A coupled one‐dimensional radiative‐convective, chemistry‐transport model of the atmosphere: 1. Model structure and steady state perturbation calculations

Owens, A. J.; Hales, Charles H.; Filkin, D. L.; Miller, C.; Steed, J. M.; Jesson, J. P.

doi:10.1029/jd090id01p02283

Cited by 47 publications

(24 citation statements)

References 42 publications

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“…The net effect from these calculations has been that methane by itself causes a net increase in ozone. For a doubling of the methane concentration (early papers went from 1.6 to 3.2 ppmv, while recent analyses assume a globally-averaged change from 1.7 to 3.4 ppmv), published effects on the calculated change in total ozone range from +0.3 % (Prather, in WMO, 1985) to +4.3 % (Owens et al, 1985). With radiative feedback effects included (allowing temperature changes in the stratosphere), the published model results tend to be in the upper end of this range (Owens et al, 1985;WMO, 1985;Isaksen and Stordal, 1986).…”

Section: Model Calculated Effects On Ozonementioning

confidence: 99%

“…Numerical models of atmospheric chemical and physical processes generally calculate that increasing methane concentrations result in a net ozone production in the troposphere and lower stratosphere and net ozone destruction in the upper stratosphere (Owens et al, 1982(Owens et al, , 1985WMO, 1985WMO, , 1991WMO, , 1995Isaksen and Stordal, 1986). The net effect from these calculations has been that methane by itself causes a net increase in ozone.…”

Section: Model Calculated Effects On Ozonementioning

confidence: 99%

“…For a doubling of methane concentration from 1.6 to 3.2 ppmv, effects on surface temperature range from 0.2 K to 0.3 K (Wang et al, 1976;Donner and Ramanathan, 1980;Lacis et al, 1981;Owens et al, 1985;Ramanathan et al, 1987;MacKay and Khalil, 1991), with the differences in model results primarily relating to uncertainties in the band strengths for methane infrared absorption. For a doubling from 1.7 to 3.4 ppmv, Owens et al (1985) calculate a direct 0.34 K increase in surface temperature, along with an additional 0.26 K due to indirect effects from methane-induced effects on carbon dioxide and ozone. For a 25 % increase in methane concentrations, Ramanathan et al (1985) determine a 0.08 K increase in surface temperature when overlap with the radiative absorption with other greenhouse gases is included, and a 0.19 K increase in surface temperature without overlap.…”

Section: Direct Effectsmentioning

confidence: 99%

See 2 more Smart Citations

Atmospheric Methane: Trends and Impacts

Wuebbles

Hayhoe

2000

Non-Co2 Greenhouse Gases: Scientific Understanding, Control and Implementation

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Abstract:The concentration of methane (CH 4 ), the most abundant organic trace gas in the atmosphere, has increased dramatically over the last few centuries, more than doubling its concentration. The increasing concentrations of methane are of special concern because of its effects on climate and atmospheric chemistry. On a per molecule basis, additional methane is much more effective as a greenhouse gas than additional CO 2 . Methane is also important to both tropospheric and stratospheric chemistry. Here, we examine past trends in the concentration of methane, the sources and sinks affecting its growth rate, and the factors that could affect its growth rate in the future. This study also examines the current understanding of the effects of methane on atmospheric chemistry and climate.

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Section: Model Calculated Effects On Ozonementioning

confidence: 99%

Section: Model Calculated Effects On Ozonementioning

confidence: 99%

Section: Direct Effectsmentioning

confidence: 99%

See 1 more Smart Citation

Atmospheric Methane: Trends and Impacts

Wuebbles

Hayhoe

2000

Non-Co2 Greenhouse Gases: Scientific Understanding, Control and Implementation

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“…A radiative-convective adjustment process was taken into account in the troposphere. Water vapor mixing ratios in the troposphere below 17.5 km was calculated from a fixed vertical distribution of relative humidity presented in Table 5 of Owens et al (1985), while in the stratosphere above 17.5 km water vapor was predicted chemically and dynamically with the vertical diffusion. At 17.5 km, the water vapor mixing ratio was fixed to 3.5 ppmv.…”

Section: Model Descriptionmentioning

confidence: 99%

Chemistry and Temperature Perturbations Due to Pinatubo Aerosols Calculated by a Chemical-radiative Coupled 1-D Model.

