Pollen-based quantitative land-cover reconstruction for northern Asia covering the last 40 ka cal BP
- 1Alfred Wegener Institute Helmholtz Centre for Polar and Marine Research, Research Unit Potsdam, Telegrafenberg A43, Potsdam 14473, Germany
- 2Department of Biology and Environmental Science, Linnaeus University, Kalmar 39182, Sweden
- 3Institute of Archaeology and Ethnography, Siberian Branch, Russian Academy of Sciences, pr. Akad. Lavrentieva 17, Novosibirsk 630090, Russia
- 4Institute of Environmental Science and Geography, University of Potsdam, Karl-Liebknecht-Str. 24, 14476 Potsdam, Germany
- 5College of Resources and Environment Science, Hebei Normal University, Shijiazhuang 050024, China
- 6Institute of Biochemistry and Biology, University of Potsdam, Karl-Liebknecht-Str. 24, Potsdam 14476, Germany
- apresent address: Key Laboratory of Alpine Ecology, CAS Center for Excellence in Tibetan Plateau Earth Sciences, Institute of Tibetan Plateau Research, Chinese Academy of Sciences, Beijing 100101, China
Correspondence: Xianyong Cao (firstname.lastname@example.org) and Ulrike Herzschuh (email@example.com)
We collected the available relative pollen productivity estimates (PPEs) for 27 major pollen taxa from Eurasia and applied them to estimate plant abundances during the last 40 ka cal BP (calibrated thousand years before present) using pollen counts from 203 fossil pollen records in northern Asia (north of 40∘ N). These pollen records were organized into 42 site groups and regional mean plant abundances calculated using the REVEALS (Regional Estimates of Vegetation Abundance from Large Sites) model. Time-series clustering, constrained hierarchical clustering, and detrended canonical correspondence analysis were performed to investigate the regional pattern, time, and strength of vegetation changes, respectively. Reconstructed regional plant functional type (PFT) components for each site group are generally consistent with modern vegetation in that vegetation changes within the regions are characterized by minor changes in the abundance of PFTs rather than by an increase in new PFTs, particularly during the Holocene. We argue that pollen-based REVEALS estimates of plant abundances should be a more reliable reflection of the vegetation as pollen may overestimate the turnover, particularly when a high pollen producer invades areas dominated by low pollen producers. Comparisons with vegetation-independent climate records show that climate change is the primary factor driving land-cover changes at broad spatial and temporal scales. Vegetation changes in certain regions or periods, however, could not be explained by direct climate change, e.g. inland Siberia, where a sharp increase in evergreen conifer tree abundance occurred at ca. 7–8 ka cal BP despite an unchanging climate, potentially reflecting their response to complex climate–permafrost–fire–vegetation interactions and thus a possible long-term lagged climate response.
High northern latitudes such as northern Asia experience above-average temperature increases in times of past and recent global warming (Serreze et al., 2000; IPCC, 2007), known as polar amplification (Miller et al., 2010). Temperature rise is expected to promote vegetation change as the vegetation composition in these areas is assumed to be controlled mainly by temperature (J. Li et al., 2017; Tian et al., 2018). However, a more complex response can occur mainly because vegetation is not linearly related to temperature change (e.g. due to resilience, stable states, or time-lagged responses; Soja et al., 2007; Herzschuh et al., 2016) and/or vegetation is only indirectly limited by temperature while other temperature-related environmental drivers such as permafrost conditions are more influential (Tchebakova et al., 2005).
Such complex relationships between temperature and vegetation may help explain several contradictory findings of recent ecological change in northern Asia. For example, simulations of vegetation change in response to a warmer and drier climate indicate that steppe should expand in the present-day forest–steppe ecotone of southern Siberia (Tchebakova et al., 2009) but, contrarily, pine forest has increased during the past 74 years, probably because the warming temperature was mediated by improved local moisture conditions (Shestakova et al., 2017). In another example, evergreen conifers, which are assumed to be more susceptible to frost damage than Larix, expanded their distribution by 10 % during a period with cooler winters from 2001 to 2012, while the distribution of Larix forests decreased by 40 % on the West Siberian Plain as revealed by a remote sensing study (He et al., 2017). Additionally, some field studies and dynamic vegetation models infer a rapid response of the treeline to warming in northern Siberia (e.g. Moiseev, 2002; Soja et al., 2007; Kirdyanov et al., 2012), but combined model- and field-based investigations of larch stands in north-central Siberia reveal only a densification of tree stands, not an areal expansion (Kruse et al., 2016; Wieczorek et al., 2017).
