Abstract
The Dansgaard–Oeschger (DO) events, as observed in oxygen isotope ratios from the North Greenland Ice Core Project (NGRIP) record, are an outstanding example of past abrupt climate transitions. Their physical cause remains debated, and previous research indicated that they are not preceded by classical earlywarning signals (EWS). Subsequent research hypothesized that the DO events are caused by bifurcations of physical mechanisms operating at decadal timescales, and proposed to search for EWS in the highfrequency fluctuation levels. Here, a time series with 5year resolution is obtained from the raw NGRIP record, and significant numbers of EWS in terms of variance and autocorrelation increases are revealed in the decadalscale variability. Wavelet analysis indicates that the EWS are most pronounced in the 10–50year periodicity band, confirming the above hypothesis. The DO events are hence neither directly noiseinduced nor purely externally forced, which provides valuable constraints regarding potential physical causes.
Introduction
The last glacial interval, which lasted roughly from 110 to 12 kyears before 2000 AD (b2k), experienced abrupt climatic transitions at millennial timescales, which are called Dansgaard–Oeschger (DO) events^{1,2,3}. They manifest themselves most concisely in time series of oxygen isotope ratios (δ^{18}O) and dust concentrations retrieved from Greenland ice core records^{3,4}, yet their impact is noticeable in different archives across the globe. The DO events are characterized by rapid, decadalscale transitions of δ^{18}O from Greenland stadial (GS) to Greenland interstadial (GI) conditions, which are followed by comparably slow relaxations back to GS conditions within centuries or millennia. Oxygen isotope ratios in ice cores provide a qualitative proxy of the atmospheric temperature at the location of the ice core, and temperature increases of up to 16.5 °C have been reported for single DO events^{5}.
An apparent periodicity for DO events at 1470 years has been suggested^{6} and put into context with astronomical forcing by centennialscale solar cycles^{7}. However, it has also been shown that the waiting times between subsequent DO events are within the highlikelihood range of an exponential distribution, implying that the timing of the DO events is consistent with a Poisson process. The proposed periodicity could, therefore, in fact be spurious^{8}.
Although different theories to explain the DO events have been proposed, there is no agreement concerning the responsible physical mechanisms. A key question to constrain the set of potential explanations is whether the DO transitions are induced by external forcing, by noise, or by bifurcations in the underlying dynamical system. In the latter case, the DO events might be preceded by statistical earlywarning signals (EWS), such as increases in variance and autocorrelation^{9,10,11}. Heuristically, these two EWS can be associated with a widening of the basin of attraction prior to the transition, and for certain classes of lowdimensional random dynamical systems, they can be inferred rigorously^{12}, e.g. in analogy with the Ornstein–Uhlenbeck process^{11}. It should be emphasized, however, that when studying complex natural systems with many degrees of freedom, the absence of statistical EWS in the corresponding time series does not necessarily imply that the transitions are not caused by bifurcations: Different factors, such as interactions with other relevant variables, potentially across different timescales, may hide the EWS even if the transition is caused by a simple fold bifurcation. Moreover, the bifurcation structure itself may not be simple enough to cause simple EWS in terms of variance and autocorrelation increases.
If statistical EWS are observed, it is typically assumed that the corresponding transitions are not entirely noiseinduced: If a transition is not caused by a bifurcation, but by increasing noise level of the underlying random dynamical system, the variance of the time series increases, but the autocorrelation remains constant. On the other hand, if the transition is caused, e.g. by a fold bifurcation, both variance and autocorrelation are expected to increase.
The fact that a forthcoming bifurcation implies the presence of EWS does, however, not exclude the possibility that statistical fluctuations indistinguishable from EWS arise either by chance or by other mechanisms unrelated to a bifurcation or abrupt transition. In other words, the presence of statistical fluctuations resembling EWS does not necessarily imply that a bifurcation is approaching, because these fluctuations might be caused by other reasons as well. Such false positives would reduce the predictive skill of a forecast scheme based on EWS. Typically, EWS are only searched for in the parts of a time series that precede abrupt transitions, which have themselves been identified beforehand. Even in this case, statistical fluctuations that could be mistaken for EWS may arise by chance. This issue, which is related to multiple comparisons, calls for a statistical test regarding the number of observed EWS, in addition to testing the significance of each single EWS.
