During field campaigns in summers, 1991 and 1993, geological-geomorphological investigations were carried out about 20–40 km to the south of the El’gygytgyn Impact Crater, which included the sedimentological description and the sampling of five fluvial outcrops of the Enmyvaam, Mechekrynnetveem, and Chanuvenvaam Rivers (sections 118, 119, 120, 121, 124, Figure 1B). Sections 118 (67.250522°N, 172.268290°E, 433 m a.s.l.) and 119 (67.239552°N, 172.233839°E, 424 m a.s.l.) are situated on the left bank of Enmyvaam River, ∼6.5 km and 1.5 km above the Mechekrynnetveem-Enmyvaam river confluence, respectively. Sections 120 (67.243589°N, 172.306890°E, 439 m a.s.l.) and 121 (67.244438°N, 171.929236°E, 429 m a.s.l.) are situated on the right banks of the Mechekrynnetveem and Chanuvenvaam Rivers, ∼4.5 km and 3.5 km above their confluences with the Enmyvaam River. Further to the south, Section 124 (67.098098°N, 171.646010°E, 399 m a.sl.) is placed on the left bank of Enmyvaam River, ∼20 km downstream from the Enmyvaam-Chanuvenvaam confluence (Figure 1B).

The stratigraphic units of these sections were distinguished in the field based on bedding, grain size, and sediment colors. A total of 56 samples were collected for pollen analysis from pre- and post-impact deposits.

Pollen preparation was mainly carried out in the pollen lab of Alfred Wegener Institute for Polar and Marine Research (Potsdam) by a standard HF technique (Berglund and Ralska-Jasiewiczowa, 1986). A tablet of Lycopodium marker spores was added to the samples to allow for the calculation of total pollen and spore concentrations following Stockmarr (1971). No Lycopodium marker spores were added to the samples from section 124, which were prepared in the pollen lab of the North-East Interdisciplinary Scientific Research Institute (Magadan). In all cases, water-free glycerol was used for sample storage and preparation of microscopic slides.

Pollen and spores were identified at magnifications of 400X, with the aid of published pollen keys and atlases (Kupriyanova and Alyoshina, 1972, 1978; Bobrov et al., 1983; Reille, 1992, 1995, 1998). Where possible, at least 250 pollen grains were counted in each sample. Some samples contain only single pollen grains and therefore were either not used for paleoenvironmental reconstructions or used with caution. In addition to pollen and spores, non-pollen-palynomorphs (NPP), such as fungi spores as well as remains of algae and invertebrate, were identified and counted, if possible. NPP are valuable indicators of past environments, especially of local microhabitats (e.g., van Geel, 2001 and references therein). The percentages of pollen taxa were calculated from the sum of terrestrial pollen taxa. The percentages of spores, NPP, and algae are based on the sums of pollen and spores, pollen and NPP, and pollen and algae, respectively.

To consider wildfires as factors influencing the vegetation composition, charcoal concentrations were calculated in 16 samples from sections 119, 121, and 124. For this purpose, a minimum of 300 microscopic charcoal particles were counted together with Lycopodium spores. Microscopic charcoal particles were categorized into six charcoal morphotypes by adopting the classification scheme of Enache and Cumming (2007), which was developed for charcoal >150 μm and supported by biomass burn experiments (Mustaphi and Pisaric, 2014; Pereboom et al., 2020). We expect that the breakage of charcoal during pollen preparation preserves the original patterns of charcoal particle appearance (shape and opaqueness), which is related to the type of burnt biomass, with high opaqueness of particles qualitatively suggesting higher fire intensities (Conedera et al., 2009). We might slightly overestimate the relative amounts of elongated, fragile relative to the massive, blocky particles that are less breakable. The percentages of the charcoal morphotypes are based on the total charcoal counts.

TGView software (Grimm, 2004) was used for the calculation of percentages and for drawing the diagrams. The diagrams were zoned by a qualitative inspection of significant changes in pollen assemblages, pollen concentrations, and the occurrence of particularly indicative pollen and NPP taxa. Sediments from horizons with coarse material often contain no palynomorphs. These samples are not presented on the pollen diagrams.