These findings on recent vegetation dynamics that contradict a straightforward vegetation–temperature relationship may be better understood in the context of vegetation change over longer timescales. Synthesizing multi-record pollen data is the most suitable approach to investigate quantitatively the past vegetation change at broad spatial and long temporal scales. Broad spatial scale pollen-based land-cover reconstructions have been made for Europe (e.g. Mazier et al., 2012; Nielsen et al., 2012; Trondman et al., 2015) and temperate China (Li, 2016) for the Holocene. However, vegetation change studies in northern Asia are restricted to biome reconstructions (Tarasov et al., 1998, 2000; Bigelow et al., 2003; Binney et al., 2017; Tian et al., 2018), which do not reflect compositional change. Syntheses of pure pollen percentage data are not appropriate due to differences in pollen productivity, which may result in an overestimation of the strength of vegetation changes (Wang and Herzschuh, 2011). This might be particularly severe when strong pollen producers such as pine (Mazier et al., 2012) invade areas dominated by low pollen producers such as larch (Niemeyer et al., 2015). Marquer et al. (2014, 2017) also demonstrated the strength of pollen-based REVEALS (Regional Estimates of Vegetation Abundance from Large Sites) estimates of plant abundance in studies of Holocene vegetation change and plant diversity indices in Europe. Accordingly, syntheses of quantitative plant cover derived from the application of pollen productivity estimates (PPEs) to multiple pollen records (Trondman et al., 2015; Li, 2016) should be a better way to investigate Late Glacial and Holocene vegetation change in northern Asia.
In this study, we employ the taxonomically harmonized and temporally standardized fossil pollen datasets available from eastern continental Asia (Cao et al., 2013, 2015) and Siberia (Tian et al., 2018) covering the last 40 ka cal BP (henceforth abbreviated to ka). We compile all the available PPEs from Eurasia and use the mean estimate for each taxon. Finally, we quantitatively reconstruct plant cover using the REVEALS model (Sugita, 2007) for 27 major taxa at 18 key time slices. We reveal the nature, strength, and timing of vegetation change in northern Asia and its regional peculiarities, and discuss the driving factors of vegetation change.
2.1 Fossil pollen data process
The fossil pollen records were obtained from the extended version of the fossil pollen dataset for eastern continental Asia containing 297 records (Cao et al., 2013, 2015) and the fossil pollen dataset for Siberia with 171 records (Tian et al., 2018). For the 468 pollen records, pollen names were harmonized to genus level for arboreal taxa and family level for herbaceous taxa, and age-depth models were re-established using the Bayesian age-depth modelling (further details are described in Cao et al., 2013). We selected 203 pollen records from lacustrine sediments (110 sites) and peat (93 sites) north of 40∘ N, with chronologies based on ≥3 dates and a <500-year-per-sample temporal resolution generally, following previous studies (Mazier et al., 2012; Nielsen et al., 2012; Fyfe et al., 2013; Trondman et al., 2015). Out of the 203 pollen records, 170 sites (83 from lakes, 87 from bogs) have original pollen counts, while in the other 33 sites only pollen percentages are available. Due to overall low site density, we decided to include these data. The pollen counts were back-calculated from percentages using the terrestrial pollen sum indicated in the original publications. Detailed information (including location, data quality, chronology reliability, and data source) on the selected sites is presented in Fig. A1 and Table A1 in the Appendix.
We selected 18 key time slices for reconstruction (Table 1) to capture the general temporal patterns of vegetation change during the last 40 ka, i.e. 40, 25, 21, 18, 14, and 12 ka during the late Pleistocene and 1000-year resolution (500-year time windows around each millennium, i.e. 0.7–1.2, 1.7–2.2 ka, etc.) during the Holocene. For the 0 ka time slice, the ca. 150-year time window (<0.1 ka) was set to represent the modern vegetation. Since few pollen records have available samples at the 0 ka time slice, the 0.2 and 0.5 ka time slices covered a 250-year or 350-year time window (0.1–0.35 and 0.35–0.7 ka, respectively) to represent the recent vegetation, following the strategy and time windows implemented for Europe (Mazier et al., 2012; Trondman et al., 2015). For the last glacial period, even broader time windows were chosen to offset the sparsely available samples (Table 1). Pollen counts of all available samples within one time window were summed up to represent the total pollen count for each time slice. In this study, we selected 27 major pollen taxa (with available PPE, pollen productivity estimate, and values) that form dominant components in both modern vegetation communities and the fossil pollen spectra and reconstruct their abundances in the past vegetation (Table 2).
2.2 The REVEALS model setting
The REVEALS model assumes the PPEs of pollen taxa are constant variables over the target period and requires parameter inputs including sediment basin radius (m), fall speed of pollen grain (FS, m s−1), and PPE with standard error (SE; Sugita, 2007). The areas of the 110 lakes were obtained from descriptions in original publications and validated by measurements on Google Earth. Their basin radii were back-calculated from their areas assuming a circular shape. There are 83 large lakes (radius >390 m; following Sugita, 2007) in our dataset with a fairly even distribution across the study area (Figs. 1 and A1), which helps ensure the reliability of the regional vegetation estimations (Sugita, 2007; Mazier et al., 2012). Only 18 bogs have published descriptions about their size and it is infeasible to measure them on Google Earth because of unclear boundaries. A test run showed that using different bog radii (i.e. 5, 10, 20, 50, 100, 200, and 500 m) did not significantly affect the REVEALS estimates (Fig. A2), hence a standard (moderate size) radius of 100 m was set for all bogs.