It was previously shown that the δ^{18}O record obtained from the North Greenland Ice Core Project (NGRIP^{4}), when interpolated to a time series with 50year temporal resolution, does not exhibit EWS if the DO events are considered individually, and if the entire frequency spectrum is taken into account^{11}. On the other hand, weak EWS have been reported when the ensemble average of DO events 2–16 (in the stratigraphic counting from younger to older events) is considered^{13}. Such an ensemble average of EWS may, however, be strongly dominated by single events, and a crossvalidation to exclude this possibility has not been performed in the latter study.
Recently, it was demonstrated that significant EWS can in fact be observed at least for some of the DO events individually, if the analysis is restricted to the highfrequency variability of the NGRIP δ^{18}O time series^{14}. The latter study is based on the more recent 20year mean time series of the NGRIP record^{15}, for the time period from 60 to 11 kyears, and focusses on the periodicity band between 40 and 60 years. Instead of the total variance and autocorrelation, scaleaveraged wavelet coefficients \(\left( {\hat w^2} \right)\) and local Hurst exponents \(\left( {\hat H^{{\mathrm{loc}}}} \right)\), respectively, are considered. In this context, \(\hat w^2\) is used to estimate the variance of highfrequency fluctuations, and \(\hat H^{{\mathrm{loc}}}\) is interpreted as an estimator of the correlation time in the high frequencies. The latter provides a suitable replacement of the autocorrelation, since an increasing \(\hat H^{{\mathrm{loc}}}\) would signal an increase in correlation time, consistent with a destabilization of the attractor. The physical hypothesis behind this approach is that there exists a subcomponent of the underlying dynamical system that operates at decadal timescales, which is responsible for the decadalscale DO transitions via a bifurcation. According to this hypothesis, EWS would be detectible in the isolated highfrequency band but masked otherwise by mechanisms operating at longer timescales. For the ensemble average of the 17 DO transitions during the studied interval, Rypdal^{14} found a significant (p < 0.05) increase of the variance of the highfrequency fluctuations. However, since the corresponding ensemble average of the autocorrelation was not studied, the significant increase of the variance could be explained by an increase of the noise level alone, instead of an approaching bifurcation. Furthermore, these ensemble results are probably dominated by the transition to the Bølling–Allerød interstadial (i.e. DO1): When considered individually, only two DO events (DO1 and DO8) are preceded by wavelet coefficient increases that are significant with p < 0.05, and only one (DO1) is preceded by a significant increase of the Hurst exponent^{14}. These numbers of EWS could, in fact, arise purely by chance.
Here the promising hypothesis of Rypdal^{14} is reevaluated with some technical modifications, using the recently published raw data of the NGRIP record, which allow for much higher temporal resolution. The raw NGRIP δ^{18}O and dust values are measured at 5cm steps in the ice core^{4}, and using the associated, annual layercounted chronology^{16,17}, these values can be interpolated to time series with regular 5year sampling steps (Fig. 1). Using these δ^{18}O and dust time series, it is thus possible to study periodicities of the NGRIP record at timescales as low as 10 years.
We refer to the Methods section below for details on the data preprocessing, as well as for definitions for the scaleaveraged wavelet coefficient \(\hat w^2\) and local Hurst exponent \(\hat H^{{\mathrm{loc}}}\), which are used to estimate the variance and correlation times, respectively, in the highfrequency bands of the δ^{18}O and dust time series.
EWS are first searched for in terms of significant positive trends in the variance (σ^{2}(t)) and lag1 autocorrelation (α_{1}(t)) of the 100year highpass filtered NGRIP data. Specifically, we apply a Chebyshev TypeI highpass filter with cutoff at 100 years to the time series and then estimate σ^{2}(t) and α_{1}(t) in sliding windows of width equal to 200 years. Thereafter, the corresponding waveletbased estimators \(\hat w^2\) and \(\hat H^{{\mathrm{loc}}}\), which are also averaged in time windows of 200 years for consistency, are analysed with particular focus on identifying the specific frequency ranges that carry the most pronounced EWS.
