Physics:Trace gas
Trace gases are gases that are present in small amounts within an environment such as a planet's atmosphere. Trace gases in Earth's atmosphere are gases other than nitrogen (78.1%), oxygen (20.9%), and argon (0.934%) which, in combination, make up 99.934% of its atmosphere (not including water vapor).
Abundance, sources and sinks
The abundance of a trace gas can range from a few parts per trillion (ppt) by volume to several hundred parts per million by volume (ppmv).[1] When a trace gas is added into the atmosphere, that process is called a source. There are two possible types of sources - natural or anthropogenic. Natural sources are caused by processes that occur in nature. In contrast, anthropogenic sources are caused by human activity.
Some sources of a trace gas are biogenic processes, outgassing from solid Earth, ocean emissions, industrial emissions, and in situ formation.[1] A few examples of biogenic sources include photosynthesis, animal excrements, termites, rice paddies, and wetlands. Volcanoes are the main source for trace gases from solid earth. The global ocean is also a source of several trace gases, in particular sulfur-containing gases. In situ trace gas formation occurs through chemical reactions in the gas-phase.[1] Anthropogenic sources are caused by human related activities such as fossil fuel combustion (e.g. in transportation), fossil fuel mining, biomass burning, and industrial activity.
In contrast, a sink is when a trace gas is removed from the atmosphere. Some of the sinks of trace gases are chemical reactions in the atmosphere, mainly with the OH radical, gas-to-particle conversion forming aerosols, wet deposition and dry deposition.[1] Other sinks include microbiological activity in soils.
Below is a chart of several trace gases including their abundances, atmospheric lifetimes, sources, and sinks.
Trace gases – taken at pressure 1 atm[1]
| Gas | Chemical formula | Fraction of volume of air by the species | Residence time or lifetime | Major sources | Major sinks |
|---|---|---|---|---|---|
| Carbon dioxide | CO2 | 419 ppm ≈ppmv (May, 2021)[2] |
Increasing, See Note[A] |
Biological, oceanic, combustion, anthropogenic | photosynthesis |
| Neon | Ne | 18.18 ppmv | _________ | Volcanic | ________ |
| Helium | He | 5.24 ppmv | _________ | Radiogenic | ________ |
| Methane | CH4 | 1.89 ppm (May, 2021)[3] |
9 years | Biological, anthropogenic | OH |
| Hydrogen | H2 | 0.56 ppmv | ~ 2 years | Biological, HCHO photolysis | soil uptake |
| Nitrous oxide | N2O | 0.33 ppmv | 150 years | Biological, anthropogenic | O(1D) in stratosphere |
| Carbon monoxide | CO | 40 – 200 ppbv | ~ 60 days | Photochemical, combustion, anthropogenic | OH |
| Ozone | O3 | 10 – 200 ppbv (troposphere) | Days – months | Photochemical | photolysis |
| Formaldehyde | HCHO | 0.1 – 10 ppbv | ~ 1.5 hours | Photochemical | OH, photolysis |
| Nitrogen species | NOx | 10 pptv – 1 ppmv | Variable | Soils, anthropogenic, lightning | OH |
| Ammonia | NH3 | 10 pptv – 1 ppbv | 2 – 10 days | Biological | gas-to-particle conversion |
| Sulfur dioxide | SO2 | 10 pptv – 1 ppbv | Days | Photochemical, volcanic, anthropogenic | OH, water-based oxidation |
| Dimethyl sulfide | (CH3)2S | several pptv – several ppbv | Days | Biological, ocean | OH |
A The Intergovernmental Panel on Climate Change (IPCC) states that "no single atmospheric lifetime can be given" for CO2.[4]:731 This is mostly due to the high rate of growth and large cumulative magnitude of the disturbances to Earth's carbon cycle by the geologic extraction and burning of fossil carbon.[5] As of year 2014, fossil CO2 emitted as a theoretical 10 to 100 GtC pulse on top of the existing atmospheric concentration was expected to be 50% removed by land vegetation and ocean sinks in less than about a century.[6] A substantial fraction (20-35%) was also projected to remain in the atmosphere for centuries to millennia, where fractional persistence increases with pulse size.[7][8] Thus CO2 lifetime effectively increases as more fossil carbon is extracted by humans.
Mixing and lifetime
The overall abundance of man-made trace gases in Earth's atmosphere is growing. Most originate from industrial activity in the more populated northern hemisphere. Time-series data from measurement stations around the world indicate that it typically takes 1–2 years for their concentrations to become well-mixed throughout the troposphere.[9][10]
The residence time of a trace gas depends on the abundance and rate of removal. The Junge (empirical) relationship describes the relationship between concentration fluctuations and residence time of a gas in the atmosphere. It can expressed as fc = b/τr, where fc is the coefficient of variation, τr is the residence time in years, and b is an empirical constant, which Junge originally gave as 0.14 years.[11] As residence time increases, the concentration variability decreases. This implies that the most reactive gases have the most concentration variability because of their shorter lifetimes. In contrast, more inert gases are non-variable and have longer lifetimes. When measured far from their sources and sinks, the relationship can be used to estimate tropospheric residence times of gases.[11]
Trace greenhouse gases
A few examples of the major greenhouse gases are water, carbon dioxide, methane, nitrous oxide, ozone, and CFCs. These gases can absorb infrared radiation from the Earth's surface as it passes through the atmosphere.
