The non-tropical coral Cladocora caespitosa as the new climate archive for the Mediterranean: high-resolution (∼weekly) trace element systematics

Montagna, Paolo; McCulloch, Malcolm T.; Mazzoli, Claudio; Silenzi, Sergio; Odorico, Roberto

doi:10.1016/j.quascirev.2006.09.008

Cited by 71 publications

(69 citation statements)

References 86 publications

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“…The boron isotope composition (δ 11 B) of biogenic CaCO 3 (δ 11 B CaCO 3 ) has been primarily used as a paleoceanographic proxy for seawater pH Montagna et al, 2007;Palmer, 1998;Pearson et al, 2009;Penman and Hönisch, 2014;Rae et al, 2011;Trotter et al, 2011;Vengosh et al, 1991;Wei et al, 2009). Boron has a residence time in seawater of ca.…”

Section: Theoretical Model Of δ 11 B Variation With Phmentioning

confidence: 99%

“…Corals are thought to accrete CaCO 3 directly from a discrete calcifying fluid (e.g., Al-Horani et al, 2003;Cohen and Holcomb, 2009;Cohen and McConnaughey, 2003 and references therein; Gaetani and Cohen, 2006;Ries, 2011a), with mineralization sites and crystal orientations being influenced by organic templates and/or calicoblastic cells (e.g., Cuif and Dauphin, 2005;Goldberg, 2001;Meibom et al, 2008;Tambutté et al, 2007). Mollusks are also thought to precipitate their shells from a discrete calcifying fluid between the external epithelium of the mantle and the inner layer of the shell known as the extrapallial fluid (EPF; e.g., Crenshaw, 1972), with hemocytes and organic templates playing a potentially important role in crystal nucleation (e.g., Marie et al, 2012;Mount et al, 2004;Weiner et al, 1984). Coralline red algae are also thought to precipitate primarily high-Mg calcite (HMC) extracellularly but within a chemically controlled fluid bound by adjacent cells.…”

Section: The Role Of Calcification Site Ph In Calcareous Biomineralizmentioning

confidence: 99%

“…4). Oysters construct their shells of LMC (aragonite during the larval stage) from a discrete calcifying fluid known as the extrapallial fluid (e.g., Crenshaw, 1972), with hemocytes and organic templates playing a potentially important role in crystal nucleation (e.g., Marie et al, 2012;Mount et al, 2004;Weiner et al, 1984;Wheeler, 1992;Wilbur and Saleuddin, 1983). The specimens of C. virginica evaluated in this study were grown in seawater conditions (pH SW = 8.2; 25 • C; 32 psu; Table 4) that yield a theoretical seawater δ 11 B B(OH) − 4 of 19.57 ‰, which is 3.54 ‰ greater than δ 11 B CaCO 3 measured for this species.…”

Section: American Oyster (C Virginica)mentioning

confidence: 99%

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δ11B as monitor of calcification site pH in divergent marine calcifying organisms

et al. 2018

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Abstract. The boron isotope composition (δ 11 B) of marine biogenic carbonates has been predominantly studied as a proxy for monitoring past changes in seawater pH and carbonate chemistry. However, a number of assumptions regarding chemical kinetics and thermodynamic isotope exchange reactions are required to derive seawater pH from δ 11 B biogenic carbonates. It is also probable that δ 11 B of biogenic carbonate reflects seawater pH at the organism's site of calcification, which may or may not reflect seawater pH. Here, we report the development of methodology for measuring the δ 11 B of biogenic carbonate samples at the multicollector inductively coupled mass spectrometry facility at Ifremer (Plouzané, France) and the evaluation of δ 11 B CaCO 3 in a diverse range of marine calcifying organisms reared for 60 days in isothermal seawater (25 • C) equilibrated with an atmospheric pCO 2 of ca. 409 µatm. Average δ 11 B CaCO 3 composition for all species evaluated in this study range from 16.27 to 35.09 ‰, including, in decreasing order, coralline red alga Neogoniolithion sp. (35.89 ± 3.71 ‰), temperate coral Oculina arbuscula (24.12 ± 0.19 ‰), serpulid worm Hydroides crucigera (19.26 ± 0.16 ‰), tropical urchin Eucidaris tribuloides (18.71 ± 0.26 ‰), temperate urchin Arbacia punctulata (16.28 ± 0.86 ‰), and temperate oyster Crassostrea virginica (16.03 ‰). These results are discussed in the context of each species' proposed mechanism of biocalcification and other factors that could influence skeletal and shell δ 11 B, including calcifying site pH, the proposed direct incorporation of isotopically enriched boric acid (instead of borate) into biogenic calcium carbonate, and differences in shell/skeleton polymorph mineralogy. We conclude that the large inter-species variability in δ 11 B CaCO 3 (ca. 20 ‰) and significant discrepancies between measured δ 11 B CaCO 3 and δ 11 B CaCO 3 expected from established relationships between abiogenic δ 11 B CaCO 3 and seawater pH arise primarily from fundamental differences in calcifying site pH amongst the different species. These results highlight the potential utility of δ 11 B as a proxy of calcifying site pH for a wide range of calcifying taxa and underscore the importance of using species-specific seawater-pH-δ 11 B CaCO 3 calibrations when reconstructing seawater pH from δ 11 B of biogenic carbonates.

