Chemistry:Greenhouse gas

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Short description: Gas in an atmosphere that absorbs and emits radiation at thermal infrared wavelengths
Greenhouse gases trap some of the heat that results when sunlight heats the Earth's surface. Three important greenhouse gases are shown symbolically in this image: carbon dioxide, water vapor, and methane.
The extent to which particular greenhouse gases are causing climate change, along with other factors.

Greenhouse gases are the gases in the atmosphere that raise the surface temperature of planets such as the Earth. What distinguishes them from other gases is that they absorb the wavelengths of radiation that a planet emits, resulting in the greenhouse effect.[1] The Earth is warmed by sunlight, causing its surface to radiate heat, which is then mostly absorbed by greenhouse gases. Without greenhouse gases in the atmosphere, the average temperature of Earth's surface would be about −18 °C (0 °F),[2] rather than the present average of 15 °C (59 °F).[3][4]

The most abundant greenhouse gases in Earth's atmosphere, listed in decreasing order of average global mole fraction, are:[5][6] Water vapor (H2O), Carbon dioxide (CO2), Methane (CH4), Nitrous oxide (N2O), Ozone (O3), Chlorofluorocarbons (CFCs and HCFCs), Hydrofluorocarbons (HFCs), Perfluorocarbons (CF4, C2F6, etc.), SF6, and NF3. Yet, while water vapor is a potent greenhouse gas, humans are not directly adding to its concentrations,[7]. so it is not one of the primary drivers of climate change, but rather one of the feedbacks.[8] On the other hand, carbon dioxide is causing about three quarters of global warming and can take thousands of years to be fully absorbed by the carbon cycle.[9][10] Methane causes most of the remaining warming and lasts in the atmosphere for an average of 12 years.[11]

Human activities since the beginning of the Industrial Revolution (around 1750) have increased atmospheric methane concentrations by over 150% and carbon dioxide by over 50%,[12][13] up to a level not seen in over 3 million years.[14] The vast majority of carbon dioxide emissions by humans come from the combustion of fossil fuels, principally coal, petroleum (including oil) and natural gas. Additional contributions come from cement manufacturing, fertilizer production, and changes in land use like deforestation.[15]:687[16][17] Methane emissions originate from agriculture, fossil fuel production, waste, and other sources.[18]

According to Berkeley Earth, average global surface temperature has risen by more than 1.2 °C (2.2 °F) since the pre-industrial (1850–1899) period as a result of greenhouse gas emissions. If current emission rates continue then temperature rises will surpass 2.0 °C (3.6 °F) sometime between 2040 and 2070, which is the level the United Nations ' Intergovernmental Panel on Climate Change (IPCC) says is "dangerous".[19]


Properties

refer to caption and adjacent text
Atmospheric absorption and scattering at different wavelengths of electromagnetic waves. The largest absorption band of carbon dioxide is not far from the maximum in the thermal emission from ground, and it partly closes the window of transparency of water—explaining carbon dioxide's major heat-trapping effect.

Greenhouse gases are infrared active, meaning that they absorb and emit infrared radiation in the same long wavelength range as what is emitted by the Earth's surface, clouds and atmosphere.[20]:2233

99% of the Earth's dry atmosphere (excluding water vapor) is made up of nitrogen (N2) (78%) and oxygen (O2) (21%). Because their molecules contain two atoms of the same element, they have no asymmetry in the distribution of their electrical charges,[21] and so are almost totally unaffected by infrared thermal radiation,[22] with only an extremely minor effect from collision-induced absorption.[23][24][25] A further 0.9% of the atmosphere is made up by argon (Ar), which is monatomic, and so completely transparent to thermal radiation. On the other hand, carbon dioxide (0.04%), methane, nitrous oxide and even less abundant trace gases account for less than 0.1% of Earth's atmosphere, but because their molecules contain atoms of different elements, there is an asymmetry in electric charge distribution which allows molecular vibrations to interact with electromagnetic radiation. This makes them infrared active, and so their presence causes greenhouse effect.[21]

Radiative forcing

Main page: Astronomy:Radiative forcing
Longwave-infrared absorption coefficients of primary greenhouse gases. Water vapor absorbs over a broad range of wavelengths. Earth emits thermal radiation particularly strongly in the vicinity of the carbon dioxide 15-micron absorption band. The relative importance of water vapor decreases with increasing altitude.

