Broad-scale climate control of vegetation is widely assumed. Vegetation-climate lags are generally thought to have lasted no more than a few centuries. Here our palaeoecological study challenges this concept over glacial–interglacial timescales. Through multivariate analyses of pollen assemblages from Lake El’gygytgyn, Russian Far East and other data we show that interglacial vegetation during the Plio-Pleistocene transition mainly reflects conditions of the preceding glacial instead of contemporary interglacial climate. Vegetation–climate disequilibrium may persist for several millennia, related to the combined effects of permafrost persistence, distant glacial refugia and fire. In contrast, no effects from the preceding interglacial on glacial vegetation are detected. We propose that disequilibrium was stronger during the Plio-Pleistocene transition than during the Mid-Pliocene Warm Period when, in addition to climate, herbivory was important. By analogy to the past, we suggest today’s widespread larch ecosystem on permafrost is not in climate equilibrium. Vegetation-based reconstructions of interglacial climates used to assess atmospheric CO2–temperature relationships may thus yield misleading simulations of past global climate sensitivity.
Natural vegetation patterns in space and time are assumed to reflect mainly climate variability on all environmentally relevant temporal and spatial scales1,2. For example, it has been shown that vegetation turnover in space can substitute for turnover in time on millennial timescales3, which fits with the findings that the climatic niches of individual plant taxa are generally stable over even longer timescales4. Although lag times between vegetation and climate changes have been extensively discussed with respect to tree migration patterns in Europe and North America following the last glacial stage5,6,7, most proxy studies do not suggest major vegetation–climate disequilibria8. Relevant model evidence is lacking. Patterns of Late Pleistocene interglacial vegetation histories (marine isotope stage (MIS) 11, 9, 7 and 5) as inferred from long-term pollen records from Greece9 and the Massif Central10 are, in addition to their established relationship with interglacial climate, hypothesized to reflect the different locations of glacial refugia, creating unique interglacial migrational patterns. This accords with the suggestion that in addition to climate, post-glacial migration limitations might also explain the current distribution of many European plant species11. Furthermore, an analysis integrating modern plant community composition, their climatic niches and climate change since the Last Glacial Maximum implies that North and South American forests are still responding to last glacial climate change12. However, systematic investigations of changes in vegetation–climate relationships over glacial-interglacial timescales are lacking and thus the concept of ‘glacial legacies’ on interglacial vegetation has not been demonstrated using proxy data.
High-northern latitudes are ideally suited to detect former non-equilibrium patterns as climate change is particularly strong due to polar amplification13. Furthermore, the southern expansion of permafrost soils during glacial climate states14 may have increased the distance between glacial refugia and potential interglacial refugial areas. However, non-climatic vegetation drivers such as herbivory15,16, fire17 or soil disturbance18 should also be considered. Finally, tectonic impacts and their climatic effects may represent a hidden driver of long-term vegetation change in the Arctic19.
The only high-latitude pollen record continuously spanning several glacial-interglacial cycles is from Lake El’gygytgyn in Chukotka, Russian Far East ranging from 3,530 to 2,150 kyr ago BP (refs 20, 21), covering both the Mid-Pliocene Warm Period (MPWP: 3,530–2,900 kyr ago) and the Plio-Pleistocene transition (PPT: 2,900–2,150 kyr ago). The identification of vegetation–climate disequilibrium requires proxy records that reliably reflect regional climate change and are independent of the Lake El’gygytgyn pollen data and of sufficient temporal length and resolution. Unfortunately, no independent climate record from Lake El’gygytgyn or any other arctic terrestrial site of sufficient data quality exists. Accordingly, only marine records can be used. Here we assume and later confirm that the globally integrating benthic isotope stack (LR04)22 and nearest sea-surface temperature (SST)23 records from the Pacific can be used to approximate the climate conditions at our study site. While all climate records indicate that the relative intensities of glacials and interglacials vary over time, a behaviour likely related to differences in orbital configuration24 and internal climate dynamics, these intensities appear to be largely globally coherent.
To assess the impact of herbivory, fire and soil disturbance on vegetation, common non-pollen palynomorphs in lake sediments can be used including Sporormiella25 (a coprophilous fungal spore), Gelasinospora26 (a fungal spore characteristic of burned soils) and Glomus27,28 (an endomycorrhizal fungal spore characteristic of disturbed soils), respectively.
