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Advances in Meteorology
Volume 2016, Article ID 2450697, 11 pages
http://dx.doi.org/10.1155/2016/2450697
Research Article

Holocene Vegetation Succession and Response to Climate Change on the South Bank of the Heilongjiang-Amur River, Mohe County, Northeast China

1Key Laboratory of Vertebrate Evolution and Human Origins of Chinese Academy of Sciences, Institute of Vertebrate Paleontology and Paleoanthropology, Chinese Academy of Sciences, Beijing 100044, China
2University of Chinese Academy of Sciences, Beijing 100049, China

Received 3 February 2015; Revised 24 May 2015; Accepted 31 May 2015

Academic Editor: Steffen Mischke

Copyright © 2016 Chao Zhao et al. This is an open access article distributed under the Creative Commons Attribution License, which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

Abstract

Pollen samples from peat sediments on the south bank of the Heilongjiang River in northern Northeast China (NE China) were analyzed to reconstruct the historical response of vegetation to climate change since 7800 cal yr BP. Vegetation was found to have experienced five successions from cold-temperate mixed coniferous and broadleaved forest to forest-steppe, steppe-woodland, steppe, and finally meadow-woodland. From 7800 to 7300 cal yr BP, the study area was warmer than present, and Betula, Larix, and Picea-dominated mixed coniferous and broadleaved forests thrived. Two cooling events at 7300 cal yr BP and 4500 cal yr BP led to a decrease in Betula and other broadleaved forests, whereas herbs of Poaceae expanded, leading to forest-steppe and then steppe-woodland environments. After 2500 cal yr BP, reduced temperatures and a decrease in evaporation rates are likely to have resulted in permafrost expansion and surface ponding, with meadow and isolated coniferous forests developing a resistance to the cold-wet environment. The Holocene warm period in NE China (7800–7300 cal yr BP) could have resulted in a strengthening of precipitation in northernmost NE China and encouraged the development of broadleaved forests.

1. Introduction

At present, global warming and its possible ecological consequences have become the focus for governments around the world, the scientific community, and the general public [1, 2]. In tackling core issues, it is very important to evaluate the effects of climate change accurately [3]. The Holocene is the most recent geological epoch. The early Holocene experienced increased temperatures, the mid-Holocene was warm and humid, and the late Holocene cooled [4, 5], providing research models for future climate change [6]. Land vegetation is an important part of the global ecological system and responds profoundly to climate change; exploring this relation between vegetation and climate change in critical areas has thus become an important approach in assessing the likely environmental impact of future climate change.

NE China, which has typical land ecosystems (including forests, steppes, and wetland) [7], is located on the eastern margin of the Eurasian continent. The northern Greater Khingan Range (GKR), in the northernmost part of NE China (on the southern margins of the permafrost zone), contains cold-temperate coniferous forest. The permafrost layer is shallow and its temperature stability is relatively low in this area, so the region is highly sensitive to climate change [810]. Over the past century, there has been a clear degradation of permafrost in NE China. Its southern boundary has moved northward 20–30 km [1114]. This has caused a series of ecological and hydrological changes, resulting in wetland and forest degradation and other environmental problems. Permafrost wetlands in the northern GKR have been characterized by original wetland atrophy and new wetland expansion [13, 15, 16].

In recent years, research into the Holocene environment in this area has focused more on climatic and environmental reconstruction [17, 18] and concentrated on the Sanjiang Plains in the northeast [1921], the Changbai Mountains in the east [2227], Hulun Lake in the western GKR [28, 29], Dali Lake in the southern GKR [30], Moon Lake in central GKR [31, 32], and so forth. These studies have highlighted a significant warming in the early mid-Holocene, followed by a transition to a dry-cold climate in the late Holocene.

However, a longer and more detailed vegetation history of NE China is still needed to verify vegetation succession interpretative studies and vegetative responses to climate change. There have until now been no other records sufficiently reliable for testing how cold-temperate vegetation on the northern margins of NE China has responded to Holocene climate change. This study is based on pollen records derived from Holocene peat sediments on the south bank of the Heilongjiang River. It aims to reconstruct a vegetation succession history, explore vegetation succession responses to climate change (especially during the Holocene Megathermal), and provide evidence for the evaluation of the possible effects of future climate change.

2. Materials and Methods

2.1. Study Area

The northern GKR (52°32′–53°41′N, 121°15′–125°58′E) (Figure 1) is located in the transition zone between a semihumid and semiarid cold-temperate continental monsoon climate; it is controlled by the cold Siberian-Mongolian High (extremely cold and dry) in winter and is marginally affected by the Pacific High (warm and humid) in summer [7]. Based on the Mohe County meteorological station, mean annual temperature (MAT) is −4.9°C, minimum temperature is −52.3°C, and the ground is frozen for up to eight months per annum. Mean annual precipitation (MAP) is 403 mm, about 80% of which is concentrated in June–September [37, 38]. In the last half century, the interannual rainfall shows fluctuation and changed between 274 mm and 635 mm [39]. The annual evaporation is ~1000 mm.

Figure 1: Map of the study area. (a) Red rectangle indicates the study area. (b) Red dot shows the Beihong Section.

The Beihong Section (53°30′8.3′′N, 123°5′24.5′′E, altitude: 280 m a.s.l.), which is located in the north of Beihong Village, on the southern bank of the Heilongjiang River in Mohe County, is dominated by peat sediments from the upper reaches of the Heilongjiang River (Figure 1). The Heilongjiang (Amur) Valley in northern NE China is dominated by taiga vegetation, with Larix gmelinii as a typical vegetation type, including Betula Platyphylla forest, Pinus sylvestris var. mongolica forest, Picea forest, and Poaceae meadow [7, 40].

The GKR has been directly administered by the central government since the Yuan Dynasty (1206–1368 CE) [41, 42]. Its native inhabitants continued to hunt and gather until the onset of the Opium Wars (1840 CE), when its forests began to undergo large-scale exploitation [7, 43, 44]. Consequently, vegetation succession in the study area has been principally affected by natural factors, with relatively weak human influence during the Holocene. It is the ideal area to study vegetation succession and its responses to climate change.

2.2. Beihong Section Sample and Pollen Analysis

The Beihong Section is 260 cm thick. The sediments are mainly peat and silt. They are delineated as follows: 0–80 cm, dark brown peat layer; 80–220 cm, light gray silty clay; 220–260 cm, gray fine sandy silt.

26 samples taken at 10 cm intervals were prepared for pollen analysis, using conventional acid-alkali treatment and heavy liquid separation [45, 46]; they were then treated by acetolysis [47]. Lycopodium tablets were added to the samples in order to estimate pollen concentrations [48]. 315–646 pollen grains were counted from each sample; pollen percentages and concentrations were calculated based on total land pollen count. TILIA software was used to draw the pollen spectra, in which a CONISS module was used to calculate distances and cluster zoning based on the square root transformation of the pollen percentage data.

