Atmospheric Oxygen: Isotopic Composition and Solubility Fractionation

Kroopnick, Peter M.; Craig, H.

doi:10.1126/science.175.4017.54

Cited by 518 publications

(317 citation statements)

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“…snowpack) NO 3 -, however, is more easily based on δ 18 O analysis (Amberger and Schmidt, 1987;Durka et al 1994;Kendall, 1998). On the theoretical assumption that nitrification derives two thirds of its oxygen from H 2 O (average for Stream 1 = -9‰), and one third from atmospheric O 2 (+23.5‰ (Kroopnick and Craig, 1972)), this would produce NO 3 -with δ 18 O NO3 = +2‰ for Site 1. In contrast, the snowpack NO 3 -ranged from δ 18 O NO3 = +60 to +85‰ (Heaton et al 2004 Earlier studies utilising δ 18 O NO3 analysis of silver nitrate samples prepared from high elevation or alpine tundra catchments have tended not to report sample purity, or consider how organic O contaminants might affect interpetation (Burns and Kendall, 2002;Campbell et al 2002;and Sickman et al 2003).…”

Section: Nitratementioning

confidence: 99%

Chemical and isotopic characteristics of weathering and nitrogen release in non-glacial drainage waters on Arctic tundra

Tye

Heaton

2007

Geochimica et Cosmochimica Acta

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Soil-water interactions in coastal tundra soils are a potential source of nutrients for surrounding fjordal and coastal ecosystems. Changes in water chemistry and stable isotope composition from 3 streams in west Spitsbergen were examined to assess the sources and losses of nitrogen, sulfur and carbon in thin organic tundra soils overlying sediments. Studies were undertaken from snowmelt (mid June) through to the end of the summer (

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Section: Nitratementioning

confidence: 99%

Chemical and isotopic characteristics of weathering and nitrogen release in non-glacial drainage waters on Arctic tundra

Tye

Heaton

2007

Geochimica et Cosmochimica Acta

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“…As the mixing ratio falls, indicating less contamination, the I 8 0 content will fall and approach that of the light variety. The kinetic isotope effect is not influenced by this behavior but will instead result from the formation of the light species, 8(180/l6O) = 5%,, from atmospheric oxygen with 6(l80/l6O) = 23.5%, (Kroopnick & Craig, 1972).…”

Section: Stable Isotope Composition Of Carbon Monoxidementioning

confidence: 99%

The global balance of carbon monoxide

Weinstock

Chang

1974

Tellus A: Dynamic Meteorology and Oceanography

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Radioactive carbon-14 monoxide produced by cosmic ray neutrons provides a useful tracer to deduce the residence time of carbon monoxide in the troposphere. From the steady-state equations for stable carbon monoxide and radioactive carbon monoxide, the production rate of stable carbon monoxide can also be derived. This rate is an order of magnitude greater than that estimated for CO sources such as the oceans, combustion, and chlorophyll decay. The oxidation of tropospheric methane initiated by hydroxyl radicals has been postulated to account for this predominant source of CO in nature. Estimates of the steady-state hydroxyl radical concentration in the troposphere are of sufficient magnitude to support this possibility. Furthermore, the hydroxyl radical can also provide the major removal mechanism for carbon monoxide by oxidation to CO, to maintain the carbon monoxide balance in nature. A critical review of the above theories is given, and some possibilities for experimcntal verification are discussed. The earlier computations are modified to refer to the northern troposphere in view of differences recently found for CO concentrations in the northern and southern troposphere. Observations of the stable isotope composition of methane, W H , and WH,, and of carbon monoxide, 12CI6O, 13C160, and lZClsO are also of significance to the proposed theory for the carbon monoxide balance. These data will be raviewed and discussed in terms of kinetic isotope effects in the reaction sequence, CH, to CO to CO,. The results of this analysis of the stable CO isotope data will be shown to be consistent with the conclusions drawn from the analysis of the radiocarbon data.

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“…The body's main oxygen sources are atmospheric O 2 , liquid water, and oxygen bound in food. Since atmospheric O 2 18 O values are relatively constant (Dole et al, 1954;Kroopnick & Craig, 1972) enamel oxygen isotope composition is controlled primarily by the composition of ingested water and, to a lesser extent, the composition of macronutrients in food. The isotopic composition of meteoric water (which is available to drink) is sensitive to climatic factors such as mean annual temperature and amount of local precipitation (Dansgaard, 1964).…”

Section: Introductionmentioning

confidence: 99%