The Atlantic meridional overturning circulation (AMOC) is a system of ocean currents that has an essential role in Earth’s climate, redistributing heat and influencing the carbon cycle1, 2. The AMOC has been shown to be weakening in recent years1; this decline may reflect decadal-scale variability in convection in the Labrador Sea, but short observational datasets preclude a longer-term perspective on the modern state and variability of Labrador Sea convection and the AMOC1, 3,4,5. Here we provide several lines of palaeo-oceanographic evidence that Labrador Sea deep convection and the AMOC have been anomalously weak over the past 150 years or so (since the end of the Little Ice Age, LIA, approximately ad 1850) compared with the preceding 1,500 years. Our palaeoclimate reconstructions indicate that the transition occurred either as a predominantly abrupt shift towards the end of the LIA, or as a more gradual, continued decline over the past 150 years; this ambiguity probably arises from non-AMOC influences on the various proxies or from the different sensitivities of these proxies to individual components of the AMOC. We suggest that enhanced freshwater fluxes from the Arctic and Nordic seas towards the end of the LIA—sourced from melting glaciers and thickened sea ice that developed earlier in the LIA—weakened Labrador Sea convection and the AMOC. The lack of a subsequent recovery may have resulted from hysteresis or from twentieth-century melting of the Greenland Ice Sheet6. Our results suggest that recent decadal variability in Labrador Sea convection and the AMOC has occurred during an atypical, weak background state. Future work should aim to constrain the roles of internal climate variability and early anthropogenic forcing in the AMOC weakening described here.
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Srokosz, M. A. & Bryden, H. L. Observing the Atlantic Meridional Overturning Circulation yields a decade of inevitable surprises. Science 348, 1255575 (2015).
Buckley, M. W. & Marshall, J. Observations, inferences, and mechanisms of the Atlantic Meridional Overturning Circulation: a review. Rev. Geophys. 54, 5–63 (2016).
Jackson, L. C., Peterson, K. A., Roberts, C. D. & Wood, R. A. Recent slowing of Atlantic overturning circulation as a recovery from earlier strengthening. Nat. Geosci. 9, 518–522 (2016).
Robson, J., Hodson, D., Hawkins, E. & Sutton, R. Atlantic overturning in decline? Nat. Geosci. 7, 2–3 (2014).
Yashayaev, I. Hydrographic changes in the Labrador Sea, 1960–2005. Prog. Oceanogr. 73, 242–276 (2007).
Rahmstorf, S. et al. Exceptional twentieth-century slowdown in Atlantic Ocean overturning circulation. Nat. Clim. Change 5, 475–480 (2015); corrigendum 5, 596 (2015).
Hodson, D. L. R. & Sutton, R. T. The impact of resolution on the adjustment and decadal variability of the Atlantic meridional overturning circulation in a coupled climate model. Clim. Dyn. 39, 3057–3073 (2012).
Ortega, P., Robson, J., Sutton, R. T. & Andrews, M. B. Mechanisms of decadal variability in the Labrador Sea and the wider North Atlantic in a high-resolution climate model. Clim. Dyn. 49, 2625–2647 (2016).
Roberts, C. D., Garry, F. K. & Jackson, L. C. A multimodel study of sea surface temperature and subsurface density fingerprints of the Atlantic Meridional Overturning Circulation. J. Clim. 26, 9155–9174 (2013).
Robson, J., Ortega, P. & Sutton, R. A reversal of climatic trends in the North Atlantic since 2005. Nat. Geosci. 9, 513–517 (2016).
Zhang, R. Coherent surface-subsurface fingerprint of the Atlantic meridional overturning circulation. Geophys. Res. Lett. 35, L20705 (2008).
Saba, V. S. et al. Enhanced warming of the Northwest Atlantic Ocean under climate change. J. Geophys. Res. Oceans 121, 118–132 (2016).
McCave, I. N., Thornalley, D. J. R. & Hall, I. R. Relation of sortable silt grain-size to deep-sea current speeds: calibration of the ‘mud current meter’. Deep Sea Res. I Oceanogr. Res. Pap. 127, 1–12 (2017).
Abram, N. J. et al. Early onset of industrial-era warming across the oceans and continents. Nature 536, 411–418 (2016).
Moreno-Chamarro, E., Zanchettin, D., Lohmann, K. & Jungclaus, J. H. An abrupt weakening of the subpolar gyre as trigger of Little Ice Age-type episodes. Clim. Dyn. 48, 727–744 (2017).
