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Climate change evidence in tree growth and stand productivity at the upper treeline ecotone in the Polar Ural Mountains



Recent warming is affecting species composition and species areal distribution of many regions. However, although most treeline studies have estimated the rates of forest expansion into tundra, still little is known about the long-term dynamic of stand productivity at the forest-tundra intersection. Here, we make use of tree-ring data from 350 larch (Larix sibirica Ledeb.) and spruce (Picea obovata Ledeb.) sampled along the singular altitudinal treeline ecotone at the Polar Urals to assess the dynamic of stand establishment and productivity, and link the results with meteorological observations to identify the main environmental drivers.


The analysis of stand instalment indicated that more than 90% of the living trees appeared after 1900. During this period, the stand became denser and moved 50 m upward, while in recent decades the trees of both species grew faster. The maximum afforestation occurred in the last decades of the twentieth century, and the large number of encountered saplings indicates that the forest is still expanding. The upward shift coincided with a slight increase of May–August and nearly doubling of September–April precipitation while the increase in growth matched with an early growth season warming (June + 0.27 °C per decade since 1901). This increase in radial growth combined with the stand densification led to a 6–90 times increase of biomass since 1950.


Tree-ring based twentieth century reconstruction at the treeline ecotone shows an ongoing forest densification and expansion accompanied by an increased growth. These changes are driven by climate change mechanism, whereby the leading factors are the significant increase in May–June temperatures and precipitation during the dormant period. Exploring of phytomass accumulation mechanisms within treeline ecotone is valuable for improving our understanding of carbon dynamics and the overall climate balance in current treeline ecosystems and for predicting how these will be altered by global change.


Global warming is most pronounced at high latitudes where temperatures over the last 30 years have risen by 0.6 °C per decade, which is twice as fast as the global average (Bekryaev et al. 2010; Core Writing Team RKP and LAM 2014). Since it is largely considered that high altitude and latitude treelines are controlled by summer temperatures (Holtmeier and Broll 2007; Gehrig-Fasel et al. 2008; MacDonald et al. 2008) and growing season parameters (Körner and Paulsen 2004; Körner 2008), the ongoing warming trend is expected to cause important vegetation shifts and lead to significant changes in species composition and biomass production (Walther et al. 2002; Epstein et al. 2004; Gonzalez et al. 2010; Paulsen and Körner 2014; Speed et al. 2015). Despite the fact that treeline advances in Polar regions are mostly limited by temperature, other factors (e.g. slope aspect, geomorphic processes, snow cover, albedo, soil temperatures, and carbon and nutrient cycling) can determine the rates of this changes (Holtmeier 2003; Lloyd 2005; Macias-Fauria and Johnson 2013; Loranty et al. 2014).

Many studies focusing on ongoing dynamics of woody vegetation at the limit of their distribution (e.g. Harsch et al. 2009; Holtmeier 2009; Körner 2012) have documented that treelines are experiencing an extension of seedling establishment, densification of forest structures and a stimulation of radial growth and biomass (e.g. Kearney 1982; Wardle and Coleman 1992; Nicolussi et al. 1995; Kullman and Engelmark 1997; Canadell et al. 2007) that are consistent with observed rates of recent (Suarez et al. 1999; Gamache and Payette 2005; Shiyatov et al. 2007) and past (Foley et al. 1994; Lloyd and Graumlich 1997; Grace et al. 2002; Körner and Paulsen 2004; Hoch and Körner 2009) temperature changes.

However, other studies suggest that winter temperature and precipitation also affect on the survival of treeline trees as they play a role on soil hydrological and thermal regimes (Harsch et al. 2009; Hagedorn et al. 2014). Indeed, increased winter precipitation may provide additional water supply for woody vegetation (especially seedlings and saplings) during the vegetation period (Grigorieva and Moiseev 2018), while snow cover plays a key role in protecting them and young trees from frost and wind damage (Holtmeier 2009; Devi et al. 2008; Kharuk et al. 2010, 2017). In contrast to low latitudes and altitudes, where forest distribution is mainly limited by lack of moisture (Woodward et al. 2004), forests from cold regions can grow with less than 400 mm of yearly precipitation, which is usually sufficient to cover trees’ transpiration needs (Pan et al. 2013).