Detrended correspondence analysis (DCA) and principal component analysis (PCA) have been widely used in forest ecosystem, shrub communities, meadow grasslands, and other vegetation researches [16, 49, 50]. DCA is a sort of gradient analysis method, which can arrange samples or pollen-taxa in a certain space, and the ordination axes can reflect the ecological gradient to explain the relationship between plant communities and the environment [51]; PCA is a method of statistics to focus on a few comprehensive indexes from a set of variables and was applied to extract main gradient changes in vegetation. DCA and PCA figures were created by CANOCO 4.5 based on samples and the terrestrial pollen percentage data (of percentage >3%). PCA function in SPSS was used to generate the PCA F1 values, extracting more comprehensive information on the environment [22].

2.3. Chronology

Macroremains of leaves and peat selected from the samples were examined to obtain an accurate age-depth framework. AMS 14C dating was conducted at the Beta Analytic Radiocarbon Dating Laboratory in America, and three AMS 14C ages at depths of 75 cm, 155 cm, and 238 cm were obtained. Radiogenic 14C ages were calibrated to calendar ages based on IntCal13 [52] and an age-depth model was produced using OxCal4.2.4 [35] (Table 1). The Beihong Section shows a positive correlation between age and depth.

Table 1: AMS 14C dating results from the Beihong Section.

A chronosequence for the Beihong Section was established using linear interpolation and extrapolation methods based on three samples. The age of the base (260 cm) was calculated as 7800 cal yr BP; the top consists of modern deposits. Consequently, the Beihong Section presents a historically continuous sedimentary sequence (Figure 2). The sedimentation rate is higher in the lower segment of the section. The average sediment rate is 0.16 cm/yr between 260 cm and 155 cm and falls to an average of 0.02 cm/yr from 155 cm to 0 cm; as a consequence the lower segment of the section has a higher resolution than the upper part.

Figure 2: Beihong Section and age-depth model.

3. Results

3.1. Pollen Assemblages in the Beihong Section

53 families and genera of pollen were identified in the Beihong Section (Table 2). They are mainly broadleaved tree pollen (19%–54%) and herb pollen (28%–64%); Betula pollen (10%–45%) was the commonest of the broadleaved tree pollen, and Poaceae pollen was the most prominent of the herb pollen, with content ranging from 3% to 36%. Total pollen concentrations exhibited considerable variation, ranging from 2.9 × 102 to 1.9 × 106 grains/g.

Table 2: Pollen types in the Beihong Section.

Based on chronological changes in pollen percentages, five successions can be recognized from pollen spectra (Figure 3).

Figure 3: Pollen percentages and concentrations for the Beihong Section (the gray values to the right are magnified tenfold to emphasize changes in concentration).

In zone 1 (260–190 cm, 7800–7300 cal yr BP), Betula, Larix, Picea, Alnus, Cupressaceae, Pinus, and other kinds of tree pollen dominate pollen assemblages (55%–66%); of these, broadleaved tree pollen percentages, especially of Betula (22%–45%), were extremely high. Coniferous tree pollen content (10%–27%), mainly Larix (7%–16%) and Picea (2%–7%), was relatively high. Shrub and herb pollen percentages fluctuated from 34% to 45% and were dominated by Liliaceae pollen (1%–19%), with some Artemisia (3%–11%), Chenopodiaceae (2%–5%), and Poaceae pollen (3%–16%). Total pollen concentrations (2.9 × 102–2.0 × 104 grains/g) were relatively low.

In zone 2 (190–80 cm, 7300–4500 cal yr BP), spectra were dominated by Poaceae, Artemisia, Chenopodiaceae, and other kinds of herb pollen, with their total content ranging from 44% to 50%. Poaceae pollen percentages (9%–28%) clearly increased, whereas Liliaceae pollen content (0–6%) decreased. In contrast, tree pollen content decreased markedly, with Larix (5%–10%), Betula (21%–32%), and Pinus pollen percentages (0–4%) dropping markedly. Total pollen concentrations (6.7 × 103–4.5 × 104 grains/g) were relatively low.

In zone 3 (80–60 cm, 4500–3500 cal yr BP), this period was characterized by high percentages (48%–55%) of herb pollen, principally Thalictrum (3%–9%), Compositae (4%-5%), Sanguisorba (3%-4%), and Artemisia (8%–11%); Poaceae pollen content (11%–20%) decreased noticeably. Coniferous (19%–21%) and broadleaved tree pollen content (26%–32%) decreased, with Betula (17%–20%) and Picea pollen percentages (3%–5%) falling markedly. Total pollen concentrations (2.9 × 104–10.0 × 104 grains/g) increased slightly.

In zone 4 (60–40 cm, 3500–2300 cal yr BP), Herb pollen, dominated by Poaceae, Artemisia, and Sanguisorba, reached its peak values at 62%–64%; among them Poaceae (32%–36%), Artemisia (12%–18%), and Sanguisorba (5%–7%) pollen markedly increased, while Chenopodiaceae pollen content (about 1%) decreased. Coniferous tree pollen (6%–14%) decreased noticeably, with Larix, Cupressaceae, and Picea pollen falling to their lowest values, while Pinus pollen increased (1%–8%). Total pollen concentrations rose (1.8 × 105–4.3 × 105 grains/g).

In zone 5 (40–0 cm, 2300 cal yr BP-modern), coniferous tree pollen (17%–51%), especially Pinus pollen percentages (6%–21%), increased greatly, with some emergence of Larix (4%–13%) and Picea (3%–6%). Broadleaved tree pollen (29%–19%) decreased, especially Betula pollen content (18%–11%), which fell to its lowest value for the entire section. Herb pollen percentages (31%–55%) decreased, but Cyperaceae, Plantago, and Umbelliferae content increased to some extent. Total pollen concentrations (1.3 × 105–1.9 × 106 grains/g) increased.

3.2. DCA and PCA Results

Of the 26 samples taken from top to bottom of Beihong Section, 31 families and genera were analyzed using DCA. The first two ordination axes were drawn on a two-dimensional ordination map (Figure 4). The score value of each sample was distributed regularly on the plane composed of the first and second principal axes. Samples from the five pollen assemblages yielded separate, individual clusters, and these clear differences verified the accuracy of the zoning (Figure 3).

Figure 4: DCA results for 26 representative plant community samples from the Beihong Section.