We collected available PPEs for the 27 selected pollen taxa from 20 studies in Eurasia (Table A2). We calculated the mean PPE from all available PPE values, but excluded records with PPE ≤ SE (Mazier et al., 2012). We included these PPEs for various species in the mean PPE calculation for their family or genus. For simplification, we did not evaluate the values or select PPE values following consistent criteria as was done in Europe (Mazier et al., 2012). Instead, we used the original values from the studies included in Mazier et al. (2012) and added new PPE values from Europe published since the synthesis by Mazier et al. (2012). SE of the mean PPE was estimated using the delta method (Stuart and Ord, 1994). Fall speeds for each of the 27 pollen taxa were retrieved from previous studies (Table 2).
The REVEALS model generally performs best with pollen records from large lakes, although multiple pollen records from small lakes and bogs (at least two sites) can also produce reliable results where large lakes are absent (Sugita, 2007; Trondman et al., 2016). Here, due to the sparse distribution of available sites, we divided the 203 sites into 42 site groups, based on criteria of geographic location, vegetation type (vegetation zone map modified from Tseplyayev, 1961; Dulamsuren et al., 2005; Hou, 2001), climate (based on modern precipitation and temperature contours), and permafrost (Brown et al., 1997) following the strategy of Li (2016); the pollen data within one site group should be of similar components and temporal patterns. To ensure the reliability of REVEALS estimates of plant cover, each group includes at least one large lake or two small sites (small lakes or bogs; Fig. 1; Table A3).
The REVEALS model was run with a mean wind speed set to 3 m s−1 and neutral atmospheric conditions following Trondman et al. (2015), and the maximum distance of regional vegetation Zmax was set to 100 km. The lake and bog sites were reconstructed using the models of pollen dispersal and deposition for lakes (Sugita, 1993) and bogs (Prentice, 1985), respectively, in REVEALS version 5.0 (Shinya Sugita, unpublished data). The mean estimate of plant abundances from lakes and bogs was calculated for each of the 42 site groups, which includes both sediment types (using the computer program bog.lake.data.fusion; Shinya Sugita, unpublished data). Finally, the 27 taxa were assigned to seven plant functional types (PFT; Table 1) following the PFT definitions for China and Siberia (Tarasov et al., 1998, 2000; Bigelow et al., 2003; Ni et al., 2010; Tian et al., 2018), with the restriction that each pollen taxon is attributed to only one PFT according to the strategy of Li (2016) (Table 2).
2.3 Numerical analyses of reconstruction
The abundance variations in the seven PFTs during the Holocene (time slices between 12 and 1 ka) from 36 site groups were used in a clustering analysis. Six site groups had to be excluded from the analysis due to poor coverage of time slices (G1, G5, G17, G19, G27, G42). For site groups with <3 missing time slices during the Holocene (G3, G16, G26, G32, G33, G35, G38, G39, G41), linear interpolation was employed to estimate the PFT abundances for the missing time slices. Time-series clustering for the three-way dataset was performed to generate a distance matrix among the site groups using the tsclust function in the dtwclust package (Sarda-Espinosa, 2018) in R 3.4.1 (R Core Team, 2017). The distance matrix was employed in hierarchical clustering (using the hclust function in R) to cluster the site groups. Constrained hierarchical clustering (using chclust function in rioja package version 0.9–15.1; Juggins, 2018) was used to determine the timing of primary vegetation changes (i.e. the first split) in each site group. A change was considered to be significant when the split passed the broken-stick test. The amount of PFT compositional change (turnover) through time during the period between 12 and 1 ka for the 36 site groups (time slices cover entire period) was estimated by detrended canonical correspondence analysis (DCCA) for each site group (ter Braak, 1986) using CANOCO 4.5 (ter Braak and Šmilauer, 2002).
3.1 Large-scale pattern
On a glacial–interglacial scale, marked temporal changes in the occurrence and abundance of PFTs are revealed, in particular the high cover of tree PFTs during the Holocene as opposed to the widespread open landscape during the glacial period. In contrast, vegetation changes in northern Asia within the Holocene are rather minor with only slight changes in PFT abundances. Cluster analyses of grouped vegetation records from the Holocene find five clusters (Fig. A3). Their spatial distribution is largely consistent with the distribution of modern vegetation types as characterized by certain PFTs. (1) Records from the forest–steppe ecotone (e.g. G12, G21; Fig. 2a) in north-central China and the Tianshan (the mentioned geographic locations are indicated in Fig. A4) have high tree PFTs during the middle Holocene. (2) Areas in southern and south-western Siberia and north-eastern China were covered by cool-temperate mixed forest or light taiga with a high diversity of trees throughout the Holocene (e.g. G2, G7, G14, G29; Fig. 2b). (3) The West Siberian Plain and south-eastern Siberia that are presently covered by open dark taiga forests (e.g. G8, G9, G33; Fig. 2c) had an even higher abundance of evergreen conifer trees during the middle Holocene than at present. (4) Larix formed light taiga forests in central Yakutia throughout the Holocene (e.g. G25, G26; Fig. 2d). (5) Northern Siberia, which is currently covered by tundra formed by boreal shrubs and herbs, had a higher share of tree PFTs during the middle Holocene (e.g. G28, G39; Fig. 2e).