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Section: Theoretical Model Of δ 11 B Variation With Phmentioning

confidence: 99%

Section: The Role Of Calcification Site Ph In Calcareous Biomineralizmentioning

confidence: 99%

Section: American Oyster (C Virginica)mentioning

confidence: 99%

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δ11B as monitor of calcification site pH in divergent marine calcifying organisms

et al. 2018

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“…The boron isotope composition ( 11 B) of biogenic CaCO3 ( 11 BCaCO3) has been primarily used as a palaeoceanographic proxy 40 for seawater pH Montagna et al, 2007;Palmer, 1998;Pearson et al, 2009;Penman and Hönisch, 2014;Rae et al, 2011;Saenger et al, 2013;Trotter et al, 2011;Vengosh et al, 1991;Zinke et al, 2014). Boron has a residence time in seawater of ca.…”

Section: Theoretical Model Of 11 B Variation With Phmentioning

confidence: 99%

δ11B as monitor of calcification site pH in marine calcifying organisms

Sutton

Liu

Ries

et al. 2017

Preprint

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Abstract. The isotope composition of boron (B) in marine biogenic carbonates has been predominantly studied as a proxy 15 for monitoring past changes in seawater pH and carbonate chemistry. In order to derive seawater pH from boron isotope ratio data, a number of assumptions related to chemical kinetics and themodynamic isotope exchange reactions are necessary. Furthermore, the boron isotope composition (

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“…However, currently, only sparse 14 C data are available for the Mediterranean Sea and those are derived from mol-lusk shells with a limited age range (Siani et al 2000;Reimer and McCormac 2002). Recent studies have revealed that the shallow-water zooxanthellate Mediterranean coral Cladocora caespitosa can serve as a reliable archive for seawater temperature and pH reconstructions (Peirano et al 2004;Silenzi et al 2005;Montagna et al 2007Montagna et al , 2008Trotter et al 2011) and thus is a potentially useful archive for 14 C studies.…”

Section: Introductionmentioning

confidence: 99%

A High-Resolution Coral-Based Δ14C Record of Surface Water Processes in the Western Mediterranean Sea

Tisnérat‐Laborde

Montagna

McCulloch³

et al. 2013

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ABSTRACT. The first high-resolution time series of pre-and post-bomb radiocarbon measurements is reported for surface waters in the western Mediterranean Sea. The  14 C record was obtained from the aragonite skeleton of Cladocora caespitosa using a 50-yr-old corallite collected in the Ligurian Sea in 1998. Laser-ablation ICP measurements of trace elements (Li/Mg and Sr/Ca) show a strong seasonal variability, enabling the chronology of the  14 C record to be determined at annual timescales. The mean  14 C of pre-bomb surface water is -56 ± 3‰, corresponding to a reservoir age of 262 ± 29 yr. The postbomb maximum occurs in 1972 with a  14 C value of 90‰, significantly lower than the peak of 150‰ observed in the North Atlantic. The dilution of the peak-amplitude of  14 C in western Mediterranean surface waters is attributed to mixing of North Atlantic Central Water inflow with relatively depleted underlying Intermediate Mediterranean and Levantine Intermediate waters. Intensification of this mixing is observed in 1963-1964, consistent with the change in atmospheric circulation from a positive to negative NAO phase (1960)(1961)(1962)(1963)(1964)(1965)(1966)(1967). The post-peak  14 C variability is relatively limited, reflecting mainly local vertical mixing forced by wind stress.

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The non-tropical coral Cladocora caespitosa as the new climate archive for the Mediterranean: high-resolution (∼weekly) trace element systematics

Cited by 71 publications

References 86 publications

<i>δ</i><sup>11</sup>B as monitor of calcification site pH in divergent marine calcifying organisms

<i>δ</i><sup>11</sup>B as monitor of calcification site pH in divergent marine calcifying organisms

δ<sup>11</sup>B as monitor of calcification site pH in marine calcifying organisms

A High-Resolution Coral-Based Δ14C Record of Surface Water Processes in the Western Mediterranean Sea

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The non-tropical coral Cladocora caespitosa as the new climate archive for the Mediterranean: high-resolution (∼weekly) trace element systematics

Cited by 71 publications

References 86 publications

&lt;i&gt;δ&lt;/i&gt;&lt;sup&gt;11&lt;/sup&gt;B as monitor of calcification site pH in divergent marine calcifying organisms

&lt;i&gt;δ&lt;/i&gt;&lt;sup&gt;11&lt;/sup&gt;B as monitor of calcification site pH in divergent marine calcifying organisms

δ&lt;sup&gt;11&lt;/sup&gt;B as monitor of calcification site pH in marine calcifying organisms

A High-Resolution Coral-Based Δ14C Record of Surface Water Processes in the Western Mediterranean Sea

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<i>δ</i><sup>11</sup>B as monitor of calcification site pH in divergent marine calcifying organisms

<i>δ</i><sup>11</sup>B as monitor of calcification site pH in divergent marine calcifying organisms

δ<sup>11</sup>B as monitor of calcification site pH in marine calcifying organisms