According to PCA results for the principal families and genera (Figure 5), the first two principal component axes accounted for 79% of all the variables (the first axis for 69% and the second for 10%). Pinus, Betula, Chenopodiaceae, and Ericaceae are the four main taxa of the original data matrix, whose vector lengths represent their degree of effect and significance, while the importance of other taxa decreases accordingly. Relations between the main taxa present a certain regularity. The plants that registered the highest positive scores for the first component axis included Ericaceae, Caryophyllaceae, and other plant types; Betula, Picea, and other vegetation types yielded the lowest scores. Pinus and Poaceae scored the highest positive values on the second component axis; Chenopodiaceae, Ephedra, and other vegetation types scored lowest here.

Figure 5: PCA results for principal pollen from the Beihong Section.

4. Discussion

Stalagmite, ice core, ocean, lake sediment, and other high resolution records show that there was a significant warm period in the mid-Holocene, similar to a scenario encompassing a 1-2°C increase in average global temperatures [5, 5355]. Marcott et al. suggested that, based on 73 globally discrete records, temperatures during 10000–5000 cal yr BP were 0.7°C warmer than the late Holocene [4]. The reconstruction of the vegetation succession on the southern bank of the Heilongjiang River in northern NE China since 7800 cal yr BP provides an important basis for establishing climate and environment change and their effect on vegetation in a cold-temperate region in the Holocene.

Pollen analysis is the technique most widely used and pollen data are most reliable for the reconstruction of paleovegetation and paleoclimate. Understanding the relation between modern pollen and vegetation is a prerequisite for interpreting fossil pollen records correctly and improving the accuracy of past vegetation type and paleoclimate reconstruction [5658].

4.1. Pollen Source in Beihong Section

The lithology changed from fine detritus gyttja at the bottom to decomposed peat in the Beihong Section (Figure 2). It may indicate that the environment of sedimentation changed over time and this lithologic transition probably occurred as the site changed from lake to swamp [59].

Source areas and relative pollen representation are shown to depend on basin size [60]. In Beihong Section, 220–260 cm gray fine sandy silt may indicate the enhancement of water-carrying capacity. This may induce a relatively low total pollen concentration because of the poor depositional environment (Figure 3). In addition, surface pollen assemblages in the marsh always includes a large number of regional pollen types usually from aquatic plants [61]; meanwhile, the total pollen concentrations may increase due to favorable depositional environment (Figure 3).

Nevertheless, studies on alluvial pollen show that the differences between alluvial pollen assemblages are the result of different pollen origins [34]. Most studies in different environment of sedimentation show that despite containing some exotic ingredients, the modern pollen assemblages can reflect characteristics of plant community in the immediate area, and the main vegetation zones along the regional can be distinguished by their modern pollen spectra [33, 36, 5658, 6165]. Therefore, the transitions of the pollen assemblages of the terrestrial pollen percentage (with the pollen sum excluding aquatics) in Beihong Section are mainly the result of the vegetation succession in the study area.

4.2. Modern Pollen Representation and Climatic Implications

Surface pollen studies have established that there is a relationship among the pollen percentages as well as vegetation type and regional climate [64]. The studies on vegetation and modern pollen distribution show that pollen assemblages are correlated well with the vegetation types in NE China [33, 36, 63].

In addition, Betula and Pinus pollen is overrepresented. The existence of birch forests was thus indicated only when the Betula content exceeded 40%. Pine forest might exist when Pinus pollen percentages are more than 30%. Poaceae and Larix pollen is of low representative feature. Larix pollen contents accounted for only 15% in larch forest [57, 62, 66]. A higher proportion of Poaceae (24%) was the main characteristic of wetland shrub. Poaceae pollen contents are <10% in Poaceae grassland, with Artemisia and Chenopodiaceae pollen percentages being more than half of the total. Hence, a high representation of Artemisia and Chenopodiaceae was found. Cyperaceae and Ephedra appeared in the middle or low relative representation values [33, 57].

Larix gmelinii and Pinus sylvestris var. mongolica are dominated in cold-temperate zone. The relationship among Pinus pollen, temperature, and humidity is more complex. Pinus pollen contents rise rapidly with increasing humidity [36]. The distribution of spruce is in cold-temperate zone (average temperature is 0–8°C) in the northern part of NE China; others grow in the cold-wet subalpine zone between 1000 and 2000 m [67]. The abundance of Picea pollen generally increases along with the humidity rise [68]. The Betula pollen count in topsoil of northern China is affected mainly by annual precipitation and will rise consistent with the increase of the amount of precipitation [67, 68].

Poaceae pollen is abundant in fossil records and is often used as a paleoclimatic indicator [69]. Poaceae pollen always concentrated in low temperature and high humidity area or semiarid warm zone, and its abundance increases with the decrease of temperature, as well as the increase of precipitation in low temperature and high humidity area [67]. The abundances of Chenopodiaceae and Ephedra pollen increased with increasing aridity; Compositae and Plantago pollens appear at low temperature and high humidity area [67, 68].

4.3. Vegetation Succession in Beihong Area

Based on the pollen assemblages and the modern pollen analysis, the vegetation history in Beihong area has experienced five chronosequences since 7800 cal yr BP.(1)In 7800–7300 cal yr BP, Betula pollen percentage is at the highest level of the section, up to 45%. Larix content (7%–16%) is also relatively high. The pollen assemblage may indicate that the study area developed Larix and Betula dominated cold-temperate coniferous and broadleaved mixed forest.(2)In 7300–4500 cal yr BP, herb pollens increase (>44%). Poaceae pollen percentages range from 9% to 28%, while Betula (<32%), Larix (<10%), Pinus pollen (<4%), and other tree pollen contents decreased markedly, suggesting a forest-steppe vegetation type.(3)In 4500–3500 cal yr BP, herb pollen increases, including Thalictrum, Compositae, Sanguisorba, and Artemisia. Tree pollen percentages decrease markedly, with Betula pollen ranging from 17% to 20%. Pollen assemblages indicate steppe-woodland.(4)In 3500–2300 cal yr BP, pollen records reveal Poaceae (32%–36%), Artemisia, and Sanguisorba dominated steppe vegetation type.(5)In 2300 cal yr BP-modern, pollen assemblages indicate that Poaceae, Cyperaceae, and other mesophydrophyte-dominated meadow vegetation developed, along with an expansion in isolated coniferous forests composed largely of Pinus pollen (up to 21%). These pollen assemblages are characterized by meadow-woodland vegetation.

4.4. Vegetation Response to Climate Change

Climate change has an important impact on terrestrial ecosystems [7072]. Similarly, vegetation successions in different regions are a good indicator of climate change and are an important index for revealing the environmental impact of climate change. Fossil pollen diagrams can be assumed to reflect information about natural vegetation dynamics and provide the evidence for the behavior of plant taxa when subjected to major climatic and environmental changes in the past [64].