Results
Earlywarning signals in the variance and autocorrelation
For each abrupt transition, we first search for significant EWS in the preceding GS period, until 200 years prior to the transition to ensure that no data from the transition itself is taken into account. Note that the highresolution version of NGRIP record extends only to 59,939 years b2k, and we thus do not have sufficient data to investigate whether DO17, which occurred approximately at 59,450 years b2k, is preceded by EWS. We thus investigate 16 DO events, as well as the YoungerDryas/Preboreal transition at approximately 11,705 years b2k.
The statistical significance of trends in the different EWS estimators is determined on the basis of surrogates with randomized phases, with the null hypotheses that the trend is equal to zero (Methods). Throughout this paper, an EWS is called significant if the corresponding p value is <0.05.
As noted above, statistical fluctuations that resemble EWS may arise by chance, potentially leading to false positives. To account for this issue, which is related to the general problem of multiple comparisons, the following significance test for the total number of observed EWS is introduced: We first choose 17 time points (corresponding to the observed number of abrupt transitions) randomly from the respective time series. Thereafter, we count how many of these are preceded by significant increases of the EWS estimator in question, within time spans for which the duration is chosen in accordance with the original GS intervals. Repeating this 10,000 times, a null model distribution is obtained for the number of EWS preceding random time points. This significance test is constructed separately for EWS in the σ^{2} time series and the α_{1} time series, as well as for EWS in both of them at the same time. Corresponding tests are constructed for the waveletbased estimators \(\hat w^2\) and \(\hat H^{{\mathrm{loc}}}\) (Supplementary Figure 1).
When searching for EWS during the GS intervals of the 100year highpass filtered δ^{18}O time series, significant EWS are found for 12 out of the 17 events in the variance σ^{2}(t). In the lag1 autocorrelation α_{1}(t), significant EWS are found for 7 out of the 17 events, and for 6 out of the 17 events, EWS are detected in both σ^{2}(t) and α_{1}(t) simultaneously (Fig. 2b, c). According to the test described above, these numbers are statistically significant at 95% confidence level (Table 1 and Supplementary Figure 1).
It seems natural to restrict the search for EWS to the GS intervals prior to the transitions^{14}. Recall, however, that the hypotheses is that a dynamical subsystem operating at decadal timescales causes the transitions via a bifurcation and that the imprints of this bifurcation are masked by mechanisms with longer (centennial to millennial) timescales. If this hypotheses is correct, then the fast subsystem might, after the bifurcation and the resulting transition, return to its prior state much faster than suggested by the slow relaxation from GI to GS conditions within centuries to millennia. In such a situation, one may argue that EWS should, as in ref. ^{13}, be searched for in the entire intervals between subsequent transitions and not only during GS intervals.
Indeed, when searching for EWS in the entire time interval between subsequent transitions, with an offset of 200 years at the beginning and at the end of the interval, similar numbers of EWS are detected: We find 13 significant EWS for σ^{2}(t) and 7 significant EWS in α_{1}(t), as well as in both of them simultaneously (Fig. 2e, f) These numbers of EWS are statistically significant (Table 1 and Supplementary Figure 1).
It might be criticized that this number of significant EWS, obtained when analysing the entire intervals between subsequent transitions, is simply due to the fact that two different physical regimes—the GI and GS intervals, respectively—are considered: it is true that the highfrequency variance σ^{2}(t) is generally lower during GI than during GS intervals. However, this is not the case for the autocorrelation coefficient α_{1}(t) and, moreover, the physical cause of the lower σ^{2}(t) during GI intervals may be directly related to the physical cause of the observed statistical EWS themselves. Ultimately, it will only become possible to answer this question once an unambiguous physical theory of the DO events is established, because that would allow to explain the statistical EWS in terms of physical processes. Since such a theory has not yet been obtained, the results for both options are presented here.
