Anomalous carbon isotope fractionation between atmospheric CO2 and dissolved inorganic carbon induced by intense photosynthesis

Herczeg, Andrew L.; Fairbanks, Richard G.

doi:10.1016/0016-7037(87)90102-5

Cited by 131 publications

(75 citation statements)

References 22 publications

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“…Above pH values of 8 to 9, there was a trend of decreasing isotopic signature for the literature survey data. This may be due to chemically enhanced diffusion of CO 2 and its associated fractionation, as was suggested to be the case in Mohonk Lake (Herczeg and Fairbanks 1987).…”

Section: Interaction Of Metabolism and Geochemical Variables-mentioning

confidence: 83%

“…Several studies have used DIC stable isotopes to understand the carbon cycle of individual lakes by tracking change in the isotope signature through time (Quay et al 1986;Herczeg 1987;Stiller and Nissenbaum 1999). Few studies have examined ␦ 13 C-DIC for a broad range of lakes to determine the causes and importance of the variation among lakes.…”

Section: Introductionmentioning

confidence: 99%

“…Indeed, studies have observed summer increases in epilimnetic ␦ 13 C-DIC as a result of increases in productivity (Herczeg 1987;Hollander and McKenzie 1991;Wang and Veizer 2000). Respiration is generally considered to be the reason for declining ␦ 13 C-DIC in the hypolimnion during the stratified season (Quay et al 1986;Miyajima et al 1997).…”

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confidence: 99%

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Controls of δ¹³C‐DIC in lakes: Geochemistry, lake metabolism, and morphometry

Bade

Carpenter

Cole

et al. 2004

Limnology & Oceanography

166

141

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We investigated ␦ 13 carbon (C)-dissolved inorganic carbon (DIC) values in 72 lakes from diverse regions using literature data as well as new measurements for 32 lakes. ␦ 13 C-DIC varied broadly among lakes from Ϫ31 to ϩ2.6‰. This variation of surface-water ␦ 13 C-DIC among lakes is greater than the seasonal variation within most lakes. Several statistical models account for a large portion of the interlake variation and indicate that geochemical (e.g., DIC, pH, alkalinity) and morphometric (area) variables are important, whereas biological (e.g., gross primary productivity [GPP], respiration [R], chlorophyll a) variables are generally not significant. A process-based model including gas exchange with the atmosphere, inorganic carbon speciation, and ecosystem metabolism was also constructed. The model provides a reasonable fit to the data for lakes, in which respiration exceeded GPP (heterotrophic lakes; 75% of lakes sampled). Lakes for which GPP exceeded respiration (autotrophic) were not fit well by the process-based model. The data and models indicate that metabolism creates substantial variation in ␦ 13 C-DIC around the potential ␦ 13 C-DIC that is set by geochemical factors of the watershed.Stable isotope analysis of dissolved inorganic carbon (DIC) has become an important tool for understanding the movement and fate of carbon (C) in lake ecosystems. Several studies have used DIC stable isotopes to understand the carbon cycle of individual lakes by tracking change in the isotope signature through time (Quay et al. 1986;Herczeg 1987;Stiller and Nissenbaum 1999). Few studies have examined ␦ 13 C-DIC for a broad range of lakes to determine the causes and importance of the variation among lakes. Early reports suggested that the possible range of ␦ 13 C-DIC values could be between Ϫ21‰ and 0‰ (Degens 1969). Striegl et al. (2001) compared DIC isotope signatures of 142 lakes during ice cover and concluded that lakes with higher partial pressure of CO 2 (pCO 2 ) had lower ␦ 13 C-DIC values as a result of the dominance of respiration of terrestrial organic material.The ratio of 13 C to 12 C in DIC is influenced by several major processes that alter the input or output of either isotope. Inputs include atmospheric CO 2 , respiration of organic

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Section: Interaction Of Metabolism and Geochemical Variables-mentioning

confidence: 83%

Section: Introductionmentioning

confidence: 99%

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Controls of δ¹³C‐DIC in lakes: Geochemistry, lake metabolism, and morphometry

Bade

Carpenter

Cole

et al. 2004

Limnology & Oceanography

166

141

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“…High inorganic carbon loadings of inflowing rivers and groundwater inputs may sustain the CO 2 excess (McDonald et al, 2013) and govern the δ 13 C DIC . Moreover, CO 2 water-air exchange reactions may have modified δ 13 C DIC values because of isotope fractionation during water-air exchange, in particular at high pH/low CO 2 values (Herczeg and Fairbanks, 1987;Bade et al, 2004;Bontes et al, 2006).…”

