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Greenhouse gases are components of the atmosphere that contribute to the Greenhouse effect. Some greenhouse gases occur naturally in the atmosphere, while others result from human activities. Naturally occurring greenhouse gases include water vapor, carbon dioxide, methane, nitrous oxide, and ozone. Certain human activities add to the levels of most of these naturally occurring gases.
The "Greenhouse effect"
When sunlight reaches the surface of earth, some of it is absorbed and warms the earth. Because the Earth's surface is much cooler than the sun, it radiates energy at much longer wavelengths than the sun (see black body radiation and Wien's displacement law). Some energy in these longer wavelengths is absorbed by greenhouse gases in the atmosphere before it can be lost to space. The absorption of this longwave radiant energy warms the atmosphere (the atmosphere also is warmed by transfer of sensible and latent heat from the surface). Greenhouse gases also emit longwave radiation both upward to space and downward to the surface. The downward part of this longwave radiation emitted by the atmosphere is the "greenhouse effect." The term is in fact a misnomer, as this process is not the primary mechanism that warms greenhouses.
The major natural greenhouse gases are water vapour, which causes about 36-70% of the greenhouse effect on Earth (not including clouds); carbon dioxide, which causes 9-26%; methane, which causes 4-9%, and ozone, which causes 3-7%. It is not possible to state that a certain gas causes a certain percentage of the greenhouse effect, because the influences of the various gases are not additive. (The higher ends of the ranges quoted are for the gas alone; the lower ends, for the gas counting overlaps.) Other greenhouse gases include, but are not limited to, nitrous oxide, sulfur hexafluoride, hydrofluorocarbons, perfluorocarbons and chlorofluorocarbons (see IPCC list of greenhouse gases).
The major atmospheric constituents (nitrogen, Nâ‚‚ and oxygen, Oâ‚‚) are not greenhouse gases. This is because homonuclear diatomic molecules such as Nâ‚‚ and Oâ‚‚ neither absorb nor emit infrared radiation, as there is no net change in the dipole moment of these molecules when they vibrate. Molecular vibrations occur at energies that are of the same magnitude as the energy of the photons on infrared light.
It is worth noting that late 19th century scientists experimentally discovered that Nâ‚‚ and Oâ‚‚ did not absorb infrared radiation (called, at that time, "dark radiation") and that COâ‚‚ and many other gases did absorb such radiation. It was recognized in the early 20th century that the known major greenhouse gases in the atmosphere did cause the Earth's temperature to be higher than it would have been without the greenhouse gases.
Anthropogenic greenhouse gases
The concentrations of several greenhouse gases have increased over time. Human activity increases the greenhouse effect primarily through release of carbon dioxide, but human influences on other greenhouse gases can also be important. Some of the main sources of greenhouse gases due to human activity include:
- burning of fossil fuels and deforestation leading to higher carbon dioxide concentrations;
- livestock and paddy rice farming, land use and wetland changes, pipeline losses, and covered vented landfill emissions leading to higher methane atmospheric concentrations. Many of the newer style fully vented septic systems that enhance and target the fermentation process also are major sources of atmospheric methane;
- use of chlorofluorocarbons (CFCs) in refrigeration systems, and use of CFCs and halons in fire suppression systems and manufacturing processes.
- agricultural activities, including the use of fertilizers, that lead to higher nitrous oxide concentrations.
Carbon dioxide, methane, nitrous oxide and three groups of fluorinated gasses (sulfur hexafluoride, HFCs, and PFCs) are the major greenhouse gases and the subject of the Kyoto Protocol, which entered into force in 2005.
CFCs, although greenhouse gasses, are regulated by the Montreal Protocol, which was motivated by CFCs' contribution to ozone depletion rather than by their contribution to global warming. Note that ozone depletion has only a minor role in greenhouse warming though the two processes often are confused.
The role of water vapor
Water vapor is a naturally occurring greenhouse gas and accounts for the largest percentage of the greenhouse effect. Water vapor concentrations fluctuate regionally, but human activity does not directly affect water vapor concentrations except at very local scales.