The turnover in PFT composition is <0.7 SD units in almost all site groups, except G8 (0.88 SD), G9 (0.73 SD), and G24 (0.76 SD), indicating only slight vegetation change during the Holocene (Fig. 3). The three site groups with higher turnover show a distinct transition from light taiga to dark taiga in the middle Holocene (at ca. 8 ka). The significant primary vegetation changes (pass the broken-stick test) occur during different intervals in each site group. Overall, the middle Holocene (including 8.5, 7.5, 6.5, and 5.5 ka time slices) has the highest frequency of primary vegetation changes. Records from inland areas such as the West Siberian Plain, central Yakutia, and northern Mongolia are characterized by relatively many middle-Holocene splits. There are seven site groups whose primary vegetation changes during the early Holocene (including 11.5, 10.5, and 9.5 ka time slices), and most of them from the south-eastern coastal part of the study area. Only three site groups have late-Holocene primary vegetation changes (Fig. 3).
3.2 Warm temperate forest margin zone in vicinity of Tianshan and north-central China (G6, G12, G13, G16, G21, G22)
Six site groups from the warm temperate forest–steppe transition zone (G6, G21, G22) and from the lowlands adjacent to mountainous forest in arid central Asia (G12, G13, G16) are clustered together (Fig. 3). Our results indicate that these areas, which are now dominated by arid-tolerant shrub and steppe species, had more arboreal species, mainly evergreen conifer tree taxa, in the middle Holocene (Fig. 2a). For example, north-central China (G21) has a marked mid-Holocene maximum in forest cover (7–4 ka; mean 51 %). However, certain peculiarities are noted: open landscape is reconstructed between 14 and 7 ka in northern Kazakhstan (G6), followed by an abundance of evergreen conifer trees and an increase in boreal deciduous trees that maintain high values (mean 30 %) after 7 ka. In the eastern branch of the Tianshan (G12), evergreen conifer trees are highly abundant from 10 to 7 ka and after 2 ka, while low abundance occurs from 14 to 11 ka and from 6 to 3 ka. In the Gobi desert near the Tianshan (G16) there was an even higher abundance of arid-tolerant species with no notable temporal trend in abundance of arboreal species. We assume that the high arboreal cover at site groups G13 and G22 at 14 and 12 ka originates from riverine transport and therefore exclude them from further analyses.
3.3 Cool-temperate mixed forest and taiga forest in southern and south-western Siberia and north-eastern China (G2, G7, G14, G15, G18, G29, G30, G31)
Eight site groups located in (or near) the temperate mixed conifer–deciduous broadleaved forest zone (G2, G29, G30, G31) and taiga–steppe transition zone (G7, G14, G15, G18) show similar PFT compositions and temporal evolutions. At these sites, evergreen conifer tree is the dominant PFT intermixed with other arboreal PFTs, such as deciduous conifers (Larix) in the Altai Mts. and northern Mongolia, and/or temperate deciduous trees in north-eastern China (Fig. 2b).
Evergreen conifer tree is the dominant PFT at 40, 25, and 21 ka in the southern part of north-eastern China (G29), Larix then becomes the dominant taxa at 14 and 12 ka, and temperate deciduous trees increase thereafter and maintain high cover between 11 and 3 ka. After 2 ka, evergreen conifer trees increase to 32 % on average while temperate deciduous trees decrease to 18 % on average. While arboreal abundance is lower in the northern part of north-eastern China (G30, G31) than in the southern part (G29), it shows a similar temporal pattern (Fig. 2b).
Open landscape is revealed for the southern Ural region (G2) with high abundances of herbaceous species at 14 ka. The cover of Larix and evergreen conifer trees increases after 12 ka and maintains high values thereafter with no notable temporal trend (Fig. 2b).
In the taiga–steppe transition zone, Larix is the dominant arboreal taxon, particularly in the northern Altai Mts. and northern Mongolia (G15, G18). Open landscapes are inferred at 40, 21, and 12 ka on the southern West Siberian Plain (G7); cover of Larix increases at 11 ka and evergreen conifer trees increase from 9 ka and become the dominant forest taxon after 4 ka. The temporal pattern of evergreen conifer trees in the Altai Mts. (G14) is similar to the southern West Siberian Plain, although Larix maintains high abundances into the late Holocene. Relative to the Altai Mts., the abundance of evergreen conifer trees for all time windows are lower in the area north of the Altai Mts. and in northern Mongolia (G15, G18), but their temporal change patterns are consistent with those of the Altai Mts. (G14; Fig. 2b).