Miller, G. H. et al. Abrupt onset of the Little Ice Age triggered by volcanism and sustained by sea-ice/ocean feedbacks. Geophys. Res. Lett. 39, L02708 (2012).
Moffa-Sánchez, P., Hall, I. R., Barker, S., Thornalley, D. J. R. & Yashayaev, I. Surface changes in the eastern Labrador Sea around the onset of the Little Ice Age. Paleoceanography 29, 160–175 (2014).
Moffa-Sanchez, P., Hall, I. R., Thornalley, D. J. R., Barker, S. & Stewart, C. Changes in the strength of the Nordic Seas overflows over the past 3000 years. Quat. Sci. Rev. 123, 134–143 (2015).
Ortega, P. et al. A model-tested North Atlantic Oscillation reconstruction for the past millennium. Nature 523, 71–74 (2015).
Bradley, R. S. & England, J. H. The Younger Dryas and the sea of ancient ice. Quat. Res 70, 1–10 (2008).
Funder, S. et al. A 10,000-year record of Arctic Ocean sea-ice variability—view from the beach. Science 333, 747–750 (2011).
Vincent, W. F., Gibson, J. A. E. & Jeffries, M. O. Ice-shelf collapse, climate change, and habitat loss in the Canadian high Arctic. Polar Rec. 37, 133–142 (2001).
Cabedo-Sanz, P., Belt, S. T., Jennings, A. E., Andrews, J. T. & Geirsdóttir, Á. Variability in drift ice export from the Arctic Ocean to the North Icelandic Shelf over the last 8000 years: a multi-proxy evaluation. Quat. Sci. Rev. 146, 99–115 (2016).
Yang, Q. et al. Recent increases in Arctic freshwater flux affects Labrador Sea convection and Atlantic overturning circulation. Nat. Comm 7, 10525 (2016).
Schulz, M., Prange, M. & Klocker, A. Low-frequency oscillations of the Atlantic Ocean meridional overturning circulation in a coupled climate model. Clim. Past 3, 97–107 (2007).
Polyakov, I. V. et al. Arctic Ocean freshwater changes over the past 100 years and their causes. J. Clim. 21, 364–384 (2008).
Vinje, T. Anomalies and trends of sea-ice extent and atmospheric circulation in the Nordic seas during the period 1864–1998. J. Clim. 14, 255–267 (2001).
Drijfhout, S., Oldenborgh, G. J. V. & Cimatoribus, A. Is a decline of AMOC causing the warming hole above the North Atlantic in observed and modeled warming patterns? J. Clim. 25, 8373–8379 (2012).
Sgubin, G., Swingedouw, D., Drijfhout, S., Mary, Y. & Bennabi, A. Abrupt cooling over the North Atlantic in modern climate models. Nat. Comm 8, 14375 (2017).
Weaver, A. J. et al. Stability of the Atlantic meridional overturning circulation: a model intercomparison. Geophys. Res. Lett. 39, L20709 (2012).
Liu, W., Xie, S.-P., Liu, Z. & Zhu, J. Overlooked possibility of a collapsed Atlantic Meridional Overturning Circulation in warming climate. Sci. Adv. 3, e1601666 (2017).
Drijfhout, S. Competition between global warming and an abrupt collapse of the AMOC in Earth’s energy imbalance. Sci. Rep. 5, 14877 (2015).
Kostov, Y., Armour, K. C. & Marshall, J. Impact of the Atlantic meridional overturning circulation on ocean heat storage and transient climate change. Geophys. Res. Lett. 41, 2108–2116 (2014).
Megann, A. et al. GO5.0: the joint NERC–Met Office NEMO global ocean model for use in coupled and forced applications. Geosci. Model Dev 7, 1069–1092 (2014).
Williams, K. D. et al. The Met Office Global Coupled model 2.0 (GC2) configuration. Geosci. Model Dev 8, 1509–1524 (2015).
Shaffrey, L. C. et al. U.K. HiGEM: the new U.K. high-resolution global environment model—model description and basic evaluation. J. Clim. 22, 1861–1896 (2009).
Bakker, P., Govin, A., Thornalley, D. J. R., Roche, D. M. & Renssen, H. The evolution of deep-ocean flow speeds and δ13C under large changes in the Atlantic overturning circulation: toward a more direct model-data comparison. Paleoceanography 30, 95–117 (2015).
