms, with the advective circulation field of Murgatroyd and Singleton (appropriately scaled) used to approximate the Lagrangian mean flow. Comparison of the model predictions with atmospheric observations of long‐lived trace species such as O3, N2O, CF2Cl2, CFCl3, and CH4 suggests that the transport parameterization gives a good representation of actual trace species motions. For constituents which are more active or whose chemistry is less well known, the model is a useful diagnostic tool for assessing our current understanding of atmospheric chemistry. A number of significant discrepancies between experiment and theory are highlighted, the most important being in the Clx and NOy families.

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Stratospheric H2O

Cited by 40 publications

References 24 publications

Measurements of stratospheric carbon dioxide and water vapor at northern midlatitudes: Implications for troposphere‐to‐stratosphere transport

Measurements of stratospheric carbon dioxide and water vapor at northern midlatitudes: Implications for troposphere‐to‐stratosphere transport

Intercomparison of stratospheric water vapor profiles obtained during the Balloon Intercomparison Campaign

A two‐dimensional model of stratospheric chemistry and transport

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