The vegetation history mainly experienced a clear decrease in Betula and other broadleaved trees, while Poaceae-dominated herbs increased in the study area (Figure 3). The pollen samples exhibited five vegetation successions, from coniferous and deciduous mixed forest at the section’s base, upward to forest-steppe, steppe-woodland, steppe, and meadow-woodland, transitioning from a forest vegetation cover, resistant to a cold-dry environment to meadow-woodland vegetation and then to cold-wet environs (Figure 4). These vegetation types and the succession process had similar records at high latitudes.

Herbaceous plants, such as Cyperaceae and Poaceae, are the most important components of wetland communities [73]. Alpine vegetation occurs from the treeline to the snow line, whose important taxa include Cyperaceae, Poaceae, Compositae, Ericaceae, Caryophyllaceae, and Rosaceae [74]. The Holocene pollen diagram from eastern Canadian Arctic Island showed that there was virtually no Betula pollen present in very cold temperature, while Poaceae pollen with varying amounts of Ericaceae and Caryophyllaceae dominated the pollen assemblages [75]. Vegetation history of the western America in the Holocene shows that the lower subalpine communities are usually closed forests, and upper communities are steppe-woodland and shrublands. Based on the meteorological data of Changbai Mountain, the distribution age of Betula ermanii was in the trend of decreasing with elevation rising in the ecotone between Betula ermanii and alpine tundra [76]. Therefore, vegetation dominated by Betula might reflect a relatively warmer environment than the later meadow-woodland community in Beihong Section.

Consequently, DCA reflected a clear relation between different plant communities as well as between plant communities and the environment. The first axis can reflect the temperature gradients for different plant communities, with ability to resist the cold strengthening leftward along the axis; the second axis can indicate changes in humidity, with a plant community’s ability to withstand drought strengthening upward along the axis. The first principal component of PCA reflected temperatures and the second changes in humidity.

The PCA F1 scores of the taxa on the first principal component axis better reflected the pollen percentage variations with temperature; that is, higher values may represent cold and lower values warm climates (Figure 5). The PCA F1 curve thus revealed that temperatures have fluctuated downward decreased since 7800 cal yr BP (Figure 6), in tandem with reductions in insolation in northern hemisphere high latitudes [77].

Figure 6: Comparison of principal pollen percentages and the PCA F1 curve from the Beihong Section with other selected proxy records. (a) Pollen index from the Beihong Section. From the right to left are the PCA F1 curve, the percentage curves of broadleaved trees, Betula, herb, Poaceae, Pinus, and Cyperaceae. (b) Dongge Cave D4 [33]. (c) Holocene drift ice record for the MC52-VM29-191 North Atlantic core [34]. (d) Northern Hemisphere July insolation at 65°N [35] and the residual atmospheric Δ14C record (~2000-year moving average) [36]. The lateral gray bands trace the interconnection between climate cooling, drift ice, a weakened EASM, reduced insolation activity, and the principal pollen taxa changes in this study. The red boxes show the main indicator plants of vegetation type conversion.

In order to better reflect the response of vegetation to climate change, the principal pollen percentages and the PCA F1 curve from the Beihong Section were compared with high-resolution climate indices from other regions (Figure 6). Results suggested that the warmest and wettest stage in the Holocene occurred at ~7800–7300 cal yr BP, when MAT and MAP suited the growth of coniferous and broadleaved mixed forest in the study area. After 7300 cal yr BP, a decrease in Betula and other broadleaved trees and an increase in Poaceae and other herbs, as well as in Pinus, Cyperaceae, and other plants resistant to the cold-wet environs of the late Holocene, correspond to documented cooling events and reduced insolation activity [78].

The Beihong Section shows that the area had developed Betula, Larix, and Picea-dominated coniferous and broadleaved mixed forests, with Liliaceae prevalent in the undergrowth during 7800–7300 cal yr BP. Such vegetation indicates a warm and humid climate and essentially agrees with the findings of many other surveys, such as those conducted at Hulun Lake in the western GKR [29], the Qindeli Section on the Sanjiang Plains [20], Hokkaido Island [79], the Kuril Islands [80], the eastern Siberian Yakutia Lake [61], and Sakhalin [79].

At ~7300 cal yr BP and ~4500 cal yr BP, warmth-loving broadleaved trees clearly decreased in number in the study area, while cold-tolerant herbs increased (Figure 6). Vegetation cover changed from mixed coniferous and broadleaved forest to forest-steppe and steppe-woodland. The two significant cooling events which had a profound impact on vegetation succession are consistent with the significant ice event identified in North Atlantic records [81] and with the weakened East Asian Summer Monsoon (EASM) revealed in stalagmite oxygen isotope records from Dongge Cave [5, 82]. At ~2500–1500 cal yr BP, broadleaved trees, Poaceae, and mesophytes-xerophytes taxa declined, while Pinus and Cyperaceae vegetation expanded. Plant type was affected by paludification, indicating that global climate cooling had a profound influence on vegetation.

The cooling event at ~7300 cal yr BP, which resulted in a vegetation succession from mixed coniferous and broadleaved forest to forest-steppe, also appears in pollen records from Moon Lake in the central GKR [31] and the Buguldeika Core from Baikal Lake [83]. The cooling event at ~4500 cal yr BP, which may have global parallels, appears in the pollen records from Erlongwan Maar Lake [84], the Gushantun Bog in Jilin [85], and Hokkaido in Japan [86]. Vegetation shows a succession from forest-steppe to steppe-woodland. The cooling during ~2500–1500 cal yr BP in the Beihong area is also apparent in paleoenvironmental records from Hulun Lake in the western GKR [29], Moon Lake in the central GKR [31], Dali Lake in the southern GKR [30], Jingpo Lake in NE China [24], and Hokkaido Island in Japan [79, 80].

Many studies show that there is a complex interaction of climatic and ecological processes in boreal permafrost formation and degradation [73, 87, 88]. Permafrost is directly influenced by climate; climate and permafrost are among the principal driving forces of vegetation establishment and successional change across Siberia [89, 90]. The investigation of potential vegetation cover progression during the Siberian Bioclimatic Model shows that permafrost is predicted to thaw. The future much warmer and drier climate would be suitable for the forest-steppe ecotone and grasslands rather than forests, and water-stress-tolerant light larch (Larix dahurica) taiga will continue to be the dominant zonobiome over eastern Siberia [89].