The analyzed fluvial terrace sections are marked by a heterogeneous sediment thickness and lithological composition, and have been classified in the field into stratigraphic units of individual composition (see detailed descriptions in Table 1). In the c. 12 m thick section 118, a total of 11 loam- to pebble-rich stratigraphic units have been identified above bedrock basalts. Section 119 comprises 20 m of sediments consisting of five stratigraphic units above the current channel bed. In section 120, two units rich in black clay in the lower 5.5 m are overlain by five units of sand- to pebble-rich sediments in the upper 3.5 m. In the c. 18 m thick section 121, 18 units could be distinguished above a basaltic tuff. Section 124 comprises 30 m thick sediments above the current Enmyvaam channel, which were distinguished into 11 units. The “chaotic horizons,” which consist of sediments with a chaotic structure that contain glass spherules of up to several mm in size, have been preserved in sections 119 and 121. The macro- and microscopic appearance of these glass spherules is very similar to those found in the El’gygytgyn Crater and ICDP core from Lake El’gygytgyn (Smirnov et al., 2011; Goderis et al., 2013; Wittmann et al., 2013). Based on their geochemical composition the glass spherules from the “chaotic horizons” of the studied sections 119 and 121 have been attributed to the meteorite impact that formed the Lake El’gygytgyn crater (Smirnov et al., 2011).

The paleoecological results obtained on the investigated sections, complemented by examples of charcoal morphotypes and woody macrofossils found in the records, are presented in Figures 2–8.

A total of 44 different pollen, spore, and NPP types have been found in the 10 samples studied for palynomorphs from section 118, which consists of 12 stratigraphic units (Table 1 and Figure 3). The revealed pollen assemblages can be subdivided into 6 pollen zones (PZ).

PZ I (∼12.0–11.5 m) is dominated by Ericales, Betula, Pinus s/g Haploxylon, and Alnus fruticosa pollen as well as Sphagnum spores. There are rather numerous coniferous Picea, Abies, Larix and Poaceae pollen, Polypodiaceae spores, and remains of green algae colonies (Botryococcus). PZ II (∼11.5–9.5 m) contains only very few pollen grains but numerous Botryococcus remains. PZ III (∼9.5–5.8 m) is dominated by pollen of Betula, A. fruticosa, Ericales, Poaceae, Pinus s/g Haploxylon, Cyperaceae and Polypodiaceae spores. Algae remains (Botryococcus colonies and cysts of Volvocales) are also very common. In PZ IV (∼5.8–3.5 m) the percentages of Cyperaceae and Artemisia pollen as well as Selaginella spores are significantly higher than in PZ III, while Botryococcus remains are very rare. PZ V (∼3.5–1.1 m) is characterized by a remarkable increase of A. fruticosa pollen and higher percentages of Botryococcus remains and cysts of Volvocales. PZ VI (∼1.1–0.0 m) is dominated by pollen of Betula sect. Nanae, A. fruticosa, Ericales, Poaceae, Artemisia, and Cyperaceae.

In the 10 samples studied for palynomorphs and charcoals from section 119, which cover four stratigraphic units bracketing the “chaotic horizon” in unit 2, a total of 40 different pollen, spore, and NPP types have been found (Figure 4). For associated stratigraphic units see Table 1. The assemblages are dominated by pollen of Picea, Pinus s/g Haploxylon, Betula, and Ericales and Sphagnum spores. Single pollen grains of broad-leaved taxa, such as Corylus, Myrica, and Carpinus, also occur. The sample from the “chaotic horizon” differs from the other samples in particular by 2–4 times higher concentration of microscopic charcoals.

The charcoals in section 119 do not only differ in concentration but also in shape. The irregularly shaped and structured morphotype M (Figure 2a) shows highest concentration in the “chaotic horizon” of unit 2. The irregularly shaped but structureless morphotype P (Figure 2b) is most abundant in units 4 and 5. The angular, structured, partially charred morphotype B (Figure 2c) and the angular, structureless morphotype C (Figure 2d) occur in all units, but much reduced in unit 4. The elongated charcoal type F (Figure 2e) is of minor importance (Figure 4).

A total of 6 samples were studied for palynomorphs from section 120, which consists of 7 stratigraphic units (Table 1). In these samples, 60 different pollen, spore, and NPP types have been found (Figure 5). The revealed pollen assemblages can be subdivided into 4 PZs.