Earth absorbs some of the radiant energy received from the sun, reflects some of it as light and reflects or radiates the rest back to space as heat. A planet's surface temperature depends on this balance between incoming and outgoing energy. When Earth's energy balance is shifted, its surface becomes warmer or cooler, leading to a variety of changes in global climate.[26] Radiative forcing is a metric calculated in watts per square meter, which characterizes the impact of an external change in a factor that influences climate. It is calculated as the difference in top-of-atmosphere (TOA) energy balance immediately caused by such an external change A positive forcing, such as from increased concentrations of greenhouse gases, means more energy arriving than leaving at the top-of-atmosphere, which causes additional warming, while negative forcing, like from sulfates forming in the atmosphere from sulfur dioxide, leads to cooling.[20]:2245[27]

Within the lower atmosphere, greenhouse gases exchange thermal radiation with the surface and limit radiative heat flow away from it, which reduces the overall rate of upward radiative heat transfer.[28]:139[29] The increased concentration of greenhouse gases is also cooling the upper atmosphere, as it is much thinner than the lower layers, and any heat re-emitted from greenhouse gases is more likely to travel further to space than to interact with the fewer gas molecules in the upper layers. The upper atmosphere is also shrinking as the result.[30]

Global warming potential (GWP) and CO2 equivalents

This section is an excerpt from Global warming potential[ edit ]

Contributions of specific gases to the greenhouse effect

Main page: Earth:Greenhouse effect
Atmospheric gases only absorb some wavelengths of energy but are transparent to others. The absorption patterns of water vapor (blue peaks) and carbon dioxide (pink peaks) overlap in some wavelengths.[31]

Overall greenhouse effect

This table shows the most important contributions to the overall greenhouse effect, without which the average temperature of Earth's surface would be about −18 °C (0 °F),[2] instead of around 15 °C (59 °F).[3] This table also specifies tropospheric ozone, because this gas has a cooling effect in the stratosphere, but a warming influence comparable to nitrous oxide and CFCs in the troposphere.[32]

Percent contribution to total greenhouse effect
K&T (1997)[33] Schmidt (2010)[34]
Contributor Clear Sky With Clouds Clear Sky With Clouds
Water vapor 60 41 67 50
Clouds 31 25
CO
2		 26 18 24 19
Tropospheric ozone (O3) 8
N
2O + CH
4		 6
Other 9 9 7

K&T (1997) used 353 ppm CO
2 and calculated 125 W/m2 total clear-sky greenhouse effect; relied on single atmospheric profile and cloud model. "With Clouds" percentages are from Schmidt (2010) interpretation of K&T (1997).
Schmidt (2010) used 1980 climatology with 339 ppm CO
2 and 155 W/m2 total greenhouse effect; accounted for temporal and 3-D spatial distribution of absorbers.

Concentrations and other characteristics of greenhouse gases

The radiative forcing (warming influence) of long-lived atmospheric greenhouse gases has accelerated, almost doubling in 40 years.[35][36][37]

Anthropogenic changes to the natural greenhouse effect are sometimes referred to as the enhanced greenhouse effect.[20]:2223 The contribution of each gas to the enhanced greenhouse effect is determined by the characteristics of that gas, its abundance, and any indirect effects it may cause. For example, the direct radiative effect of a mass of methane is about 84 times stronger than the same mass of carbon dioxide over a 20-year time frame.[38] Since the 1980s, greenhouse gas forcing contributions (relative to year 1750) are also estimated with high accuracy using IPCC-recommended expressions derived from radiative transfer models.[39]

The concentration of a greenhouse gas is typically measured in parts per million (ppm) or parts per billion (ppb) by volume. A CO
2 concentration of 420 ppm means that 420 out of every million air molecules is a CO
2 molecule. The first 30 ppm increase in CO
2 concentrations took place in about 200 years, from the start of the Industrial Revolution to 1958; however the next 90 ppm increase took place within 56 years, from 1958 to 2014.[13][40][41] Similarly, the average annual increase in the 1960s was only 37% of what it was in 2000 through 2007.[42]

