Absolute isotopic scale for deuterium analysis of natural waters.
                        Absolute D/H ratio for SMOW&lt;sup&gt;1&lt;/sup&gt;

Hagemann, Robert; Nief, G.; Roth, E.

doi:10.3402/tellusa.v22i6.10278

Cited by 139 publications

(73 citation statements)

References 4 publications

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“…In fact, the 2 H/ 1 H abundance ratio of the calibration materials VSMOW and SLAP are known absolutely by way of gravimetrical mixing. [20][21][22] For 18 O and 17 O, the situation is not so simple. Neither is it possible to obtain 100% pure 16 O, 17 O, or 18 O containing water, nor it is possible to know the isotope composition with a high degree of accuracy, although some efforts toward this goal have been published.…”

Section: Methodsmentioning

confidence: 99%

Stable Isotope Ratio Measurements on Highly Enriched Water Samples by Means of Laser Spectrometry

et al. 2001

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We demonstrate the feasibility of using laser spectrometry (LS) to analyze isotopically highly enriched water samples (i.e., δ2H ≤ 15 000‰, δ18O ≤ 1200‰), as often used in the biomedical doubly labeled water (DLW) method to quantify energy metabolism. The method is an important extension of a recently developed infrared laser direct absorption spectrometer. The measurements on highly enriched, small-size (10 μL liquid water) samples show a clearly better accuracy for the 2H/1H ratio. In the case of 18O/16O, the same level of accuracy is obtained as with conventional isotope ratio mass spectrometer (IRMS) analysis. With LS, the precision is better for both 18O/16O and 2H/1H. New is the ability to measure 17O/16O with the same accuracy as 18O/16O. A major advantage of the present technique is the absence of chemical sample preparation. The method is proven to be reliable and accurate and is ready to be used in many biomedical applications.

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Section: Methodsmentioning

confidence: 99%

Stable Isotope Ratio Measurements on Highly Enriched Water Samples by Means of Laser Spectrometry

et al. 2001

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“…The isotopic composition is expressed in δ notation as the relative deviation of the D/H ratio in a sample (SA) from a standard (ST), δ=((D/H) SA /(D/H) ST −1)*1000‰. The international standard for hydrogen isotopes is Vienna Standard Mean Ocean Water (VSMOW) with an absolute D/H ratio of (155.76±0.05)·10 −6 (Hagemann et al, 1970). Kinetic fractionation factors in chemical reactions are expressed as the reaction rate of the heavy isotopologue relative to the light isotopologue, e.g., α HD−sink =k(HD-removal)/k(HHremoval).…”

Section: Methodsmentioning

confidence: 99%

Heavy hydrogen in the stratosphere

2003

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Abstract. We report measurements of the deuterium content of molecular hydrogen (H 2 ) obtained from a suite of air samples that were collected during a stratospheric balloon flight between 12 and 33 km at 40 • N in October 2002. Strong deuterium enrichments of up to 400‰ versus Vienna Standard Mean Ocean Water (VSMOW) are observed, while the H 2 mixing ratio remains virtually constant. Thus, as hydrogen is processed through the H 2 reservoir in the stratosphere, deuterium is accumulated in H 2 . Using box model calculations we investigated the effects of H 2 sources and sinks on the stratospheric enrichments. Results show that considerable isotope enrichments in the production of H 2 from CH 4 must take place, i.e., deuterium is transferred preferentially to H 2 during the CH 4 oxidation sequence. This supports recent conclusions from tropospheric H 2 isotope measurements which show that H 2 produced photochemically from CH 4 and non-methane hydrocarbons must be enriched in deuterium to balance the tropospheric hydrogen isotope budget. In the absence of further data on isotope fractionations in the individual reaction steps of the CH 4 oxidation sequence, this effect cannot be investigated further at present. Our measurements imply that molecular hydrogen has to be taken into account when the hydrogen isotope budget in the stratosphere is investigated.

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“…δ 18 O(H 2 O) =(R18 O, sample /R18 O, V−SMOW −1)·1000‰, where R18 O denotes the isotopologue ratio H 2 18 O/H 2 16 O of a sample or V-SMOW, respectively. R D, V−SMOW is 0.31152·10 −3 (Hagemann et al, 1970;DeWit et al, 1980;Tse et al,δ 17 O, and δ 18 O values in this paper are given with respect to V-SMOW.…”

Section: Introductionmentioning

confidence: 99%

Modelling the budget of middle atmospheric water vapour isotopes

Zahn¹,

Franz

Bechtel

et al. 2006

Atmos. Chem. Phys.

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Abstract.A one-dimensional chemistry model is applied to study the stable hydrogen (D) and stable oxygen isotope ( 17 O, 18 O) composition of water vapour in stratosphere and mesosphere. In the troposphere, this isotope composition is determined by "physical" fractionation effects, that are phase changes (e.g. during cloud formation), diffusion processes (e.g. during evaporation from the ocean), and mixing of air masses. Due to these processes water vapour entering the stratosphere first shows isotope depletions in D/H relative to ocean water, which are ∼5 times of those in 18 In the stratosphere the known mass-independent fractionation (MIF) signal in O 3 is in a first step transferred to the NO x family and only in a second step to HO x and H 2 O. In contrast to CO 2 , O( 1 D) only plays a minor role in this MIF transfer. The major uncertainty in our calculation arises from poorly quantified isotope exchange reaction rate coefficients and kinetic isotope fractionation factors.

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Absolute isotopic scale for deuterium analysis of natural waters. Absolute D/H ratio for SMOW<sup>1</sup>

Cited by 139 publications

References 4 publications

Stable Isotope Ratio Measurements on Highly Enriched Water Samples by Means of Laser Spectrometry

Stable Isotope Ratio Measurements on Highly Enriched Water Samples by Means of Laser Spectrometry

Heavy hydrogen in the stratosphere

Modelling the budget of middle atmospheric water vapour isotopes

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