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Contrasting paired benthic and planktonic foraminifera radiocarbon ages from Bermuda Rise ODP Site 1063 during Heinrich Stadials 1 and 2

Published online by Cambridge University Press:  04 October 2024

Jörg Lippold Open the ORCID record for Jörg Lippold [Opens in a new window] ,
Jens Fohlmeister ,
Lukas Wacker Open the ORCID record for Lukas Wacker [Opens in a new window] ,
Michal Kucera ,
Bernd Kromer  and
Jens Grützner Open the ORCID record for Jens Grützner [Opens in a new window]
Jörg Lippold*
Affiliation:
Institute of Earth Sciences, Heidelberg University, Heidelberg, Germany
Jens Fohlmeister
Affiliation:
Federal Office for Radiation Protection, Berlin, Berlin, Germany Institute for Environmental Physics, Heidelberg University, Heidelberg, Germany
Lukas Wacker
Affiliation:
Laboratory of Ion Beam Physics, ETH Zurich, Zurich, Switzerland
Michal Kucera
Affiliation:
MARUM Center for Marine Environmental Sciences, University of Bremen, Bremen, Germany
Bernd Kromer
Affiliation:
Institute for Environmental Physics, Heidelberg University, Heidelberg, Germany Curt-Engelhorn-Zentrum Archäometrie gGmbH, Mannheim, Germany
Jens Grützner
Affiliation:
Alfred Wegener Institute, Helmholtz-Zentrum für Polar- und Meeresforschung, Bremerhaven, Germany
*
Corresponding author: Jörg Lippold; Email: [email protected]
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Abstract

We report 27 planktonic and 21 benthic radiocarbon ages from the subtropical marine sediment core ODP Site 1063 (Bermuda Rise) for the time range between 30 and 14 ka before present. Despite low abundances of benthic specimens, it was possible to measure radiocarbon ages down to ∼10 µg carbon using a MICADAS and the gas ion source developed at ETH Zurich. Based on a tentative radiocarbon–independent age-model we found that the radiocarbon reservoir of the bottom water varied moderately relative to the analytical and age-model related uncertainties throughout the examined time-period, but larger differences in the radiocarbon reservoir appear to have affected the upper ocean layer. In particular, radiocarbon levels around Heinrich Stadial 2 reveal surface radiocarbon content similar to that of the atmosphere, while during Heinrich Stadial 1 surface waters were significantly depleted in 14C.

Keywords

Heinrich eventsLast Glacial MaximumMarine Isotopic Stage 3North Atlanticventilation 14C ages
Type
Date List
Information
Radiocarbon , Volume 66 , Issue 4 , August 2024 , pp. 816 - 823
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Creative Common License - CCCreative Common License - BY
This is an Open Access article, distributed under the terms of the Creative Commons Attribution licence (https://creativecommons.org/licenses/by/4.0/), which permits unrestricted re-use, distribution and reproduction, provided the original article is properly cited.
Copyright
© The Author(s), 2024. Published by Cambridge University Press on behalf of University of Arizona

Introduction

Ocean Drilling Program (ODP) Site 1063 (33°41´N, 57°37´W) was drilled during ODP Leg 172 at a water depth of 4,584 m (Keigwin et al. Reference Keigwin, Rio and Acton1998) at the Bermuda Rise. The sediment drifts of the Bermuda Rise represent a high-resolution archive of paleoclimatic and paleoceanographic information. Due to sedimentation rates partly exceeding 150 cm/kyr during glacials (Channell et al. Reference Channell, Hodell and Curtis2012) and because the site is bathed by the deepest water masses of the North Atlantic, this region has been intensively studied in particular in terms of reconstructing late Pleistocene deep-water mass geometry and the strength of the Atlantic Meridional Overturning Circulation (Böhm et al. Reference Böhm, Lippold, Gutjahr, Frank and Blaser2015; Deaney et al. Reference Deaney, Barker and van de Flierdt2017; Gutjahr and Lippold, Reference Gutjahr and Lippold2011; Henry et al. Reference Henry, McManus, Curry, Roberts, Piotrowski and Keigwin2016; Jaume-Seguí et al. Reference Jaume-Seguí, Kim, Pena, Goldstein and Knudson2020; Keigwin and Boyle, Reference Keigwin and Boyle2008; Keigwin and Boyle, Reference Keigwin and Boyle2000; Lippold et al. Reference Lippold, Grützner, Winter, Lahaye, Mangini and Christl2009; Lippold et al. Reference Lippold, Pöppelmeier, Süfke, Gutjahr and Goepfert2019; McManus et al. Reference McManus, Francois, Gherardi, Keigwin and Brown-Leger2004; Roberts et al. Reference Roberts, Piotrowski, McManus and Keigwin2010), while paleoceanographic reconstructions from this core location are repeatedly under discussion given the presence of benthic nepheloid layers (Lerner et al. Reference Lerner, Marchal, Lam, Gardner, Richardson and Mishonov2019) and indications for high levels of bioturbation at this drift deposit site (Çağatay et al. Reference Çağatay, Borowski and Ternois2001).