3.4 Dark taiga forest in western and south-eastern Siberia (G3, G4, G8, G9, G20, G32, G33, G34)
Site groups with dark taiga forest from western Siberia (G3, G4, G8, G9), the Baikal region (G20), and south-eastern Siberia (G32, G33, G34) form one cluster sharing similar PFT compositions dominated by evergreen conifer trees, with Larix and boreal broadleaved shrubs as the common woody taxa during the Holocene (Fig. 2c).
On the West Siberian Plain (G8, G9), high cover of Larix is reconstructed during the early Holocene as well as high woody cover since the middle Holocene formed by evergreen conifer trees and boreal shrubs. In the Ural region (G3, G4), evergreen conifer trees dominate the arboreal species throughout the Holocene. The absence of Larix in the early Holocene in this Ural region is a notable difference to the West Siberian Plain (Fig. 2c).
In the Baikal region (G20), a relatively closed landscape is revealed at 40 ka; openness then increases to >95 % at 25 and 21 ka. Since 14 ka, woody cover increases as shown by a notable rise in evergreen conifer trees from 14 to 8 ka and by increases of Larix after 7 ka (Fig. 2c).
In south-eastern Siberia (G32, G34), arboreal abundance is high in the early and late Holocene, but low in the middle Holocene. South of Sakhalin Island (G33), a closed landscape is revealed between 40 and 1 ka with >80 % woody cover. Evergreen conifer tree PFT has lower cover than boreal shrub PFT at 25 and 21 ka but increases in abundance around 14 ka rising to 83 % on average between 11 and 3 ka, and reduces thereafter (Fig. 2c).
3.5 Light taiga forest in north-western Siberia and central Yakutia (G10, G23, G24, G25, G26)
Plant composition of this cluster is dominated by Larix with high arboreal cover during the Holocene. Evergreen conifer trees are present at ca. 15 % cover between 11 and 2 ka, with high arboreal values (mean 73 %) during the Holocene in north-western Siberia (G10). In central Yakutia (G23, G24, G25), evergreen conifer trees increase markedly from ca. 8, 6, and 7 ka, respectively, and maintain high cover thereafter, with ca. 60 % arboreal cover throughout the Holocene. Evergreen conifer trees are almost absent in the taiga–tundra ecotone (G26; Fig. 2d).
3.6 Tundra on the Taymyr Peninsula and taiga–tundra ecotone in north-eastern Siberia (G11, G28, G35, G36, G37, G38, G39, G40, G41)
Plant compositions of this cluster are characterized by high abundances of boreal shrubs and tundra forbs. Larix is the only tree species on the Taymyr Peninsula (G11) and its abundance increases from 18 % at 14 ka to 60 % at 10 ka, and then decreases to 18 % at 5 ka. The landscape of the north Siberian coast (G28) is dominated by shrub tundra from 14 to 10 ka, then Larix increases sharply and maintains high values between 9 and 6 ka. After 5 ka, Larix reduces, and shrub tundra becomes the dominant landscape again (Fig. 2e).
In north-eastern Siberia, arboreal cover shows a decreasing trend from southerly site groups (G35, G36, G37; Fig. 2d) to northerly ones (G40, G38, G39, G41) following the increasing latitude. In the Olsky District, temporal patterns of vegetation changes in G37 are consistent with G36, with stable vegetation during the Holocene and increases in evergreen conifer tree abundance from ca. 9 ka. Arboreal composition on the southern Kamchatka Peninsula (G35) is dominated by boreal deciduous trees during the first stage of the Holocene, followed by rising abundances of Larix and evergreen conifer trees from 5 ka.
In north-eastern Siberia (G40, G38, G39, G41), the landscape is dominated by forb tundra with sparse shrubs between 40 and 21 ka; the cover of shrubs increases at 14 ka and arboreal cover (dominated by boreal deciduous trees) increases in the early Holocene (11 or 10 ka). Shrubs maintain a high abundance throughout the Holocene, while trees peak between 10 and 2 ka generally (Fig. 2e).
4.1 Land-cover changes and potential biases
The overall patterns of pollen-based REVEALS estimates of land cover are generally consistent with previous vegetation reconstructions. Although only a few site groups cover the period from 40 to 21 ka, a consistent vegetation signal indicates that relatively closed landscapes occurred in south-eastern Siberia, north-eastern China, and the Baikal region (Fig. 2), while most of Siberia was rather open, particularly around 21 ka (Fig. 2). These findings are consistent with previous pollen-based (Tarasov et al., 1998, 2000; Bigelow et al., 2003; Binney et al., 2017; Tian et al., 2018) and model-estimated biome reconstructions (Tian et al., 2018). During the late Pleistocene (40, 25, 21, 14 ka), steppe PFT abundance was high in central Yakutia and north-eastern Siberia (e.g. G25, G36, G37, G39, G40, G41), which may reflect the expansion of tundra–steppe, consistent with results from ancient sediment DNA which reveal abundant forb species during the period between 46 and 12.5 ka on the Taymyr Peninsula (Jørgensen et al., 2012). The tundra–steppe was replaced by light taiga in southern Siberia and by tundra in northern Siberia at the beginning of Holocene or the last deglaciation, which is consistent with ancient DNA results (forbs-dominated steppe-tundra; Willerslev et al., 2014).