PZ I (∼2.7–2.8 m) is dominated by Poaceae, Ericales, A. fruticosa, and coniferous (Pinus s/g Haploxylon, Picea, Abies, Larix) pollen. There are rather numerous spores of Glomus and remains of Botryococcus colonies. PZ II (∼2.7–1.7 m) is characterized by an increase of Betula and Alnus pollen percentages, while percentages of Glomus spores are significantly lower. PZ III (∼1.7–0.2 m) is dominated by pollen of Poaceae, Cyperaceae, and Artemisia. Spores of Selaginella rupestris become an important component in this zone and Botryococcus remains keep common. Pollen spectra in PZ IV (∼0.2–0.0 m) are dominated by Betula sect. Nanae and A. fruticosa. Percentages of Poaceae, Cyperaceae, and Artemisia pollen are significantly decreased, while Selaginella spores and Botryococcus remains completely disappear.

In section 121, which consists of 19 stratigraphic units (Table 1), 22 samples were investigated for palynomorphs. However, only 8 samples contain pollen grains. They were also studied for charcoals (Figure 6). In these samples, a total of 56 different pollen, spore, and NPP types have been identified. The samples below 17.8 m (basaltic tuff debris, Table 1) do not contain pollen. The pollen assemblages revealed in samples above 17.8 m can be subdivided into 4 PZs.

PZ I (∼17.6–17.2 m) is dominated by pollen of A. fruticosa, Picea, Pinus s/g Haploxylon, Ericales, and Betula and Sphagnum spores. Pollen of broad-leaved taxa (Corylus, Carpinus) are also found. The zone differs from the other PZs by rather numerous algae remains (Botryococcus and Pediastrum). In PZ II (∼17.2–14.2 m) pollen of Picea, Pinus s/g Haploxylon, Abies, Betula, Alnus, Ericales, Poaceae, and Cyperaceae are dominating. Sphagnum and Polypodiaceae spores are very numerous. PZ III (∼14.2–13.5 m) is characterized by a drastic increase in pollen concentration. The percentages of Cyperaceae and A. fruticosa pollen and Sphagnum spores are significantly increased in the upper two samples. In addition, PZ III contains numerous woody remains, some of which have been identified at magnifications of 400× as Abies, Larix, and Ericaceae based on their cell structures (V. Filin personal comm., 2019; Figure 7). The only one sample from the upper sediments (∼9.5–0 m, PZ IV) contained pollen. The spectrum is dominated by pollen of A. fruticosa, Pinus s/g Haploxylon, Betula sect. Nanae, and Ericales. Percentages of Sphagnum spores are highly reduced, while Selaginella spores are increased.

The charcoal concentration in section 121 is comparable to that in the sediments underlying the “chaotic horizon” in section 119. It shows little variation in total charcoal concentration, but the charcoal morphotype composition varies across PZ (Figure 6, for charcoal morphotype images see Figure 2). In PZ I, morphotype M (Figure 2a) shows highest concentration. PZ II shows roughly equal contributions from morphotypes M and P (Figure 6) and differs from the other zones mainly by highest concentration of morphotype B (Figure 6, for example of morphotype B see Figure 2c). In PZ III, the charcoal concentration is slightly reduced, showing elevated percentages in morphotype P and maximum values in the record of morphotypes C and F (Figure 6). The charcoal composition of PZ IV is characterized by a maximum of morphotype P (Figure 2b), relatively high content of morphotype C (Figure 2d), and low values of all other morphotypes.

In section 124, which consists of 11 stratigraphic units (Table 1), 5 samples were investigated for palynomorphs and charcoal (Figure 8). A total of 51 pollen, spore, and NPP types have been found and the revealed pollen assemblages were subdivided into 3 PZs.

PZ I (∼29.7–28.5 m) is dominated by Ericales, Pinus, Alnus, Picea, Abies, and Betula pollen and Sphagnum spores. Single pollen of broad-leaved taxa (Corylus, Carpinus, and Ulmus) also occur. PZ II (∼7–6 m) is very poor in pollen and spore grains, but there are numerous Botryococcus remains. PZ III (∼6.0–4.9 m) is dominated by pollen of Betula, A. fruticosa, Salix, Ericales, Poaceae, and Cyperaceae. The uppermost sample furthermore has a much higher concentration of pollen and spores then the other samples and an elevated percentages of Artemisia pollen and Botryococcus remains. Unfortunately, total pollen and charcoal concentrations cannot be determined as no Lycopodium spores were added in the samples prepared in the Magadan pollen laboratory.