Here through multivariate analyses we show that variation among interglacial pollen assemblages at Lake El’gygytgyn through the PPT is best explained by long-term drivers (that is, proxies for climate and the vegetation condition of the preceding glacial), which we interpret to indicate major vegetation–climate disequilibrium. In contrast, short-term drivers (that is, proxies for contemporaneous climate, soil disturbance/erosion and/or herbivory) best explain statistically the variations in the pollen data of the PPT glacial and MPWP interglacials and glacials. From these results we conclude that the severe glacial climate and related extensive permafrost during some PPT led to distant glacial refugia, particularly of evergreen tree taxa, that hindered their subsequent interglacial establishment and the development of forests attaining equilibrium with climate. Our results imply that the current widespread larch ecosystem actually represents a transitional vegetation type reflecting severe last glacial (MIS2) conditions rather than contemporaneous Holocene interglacial (MIS1) climate.
Vegetation change on glacial–interglacial timescales
A principal curve of the Lake El’gygytgyn pollen record, which summarizes complex multivariate data in one dimension, shows strong temporal variations (Fig. 1 and Supplementary Figs 1 and 2, 47% variation explained). The most obvious turnover at the glacial–interglacial timescale has already been described and related to 41 kyr obliquity insolation cyclicity20. Furthermore, the principal curve is consistent with a landscape openness curve based on the pollen-based biome-reconstruction technique of the same pollen record29. This suggests that millennial-scale vegetation variability generally reflects global climate shifts between glacial and interglacial states known from many proxy-based reconstructions22,23,30. The sequence of pollen types along the principal curve (Fig. 2) generally reflects their present-day relative occurrences in vegetation ranging from arctic steppe-tundra to dark needle-leaf forests31. As we focus on variability at glacial–interglacial timescales, similar principal curve analyses were performed with pollen spectra averaged for each marine isotope stage (see Methods). They show a very similar trend (Fig. 1, 75% variation explained: Supplementary Fig. 3). Inferred glacial–interglacial vegetation variability generally confirms SST reconstructions23, suggesting that the glacial–interglacial amplitude during the MPWP was rather low compared with that of the PPT. Furthermore, the principal curve suggests that differences in pollen composition among glacials and among interglacials are in the same range as glacial–interglacial variability, particularly during the PPT. As expected, the pollen spectra-specific contribution to compositional turnover (=Local-Contribution-to-Beta-Diversity32), here used as a measure of the uniqueness of the pollen composition in a marine isotope stage, is generally high for stages with extreme principal curve values.
A globally coherent pattern of stage intensities
To test our assumption that we can approximate the climate conditions at our site with remote marine temperature and isotope records, we first investigate the global pattern of glacial and interglacial intensities. We compare the time series of glacial peak temperatures of a global set of SST records (Supplementary Table 1 and Supplementary Fig. 4) with the glacial intensities recorded in the LR04 stack (see Methods). The same analysis is also performed on the interglacial intensities. To ensure that most of the records overlap, we analyse the correlation during the PPT (2,150–2,900 kyr ago). The glacial intensities in all records cores show a significant (P<0.05) positive correlation to the inverted LR04 stack (Fig. 3) with a mean correlation of r=0.81. Interglacial intensities also show a positive correlation at all core sites with the inverted LR04 stack (mean r=0.69). The weakest correlations are obtained for the tropical cores from the Indian Ocean (ODP722) and Atlantic (ODP662). As the interglacial temperatures at these cores are also at the temperature limit of the specific (UK33) proxy (Supplementary Table 1), it is unclear if this is a climatic signal or a proxy artefact.
While a systematic Plio-Pleistocene analysis, omitting pollen-based records to avoid circular reasoning, is limited to marine temperature proxies, analysing the Late Quaternary period also allows the inclusion of other climate proxy records. Here Antarctic ice cores provide independent evidence for the coherency of glacial–interglacial intensities34. Our comparison of stage extremes in isotope, CO2 and methane records (Supplementary Fig. 5) show a significant correlation of the glacial intensities (mean correlation of ice-core records with the LR04 stack r=0.52) and a very strong correlation of the interglacial intensities (r=0.91). This result strongly suggests that the synchronizing factors (including greenhouse gases) are dominant over the local imprint of seasonal insolation24 in shaping the strength of the interglacials.