During the Holocene, reconstructed land cover for each site group is generally consistent with their modern vegetation. The slight vegetation changes are represented by changes in PFT abundances rather than by changes in PFT presence or absence. Minor changes are also indicated in the cluster analysis, which shows that plant compositions and their temporal patterns are consistent among the site groups within the same modern vegetation zone (Fig. 3). PFT datasets from only 19 site groups pass the broken-stick test for clustering analysis, and most of them have only one significant vegetation change, further supporting the case that only slight changes occurred during the Holocene in northern Asia. In addition, the low total amount of PFT change (turnover) over the Holocene for most site groups supports the view of slight temporal changes in land cover.
Vegetation turnover on the Tibetan Plateau inferred from pollen percentages is documented to overestimate the strength of vegetation changes (Wang and Herzschuh, 2011). This matches with our results. In central Yakutia, the pollen percentage data indicate a strong vegetation change during the middle Holocene, represented by a sharp increase in Pinus pollen, but the strength of the vegetation change is overestimated because of the high PPE of Pinus. The PPE-corrected arboreal abundances in central Yakutia after ca. 7 ka with ca. 70 % Larix and ca. 10 % Pinus are consistent with modern light taiga (Katamura et al., 2009). Furthermore, the absence of Pinus macrofossils in central Yakutia throughout the Holocene (Binney et al., 2009) also suggests a restricted distribution of Pinus, possibly to sandy places such as river banks (Isaev et al., 2010).
Pollen-based turnover estimates from southern Norway range from 0.84 to 1.3 SD (mean 1.02 SD) for 10 Holocene pollen spectra (Birks, 2007), and from northern Europe from 0.01 (recent) to 0.99 (start of the Holocene) SD for three sites (N Sweden, NW and SE Finland) (Marquer et al., 2014). Moreover, the REVEALS-based turnover estimates (0.3–1) for northern Europe are significantly higher than the pollen-based one (0.2–0.8) from 11 to 5.5 kyr BP. The same is true for all other regions studied by Marquer et al. (2014) in north-western Europe, and the turnover estimates (pollen- and REVEALS-based) are generally higher at lower latitudes from southern Sweden down to Switzerland and eastwards to Britain and Ireland. These European values are higher than our REVEALS-based turnover estimates (from 0.37 to 0.88 SD, mean 0.66 SD; G3, G8, G9, G23, G24, G25, G36, G37) from a similar latitudinal range (Fig. 3). The fewer parameters used in the turnover calculations for northern Asia (PFTs) compared to Europe (pollen taxa) is a potential reason for the lower turnover obtained in this study. In addition, the PPE-based transformation from pollen percentages to plant abundances may reduce the strength of vegetation changes (Wang and Herzschuh, 2011). Aside from the methodological aspects, the lower turnover in northern Asia may, at least partly, originate from differences in the environmental history between northern Europe compared with northern Asia, i.e. glaciation followed by postglacial re-vegetation vs. non-glaciated areas with trees in refugia, respectively, and a maritime climate with temperature-limited vegetation distribution vs. a continental climate with temperature- and moisture-limited vegetation.
We consider the REVEALS-based regional vegetation-cover estimations in this study as generally reliable with reasonable standard errors (Fig. A5) thanks to the thorough selection of records with high-quality pollen data and reliable chronologies. In addition, the landscape reconstructions are generally consistent with previous syntheses of past vegetation change (e.g. Tian et al., 2018) and known global climate trends (Marcott et al., 2013), plus the clustering results of PFT abundance are consistent with modern spatial vegetation patterns. That said, this study faced two major methodological challenges, discussed below, that may reduce the reliability of the obtained quantitative land-cover reconstructions: (1) the low number of PPEs and their origin and (2) restrictions with respect to the number, distribution, and type of available sites.