Section: A De Kluijver Et Al: Stable Carbon Isotopes In Lakesmentioning

confidence: 99%

Stable carbon isotope biogeochemistry of lakes along a trophic gradient

et al. 2014

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Abstract. The stable carbon (C) isotope variability of dissolved inorganic and organic C (DIC and DOC), particulate organic carbon (POC), glucose and polar-lipid derived fatty acids (PLFAs) was studied in a survey of 22 North American oligotrophic to eutrophic lakes. The δ 13 C of different PLFAs were used as proxy for phytoplankton producers and bacterial consumers. Lake pCO 2 was primarily determined by autochthonous production (phytoplankton biomass), especially in eutrophic lakes, and governed the δ 13 C of DIC. All organic-carbon pools showed overall higher isotopic variability in eutrophic lakes (n = 11) compared to oligomesotrophic lakes (n = 11) because of the high variability in δ 13 C at the base of the food web (both autochthonous and allochthonous carbon). Phytoplankton δ 13 C was negatively related to lake pCO 2 over all lakes and positively related to phytoplankton biomass in eutrophic lakes, which was also reflected in a large range in photosynthetic isotope fractionation (ε CO 2 −phyto , 8-25 ‰). The carbon isotope ratio of allochthonous carbon in oligo-mesotrophic lakes was rather constant, while it varied in eutrophic lakes because of maize cultivation in the watershed.

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“…5). During intense photosynthesis, the water becomes depleted in dissolved CO 2 (Herczeg & Fairbanks 1987). When this occurs, CO 2 enters water from the atmosphere.…”

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confidence: 99%

Stable isotope composition of Chara rudis incrustation in Lake Jasne, Poland

et al. 2010

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Stable isotope composition (d 13 C and d18 O) was analysed in mineral incrustation of Chara rudis and surrounding waters. This macroalga forms dense and extensive charophyte meadows and may significantly contribute to the calcium carbonate precipitation and deposition of marl lake sediments. The study aimed to find out if charophyte calcium carbonate was precipitated in an isotopic equilibrium with lake water and if the precipitation was related to the environmental conditions. Two apical internodes of 10 individuals of C. rudis were collected monthly between June and late October 2008 at three permanent study sites (1.0 m, 1.5 m and 2.0 m deep) in a small (15.1 ha) and shallow (mean depth: 4.3 m) mid-forest lake with extensively developed charophyte meadows (Lake Jasne, mid-Western Poland). Basic physical-chemical analyses were performed at each study site, and water samples for further laboratory determinations, including stable isotope analyses, were collected from the above searched C. rudis stands and, simultaneously, at three comparative sites in the macrophyte-free pelagial. The difference in d 13 C between incrustation and water from above C. rudis exceeded 2% V-PDB at each site. In the case of d 18 O, it exceeded 2% between July and September. Accordingly, it is postulated that calcium carbonate was not precipitated in an isotopic equilibrium with lake water. Incrustation was enriched in heavier carbon isotope, 13 C, and water was enriched in 18 O. d 13 C of incrustation and DIC were positively correlated, whereas negative relation 18 O of incrustation and water. Several dependencies were found with water chemistry above the plants. The content of mineral incrustation in Chara dry weight had negative influence on the d 18 O but not on the d 13 C. Community depth, structure and PVI had no effect. No significant differences appeared between isotope composition in the pelagic zone and Chara stands.

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Anomalous carbon isotope fractionation between atmospheric CO2 and dissolved inorganic carbon induced by intense photosynthesis

Cited by 131 publications

References 22 publications

Controls of δ¹³C‐DIC in lakes: Geochemistry, lake metabolism, and morphometry

Controls of δ¹³C‐DIC in lakes: Geochemistry, lake metabolism, and morphometry

Stable carbon isotope biogeochemistry of lakes along a trophic gradient

Stable isotope composition of Chara rudis incrustation in Lake Jasne, Poland

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Anomalous carbon isotope fractionation between atmospheric CO2 and dissolved inorganic carbon induced by intense photosynthesis

Cited by 131 publications

References 22 publications

Controls of δ13C‐DIC in lakes: Geochemistry, lake metabolism, and morphometry

Controls of δ13C‐DIC in lakes: Geochemistry, lake metabolism, and morphometry

Stable carbon isotope biogeochemistry of lakes along a trophic gradient

Stable isotope composition of Chara rudis incrustation in Lake Jasne, Poland

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Controls of δ¹³C‐DIC in lakes: Geochemistry, lake metabolism, and morphometry

Controls of δ¹³C‐DIC in lakes: Geochemistry, lake metabolism, and morphometry