Waveletbased earlywarning signals
As an alternative to \(\sigma ^2\left( t \right)\) and \(\alpha _1\left( t \right)\), it was suggested by Rypdal^{14} to consider the scaleaveraged wavelet coefficient \(\hat w^2\left( t \right)\) and the local Hurst exponent \(\hat H^{{\mathrm{loc}}}\left( t \right)\) of the \(\mathrm{\updelta} ^{18}{\mathrm{O}}\) time series. When restricting the latter two estimators to the 10–50 year periodicity band, we observe significant correlations with \(\sigma ^2\left( t \right)\) and \(\alpha _1\left( t \right)\): \(\rho \left( {\sigma ^2(t),\hat w^2\left( t \right)} \right) = 0.97\), and \(\rho \left( {\alpha _1\left( t \right),\hat H^{{\mathrm{loc}}}\left( t \right)} \right) = 0.71\). This indicates that the waveletbased estimators are indeed suitable as EWS indicators.
When restricting the search for EWS to the GS intervals and the 10–50 year periodicity band, we find 12 significant EWS in \(\hat w^2\left( t \right)\), 8 significant EWS in \(\hat H^{{\mathrm{loc}}}\left( t \right)\) and 7 significant EWS simultaneously in both (Fig. 3b, c). Again, these numbers are significant at 95% confidence according to the test described above (Table 1 and Supplementary Figure 1). While we find 13 EWS in \(\hat w^2\left( t \right)\) when searching for EWS in the entire intervals between DO transitions, the number of EWS in \(\hat H^{{\mathrm{loc}}}\left( t \right)\) and hence also the number of simultaneous EWS in both is reduced to 3 (Fig. 3e, f). Although a comparably small number, this is still a statistically significant result (Table 1 and Supplementary Figure 1). Note that, if the Morlet wavelet basis is used in this situation instead of the Paul wavelet basis, 14 significant EWS are found in \(\hat w^2\left( t \right)\), and 6 significant EWS in \(\hat H^{{\mathrm{loc}}}\left( t \right)\), as well as in both estimators simultaneously (Supplementary Figure 2).
Remarkably, the corresponding analysis of the dust time series reveals a substantially smaller (and not significant) number of EWS (Table 1 and Supplementary Figure 3), although the dust time series itself is quite strongly correlated with the δ^{18}O time series (the Pearson correlation is ρ = 0.76).
The fact that we find significant numbers of simultaneous EWS in σ^{2}(t) and α_{1}(t) of the 100year highpass filtered δ^{18}O time series, as well as in \(\hat w^2\) and \(\hat H^{{\mathrm{loc}}}\) confined to the 10–50 year periodicity band of the same variable, provides direct evidence for a widening of the basin of attraction associated with the hypothesized mechanism operating at decadal scales. To find the periodicity band with the highest number of significant EWS in the δ^{18}O time series, the above analysis of the waveletbased estimators is repeated for different values of the lower (s_{1}) and upper (s_{2}) bound of the investigated periodicity band, namely, all combinations with s_{2} ∈ [20, 30,…, 100, 110], and s_{1} ∈ [10,…, s_{2} − 10] such that s_{1} < s_{2}. When searching for EWS only in the GS intervals prior to the transitions, \(\hat w^2\) exhibits a maximum of 12 EWS for several combinations of s_{1} and s_{2}, but with s_{1} at most equal to 30 years (Fig. 4a). For \(\hat H^{{\mathrm{loc}}}\), less EWS are observed, with highest numbers found for s_{1} = 10 years and s_{2} < 60 years (Fig. 4c). The highest numbers of simultaneous EWS in both \(\hat w^2\) and \(\hat H^{{\mathrm{loc}}}\) is 7, found for s_{1} = 10 years and s_{2} = 50 or 60 years (Fig. 4e).
When, instead, searching for EWS in the entire interval between subsequent transitions, the averaged wavelet power \(\hat w^2\) exhibits 13 significant EWS for s_{1} = 10 years and s_{2} = 40 years or s_{2} = 50 years (Fig. 4b). However, \(\hat H^{{\mathrm{loc}}}\) exhibits substantially less significant EWS in this situation, with highest number equal to 6, observed for (s_{1}, s_{2}) = (10, 20) years and (s_{1}, s_{2}) = (70, 80) years (Fig. 4d). The highest numbers of simultaneous EWS in both estimators are 4 and 5, detected in the latter two periodicity bands (Fig. 4f).