Twenty PPE sets were used which mostly originate from Europe and temperate northern China. The available PPEs were estimated from various environmental and ecological settings, which might cause regional differences in each PPE. And PPEs of different species within one family or genus were included in our mean PPE calculation for the family or genus, ignoring the inter-species differences. Also, some taxa have few available PPEs with significant differences (such as Abies, Larix, Juglans, Brassicaceae), and their mean PPE could fail to represent their real pollen productivities. These aspects can cause uncertainty in the mean PPE to some extent. However, we believe that the compiled PPE sets can be used to extract major broad-scale and long-term vegetation patterns because the regional differences in the PPE for most taxa are small compared to the large between-taxa differences. The mean PPEs used in this REVEALS modelling (Table 2) are broadly consistent with those obtained from Europe (Mazier et al., 2012). In addition, although there are no PPEs for the core from the Siberia taiga forest, available studies on modern pollen composition support the weightings in the applied PPEs for major taxa in terms of pollen under- or over-representation of vegetation abundance. For example, modern pollen investigations in north-eastern Siberia revealed that pollen records from northern Larix forest often have less than 13 % Larix pollen, confirming the low pollen productivity of Larix relative to over-represented pollen taxa such as Betula and Alnus (Pisaric et al., 2001a; Klemm et al., 2016). Similarly, a study on modern pollen in southern Siberia (transitional area of steppe and taiga) finds that Artemisia, Betula, and Pinus are high pollen producers compared to Larix (Pelánková et al., 2008). Also, despite Larix being the most common tree in taiga forest in north-central Mongolia, the pollen abundance of Larix is generally lower than 3 % (Ma et al., 2008), implying its low pollen productivity.
In this study, we attempt to reconstruct past landscape changes at a regional scale. Pollen signals from large lakes are assumed to reflect regional vegetation patterns (e.g. Sugita et al., 2010; Trondman et al., 2015). If large lakes are absent in a region, multiple small-sized sites can be used, although error estimates are usually large (Sugita, 2007; Mazier et al., 2012; Trondman et al., 2016). In our study, 70 % of the time slices for the 42 site groups include pollen data from large lakes (i.e. radii >390 m), which supports the reliability of REVEALS reconstructions (Table A3). However, sites are unevenly distributed and occasionally sites from different areas were combined into one group (G2, G6, G34), which might produce a different vegetation-change signal because of the broad distribution of these sites (Fig. 1). In addition, the linear interpolation of pollen abundances for time windows with few pollen data might be another source of uncertainty, particularly for the late Pleistocene and its broad time windows (Table 1). Finally, pollen signals from certain sites and during certain periods may be of water-runoff origin rather than aerial origin violating the assumption of the REVEALS model that pollen is transported by wind.
4.2 Driving factors of vegetation changes
On a glacial–interglacial scale, pollen-based reconstructed land-cover changes in northern Asia are generally consistent with the global climate signal (e.g. sea-surface temperature: Pailler and Bard, 2002; ice-core: Andersen et al., 2004; solar insolation: Laskar et al., 2004; and cave deposits: Cheng et al., 2016; Fig. A6). For example, the relatively high arboreal cover at 40 ka (e.g. G20) corresponds with the warm MIS 3 record from the Baikal region (Swann et al., 2005). The open landscape at 25 and 21 ka (e.g. G25, G36) reflects the cold and dry last glacial maximum (e.g. Swann et al., 2010). Furthermore, the relatively high arboreal cover during the Holocene is consistent with the warm and wet climate (occurring in most site groups). The primary vegetation change in north-eastern China (G29, G30) occurs in the early Holocene (11.5 and 10.5 ka), caused by the rapid increase in abundance of temperate deciduous trees, which may reflect the warmer climate and enhanced summer monsoon known from that region at the beginning of the Holocene (Hong et al., 2009; Liu et al., 2014).
A sensitivity analysis of model-based biome estimation reveals that precipitation plays an important or even dominant role in controlling vegetation changes in arid central Asia (e.g. Tian et al., 2018). The climate of central Asia during the early Holocene is inferred to be quite dry and moisture increase occurs at ca. 8 ka revealed by a series of multi-proxy syntheses (Chen et al., 2008, 2016; Xie et al., 2018) and model-based estimations (Jin et al., 2012). In the taiga–steppe transition zone (south-eastern Siberia and north-central Asia, e.g. G6, G12, G14, G18), a relatively open landscape is reconstructed for the early Holocene and abundances of forest taxa increase after ca. 8 ka, which are consistent with the moisture evolution, and imply the importance of moisture in controlling vegetation changes. Our results support the prediction of an expansion of steppe in the present forest–steppe ecotone of southern Siberia in response to a warmer and drier climate in the future (Tchebakova et al., 2009). During the late Holocene, the decreases in forest cover in the forest–steppe ecotone of north-central China and central Asia are ascribed to the drying or cooling climate, respectively, by sensitivity analysis (Tian et al., 2018). Previous studies argued that the enhanced human impacts might be important factors for the reduction in forest cover (e.g. Ren, 2007); however, our study fails to determine its contribution on vegetation changes.
High abundances of Larix or boreal deciduous woody taxa (mostly shrubs) pollen occur in northern Siberia (e.g. G28, G38, G39, G40) during the middle Holocene, which is now covered by tundra. This is consistent with non-vegetation climate records of a mid-Holocene temperature maximum (e.g. Biskaborn et al., 2012; Nazarova et al., 2013). This result indicates that the boreal treeline in northern Siberia reacts sensitively to warming on millennial timescales, which contrasts with the observed lack of response on a decadal timescale (Wieczoreck et al., 2017). This may point to a highly non-linear vegetation–climate relationship in northern Siberia.