We carried out 14C measurements from co-existing planktonic and benthic foraminifera covering the time period between 30 and 14 ka before present (BP) to examine radiocarbon surface and bottom reservoir effects and to derive the ventilation age of the deep-water masses in the NW Atlantic since the Marine isotopic Stage 3 (MIS3).

Methods

Sediment samples

The examined 27 samples from ODP Site 1063 (Holes B and D) cover the interval from 2.13 to 14.62 meters of composite depth, which previous age models indicated to encompass the time period across Heinrich Events 2 and 1 (Keigwin et al. Reference Keigwin, Rio and Acton1998, Reference Keigwin, Rio and Acton2005). Prior to sampling, depth correlation between Hole D (22 samples) and Hole B (5 samples) has been refined by aligning high resolution magnetic susceptibility records from both holes (Keigwin et al. Reference Keigwin, Rio and Acton2005), such that the selected samples covered the target interval evenly in age. Due to the high sedimentation rate, where accumulated material predominantly contains clays, silts, and nannofossils, and the water depth close to the regional lysocline, only small amounts of carbonate material were available in each sample and we therefore requested large samples, covering 2-cm core slices for analyses. Foraminifera were extracted from the sediment using standard methods (disintegration of sediment in de-ionized water followed by washing over a 0.063 mm sieve and manual picking from the dry-sieved 0.150 mm residue) at the Department for Geosciences, University of Tübingen. For the analysis of surface water radiocarbon ages, monospecific aliquots of the only sufficiently abundant planktonic foraminifera (Globorotalia inflata) were obtained. Other surface dwellers, such as Globigerinoides ruber or Trilobatus sacculifer, occurred in too low abundance only. For the analysis of deep-water radiocarbon ages, assemblages of mixed benthic species (including epifaunal and infaunal species) were sampled and separated. Sample masses of the planktonic foraminifera were between 4 and 37 mg, while benthic samples always yielded less than 1 mg (Table 1).

Table 1. Samples, core depth, sample weight, radiocarbon results and age of foraminifera from ODP Site 1063