Many observations are available online in a variety of atmospheric chemistry observational databases. The table below shows the most influential long-lived, well-mixed greenhouse gases, along with their tropospheric concentrations and direct radiative forcings, as identified by the Intergovernmental Panel on Climate Change (IPCC).[43] Abundances of these trace gases are regularly measured by atmospheric scientists from samples collected throughout the world.[44][45][46] It excludes water vapor because changes in its concentrations are calculated as a climate change feedback indirectly caused by changes in other greenhouse gases, as well as ozone, whose concentrations are only modified indirectly by various refrigerants that cause ozone depletion. Some short-lived gases (e.g. carbon monoxide, NOx) and aerosols (e.g. mineral dust or black carbon) are also excluded because of limited role and strong variation, alongside with minor refrigants and other halogenated gases, which have been mass-produced in smaller quantities than those in the table.[43]:731-738 and Annex III of the 2021 IPCC WG1 Report[47]:4-9

IPCC list of greenhouse gases with lifetime, 100-year global warming potential, concentrations in the troposphere and radiative forcings. The abbreviations TAR, AR4, AR5 and AR6 refer to the different IPCC reports over the years. The baseline is pre-industrialization (year 1750).
Species Lifetime

(years) [43]:731

100-yr

GWP [43]:731

Mole Fraction [ppt - except as noted]a + Radiative forcing [W m−2] [B] Concentrations

over time[48][49]

up to year 2020

Baseline

Year 1750

TAR[50]

Year 1998

AR4[51]

Year 2005

AR5[43]:678

Year 2011

AR6[47]:4-9

Year 2019

CO2 [ppm] [A] 1 278 365 (1.46) 379 (1.66) 391 (1.82) 410 (2.16) Mauna Loa CO2 monthly mean concentration.svg
CH4 [ppb] 12.4 28 700 1,745 (0.48) 1,774 (0.48) 1,801 (0.48) 1866 (0.54) Mlo ch4 ts obs 03437.png
N2O [ppb] 121 265 270 314 (0.15) 319 (0.16) 324 (0.17) 332 (0.21) HATS Nitrous Oxide concentration.png
CFC-11 45 4,660 0 268 (0.07) 251 (0.063) 238 (0.062) 226 (0.066) Hats f11 global.png
CFC-12 100 10,200 0 533 (0.17) 538 (0.17) 528 (0.17) 503 (0.18) Hats f12 global.png
CFC-13 640 13,900 0 4 (0.001) - 2.7 (0.0007) 3.28 (0.0009) cfc13
CFC-113 85 6,490 0 84 (0.03) 79 (0.024) 74 (0.022) 70 (0.021) Hats f113 global.png
CFC-114 190 7,710 0 15 (0.005) - - 16 (0.005) cfc114
CFC-115 1,020 5,860 0 7 (0.001) - 8.37 (0.0017) 8.67 (0.0021) cfc115
HCFC-22 11.9 5,280 0 132 (0.03) 169 (0.033) 213 (0.0447) 247 (0.0528) HCFC22 concentration.jpg
HCFC-141b 9.2 2,550 0 10 (0.001) 18 (0.0025) 21.4 (0.0034) 24.4 (0.0039) HCFC141b concentration.jpg
HCFC-142b 17.2 5,020 0 11 (0.002) 15 (0.0031) 21.2 (0.0040) 22.3 (0.0043) HCFC142b concentration.jpg
CH3CCl3 5 160 0 69 (0.004) 19 (0.0011) 6.32 (0.0004) 1.6 (0.0001) BK MC.jpg
CCl4 26 1,730 0 102 (0.01) 93 (0.012) 85.8 (0.0146) 78 (0.0129) Hats ccl4 global.png
HFC-23 222 12,400 0 14 (0.002) 18 (0.0033) 24 (0.0043) 32.4 (0.0062) HFC-23 mm.png
HFC-32 5.2 677 0 - - 4.92 (0.0005) 20 (0.0022) BK HFC32.jpg
HFC-125 28.2 3,170 0 - 3.7 (0.0009) 9.58 (0.0022) 29.4 (0.0069) HFC125 concentration.jpg
HFC-134a 13.4 1,300 0 7.5 (0.001) 35 (0.0055) 62.7 (0.0100) 107.6 (0.018) Mauna Loa HFC-134a (CH2FCF3) concentration.png
HFC-143a 47.1 4,800 0 - - 12.0 (0.0019) 24 (0.0040) HFC143a concentration.jpg
HFC-152a 1.5 138 0 0.5 (0.0000) 3.9 (0.0004) 6.4 (0.0006) 7.1 (0.0007) HFC152a concentration.jpg
CF4 (PFC-14) 50,000 6,630 40 80 (0.003) 74 (0.0034) 79 (0.0040) 85.5 (0.0051) Mauna Loa Tetrafluoromethane.jpg
C2F6 (PFC-116) 10,000 11,100 0 3 (0.001) 2.9 (0.0008) 4.16 (0.0010) 4.85 (0.0013) Hexafluoroethane concentration.jpg
SF6 3,200 23,500 0 4.2 (0.002) 5.6 (0.0029) 7.28 (0.0041) 9.95 (0.0056) Mauna Loa Sulfur Hexafluoride concentration.jpg
SO2F2 36 4,090 0 - - 1.71 (0.0003) 2.5 (0.0005) SO2F2 mm.png
NF3 500 16,100 0 - - 0.9 (0.0002) 2.05 (0.0004) Nitrogen Trifluoride concentration.jpg

