Evaporation and carbonic anhydrase activity recorded in oxygen isotope signatures of net CO2 fluxes from a Mediterranean soil

The oxygen stable isotope composition (δ¹⁸O) of CO₂ is a valuable tool for studying the gas exchange between terrestrial ecosystems and the atmosphere. In the soil, it records the isotopic signal of water pools subjected to precipitation and evaporation events. The δ¹⁸O of the surface soil net CO₂ flux is dominated by the physical processes of diffusion of CO₂ into and out of the soil and the chemical reactions during CO₂–H₂O equilibration. Catalytic reactions by the enzyme carbonic anhydrase, reducing CO₂ hydration times, have been proposed recently to explain field observations of the δ¹⁸O signatures of net soil CO₂ fluxes. How important these catalytic reactions are for accurately predicting large‐scale biosphere fluxes and partitioning net ecosystem fluxes is currently uncertain because of the lack of field data. In this study, we determined the δ¹⁸O signatures of net soil CO₂ fluxes from soil chamber measurements in a Mediterranean forest. Over the 3 days of measurements, the observed δ¹⁸O signatures of net soil CO₂ fluxes became progressively enriched with a well‐characterized diurnal cycle. Model simulations indicated that the δ¹⁸O signatures recorded the interplay of two effects: (1) progressive enrichment of water in the upper soil by evaporation, and (2) catalytic acceleration of the isotopic exchange between CO₂ and soil water, amplifying the contributions of ‘atmospheric invasion’ to net signatures. We conclude that there is a need for better understanding of the role of enzymatic reactions, and hence soil biology, in determining the contributions of soil fluxes to oxygen isotope signals in atmospheric CO₂.     

A mass spectrometric analysis of the water-splitting reaction

Earlier mass spectrometric measurements, in which oxygen evolution was measured following short saturating light flashes, indicated that with a time resolution of about 30 s no form of bound water and/or an oxidation product exists up to the redox state S₃ of the oxygen evolving center (R. Radmer and O. Ollinger, 1986, FEBS Lett 195: 285–289; K.P. Bader, P. Thibault and G.H. Schmid, 1987, Biochim Biophys Acta 893: 564–571). In the present study, isotope exchange experiments with H₂ ¹⁸O were performed under different experimental conditions. We found: a) the isotope exchange pattern is virtually the same at both pH 6.0 and 7.8, although marked structural changes of the PS II donor side are inferred to take place within this pH-range (Renger G., Messinger J. and Wacker U., 1992, Research in Photosynthesis, II: 329–332); b) injection of H₂ ¹⁸O at about 0°C gives rise to mass ratios of the evolved oxygen which markedly deviate from the theoretically expected values of complete isotope scrambling; and c) rapid injection of H₂ ¹⁸O into samples with high population of S₁ and S₂ and subsequent illumination with three and two flashes, respectively, spaced by a dark time of only 1.5 ms lead to similar ¹⁸O-labeling of the evolved oxygen. Based on the published data on the interaction with redox active amines, possible pathways of substrate exchange in the water oxidase are discussed.Abbreviations atom fraction of ¹⁸O - PS II Photosystem II - S_i redox states of the water oxidase - Y_z redox active tyrosine of polypeptide D1     

Variations in the natural abundance of oxygen-18 and deuterium in plant carbohydrates

Variations in the natural abundance of ¹⁸O and ²H in plant cellulose are influenced by the isotopic composition of the water directly involved in metabolism—the metabolic water fraction. The isotopic distinction between the metabolic source water and total tissue water must reflect the formation of isotopic gradients within the tissue that are influenced by the rate of water turnover, by properties of the water conducting system and by environmental conditions. It seems that the ¹⁸O abundance in the metabolic water is conserved in cellulose with a relatively constant isotope effect. The relationship of the ²H abundance between metabolic water and cellulose is more complex. Hydrogen incorporated into photosynthetic products during primary reduction steps is highly depleted in ²H. However, a large proportion of these hydrogens are subsequently replaced by exchange with water, leading to ²H enrichment during heterotrophic metabolism. Deciphering the oxygen isotope ratio of cellulose could help in providing insights into the carbon and oxygen fluxes exchanged between plants and the atmosphere. This is because the ¹⁸O abundance in cellulose records the ¹⁸O abundance in the metabolic water, which in turn, controls the oxygen isotopic signatures of the CO₂ and O₂ released by plants into the atmosphere. The hydrogen isotope effects associated with carbohydrate metabolism provide insights into the autotrophic state of a plant tissue. This is because the hydrogen isotope ratio of carbohydrates must reflect the net effects of the two opposing isotope effects associated with photosynthesis and heterotrophic metabolism.     