Most treeline studies have focused on understanding drivers and limitations of the treeline shift, whereas knowledge of tree biomass and productivity and the environmental factors influencing biomass production is severely limited. Extensive studies have assessed biomass changes using remote sensing methods (e.g. Pan et al. 2013; Zolkos et al. 2013) and have mainly focused on mountain systems from temperate climatic zones that are exposed to anthropogenic disturbances. However, satellites or aerial scanning data can only assess biomass dynamics of the last decades and the current changes in anthropogenic pressure might have slightly biased the obtained results. Currently, only some studies have investigated centennial trends in aboveground biomass as a result of changing environmental conditions based on direct field observations (Clark et al. 2001; Babst et al. 2014; Grafius and Malanson 2015; Moiseev et al. 2016; Liu et al. 2016; Xu et al. 2019) and analyzing tree-ring data (Graumlich et al. 1989; Dye et al. 2016), making it difficult to quantify current trends in the carbon sequestration and productivity of terrestrial ecosystems.

The Polar Ural Mountains are particularly suitable for investigating climate-induced processes as they have not been influenced by any significant disturbances. Indeed, the mountainous part of the Polar Urals has been excluded from reindeer grazing, logging and other management activities, and its vegetation has not been exposed to forest fires for the last 500 years, as evidenced by the absence of charred tree and coal residues in the upper soil layers (Mazepa 2005).

The aim of this investigation was to identify the main drivers of the treeline dynamic processes at the Polar Urals. Our specific objectives were to assess, along an altitudinal gradient and over the last century, the development of (1) stand formation; (2) radial growth; (3) and biomass accumulation; (4) to eventually identify the climatic drivers to such developments.


Study area

The investigated treeline ecotone is located about 30 km north of the Arctic Circle on the western slope of the mountain Slantsevaya (66°54′ N, 65°44′ E), close to Sob River basin, an eastern slope of the Polar Ural Mountains (Fig. 1, Fig. 3). The area belongs to the Yamalo-Nenets Autonomous Okrug (YANAO) of Russia and is part of the continental subarctic zone.

Fig. 1
figure 1

Location of the study area (a and b) and scheme of study plots establishment (c). The numbers indicate the types of forest (1 – Treeline, 2 – Open forest, 3- Closed forest)

Monthly meteorological records from 1892 to 2015 of the nearest weather station of Salekhard (66°32′ N, 66°32′ E; 35 m a.s.l.; located 50 km southeast from the research area) indicate a negative average annual temperature (− 6.4 °C) and mean annual precipitation of 415 mm, with 45% of which fall as snow (Fig. 2). The region is characterized by a complex wind regime dominated by westerly winds, with average speed of 8.5–8.8 m∙s− 1 in winter and 6.5–7.0 m∙s− 1 in summer. The current treeline occurs between 260 to 310 m a.s.l. and is dominated by Siberian larch (Larix sibirica Ledeb.) in association with Siberian spruce (Picea obovata Ledeb.) and mountain alder (Alnus alnobetula ssp. fruticosa (Rupr.) Raus.). The shrub layer is dominated by Betula nana L. with a mixture of different willows species and other dwarf shrubs (e.g. Vaccinium uliginosum L., Empetrum nigrum subsp. hermaphroditum (Hagerup) Böcher). The ground cover consists of mosses and lichens. The area is pristine.

Fig. 2
figure 2

Climadiagram for Salekhard weather station (66°32′ N, 66°32′ E; 35 m a.s.l.; 1892–2015). Blue line and red columns are the long-term average sum of precipitation and average monthly temperature, respectively

Data collection

In August 2015, we established study plots within three different forest types along an altitudinal gradient, starting at the current treeline and moving down slope. The forest types were defined based on the stand density according to Shiyatov et al. (2007). Specifically, we defined the type Treeline as the stand with trees distances ranging between 20 and 50 m and average tree height ≤ 2 m; the Open forest with distances between 7 and 20 m, and the Closed forest with distances inferior of 7 m (Fig. 3).

Fig. 3
figure 3

Photos of treeline ecotone on the Slantsevaya Mountain. a General view, (b) treeline, (c) open and (d) closed forest

At each forest area, we established 3 research plots that together contained at least 100 trees, thus with different size. The total area was 11,306 m2. The main characteristics of the forest types are presented in Table 1.