In climate models an increase in atmospheric temperature caused by the greenhouse effect due to anthropogenic gases will in turn lead to an increase in the water vapor content of the troposphere, with approximately constant relative humidity. The increased water vapor in turn leads to an increase in the greenhouse effect and thus a further increase in temperature; the increase in temperature leads to still further increase in atmospheric water vapor; and the feedback cycle continues until equilibrium is reached. Thus water vapor acts as a positive feedback to the forcing provided by human-released greenhouse gases such as COâ‚‚ (but has never, so far, acted on Earth as part of a runaway feedback). Changes in water vapor may also have indirect effects via cloud formation.
Intergovernmental Panel on Climate Change (IPCC) IPCC Third Assessment Report chapter lead author Michael Mann considers citing "the role of water vapor as a greenhouse gas" to be "extremely misleading" as water vapor can not be controlled by humans. The IPCC report has discussed water vapor feedback in more detail.
Increase of greenhouse gases
Measurements from Antarctic ice cores show that just before industrial emissions began, atmospheric COâ‚‚ levels were about 280 parts per million by volume (ppm; the units ÂµL/L are occasionally used and are identical to parts per million by volume). From the same ice cores it appears that COâ‚‚ concentrations stayed between 260 and 280 ppm during the preceding 10,000 years. Studies using evidence from stomata of fossilized leaves suggest greater variability, with COâ‚‚ levels above 300 ppm during the period 7,000-10,000 years ago, though others have argued that these findings more likely reflect calibration/contamination problems rather than actual COâ‚‚ variability.
Since the beginning of the Industrial Revolution, the concentrations of many of the greenhouse gases have increased. The concentration of COâ‚‚ has increased by about 100 ppm (i.e., from 280 ppm to 380 ppm). The first 50 ppm increase took place in about 200 years, from the start of the Industrial Revolution to around 1973; the next 50 ppm increase took place in about 33 years, from 1973 to 2006. Template:PDFlink. Many observations are available on line in a variety of Atmospheric Chemistry Observational Databases. The greenhouse gases with the largest radiative forcing are:
|Gas||Current (1998) Amount by volume||Increase over pre-industrial (1750)||Percentage increase||Radiative forcing (W/m2)|
Amount by volume
|Radiative forcing |
Removal from the atmosphere and global warming potential
Aside from water vapor near the surface, which has a residence time of days, most greenhouse gases take a very long time to leave the atmosphere. Although it is not easy to know with precision how long, there are estimates of the duration of stay, i.e., the time which is necessary so that the gas disappears from the atmosphere, for the principal greenhouse gases. Greenhouse gases can be removed from the atmosphere by various processes:
- as a consequence of a physical change (condensation and precipitation remove water vapor from the atmosphere).
- as a consequence of chemical reactions within the atmosphere. This is the case for methane. It is oxidized by reaction with naturally occurring hydroxyl radical, OHÂ· and degraded to COâ‚‚ and water vapor at the end of a chain of reactions (the contribution of the COâ‚‚ from the oxidation of methane is not included in the methane GWP). This also includes solution and solid phase chemistry occurring in atmospheric aerosols.
- as a consequence of a physical interchange at the interface between the atmosphere and the other compartments of the planet. An example is the mixing of atmospheric gases into the oceans at the boundary layer.
- as a consequence of a chemical change at the interface between the atmosphere and the other compartments of the planet. This is the case for COâ‚‚, which is reduced by photosynthesis of plants, and which, after dissolving in the oceans, reacts to form carbonic acid and bicarbonate and carbonate ions (see ocean acidification).
- as a consequence of a photochemical change. Halocarbons are dissociated by UV light releasing ClÂ· and FÂ· as free radicals in the stratosphere with harmful effects on ozone (halocarbons are generally too stable to disappear by chemical reaction in the atmosphere).
- as a consequence of dissociative ionization caused by high energy cosmic rays or lightning discharges, which break molecular bonds. For example, lightning forms N atoms from Nâ‚‚ which then react with Oâ‚‚ to form NOâ‚‚.
Two scales can be used to describe the effect of different gases in the atmosphere. The first, the atmospheric lifetime, describes how long it takes to restore the system to equilibrium following a small increase in the concentration of the gas in the atmosphere. Individual molecules may interchange with other reservoirs such as soil, the oceans, and biological systems, but the mean lifetime refers to the decaying away of the excess. It is sometimes erroneously claimed that the atmospheric lifetime of COâ‚‚ is only a few years because that is the average time for any COâ‚‚ molecule to stay in the atmosphere before being removed by mixing into the ocean, uptake by photosynthesis, or other processes. This ignores the balancing fluxes of COâ‚‚ into the atmosphere from the other reservoirs. It is the net concentration changes of the various greenhouse gases by all sources and sinks that determines atmospheric lifetime, not just the removal processes.