Discussion
The hypotheses that the DO transitions are caused by bifurcations in a dynamical subsystem operating at decadal timescales, which was first postulated by Rypdal^{14}, is thus confirmed by the results presented here, using the higherresolution NGRIP δ^{18}O data.
The EWS detected here carry, despite the terminology, little predictive power: First, the above significance test on the number of EWS shows that a considerable number of false positives would be involved in a forecast based on these EWS. Second, a forecast issued on the basis of EWS would require to quantify a lead time, and it is unclear how to achieve this with observational data. Note that these issues are not specific to the results presented in this study but apply generally to EWS in empirical time series. To address them, substantial further research is needed; in particular, a very detailed reconstruction of the underlying attractor basin, alongside a precise estimation of the internal noise level, would be needed, and both would have to be put into quantitative relation with the changes in EWS estimators, such as variance or autocorrelation. Note that the restriction to specific frequency bands, and thus considering \(\hat w^2\) and \(\hat H^{{\mathrm{loc}}}\) instead of the variance and autocorrelation, further complicates the problem of using the signals revealed here in a predictive setting.
The EWS presented here are, however, very useful from a different perspective, namely, in the context of relating statistical EWS with associated physical mechanisms. In the case at hand, the presence of EWS in both σ^{2} and α_{1}, as well as in the waveletbased estimators \(\hat w^2\) and \(\hat H^{{\mathrm{loc}}}\), obviously suggests that the DO events are neither directly externally forced nor purely induced by noise. Furthermore, the timescale at which the EWS are overall most pronounced, i.e. the 10–50 year periodicity band, helps to constrain the set of potential physical mechanisms responsible for the DO transitions: It is unlikely that oceanic circulation processes alone, such as changes in the Atlantic Meridional Overturning Circulation (AMOC^{18,19}), would leave their imprint in such high frequencies. Hence, the covariability between NGRIP δ^{18}O and AMOC strength that is inferred from paleoclimate proxy data^{20} is, on the basis of the results presented here, more likely to be due to a response of the AMOC to the bifurcation in the proposed, fast subsystem, than by a driving role of the AMOC. On the other hand, the dust concentration in ice cores is typically interpreted as a proxy for atmospheric circulation variability^{21,22}. The fact that substantially less EWS are found in the dust time series therefore indicates that atmospheric processes are less likely to be the direct triggers of the DO events.
It has previously been suggested that the DO transitions in Greenland could be triggered by a rapid retreat of sea ice in the northern North Atlantic^{23,24,25,26,27}. The δ^{18}O values in ice cores are not a direct proxy of the air temperature at the ice core site, because they depend, in fact, on the temperature gradient between the source region of the precipitation and the location of the ice core^{28,29}. Indeed, a substantial cooling of the source temperatures around the DO events has been inferred from the deuterium excess^{30}. There are, therefore, two mechanisms related to sea ice extent that affect this temperature gradient: First, a rapid retreat of sea ice, e.g. due to warming subsurface waters, would lead to the abrupt release of heat to the atmosphere, which was previously trapped below the ice^{26,31}. This would enhance air temperatures at the ice core site and thereby reduce the temperature gradient to the source region. Second, rapid sea ice retreat would shift the evaporative source region of the water precipitating in Greenland northward and thereby reduce the temperature gradient as well. Both mechanisms would thus lead to an increase of δ^{18}O in the ice.
For these reasons, it is indeed very likely that variations of the extent of the sea ice cover are noticeable in the 10–50 year periodicity band of the NGRIP δ^{18}O time series, and the EWS signals reported here could hence be physically explained by enhanced fluctuations of the sea ice extent as this dynamical subsystem destabilizes on its way to the bifurcation. In this sense, the results presented here support hypotheses on mechanisms related to rapid sea ice retreat to explain the DO events.