Drivers of vegetation change
To separate the effects of long-term and short-term drivers on interglacial vegetation, redundancy analysis (RDA) was applied to the data set of PPT averaged interglacial pollen spectra and proxy-based environmental variables (Fig. 1). We find that variables reflecting contemporaneous interglacial climate and fire, that is, short-term ecological drivers, explain only a small portion of the variation in the pollen data when included separately in RDA (15% P<0.1, 18% P<0.05, respectively, Fig. 4 and Supplementary Table 2) compared with variables reflecting climate and vegetation type from the preceding glacial stage (42% P<0.001, 29% P<0.01, respectively). Though a large part of pollen variation is shared by all or is a combination of several variables, each variable explains a unique portion of variation as inferred from variation partitioning using a specific ensemble of RDA runs (Fig. 4 and Supplementary Figs 6 and 7). Preceding glacial climate explains the highest unique portion (18%) of pollen variation.
To test whether this result is sensitive on the choice of the climate record, RDAs of PPT interglacial pollen assemblages were repeated for each of the globally available climate records (Supplementary Table 1) with reasonable data quality. Results (Supplementary Table 3) reveal that the preceding glacial climate in all tested cases explains a significant unique portion while interglacial climate does not explain a unique portion or only a small portion. Consistent with the global coherency of the glacial–interglacial intensities, this indicates that neither the selection of a specific proxy type nor the selection of a specific site would impact the major outcome of this study.
In addition, similar RDAs were applied to the other averaged data sets. We find that the variation in the PPT glacial pollen spectra is most parsimoniously explained by the contemporary climate variable and to a lesser extent by the soil disturbance/erosion proxy, with both explaining a unique and statistically significant portion of the variation (Fig. 4). MPWP interglacial pollen are significantly correlated to climate, vegetation of the preceding glacial, herbivory and fire when each variable (or variable set) is considered separately in RDA. However, variation partitioning shows that the major part of the explained variation is shared by all or a combination of several variables. MPWP glacial pollen spectra are most strongly related to contemporaneous glacial climate and herbivory (Fig. 4).
Differences among PPT interglacial vegetation histories
On the basis of the RDA biplots (Supplementary Fig. 6a,b) where variables for the preceding glacial are constrained to the first RDA axes and all the remaining known environmental variation is partialled out, we conclude that interglacials with preceding weak glacials and prevailing tree-tundra, such as G9, G7, G3, MIS101 and MIS93, are characterized by Pinus (pine) and Picea (spruce) forests (see also interglacial sequences in Supplementary Figs 8 and 9). Furthermore, these interglacials are closely located in the principal curve versus Local-Contribution-to-Beta-Diversity plot (Fig. 5a). Interglacials with preceding warm glacials are also characterized by similar inter-taxa relationships as inferred from the statistically significant fit of all interglacial pairs of ordination-derived taxa scores shown by Procrustes analyses and associated Protests (see Methods, Fig. 5b, see also taxa-specific residuals in Supplementary Fig. 10). This suggests that they reflect similar interglacial vegetation histories. In summary, during the PPT, interglacials with preceding warm glacial stages share similar evergreen forest vegetation, which we assume is driven by and is in equilibrium with the contemporaneous climate.
In contrast, Pinus and Picea are absent or rarely occur during interglacials with a preceding cold glacial-stage climate and extensive arctic steppe such as G1, MIS103, MIS99, MIS95 and MIS87 while deciduous shrubs (in particular Alnus (alder)) and wetlands (indicated by high Cyperaceae (sedge) and Sphagnum (bog-moss) values) are abundant (Supplementary Figs 2, 8 and 9; see also taxa-specific residuals in Supplementary Fig. 10). Some of these interglacial spectra strongly contribute to the Local-Contribution-to-Beta-Diversity when compared with spectra from other stages with similar principal curve values (Fig. 5a). Also, the inter-taxa relationships differ strongly among single interglacials as indicated by high Protest P values (Fig. 5b and Supplementary Figs 8 and 9). In summary, interglacials with preceding strong (cold) glacial stages lack Pinus and Picea and their vegetation characteristics are non-analogous among each other.