Toole, J. M., Andres, M., Le Bras, I. A., Joyce, T. M. & McCartney, M. S. Moored observations of the Deep Western Boundary Current in the NWAtlantic: 2004–2014. J. Geophys. Res. Oceans 122, 7488–7505 (2017).
Rose, N. L. Spheroidal carbonaceous fly ash particles provide a globally synchronous stratigraphic marker for the Anthropocene. Environ. Sci. Technol. 49, 4155–4162 (2015).
McCave, I. N., Manighetti, B. & Robinson, S. G. Sortable silt and fine sediment size/composition slicing: parameters for palaeocurrent speed and palaeoceanography. Paleoceanography 10, 593–610 (1995).
Dima, M. & Lohmann, G. Evidence for two distinct modes of large-scale ocean circulation changes over the last century. J. Clim. 23, 5–16 (2010).
Muir, L. C. & Fedorov, A. V. How the AMOC affects ocean temperatures on decadal to centennial timescales: the North Atlantic versus an interhemispheric seesaw. Clim. Dyn. 45, 151–160 (2015).
Ortega, P., Robson, J., Moffa-Sanchez, P., Thornalley, D. J. R. & Swingedouw, D. A last millennium perspective on North Atlantic variability: exploiting synergies between models and proxy data. CLIVAR Exch. 72, 61–67 (2017).
McGregor, H. V. et al. Robust global ocean cooling trend for the pre-industrial Common Era. Nat. Geosci. 8, 671–677 (2015).
McCave, I. N. A poisoned chalice? Science 298, 1186–1187 (2002).
Filippova, A., Kienast, M., Frank, M. & Schneider, R. R. Alkenone paleothermometry in the North Atlantic: a review and synthesis of surface sediment data and calibrations. Geochem. Geophys. Geosyst. 17, 1370–1382 (2016).
Marchitto, T. & deMenocal, P. Late Holocene variability of upper North Atlantic Deep Water temperature and salinity. Geochem. Geophys. Geosyst. 4, 1100 (2003).
Keigwin, L. D., Sachs, J. P. & Rosenthal, Y. A. 1600-year history of the Labrador Current off Nova Scotia. Clim. Dyn. 21, 53–62 (2003).
Keigwin, L. D. & Pickart, R. S. Slope water current over the Laurentian Fan on interannual to millennial time scales. Science 286, 520–523 (1999).
Genovesi, L. et al. Recent changes in bottom water oxygenation and temperature in the Gulf of St. Lawrence: micropaleontological and geochemical evidence. Limnol. Oceanogr. 56, 1319–1329 (2011).
Hall, I. R., Boessenkool, K. P., Barker, S., McCave, I. N. & Elderfield, H. Surface and deep ocean coupling in the subpolar North Atlantic during the last 230 years. Paleoceanography 25, PA2101 (2010).
Moffa-Sanchez, P., Born, A., Hall, I. R., Thornalley, D. J. R. & Barker, S. Solar forcing of North Atlantic surface temperature and salinity over the past millennium. Nat. Geosci. 7, 275–278 (2014).
Thornalley, D. J. R., Elderfield, H. & McCave, I. N. Holocene oscillations in temperature and salinity of the surface subpolar North Atlantic. Nature 457, 711–714 (2009).
Richter, T. O., Peeters, F. J. C. & van Weering, T. C. E. Late Holocene (0-2.4 ka BP) surface water temperature and salinity variability, Feni Drift, NE Atlantic Ocean. Quat. Sci. Rev. 28, 1941–1955 (2009).
Morley, A. et al. Solar modulation of North Atlantic central water formation at multidecadal timescales during the late Holocene. Earth Planet. Sci. Lett. 308, 161–171 (2011).
Morley, A., Rosenthal, Y. & deMenocal, P. Ocean-atmosphere climate shift during the mid-to-late Holocene transition. Earth Planet. Sci. Lett. 388, 18–26 (2014).
Sicre, M.-A. et al. A 4500-year reconstruction of sea surface temperature variability at decadal time-scales off North Iceland. Quat. Sci. Rev. 27, 2041–2047 (2008).
Joyce, T. M. & Zhang, R. On the path of the Gulf Stream and the Atlantic Meridional Overturning Circulation. J. Clim. 23, 3146–3154 (2010).
Suman, D. O. & Bacon, M. P. Variations in Holocene sedimentation in the North American Basin determined from 230Th measurements. Deep-Sea Res. 36, 869–878 (1989).
Adkins, J. F., Boyle, E. A., Keigwin, L. & Cortijo, E. Variability of the North Atlantic thermohaline circulation during the last interglacial period. Nature 390, 154–156 (1997).