Our results indicate that climate change is the major factor driving land-cover change in northern Asia on a long temporal scale. However, climate change cannot fully explain the changes in arboreal taxa abundance for the West Siberian Plain (G8, G9) and sandy places in central Yakutia (G23, G24, G25). In addition to climate, changes in permafrost condition (Vandenberghe et al., 2014) and fire regime may have played a central role in vegetation change. Larix is the dominant arboreal taxon during the early Holocene (between ca. 12 and 8 ka), which is replaced by evergreen conifer trees, mostly pine and spruce at 8 or 7 ka. Larix can survive on permafrost with an active-layer depth of <40 cm (Osawa et al., 2010) and a high fire frequency, while pine trees can only grow on soil with >1.5 m of active-layer depth (Tzedakis and Bennett, 1995), and spruce is a fire avoider. Probably the compositional change of boreal trees was not in equilibrium with climate but rather driven by changes in the permafrost and fire characteristics that were themselves affected by forest composition, resulting in complex feedback mechanisms. This explanation would be in agreement with the finding by Herzschuh et al. (2016) that the boreal forest composition of nearby refugia during a glacial period influences the initial interglacial forest composition that is then only slowly replaced by a forest composition that is in equilibrium with climate.
Population changes in herbivores could also be an important factor for vegetation change at a regional scale during certain intervals (Zimov et al., 1995; Guthrie, 2006). As with our pollen-based land-cover reconstruction, a circumpolar ancient DNA meta-barcoding study confirms the replacement of steppe-like tundra by moist tundra with abundant woody plants at the Pleistocene–Holocene transition (Willerslev et al., 2014). According to Zimov et al. (1995, 2012), such a change cannot be explained by climate change alone, and thus a reduced density of herbivores is considered to be a major driving factor of steppe composition reduction, since a reduced number of herbivores is insufficient to maintain the open steppe landscapes and so causes a decrease in steppe area (Zimov et al., 1995; Guthrie, 2006). Our land-cover reconstruction fails to address the contribution of herbivores to vegetation changes, but the extinction of herbivorous megafauna would add to the complexity of the interactions among vegetation, climate, and permafrost.
Regional vegetation based on pollen data has been estimated using the REVEALS model for northern Asia during the last 40 ka cal BP. Relatively closed land cover was replaced by open landscapes in northern Asia during the transition from MIS 3 to the last glacial maximum. Abundances of woody components increase again from the last deglaciation or early Holocene. Pollen-based REVEALS estimates of plant abundances should be a more reliable reflection of the vegetation as pollen may overestimate the turnover, and indicates that the vegetation was quite stable during the Holocene as only slight changes in the abundances of PFTs were recorded rather than mass expansion of new PFTs. From comparisons of our results with other data, we infer that climate change is likely the primary driving factor for vegetation changes on a glacial–interglacial scale. However, the extension of evergreen conifer trees since ca. 8–7 ka throughout Siberia could reflect vegetation–climate disequilibrium at a long-term scale caused by the interaction of climate, vegetation, fire, and permafrost, which could be a palaeo-analogue not only for the recent complex vegetation response to climate changes but also for the vegetation prediction in future.
The used fossil pollen dataset with the re-established age-depth model for each pollen record have been made publicly available in PANGAEA (https://doi.pangaea.de/10.1594/PANGAEA.898616, Cao et al., 2019).
LSC: liquid-scintillation counting; A: terrestrial plant macrofossil; B: non-terrestrial plant macrofossil; C: peat; D: pollen; U: unknown; E: total organic matter from silt; F: animal remains or shell; G: charcoal; H: CaCO3; I: tephra.
XC and UH initiated and designed the study; XC and FT performed the land-cover reconstruction; FL and MJG were involved with the methods of the reconstruction; NR and QX contributed pollen data; XC wrote the preliminary version of the article, on which all co-authors commented.
The authors declare that they have no conflict of interest.
This article is part of the special issue “Paleoclimate data synthesis and analysis of associated uncertainty (BG/CP/ESSD inter-journal SI)”. It is not associated with a conference.
The authors would like to express their gratitude to all the palynologists who, either directly or indirectly, contributed their pollen records and PPE results to our study. This research was supported by the German Research Foundation (DFG) and the PalMod project (BMBF). Furong Li and Marie-José Gaillard thank the Faculty of Health and Life Science of Linnaeus University (Kalmar, Sweden), the China-Swedish STINT Exchange Grant 2016–2018, and the Swedish Strategic Research Area on ModElling the Regional and Global Earth system (MERGE) for financial support. This study is a contribution to the Past Global Changes (PAGES) LandCover6k working group project.
This research has been supported by the German Research Foundation (DFG) and the PalMod project (BMBF).
The article processing charges for this open-access
publication were covered by a Research
Centre of the Helmholtz Association.
This paper was edited by Lukas Jonkers and reviewed by two anonymous referees.
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