AMS

All planktonic foraminifera samples with more than 5 mg were prepared for conventional radiocarbon AMS measurements with solid C targets. The samples were dissolved in 3N HCl under vacuum and dried in a water trap using a dry-ice acetone mixture. The remaining pure CO2 gas is captured with liquid nitrogen and attached to the graphitisation line. Here, the CO2 reacts with H2 to C and H2O at 575°C using an iron catalyst (Alfa Aesar, -325 mesh). The solid C samples were measured at the Klaus Tschira Laboratory for scientific dating (Kromer et al. Reference Kromer, Lindauer, Synal and Wacker2013) against the Oxalic Acid II standard and blank values derived from approximately ∼200 ka old foraminifera from the same marine sediment core. Benthic foraminifera were much less abundant yielding amounts of less than 1 mg CaCO3. Therefore, to determine the radiocarbon content in the scarce benthic species in addition to the contemporaneous planktonic samples, we measured the 14C content of CO2 evolved from the carbonate and directly introduced it to the gas ion source as developed at the AMS lab in Zurich (Wacker et al. Reference Wacker, Lippold, Molnár and Schulz2013a). This method allows analyses using as little as 100–600 μg of carbonate (about 10–60 μg C). A sample of 400 μg carbonate (40 μg C) gives typically a 12C- current of 10–15 μA over 20 minutes and yields a measurement precision of less than 7 ‰ for a modern sample (Wacker et al. Reference Wacker, Fahrni, Hajdas, Molnár, Synal, Szidat and Zhang2013b). All samples were measured against the Oxalic Acid II standard accompanied by measurements of 14C-free ∼200 ka old foraminifera from the same sediment core for blank corrections. Using the gas ion source allows to measure radiocarbon in the CO2 phase and reduces the risk of contamination during sample handling in the conventional AMS method. Nevertheless, measurement errors are generally larger due to the limited sample mass and the reduced ionization probability using the gas ion source compared to the solid target technique. The applicability of the gas ion source has been well addressed in several studies, which compared results of solid targets and the gas ion source of identical carbonate samples (Bard et al. Reference Bard, Tuna, Fagault, Bonvalot, Wacker, Fahrni and Synal2015; Gottschalk et al. Reference Gottschalk, Szidat, Michel, Mazaud and Salazar2018; Molnár et al. Reference Molnár, Mészáros, Janovics, Major and Hubay2021; Wacker et al. Reference Wacker, Lippold, Molnár and Schulz2013a).

Tentative 14 C-independent age model

We refined the available age model for ODP Site 1063 for the examined time period (Böhm et al. Reference Böhm, Lippold, Gutjahr, Frank and Blaser2015; Grützner et al. Reference Grützner, Giosan, Franz, Tiedemann and Cortijo2002) by tuning XRF derived CaCO3 content of the sediment to the δ18O signal of Greenland NGRIP ice core (Andersen et al. Reference Andersen, Azuma, Barnola, Bigler and Biscaye2004). As both records reflect a Daansgard/Oeschger event (DO) like behaviour in their signals with the ice core being well dated in the period of interest by annual layer counting, we use the prominent DO pattern to derive an absolute age for ODP Site 1063. We identified DO events between 40 and 15 ka BP in ODP Site 1063 sediment properties, allowing a millennial-resolution age tuning. For the time interval between 36 and 10 ka we identified 12 tuning points, hence one tuning point per approximately 2200 a (Figure 1, Table 2). We set the tuning points preferentially to the start and end-points of DO-events, and thus mark identical time stamps in both records, on which the tuning is based. Here, we assume, that there is no significant lag in the CaCO3 content of ODP Site 1063 compared to the δ18O signal from NGRIP (Buizert et al. Reference Buizert, Adrian, Ahn, Albert and Alley2015), as fine scale variations (< 200 a) are recorded consistently in both archives. In order to improve our decision in setting the tuning points, we applied a Monte Carlo algorithm (Fohlmeister, Reference Fohlmeister2012), which varies all tuning points within its given uncertainties to maximize the correlation between the ice core data and the elemental composition of the sediment core. Thus, we assume an age error of 0.2 ka for the absolute ages, i.e. the subjectively chosen tie points where optimised by an objective statistical method. The assumed age error of 0.2 ka is accounted for in the resulting radiocarbon reservoir ages (in addition to the 14C analytical uncertainties). Even if the variations in NGRIP δ18O and ODP Site 1063 CaCO3 content did not occur simultaneously, a potential lagging mechanism must have been rather constant and small as the shape of the DO events is maintained during the sedimentation process, potentially resulting only in minor reservoir age offsets. Nonetheless, we note that the alignment of the variations in sedimentary CaCO3 to the δ18O of NGRIP is based on the assignment of wiggles and may therefore represent only one out of other possible age-depth realisations.

Table 2. List of used tie points for the age model construction

Figure 1. Alignment of the CaCO3 profile from ODP site 1063 (Keigwin et al. Reference Keigwin, Rio and Acton2005) to the δ18O profile of the NGRIP ice core (Andersen et al. Reference Andersen, Azuma, Barnola, Bigler and Biscaye2004). Red triangles denote position of tie points used for the age-model tuning. Blue symbols indicate positions of 14C-measurements of benthic (crosses) and planktonic (circles) foraminifera for this study.