PZ I shows clearly elevated percentages of charcoal morphotypes B and C (Figure 8, see examples for morphotypes in Figures 2c,d). In PZ II, morphotype M (Figure 2a) is enriched and morphotype P (Figure 2b) shows highest values in the entire record. In the uppermost sample of PZ III, in contrary, morphotype M reaches highest values in the record (Figure 8).

According to Ar/Ar dating of impact glass, the El’gygytgyn Impact took place at 3.58 ± 0.04 Ma (Layer, 2000). This age is supported by a normal polarity of the oldest sediments in Lake El’gygytgyn that are thought to be formed after the impact event in Lake El’gygytgyn, suggesting deposition during the Gauss Chron, after 3.588 Ma (Nowaczyk et al., 2013).

The oldest pollen and spore assemblages in the region may occur in the black clays at the bottom section 120 (units 6 and 7, Table 1). According to Belaya (personal comm., 2005), samples from these layers, from which no material was left for new pollen analyses, contained numerous pollen grains of Taxodiaceae, such as Taxodiaceaepolentis, Taxodiumpolentis, Sequoipolentis, and spores, such as Laevigatosporites and Sphagumsporites. They were attributed to the late Turonian Stage (c. 90 Ma), based on similarities to pollen assemblages in dated sections in the Mechekrynnetveem River valley (sections 105 and 106 in Belyi and Belaya, 1998; Figure 1B). These black clays with Turonian palynomorphs are discontinuously overlain by Quaternary deposits (Figure 5), without a “chaotic horizon” containing impactite glass spherules in between, as evidenced by the dominance of typical Quaternary taxa in the respective sediments (see below).

We do not know the absolute age of the studied pre-“chaotic horizon” sediments accumulated in the sections 119 and 121. Paleomagnetic measurements of the lowermost sediments below the chaotic horizon in the closely situated sections 2303 and 2403 (Figure 1B) yield an inverse polarity most likely pointing to a formation during the Gilbert Chron, ca. 5.9–3.6 Ma (Minyuk et al., 2006). However, the majority of the paleomagnetic samples from the pre-chaotic horizon from these sections demonstrate a normal polarity implying a sedimentation after the Gilbert/Gauss polarity change at 3.588 Ma (Nowaczyk et al., 2013). Taking in consideration paleomagnetic measurements of the sediments from the sections 2303 and 2403 and the age of the meteorite impact, we assume that the pre-“chaotic horizon” sediments in the sections 119 and 121 were also accumulated shortly before and/or after the Gilbert/Gauss polarity change but before the El’gygytgyn impact event around 3.588 Ma.

Pliocene sediments overlain by the chaotic horizon and most likely accumulated shortly before the meteorite impact event were found only in sections 119 (Figure 4) and 121 (Figure 6 and Table 1). Based on the section stratigraphy and its pollen composition (rather high percentages of broadleaved taxa), we assume that the oldest pollen assemblage of all analyzed samples is present in PZ I of section 121 (Figure 6). Pollen composition of PZ I reflects a dominance of spruce and shrub alder in the local vegetation. Pines were also common, however, it is difficult to conclude, whether pollen of Pinus s/g Haploxylon-type was produced by tree pines (e.g., modern trees of P. sibirica or P. koraiensis that belong to this subgenus are growing in southern regions of Siberia and southern Far East) or by shrub stone pine (e.g., P. pumila broadly distributed today in the north-eastern and southern Siberia, Kamchatka, and northern Japan). Because of the high percentages of Picea and Corylus as well as presence of Abies, we assume that most of fossil Pinus pollen grains were presumably produced by tree pines. The relatively high percentages of A. fruticosa pollen suggests that shrub alders were also common in the regional forests and most likely stone pine could also grow in the area, especially at higher elevations.

Pollen grains of Larix/Pseudotsuga-type are also rather common in PZ I, suggesting that larch was common in the region. However, it is also possible that these pollen grains might at least partly be produced by Pseudotsuga (Douglas fir), which nowadays grows in western North America and in eastern Asia.

High charcoal percentages in PZ I of section 121 indicate that wildfires were frequent during the accumulation of PZ I sediments. The dominance of morphotype M charcoals with some contributions of elongated morphotypes point to burning of leaves, structured woody biomass and grasses present in forest undergrowth (Enache and Cumming, 2007; Pereboom et al., 2020).