With respect to PPT interglacials, we infer from our analyses of the Lake El’gygytgyn pollen record that the environmental state of the preceding glacial was more relevant for subsequent interglacial vegetation development, in particular for the presence or absence of evergreen conifers, than the contemporaneous interglacial climate, contradicting the hypothesis of a close vegetation–climate equilibrium. One alternative explanation for the observed weak relationship between proxy series for interglacial climate and interglacial pollen data would be that the analysed δ18Ostack and mid-latitude Pacific SST do not represent the regional interglacial climate around Lake El’gygytgyn due to proxy-specific or regional-specific differences. However, our analysis shows that the strength of an interglacial is largely coherent in the PPT between all available high-quality SST records from the Northern Hemisphere (Fig. 3), and is coherent between different proxy records, including Antarctic temperature and greenhouse gases in the last 800 kyr (Supplementary Fig. 4). This is consistent with theoretical and model considerations that climate variations on long timescales are typically associated with broad spatial scales35,36 and with evidence from climate-model simulations using orbital forcing as well as greenhouse-gas forcing37.
Such a ‘local climate’ hypothesis would also be inconsistent with our finding that the climate of the preceding glacial as recorded by the δ18Ostack and mid-latitude Pacific SST should influence the local vegetation of the interglacial. Hence, we conclude that the most parsimonious explanation for our results is that glacial climate and vegetation conditions are the main drivers of interglacial vegetation.
Accordingly, we interpret the absence of Pinus and Picea in Lake El’gygytgyn pollen spectra from interglacials following strong glacial stages to be related to three main factors: permafrost extent, distant glacial refugia, and extensive fires, plus possible interactions (Fig. 6). Today the vast continuous permafrost zone in NE Asia is covered by mono-specific larch forests with a deciduous-shrub understorey9. Occurrences of evergreen taxa (for example, Picea obovata and Pinus sibirica: for Pinus pumila see Supplementary Note 1) are restricted to the southern and western permafrost limit characterized by a summer thaw depth >1.5 m and azonal vegetation, such as on deep soils in river beds9. Permafrost with a shallow active layer is also assumed to limit the northward extent of Picea in Alaska33. In contrast, Larix gmelinii and Larix cajanderi can grow on soils with an active-layer depth of <40 cm (ref. 38). Thus, the question arises whether glacial-stage permafrost conditions are able to persist through strong interglacial warming and hence hinder or slow down the invasion of evergreen taxa and are therefore the key environmental link causing vegetation–climate disequilibrium. It can be assumed that permafrost during strong glacials was particularly extensive and deep because widespread continental-scale ice sheets were absent here and would not insulate soils from the very cold and harsh glacial climate39. Furthermore, during strong glacials, permafrost was likely more widespread due to enhanced continentality related to the absence of in-land moisture transport (that is, no snow in winter), perhaps as a result of lower sea level (60–70 m)40 and more persistent sea-ice over the Arctic ocean41. Though permafrost was inferred to persist even to a few metres below the surface in warmer climates during the Eemian interglacial in areas that are today located in the discontinuous permafrost zone42, modelling results indicate that the active-layer depth responds rather directly to climate43 while only deep permafrost may have millennial-scale lags to insolation maxima44. However, model studies have not been performed over long timescales and most do not include all relevant Earth-system components and their interactions. Our knowledge of permafrost response to climate change during the PPT is thus very limited.
The more southerly extensive permafrost during strong glacial stages possibly shifted the glacial refugia of Pinus and Picea farther south in addition to the severe glacial climate. For example, the vast steppes recorded at Lake El’gygytgyn during MIS96 stretched as far south as the Lake Baikal region, which accompanied the widespread extinction of evergreen needle-leaf taxa45. In contrast, Larix (larch) probably survived in NE Russia during all glacials, by analogy to its last glacial maximum (LGM) history46. The pollen compositional turnover of the PPT interglacials indicates the establishment of dense larch forests with shrub Alnus (Supplementary Fig. 9). These forests in particular, when occurring in combination with a thick Sphagnum cover47, insulate the soil from climate, thereby stabilizing the permafrost38 and likely hinder the germination and establishment of Picea and Pinus. Such an ecosystem with a high-standing biomass in a warm, continental early interglacial climate is likely to experience frequent fires. This is indicated by the maximum Gelasinospora abundance coincident with the Larix–Alnus-type optimum in the interglacial sequences (Supplementary Fig. 9). By a study of succession in present forests from central Siberia it has been shown that the ratio of deciduous (Larix and short-lived shrubs) to evergreen taxa cover (Picea and Pinus) is higher at sites characterized by frequent fires48. Hence it is reasonable to assume that no single driver caused the expansion of deciduous shrubs and larch forests in warm interglacials but the combination of persistent permafrost, distant refugia and high fire frequency may have slowed the invasion of Picea and Pinus and thus caused long-term vegetation–climate disequilibrium (Fig. 6).