Hodson, D. L. R., Robson, J. I. & Sutton, R. T. An anatomy of the cooling of the North Atlantic Ocean in the 1960s and 1970s. J. Clim. 27, 8229–8243 (2014).
We thank E. Roosen for help with core sampling; H. Abrams, S. O’Keefe, K. Pietro, L. Owen and F. Pallottino for assistance in processing sediment samples; K. Green for faunal counts in core 10MC; M. Andrews at the UK Met Office for providing the GC2 model data; and S. Rahmstorf for useful suggestions. This work made use of the high-performance computing facilities of ARCHER, which was provided by the University of Edinburgh. Funding was provided from: National Science Foundation (NSF) grant OCE-1304291 to D.W.O., D.J.R.T. and L.D.K.; National Environment Research Council (NERC) Project DYNAMOC grant NE/M005127/1 to P.O. and J.I.R.; the NERC’s Long-Term Science, Multi-Centre (LTSM) North Atlantic Climate System Integrated Study (ACSIS) (to J.I.R.); and the Leverhulme Trust and the ATLAS project (to D.J.R.T.). This project has received funding from the European Union’s Horizon 2020 research and innovation programme under grant agreement 678760 (ATLAS). This paper reflects only the authors’ views and the European Union cannot be held responsible for any use that may be made of the information contained herein.
Nature thanks P. Bakker, S. Rahmstorf, M. Srokosz and the other anonymous reviewer(s) for their contribution to the peer review of this work.
The authors declare no competing interests.
Publisher’s note: Springer Nature remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
Extended data figures and tables
a, 14C and 210Pb dating. The 14C ages (with 1σ ranges; grey, rejected dates) from planktic foraminifera yield a modern core-top age and indicate an average sedimentation rate over the past 1,000 years of 320 cm kyr−1 (dashed line). The presence throughout the core of abundant lithogenic grains in the >150-μm fraction—along with the coarse sortable-silt mean grain size values—suggests that some reworking of foraminifera has probably occurred, resulting in average 14C ages that may be slightly (around 50 years) older than their final depositional age, consistent with the fact that the 210Pb dates do not splice smoothly into the 14C ages (the 14C ages appear slightly too old). The final age model was therefore based on the 210Pb ages for the past century, and was then simply extrapolated back in time using the linear sedimentation rate of 320 cm kyr−1. Given that none of our findings depend on close age control in the older section of this core (that is, before ad 1880), this uncertainty (with converted 14C ages being about 50 years older than the extrapolated linear age model) does not affect our conclusions. b, Left, the age model for the top 80 cm of core 56JPC is based on 210Pb dating of bulk sediment, using the constant initial concentration (CIC) method (rejecting the date at 47 cm, which probably indicates a burrow). A simple two-segment linear fit to the 210Pb dates is adopted (rather than point-to-point interpolation or a spline) because sedimentological evidence—an abrupt increase in the percentage of coarse fraction at 23 cm depth, not observed elsewhere in the core—is indicative of a step change in the sedimentation rate. Horizontal dashed lines denote the depths of the segments at which the sedimentation rate is inferred to change. Centre, further support for the age model of 56JPC over the past century comes from the down-core abundance profile of spheroidal carbonaceous particles (SCPs, derived from high-temperature fossil fuel combustion, counted as described39), which ramped up from the mid to late 1800s and peaked in the 1950s to 1970s (40 cm to 25 cm) before declining over recent decades, consistent with the 210Pb-based age model. Right, the occurrence of 137Cs in the top 40 cm or so of the core is also consistent with the 210Pb-based age of around 1950 at 40 cm. The age uncertainty (1σ) for the past 60 years of the core is estimated at ±2–3 years. We note that the sediment core top is at 3 cm depth in the core-liner. Source data
a, 14C-based age model, derived from linear interpolation of 14C-dated planktic foraminifera (with 1σ ranges) in sediment core KNR-178-48JPC (used for the DWBCLSW sortable-silt reconstruction), yielding a modern core-top age and an average sedimentation rate of around 50 cm kyr−1. We note that the core top is at 3 cm depth in the core-liner. The inset shows the SCP profile for 48JPC on the basis of the 14C age model, confirming the modern age of the top sediments, with SCPs showing the expected profile—increasing in concentration from the late 1800s onwards, peaking at around 1950 to 1970, and declining afterwards. b, Updated age model for core KNR-158-10MC (after ref. 47; used in Extended Data Fig. 5 examining regional near-surface