Table 1 Characteristics of the selected forest types along the altitudinal transect

The current altitude position of each forest type was defined as the average altitude, measured at the center of three rectangular research plots.

Dendrometric survey and tree-ring width measurements

To assess the current state and reconstruct the stand structure in different periods of the twentieth century, we first assessed the position of all individuals (trees and saplings) within each plots with a GPS receiver (Garmin Oregon 650). Since all woody remnants on the sites were accounted, all trees, even those that died earlier, were included in our analysis. The phenomenon of mass mortality at the treeline mainly affects seedlings, since in the life of shoots, the first years are the most critical period, when they are especially sensitive to the effects of sharp fluctuations in temperature and humidity, and when the mortality is greatest. In total, 346 individuals were considered. Subsequently, we measured the height, base diameter, and crown projection of each individual. Height of tall trees (> 5 m) was assessed with a digital rangefinder (accuracy 0.3 m, TruPulse 200B) while a telescopic ruler (accuracy 1 cm) was used for small trees. Stem perimeters and crown projections were measured using a measuring tape (accuracy 0.5 cm).

Additionally, to determine age and annual growth, each individual with a stem diameter > 2–3 cm was cored using 5-mm increment borer (Haglöf, Sweden) at a height of up to 10 cm. Smaller individuals were sawed at the ground level and then through every two centimeters of height to determine the local height-age growth function. The obtained relationship served to refine age determination of trees > 2–3 cm in diameter (Niklasson 2002; Hagedorn et al. 2014).

All discs and cores (pre-mounted in a wooden holder) were cleaned with razor blades and whitened with wet chalk to increase the visibility of the tree-ring boundaries. The measurement of the wood cores and discs was carried out according to standard dendrochronological techniques (Cook and Kairiukstis 1990; Rinn 1996). Tree-ring width was measured using a binocular microscope above a moving measure table with an accuracy of 0.01 mm (LINTAB, F. Rinn SA, Heidelberg, Germany). Ring widths were recorded using the TSAP program v4 ( All samples were first visually cross-dated in TSAP and cross-dating quality checked using the program COFECHA (Holmes 1995) by matching the undated samples against the dated local larch chronology (Briffa et al. 2013). The sample depths and the statistical characteristics of the tree-ring series are presented in Appendix 1 and 2.

We defined the current treeline position as a stand with a canopy cover ≥0.07±0.01 and an average height of trees  ≤ 2 m and assumed that the same criterion was the same in the past. The reconstruction of the former treeline position has been carried out based on a retrospective assessment of the density of tree stands (Shiyatov 1986), as well as the age and morphometric characteristics of individual trees (height) on research plots. Using a dated tree ring series, the stem diameters of all trees were reconstructed yearly. The historical tree heights were reconstructed based on dependency between the actual heights and diameters of the stems. Treeline shift was calculated as the difference between the current and historical treeline position.

To study age-related trends in radial growth, trees (this analysis was performed only for larch due to insufficient number of spruce models) were divided into four age groups that included at least 15 individuals, namely 1–30, 31–60, 61–90 and 91–120 years.

To study climate-growth relationships, ring-width chronologies for each forest type were assessed by combining individual age-detrended timeseries of each forest type into a site chronology using a biweight robust mean. Age-detrending were performed individually with a 60% cut-off at half-length of the series cubic spline (Cook and Peters 1981) using ARSTAN (Cook and Krusic 2006). Calculations of radial growth responses to climate (monthly temperature and precipitation of Salekhard meteo station) were conducted for each forest type using the bootstrapped response function of DENDROCLIM 2002 (Biondi and Waikul 2004). This statistical procedure allows estimating the relative contribution of different climate variables (e.g. air temperature and precipitation) using regression coefficients, by constructing a multiple regression model describing the variability of tree growth indices (Fritts 1976). A 95% confidence level was used to determine the statistical significance within a 12-month window spanning from previous September to current August. All statistical analyses were conducted using STATISTICA 8.0. Kruskal–Wallis criteria for independent groups was used to examine differences of morphometric parameters and trees ages between elevation zones.