Results

We report 27 planktonic and 21 benthic radiocarbon ages and thus 21 benthic-planktonic (B-P) ventilation ages from ODP Site 1063 in the time range between 30 and 14 ka BP (Table 1).

The B-P ages in our study vary from a range between –120 to 5000 14C-years with an average of 1500. The bulk of the data falls within a broad band of values between 330 and 1990 14C-years. The temporal variations within this band might not be subject to fine-scale interpretation given the analytical uncertainties introduced largely by the benthic measurements and the relatively coarse resolution of our 14C samples.

Discussion and conclusions

Deviating from the majority of our data three values stand out with very large (5000 and 3600 14C-years) or very small (–120 14C-years) B-P ages. Both the small negative B-P age around 17.4 ka BP (close to the onset of Heinrich Stadial 1), which would suggest the same water mass origin for the near-surface and the bottom water at this site, and the old B-P ages at 26.1 and 27.4 ka BP (before Heinrich Stadial 2), potentially indicating near-surface and bottom water masses of very different origin, are not reflected by the surrounding B-P ages of our record. We cannot exclude the possibility that such features might have been introduced by bioturbation or transport of allochthonous tests albeit the high sedimentation rate (on average ∼90 cm/ka) suggests this process to have a limited effect throughout the core. In particular, the three observed very high or very low B-P ages are not exclusively associated with high or low sedimentation rates. In support of these more extreme values representing real B-P differences, there is 14C-based evidence for similar fast and strong ventilation changes from various other Atlantic bottom water locations (e.g., data compilation by Rafter et al. Reference Rafter, Gray, Hines, Burke and Costa2022) within the time range between 25 and 15 ka BP.

Based on our tentative 14C-independent age model we calculated the radiocarbon surface reservoir age by comparing the 14C results of the planktonic species with the contemporaneous atmospheric value for the (14C-independent) site-specific chronology. The radiocarbon surface reservoir is a measure for the interaction of old deep-water masses with water at the surface or the intensification of exchange between deep and surface waters. In addition, we calculated the radiocarbon difference between the benthic foraminifera and atmospheric values. The benthic radiocarbon offset gives an information on how long the deep water mass was separated from the atmosphere (Skinner and Bard Reference Skinner and Bard2022). When considering the analytical uncertainties and assuming that our 14C-independent age model is correct, we found that based on our benthic results the radiocarbon reservoir of the bottom water was on average 2400 +/–800 14C-years and varied little throughout the examined time-period. In contrast, derived from the planktonic data we found larger relative differences in the radiocarbon reservoir at the surface (1040 +/–910 14C-years, Table 2, Figure 2). In particular, surface water radiocarbon levels around Heinrich Stadial 2 nearly reach those of the atmosphere, whereas during Heinrich Stadial 1 the surface waters were significantly depleted in 14C. These differences between both prominent Northern Hemisphere cold events require further research (Bauska et al. Reference Bauska, Marcott and Brook2021; Shuttleworth et al. Reference Shuttleworth, Bostock, Chalk, Calvo and Jaccard2021), since deep ocean circulation proxies (e.g. 231Pa/230Th, εNd) indicate similar conditions for both cold events (Gutjahr and Lippold Reference Gutjahr and Lippold2011; Lippold et al. Reference Lippold, Grützner, Winter, Lahaye, Mangini and Christl2009; McManus et al. Reference McManus, Francois, Gherardi, Keigwin and Brown-Leger2004; Roberts et al. Reference Roberts, Piotrowski, McManus and Keigwin2010). Surface water radiocarbon content around Heinrich Stadial 2 indicates a good ventilation and equilibration of surface waters with the atmosphere. This implies a relatively strong stratification of surface waters preventing old, carbon rich bottom waters from upwelling. In contrast to Heinrich Stadial 2, Heinrich Stadial 1 surface waters seem not to have experienced such stratification. The high variability of the B-P ages at ODP Site 1063 and the deviating observations for Heinrich Stadial 2 and 1 are not in agreement with interpretation of other paleocirculation proxies from the Bermuda Rise (Gutjahr and Lippold Reference Gutjahr and Lippold2011; Lippold et al. Reference Lippold, Grützner, Winter, Lahaye, Mangini and Christl2009; McManus et al. Reference McManus, Francois, Gherardi, Keigwin and Brown-Leger2004; Roberts et al. Reference Roberts, Piotrowski, McManus and Keigwin2010) and might be related not purely to oceanographic explanations. It is possible that the planktonic signal may not represent the surface mixed layer, because the analysed planktonic species G. inflata is known to add a significant portion of the shell calcite within the thermocline (van Raden et al. Reference van Raden, Groeneveld, Raitzsch and Kucera2011). However, it is unlikely that the depth habitat of the species changed significantly between the two Heinrich Events (Jonkers et al. Reference Jonkers, Gopalakrishnan, Weßel, Chiessi and Groeneveld2021). Another process potentially capable of influencing the apparent 14C age of a sediment horizon is bioturbation, in particular during times of variability in the abundances of different species. Bioturbational mixing of tests out of abundance maxima into older or younger sediment layers can result in apparent isotopic gradients between different species (Löwemark et al. Reference Löwemark, Konstantinou and Steinke2008). However, the high sedimentation rate at this site and the clear manifestation of DO-cycles in the sedimentary record argue against a crucial role of bioturbation.

