Oxygen-Isotope Analysis of Recent Tropical Pacific Benthonic Foraminifera

Smith, Patsy Beckstead; Emiliani, Cesare

doi:10.1126/science.160.3834.1335

Cited by 13 publications

(6 citation statements)

References 2 publications

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“…The dissolution process of the host organism could modify the chemistry of the ambient seawater in a limited area around the foraminifera (Toyofuku et al, 2017), although this process is hard to imagine in an environment (cold-water coral reef) that relies on constant water movement to provide nutrients to the main inhabitants (Mienis et al, 2007). As such, we suggest it is more likely that the dissolved material is transported through the cytoplasm to the calcification site (Spero, 1988;Erez, 2003), although further work is required to confirm this.…”

Section: Mixing Modelmentioning

confidence: 84%

Host-influenced geochemical signature in the parasitic foraminifera <i>Hyrrokkin sarcophaga</i>

et al. 2021

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Abstract. Hyrrokkin sarcophaga is a parasitic foraminifera that is commonly found in cold-water coral reefs where it infests the file clam Acesta excavata and the scleractinian coral Desmophyllum pertusum (formerly known as Lophelia pertusa). Here, we present measurements of the trace element and isotopic composition of these parasitic foraminifera, analyzed by inductively coupled optical emission spectrometry (ICP-OES), electron probe microanalysis (EPMA) and mass spectrometry (gas-source MS and inductively-coupled-plasma MS). Our results reveal that the geochemical signature of H. sarcophaga depends on the host organism it infests. Sr / Ca ratios are 1.1 mmol mol−1 higher in H. sarcophaga that infest D. pertusum, which could be an indication that dissolved host carbonate material is utilized in shell calcification, given that the aragonite of D. pertusum has a naturally higher Sr concentration compared to the calcite of A. excavata. Similarly, we measure 3.1 ‰ lower δ13C and 0.25 ‰ lower δ18O values in H. sarcophaga that lived on D. pertusum, which might be caused by the direct uptake of the host's carbonate material with a more negative isotopic composition or different pH regimes in these foraminifera (pH can exert a control on the extent of CO2 hydration/hydroxylation) due to the uptake of body fluids of the host. We also observe higher Mn / Ca ratios in foraminifera that lived on A. excavata but did not penetrate the host shell compared to specimen that penetrated the shell, which could be interpreted as a change in food source, changes in the calcification rate, Rayleigh fractionation or changing oxygen conditions. While our measurements provide an interesting insight into the calcification process of this unusual foraminifera, these data also indicate that the geochemistry of this parasitic foraminifera is unlikely to be a reliable indicator of paleoenvironmental conditions using Sr / Ca, Mn / Ca, δ18O or δ13C unless the host organism is known and its geochemical composition can be accounted for.

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Section: Mixing Modelmentioning

confidence: 84%

Host-influenced geochemical signature in the parasitic foraminifera <i>Hyrrokkin sarcophaga</i>

et al. 2021

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“…Many of the species showing a tendency toward isotopic equilibrium occupy the oxygen minimum layers of the eastern Pacific (Smith and Emiliani, 1968;Dunbar and Wefer, 1984;Grossman, 1984a) and the eastem Atlantic (Ganssen, 1983), including many buliminaceans. Perhaps the same traits that enable species to inhabit inhospitable low oxygen environments also bring about equilibrium precipitation of tests.…”

Section: Vital Effect and Foraminiferal Ecologymentioning

confidence: 99%

Stable isotopes in modern benthic foraminifera; a study of vital effect

Grossman¹

1987

The Journal of Foraminiferal Research

176

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Fundamental to the application of stable isotopes in paleoenvironmental studies is an understanding of the processes influencing the isotopic composition of biogenic carbonate. This paper examines carbon and oxygen isotopic equilibrium in foraminiferal calcite and aragonite, and the characteristics and causes of disequilibria (i.e., vital effect).The major cause of vital effect appears to be incorporation of metabolic carbon-oxygen compounds into the test. Furthermore, a relationship is observed between isotopic "behavior" and environment. Taxa that tolerate low oxygen conditions, such as buliminaceans and cassidulinaceans, tend to precipitate their tests in oxygen isotopic equilibrium with the water. Discorbaceans, which generally occur in oxygenated environments, tend to exhibit vital effect.The 613C of Uvigerina, Cassidulina spp., and Planulina wuellerstorfi reflects the isotopic composition of the ambient dissolved inorganic carbon (DIC) of bottom waters. Carbon isotopic compositions of certain benthic foraminifera, such as Globobulimina spp., record the chemistry of pore waters rather than bottom waters. Isotopic fractionation between the aragonitic Hoeglundina and ambient DIC shows a temperature dependence of -0.1 1% per "C. No temperature dependence is observed in the carbon isotopic fractionation of Uvigerina spp.

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“…A large number of publications on Cenozoic palaeoclimates and palaeoceanography using stable isotopic data on foraminifers have appeared, but whether foraminifers secrete the test in equilibrium with the ambient sea-water has not yet been resolved. Various observations suggest deposition in equilibrium (Smith &Emiliani 1968) to near equilibrium (Savin et al 1975;Berger et al 1981) and out of equilibrium (Vinot-Bertouille & Duplessy 1973;Erez 1978). Studies on Recent larger foraminifers have shown that the oxygen isotopic ratios are either close to expected equilibrium values (Luz et al 1983), or, despite the biological fractionation, they are chiefly the function of surface-water temperatures and record the seasonal variations (Wefer & Berger 1980;Wefer et al 1981).…”

Section: Limitationsmentioning

confidence: 97%

Palaeogene isotopic temperatures of western India

Saraswati

Ramesh

Navada

1993

LET

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Oxygen isotopic measurements of larger benthic foraminifers from western India suggest that the Palaeogene temperature varied between 22deg;C and 32deg;C in this region. The warm climate of the Palaeocene and the Early Eocene, hovering around 32°C, deteriorated in late Middle Eocene (corresponding to planktic zones P13‐P14) when the temperature dropped by 6deg;C. With progressive cooling through the Late Eocene, the temperature reached 22deg;C during Early Oligocene times. The cooling trend set in the Middle Eocene seems to have been terminated towards the end of the Palaeogene when the temperature rose to 25°C. □Palaeotemperature, Palaeogene, oxygen isotopes, larger foraminifiers, India.

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Oxygen-Isotope Analysis of Recent Tropical Pacific Benthonic Foraminifera

Cited by 13 publications

References 2 publications

Host-influenced geochemical signature in the parasitic foraminifera <i>Hyrrokkin sarcophaga</i>

Host-influenced geochemical signature in the parasitic foraminifera <i>Hyrrokkin sarcophaga</i>

Stable isotopes in modern benthic foraminifera; a study of vital effect

Palaeogene isotopic temperatures of western India

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Oxygen-Isotope Analysis of Recent Tropical Pacific Benthonic Foraminifera

Cited by 13 publications

References 2 publications

Host-influenced geochemical signature in the parasitic foraminifera &lt;i&gt;Hyrrokkin sarcophaga&lt;/i&gt;

Host-influenced geochemical signature in the parasitic foraminifera &lt;i&gt;Hyrrokkin sarcophaga&lt;/i&gt;

Stable isotopes in modern benthic foraminifera; a study of vital effect

Palaeogene isotopic temperatures of western India

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Resources

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Host-influenced geochemical signature in the parasitic foraminifera <i>Hyrrokkin sarcophaga</i>

Host-influenced geochemical signature in the parasitic foraminifera <i>Hyrrokkin sarcophaga</i>