The prevailing transient vegetation types during interglacials following strong glacials have unique characteristics, which probably originated from taxon reshuffling. In contrast, during interglacials following weak glacial stages, Pinus and Picea remained in the area or in nearby refugia and invaded northern Siberia and the northern Russian Far East before shrub-rich larch forests became stabilized by feedbacks with permafrost and fire. Accordingly, vegetation–climate equilibrium, characterized by a fixed vegetation composition, was reached in a consistent manner. Hence, we conclude that disequilibrium versus equilibrium conditions differentiate interglacials with strong or weak preceding glacial states rather than a bifurcation with two stable states.
Our reasoning that permafrost presence likely contributed to the slow invasion of evergreen taxa is further supported by results from numerical analyses with the remaining averaged data sets. We find that the effect of preceding glacial drivers is much smaller during MPWP interglacials when widespread permafrost was probably absent. In contrast, contemporaneous climate during the MPWP was a main driver. For example, the warm climate supported the expansion of dark needle-leaf forests during MPWP interglacials, in particular during the two oldest recorded interglacials (MG7 and MG5) that were also among the warmest with the smallest ice-sheet extent22,23. Furthermore, MPWP and PPT glacial vegetation is not related to interglacial climate or vegetation conditions but is best explained statistically by contemporaneous climate. In other words, severe climate change during a glacial-to-interglacial transition causes a leading-edge disequilibrium due to slow invasion8, while a slow die-back of long-lived trees (trailing-edge disequilibrium) is unlikely given the severe climate deterioration during an interglacial–glacial transition; the Arctic is known for its strong feedback mechanisms13.
In addition to long-term drivers, our study provides evidence that short-term drivers can disturb the vegetation–climate relationship on glacial–interglacial timescales. Our analyses suggest that MPWP glacial and interglacial vegetation is significantly related to changes in herbivory (Fig. 4). It is assumed that large herbivores, particularly mammoths and mastodons but also deer and bison, have the potential to act as ‘ecological keystones’ in high-latitude vegetation15,16,49. The herbivore fauna of the MPWP was potentially even richer than that of MIS2 and potentially exerted its impact far into the forested areas. This is suggested by, for example, fossil records of camel ancestors on Ellesmere Island (Canadian High Arctic) formerly covered by boreal larch forests50. The varying herbivore abundance, as inferred from the coprophilous Sporormiella spore record during the MPWP, may have led to marked vegetation variation. Our results suggest that herbivory during MPWP glacials turned a deciduous shrub-tundra (less Betula nana type (dwarf birch) in the pollen spectra, Supplementary Fig. 6f) into an open steppe forest (more Larix and Poaceae (grasses)) comparable to the ‘mammoth steppe’ proposed for the LGM in Beringia51. A parallel decline of large herbivores and deciduous-shrub encroachment also occurs at the end of the late-glacial in North America52,53 and this pattern is supported by modern exclosure experiments53. Accordingly, our results indicate that herbivory may represent a significant vegetation driver on glacial–interglacial timescales acting independently of climate, thereby weakening the vegetation–climate link. However, no vegetation–herbivore relationship is indicated for the PPT, which contradicts the exploitation–ecosystem hypothesis54,55. According to this hypothesis unproductive ecosystems can only support food-limited grazers that exert a strong control on vegetation. More productive ecosystems such as occurred during the MPWP, in contrast, should be characterized by community-level trophic cascades, which should, according to this hypothesis, result in a weaker vegetation–herbivore relationship. However, the weak vegetation–herbivore ties during the PPT can potentially be explained by a local functional extinction of the megafauna, which was previously assumed when Sporormiella declined to <2% of the pollen sum53. However, it remains unknown if our observation of generally lower herbivore densities during the PPT compared with the MPWP represents a regional peculiarity or an Arctic-wide picture. Interestingly, the two major Sporormiella declines, that is, at the M2/M1 and G18/G17 transitions, occur when the magnitude of late-glacial warming was particularly strong. By analogy with the climate-driven extinction of some megaherbivores during the MIS2/Holocene transition56 we can only speculate that random processes such as extinctions during severe warming, at least partly, explain the observed herbivore density pattern around Lake El’gygytgyn. Furthermore, the potential refugia for cold-restricted plants and animals in the Asian Arctic are, compared with the North American Arctic, particularly small because the arctic coast is located further to the south and because the Bering Land Bridge was submerged during interglacials40, which may have enhanced random effects in interglacial colonization processes.