Figure 2. Decay-corrected (Δ14C) for the atmosphere (black solid line, IntCal2020; Reimer et al. Reference Reimer, Austin, Bard, Bayliss and Blackwell2020) in comparison with the radiocarbon content measured in planktonic (red ellipses) and benthic (blue ellipses) foraminifera. Error ellipses denote 95% confidence intervals. Cyan rectangles denote the approximate timing of Heinrich Stadials 1 and 2 as derived from peaks in sedimentary 231Pa/230Th from the Bermuda Rise (Lippold et al. Reference Lippold, Grützner, Winter, Lahaye, Mangini and Christl2009; McManus et al. Reference McManus, Francois, Gherardi, Keigwin and Brown-Leger2004).

Nevertheless, this data set reports high variability in radiocarbon levels during the coldest period of the last glacial cycle. This observation may provide helpful information for future studies on past ventilation changes of the Atlantic Ocean.

Acknowledgments

The authors thank the IODP Core Repository in Bremen for providing sample material, Margret Bayer and Hartmut Schulz for support in the lab and Julia Gottschalk for discussions. We thank the Deutsche Forschungsgemeinschaft (DFG) for funding this study via grants FO809/1-1 and LI1815/4-2.

References

Andersen, KK, Azuma, N, Barnola, JM, Bigler, M, Biscaye, P, et al. (2004) High-resolution record of Northern Hemisphere climate extending into the last interglacial period. Nature 431(7005), 147–151.Google ScholarPubMed
Bard, E, Tuna, T, Fagault, Y, Bonvalot, L, Wacker, L, Fahrni, S and Synal, H-A (2015) AixMICADAS, the accelerator mass spectrometer dedicated to 14C recently installed in Aix-en-Provence, France. Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with Materials and Atoms 361, 80–86.CrossRefGoogle Scholar
Bauska, TK, Marcott, SA and Brook, EJ (2021) Abrupt changes in the global carbon cycle during the last glacial period. Nature Geoscience 14(2), 91–96.CrossRefGoogle Scholar
Böhm, E, Lippold, J, Gutjahr, M, Frank, M, Blaser, P, et al. (2015) Strong and deep Atlantic meridional overturning circulation during the last glacial cycle. Nature 517, 73–76.CrossRefGoogle ScholarPubMed
Buizert, C, Adrian, B, Ahn, J, Albert, M, Alley, RB, et al. (2015) Precise interpolar phasing of abrupt climate change during the last ice age. Nature 520(7549), 661–665.Google Scholar
Çağatay, MN, Borowski, WS, Ternois, YG (2001) Factors affecting the diagenesis of Quaternary sediments at ODP Leg 172 sites in western North Atlantic: evidence from pore water and sediment geochemistry. Chemical Geology 175, 467–484.CrossRefGoogle Scholar
Channell, JET, Hodell, DA and Curtis, J (2012) ODP Site 1063 (Bermuda Rise) revisited: Oxygen isotopes, excursions and paleointensity in the Brunhes Chron. Geochemistry Geophysics Geosystems 13(1).CrossRefGoogle Scholar
Deaney, EL, Barker, S and van de Flierdt, T (2017) Timing and nature of AMOC recovery across Termination 2 and magnitude of deglacial CO2 change. Nature Communications 8, 14595.CrossRefGoogle Scholar
Fohlmeister, J (2012) A statistical approach to construct composite climate records of dated archives: Quaternary Geochronology 14, 48–56.CrossRefGoogle Scholar
