Oxygen isotope composition of modern and archaeological otoliths from the estuarine hardhead catfish (Ariopsis felis) and their potential to record low-latitude climate change

Surge, Donna; Walker, Karen

doi:10.1016/j.palaeo.2005.03.051

Cited by 53 publications

(37 citation statements)

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“…metabolic water | isotope probing | phosphate oxygen isotopes M etabolic water, more precisely defined as an isotopically distinct flux of O (and H) produced during metabolism (1), has been studied extensively as an alternative water source contributing to body water in animals, such as desert mammals, insects, and migrating birds (2-6), but does not easily lend itself to direct measurement. In recent years, interest in metabolic water has been extended to its oxygen isotopic composition ( 18 O/ 16 O ratio or δ 18 O value) and contribution to body water because this information is crucial to the interpretation of biomineral [e.g., carbonate-CaCO 3 -and phosphate-Ca 3 (PO 4 ) 2 ] oxygen isotopic compositions used heavily in paleoclimate/paleohydrological research (7)(8)(9)(10)(11)(12)(13)(14). This includes biomineral shells of aquatic marine organisms that are preserved in the geologic record and used to infer Earth's climate history (15)(16)(17)(18)(19).…”

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confidence: 99%

Probing the metabolic water contribution to intracellular water using oxygen isotope ratios of PO ₄

Wang

et al. 2016

Proc. Natl. Acad. Sci. U.S.A.

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Knowledge of the relative contributions of different water sources to intracellular fluids and body water is important for many fields of study, ranging from animal physiology to paleoclimate. The intracellular fluid environment of cells is challenging to study due to the difficulties of accessing and sampling the contents of intact cells. Previous studies of multicelled organisms, mostly mammals, have estimated body water composition-including metabolic water produced as a byproduct of metabolism-based on indirect measurements of fluids averaged over the whole organism (e.g., blood) combined with modeling calculations. In microbial cells and aquatic organisms, metabolic water is not generally considered to be a significant component of intracellular water, due to the assumed unimpeded diffusion of water across cell membranes. Here we show that the 18 O/ 16 O ratio of PO 4 in intracellular biomolecules (e.g., DNA) directly reflects the O isotopic composition of intracellular water and thus may serve as a probe allowing direct sampling of the intracellular environment. We present two independent lines of evidence showing a significant contribution of metabolic water to the intracellular water of three environmentally diverse strains of bacteria. Our results indicate that ∼30-40% of O in PO 4 comprising DNA/biomass in early stationary phase cells is derived from metabolic water, which bolsters previous results and also further suggests a constant metabolic water value for cells grown under similar conditions. These results suggest that previous studies assuming identical isotopic compositions for intracellular/extracellular water may need to be reconsidered. metabolic water | isotope probing | phosphate oxygen isotopes M etabolic water, more precisely defined as an isotopically distinct flux of O (and H) produced during metabolism (1), has been studied extensively as an alternative water source contributing to body water in animals, such as desert mammals, insects, and migrating birds (2-6), but does not easily lend itself to direct measurement. In recent years, interest in metabolic water has been extended to its oxygen isotopic composition ( 18 O/ 16 O ratio or δ 18 O value) and contribution to body water because this information is crucial to the interpretation of biomineral [e.g., carbonate-CaCO 3 -and phosphate-Ca 3 (PO 4 ) 2 ] oxygen isotopic compositions used heavily in paleoclimate/paleohydrological research (7)(8)(9)(10)(11)(12)(13)(14). This includes biomineral shells of aquatic marine organisms that are preserved in the geologic record and used to infer Earth's climate history (15)(16)(17)(18)(19).A core assumption of applications of biomineral oxygen isotopic compositions to infer environmental conditions is that the 18 O: 16 O ratio is controlled by exchange of oxygen isotopes between oxyanions comprising the biomineral and ambient water in bodily fluids (i.e., body water) (9,(20)(21)(22)(23)(24). In multicellular eukaryotic organisms, body water includes all water found in various body compartments (...

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confidence: 99%

Probing the metabolic water contribution to intracellular water using oxygen isotope ratios of PO ₄

Wang

et al. 2016

Proc. Natl. Acad. Sci. U.S.A.

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“…Stable isotopic signatures in the otoliths (ear stones) of marine fishes are often linked to water mass properties, and as with other biogenic carbonates, chemical information contained in these structures has been used to reconstruct past climates and environmental conditions (Gao and Beamish 1999;Surge and Walker 2005). Temperature, salinity, and ambient ocean isotope concentration have all been linked to changes in otolith d 13 C and d 18 O (Kalish 1991;Thorrold et al 1997;Elsdon and Gillanders 2002), and can lead to variability of otolith isotope signatures within and across years.…”