Accordingly, it can be predicted that falling global temperatures and a weakening EASM gave rise to decreased rates of evaporation and an increase in effective humidity levels in the late Holocene. At the same time, an expansion in permafrost led to precipitation and runoff being unable to seep underground, causing surface ponding, marsh expansion, and peat development [13]. As a result, the vegetation type changed gradually to meadow and swamp-meadow, with isolated areas of cold-wet tolerant coniferous woodland [91] and a severe reduction in warmth-loving broadleaved trees. The long-term data from our studies (especially during the Holocene Megathermal) in the permafrost ecosystem suggest that responses of vegetation to climate warming might be the thaw of permafrost which will be deep enough to sustain the growth of Betula and Larix dominated taiga in south bank of Heilongjiang-Amur River [89].

5. Conclusions

The pollen records of peat sediments from the southern bank of the Heilongjiang River in northernmost NE China show that the period 7800–7300 cal yr BP was the warmest and wettest stage of the Holocene. At that time, the study area developed Betula and Larix-dominated mixed coniferous and broadleaved forest. This indicates that increases in temperature and precipitation were conducive to the growth of broadleaved forests in the study area. At ~7300 cal yr BP and ~4500 cal yr BP, two significant cooling events resulted in a reduction in broadleaved forests and an expansion of herbs, with a vegetation succession into forest-steppe and then steppe-woodland. After a decrease in temperatures during ~2500–1500 cal yr BP, the vegetation type changed into meadow, accompanied by the development of “islands” of cold-wet tolerant coniferous forest. In the late Holocene, lower global temperatures and a weakening EASM led to decreases in evaporation and increases in effective humidity; the expansion of permafrost might have hindered the infiltration of precipitation and runoff, causing surface ponding and an expansion in marsh and meadow vegetation.

Conflict of Interests

The authors declare that there is no conflict of interests regarding the publication of this paper.

Acknowledgments

The authors sincerely thank the editor and other anonymous two reviewers for their thoughtful reviews and constructive suggestions, which helped to improve the paper. This research was supported by the CAS Strategic Priority Research Program (Grant no. XDA01020304), the National Basic Research Program of China (Grant no. 2015CB953803), and the National Natural Science Foundation of China (Grant no. 41372175). The authors thank Hanbin Liu and Qiang Gao for assistance with fieldwork.