Methods
Data preprocessing
We employ the raw δ^{18}O and dust concentration data from the NGRIP at 5cm depth resolution for the period from 60 to 11.7 kyears b2k^{4,21,32}. In combination with the Greenland Ice Core Chronology 2005^{16,17}, which provides annuallayercounted ages until approximately 60 kyears b2k, the δ^{18}O and dust values are interpolated to time series with regular 5year sampling steps using cubic splines. The cumulative dating uncertainties, which arise from dating this record by counting annual layers, are not relevant for the kind of analysis presented in this study^{33}. Figure 1 shows the temporal sampling steps between subsequent measurements and indicates that a temporal resolution of 5 years can be regarded as a lower bound^{34}, below which the possibility of biasing artefacts arising from the interpolation cannot be excluded: a fraction of 0.4% of the total number sampling steps is >5 years, but a comparably high fraction of 5.2% is >4 years. Note that, for the dust record, we consider log(dust), because its values are approximately lognormally distributed^{21}.
Scaleaveraged wavelet coefficient and local Hurst exponent
A comprehensive introduction to Wavelets can be found, e.g. in ref. ^{35}. For our analysis, we use the Paul wavelet basis (of order 4) because we are mainly interested in wavelet estimates that are sharp in time. However, corresponding results using the Morlet wavelet basis are also considered.
As an estimate of the wavelet power in a periodicity band between scales s_{1} and s_{2}, we compute the following weighted average of the wavelet power spectrum W_{ t }(s)^{2}, over all periodicities from s_{1} to s_{2}:
where 〈⋅〉_{Δt} denotes a moving average of width Δt, centred around t. For the reconstruction factor, we use C_{δ} = 1.132 (ref. ^{35}), the resolution of frequency scales is set to δj = 0.1, and the temporal sampling resolution is δt = 5 years. Note that, in contrast to ref. ^{14}, a weighted average of W_{ t }(s_{ j })^{2} is considered, in accordance with Eq. (24) in ref. ^{35}. This choice assures that, when summing over all scales, the total variance is recovered (see Eq. (14) in ref. ^{35}). Practically, the results on numbers of significant EWS do not depend on this choice.
For the local Hurst exponent \(\hat H^{{\mathrm{loc}}}\left( t \right)\), we have the scaling
and \(\hat H^{{\mathrm{loc}}}\left( t \right)\) is thus, as in ref. ^{14}, determined from the slope of a linear fit between log(s) and \({\mathrm{log}}\,\left\langle {\left( {\left {W_t\left( s \right)} \right^2/s} \right)} \right\rangle\), for s_{1} ≤ s ≤ s_{2}. Finally, both \(\hat w^2\left( t \right)\) and \(\hat H^{{\mathrm{loc}}}\left( t \right)\) are smoothed using a Chebyshev TypeI lowpass filter (with cutoff at 800 years) to extract the millennialscale variability of these highfrequency components.
Testing for significant trends
The σ^{2}, α_{1}, \(\hat w^2\) and \(\hat H^{{\mathrm{loc}}}\) time series are, by construction, significantly autocorrelated. Therefore, the classical Mann–Kendal test for significance of trends is not applicable^{36,37}. A null model based on phaserandomized surrogates preserves the spectral density and hence also the autocorrelation structure and is thus more suitable. However, it should be noted that an existing trend leads to an overestimation of the autocorrelation^{37,38}. Therefore, a linear model with autocorrelated noise is first fitted (using Maximum Likelihood) to each time series segment that is tested for EWS in terms of significantly positive trend in either of the estimators. If a nonzero trend is detected by this linear model, the trend is removed from the time series segment in question. Thereafter, surrogates are constructed from the detrended segment by randomizing the phases in Fourier space^{14,39,40}. For each time series segment, we construct 10,000 surrogates, compute the linear trend by fitting a linear model for each of them, and then derive a null model distribution for the linear slopes under the assumption that there is no trend (Supplementary Figure 4). Observed trends in σ^{2}, α_{1}, \(\hat w^2\) and \(\hat H^{{\mathrm{loc}}}\)—correspondingly computed by fitting a linear model—are considered to be significant if their p value with respect to these null model distributions is <0.05. Note that separate null models are constructed for each segment of σ^{2}(t), α_{1}(t), \(\hat w^2\) and \(\hat H^{{\mathrm{loc}}}\).