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confidence: 99%

Interdecadal variation in seawater d13C and d18O recorded in fish otoliths

Schloesser

Rooker

Louchuoarn

et al. 2009

Limnology & Oceanography

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Stable carbon (d 13 C) and oxygen (d 18 O) in the otolith cores of Atlantic bluefin tuna (Thunnus thynnus) vary temporally, with changes that quantitatively follow interdecadal variation in atmospheric and oceanic reservoirs. Both carbon and oxygen isotopic signatures vary significantly by year of birth over the range investigated , with d 13 C decreasing and d 18 O increasing (22.56 3 10 22 % and 4.3 3 10 23 % yr 21 , respectively). The rate of change in otolith d 13 C was similar to reported rates of atmospheric d 13 C depletion, attributed to deforestation and the burning of fossil fuels (referred to as the Suess effect), suggesting a close link between atmospheric and oceanic carbon pools. Increases in otolith d 18 O were evident but less pronounced, with observed variation possibly attributable to changing salinity in the Atlantic Ocean. Otolith cores of bluefin tuna effectively track interdecadal trends and record past seawater d 13 C and d 18 O.Atmospheric and oceanic (seawater) reservoirs of stable carbon (d 13 C) and oxygen (d 18 O) isotopes are known to fluctuate over time because of natural and anthropogenic processes (Quay et al. 1992;Delaygue et al. 2000). Over the last century, atmospheric d 13 C has decreased significantly because of increased inputs of isotopically light carbon from both the burning of fossil fuels and the reduction of forest and soil carbon reservoirs (the Suess effect; Verburg 2007). This effect has accelerated in recent decades and translates into parallel shifts in animal tissue d 13 C within terrestrial (Bump et al. 2007) and aquatic ecosystems, with decreasing d 13 C detected in producers (phytoplankton; Bauch et al. 2000) and low-level consumers (sponges; Druffel and Benavides 1986). Still, shifts in d 13 C are seldom studied beyond the base of the food web, and no link to the Suess effect has been documented in marine vertebrates. Similarly, atmospheric and oceanic d 18 O reservoirs appear to be coupled (Jouzel et al. 2002), and carbonates precipitated in equilibrium with these reservoirs are affected by ambient concentrations as well as physicochemical conditions (Kim and O'Neil 1997;Thorrold et al. 1997 Thorrold et al. 1997;Elsdon and Gillanders 2002), and can lead to variability of otolith isotope signatures within and across years. Although otolith composition is also regulated by metabolic and physiological processes (Radtke et al. 1987;Kalish 1991), these properties still yield consistent isotope signatures in otolith cores over annual time periods, justifying their use as natural tracers for specific water masses (Kerr et al. 2007;Rooker et al. 2008). Given the potential usefulness of otolith d 13 C and d 18 O for historical reconstructions (i.e., climate, physicochemical) and as natural tracers, evaluating the temporal variability of these signatures over decadal periods is critically needed.Here, we examined temporal variation in d 13 C and d 18 O in the otolith cores (representing the first year of life) of a pelagic fish, Atlantic bluefin tuna (Thunnus ...

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“…6) are close to those for alkenones in Chesapeake Bay water in the salinity range 10-28 (Schwab and Sachs, 2011), the range of salinity in Charlotte Harbor estuary today (e.g. Miller and McPherson, 1991;Surge and Walker, 2005). Since there are no experimental data for C 36:2 ethyl ketones, it is not possible to directly calculate corresponding salinity values.…”

Section: Discussionmentioning

confidence: 57%

Unusual C35 to C38 alkenones in mid-Holocene sediments from a restricted estuary (Charlotte Harbor, Florida)

Soelen

Lammers

Eglinton

et al. 2014

Organic Geochemistry

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Unusual C 35 to C 38 alkenones were identified in mid-Holocene (8-3.5 kyr BP) sediments from a restricted estuary in southwest Florida (Charlotte Harbor). The distribution was dominated by a C 36 diunsaturated (ω15,20) ethyl ketone, identical to the one present in Black Sea Unit 2 sediments. Other unusual alkenones were tentatively assigned as a C 35:2 (ω 15,20) methyl ketone, a C 37:2 (ω 17,22) methyl ketone and a C 38:2 (ω 17,22) ethyl ketone. In late Holocene sediments < 3.5 kyr BP, the common C 37 to C 39 alkenones were found. Compound-specific 14 C, 13 C, and D isotope measurements were used to constrain the possible origin of the alkenones. Conventional radiocarbon ages of alkenones and higher plant-derived long chain n-alcohols indicated no significant difference in age between mid-Holocene alkenones and higher plant n-alcohols. Both alcohols and alkenones were offset vs. calibrated ages of shell fragments in the same sediment core, which suggests they were pre-aged by 500-800 yr, implying resuspension and redistribution of the fine-grained sedimentary particles with which they are associated. The hydrogen isotopic (δD) composition (-190‰ to -200‰) of the C 37 and C 38 alkenones in the late Holocene sediments is in line with values for coastal haptophytes in brackish water. However, the unusual C 36 and C 38 alkenones from the mid Holocene sediments were enriched in D (by ca. 100‰) vs. the late Holocene alkenones. Also, δ 13 C values of mid-Holocene alkenones were consistently offset compared with late Holocene alkenones (-21‰ to -22‰ and -22‰ to -23‰, respectively). We suggest that the alkenones in Charlotte Harbor were produced by unknown alkenone-producing haptophyte.

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Oxygen isotope composition of modern and archaeological otoliths from the estuarine hardhead catfish (Ariopsis felis) and their potential to record low-latitude climate change

Cited by 53 publications

References 24 publications

Probing the metabolic water contribution to intracellular water using oxygen isotope ratios of PO ₄

Probing the metabolic water contribution to intracellular water using oxygen isotope ratios of PO ₄

Interdecadal variation in seawater d13C and d18O recorded in fish otoliths

Unusual C35 to C38 alkenones in mid-Holocene sediments from a restricted estuary (Charlotte Harbor, Florida)

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Oxygen isotope composition of modern and archaeological otoliths from the estuarine hardhead catfish (Ariopsis felis) and their potential to record low-latitude climate change

Cited by 53 publications

References 24 publications

Probing the metabolic water contribution to intracellular water using oxygen isotope ratios of PO 4

Probing the metabolic water contribution to intracellular water using oxygen isotope ratios of PO 4

Interdecadal variation in seawater d13C and d18O recorded in fish otoliths

Unusual C35 to C38 alkenones in mid-Holocene sediments from a restricted estuary (Charlotte Harbor, Florida)

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Probing the metabolic water contribution to intracellular water using oxygen isotope ratios of PO ₄

Probing the metabolic water contribution to intracellular water using oxygen isotope ratios of PO ₄