References

  1. Intergovernmental Panel on Climate Change (IPCC), Climate Change 2013: The Physical Sciences Basis, Cambridge University Press, New York, NY, USA, 2013.
  2. M. E. Mann, Z. H. Zhang, M. K. Hughes et al., “Proxy-based reconstructions of hemispheric and global surface temperature variations over the past two millennia,” Proceedings of the National Academy of Sciences of the United States of America, vol. 105, no. 36, pp. 13252–13257, 2008. View at Publisher · View at Google Scholar · View at Scopus
  3. Z. L. Ding, X.-N. Duan, Q.-S. Ge, and Z.-Q. Zhang, “On the major proposals for carbon emmission reduction some related issues,” Science in China Series D: Earth Sciences, vol. 39, no. 12, pp. 1659–1671, 2009. View at Google Scholar
  4. S. A. Marcott, J. D. Shakun, P. U. Clark, and A. C. Mix, “A reconstruction of regional and global temperature for the past 11,300 years,” Science, vol. 339, no. 6124, pp. 1198–1201, 2013. View at Publisher · View at Google Scholar · View at Scopus
  5. Y.-J. Wang, H. Cheng, R. L. Edwards et al., “The holocene Asian monsoon: links to solar changes and North Atlantic climate,” Science, vol. 308, no. 5723, pp. 854–857, 2005. View at Publisher · View at Google Scholar · View at Scopus
  6. Y. F. Shi, Z. C. Kong, S. M. Wang et al., “The climate variation and important events during Holocene Megethemal in China,” Science in China Series B, vol. 22, no. 12, pp. 1300–1308, 1992. View at Google Scholar
  7. Y. L. Zhou, Y. G. Zu, D. Yu et al., Geography of the Vegetation in Northeast China, Science Press, Beijing, China, 1997.
  8. X. C. Wu, H. Y. Liu, D. L. Guo, O. A. Anenkhonov, N. K. Badmaeva, and D. V. Sandanov, “Growth decline linked to warming-induced water limitation in Hemi-Boreal forests,” PLoS ONE, vol. 7, no. 8, Article ID e42619, 2012. View at Publisher · View at Google Scholar · View at Scopus
  9. M. Lu, F. Zhang, and S.-Z. Feng, “Climate change and its impact on the agriculture of the Greater Khingan Range area in resent 30 years,” Climate in Inner Mongolia, no. 3, pp. 35–37, 2005. View at Google Scholar
  10. G.-L. Tang and G.-Y. Ren, “Reanalysis of surface air temperature change of the last 100 years over China,” Climatic and Environmental Research, vol. 10, no. 4, pp. 791–798, 2005. View at Google Scholar
  11. H.-J. Jin, S.-P. Yu, D.-X. Guo, L.-Z. Lu, and Y.-W. Li, “Degradation of permafrost in the Da and Xiao Hinggan Mountains, northeast China, and preliminary assessment of its trend,” Journal of Glaciology and Geocryology, vol. 28, no. 4, pp. 467–476, 2006. View at Google Scholar
  12. J. Shi, G. Y. Wang, C.-Y. Du, and P. Wang, “Distribution and characteristic of permafrost of Heilongjiang Province,” Heilongjiang Meteorology, vol. 3, pp. 32–34, 2003. View at Google Scholar
  13. M. Zhou, X.-X. Yu, L. Feng, L.-H. Wang, and P.-S. Na, “Effects of permafrost and wetland in forests in Great Xing'an Mountains on ecology and environment,” Journal of Beijing Forestry University, vol. 25, no. 6, pp. 91–93, 2003. View at Google Scholar
  14. J. Tan and X.-H. Li, “The impact of the climate warming on degradation the Great Hinggan Mountains permafrost and northward movement of Larix gmelinii,” Inner Mongolia Forestry Investigation and Design, vol. 1, pp. 25–31, 1995. View at Google Scholar
  15. Y.-Z. Zhao, Z.-L. Gao, M. Zhao, and L. Wang, “The influence of climate change on forest and wetland ecosystems at Mohe region,” Science & Technology Information, pp. 449–450, 2012. View at Google Scholar
  16. S. Ju, X.-Z. Li, Y.-M. Hu et al., “Classification, species diversity, and species distribution gradient of permafrost wetland plant communities in Great Xing’an Mountains valleys of Northeast China,” Chinese Journal of Applied Ecology, vol. 20, no. 9, pp. 2049–2056, 2009. View at Google Scholar · View at Scopus
  17. G.-Y. Ren, “Changes in forest cover in China during the Holocene,” Vegetation History and Archaeobotany, vol. 16, no. 2-3, pp. 119–126, 2007. View at Publisher · View at Google Scholar · View at Scopus
  18. G.-Y. Ren, “Wetness changes of the Holocene in northeast China,” Geological Review, vol. 45, no. 3, pp. 255–264, 1999. View at Google Scholar
  19. C. Y. Gao, K. S. Bao, Q. X. Lin et al., “Characterizing trace and major elemental distribution in late Holocene in Sanjiang Plain, Northeast China: paleoenvironmental implications,” Quaternary International, vol. 349, pp. 376–383, 2014. View at Publisher · View at Google Scholar · View at Scopus
  20. X.-Q. Li, H.-L. Zhao, M.-H. Yan, and S.-Z. Wang, “Fire variations relationship among fire and vegetation and climate during Holocene at Sanjiang Plain, Northeast China,” Scientia Geographica Sinica, vol. 25, no. 2, pp. 177–182, 2005. View at Google Scholar
  21. S. Q. Zhang, W. Deng, M. H. Yan, X. Q. Li, and S. Z. Wang, “Pollen record and forming process of the peatland in late Holocene in the north bank of Xingkai Lake, China,” Wetland Science, vol. 2, no. 2, pp. 110–115, 2004. View at Google Scholar
  22. D. K. Xu, H. Y. Lu, G. Q. Chu et al., “500-year climate cycles stacking of recent centennial warming documented in an East Asian pollen record,” Scientific Reports, vol. 4, article 3611, 2014. View at Publisher · View at Google Scholar · View at Scopus
  23. J. Zhu, J. Mingram, and A. Brauer, “Early Holocene aeolian dust accumulation in northeast China recorded in varved sediments from Lake Sihailongwan,” Quaternary International, vol. 290-291, pp. 299–312, 2013. View at Publisher · View at Google Scholar · View at Scopus
  24. C. H. Li, Y. H. Wu, and X. H. Hou, “Holocene vegetation and climate in Northeast China revealed from Jingbo Lake sediment,” Quaternary International, vol. 229, no. 1-2, pp. 67–73, 2011. View at Publisher · View at Google Scholar · View at Scopus
  25. B. Hong, C. Q. Liu, Q. H. Lin et al., “Temperature evolution from the δ18O record of Hani peat, Northeast China, in the last 14000 years,” Science in China, Series D: Earth Sciences, vol. 52, no. 7, pp. 952–964, 2009. View at Publisher · View at Google Scholar · View at Scopus
  26. Y. T. Hong, B. Hong, Q. H. Lin et al., “Synchronous climate anomalies in the western North Pacific and North Atlantic regions during the last 14,000 years,” Quaternary Science Reviews, vol. 28, no. 9-10, pp. 840–849, 2009. View at Publisher · View at Google Scholar · View at Scopus
  27. M. Stebich, J. Mingram, J. Han, and J. Liu, “Late Pleistocene spread of (cool-)temperate forests in Northeast China and climate changes synchronous with the North Atlantic region,” Global and Planetary Change, vol. 65, no. 1-2, pp. 56–70, 2009. View at Publisher · View at Google Scholar · View at Scopus
  28. R.-L. Wen, J. L. Xiao, Z. G. Chang et al., “Holocene precipitation and temperature variations in the East Asian monsoonal margin from pollen data from Hulun Lake in northeastern Inner Mongolia, China,” Boreas, vol. 39, no. 2, pp. 262–272, 2010. View at Publisher · View at Google Scholar · View at Scopus
  29. R.-L. Wen, J.-L. Xiao, Z.-G. Chang et al., “Holocene climate changes in the mid-high-latitude-monsoon margin reflected by the pollen record from Hulun Lake, northeastern Inner Mongolia,” Quaternary Research, vol. 73, no. 2, pp. 293–303, 2010. View at Publisher · View at Google Scholar · View at Scopus
