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Trace gas

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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

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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

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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

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See also: List of 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 (N
2,O
2, 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

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  1. ^ a b c d e Wallace, John; Hobbs, Peter (2006). Atmospheric Science: An Introductory Survey. Amsterdam, Boston: Elsevier Academic Press. ISBN 9780127329512.
  2. ^ "Trends in Atmospheric Carbon Dioxide". NOAA Earth System Research Laboratories. Retrieved 2022-01-20.
  3. ^ "Trends in Atmospheric Methane". NOAA Earth System Research Laboratories. Retrieved 2022-01-20.
  4. ^ "Chapter 8". AR5 Climate Change 2013: The Physical Science Basis.
  5. ^ 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
  6. ^ "Figure 8.SM.4" (PDF). Intergovernmental Panel on Climate Change Fifth Assessment Report - Supplemental Material. p. 8SM-16.
  7. ^ Archer, David (2009). "Atmospheric lifetime of fossil fuel carbon dioxide". Annual Review of Earth and Planetary Sciences. 37 (1): 117–34. Bibcode:2009AREPS..37..117A. doi:10.1146/annurev.earth.031208.100206. hdl:2268/12933.
  8. ^ Joos, F.; Roth, R.; Fuglestvedt, J.D.; 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. hdl:20.500.11850/58316.
  9. ^ "Long-term global trends of atmospheric trace gases". NOAA Earth System Research Laboratories. Retrieved 8 January 2022.
  10. ^ "AGAGE Data and Figures". Massachusetts Institute of Technology. Retrieved 8 January 2022.
  11. ^ a b 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. Bibcode:1988TellB..40..229S. doi:10.3402/tellusb.v40i3.15909.
  12. ^ a b c d e Trogler, William C. (1995). "The Environmental Chemistry of Trace Atmospheric Gases". Journal of Chemical Education. 72 (11): 973. Bibcode:1995JChEd..72..973T. doi:10.1021/ed072p973.
  13. ^ a b Gavin Schmidt (2010-10-01). "Taking the Measure of the Greenhouse Effect". NASA Goddard Institute for Space Studies - Science Briefs.
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