a Mole fractions: μmol/mol = ppm = parts per million (106); nmol/mol = ppb = parts per billion (109); pmol/mol = ppt = parts per trillion (1012).

A The IPCC states that "no single atmospheric lifetime can be given" for CO2.[43]:731 This is mostly due to the rapid growth and cumulative magnitude of the disturbances to Earth's carbon cycle by the geologic extraction and burning of fossil carbon.[52] 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, as based on the projections of coupled models referenced in the AR5 assessment.[53] A substantial fraction (20-35%) was also projected to remain in the atmosphere for centuries to millennia, where fractional persistence increases with pulse size.[54][55]

B Values are relative to year 1750. AR6 reports the effective radiative forcing which includes effects of rapid adjustments in the atmosphere and at the surface.[56]

Factors affecting concentrations

Atmospheric concentrations are determined by the balance between sources (emissions of the gas from human activities and natural systems) and sinks (the removal of the gas from the atmosphere by conversion to a different chemical compound or absorption by bodies of water).[57]:512

Airborne fraction

The proportion of an emission remaining in the atmosphere after a specified time is the "airborne fraction" (AF). The annual airborne fraction is the ratio of the atmospheric increase in a given year to that year's total emissions.

As of 2006 the annual airborne fraction for CO2 was about 0.45. The annual airborne fraction increased at a rate of 0.25 ± 0.21% per year over the period 1959–2006.[58]

Atmospheric lifetime

Most CO
2 emissions have been absorbed by carbon sinks, including plant growth, soil uptake, and ocean uptake (2020 Global Carbon Budget).

Aside from water vapor, which has a residence time of about nine days,[59] major greenhouse gases are well mixed and take many years to leave the atmosphere.[60] Although it is not easy to know with precision how long it takes greenhouse gases to leave the atmosphere, there are estimates for the principal greenhouse gases. Jacob (1999)[61] defines the lifetime [math]\displaystyle{ \tau }[/math] of an atmospheric species X in a one-box model as the average time that a molecule of X remains in the box. Mathematically [math]\displaystyle{ \tau }[/math] can be defined as the ratio of the mass [math]\displaystyle{ m }[/math] (in kg) of X in the box to its removal rate, which is the sum of the flow of X out of the box ([math]\displaystyle{ F_\text{out} }[/math]), chemical loss of X ([math]\displaystyle{ L }[/math]), and deposition of X ([math]\displaystyle{ D }[/math]) (all in kg/s):

[math]\displaystyle{ \tau = \frac{m}{F_\text{out}+L+D} }[/math].[61]

If input of this gas into the box ceased, then after time [math]\displaystyle{ \tau }[/math], its concentration would decrease by about 63%.

The atmospheric lifetime of a species therefore measures the time required to restore equilibrium following a sudden increase or decrease in its concentration in the atmosphere. Individual atoms or molecules may be lost or deposited to sinks such as the soil, the oceans and other waters, or vegetation and other biological systems, reducing the excess to background concentrations. The average time taken to achieve this is the mean lifetime.