A rather high percentages of Corylus pollen as well as the presence of pollen of other relatively thermophilic taxa in the sediments point to a relatively open forest and a rather warm climate during the PZ I interval. The summer temperatures were probably at least 10°C warmer than today as suggested by the presence of hazel in the local vegetation, thus further supporting the spread of fires. The high presence of ericaceous pollen and Sphagnum spores reflect that open wetlands with shrubby and boggy habitats were common in the area. Numerous colonies of Botryococcus and Pediastrum found in the spectrum of the loamy host sediments indicate a sedimentation in a small pond, in which these green algae could grow (Table 1).

Pollen assemblages of PZ II of section 121 (Figure 6) are similar to the lowermost three samples in section 119 (Figure 4) and reflect a dominance of spruce forests in the study area. Pines, firs, birches, larches, and alder, however, became more common compared to the time interval reflected by PZ I of section 121. Charcoal percentages reaching maximum values in two PZ II samples document increased wildfire activities around the study site. The permanent presence of pollen of broad-leaved (Corylus, Carpinus, and Ulmus) and single pollen grains of other relatively thermophilic taxa (Tsuga, Myrica, and Lonicera) indicate the growth of these plants might have also grown in the study area. The inferred climate conditions remained rather warm during this interval, although the broader distribution of shrubby ericaceous, fern- and Sphagnum-dominated habitats in the area point to wetter conditions.

Generally, pollen assemblages from PZ III of section 121, which directly underlies the chaotic horizon (Figure 6 and Table 1), reflect environmental conditions similar to the previous interval. However, the PZ III sediments are especially rich in plant remains compared to the underlain sediments. The identified macrofossil remains (Figure 7) confirm that firs, larches and ericaceous shrubs grew in the area. The increased pollen percentages of Alnus, Cyperaceae, and Sphagnum spores in the uppermost pollen assemblage point to significantly wetter conditions shortly before the impact event. This is also supported by a slightly lower charcoal concentrations, which were maximum in comparison of all analyzed samples. A slight shift from dominating more translucent morphotype M charcoals to opaque type P might reflect a slight change toward woodier burnt biomass or slightly higher intensities of fires.

Generally, sediments below the chaotic horizon were previously known from the study area: sites 10, 107, and 108 on Figure 1B (Belyi et al., 1994) sites 2304 and 2303 on Figure 1B (Glushkova et al., 2005; Minyuk et al., 2006). These sediments contain pollen of Picea, Pinus s/g Haploxylon, Larix, Abies, Betula, and Alnus with some rare pollen of relatively thermophilic taxa like Tsuga, Myrica, Carpinus, Corylus, Quercus, Juglans, Ulmus, Ilex, and Acer, Unfortunately, these pollen data were not properly published, and therefore are not available for the comparison with the newly studied records.

Sediments below the chaotic horizon collected for macrofossil and pollen studies during the expedition ‘El’gygytgyn Lake 2003’ (sites 2303 and 2403 on Figure 1B; Glushkova et al., 2005) contained numerous plant remains of Larix, Betula, Alnus, Pinus, Rubus, and Aracispermum, an extinct thermophilic shrub from the Myricaceae family (Minyuk et al., 2006). Numerous remains of Sphagnum and ericaceous plants (Ledum palustre, Andromeda, and Vaccinium) typical for Sphagnum-dominated habitats also occur in the studied sediments.

Upper Pliocene pollen records from adjacent areas of Chukotka and northeastern Siberia (e.g., Fradkina, 1983, 1988; Giterman, 1985; Volobueva et al., 1990; Grinenko et al., 1998; Fradkina et al., 2005a,b and references therein) also document the widespread distribution of forests with spruce, birch, alder, larch, and hemlock. Unfortunately, the poor age control does not allow a more precise comparison of the records. Early Pliocene pollen and macrofossil records from central and northern Yukon and Alaska exhibit that mixed boreal forests with pine, fir, larch, spruce, birch, alder, larch, and Douglas fir dominated the local vegetation there (e.g., Schweger et al., 2011 and references therein). In the Canadian Arctic (Ellesmere Island), an early Pliocene record from Strathcona Fjord shows that forest with larch, spruce, pine, birch and alder dominated nowadays treeless area (Fletcher et al., 2019).