Our results suggest that vegetation–climate disequilibrium may have lasted for millennia. With the background of our results and the severity of the LGM (MIS2) we hypothesize that today’s widely distributed larch forests lacking Picea and Pinus may not be in equilibrium with contemporary climate. Support for this comes from the fact that compared with Larix, which colonized Yakutia during the late-glacial, evergreen taxa expanded only during the early- and mid-Holocene57. However, they did not significantly extend their ranges beyond the present-day limit during the Holocene thermal maximum, in contrast to Larix46. Furthermore, evergreen taxa in southern and western Siberia probably represent late-successional vegetation in present-day larch-forest regions but they only become established when fire frequency is low48.
Vegetation records are commonly used to infer past temperature quantitatively, which is then compared with modelled or reconstructed atmospheric CO2 concentrations to assess Earth-system sensitivity58. When either the modern analogues or fossil records originate from vegetation in disequilibrium with climate, the inferred climate may be misleading. As expected from our results, the PPT temperature reconstruction based on El´gygytgyn pollen data30 poorly reflects the global SST23 and global ice-volume22 trends. This suggests that pollen-based quantitative climate reconstructions are less reliable than previously assumed, particularly for interglacials. However, independent regional climate records are necessary to quantify the uncertainties of pollen-based climate reconstructions. Likewise, only transient Earth-system simulations that include realistic long-term tree-population and permafrost dynamics and run over several glacial–interglacial cycles can resolve the timing and effectiveness of vegetation-related feedback mechanisms and thus provide realistic model-based estimates for Earth-system sensitivity.
With the appearance of permafrost and the functional disappearance of herbivory, the PPT at northern high latitudes represents a valuable natural experiment in a palaeoenvironmental setting with the potential to understand better the dynamics of Earth’s past states when new system components are included.
Numerical analyses of original Lake El’gygytgyn pollen data
This paper uses a pollen data set from Lake El’gygytgyn21. Of the 1,166 samples that were analysed, 1,043 contained pollen. Of these, 844 samples with at least 150 terrestrial pollen grains and spores were included in the numerical analyses here. The pollen sum is >300 in most samples.
Principal curves59 were derived to best summarize, in a mathematical sense, the overall pollen compositional turnover and thus to maximize the variation represented in one dimension. To increase the signal-to-noise ratio, we a priori decided to include only half of the original 92 reliably recorded taxa (that is, taxa recorded at least twice in the entire data set); thus, all taxa with occurrences in >74 samples were retained for the principal curve analyses. Sample scores on the first correspondence axis were used as a starting curve. The principal curve was fitted using cubic smoothing splines allowing the complexity of the individual smoothers used in the local averaging step to vary between pollen taxa, using generalized cross-validation to select the optimal degree of smoothing for each taxon. A penalty term of 1.4 was used to increase the cost of degrees of freedom in the generalized cross-validation calculations60. Analyses were implemented in R using the pcurve package.
Analyses of averaged interglacial and glacial pollen data
To obtain averaged interglacial and glacial data sets, principal curve minima and maxima were first assigned to marine isotope stages22 based on the original age model20. MIS84 was split into two glacial stages (MIS84a/c) and an interglacial stage (MIS84b) because a full glacial–interglacial turnover is clearly reflected in the pollen data. Boundaries between glacial and interglacials were set at the point where the mean principal curve value was crossed, calculated from the minimum principal curve values for interglacials and the maximum principal curve values for glacials. Original counts of those samples that are below/above the median PC values for each glacial/interglacial were then summed for all taxa. This step was done to ensure that the averaged data sets represent the ‘characteristic’ pollen assemblages of each stage rather than the ‘transitional’ assemblages between stages. To reduce the noise in the data set, percentages were calculated including vascular-plant pollen taxa that occur in at least 12 stages with a value of at least 2% once. Finally, a data set of 32 averaged interglacial pollen spectra and another of 32 averaged glacial pollen spectra were obtained.