Carbon dioxide has a variable atmospheric lifetime, and cannot be specified precisely.[62][38][20]:2237 Similar issues apply to other greenhouse gases, many of which have longer mean lifetimes than CO2, e.g. N2O has a mean atmospheric lifetime of 121 years.[38]

Water vapor

Water vapor concentrations fluctuate regionally, but human activity does not directly affect water vapor concentrations except at local scales, such as near irrigated fields. Indirectly, human activity that increases global temperatures will increase water vapor concentrations, because Clausius–Clapeyron relation establishes that more water vapor will be present per unit volume at elevated temperatures. This process known as water vapor feedback.[63] The atmospheric concentration of vapor is highly variable and depends largely on temperature, from less than 0.01% in extremely cold regions up to 3% by mass in saturated air at about 32 °C.[64]

Sources

Natural sources

Most greenhouse gases have both natural and human-caused sources. An exception are purely human-produced synthetic halocarbons which have no natural sources. During the pre-industrial Holocene, concentrations of existing gases were roughly constant, because the large natural sources and sinks roughly balanced. In the industrial era, human activities have added greenhouse gases to the atmosphere, mainly through the burning of fossil fuels and clearing of forests.[65][4]:115

Greenhouse gas emissions from human activities

Taking into account direct and indirect emissions, industry is the sector with the highest share of global emissions. Data as of 2019 from the IPCC.
This section is an excerpt from Greenhouse gas emissions § Overview of main sources[ edit ]

Monitoring

Greenhouse gas monitoring involves the direct measurement of greenhouse gas emissions and levels. There are several different methods of measuring carbon dioxide concentrations in the atmosphere, including infrared analyzing and manometry. Methane and nitrous oxide are measured by other instruments. Greenhouse gases are measured from space such as by the Orbiting Carbon Observatory and networks of ground stations such as the Integrated Carbon Observation System.[citation needed]

The Annual Greenhouse Gas Index (AGGI) is defined by atmospheric scientists at NOAA as the ratio of total direct radiative forcing due to long-lived and well-mixed greenhouse gases for any year for which adequate global measurements exist, to that present in year 1990.[37][66] These radiative forcing levels are relative to those present in year 1750 (i.e. prior to the start of the industrial era). 1990 is chosen because it is the baseline year for the Kyoto Protocol, and is the publication year of the first IPCC Scientific Assessment of Climate Change.

As such, NOAA states that the AGGI "measures the commitment that (global) society has already made to living in a changing climate. It is based on the highest quality atmospheric observations from sites around the world. Its uncertainty is very low."[67]

Data networks

This section is an excerpt from Carbon dioxide in Earth's atmosphere#Data networks[ edit ]

Removal from the atmosphere

Further information: Physics:Carbon sink and Earth:Carbon sequestration

Natural processes

Further information: Earth:Carbon cycle

Carbon dioxide is removed from the atmosphere primarily through photosynthesis and enters the terrestrial and oceanic biospheres. Carbon dioxide also dissolves directly from the atmosphere into bodies of water (ocean, lakes, etc.), as well as dissolving in precipitation as raindrops fall through the atmosphere. When dissolved in water, carbon dioxide reacts with water molecules and forms carbonic acid, which contributes to ocean acidity. It can then be absorbed by rocks through weathering. It also can acidify other surfaces it touches or be washed into the ocean.[68]

This section is an excerpt from Atmospheric carbon cycle[ edit ]

Negative emissions

Main pages: Earth:Carbon dioxide removal and Earth:Net zero emissions

A number of technologies remove greenhouse gases emissions from the atmosphere. Most widely analyzed are those that remove carbon dioxide from the atmosphere, either to geologic formations such as bio-energy with carbon capture and storage and carbon dioxide air capture,[69] or to the soil as in the case with biochar.[69] Many long-term climate scenario models require large-scale human-made negative emissions to avoid serious climate change.[70] Negative emissions approaches are also being studied for atmospheric methane, called atmospheric methane removal.[71]

During geologic time scales

This section is an excerpt from Carbon dioxide in Earth's atmosphere#Concentrations in the geologic past[ edit ]

History of discovery

This 1912 article succinctly describes how burning coal creates carbon dioxide that causes climate change.[72]

In the late 19th century, scientists experimentally discovered that N2 and O2 do not absorb infrared radiation (called, at that time, "dark radiation"), while water (both as true vapor and condensed in the form of microscopic droplets suspended in clouds) and CO
2 and other poly-atomic gaseous molecules do absorb infrared radiation.[73][74] In the early 20th century, researchers realized that greenhouse gases in the atmosphere made Earth's overall temperature higher than it would be without them. The term greenhouse was first applied to this phenomenon by Nils Gustaf Ekholm in 1901.[75][76]

During the late 20th century, a scientific consensus evolved that increasing concentrations of greenhouse gases in the atmosphere cause a substantial rise in global temperatures and changes to other parts of the climate system,[77] with consequences for the environment and for human health.