Influence of vegetation and soil CO2 exchange on the concentration and stable oxygen isotope ratio of atmospheric CO2 within a Pinus resinosa canopy

Measurements were made of the concentration and stable oxygen isotopic ratio of carbon dioxide in air samples collected on a diurnal basis at two heights within a Pinus resinosa canopy. Large changes in CO₂ concentration and isotopic composition were observed during diurnal time courses on all three symple dates. In addition, there was strong vertical stratification in the forest canopy, with higher CO₂ concentrations and more negative ¹⁸O values observed closer to the soil surface. The observed daily increases in ¹⁸O values of forest CO₂ were dependent on relative humidity consistent with the modelled predictions of isotopic fractionation during photosynthetic gas exchange. During photosynthetic gas exchange, a portion of the CO₂ that enters the leaf and equilibrates with leaf water is not fixed and diffuses back out of the leaf with an altered oxygen isotopic ratio. The oxygen isotope ratio of CO₂ diffusing out of a leaf depends primarily on the ¹⁸O content of leaf water which changes in response to relative humidity. In contrast, soil respiration caused a decline in the ¹⁸O values of forest CO₂ at night, because CO₂ released from the soil has equilibrated with soil water which has a lower ¹⁸O content than leaf water. The observed relationship between diurnal changes in CO₂ concentration and oxygen isotopic composition in the forest environment were consistent with a gas mixing model that considered the relative magnitudes of CO₂ fluxes associated with photosynthesis, respiration and turbulent exchange between the forest and the bulk atmosphere.     

Essai d'interprétation des cinétiques d'échange isotopique entre C18O2 et eau d'une feuille: Expériences à l'obscurité

Summary The interpretation of photosynthesis experiments using ¹⁸O as a tracer becomes very difficult on account of the exchange rate between oxygen atoms of carbon dioxide and water. The mathematical analysis of the kinetics of isotope exchange between CO₂ highly enriched with ¹⁸O and the water of an aerial leaf kept in darkness allows the determination of two velocity coefficients, k _e and k. k _e, related to the gaseous CO₂ diffusion, makes it possible to evaluate the CO₂ flow between the gaseous phase and the leaf, as well as the diffusion resistance of the boundary layer and the leaf stomata. k, related to the CO₂ hydration, gives the in situ enzymic activity of carbonic anhydrase. Measurements carried out on a great number of leaves show that k _e and k vary in the same direction.In addition, a simple relation exists between the isotopic composition of the gaseous phase and the corresponding values of the C¹⁸O₂ inside the leaf. Thus it is possible to determine the conditions for a leaf that may be favourable for light experiments designed to ascertain the origin of photosynthetic oxygen by use of ¹⁸O.     

Mechanism of the enzyme-catalyzed bioluminescent oxidation of coelenterate-type luciferin.

The use of a fully active, synthetic analogue of coelenterate-type luciferin labeled in the carbonyl position with ¹⁴C and ¹⁸O was used to probe the mechanism of the $\text{Renilla}$ luciferase catalyzed oxidative decarboxylation of this compound. In the presence of ¹⁷O₂, the CO₂ produced in this oxidation can be shown to contain approximately one ¹⁷O atom per CO₂ molecule. This result is consistent with a cyclic peroxide or dioxetanone-type mechanism. In the presence of luciferase, the oxygen in the luciferin carbonyl group is rapidly exchanged with solvent water prior to the production of CO₂. Thus, the $\text{reaction}$ CO₂ contains considerable oxygen derived from water, via exchange with the carbonyl group, and about one oxygen from O₂ via a cyclic peroxide.     

