Factors determining δ13C and δ18O fractionation in aragonitic otoliths of marine fish

Thorrold, Simon R.; Campana, Steven E.; Jones, Cynthia M.; Swart, Peter K.

doi:10.1016/s0016-7037(97)00141-5

Cited by 323 publications

(374 citation statements)

References 37 publications

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“…However, our estimated values of δ c -δ w are consistent with previous studies on different fish species carried out in laboratory conditions (Kalish 1991b, Thorrold et al 1997, Gao et al 2001, Høie et al 2004b). All those investigations concluded that deposition occurs at or near equilibrium in fish otoliths.…”

Section: Environmental Influences On Hake Recruits and Juvenilessupporting

confidence: 92%

Environmental influences on the recruitment process inferred from otolith stable isotopes in Merluccius merluccius off the Balearic Islands

Hidalgo¹,

Tomás²,

Høie³

et al. 2008

Aquat. Biol.

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Oxygen (δ 18 O) and carbon (δ 13 C) isotope ratios in sagittal otoliths were analysed in recruits and juveniles of European hake Merluccius merluccius L. caught in the northwest (Sóller, SO) and south (Cabrera, CA) of the Island of Mallorca (western Mediterranean) over 2 consecutive years (2003 and 2004). The analytical method used allowed data to be gathered on both environmental and trophic conditions experienced by fish during the pelagic early life stages (registered in the composition of the inner part of the otolith, core area) and the demersal aggregations of recruits (at the otolith edge). Results on the seasonal variation of oxygen isotope signatures at the edge of fish otoliths captured in SO and CA indicated different vertical migration behaviours of hake between the bottom and the thermocline. δ 13 C showed a clear ontogenetic pattern between the core area and the edge, confirming the differences in diet from the early stages to post-recruits. The seasonal analysis of δ 13 C data from the otolith edge indicated that fish from the early stages in June 2003 encountered poorer trophic resources, which resulted in poor fish condition and subsequent poorer recruitment. The estimated temperature from the core area of otoliths showed lower temperature regimes in the 2002 hatching season compared to the 2003 hatching season, which could be a possible explanation for the observed differences in success of subsequent recruitment.

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Section: Environmental Influences On Hake Recruits and Juvenilessupporting

confidence: 92%

Environmental influences on the recruitment process inferred from otolith stable isotopes in Merluccius merluccius off the Balearic Islands

Hidalgo¹,

Tomás²,

Høie³

et al. 2008

Aquat. Biol.

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“…1), corresponding to an approximate 1.51% depletion in d 13 C over the 59-yr period investigated . Despite the ability of physicochemical factors (i.e., temperature and salinity) to affect seawater d 13 C (Thorrold et al 1997;Elsdon and Gillanders 2002), they do not appear linked to the observed decadal shift in otolith d 13 C. Changes in oceanic temperature and salinity have been documented over the approximate time period analyzed (1950s-1990s). The largest mean temperature anomaly was found to be 0.37uC for the 0-300-m-depth layer of the North Atlantic Ocean (Levitus et al 2000).…”

Section: Resultsmentioning

confidence: 86%

“…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).…”

mentioning

confidence: 99%

“…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. 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).…”

mentioning

confidence: 99%

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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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“…8), carbonate mineralogy (e.g. aragonite versus calcite, Tarutani et al, 1969;Romanek et al, 1992;Patterson et al, 1993;Thorrold et al, 1997;White et al, 1999;Böhm et al, 2000;Lécuyer et al, 2004) and to kinetic effects due to fast degassing and high precipitation rates or in-stream biological activity, organic matter degradation (Andrews and Riding, 2000;Fouke et al, 2000;Andrews, 2006), pH and temperature of precipitation (Deocampo, 2010;Swart, 2015). Carbon and oxygen stable isotope signatures can thus be valuable archives of paleoenvironmental, and -climatic variations with seasonal, annual or decadal resolution (Fairchild et al, 2006;Kawai et al, 2009;Tanner, 2010;Renaut et al, 2013;Frantz et al, 2014), especially when records of different deposits (e.g.…”

mentioning

confidence: 99%

What do we really know about early diagenesis of non-marine carbonates?

Boever

Brasier

Foubert

et al. 2017

Sedimentary Geology

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Non-marine carbonate rocks including cave, spring, stream, calcrete and lacustrine-palustrine sediments, are susceptible to early diagenetic processes. These can profoundly alter the carbonate fabric and affect paleoclimatic proxies. This review integrates recent insights into diagenesis of non-marine carbonates and in particular the variety of early diagenetic processes, and presents a conceptual framework to address them. With ability to study at smaller and smaller scales, down to nanometers, one can now observe diagenesis taking place the moment initial precipitates have formed, and continuing thereafter. Diagenesis may affect whole rocks, but it typically starts in nano-and micro-environments. The potential for diagenetic alteration depends on the reactivity of the initial precipitate, commonly being metastable phases like vaterite, Ca-oxalates, hydrous Mg-carbonates and aragonite with regard to the ambient fluid. Furthermore, organic compounds commonly play a crucial role in hosting these early transformations. Processes like neomorphism (inversion and recrystallization), cementation and replacement generally result in an overall coarsening of the fabric and homogenization of the wide range of complex, primary microtextures. If early diagenetic modifications are completed in a short time span compared to the (annual to millennial) time scale of interest, then recorded paleoenvironmental signals and trends could still acceptably reflect original, depositional conditions. However, even compact, non-marine carbonate deposits may behave locally and temporarily as open systems to crystal-fluid exchange and overprinting of one or more geochemical proxies is not unexpected. Looking to the future, relatively few studies have examined the behaviour of promising geochemical records, such as clumped isotope thermometry and (non-conventional) stable isotopes, in well-constrained diagenetic settings. Ongoing and future in-vitro and in-situ experimental approaches will help to investigate and detangle sequences of intermediate, diagenetic products, processes and controls, and to quantify rates of early diagenesis, bridging a gap between nanoscale, molecular lab studies and the fossil field rock record of non-marine carbonates.

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Factors determining δ13C and δ18O fractionation in aragonitic otoliths of marine fish

Cited by 323 publications

References 37 publications

Environmental influences on the recruitment process inferred from otolith stable isotopes in Merluccius merluccius off the Balearic Islands

Environmental influences on the recruitment process inferred from otolith stable isotopes in Merluccius merluccius off the Balearic Islands

Interdecadal variation in seawater d13C and d18O recorded in fish otoliths

What do we really know about early diagenesis of non-marine carbonates?

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