Other planets

Greenhouse gases exist in many atmospheres, creating greenhouse effects on Mars, Titan and particularly in the thick atmosphere of Venus.[78] While Venus has been described as the ultimate end state of runaway greenhouse effect, such a process would have virtually no chance of occurring from any increases in greenhouse gas concentrations caused by humans,[79] as the Sun's brightness is too low and it would likely need to increase by some tens of percents, which will take a few billion years.[80]

See also

References

  1. ↑ Matthews, J.B.R. et al. (2021-08-09). "Annex VII: Glossary". Climate Change 2021: The Physical Science Basis. Contribution of Working Group I to the Sixth Assessment Report of the Intergovernmental Panel on Climate Change. IPCC / Cambridge University Press. pp. 2215–2256. doi:10.1017/9781009157896.022. ISBN 9781009157896. https://www.ipcc.ch/report/ar6/wg1/downloads/report/IPCC_AR6_WGI_AnnexVII.pdf. 
  2. ↑ 2.0 2.1 "NASA GISS: Science Briefs: Greenhouse Gases: Refining the Role of Carbon Dioxide". http://www.giss.nasa.gov/research/briefs/ma_01/. 
  3. ↑ 3.0 3.1 "Modern global climate change". Science 302 (5651): 1719–23. 2003. doi:10.1126/science.1090228. PMID 14657489. Bibcode: 2003Sci...302.1719K. https://zenodo.org/record/1230878. Retrieved 26 July 2019. 
  4. ↑ 4.0 4.1 Le Treut, H., R. Somerville, U. Cubasch, Y. Ding, C. Mauritzen, A. Mokssit, T. Peterson and M. Prather, 2007: Chapter 1: Historical Overview of Climate Change. In: Climate Change 2007: The Physical Science Basis. Contribution of Working Group I to the Fourth Assessment Report of the Intergovernmental Panel on Climate Change [Solomon, S., D. Qin, M. Manning, Z. Chen, M. Marquis, K.B. Averyt, M. Tignor and H.L. Miller (eds.)]. Cambridge University Press, Cambridge, United Kingdom and New York, NY, USA
  5. ↑ "Atmospheric Concentration of Greenhouse Gases". U.S. Environmental Protection Agency. 2016-08-01. https://www.epa.gov/sites/default/files/2016-08/documents/print_ghg-concentrations-2016.pdf. 
  6. ↑ "Inside the Earth's invisible blanket.". http://sequestration.org/science/greenhousegases.html. 
  7. ↑ 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/. 
  8. ↑ "NASA Science Mission Directorate article on the water cycle". Nasascience.nasa.gov. http://nasascience.nasa.gov/earth-science/oceanography/ocean-earth-system/ocean-water-cycle. 
  9. ↑ "Global Greenhouse Gas Emissions Data". United States Environmental Protection Agency. 12 January 2016. https://www.epa.gov/ghgemissions/global-greenhouse-gas-emissions-data. 
  10. ↑ "Climate Change Indicators: Greenhouse Gases". United States Environmental Protection Agency. 16 December 2015. https://www.epa.gov/climate-indicators/greenhouse-gases. "Carbon dioxide's lifetime cannot be represented with a single value because the gas is not destroyed over time, but instead moves among different parts of the ocean–atmosphere–land system. Some of the excess carbon dioxide is absorbed quickly (for example, by the ocean surface), but some will remain in the atmosphere for thousands of years, due in part to the very slow process by which carbon is transferred to ocean sediments." 
  11. ↑ "Understanding methane emissions". International Energy Agency. https://www.iea.org/reports/global-methane-tracker-2023/understanding-methane-emissions. 
  12. ↑ "Understanding methane emissions". International Energy Agency. https://www.iea.org/reports/global-methane-tracker-2023/understanding-methane-emissions. "The concentration of methane in the atmosphere is currently over two-and-a-half times greater than its pre-industrial levels" 