Biomass calculation

Allometric functions between tree biomasses and stem base diameters were assessed using trees from outside the research plots but in similar forest types. In total 33 model trees were felled and sectioned to collect stem disks at the stem base, at 0.25 m and breast height (1.3 m), and then at every subsequent meter in stem height. Stems fresh mass was determined with a hand weight scales with 50 g accuracy. The crown was divided into three equal sections, and from each section, the sample of the middle section was taken for biomass assessment. The fresh mass of the leafless branches, needles and cones were separately determined with a digital weight scales with an accuracy of 0.01 g. All the wood, branches, needles, and cones were then oven-dried at 106 °C until a stable weight and the dry masses of all the components were calculated for each tree and used to assess the allometric functions. These relations (Fig. 4), combined with the dependencies between the actual heights and stem diameters, were then combined with the tree-ring width measurements to assess biomass accumulation over time. The stem diameters of all examined trees were reconstructed at each decade of the twentieth century considering geometric relations (see Bakker 2005), and according to the following formula:

$$ {D}_n=\left({R}_n/{R}_{\mathrm{final}}\right)\times {D}_{\mathrm{final}} $$

where Dn is the computed tree diameter in a given year; Rn is the radius of the correponding annual ring; Rfinal is the current tree radius; and Dfinal is the current tree diameter.

Fig. 4
figure 4

Relation between aboveground biomass and stem base diameter for (a) larch and (b) spruce

Since the rate of biomass growth results from both radial growth increase and establishment of new trees, we analysed the influence of temperature and precipitation on biomass. May–August climatic variables were nominally attributed to the “growth period”, while the rest 8 months - to the “dormant period”. Spring and autumn phenophases (due to their short duration and variability of the beginning and end of vegetation) were not identified.

Pearson’s correlation was used for annual resolution data. Averaged over decades values were analyzed with Spearman rank correlation.


Forest establishment

Siberian larch dominated at all altitudinal levels, accounting for more than 70% of the tree stems. When moving along the altitude gradient, the percentage of Siberian spruce in the tree stands decreased slightly: from 26% at the treeline to 19% in the closed forest. The number of living trees per hectare showed an eightfold increase (from 148 trees·ha− 1 at the treeline to 1166 trees·ha− 1 in the closed forest). Similar proportions were observed regarding the number of saplings (individuals less than 2 m high) since Siberian larch saplings accounted for 69% of the total. The ratio of larch and spruce saplings (70%/30%) suggest further preservation of the share of these species in the tree stand. Results also indicated a large presence of saplings (up to 110 PCs·ha− 1) at the upper part of the treeline ecotone. No dead seedlings nor saplings where observed.

The analysis of the age structure (Fig. 5) showed that modern stands in the treeline ecotone was formed in the last 1.5 centuries. The mass establishment of trees of both species is dated to the beginning of the twentieth century, before which time only 17% of the currently living trees were represented. In particular, 91% of spruce and 79% of larch appeared in the last 115 years. The stands were mostly composed by young trees especially in the upper part of the treeline ecotone. The afforestation at the treeline mostly occurred in the last decades of the twentieth century, as indicated by the important number of saplings. Indeed, the maximum age of the trees did not exceed 120 years, and there were only a few old trees. However, the trees establishment in the open forest occurred earlier in the second half of the twentieth century, and the larch and spruce trees at this level had the same average age. In the closed forest, the average age of the trees was > 100 years. Individuals under 30 years of age were almost absent, and only few individuals were between 30 and 60 years old. The maximum age of the trees exceeded 250 years. Hence, the displacement of the treeline by 50 m, which occurred in the last 100 years, is indicated by a large amount of saplings in the upper part of the ecotone, the absence of saplings in the stands formed earlier, and a decrease in the average and maximum age of the trees up the altitude gradient.

Fig. 5
figure 5

Time of tree establishment and age structure at the different forest types

Growth dynamics

The changes in the main dendrometric characteristics at each forest types are shown in Table 2 and Appendix 3. These data indicate that there was a gradual increase in the average tree size along the transition from the treeline to the closed forest. The stem diameter, height, and age of the trees increased 1.6–4.7 times, but were more pronounced for larch (3.1–4.7 times) than for spruce (1.5–3 times).