Akiyoshi

2002

Journal of the Meteorological Society of Japan

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The increase of stratospheric aerosol caused by the Mt. Pinatubo eruption, and its effects on atmospheric temperature and chemical constituents, are studied by using a chemical-radiative coupled 1-D model. The optical parameters of the aerosols and the surface area are calculated, assuming the size distribution of the aerosols and the composition. Two kinds of numerical experiments were made in this study. In the first experiment, a simple form of vertical distribution and the time variation of the aerosols are assumed based on lidar measurement data, and satellite data analyses. The simplification is necessary for an easy and clear understanding of chemistry-radiation coupled variations in temperature and ozone. In the second experiment, lidar data are used for calculation and input into the model as a function of altitude and time. These experiments show that the temperature increased in the range of 4.7-5.8 K and the ozone concentration decreased by 13-14% at the maximum perturbation phase in the center of the aerosol layer at 20 km. The maximum total ozone decrease was 18-20 DU (5.0-5.5%). The total ozone decrease, however, was 13-15 DU (3.5-4.0%) when the effect of the temperature variation on chemistry was ignored. Sedimentation of the aerosols within the first 1-2 years after the Pinatubo eruption explains the small difference in the results of these two experiments. The experiments also show that the ground surface temperature rapidly dropped by 0.1 K-0.35 K in the first 6 months, depending on the solar radiation absorption efficiency of the aerosols, followed by a recovery of more than a half in magnitude in the next 6 months. A cooling of less than 0.1 K then continued for the next 3-4 years, until the stratospheric ozone loss disappeared. The mechanisms of this surface temperature variation in the 1-D model are studied examining the results of the first experiment. The effects of a hydrolysis reaction of BrONO 2 on ozone loss are also examined. The results suggest that the hydrolysis reaction more than doubled the ozone loss. All these results from the 1-D model show substantially larger positive temperature perturbations, and a somewhat longer duration of chemical perturbations than observed.

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“…The response of the atmosphere to the emissions of trace gases has been extensively studied in recent years (see e.g., Wang et al, 1976;Wang and Molnar, 1985;Ramanathan, 1976;Ramanathan et al, 1985;Donner and Ramanathan, 1980;Lacis et al, 1981;Wuebbles, 1983;Callis et al, 1983;Wuebbles et al, 1983;Brasseur, 1984;Brasseur et al, 1985;de Rudder and Brasseur, 1985;Bruehl and Crutzen, 1984;Owens et al, 1985;Solomon et al, 1985;Isaksen and Stordal, 1986;Dickinson and Cicerone, 1986;Connell and Wuebbles, 1986;Tricot and Berger, 1986;and others). Some of these papers have either studied the chemical sensitivity of ozone to changes in the amount of injected "source gases" (parameterizing crudely the radiative feedbacks and, in certain cases, ignoring the climatic impact at the earth's surface) or considered the pure radiative and climatic response of the injection in the atmosphere of "greenhouse gases" (neglecting chemical feedbacks).…”

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confidence: 99%

The potential impact on atmospheric ozone and temperature of increasing trace gas concentrations

Brasseur

Rudder

1987

J. Geophys. Res.

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The response of the atmosphere to emissions of chlorofluorocarbons (CFCs) and other chlorocarbons and to increasing concentrations of other radiatively active trace gases such as CO2, CH4, and N2O is calculated by means of a coupled chemical‐radiative‐transport one‐dimensional model. It is shown that significant reductions in the ozone concentration and in the temperature should be expected in the upper stratosphere as a result essentially of increasing concentrations of active chlorine produced by photo decomposition of the CFCs. For a constant emission of chlorofluorocarbons‐11 and ‐12 at approximately the 1980 level (309 kT/yr for F‐11 and 433 kT/yr for F‐12) the calculated decrease (assuming no other changes) in the ozone concentration relative to the preindustrial atmosphere is approximately 60–70% at 40 km, and the reduction in the ozone column is 8.7% when temperature feedback is included in the model and 5.5% when it is omitted. The model also shows that a doubling of CO2 leads to a 1.8% increase in the ozone column abundance and a 2 K increase in the surface temperature. At 40 km the ozone density is enhanced by 15% and the temperature reduced by 8 K. A doubling of methane produces a 2.4% increase in the ozone column. A 20% enhancement in the nitrous oxide content leads to an ozone depletion of 1.4%. Time‐dependent calculations of ozone and temperature show that if the production of F‐11 and F‐12 increases by 3%/yr until it reaches a capacity cap equal to 1.5 times the 1985 world production level, the maximum ozone depletion should be of the order of 4–5%, assuming a growth in the concentration of CO2, CH4, and N2O of about 0.5, 1.0, and 0.25%/yr, respectively. For this scenario the maximum ozone depletion is found to occur in year 2070. The slight increase appearing after 2070 is directly dependent on the future growth in the methane concentration. If the production of F–11 and F–12 increases continuously by 3%/yr, without capacity cap, and if the changes in the concentration of other trace gases are ignored, the ozone column abundance is predicted to be reduced by more than 10% after year 2050. The model shows an almost linear relation between the ozone depletion and the chlorine content as long as the mixing ratio of active chlorine remains smaller than that of active nitrogen. The O3/Clx sensitivity, however, is a strong function of NOy content. For amounts of chlorine comparable or larger than those of active nitrogen the ozone depletion increases rapidly with the amount of chlorine present in the atmosphere.

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A coupled one‐dimensional radiative‐convective, chemistry‐transport model of the atmosphere: 1. Model structure and steady state perturbation calculations

Cited by 47 publications

References 42 publications

Atmospheric Methane: Trends and Impacts

Atmospheric Methane: Trends and Impacts

Chemistry and Temperature Perturbations Due to Pinatubo Aerosols Calculated by a Chemical-radiative Coupled 1-D Model.

The potential impact on atmospheric ozone and temperature of increasing trace gas concentrations

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