temperature trends in the Northwest Atlantic during the industrial era), using new 210Pb dating (CIC method) for the top 7 cm and rejecting the anomalously old 14C age at 4 cm depth; the inset shows 210Pb age constraints in the top 8 cm. A single detectable occurrence of 137Cs at 2–2.5 cm (equivalent to 1957 on the 210Pb-based age model) can be linked to the bomb peak at 1963, supporting the age model. Also, SCPs were found in the top 5 cm of this core, confirming the industrial-era age for the top 5 cm; however, the low concentrations of SCPs prevent meaningful interpretation of the down-core trends and are not shown. c, Age model for core OCE-326-MC29B (used for Tsub reconstruction of the Northwest Atlantic shelf): 14C ages of planktic foraminifera (with 1σ ranges), from ref. 48. Support for this age model is provided by the SCP concentrations (inset; this study), which show the expected down-core profile39 when plotted using the 14C ages. 210Pb dating48 also suggests a sedimentation rate of around 120 cm kyr−1 for the uppermost sediments, consistent with the 14C ages and SCP profile. Source data
Locations are shown in Fig. 2b. a–c, Temperature proxy records48,49,50 used for the Northwest Atlantic stack (Emerald Basin, Laurentian Fan and Gulf of St Lawrence), where model studies11, 12 indicate that AMOC weakening results in warming of surface and subsurface waters. d–g, Records used to reconstruct Northeast Atlantic SPG subsurface temperatures: d, Gardar drift51; e, combined South Iceland data (Bjorn drift)52, 53; f, Feni drift54; g, Eastern North Atlantic Central Water (ENACW), largely composed of waters formed in the eastern SPG55, 56. h, The high-resolution alkenone sea-surface temperature (SST) record from the North Iceland shelf57 was not included because it is not located within the open North Atlantic SPG (although it does also show, like the other Northeast Atlantic records, that the lowest temperature of the past 1,600 years occurred during the most recent century). Also shown for reference is the Rahmstorf central SPG SST reconstruction (based largely on terrestrial proxies)6.
Extended Data Fig. 4 Different binning and averaging approaches and the residual temperature signal.
a, b, Stacked, normalized proxy temperature data (Tsub) from the Northwest Atlantic shelf/slope (a) and Northeast Atlantic SPG (b). c, The derived Tsub AMOC proxy, calculated as the numerical difference between the stacks shown in a and b. d, The residual temperature variability in stacks a and b that is not described by the (anti-phased dipole) Tsub AMOC proxy shown in c—that is, the in-phase temperature variability common to both stacks, calculated as the numerical sum of the two stacks (if divided by two, this would be the numerical mean). This represents the inferred non-AMOC-related temperature variability common to both regions, and broadly resembles Northern Hemisphere temperature reconstructions, most notably colder residual temperatures during the LIA, around 1350 to 1850. For a–d, black solid lines and squares represent preferred binning (50 years for 1800–2000; 100 years for 400–1800); green line and symbols, as for preferred binning, but with stacks produced by first binning the proxy data at each site and then averaging these binned site values, as opposed to binning all the proxy data together in one step (the former ensures equal weighting for each site, the latter biases the final result to the higher-resolution records); black dashed lines and symbols, 100-year bins offset by 50 years from the preferred bins; grey lines and symbols, 50-year bins (not shown for c and d); blue lines and symbols; 30-year bins for 1790–2000. Error bars for a–d are ±2 s.e. e–g, As for a–c, except using a Monte Carlo approach and published uncertainties for age assignment and temperature reconstructions; light and dark grey shading represent ±1σ and ±2σ, respectively. h, Jackknife version of c, with each line representing the Tsub AMOC proxy but leaving out one of the individual proxy records each time. Source data
a, Modelled SST difference between a weak (negative) and strong (positive) AMOC58. This pattern is model-dependent, with the study cited here58 chosen because of its good agreement with observations of Gulf Stream variability. The locations of cores used for panel b are shown by black stars. b, Percentage abundances of the polar species N. pachyderma (sinistral) in marine sediment cores from the Northwest Atlantic, as an indicator of near-surface (around 75 m) temperatures. A 15% increase indicates around 1 °C of cooling (we note the reversed y axes). The opposing trends over the past 200 years are consistent with the SST pattern modelled for a weakening of the AMOC, as shown in panel a. Data and age models for the cores are: OCE326-MC2948 using the original 14C dating and as shown in Extended Data Fig. 2; OCE326-MC13 and OCE326-MC2549 using the original 14C age ties at the top and bottom of the core and scaling the intervening sedimentation rate to the percentage of CaCO3 content49, 59, 60; KNR158-MC10, this study, using the age model in Extended Data Fig. 2. Source data