Table 2 Mean and standard errors of the main dendrometric parameters at the different forest type, differentiated by species

Considering the tree-ring data, in recent decades there has been a sizeable increase in radial growth at all forest types, both for larch and spruce (Figs. 6 and 7). Relatively weak growth since the first half of the twentieth century was replaced by a significant acceleration after the 1950s. At the same time, after a sudden increase, the growth of larch stabilized, and the growth of spruce continued to rise. However there are some differences between the forest types. At the treeline, the trend in radial growth of the lower age group (1–30 years) shows an overall negative trend. This finding is connected to the age-related characteristics high growth trend at very young ages. Indeed, an opposite trend with increasing ring width has started after 2000. The 31–60-year-old trees at the treeline and in the open forest showed an increase in growth in the 1980s and which also become important after 2000. At the same time, trees of the same age in the closed forest only showed stable growth with a downward trend in radial growth, since they grow under the pressure of older trees and their growth is certainly influenced by competition for light and nutrients. In contrast, the dominant trees belonging to the 61–90 and the 91–120 age groups, show a strong increase in the growth rate since the 1970s. The absolute values of the larch and spruce growth were significantly higher in the open forest compared to other levels (F = 20.423, p < < 0.001), (F = 3.75, p = 0.047), respectively.

Fig. 6
figure 6

Radial growth dynamics of larch trees in different age groups. Black line: Treeline; grey line: Open forest; dotted line: Closed forest

Fig. 7
figure 7

Radial growth (black) and rate of biomass accumulation (red) of larch (a) and spruce (b) at different forest type (smoothed by decades)

Biomass accumulation

Since stand biomass accumulation summarizes both the processes of growth increment and tree recruitment and mortality (Gower et al. 1996; Pan et al. 2013), the changes in climatic conditions occurring in the second half of the twentieth century led to multiple increases in the rates of biomass accumulation. Since mortality has almost not been observed (only 10 dead tree trunks were found in our sample areas) and since these arctic conditions (permafrost, short vegetation season, low rate of wood decomposition) favour the preservation of tree remains for hundreds of years (Yatskov et al. 2003; Mazepa 2005), mortality was not included in our analysis.

Changes in the stand structure and radial growth of the trees resulted in significant changes in the stock and rate of aboveground biomass accumulation within the treeline ecotone (Table 3, Fig. 6).

Table 3 Stock and rate of accumulation of the aboveground biomass at the different forest types during the 20th century

In the early twentieth century in the upper part of the ecotone, the stock of aboveground biomass was near zero. The average rate of biomass accumulation between 1900 and 1950 was very low at 0.0003 t·ha− 1 per year. After 1950, this value increased by 86 times. At the moment, the aboveground biomass is 1.12–2.86 t·ha− 1. The contribution of spruce to the stock of the stand biomass was and remains irrelevant since for the entire period it only increased from 0 to 1.3%.

In the open forest the rate of biomass accumulation in the first half of the twentieth century was 0.014 t·ha− 1·yr− 1. By 2015, the annual production increased by 59 times. The current aboveground stand biomass of the three research plots ranged 15.67–62.82 t·ha− 1, with spruce contribution averaging 15%.

In the closed forest stands, which were almost formed in the nineteenth century, the aboveground stand biomass at the beginning of 1900 was 2.45 t·ha− 1, with annual increments of 0.029 t·ha− 1·yr− 1. Over the next 115 years, the rate of biomass accumulation increased by 39 times reaching now an aboveground biomass stock of 94.22–110.11 t·ha− 1 with an average annual growth rate of 1.14 t·ha− 1·yr− 1. The contribution of spruce in 115 years increased by only 3%.

At the treeline, the change in the rate of biomass accumulation of larch during the twentieth century was more associated with the establishment of new trees (r = 0.94, p < < 0.01, Table 4) while at other forest types and for spruce the rate of biomass accumulation was mostly associated to radial growth.

Table 4 Correlation between rate of biomass accumulation and radial growth (annual data)/tree establishment (averaged over decades) for the tree forest types differentiated by species

Association to climate

According to the meteorological data from Salekhard, significant warming and moistening occurred over the last 135 years and which are still ongoing (Fig. 8). In particular, both growth and dormant periods temperatures increased by 1.7 °C since 1900. Meanwhile, May–August precipitation increased by 49 mm (from 175 to 224 mm), and by 103 mm in September–April (from 135 to 238 mm).