Gottschalk, J, Szidat, S, Michel, E, Mazaud, A, Salazar, G, et al. (2018) Radiocarbon measurements of small-size foraminiferal samples with the Mini Carbon Dating System (MICADAS) at the University of Bern: implications for paleoclimate reconstructions. Radiocarbon 60(2), 1–23.CrossRefGoogle Scholar
Grützner, J, Giosan, L, Franz, SO, Tiedemann, R, Cortijo, E, et al. (2002) Astronomical age models for Pleistocene drift sediments from the western North Atlantic (ODP Sites 1055-1063). Marine Geology 189, 5–23.CrossRefGoogle Scholar
Gutjahr, M and Lippold, J (2011) Early arrival of Southern Source Water in the deep North Atlantic prior to Heinrich event 2. Paleoceanography 26, PA2101.CrossRefGoogle Scholar
Henry, LG, McManus, JF, Curry, WB, Roberts, NL, Piotrowski, AM and Keigwin, LD (2016) North Atlantic ocean circulation and abrupt climate change during the last glaciation. Science 353(6298), 470–474.CrossRefGoogle ScholarPubMed
Jaume-Seguí, M, Kim, J, Pena, L, Goldstein, S and Knudson, K, et al. (2020) Distinguishing Glacial AMOC and Interglacial non–AMOC Nd Isotopic Signals in the Deep Western Atlantic over the last 1 Myr. Paleoceanography and Paleoclimatology 12(12), e2020PA003877.Google Scholar
Jonkers, L, Gopalakrishnan, A, Weßel, L, Chiessi, CM and Groeneveld, J, et al. (2021) Morphotype and crust effects on the geochemistry of Globorotalia inflata . Paleoceanography and Paleoclimatology 36(4), e2021PA004224.CrossRefGoogle Scholar
Keigwin, D and Boyle, E (2008) Did North Atlantic overturning halt 17,000 years ago?: Paleoceanography 23, PA1101.CrossRefGoogle Scholar
Keigwin, L and Boyle, E (2000) Detecting Holocene changes in thermohaline circulation. Proceedings of the National Academy of Sciences 97(4), 1343–1346.CrossRefGoogle ScholarPubMed
Keigwin, L, Rio, D, Acton, G, et al. (1998) Bermuda Rise and Sohm abyssal plain, Sites 1063 and 1064. Proceedings of the Ocean Drilling Program, Initial Reports 172.Google Scholar
Keigwin, LD, Rio, D, Acton, GD and Shipboard Scientific (2005) Magnetic susceptibility on ODP Hole 172-1063B. PANGAEA. https://doi.org/10.1594/PANGAEA.266175.CrossRefGoogle Scholar
Kromer, B, Lindauer, S, Synal, H-A and Wacker, L (2013) MAMS–a new AMS facility at the Curt-Engelhorn-Centre for Achaeometry, Mannheim, Germany. Nuclear Instruments and Methods in Physics Research Section B: Beam Interactions with Materials and Atoms 294, 11–13.CrossRefGoogle Scholar
Lerner, P, Marchal, O, Lam, PJ, Gardner, W, Richardson, MJ, and Mishonov, A (2019) A model study of the relative influences of scavenging and circulation on 230Th and 231Pa in the western North Atlantic: Deep Sea Research Part I. Oceanographic Research Papers 155, 103159.CrossRefGoogle Scholar
Lippold, J, Grützner, J, Winter, D, Lahaye, Y, Mangini, A and Christl, M (2009) Does sedimentary 231Pa/230Th from the Bermuda Rise monitor past Atlantic Meridional Overturning Circulation? Geophysical Research Letters 36, L12601.CrossRefGoogle Scholar
Lippold, J, Pöppelmeier, F, Süfke, F, Gutjahr, M, Goepfert, TJ, et al. (2019) Constraining the variability of the Atlantic Meridional Overturning Circulation during the Holocene. Geophysical Research Letters 46(20), 11338–11346.CrossRefGoogle Scholar
Löwemark, L, Konstantinou, K and Steinke, S (2008) Bias in foraminiferal multispecies reconstructions of paleohydrographic conditions caused by foraminiferal abundance variations and bioturbational mixing: A model approach. Marine Geology 256(1–4), 101–106.CrossRefGoogle Scholar