Experimental determination of stable isotope variability in Globigerina bulloides: implications for paleoceanographic reconstructions

We have quantified the environmental and physiological parameters responsible for stable isotopic disequilibrium in the non-symbiotic planktic foraminifera, Globigerina bulloides, via controlled experiments with living specimens. Individual test chambers secreted in the laboratory were amputated, pooled with other chambers from defined positions in the shell whorl and analyzed for their carbon and oxygen isotopic composition. When temperature, δ¹⁸O_water and δ¹³C of ΣCO₂ are kept constant, the chamber δ¹³C and δ¹⁸O values increase 2.6 and 0.8%. respectively between the smallest chambers (chs. 1–9, shell size ≈180 μm) and final chamber (ch. 14, shell size ≈500 μm). Feeding experiments with prey of different δ¹³C values show that 8–15% of the chamber δ¹³C signal is due to the incorporation of metabolic CO₂. The observed ontogenetic trend is responsible for the stable isotope size-dependency in this species and may be due to a fractionation mechanism involving the incorporation of metabolic CO₂ during calcification. Temperature experiments show that shell δ¹⁸O varies as predicted by paleotemperature equations, but is offset from equilibrium. We present correction factors that should be applied to δ¹³C and δ¹⁸O data from well constrained size ranges to yield either oxygen isotope equilibrium or ambient δ¹³C of seawater ΣCO₂. Our results suggest that for paleoceanographic applications, shells in the 270–320 μm size range are optimal for paleoenvironmental reconstructions     

Fixation of O(2) during Photorespiration: Kinetic and Steady-State Studies of the Photorespiratory Carbon Oxidation Cycle with Intact Leaves and Isolated Chloroplasts of C(3) Plants

Mass spectrometric techniques were used to trace the incorporation of [¹⁸O]oxygen into metabolites of the photorespiratory pathway. Glycolate, glycine, and serine extracted from leaves of the C₃ plants, Spinacia oleracea L., Atriplex hastata, and Helianthus annuus which had been exposed to [¹⁸O]oxygen at the CO₂ compensation point were heavily labeled with ¹⁸O. In each case one, and only one of the carboxyl oxygens was labeled. The abundance of ¹⁸O in this oxygen of glycolate reached 50 to 70% of that of the oxygen provided after only 5 to 10 seconds exposure to [¹⁸O]oxygen. Glycine and serine attained the same final enrichment after 40 and 180 seconds, respectively. This confirms that glycine and serine are synthesized from glycolate.

The labeling of photorespiratory intermediates in intact leaves reached a mean of 59% of that of the oxygen provided in the feedings. This indicates that at least 59% of the glycolate photorespired is synthesized with the fixation of molecular oxygen. This estimate is certainly conservative owing to the dilution of labeled oxygen at the site of glycolate synthesis by photosynthetic oxygen. We examined the yield of ¹⁸O in glycolate synthesized in vitro by isolated intact spinach chloroplasts in a system which permitted direct sampling of the isotopic composition of the oxygen at the site of synthesis. The isotopic enrichment of glycolate from such experiments was 90 to 95% of that of the oxygen present during the incubation.

The carboxyl oxygens of 3-phosphoglycerate also became labeled with ¹⁸O in 20- and 40-minute feedings with [¹⁸O]oxygen to intact leaves at the CO₂ compensation point. Control experiments indicated that this label was probably due to direct synthesis of 3-phosphoglycerate from glycolate during photorespiration. The mean enrichment of 3-phosphoglycerate was 14 ± 4% of that of glycine or serine, its precursors of the photorespiratory pathway, in 10 separate feeding experiments. It is argued that this constant dilution of label indicates a constant stoichiometric balance between photorespiratory and photosynthetic sources of 3-phosphoglycerate at the CO₂ compensation point.

Oxygen uptake sufficient to account for about half of the rate of ¹⁸O fixation into glycine in the intact leaves was observed with intact spinach chloroplasts. Oxygen uptake and production by intact leaves at the CO₂ compensation point indicate about 1.9 oxygen exchanged per glycolate photorespired. The fixation of molecular oxygen into glycolate plus the peroxisomal oxidation of glycolate to glyoxylate and the mitochondrial conversion of glycine to serine can account for up to 1.75 oxygen taken up per glycolate.

These studies provide new evidence which supports the current formulation of the pathway of photorespiration and its relation to photosynthetic metabolism. The experiments described also suggest new approaches using stable isotope techniques to study the rate of photorespiration and the balance between photorespiration and photosynthesis in vivo.

     

Influence of buffer system and pH on the amount of oxygen exchanged between solvent H2O and the CO2 produced in the aerobic oxidation of Cypridina luciferin catalyzed by Cypridina luciferase.