Fig. 8
figure 8

Temperature (a–d) and precipitation (e–f) anomalies (compared to 1961–1990) at Salekhard

Trees establishment at treeline correlated positively with precipitation of both periods (Table 5). For spruce, this relationship was maintained also for the closed forest. Regarding temperature, a relationship with May–August temperature has been detected only for the larch trees at the treeline.

Table 5 Spearman rank correlation between the frequency of tree appearance and seasonal climatic variables

The response function analysis comparing the annual tree-ring growth of the two species showed no significant relationships with monthly precipitation (Fig. 9). However, both species showed a positive response to June–July temperature. Responses were stronger for July and for larch than for spruce. A significant increase in the May and June temperatures correlation might also indicate an earlier start of the growing season.

Fig. 9
figure 9

Climate-growth correlation for larch (a) and spruce (b). Blue = precipitation, red = temperatures; * - significant at p < 0.01, N = 123

Linkage between the rate of biomass accumulation and main climatic variables indicated that precipitation during dormant period had a weak positive effect but the most important climatic factor determining the biomass accumulation was growth season temperatures. The June and July temperatures were significant for larch and the May and June temperatures were significant for spruce (Table 6).

Table 6 Pearson’s correlation between rate of biomass accumulation and selected climatic variables


Our study showed that the forest-tundra intersection at the Polar Urals has been undergoing important changes during the twentieth century. Forests expanded upwards with more than 90% of trees established during the last 115 years. Tundra areas which were treeless at the beginning of the twentieth century are now covered by dense forest (150–900 trees·ha− 1). The big number of saplings in the upper part of treeline implies that forest is currently expanding. In particular, thanks to our relation with long term climatic data, we suggest that the forest expansion was mainly caused by changes in the moisture regime and, to a lesser extent, by temperature. On one hand, the increase of 1.15 times of summer precipitation facilitated the mass emergence and better survival of seedlings which is consistent with the data for other areas of the Polar Ural (Mazepa 2005; Devi et al. 2008; Kukarskih et al. 2018) and northern Eurasian treelines (Vaganov et al. 1996; Briffa et al. 1998; Esper et al. 2002; Matskovsky 2016). However, the lack of a strong relationship is related to the fact that the soil moisture content is usually sufficient for tree growth (Pan et al. 2013). On the other hand, the increase in precipitation during the dormant period by 1.25 times contributed to the survival of saplings, affecting plants through changes in snow depth and soil temperature. This is consistent with observation of Shiyatov (1967), who suggested that the main limiting factor for the emergence of seedlings in the Polar Urals is the humidity of the substrate in the first years of the life since 1–2-year-old seedlings have insufficient rooting and low water-holding capacity. The influence of winter conditions (snow cover, air temperature and wind speed) on trees recruitment and survival can affect soil freezing and cause shoots desiccation (Gorchakovsky and Shiyatov 1978; Lavoie and Payette 1992; Weisberg and Baker 1995; Kullman and Engelmark 1997; Holtmeier and Broll 2007; Hagedorn et al. 2014; Renard et al. 2016; Davis and Gedalof 2018; Frei et al. 2018; Grigorieva and Moiseev 2018).

Our observations of treeline upshift of 50 m during the last century are supported by large-scale studies of the Polar Urals using GIS technology and repeated photograph analysis. These studies have shown a treeline upshift by 35–80 m since the 1920s and which was accompanied by an increase in stand density (Shiyatov et al. 2005; Shiyatov et al. 2007; Shiyatov and Mazepa 2015). These rates are similar to forest boundary expansion of 30–60 m during the last 60–80 years observed over the globe (Lavoie and Payette 1992; Wardle and Coleman 1992; Lloyd and Graumlich 1997; Moiseev 2002; Kullman and Öberg 2009; Kharuk et al. 2010, 2017; Kirdyanov et al. 2012).