The most influential greenhouse gas is water vapor. It frequently occurs in high concentrations, may transition to and from an aerosol (clouds), and is thus not generally classified as a trace gas. Regionally, water vapor can trap up to 80 percent of outgoing IR radiation.[12] Globally, water vapor is responsible for about half of Earth's total greenhouse effect.[13]
The second most important greenhouse gas, and the most important trace gas affected by man-made sources, is carbon dioxide.[12] It contributes about 20% of Earth's total greenhouse effect.[13] The reason that greenhouse gases can absorb infrared radiation is their molecular structure. For example, carbon dioxide has two basic modes of vibration that create a strong dipole moment, which causes its strong absorption of infrared radiation.[12]
In contrast, the most abundant gases (N2,O2, and Ar) in the atmosphere are not greenhouse gases. This is because they cannot absorb infrared radiation as they do not have vibrations with a dipole moment.[12] For instance, the triple bonds of atmospheric dinitrogen make for a symmetric molecule with vibrational energy states that are almost totally unaffected at infrared frequencies.
Below is a table of some of the major trace greenhouse gases, their man-made sources, and an estimate of the relative contribution of those sources to the enhanced greenhouse effect that influences global warming.
Key Greenhouse Gases and Sources[12]
| Gas | Chemical formula | Major human sources | Contribution to Increase (Year 1995 estimate) |
|---|---|---|---|
| Carbon dioxide | CO2 | fossil fuel combustion, deforestation | 55% |
| Methane | CH4 | rice fields, cattle and dairy cows, landfills, oil and gas production | 15% |
| Nitrous oxide | N2O | fertilizers, deforestation | 6% |
References
- ↑ 1.0 1.1 1.2 1.3 1.4 Wallace, John; Hobbs, Peter (2006). Atmospheric Science: An Introductory Survey. Amsterdam, Boston: Elsevier Academic Press. ISBN 9780127329512.
- ↑ "Trends in Atmospheric Carbon Dioxide". NOAA Earth System Research Laboratories. https://gml.noaa.gov/ccgg/trends/.
- ↑ "Trends in Atmospheric Methane". NOAA Earth System Research Laboratories. https://gml.noaa.gov/ccgg/trends_ch4/.
- ↑ "Chapter 8". AR5 Climate Change 2013: The Physical Science Basis. https://www.ipcc.ch/report/ar5/wg1/.
- ↑ Friedlingstein, P., Jones, M., O'Sullivan, M., Andrew, R., Hauck, J., Peters, G., Peters, W., Pongratz, J., Sitch, S., Le Quéré, C. and 66 others (2019) "Global carbon budget 2019". Earth System Science Data, 11(4): 1783–1838. doi:10.5194/essd-11-1783-2019
- ↑ "Figure 8.SM.4". Intergovernmental Panel on Climate Change Fifth Assessment Report - Supplemental Material. p. 8SM-16. https://www.ipcc.ch/site/assets/uploads/2018/07/WGI_AR5.Chap_.8_SM.pdf.
- ↑ Archer, David (2009). "Atmospheric lifetime of fossil fuel carbon dioxide". Annual Review of Earth and Planetary Sciences 37 (1): 117–34. doi:10.1146/annurev.earth.031208.100206. Bibcode: 2009AREPS..37..117A. https://orbi.uliege.be/handle/2268/12933.
- ↑ Joos, F. et al. (2013). "Carbon dioxide and climate impulse response functions for the computation of greenhouse gas metrics: A multi-model analysis". Atmospheric Chemistry and Physics 13 (5): 2793–2825. doi:10.5194/acpd-12-19799-2012. https://www.atmos-chem-phys.net/13/2793/2013/.
- ↑ "Long-term global trends of atmospheric trace gases". NOAA Earth System Research Laboratories. https://www.esrl.noaa.gov/gmd/hats/data.html.
- ↑ "AGAGE Data and Figures". Massachusetts Institute of Technology. https://agage.mit.edu/data/agage-data.
- ↑ 11.0 11.1 Slinn, W. G. N. (1988). "A Simple Model for Junge's Relationship between Concentration Fluctuations and Residence Times for Tropospheric Trace Gases". Tellus B: Chemical and Physical Meteorology 40 (3): 229–232. doi:10.3402/tellusb.v40i3.15909. Bibcode: 1988TellB..40..229S.
- ↑ 12.0 12.1 12.2 12.3 12.4 Trogler, William C. (1995). "The Environmental Chemistry of Trace Atmospheric Gases". Journal of Chemical Education 72 (11): 973. doi:10.1021/ed072p973. Bibcode: 1995JChEd..72..973T.
- ↑ 13.0 13.1 Gavin Schmidt (2010-10-01). "Taking the Measure of the Greenhouse Effect". NASA Goddard Institute for Space Studies - Science Briefs. https://www.giss.nasa.gov/research/briefs/2010_schmidt_05/.
External links
 |  |