Incorporation of ¹⁸O into CO₂ was measured under various buffer conditions when the bioluminescent oxidation of Cypridina luciferin, catalyzed by luciferase, was carried out either in H₂¹⁶O medium with ¹⁸O₂ gas, or in H₂¹⁸O medium with ¹⁶O₂ gas. The results indicate that (1) the exchange of oxygen between CO₂ and solvent H₂O is significantly influenced by the kind of buffer as well as by pH, (2) the exchange of oxygen between solvent H₂O and CO₂ produced from luciferin in a neutral buffer can be reasonably well estimated from the exchange that takes place when the same amount of CO₂ gas is introduced into the same buffer by the presently employed method, and (3) in the Cypridina bioluminescent reaction, one of two oxygens of O₂ is quantitatively incorporated into the product CO₂ prior to the exchange of oxygen between CO₂ and solvent H₂O.     

Strong seasonal disequilibrium measured between the oxygen isotope signals of leaf and soil CO2 exchange

The oxygen isotope composition (δ¹⁸O) of atmospheric CO₂ is among a very limited number of tools available to constrain estimates of the biospheric gross CO₂ fluxes, photosynthesis and respiration at large scales. However, the accuracy of the partitioning strongly depends on the extent of isotopic disequilibrium between the signals carried by these two gross fluxes. Chamber‐based field measurements of total CO₂ and CO¹⁸O fluxes from foliage and soil can help evaluate and refine our models of isotopic fractionation by plants and soils and validate the extent and pattern of isotopic disequilibrium within terrestrial ecosystems. Owing to sampling limitations in the past, such measurements have been very rare and covered only a few days. In this study, we coupled automated branch and soil chambers with tuneable diode laser absorption spectroscopy techniques to continuously capture the δ¹⁸O signals of foliage and soil CO₂ exchange in a Pinus pinaster Aït forest in France. Over the growing season, we observed a seasonally persistent isotopic disequilibrium between the δ¹⁸O signatures of net CO₂ fluxes from leaves and soils, except during rain events when the isotopic imbalance became temporarily weaker. Variations in the δ¹⁸O of CO₂ exchanged between leaves, soil and the atmosphere were well explained by theory describing changes in the oxygen isotope composition of ecosystem water pools in response to changes in leaf transpiration and soil evaporation.     

Elevated CO2 and temperature impacts on different components of soil CO2 efflux in Douglas-fir terracosms

Although numerous studies indicate that increasing atmospheric CO₂ or temperature stimulate soil CO₂ efflux, few data are available on the responses of three major components of soil respiration [i.e. rhizosphere respiration (root and root exudates), litter decomposition, and oxidation of soil organic matter] to different CO₂ and temperature conditions. In this study, we applied a dual stable isotope approach to investigate the impact of elevated CO₂ and elevated temperature on these components of soil CO₂ efflux in Douglas-fir terracosms. We measured both soil CO₂ efflux rates and the ¹³C and ¹⁸O isotopic compositions of soil CO₂ efflux in 12 sun-lit and environmentally controlled terracosms with 4-year-old Douglas fir seedlings and reconstructed forest soils under two CO₂ concentrations (ambient and 200 ppmv above ambient) and two air temperature regimes (ambient and 4 °C above ambient). The stable isotope data were used to estimate the relative contributions of different components to the overall soil CO₂ efflux. In most cases, litter decomposition was the dominant component of soil CO₂ efflux in this system, followed by rhizosphere respiration and soil organic matter oxidation. Both elevated atmospheric CO₂ concentration and elevated temperature stimulated rhizosphere respiration and litter decomposition. The oxidation of soil organic matter was stimulated only by increasing temperature. Release of newly fixed carbon as root respiration was the most responsive to elevated CO₂, while soil organic matter decomposition was most responsive to increasing temperature. Although some assumptions associated with this new method need to be further validated, application of this dual-isotope approach can provide new insights into the responses of soil carbon dynamics in forest ecosystems to future climate changes.     

Oxygen Isotope Fractionation during Photosynthesis in a Blue-Green and a Green Alga

Oxygen isotope fractionation (¹⁸O/¹⁶O) at the natural abundance level has been measured during photosynthesis of a blue-green and a green alga. When sufficient attention is paid to removal of contaminating air O₂ before and during the experiments, then the photosynthetic O₂ evolved, as compared to the water O₂, had an average difference of −0.36% for a blue-green alga and −0.80% for a green alga. These experiments suggest that there is no reason to invoke an inverse isotope effect in photosynthesis as part of the explanation for the ¹⁸O enrichment in atmospheric O₂ relative to O₂ in oceanic waters. In addition, in an indirect way, the experiments also support the argument that the bulk of O₂ evolved during photosynthesis comes from water. A 10% contribution of O₂ arising from CO₂ would have been detectable in the present work.     