Code availability
All python code used for the analysis is available upon request via email (nboers@ic.ac.uk or boers@pikpotsdam.de).
Data availability
The raw NGRIP data are freely available at http://www.iceandclimate.nbi.ku.dk/data/.
References
Dansgaard, W. et al. A new Greenland deep ice core. Science 218, 1273–1277 (1982).
Johnsen, S. J. et al. Irregular glacial interstadials recorded in a new Greenland ice core. Nature 359, 311–313 (1992).
Dansgaard, W. et al. Evidence for general instability of past climate from a 250kyr icecore record. Nature 364, 218–220 (1993).
Andersen, K. K. et al. Highresolution record of Northern Hemisphere climate extending into the last interglacial period. Nature 431, 147–151 (2004).
Kindler, P. et al. Temperature reconstruction from 10 to 120 kyr b2k from the NGRIP ice core. Clim. Past 10, 887–902 (2014).
Schulz, M. On the 1470year pacing of DansgaardOeschger warm events. Paleoceanography 17, 4–1–4–9 (2002).
Braun, H. et al. Possible solar origin of the 1,470year glacial climate cycle demonstrated in a coupled model. Nature 438, 208–211 (2005).
Ditlevsen, P. D., Andersen, K. K. & Svensson, A. The DOclimate events are probably noise induced: statistical investigation of the claimed 1470 years cycle. Clim. Past 3, 129–134 (2007).
Dakos, V. et al. Slowing down as an early warning signal for abrupt climate change. Proc. Natl Acad. Sci. USA 105, 14308–14312 (2008).
Scheffer, M. et al. Earlywarning signals for critical transitions. Nature 461, 53–59 (2009).
Ditlevsen, P. D. & Johnsen, S. J. Tipping points: early warning and wishful thinking. Geophys. Res. Lett. 37, 2–5 (2010).
Kuehn, C. A mathematical framework for critical transitions: bifurcations, fast–slow systems and stochastic dynamics. Phys. D Nonlinear Phenom. 240, 1020–1035 (2011).
Cimatoribus, A. A., Drijfhout, S. S., Livina, V. & Van Der Schrier, G. DansgaardOeschger events: Bifurcation points in the climate system. Clim. Past 9, 323–333 (2013).
Rypdal, M. Earlywarning signals for the onsets of Greenland Interstadials and the Younger DryasPreboreal transition. J. Clim. 29, 4047–4056 (2016).
Rasmussen, S. O. et al. A stratigraphic framework for abrupt climatic changes during the Last Glacial period based on three synchronized Greenland icecore records: refining and extending the INTIMATE event stratigraphy. Quat. Sci. Rev. 106, 14–28 (2014).
Andersen, K. K. et al. The Greenland Ice Core Chronology 2005, 1542 ka. Part 1: constructing the time scale. Quat. Sci. Rev. 25, 3246–3257 (2006).
Svensson, A. et al. A 60 000 year Greenland stratigraphic ice core chronology. Clim. Past 4, 47–57 (2008).
Ganopolski, A. & Rahmstorf, S. Rapid changes of glacial climate simulated in a coupled climate model. Nature 409, 153–158 (2001).
Dijkstra, H. A. & Ghil, M. Lowfrequency variability of the largescale ocean circulation: a dynamical systems approach. Rev. Geophys. 43, 1–38 (2005).
Henry, L. G. et al. North Atlantic ocean circulation and abrupt climate change during the last glaciation. Science 353, 470–474 (2016).
Ruth, U., Wagenbach, D., Steffensen, J. P. & Bigler, M. Continuous record of microparticle concentration and size distribution in the central Greenland NGRIP ice core during the last glacial period. J. Geophys. Res. 108, 1–12 (2003).
Rousseau, D.D. et al. (MIS3 & 2) millennial oscillations in Greenland dust and Eurasian aeolian records  a paleosol perspective. Quat. Sci. Rev. 196, 99–113 (2017).