In parallel with the establishment of new individuals, the vast majority of trees within all forest types have showed an increase of radial growth. These changes are evident in all age groups, including aged trees. The general increasing trend of radial growth in recent decades indicates the predominant influence of common external factors on tree growth, as well as the benefits of modern climate change for the growth of tree plants. Most researchers attribute this to an increase in average summer temperature and precipitation, as these factors determine the intensity of physiological processes in plants (Taylor 1995; Esper et al. 2002; Körner and Paulsen 2004; Körner 2012; Keane et al. 2018; Kukarskih et al. 2018). The analysis of the climatic-growth relationships with the data of Salekhard weather station clearly indicated that most of the increases are related to early summer temperatures (June + 0.27 °C per decade since 1901). Another positive effect of temperatures is the promotion of tree growth at the beginning of growing season. The influence of May conditions on the evergreen spruce trees is associated with an earlier onset of photosynthesis, while June air temperatures has common positive role for both tree species, as it coincides with the beginning of active tree growth (Rossi et al. 2007, 2008).

Advancing the forest treeline and increasing of stand’s density may further alter the energy balance of new forested areas (Körner 2012; de Wit et al. 2014; Schwaab et al. 2015) by increasing C sequestration in plants and soils (Devi et al. 2008; Kammer et al. 2009). We observed that biomass stocks steadily increased by 39–86 times during the last 50 years, especially in the upper and middle parts of the ecotone. At the upper level, biomass accumulation was mainly associated with new tree’s establishment. However, the relevance of this process decreases with altitude while the role of radial growth to the production process increases. These observations partially contrasts with studies from other subarctic regions that also have shown a clear increase in stand productivity in the second half of the twentieth century, but with a recent decline in the accumulation rate attributed to stand aging (Myneni et al. 1997; Houghton 2005; Bunn et al. 2007).

Thus, our investigation show that observed changes of climatic conditions (an increase in precipitation in the dormant period and an increase in the average temperatures of the growth period in the absence of strong disruptive factors) had a multiplier effect on the growth and productivity of the examined treeline communities. Such a predictive tool can also assist in estimating potential future changes of treeline position. Taking into account local biotic and abiotic factors and processes the obtained patterns can be applied for entire upper treelines at the Polar Urals.


The present work for the first time quantified with annual resolution and for more than a century the impact of ongoing climate change on stand expansion, growth and productivity of a Polar Urals treeline ecotone, supporting numerous studies indicating the rapid shift of upper treelines. In particular we observed that the treeline moved 50 m upward and became denser. The long-term biomass assessment presented here provided information largely compatible with stand dynamic and tree-growth changes observed at the treeline ecotone at the Polar Urals during the last century. Our results also showed that the rate of afforestation, tree-ring growth, and biomass accumulation unidirectionally grew during the twentieth century and continue to accrue to the present time. These changes are driven by climate change mechanism, whereby the leading factors are the significant increase in early growth season temperatures and precipitation of the dormant period.

Availability of data and materials

The datasets used during the current study are available from the corresponding author on reasonable request.


m a.s.l.:

Meters above sea level


Tree-ring width


Time Series and Analysis Program


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We express our gratitude to Dr. Pavel Moiseev for constructive discussion on earlier version of the manuscript, as well as to Mr. Alexander Zubkov for his contribution during field survey. We thank Dr. Patrick Fonti for language editing and proofreading.


N.D., V.K., A.G., and A.G. were supported by the Russian Science Foundation (Grant No. 17–14-01112). V.M. was supported by the Russian Foundation of Basic Research (Grant No. 19–05-00756). Data collection was partly performed within the frameworks of a state contract with the Institute of Plant and Animal Ecology, Ural Branch, Russian Academy of Sciences.

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All co-authors performed the fieldwork. V. M, N.D., and V.K. measured the tree ring with, carried out the biomass calculation and interpreted the results. N.D. and V.K. wrote the manuscript. All authors read and approved the final manuscript.

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Correspondence to Vladimir V. Kukarskih.

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Appendix 1

Table 7 Statistical characteristics of tree-ring series

Appendix 2

Fig. 10
figure 10

Sample depth for larch (a) and spruce (b) at each selected forest type

Appendix 3

Fig. 11
figure 11

Kruskal-Wallis ANOVA and median test for dendrometric parameters of spruce (a, b, c) and larch (d, e, f) at each forest type

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Devi, N.M., Kukarskih, V.V., Galimova, А.A. et al. Climate change evidence in tree growth and stand productivity at the upper treeline ecotone in the Polar Ural Mountains. For. Ecosyst. 7, 7 (2020).

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