  13. ↑ 13.0 13.1 "Carbon dioxide now more than 50% higher than pre-industrial levels" (in en). National Oceanic and Atmospheric Administration. 3 June 2022. https://www.noaa.gov/news-release/carbon-dioxide-now-more-than-50-higher-than-pre-industrial-levels. 
  14. ↑ "Climate Change: Atmospheric Carbon Dioxide". https://www.climate.gov/news-features/understanding-climate/climate-change-atmospheric-carbon-dioxide. 
  15. ↑ Canadell, J.G., P.M.S. Monteiro, M.H. Costa, L. Cotrim da Cunha, P.M. Cox, A.V. Eliseev, S. Henson, M. Ishii, S. Jaccard, C. Koven, A. Lohila, P.K. Patra, S. Piao, J. Rogelj, S. Syampungani, S. Zaehle, and K. Zickfeld, 2021: Chapter 5: Global Carbon and other Biogeochemical Cycles and Feedbacks. In Climate Change 2021: The Physical Science Basis. Contribution of Working Group I to the Sixth Assessment Report of the Intergovernmental Panel on Climate Change [Masson-Delmotte, V., P. Zhai, A. Pirani, S.L. Connors, C. Péan, S. Berger, N. Caud, Y. Chen, L. Goldfarb, M.I. Gomis, M. Huang, K. Leitzell, E. Lonnoy, J.B.R. Matthews, T.K. Maycock, T. Waterfield, O. Yelekçi, R. Yu, and B. Zhou (eds.)]. Cambridge University Press, Cambridge, United Kingdom and New York, NY, USA, pp. 673–816, doi:10.1017/9781009157896.007.
  16. ↑ "Global Greenhouse Gas Emissions Data". U.S. Environmental Protection Agency. 12 January 2016. https://www.epa.gov/ghgemissions/global-greenhouse-gas-emissions-data. "The burning of coal, natural gas, and oil for electricity and heat is the largest single source of global greenhouse gas emissions." 
  17. ↑ "AR4 SYR Synthesis Report Summary for Policymakers – 2 Causes of change". ipcc.ch. https://www.ipcc.ch/publications_and_data/ar4/syr/en/spms2.html. 
  18. ↑ "Global Methane Tracker 2023". International Energy Agency. https://www.iea.org/reports/global-methane-tracker-2023. 
  19. ↑ "Analysis: When might the world exceed 1.5C and 2C of global warming?" (in en). 2020-12-04. https://www.carbonbrief.org/analysis-when-might-the-world-exceed-1-5c-and-2c-of-global-warming. 
  20. ↑ 20.0 20.1 20.2 20.3 IPCC, 2021: Annex VII: Glossary [Matthews, J.B.R., V. Möller, R. van Diemen, J.S. Fuglestvedt, V. Masson-Delmotte, C.  Méndez, S. Semenov, A. Reisinger (eds.)]. In Climate Change 2021: The Physical Science Basis. Contribution of Working Group I to the Sixth Assessment Report of the Intergovernmental Panel on Climate Change [Masson-Delmotte, V., P. Zhai, A. Pirani, S.L. Connors, C. Péan, S. Berger, N. Caud, Y. Chen, L. Goldfarb, M.I. Gomis, M. Huang, K. Leitzell, E. Lonnoy, J.B.R. Matthews, T.K. Maycock, T. Waterfield, O. Yelekçi, R. Yu, and B. Zhou (eds.)]. Cambridge University Press, Cambridge, United Kingdom and New York, NY, USA, pp. 2215–2256, doi:10.1017/9781009157896.022.
  21. ↑ 21.0 21.1 Archer, David (2011). Global Warming: Understanding the Forecast, Chapter 4: Greenhouse Gases (2 ed.). Wiley. ISBN 978-0470943410. http://forecast.uchicago.edu/chapter4.pdf. Retrieved 14 June 2023. 
  22. ↑ Wei, Peng-Sheng; Hsieh, Yin-Chih; Chiu, Hsuan-Han; Yen, Da-Lun; Lee, Chieh; Tsai, Yi-Cheng; Ting, Te-Chuan (6 October 2018). "Absorption coefficient of carbon dioxide across atmospheric troposphere layer". Heliyon 4 (10): e00785. doi:10.1016/j.heliyon.2018.e00785. PMID 30302408. Bibcode: 2018Heliy...400785W. 
  23. ↑ Höpfner, M.; Milz, M.; Buehler, S.; Orphall, J.; Stiller, G. (24 May 2012). "The natural greenhouse effect of atmospheric oxygen (O2) and nitrogen (N2)" (in en). Geophysical Research Letters 39 (L10706). doi:10.1029/2012GL051409. ISSN 1944-8007. Bibcode: 2012GeoRL..3910706H. 
  24. ↑ "Which Gases Are Greenhouse Gases?". American Chemical Society. https://www.acs.org/content/acs/en/climatescience/greenhousegases/whichgases.html. 
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