Principal curve analysis of the combined glacial–interglacial averaged data set was run with a similar configuration as for the original data set, only the penalty term was set to 2 to account for the lower number of samples. Local-Contributions-To-Beta-Diversity32, that is, representing an estimation of the compositional uniqueness of a stage was likewise calculated using the combined averaged glacial–interglacial data set.
Correlation analyses of global climate data sets
We analysed the global LR04 benthic inverted δ18Ostack (ref. 22) as well as a global collection of high-resolution SST records. We required that the full PPT (2,150–2,900 kyr ago) is covered with a mean resolution of at least 5 kyr per sample. Ten published UK33 records and the LR04 benthic stack meet these criteria (Supplementary Table 1).
The irregular raw data of every core were low-pass filtered using a Gaussian Kernel Smoother with an effective cutoff frequency of 1/15 kyr. The assignment of the glacial minima and interglacial maxima was performed in two steps. (1) Local maxima and minima were automatically identified from the smoothed time series. (2) All records were visually compared using their published age model, and the corresponding glacial minima and interglacial maxima were manually chosen from the minima and maxima of step 1. We only interpreted time periods where a 100-kyr window did not contain a data gap >15 kyr to reduce the possibility that we missed major peaks or troughs. In some cases, where no clear assignment was possible, no assignment was made; thus most records only contain a subset of all extremes. For ODP1082 and ODP1012, only a small number of maxima and minima could be assigned, probably due to the poor data quality of the records in the time period of interest. We thus excluded both these cores from further analysis. As the ODP982 SST record does not have a high enough resolution until 2,600 kyr ago, we correlated ODP982 and LR04 on an extended time window (2,600–3,500 kyr ago) to obtain a meaningful overlap with the LR04 stack. The results are summarized in Supplementary Fig. 4.
We also investigated whether the coherency between glacial and interglacial intensities was restricted to the marine SST records. For the last 800 kyr, we analysed several proxies derived from Antarctic ice cores34: water isotopes related to local temperature; a methane record potentially related to low-latitude wetland dynamics; and the CO2 record representing the global carbon cycle. We compared these records with the global benthic δ18Ostack (ref. 22) using the same method as in the previous section (Gaussian smoothing, automatic local extremes identification and manual assignment according to the marine isotope stages22) (Supplementary Fig. 5). We used the same technique of comparing local extremes instead of analysing the same points in time to be consistent with our main analyses of the Plio-Pleistocene time series.
Constrained ordination analyses were run to relate statistically the variation in the averaged glacial and interglacial pollen data sets to the proxy environmental variables. RDA was chosen over canonical correspondence analysis because of the compositional gradient lengths of the pollen data being <2 s.d. as revealed by initial detrended correspondence analyses, indicating that linear-based ordination methods are appropriate with these data sets. Because the boundary conditions strongly changed, we a priori separated the data of the MPWP (3,510–2,900 kyr ago, 12 glacials, 12 interglacials) from the PPT (2,900–2,150 kyr ago, 20 glacials, 20 interglacials) following definitions of the PLIOMAX group61. This boundary also accounts for the finding that the major decrease in atmospheric CO2 concentrations occurred around 2,900 kyr ago (ref. 62), that the phase of interglacials having higher than present sea-level ended40 and that ice-rafted debris markedly increased in glacial stages from MIS16 onwards63. Setting the boundary to that time also agrees with the results of the biome reconstruction using Lake El’gygytgyn pollen data, which indicates that MIS17 was the last interglacial that was at least temporarily dominated by cool coniferous forests29.