  30. J. L. Xiao, B. Si, D. Y. Zhai, S. Itoh, and Z. Lomtatidze, “Hydrology of Dali lake in central-eastern Inner Mongolia and Holocene East Asian monsoon variability,” Journal of Paleolimnology, vol. 40, no. 1, pp. 519–528, 2008. View at Publisher · View at Google Scholar · View at Scopus
  31. J. Wu and Q. Liu, “Charcoal-recorded climate changes from Moon Lake in Late Glacial, Chinese,” Earth Science—Journal of China University of Geosciences, vol. 37, no. 5, pp. 947–954, 2012. View at Google Scholar
  32. Q. Liu, Q. Li, L. Wang, and G. Q. Chu, “Stable carbon isotope record of bulk organic matter from a sediment core at Moon Lake in the middle part of the Daxing'an Mountain Range, northeast China during the last 21 ka,” Quaternary Sciences, vol. 30, no. 6, pp. 1069–1077, 2010. View at Google Scholar
  33. Y. Li, X. Zhang, and G. Zhou, “Quantitative relationships between vegetation and several pollen taxa in surface soil from North China,” Chinese Science Bulletin, vol. 45, no. 16, pp. 1519–1523, 2000. View at Publisher · View at Google Scholar · View at Scopus
  34. S. A. Hall, “Pollen analysis and paleoecology of alluvium,” Quaternary Research, vol. 31, no. 3, pp. 435–438, 1989. View at Publisher · View at Google Scholar · View at Scopus
  35. C. B. Ramsey and S. Lee, “Recent and planned developments of the program OxCal,” Radiocarbon, vol. 55, no. 2-3, pp. 720–730, 2013. View at Publisher · View at Google Scholar · View at Scopus
  36. Q. H. Xu, Y. C. Li, X. L. Yang, and Z. H. Zheng, “Quantitative relationship between pollen and vegetation in northern China,” Science in China, Series D: Earth Sciences, vol. 50, no. 4, pp. 582–599, 2007. View at Publisher · View at Google Scholar · View at Scopus
  37. L. L. Wang, X. M. Shao, L. Huang, and E. Y. Liang, “Tree-ring characteristics of Larix emelinii and Pinus sylvestris var. mongolica and their response to climate in Mohe, China,” Acta Phytoecologica Sinica, vol. 29, no. 3, pp. 380–385, 2005. View at Google Scholar
  38. D. X. Guo, S. L. Wang, G. W. Lu, J. B. Dai, and E. Y. Li, “Division of permafrost regions in Daxiao Hinggan Ling northeast China,” Journal of Glaciology and Geocryology, vol. 3, no. 3, pp. 1–9, 1981. View at Google Scholar
  39. H. L. Gui, X. H. Zhang, C. H. Wang, L. Huang, and G. S. Wu, “Mohe County climate change trend analysis during the last 50 years,” Modernization Agriculture, no. 6, pp. 24–26, 2009. View at Google Scholar
  40. Editorial Committee of Vegetation Map of China. Chinese Academy of Sciences, Vegetation Map of the People's Republic of China (1:1000,000), Geological Publishing House, Beijing, China, 2007.
  41. Y. Lan, Chinese Historical Geography, Higher Education Press, Beijing, China, 2002.
  42. J. S. Feng, “The origin of the Oroqen nationality,” Jilin Normal University Journal, no. 2, pp. 77–85, 1979. View at Google Scholar
  43. G. Y. Ren, “Decline of the mid-to late Holocene forests in China: climatic change or human impact?” Journal of Quaternary Science, vol. 15, no. 3, pp. 273–281, 2000. View at Publisher · View at Google Scholar · View at Scopus
  44. S. G. Zhu, “Vegetation changes during the history in Northeast China,” Journal of Chinese Historical Geography, vol. 4, pp. 105–119, 1992. View at Google Scholar
  45. X.-Q. Li and N.-Q. Du, “The acid-alkali-free analysis of Quaternary pollen,” Acta Botanica Sinica, vol. 41, no. 7, pp. 782–784, 1999. View at Google Scholar · View at Scopus
  46. K. Feagri and J. Iversen, Textbook of Pollen Analysis, Blackwell, Oxford, UK, 3rd edition, 1989.
  47. G. Erdtman, “The acetolysis method. A revised description,” Svensk Botanisk Tidskrift, vol. 54, pp. 561–564, 1960. View at Google Scholar
  48. R. M. Peck, “A comparison of four absolute pollen preparation techniques,” New Phytologist, vol. 73, no. 3, pp. 567–587, 1974. View at Publisher · View at Google Scholar
  49. B.-R. Chen, Y.-X. Zhu, H. B. Zhang, L. Zhou, and X. P. Xin, “Quantitative classification and ordination of eadow grassland vegetations in Hulunber,” Journal of Wuhan Botanical Research, vol. 26, no. 5, pp. 476–481, 2008. View at Google Scholar
  50. X. C. Wang, “A pollen profile from the permafrost region in southwest Yukon territory and its paleoenvironmental significance,” Journal of Glaciology and Geocryology, vol. 11, no. 2, pp. 99–112, 1989. View at Google Scholar
  51. M. O. Hill and H. G. Gauch Jr., “Detrended correspondence analysis: an improved ordination technique,” Vegetatio, vol. 42, no. 1–3, pp. 47–58, 1980. View at Publisher · View at Google Scholar · View at Scopus
  52. P. J. Reimer, E. Bard, A. Bayliss et al., “IntCal13 and Marine13 radiocarbon age calibration curves 0–50,000 years cal BP,” Radiocarbon, vol. 55, no. 4, pp. 1869–1887, 2013. View at Publisher · View at Google Scholar · View at Scopus
  53. Intergovernmental Panel on Climate Change (IPCC), Climate Change 2007: The Physical Sciences Basis, Cambridge University Press, New York, NY, USA, 2007.
  54. M. Tan, A. Baker, D. Genty, C. Smith, J. Esper, and B. Cai, “Applications of stalagmite laminae to paleoclimate reconstructions: comparison with dendrochronology/climatology,” Quaternary Science Reviews, vol. 25, no. 17-18, pp. 2103–2117, 2006. View at Publisher · View at Google Scholar · View at Scopus
  55. D. X. Yuan, H. Cheng, R. L. Edwards et al., “Timing, duration, and transitions of the last interglacial Asian monsoon,” Science, vol. 304, no. 5670, pp. 575–578, 2004. View at Publisher · View at Google Scholar · View at Scopus
  56. Z. Zheng, K. Y. Huang, Q. H. Xu et al., “Comparison of climatic threshold of geographical distribution between dominant plants and surface pollen in China,” Science in China, Series D: Earth Sciences, vol. 51, no. 8, pp. 1107–1120, 2008. View at Publisher · View at Google Scholar · View at Scopus
  57. Y. Zhao and U. Herzschuh, “Modern pollen representation of source vegetation in the Qaidam Basin and surrounding mountains, north-eastern Tibetan Plateau,” Vegetation History and Archaeobotany, vol. 18, no. 3, pp. 245–260, 2009. View at Publisher · View at Google Scholar · View at Scopus
  58. Q. Xu, F. Tian, M. J. Bunting et al., “Pollen source areas of lakes with inflowing rivers: modern pollen influx data from Lake Baiyangdian, China,” Quaternary Science Reviews, vol. 37, pp. 81–91, 2012. View at Publisher · View at Google Scholar · View at Scopus
  59. D. S. Sea and C. Whitlock, “Postglacial vegetation and climate of the Cascade Range, central Oregon,” Quaternary Research, vol. 43, no. 3, pp. 370–381, 1995. View at Publisher · View at Google Scholar · View at Scopus
  60. I. C. Prentice, “Pollen representation, source area, and basin size: toward a unified theory of pollen analysis,” Quaternary Research, vol. 23, no. 1, pp. 76–86, 1985. View at Publisher · View at Google Scholar · View at Scopus
  61. S. Sugita, “A model of pollen source area for an entire lake surface,” Quaternary Research, vol. 39, no. 2, pp. 239–244, 1993. View at Publisher · View at Google Scholar · View at Scopus