The Human Enzyme That Converts Dietary Provitamin A Carotenoids to Vitamin A Is a Dioxygenase

β-Carotene 15–15′-oxygenase (BCO1) catalyzes the oxidative cleavage of dietary provitamin A carotenoids to retinal (vitamin A aldehyde). Aldehydes readily exchange their carbonyl oxygen with water, making oxygen labeling experiments challenging. BCO1 has been thought to be a monooxygenase, incorporating oxygen from O₂ and H₂O into its cleavage products. This was based on a study that used conditions that favored oxygen exchange with water. We incubated purified recombinant human BCO1 and β-carotene in either ¹⁶O₂-H₂¹⁸O or ¹⁸O₂-H₂¹⁶O medium for 15 min at 37 °C, and the relative amounts of ¹⁸O-retinal and ¹⁶O-retinal were measured by liquid chromatography-tandem mass spectrometry. At least 79% of the retinal produced by the reaction has the same oxygen isotope as the O₂ gas used. Together with the data from ¹⁸O-retinal-H₂¹⁶O and ¹⁶O-retinal-H₂¹⁸O incubations to account for nonenzymatic oxygen exchange, our results show that BCO1 incorporates only oxygen from O₂ into retinal. Thus, BCO1 is a dioxygenase.     

Mechanism of oxidation of carbon monoxide by bacteria

Double label experiments were performed employing ¹³CO and either H₂¹⁸O or ¹⁸O₂ in the presence of a CO utilizing bacterium. CO₂ generated was trapped and $\text{m}\text{e}$ ratios $\text{47}\text{45}$ showed that the second oxygen atom in the oxidation of CO to CO₂ by this bacterium comes neither from O₂ nor H₂O.     

18O composition of CO2 and H2O ecosystem pools and fluxes in a tallgrass prairie: Simulations and comparisons to measurements

In this paper we describe measurements and modeling of ¹⁸O in CO₂ and H₂O pools and fluxes at a tallgrass prairie site in Oklahoma. We present measurements of the δ¹⁸O value of leaf water, depth‐resolved soil water, atmospheric water vapor, and Keeling plot δ¹⁸O intercepts for net soil‐surface CO₂ and ecosystem CO₂ and H₂O fluxes during three periods of the 2000 growing season. Daytime discrimination against C¹⁸OO, as calculated from measured above‐canopy CO₂ and δ¹⁸O gradients, is also presented. To interpret the isotope measurements, we applied an integrated land‐surface and isotope model (ISOLSM) that simulates ecosystem H₂¹⁸O and C¹⁸OO stocks and fluxes. ISOLSM accurately predicted the measured isotopic composition of ecosystem water pools and the δ¹⁸O value of net ecosystem CO₂ and H₂O fluxes. Simulations indicate that incomplete equilibration between CO₂ and H₂O within C₄ plant leaves can have a substantial impact on ecosystem discrimination. Diurnal variations in the δ¹⁸O value of above‐canopy vapor had a small impact on the predicted δ¹⁸O value of ecosystem water pools, although sustained differences had a large impact. Diurnal variations in the δ¹⁸O value of above‐canopy CO₂ substantially affected the predicted ecosystem discrimination. Leaves dominate the ecosystem ¹⁸O‐isoflux in CO₂ during the growing season, while the soil contribution is relatively small and less variable. However, interpreting daytime measurements of ecosystem C¹⁸OO fluxes requires accurate predictions of both soil and leaf ¹⁸O‐isofluxes.     

