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## (NAS Colloquium) Carbon Dioxide and Climate Change (1997) National Academy of Sciences (NAS)

### Citation Manager

. "Gases in ice cores." (NAS Colloquium) Carbon Dioxide and Climate Change. Washington, DC: The National Academies Press, 1997.

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FIG. 1. (From Martinerie et al., ref. 3). (Upper) Closed porosity vs. density in the firn at Summit, Greenland. Note the monotonic relationship between the two properties. When density = 0.83, open porosity = 0. The decrease in closed porosity at higher densities is due to compression of bubbles. (Lower) Closed porosity vs. depth for maximum-density layers and minimum-density layers. Note how maximum-density layers are completely closed by 75-m depth, and minimum-density layers by 83-m depth. In the intervening depth interval, parts of the firn remain permeable but gases cannot migrate vertically.

Several additional factors influence the composition of air in the firn. Gravitational fractionation is one ( 8 , 9 , 10 ). The pressure of gases increases with depth below the surface of the firn according to the barometric equation:

P/Pz = exp(mgz/RT).

m = mass in units of g mol-1, g is the gravitational acceleration constant, z is depth, R is the ideal gas constant, and T is Kelvin temperature.

FIG. 2. d15N (Left) and CH4 (Right) vs. depth in firn air from the GISP2 site at Summit, Greenland. The subsurface maximum in d15N is due to thermal fractionation (15N is enriched at 5- and 10-m depth because the firn at these depths, which remains at the mean annual temperature, is colder than air at the surface during summertime, when sampling was done). The increase below 20-m depth is due to gravitational fractionation. CH4 decreases very slowly to the top of the bubble closeoff zone at 70-m depth. Below it decreases very rapidly because gases cannot migrate vertically and the age of the gas in the firn increases as rapidly as the age of the ice (about 4 yr/m).

As Craig et al. ( 8 ) and Schwander ( 10 ) recognized, this equation applies not only to bulk air but to each individual constituent of air in that (dominant) depth interval of the firn where transport is essentially entirely by diffusion (the stagnant air column). The rate at which the enrichment-per-mass unit increases with depth, expressed in the d notation, is (?mg/RT -1)·1,000, or about 0.005‰/amu per meter at typical firn air temperatures. The relative enrichment with depth for different species is directly proportional to the mass difference. The firn air data for the GISP2 site, central Greenland, demonstrate the expected enrichment for the d15N of N2 ( Fig. 2 ). The enrichment or depletion is significant for nearly all species, corresponding to 3 ppmv of CO2 at the base of deep firn profiles, for example.

Seasonal changes in the concentrations of gases in air cause seasonal variations in firn air chemistry. The magnitude of these variations relative to their secular trends depends on location and property. The effect is perhaps largest for O2, CO2, and d13C of CO2 in Greenland. Seasonal variations are damped out with depth and become very small below 30–50 m.

Thermal fractionation also affects the isotopic and elemental composition of firn air. Severinghaus ( 11 ) and Severinghaus et al. ( 12 ) first recognized the importance of thermal fractionation in porous environmental media in their studies of the composition of air in sand dunes. Temperature gradients cause fractionation, with heavier gases or isotopes being enriched in colder regions. For 15N, the fractionation is about 0.025‰/°C. Thermal fractionation is large in firn because gases diffuse faster than heat. In consequence, steep seasonal temperature gradients occur in the upper ˜5 m of the firn and gases nearly equilibrate with these temperature gradients. This effect produces large seasonal variations in isotopic compositions and in the O2/N2 ratio in the top few meters of the firn. The seasonal anomalies decrease with depth, and for most species are insignificant below 30 m. O2 is an exception; the concentration of this gas in air is changing so slowly (on a percentage basis) that seasonal thermal gradients are significant down to 60-m depth.

These processes combine to influence the composition of gas throughout the firn, and at its base where gases are trapped as bubbles in impermeable ice. Here, two modes of trapping are possible. First, seasonal layering may be absent and air may be trapped throughout the bubble closeoff zone. In this case, the composition of the bulk trapped gases in ice cores will be further convoluted because of the finite closeoff interval. At Vostok, for example, the bubble closeoff zone is about 8 m

FIG. 1. (From Martinerie et al., ref. 3). (Upper) Closed porosity vs. density in the firn at Summit, Greenland. Note the monotonic relationship between the two properties. When density = 0.83, open porosity = 0. The decrease in closed porosity at higher densities is due to compression of bubbles. (Lower) Closed porosity vs. depth for maximum-density layers and minimum-density layers. Note how maximum-density layers are completely closed by 75-m depth, and minimum-density layers by 83-m depth. In the intervening depth interval, parts of the firn remain permeable but gases cannot migrate vertically.

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 Contents (R1-R4) Climate change and carbon dioxide: An introduction (1-2) Tribute to Roger Revelle and his contribution to studies of carbon dioxide and climate change (3-7) Equilibration of the terrestrial water, nitrogen, and carbon cycles (8-11) Potential responses of soil organic carbon to global environmental change (12-19) Global air-sea flux of CO2: An estimate based on measurements of sea-air pCO2 differences (20-27) Characteristics of the deep ocean carbon system during the past 150,000 years: CO2 distributions, deep water flow patterns, and abrupt climate change (28-35) Direct observation of the oceanic CO2 increase revisited (36-41) The observed global warming record: What does it tell us? (42-48) Possible forcing of global temperature by the oceanic tides (49-56) Spectrum of 100-kyr glacial cycle: Orbital inclination, not eccentricity (57-62) Can increasing carbon dioxide cause climate change? (63-70) Gases in ice cores (71-77) Tree rings, carbon dioxide, and climatic change (78-81) Geochemistry of corals: Proxies of past ocean chemistry, ocean circulation, and climate (82-89) A long marine history of carbon cycle modulation by orgital-climatic changes (90-97) Dependence of global temperatures on atmospheric CO2 and solar irradiance (98-107)