Chemical Hydrography of the South Atlantic During the Last Glacial Maximum: Cd vs. δ13C

Boyle, E.; Rosenthal, Yair

doi:10.1007/978-3-642-80353-6_23

Cited by 96 publications

(85 citation statements)

References 41 publications

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“…The ''treated'' powder subsamples were exposed to a mixture of H 2 O 2 and NaOH and then leached with a weak HNO 3 solution according to methods outlined for cleaning foraminifera for Mg/Ca [Boyle and Keigwin, 1985;Boyle and Rosenthal, 1996]. This treatment is similar to Mitsuguchi et al's [2001] suggestion for cleaning coral for Mg/Ca, with the exception that the oxidation step is buffered.…”

Section: Methodsmentioning

confidence: 99%

Impact of skeletal dissolution and secondary aragonite on trace element and isotopic climate proxies in Porites corals

et al. 2007

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[1] Restricted zones of recent dissolution and secondary aragonite infilling were identified in a coral core collected in 1986 from a living massive Porites colony from the central Great Barrier Reef, Australia. Secondary aragonite needles, !20 mm long, cover skeletal surfaces deposited from 1972 to late 1974 and increase bulk density by 10%. Dissolution is observed above this zone, whereas older skeleton is pristine. We investigate the impact of both types of early marine diagenesis on skeletal geochemistry and coral paleoclimate reconstructions by comparison with similar records from eight contemporary Porites colonies collected at nearby reefs. Secondary aragonite overgrowth causes anomalies in skeletal density, Mg/Ca, Sr/Ca, U/Ca, d Dissolution, through incongruent leaching, also causes cool SST artifacts but only for trace element ratios (Mg/Ca-SST À1.2°C; Sr/Ca-SST À1.2°C; U/Ca-SST À2.1°C). The sequence of preference with respect to dissolution of coral skeleton in seawater is Mg > Ca > Sr > U. Rigorous screening of coral material for paleoclimate reconstructions is therefore necessary to detect both dissolution and the presence of secondary minerals. The excellent agreement between apparent SST anomalies generated by different modes of diagenesis means that replication of tracers within a single coral cannot be used to validate climate-proxy interpretations. Poor replication of records between different coral colonies, however, provides a strong indication of nonclimatic artifacts such as dissolution and secondary aragonite.

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Section: Methodsmentioning

confidence: 99%

Impact of skeletal dissolution and secondary aragonite on trace element and isotopic climate proxies in Porites corals

et al. 2007

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“…Sample intervals were decreased to 1-1.5 cm, corresponding to 0.01-0.5ky time steps, at the Last Glacial Maximum (LGM) and in Heinrich events. Core M16004 was sampled at 5-10 cm intervals, corresponding to time steps of 2-5kyr; in core sections Ocean Cd and nutrient budgets have been reasonably stable on glacial-interglacial timescales [Boyle, 1992;Boyle and Rosenthal, 1996], so that it is not immediately obvious how a potential increase in Cd during Heinrich events should have been generated there. Taking the Heinrich event CdW':ti13C proxy coordinates at face value and using mean glacial Cd:ti13C end-member signals of AAIW and UNADW for comparison (Figure 3a), the position of Heinrich event proxy coordinates suggests that North Atlantic middepth water masses during the meltwater events consisted of >60% of Southern Hemisphere waters.…”

Section: All Isotope Values Are Referred To the Peedee Belemnite (Pdb)mentioning

confidence: 99%

Upper ocean circulation in the glacial North Atlantic from benthic foraminiferal isotope and trace element fingerprinting

Willamowski¹

2000

Paleoceanography

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“…We have completed a series of oxygen and carbon isotope analyses on foraminifera from GPC-5 using standard techniques in the interval 1980-2380 cm. In addition, across one of the interstadial/stadial oscillations in each of the cores we have measured Cd/Ca in benthic foraminifera using standard techniques [Boyle and Rosenthal, 1996]. According to an existing age model for this We also find very rare but consistently present specimens of the polar planktonic foraminifer Neogloboquadrina pachyderma (s.) in the samples containing the ice-rafted grains.…”

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confidence: 98%

Surface and deep ocean variability in the northern Sargasso Sea during marine isotope stage 3

Keigwin¹,

Boyle²

1999

Paleoceanography

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Abstract. New geochemical proxy data from Bermuda Rise piston cores reveal ocean and climate conditions in the northern Sargasso Sea during marine isotope stage 3. Using fi180 on the planktonic foraminifer Globigerinoides ruber, we can correlate explicitly with every stadial/interstadial change in Greenland ice between -32 and 58 ka. These data suggest repetitive changes of-4øC in the annual average sea surface temperature (SST), with maximum cooling comparable to or greater than SST during glacial maximum conditions. The extent of SST depression is about the same for typical stadial events and for Heinrich events 4 and 5, which we have identified on the Bermuda Rise by traces of ice rafting.

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Chemical Hydrography of the South Atlantic During the Last Glacial Maximum: Cd vs. δ13C

Cited by 96 publications

References 41 publications

Impact of skeletal dissolution and secondary aragonite on trace element and isotopic climate proxies in Porites corals

Impact of skeletal dissolution and secondary aragonite on trace element and isotopic climate proxies in Porites corals

Upper ocean circulation in the glacial North Atlantic from benthic foraminiferal isotope and trace element fingerprinting

Surface and deep ocean variability in the northern Sargasso Sea during marine isotope stage 3

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