In accordance with these Pliocene pollen data showing widespread forests north of the modern treeline, the Late Pliocene pollen record from Lake Baikal yielded widespread mixed coniferous (Pinus, Abies, Larix, and Tsuga) forests with some broadleaved taxa (Quercus, Tilia, Corylus, and Juglans) in southern Siberia (Demske et al., 2002). This points to significantly warmer environmental conditions than today also in the southern boreal forests around Lake Baikal.

Based on pollen and macrofossil records from several sites in Chukotka, Glushkova and Smirnov (2007) assumed that the Pliocene climate was much warmer than today, with mean January temperatures estimated to be −13 to −17°C (at least 15° higher than modern) and mean July temperatures 14–17°C (ca. 8–10° higher than modern). These estimates are similar to biomarker-based average mean summer temperature estimates of 15.4 ± 0.8°C in the Canadian Arctic around that time (Fletcher et al., 2019). This summer temperature estimate clearly exceed the proposed threshold that predicts a substantial increase in wildfire in the modern high latitudes (Young et al., 2017), which is confirmed by high concentrations of sedimentary charcoal in the pre-impact sediments.

Investigations of palynomorphs and charcoal in the “chaotic horizon” were carried out in the upper part of section 119 (Figure 4). Palynomorph compositions are similar to the pre-impact pollen assemblages, except for a lower pollen and a higher charcoal concentration. This confirms earlier palynological studies by Belaya (personal comm., 2005) on the “chaotic horizon” of sections 121, 10, and 108 (Figure 1B; Belyi et al., 1994). In contrast to the pre-impact sediments, the “chaotic horizon” of section 119 is distinctive because of its high charcoal concentrations (Figure 4).

We assume that the “chaotic horizon,” which has a thickness of ca. 2 m in section 119, was caused by the meteorite impact and accumulated soon after the event. The chaotic nature of the sediments and the similarity of the pollen assemblages within and below the horizon suggest that the sediments originates from pre-impact material that was disturbed by impact-induced earthquake activity or shock waves of near-surface sediments, which were formed shortly before the impact and redeposited by fluvial-alluvial or aerial transport. An allochthonous contribution to the “chaotic horizon” is evident by the distinctly increased admixture of charcoal (maximal charcoal concentrations in comparison of all analyzed samples), which originates from widespread burning of existing vegetation caused by the meteorite impact affecting a much larger amount of biomass compared to normal wildfires.

It is difficult to estimate the age of the investigated sediments on top of the chaotic horizon, taking in consideration the possible hiatuses and lack of any absolute age control. From the comparison with the El’gygytgyn pollen record (Andreev et al., 2014), however, the pollen assemblages and in particular the common high percentages of Picea and Abies pollen in PZ I of section 124 (Figure 8), PZ I of section 120 (Figure 5), and PZ I of section 118 (Figure 3) enables us to constrain to a Late Pliocene age of these deposits.

Amongst the Late Pliocene sediments, PZ I in section 124 (Figure 8) is unique, because the sequence lacks a ‘chaotic horizon’, suggesting a post-impact age. Its pollen assemblages however, document that pine-spruce forests with some firs, birches, larches, and alder dominated the vegetation. The presence of pollen of thermophilic taxa (Corylus, Carpinus, Ulmus, Tsuga, and Myrica) reflect that these taxa might still have grown in the area, thus suggesting that the sediments were deposited during an interval, which was the warmest of all post-impact sequences, potentially equivalent to oldest Late Pliocene in the Lake El‘gygytgyn record (Andreev et al., 2014). The dominance of irregular, opaque morphotype P charcoals with minor contribution of the angular opaque type C suggests relatively high fire intensities typical for burning woody biomass in forest fires. Sphagnum-dominated habitats with numerous ericaceous plants were common, thus pointing to a relatively wet climate. Hence, the vegetation cover and climate conditions shortly after the impact event were rather similar to those before, though decreased amounts of broad-leaved pollen taxa suggest a slight cooling.

The pollen spectra from PZs I of sections 120 (Figure 5) and 118 (Figure 3) reflect that mainly pine forests with some spruce, birches, larches, firs and alder dominated the vegetation in the area. Despite an obvious sub-aquatic formation of the partly loamy sediments (Table 1) as also indicated by high percentages of Botryococcus colonies, reduced amounts of Sphagnum spores and Ericales pollen indicate a general reduction of boggy habitats in the study area. The climate conditions reconstructed for PZs I of sections 120 and 118 were much drier and colder compared to PZ I of section 124, indicating an asynchronous formation, presumably some time later.