Oxygen isotope analysis of bacterial and fungal manganese oxidation

The ability of micro‐organisms to oxidize manganese (Mn) from Mn(II) to Mn(III/IV) oxides transcends boundaries of biological clade or domain. Many bacteria and fungi oxidize Mn(II) to Mn(III/IV) oxides directly through enzymatic activity or indirectly through the production of reactive oxygen species. Here, we determine the oxygen isotope fractionation factors associated with Mn(II) oxidation via various biotic (bacteria and fungi) and abiotic Mn(II) reaction pathways. As oxygen in Mn(III/IV) oxides may be derived from precursor water and molecular oxygen, we use a twofold approach to determine the isotope fractionation with respect to each oxygen source. Using both ¹⁸O‐labeled water and closed‐system Rayleigh distillation approaches, we constrain the kinetic isotope fractionation factors associated with O atom incorporation during Mn(II) oxidation to ?17.3‰ to ?25.9‰ for O₂ and ?1.9‰ to +1.8‰ for water. Results demonstrate that stable oxygen isotopes of Mn(III/IV) oxides have potential to distinguish between two main classes of biotic Mn(II) oxidation: direct enzymatic oxidation in which O₂ is the oxidant and indirect enzymatic oxidation in which superoxide is the oxidant. The fraction of Mn(III/IV) oxide‐associated oxygen derived from water varies significantly (38%–62%) among these bio‐oxides with only weak relationship to Mn oxidation state, suggesting Mn(III) disproportionation may account for differences in the fraction of mineral‐bound oxygen from water and O₂. Additionally, direct incorporation of molecular O₂ suggests that Mn(III/IV) oxides contain a yet untapped proxy of of environmental O₂, a parameter reflecting the integrated influence of global respiration, photorespiration, and several other biogeochemical reactions of global significance.     

34S/32S and 18O/16O Fractionation During Sulfur Disproportionation by Desulfobulbus propionicus

In the present study, coupled stable sulfur and oxygen isotope fractionation during elemental sulfur disproportionation according to the overall reaction: 4H₂O + 4S^? → 3H₂S + SO₄ ^{2 ?} + 2H⁺, was experimentally investigated for the first time using a pure culture of the sulfate reducer Desulfobulbus propionicus at 35^?C. Bacterial disproportionation of elemental sulfur is an important process in the sulfur cycle of natural surface sediments and leads to the simultaneous formation of sulfide and sulfate. A dual-isotope approach considering both sulfur and oxygen isotope discrimination has been shown to be most effective in evaluating specific microbial reactions. The influence of iron- and manganese bearing-solids (Fe(II)CO₃, Fe(III)OOH, Mn(IV)O₂) acting in natural sediments as scavengers for hydrogen sulfide, was considered, too. Disproportionation of elemental sulfur was observed in the presence of iron solids at a cell-specific sulfur disproportionation rate of about 10^{? 9.5± 0.4} μ mol S^? cell^{? 1} h^{? 1}. No disproportionation, however, was observed with MnO₂. In the presence of iron solids, newly formed sulfate was enriched in ¹⁸ O compared to water by about +21‰ (≡ ? _H2O ), in agreement with a suggested oxygen isotope exchange via traces of intra- or extracellular sulfite that is formed as a disproportionation intermediate. Dissolved sulfate was also enriched in ³⁴S compared to elemental sulfur by up to +35%. Isotope fractionation by Desulfobulbus propionicusis highest for all disproportionating bacteria investigated, so far, and may impact on the development of isotope signals at the redox boundary of surface sediments.     

Use of 14C-carboxyl-luciferin in determining the mechanism of the firefly luciferase catalyzed reactions

The use of ¹⁴C-carboxyl-labelled luciferin as a substrate for the firefly luciferase catalyzed reaction produces ¹⁴CO₂ as a product. We have studied this reaction in the presence of ¹⁷O₂ and H¹⁸OH, using an excess of luciferin over luciferase. The initial collection of CO₂ contained close to one oxygen from ¹⁷O₂ for each molecule of ¹⁴CO₂ derived from luciferin, which is consistent with a cyclic peroxide mechanism. About half of the ¹⁴CO₂ remained bound to the enzyme and was collected after acidification of the medium. This CO₂ contained less than 0.1 of an atom of oxygen from ¹⁷O₂ for each molecule of ¹⁴CO₂ derived from luciferin. Exchange of medium CO₂-HCO₃ su? with water was not sufficiently great to account for the loss of any ¹⁷O previously incorporated. The most likely explanation appears to be a preferential exchange of oxygens of enzyme-bound CO₂ with water oxygens. Such exchange, and dilution of CO₂ from luciferin by medium CO₂, may explain previous results in which little incorporation of atmospheric oxygen was noted.     

Exchange of oxygen between solvent H 2 O and the CO 2 produced in Cypridina bioluminescence

Bioluminescent oxidation of $\text{Cypridina}$ luciferin yields CO₂ besides oxyluciferin and light. The exchange of oxygen between the CO₂ and H₂O of the solvent becomes significant when less than approximately 1 μmol of luciferin is reacted in 4 ml of buffer solution, and the exchanged oxygen in CO₂ markedly increases by decreasing the amount of luciferin. Such an exchange is to be expected in any such system which produces CO₂ in aqueous solution, and must be taken into account in interpreting the results of experiments.