a, Top, Tsub AMOC fingerprint11 obtained using empirical orthogonal function (EOF) analysis of the EN4 dataset (light green, the leading mode (EOF1) of Tsub variability from 1993–2003, as defined by Zhang11, applied to the EN4 data; dark green, the second mode of Tsub variability (EOF2) of the North Atlantic for 1900–2015, equivalent to the EOF1 defined for 1993–2003). No substantial twentieth-century AMOC decline is seen in this observation-based reconstruction. Bottom, instrument-based reanalysis of the ‘cold blob’ central SPG region (red; 3-year (thin line) and 11-year (thick line) smoothing; 47° N to 57° N, 30° W to 45° W) used in the Rahmstorf SST AMOC proxy6. The data are from the HadISST project. The reconstructed central SPG SST bears some resemblance to the Tsub AMOC fingerprint record, which is not unexpected given that the central SPG forms a substantial spatial component of the Tsub fingerprint. No clear decrease is shown in the central SPG SST, and the equivalent Rahmstorf AMOC proxy6 (blue; central SPG minus the Northern Hemisphere (NH) temperature) declines during the twentieth century because of the subtraction of the NH warming trend. b, Reconstructed (predominantly terrestrial-based) AMOC proxy (orange; the temperature difference between the central SPG and the NH) and the central SPG SST reconstruction6 (blue). There is a two-step decline in the AMOC proxy, at 1850–1900 and 1950–2000—the former being mainly the result of a strong cooling of the SPG (which probably weakened northward heat transport, paralleling the weakening shown by our DWBC proxy), and the latter being due mainly to subtraction of the strong NH warming trend, rather than a persistent SPG cooling. Source data
a, b, Climatological surface current direction (in arrows) and speed (shaded, m s−1) obtained from the control simulation with HadGEM3-GC2 and the satellite product OSCAR.
a, Correlation (colour bar) of the vertically averaged ocean density (at 1,000–2,500 m) with the DLSD index (as defined in ref. 4; green box, 1,000–2,500 m average) in a 340-year present-day control run of the HiGEM model (see ref. 36). b, Climatology of the modelled meridional ocean velocity (in m s−1) averaged between 30° N and 35° N, illustrating the modelled position of the DWBC. The y axis shows the water depth in metres. c, Cross-correlations between the modelled average DWBC flow speed in the pink box in panel b and indices of DLSD and AMOC at 45° N (the dashed line omits the Ekman component). We note that the box over which the DWBC flow index in panel c is averaged has changed with respect to Fig. 1, in order to take into account of the fact that the return flow is deeper in the HiGEM model than in HadGEM3-GC2.
The model-based DLSD parameter—proposed in ref. 4 and using the EN4 reanalysis dataset—incorporates a larger area and greater depth range than do instrumental-data-only studies, such as ref. 5, which examines past variability in Labrador Sea convection and focuses on the central Labrador Sea and on depths less than 2,000 m, where most observational data are available. The comparison here of DLSD (purple line, three-year mean) from the EN4 dataset with instrumental data on density changes in the central Labrador Sea at 1,500–1,900 m depth (grey line, annual averages; black line, three-year mean) illustrates that the two parameters show very similar variability. Both are dominated by the density changes caused by deep convection in the Labrador Sea, which can reach down to around 2,000 m. Estimates of uncertainty are discussed in ref. 61. Source data
A direct influence of the changing position of the Gulf Stream on the grain size of our core sites can be ruled out by comparing instrumental records of the Gulf Stream position (red, GSI58) with the down-core sortable-silt (SS) mean grain size data in 56JPC (blue; thicker line is three-point smoothed). There is no clear correlation between these two proxies (bottom). However, there is a coupling between our SS data (which represent inferred DWBCLSW flow speed) and density changes in the deep Labrador Sea (grey, annual; black, three-point smoothed; top panel). The 2σ SS error bar (n = 30) is for the three-point mean.
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Thornalley, D.J.R., Oppo, D.W., Ortega, P. et al. Anomalously weak Labrador Sea convection and Atlantic overturning during the past 150 years. Nature 556, 227–230 (2018). https://doi.org/10.1038/s41586-018-0007-4