The second scale is global warming potential (GWP). The GWP depends on both the efficiency of the molecule as a greenhouse gas and its atmospheric lifetime. GWP is measured relative to the same mass of COâ‚‚ and evaluated for a specific timescale. Thus, if a molecule has a high GWP on a short time scale (say 20 years) but has only a short lifetime, it will have a large GWP on a 20 year scale but a small one on a 100 year scale. Conversely, if a molecule has a longer atmospheric lifetime than COâ‚‚ its GWP will increase with time.
Examples of the atmospheric lifetime and GWP for several greenhouse gases include:
- COâ‚‚ has a variable atmospheric lifetime (approximately 200-450 years for small perturbations). Recent work indicates that recovery from a large input of atmospheric COâ‚‚ from burning fossil fuels will result in an effective lifetime of tens of thousands of years. Carbon dioxide is defined to have a GWP of 1 over all time periods.
- methane has an atmospheric lifetime of 12 Â± 3 years and a GWP of 62 over 20 years, 23 over 100 years and 7 over 500 years. The decrease in GWP associated with longer times is associated with the fact that the methane is degraded to water and COâ‚‚ by chemical reactions in the atmosphere.
- nitrous oxide has an atmospheric lifetime of 120 years and a GWP of 296 over 100 years.
- CFC-12 has an atmospheric lifetime of 100 years and a GWP(100) of 10600.
- HCFC-22 has an atmospheric lifetime of 12.1 years and a GWP(100) of 1700.
- tetrafluoromethane has an atmospheric lifetime of 50,000 years and a GWP(100) of 5700.
- sulfur hexafluoride has an atmospheric lifetime of 3,200 years and a GWP(100) of 22000.
Carbon monoxide has an indirect radiative effect by elevating concentrations of methane and tropospheric ozone through scavenging of atmospheric constituents (e.g., the hydroxyl radical, OH) that would otherwise destroy them. Carbon monoxide is created when carbon-containing fuels are burned incompletely. Through natural processes in the atmosphere, it is eventually oxidized to carbon dioxide. Carbon monoxide has an atmospheric lifetime of only a few months and as a consequence is spatially more variable than longer-lived gases.
Another potentially important indirect effect comes from methane, which in addition to its direct radiative impact also contributes to ozone formation. Shindell et al (2005) argue that the contribution to climate change from methane is at least double previous estimates as a result of this effect.
Carbon dioxide emissions
- International Energy Annual: Reserves
- International Energy Annual 2003: Carbon Dioxide Emissions
- International Energy Annual 2003: Notes and Sources for Table H.1co2 (Metric tons of carbon dioxide can be converted to metric tons of carbon equivalent by multiplying by 12/44)
- DOE - EIA - Alternatives to Traditional Transportation Fuels 1994 - Volume 2, Greenhouse Gas Emissions (includes "Greenhouse Gas Spectral Overlaps and Their Significance")
- NOAA Paleoclimatology Program - Vostok Ice Core
- NOAA CMDL CCGG - Interactive Atmospheric Data Visualization NOAA COâ‚‚ data
- Carbon Dioxide Information Analysis Centre FAQ Includes links to Carbon Dioxide statistics
Policy and advocacy
- Australian Greenhouse Gas Initiative
- Carbon Dioxide is Good for the Environment 2001 paper by The National Center for Public Policy Research
- Environmental Effects of Increased Atmospheric Carbon Dioxide paper by The Oregon Institute of Science and Medicine
- EU page about reducing COâ‚‚ emissions from light-duty vehicles : the EU's aim is to reach - by 2010 at the latest -an average COâ‚‚ emission figure of 120 g/km for all new passenger cars marketed in the Union.
|This article is based on a GNU FDL Ecology Wikia article: gas Greenhouse gas||Eco|
|List of global warming related subjects|
|greenhouse gas | greenhouse effect | environmentalism | ecology|
|Related topics: nature | Earth | eco-anarchism | Green anarchism|
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- Methane's Impacts on Climate Change May Be Twice Previous Estimates