  62. M. J. Bunting, M.-J. Gaillard, S. Sugita, R. Middleton, and A. Broström, “Vegetation structure and pollen source area,” The Holocene, vol. 14, no. 5, pp. 651–660, 2004. View at Publisher · View at Google Scholar · View at Scopus
  63. C. Prentice, “Records of vegetation in time and space: the principles of pollen analysis,” in Vegetation History, vol. 7 of Handbook of Vegetation Science, pp. 17–42, Springer, Dordrecht, The Netherlands, 1988. View at Publisher · View at Google Scholar
  64. B. V. Odgaard, “Fossil pollen as a record of past biodiversity,” Journal of Biogeography, vol. 26, no. 1, pp. 7–17, 1999. View at Publisher · View at Google Scholar · View at Scopus
  65. S. H. Yu, Z. Zheng, K. Y. Huang, and M. I. Skrypnikova, “Modern pollen distribution in the Heilongjiang-Amur cold-temperate regions of China and Russia,” Acta Palaeontologica Sinica, vol. 51, no. 3, pp. 370–384, 2012. View at Google Scholar
  66. X. J. Sun, F. Y. Wang, and C. Q. Song, “Pollen-climate response surfaces of selected taxa from Northern China,” Science in China, Series D: Earth Sciences, vol. 39, no. 5, pp. 486–493, 1996. View at Google Scholar · View at Scopus
  67. H. Y. Liu and Y. Y. Li, “Pollen indicators of climate change and human activities in the semi-arid region,” Acta Palaeontologica Sinica, vol. 48, no. 2, pp. 211–221, 2009. View at Google Scholar
  68. X. H. Wu, “A study of palaeotemperatures recorded by the Pleistocene Picea-Abies floras in east and southwest China,” Bulletin of the Institute of Geomechaincs CAGS, vol. 6, pp. 155–166, 1985. View at Google Scholar
  69. M. B. Bush, “On the interpretation of fossil Poaceae pollen in the lowland humid neotropics,” Palaeogeography, Palaeoclimatology, Palaeoecology, vol. 177, no. 1-2, pp. 5–17, 2002. View at Publisher · View at Google Scholar · View at Scopus
  70. J. Y. Fang, Y. H. Tang, J. D. Lin, and G. M. Jiang, Global Ecology: Climate Change and Ecological Responses, Higher Education Press, Beijing, China, 2000.
  71. P. J. Bartlein, I. C. Prentice, and T. Webb III, “Climatic response surfaces from pollen data for some eastern North American taxa,” Journal of Biogeography, vol. 13, no. 1, pp. 35–57, 1986. View at Publisher · View at Google Scholar · View at Scopus
  72. B. Huntley and H. J. B. Birks, An Atlas of Past and Present Pollen Maps for Europe: 0–13000 B.P., Cambridge University Press, Cambridge, UK, 1983.
  73. A. Miola, A. Bondesan, L. Corain et al., “Wetlands in the Venetian Po Plain (northeastern Italy) during the Last Glacial Maximum: interplay between vegetation, hydrology and sedimentary environment,” Review of Palaeobotany and Palynology, vol. 141, no. 1-2, pp. 53–81, 2006. View at Publisher · View at Google Scholar · View at Scopus
  74. R. G. Baker, “Holocene vegetational history of the western United States,” in Late-Quaternary Environments of the United States: The Late Pleistocene, vol. 1, p. 109, University of Minnesota Press, 1983. View at Google Scholar
  75. J. T. Andrews, W. N. Mode, and P. T. Davis, “Holocene climate based on pollen transfer functions, eastern Canadian Arctic,” Arctic and Alpine Research, vol. 12, no. 1, pp. 41–64, 1980. View at Publisher · View at Google Scholar · View at Scopus
  76. Z. Yang-Jian, D. Li-Min, and P. Jie, “The trend of tree line on the northern slope of Changbai Mountain,” Journal of Forestry Research, vol. 12, no. 2, pp. 97–100, 2001. View at Publisher · View at Google Scholar
  77. A. Berger and M. F. Loutre, “Insolation values for the climate of the last 10 million years,” Quaternary Science Reviews, vol. 10, no. 4, pp. 297–317, 1991. View at Publisher · View at Google Scholar · View at Scopus
  78. P. J. Reimer, M. G. L. Baillie, E. Bard et al., “Residual delta 14C around 2000 year moving average of IntCal04,” Radiocarbon, vol. 46, no. 3, pp. 1029–1058, 2000. View at Google Scholar
  79. Y. Igarashi and A. E. Zharov, “Climate and vegetation change during the late Pleistocene and early Holocene in Sakhalin and Hokkaido, northeast Asia,” Quaternary International, vol. 237, no. 1-2, pp. 24–31, 2011. View at Publisher · View at Google Scholar · View at Scopus
  80. N. G. Razjigaeva, L. A. Ganzey, T. A. Grebennikova et al., “Holocene climatic changes and vegetation development in the Kuril Islands,” Quaternary International, vol. 290-291, pp. 126–138, 2013. View at Publisher · View at Google Scholar · View at Scopus
  81. G. Bond, W. Showers, M. Cheseby et al., “A pervasive millennial-scale cycle in North Atlantic holocene and glacial climates,” Science, vol. 278, no. 5341, pp. 1257–1266, 1997. View at Publisher · View at Google Scholar · View at Scopus
  82. C. A. Dykoski, R. L. Edwards, H. Cheng et al., “A high-resolution, absolute-dated Holocene and deglacial Asian monsoon record from Dongge Cave, China,” Earth and Planetary Science Letters, vol. 233, no. 1-2, pp. 71–86, 2005. View at Publisher · View at Google Scholar · View at Scopus
  83. P. Tarasov, E. Bezrukova, E. Karabanov et al., “Vegetation and climate dynamics during the Holocene and Eemian interglacials derived from Lake Baikal pollen records,” Palaeogeography, Palaeoclimatology, Palaeoecology, vol. 252, no. 3-4, pp. 440–457, 2007. View at Publisher · View at Google Scholar · View at Scopus
  84. Y. Y. Liu, S. Q. Zhang, J. Q. Liu, H. T. You, and J. T. Han, “Vegetation and environment history of Erlongwan Maar Lake during the late Pleistocene on pollen record,” Acta Micropalaeontologica Sinica, vol. 25, no. 3, pp. 274–280, 2008. View at Google Scholar
  85. J. L. Liu, “Vegetational and climatic changes at Gushantun bog in Jilin, NE China since 13,000 yr BP,” Acta Palaeontologica Sinica, vol. 28, no. 4, pp. 495–511, 1989. View at Google Scholar
  86. Y. Igarashi, “Holocene vegetation and climate on Hokkaido Island, northern Japan,” Quaternary International, vol. 290-291, pp. 139–150, 2013. View at Publisher · View at Google Scholar · View at Scopus
  87. Y. L. Shur and M. T. Jorgenson, “Patterns of permafrost formation and degradation in relation to climate and ecosystems,” Permafrost and Periglacial Processes, vol. 18, no. 1, pp. 7–19, 2007. View at Publisher · View at Google Scholar · View at Scopus
  88. P. Camill and J. S. Clark, “Long-term perspectives on lagged ecosystem responses to climate change: permafrost in boreal peatlands and the grassland/woodland boundary,” Ecosystems, vol. 3, no. 6, pp. 534–544, 2000. View at Publisher · View at Google Scholar · View at Scopus
  89. A. J. Soja, N. M. Tchebakova, N. H. F. French et al., “Climate-induced boreal forest change: predictions versus current observations,” Global and Planetary Change, vol. 56, no. 3-4, pp. 274–296, 2007. View at Publisher · View at Google Scholar · View at Scopus
  90. N. M. Tchebakova, E. Parfenova, and A. J. Soja, “The effects of climate, permafrost and fire on vegetation change in Siberia in a changing climate,” Environmental Research Letters, vol. 4, no. 4, Article ID 045013, 2009. View at Publisher · View at Google Scholar · View at Scopus
  91. C. C. Mou, “Succession of Larix olgensis and Betula platyphylla-marsh ecotone communities in Changbai Mountain,” Chinese Journal of Applied Ecology, vol. 14, no. 11, pp. 1813–1819, 2003. View at Google Scholar