The climate proxy set includes the δ18Ostack record22 and two alkenone-based SST records from the Pacific as no other suitable regional climate proxy data are available. Total organic carbon (TOC) values or Si/Ti ratios from Lake El’gygytgyn were not used as proxy environmental variables because terrestrial vegetation changes could have strongly impacted lake chemistry64, thereby risking circular reasoning in our analyses. We selected the LR04 δ18Ostack record22, which, in addition to the temperature-sensitive ice-sheet extent, reflects the sea-level position and thus variability in continentality in northern Asia. Furthermore, the proxy set includes the high-resolution alkenone-based SST record from the northern mid-latitude ODP site 1208 in the Pacific30. This SST record represents the closest record to Lake El’gygytgyn and is located near to the potential glacial refugia in north-eastern Asia and has, furthermore, a high data quality. Because the SST record from ODP site 1208 does not fully cover the MPWP the alkenone-based SST from the eastern Pacific ODP846 site23, which is well correlated to ODP site 1208 during the PPT65, is used for analysing the MPWP. The δ18O stack and SST records were interpolated to 2.5 kyr ago time slices and the maximum/minimum value for each interglacial/glacial was used. The same proxy records were used as variables to represent the preceding stage climate.
Square-root-transformed values of Sporormiella spore percentages (relative to the vascular-plant pollen sum), a coprophilous fungus commonly occurring in the palynomorph record, were used as a herbivore intensity proxy31. Likewise, percentages of Gelasinospora spores, which are often found at times of massive charcoal input66,67, were used as a fire-frequency proxy. Support for this comes from the observation that the occurrence of Gelasinospora is significantly related to burnt soils26, which is explained by its rapid growth rate and the resistance of its spores to high temperatures compared to other fungi. Preceding stage PC values of the combined glacial/interglacial averaged data set were used to explore long-term vegetation drivers. Furthermore, percentages of Glomus spores were used to indicate changes in the disturbance and erosion of soils28.
The following sets of RDAs were run on each of the Hellinger-transformed glacial and interglacial averaged pollen data sets. Those variables (or variable sets), which when solely included in an initial RDA yielded a statistically significant relationship with the data set (P<0.1), were included together in variation partitioning to extract the uniquely explained variation by each single environmental variable (or variable set) and the shared explained variation. Explained variations represent adjusted r2 values68.
Analyses of PPT interglacial vegetation histories
We aimed to investigate whether pollen inter-taxa relationships among PPT interglacials with preceding warm glacials (that is, ‘warm interglacials’) are different from those among interglacials with preceding cold glacials (that is, ‘cold interglacials’). For that purpose, warm interglacials (that is, having a combination of low δ18Ostack and high SST values compared with all interglacials during the PPT, and having a minimum of 12 samples: G9, G7, G3, MIS101 and MIS93) and cold glacials (that is, having a combination of high δ18Ostack and low SST, and having a minimum of 12 samples: G1, MIS103, MIS99, MIS95 and MIS83) were selected based on the climate proxy information and the minimum sample number. Inter-taxa relationships of a single interglacial are reflected by the species scores in an ordination. Accordingly, principal component analyses (with scaling focused on variable correlations) were performed on the original pollen samples of the respective warm or cold interglacials. Analyses were based on Hellinger-transformed pollen percentages of taxa that occur at least three times in each stage. To compare the ordination results of two interglacials the correlation of variable scores on the first four principal component analysis (PCA) axes was assessed using Procrustes analysis69 and its associated Protest test70. Finally, the Protest P values gained from pair-wise comparisons among all ‘warm interglacials’ and among all ‘cold interglacials’ were presented in boxplots.
Statistical programmes used and data availability
All analyses were implemented in R version 3.03 using functions in packages analogue 0.12-0, calibrate 1.7.2, pcurve 0.6-5, vegan 2.0-10 and the function beta.div. Averaged data sets and environmental proxy data used for redundancy analyses are available at www.pangaea.de.
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Arne Ramisch and Stefan Kruse contributed ideas and discussion to a very early version of the data-set analyses. We acknowledge Chris Brierley, Petra Dekens, Zhonghui Liu as well as the other data contributors for making their SST data sets publicly available and David Naafs for discussion of SST records. Cathy Jenks is thanked for her meticulous editing. This study was funded by the German Federal Ministry of Education and Research (grant no.03G0642A) and the German Research Foundation (grant nos. HE 3622/20 and ME 1169/24).
The authors declare no competing financial interests.
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Herzschuh, U., Birks, H., Laepple, T. et al. Glacial legacies on interglacial vegetation at the Pliocene-Pleistocene transition in NE Asia. Nat Commun 7, 11967 (2016). https://doi.org/10.1038/ncomms11967
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