Gildor, H. & Tziperman, E. Seaice switches and abrupt climate change. Philos. Trans. R. Soc. A 361, 1935–1942; discussion 1942–1944 (2003).
Li, C., Battisti, D. S. & Bitz, C. M. Can North Atlantic sea ice anomalies account for DansgaardOeschger climate signals? J. Clim. 23, 5457–5475 (2010).
Dokken, T. M., Nisancioglu, K. H., Li, C., Battisti, D. S. & Kissel, C. DansgaardOeschger cycles: Interactions between ocean and sea ice intrinsic to the Nordic seas. Paleoceanography 28, 491–502 (2013).
Petersen, S. V., Schrag, D. P. & Clark, P. U. A new mechanism for DansgaardOeschger cycles. Paleoceanography 28, 24–30 (2013).
Hoff, U., Rasmussen, T. L., Stein, R., Ezat, M. M. & Fahl, K. Sea ice and millennialscale climate variability in the Nordic seas 90 kyr ago to present. Nat. Commun. 7, 12447 (2016).
Jouzel, J., Hoffmann, G., Koster, R. & Masson, V. Water isotopes in precipitation: data/model comparison for presentday and past climates. Quat. Sci. Rev. 19, 363–379 (2000).
SteenLarsen, H. C. et al. Continuous monitoring of summer surface water vapor isotopic composition above the Greenland Ice Sheet. Atmos. Chem. Phys. 13, 4815–4828 (2013).
MassonDelmotte, V. et al. GRIP deuterium excess reveals rapid and orbitalscale changes in Greenland moisture origin. Science 309, 118–121 (2005).
Rasmussen, T. L. & Thomsen, E. The role of the North Atlantic Drift in the millennial timescale glacial climate fluctuations. Palaeogeogr. Palaeoclimatol. Palaeoecol. 210, 101–116 (2004).
Gkinis, V., Simonsen, S. B., Buchardt, S. L., White, J. W. C. & Vinther, B. M. Water isotope diffusion rates from the NorthGRIP ice core for the last 16,000 years—glaciological and paleoclimatic implications. Earth. Planet. Sci. Lett. 405, 132–141 (2014).
Boers, N., Goswami, B. & Ghil, M. A complete representation of uncertainties in layercounted paleoclimatic archives. Clim. Past 13, 1169–1190 (2017).
Boers, N. et al. Inverse stochasticdynamic models for highresolution Greenland ice core records. Earth Syst. Dyn. 8, 1171–1190 (2017).
Torrence, C. & Compo, G. A practical guide to wavelet analysis. Bull. Am. Meteorol. Soc. 79, 61–78 (1998).
Storch von, H. in Analysis of Climate Variability: Applications of Statistical Techniques (eds von Storch, H. & Navarra, A.) Ch. 2 (Springer, Berlin, 1995).
Zhang, Y. & Zwiers, F. W. Comment on “Applicability of prewhitening to eliminate the influence of serial correlation on the MannKendall test” by Sheng Yue and Chun Yuan Wang. Water Resour. Res. 40, W03805 (2004).
Wang, X. L. & Swail, V. R. Changes of extreme Wave Heights in northern Hemisphere Oceans and related atmospheric circulation regimes. J. Clim. 14, 2204–2221 (2001).
Schreiber, T. & Schmitz, A. Improved surrogate data for nonlinearity tests. Phys. Rev. Lett. 77, 635–638 (1996).
Räth, C. & Monetti, R. Surrogates with random Fourier phases. In Topics on Chaotic Systems: Selected Papers from Chaos 2008 International Conference (eds Skiadas, C. H. et al.) 274–285 (World Scientific, Singapore, 2009).
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The author acknowledges funding by the Alexander von Humboldt Foundation, the German Federal Ministry for Education and Research, and the German Science Foundation. Helpful discussions with Michael Ghil and Andreas Groth are gratefully acknowledged.
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Boers, N. Earlywarning signals for DansgaardOeschger events in a highresolution ice core record. Nat Commun 9, 2556 (2018). https://doi.org/10.1038/s41467018048817
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DOI: https://doi.org/10.1038/s41467018048817
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