Although the age control of PZ II in section 120 is also limited, the comparison with the continuous El’gygytgyn pollen record (Andreev et al., 2014) suggests that the pollen spectra were accumulated during some Late Pliocene interstadial. Larch forests with stone pines and some birches, spruces, and shrub alders dominated the vegetation in the area. Open shrubby habitats with dwarf birches and ericaceous low shrubs were also common.

Pollen assemblages of PZ III in section 118 (Figure 3) are dominated by Betula, Alnus and Pinus. In the El’gygytgyn pollen record (e.g., Lozhkin et al., 2007, 2017; Matrosova, 2009; Andreev et al., 2014; Zhao et al., 2018, 2019), similar pollen assemblages have only been reported from the Late Pleistocene. During PZ III of section 118, larch forests with stone pines, shrub alders, dwarf birches, and ericaceous low shrubs in underbrush dominated the vegetation cover. Climate conditions were relatively mild as can be inferred from pollen assemblages. High percentages of Botryococcus colonies and cysts of Volvocales (Figure 2) point to accumulation in an aquatic environment, probably in a floodplain pond. Similar contributions of larch pollen enables a correlation of PZ III in section 118, to environmental conditions during an interglacial in the well-dated Lake El’gygytgyn record, tentatively Marine Isotope Stage (MIS) 5e. The pollen assemblage of the overlaying PZ IV of section 118 (Figure 3), with increased Artemisia and S. rupestris percentages, reflects colder and drier environmental conditions, which might have occurred during Late Pleistocene (MIS 4 – MIS 2). Furthermore, the drastic decrease in algae remains points to a local shift toward sedimentation in a non-lacustrine environment.

Very similar pollen assemblages of PZ III in section 124 (Figure 8) and PZ IV in section 121 (Figure 6) indicate a synchronous deposition during MIS 5. Differing charcoal morphotype compositions, on the other hand, suggest that fire regimes were different during the deposition of the associated stratigraphic units of section 121 and 124. A dominance of irregular, translucent morphotype M charcoals and high contributions of elongated charcoals in PZ III of section 124 potentially points to lower fire intensities due to burning of leaves, branches and grasses during forest surface fires. In PZ IV of section 121, in contrast, opaque, irregular morphotype P and angular opaque type C point to higher-intensity fires, which have burned woodier biomass.

PZ III pollen assemblages of section 120 (Figure 5) exhibit low pollen percentages of shrubs and trees, while Artemisia and S. rupestris percentages are relatively high. Comparisons with regional pollen records (e.g., Lozhkin et al., 2007; Matrosova, 2009; Andreev et al., 2012) suggest that the PZ III sediments were formed during the Late Glacial.

The topmost PZ V pollen spectrum of section 118 (Figure 3) with relatively high percentages of shrubs and trees, most likely accumulated during the Holocene thermal optimum (early and middle Holocene). Shrub alder stands dominated the study area during this time, whereas, open dwarf birch and herb (Poaceae, Cyperaceae, Artemisia) plant communities were also common in the Lake El’gygytgyn area (Andreev et al., 2012 and references therein). Furthermore, relatively high percentages of Botryococcus colonies in the sediments point to an accumulation in an aquatic environment (e.g., floodplain pond as also suggested be the loamy host sediment, Table 1).

Finally, the pollen assemblages from the uppermost PZs of sections 120 (Figure 5) and 118 (Figure 3), representing the modern soils (Table 1), well reflect the modern regional vegetation cover with numerous dwarf birches and some shrub alder stands that prevailed during most of the Holocene in the valleys of the rivers around Lake El’gygytgyn (Andreev et al., 2012 and references therein).

Overall, the preservation of fluvial sediments downstream of Lake El’gygytgyn during the Late Pliocene and Late Pleistocene and the lack of sediments with typical early Pleistocene pollen assemblages might be related to an incomplete record of fluvial sediment sequences mapped in the field. However, it could also point to distinct changes in the long-term fluvial network evolution of the upper catchment of the Anadyr River basin due to varying rates of fluvial backward incision and sediment aggregation in response to global sea and base level changes – requiring a more comprehensive mapping of fluvial terrace sediments together with the usage of modern dating approaches.