McManus, J, Francois, R, Gherardi, J, Keigwin, L and Brown-Leger, S (2004) Collapse and rapid resumption of Atlantic meridional circulation linked to deglacial climate change. Nature 428, 834–837.CrossRefGoogle Scholar
Molnár, M, Mészáros, M, Janovics, R, Major, I, Hubay, K, et al. (2021) Gas ion source performance of the environmicadas at Hekal Laboratory, Debrecen, Hungary. Radiocarbon 63(2), 499–511.CrossRefGoogle Scholar
Rafter, PA, Gray, WR, Hines, SKV, Burke, A, Costa, KM, et al. (2022) Global reorganization of deep-sea circulation and carbon storage after the last ice age. Science Advances 8(46), eabq5434.CrossRefGoogle ScholarPubMed
Reimer, PJ, Austin, WEN, Bard, E, Bayliss, A, Blackwell, PG, et al. (2020) The IntCal20 Northern Hemisphere radiocarbon age calibration curve (0–55 cal kBP). Radiocarbon 62(4), 725–757.CrossRefGoogle Scholar
Roberts, N, Piotrowski, A, McManus, J and Keigwin, L (2010) Synchronous deglacial overturning and water mass source changes. Science 327, 75–78.CrossRefGoogle ScholarPubMed
Shuttleworth, R, Bostock, HC, Chalk, TB, Calvo, E, Jaccard, SL, et al. (2021) Early deglacial CO2 release from the Sub-Antarctic Atlantic and Pacific oceans. Earth and Planetary Science Letters 554, 116649.CrossRefGoogle Scholar
Skinner, LC and Bard, E (2022) Radiocarbon as a dating tool and tracer in palaeoceanography. Reviews of Geophysics 60(1).CrossRefGoogle Scholar
van Raden, UJ, Groeneveld, J, Raitzsch, M and Kucera, M (2011) Mg/Ca in the planktonic foraminifera Globorotalia inflata and Globigerina bulloides from Western Mediterranean plankton tow and core top samples. Marine Micropalaeontology 78, 3–4.CrossRefGoogle Scholar
Wacker, L, Lippold, J, Molnár, M and Schulz, H (2013a) Towards single-foraminifera-dating with a gas ion source. Nuclear Instruments and Methods in Physics Research B 294, 307–310.CrossRefGoogle Scholar
Wacker, LS, Fahrni, SM, Hajdas, I, Molnár, M, Synal, H-A, Szidat, S and Zhang, YL (2013b) A versatile gas interface for routine radiocarbon analysis with a gas ion source. Nuclear Instruments and Methods in Physics Research B 294, 315–319.CrossRefGoogle Scholar
Figure 0

Table 1. Samples, core depth, sample weight, radiocarbon results and age of foraminifera from ODP Site 1063

Figure 1

Table 2. List of used tie points for the age model construction

Figure 2

Figure 1. Alignment of the CaCO3 profile from ODP site 1063 (Keigwin et al. 2005) to the δ18O profile of the NGRIP ice core (Andersen et al. 2004). Red triangles denote position of tie points used for the age-model tuning. Blue symbols indicate positions of 14C-measurements of benthic (crosses) and planktonic (circles) foraminifera for this study.

Figure 3

Figure 2. Decay-corrected (Δ14C) for the atmosphere (black solid line, IntCal2020; Reimer et al. 2020) in comparison with the radiocarbon content measured in planktonic (red ellipses) and benthic (blue ellipses) foraminifera. Error ellipses denote 95% confidence intervals. Cyan rectangles denote the approximate timing of Heinrich Stadials 1 and 2 as derived from peaks in sedimentary 231Pa/230Th from the Bermuda Rise (Lippold et al. 2009; McManus et al. 2004).