Impact of climate change on radial growth of Siberian spruce and Scots pine in North-western Russia

Abstract

Impact of climate change on radial growth of Siberian spruce and Scots pine in North-western Russia

Lopatin E (1-3), Kolström T (2), Spiecker H (4)

(1) University of Joensuu, Faculty of Forestry, P.O. Box 111, FI-80101, Joensuu (Finland); (2) Mekrijärvi Research Station, University of Joensuu, Yliopistontie 4, FI-82900, Ilomantsi (Finland); (3) Institute of Biology, Komi Scientific Center, Russian Academy of Sciences, Kommunisticheskaya str. 28, 167000, Syktyvkar (Russia); (4) Institute for Forest Growth, University of Freiburg, Tennenbacherstr. 4, D-79085 Freiburg (Germany)

: When adapting forest management practices to a changing environment, it is very important to understand the response of an unmanaged natural forest to climate change. The method used to identify major climatic factors influencing radial growth of Siberian spruce and Scots pine along a latitudinal gradient in north-western Russia is dendroclimatic analysis. A clear increasing long-term trend was identified in air temperature and precipitation. During the last 20 years, all meteorological stations experienced temperature increases, and 40 years ago precipitation began to increase. This is shown by the radial increment of Siberian spruce and Scots pine. Therefore, climate change could partly explain the increased forest productivity. The total variance explained by temperature varied from 22% to 41% and precipitation from 19% to 38%. The significant climatic parameters for radial increment in Komi Republic were identified, and the relation between temperature and precipitation in explained variance changes over time for Siberian spruce.

Keywords: Climate change, Growth trends, Pinus sylvestris L., Picea obovata Ledeb., Dendrochronology

Forest@ 4 (1): 28-41.© by the Italian Society of Silviculture and Forest Ecology.


Introduction

Climatic changes including a lengthening growing season (Menzel & Fabian 1999), increasing CO2 and nitrogen deposition (Makinen et al. 2003, Spiecker 1999, Spiecker 2000, Spiecker 2002) are assumed to cause increased forest growth. Climate change has been defined at global and local scales (Da Motta 2004, Knowlton et al. 2004, Mauro 2004, Meyneeke 2004, Miller 2003). Predictions of the future development of forest resources cannot be made without studying the response of trees to climate change.

Previous results indicate that northern forest ecosystems are among the regions at greatest risk from the impacts of climate change (IPCC 2001). According to IPCC (2001), warming trends have already started and in the future will increase. Most studies attribute the warming trends to accumulation of greenhouse gas (IPCC 2001).

In Europe, most forests are managed, except for those in north-western Russia, where there is a dominance of old-growth natural forests. It is important to understand the response of unmanaged natural forest to changing climate because it is possible to adapt forest management practices to a changing environment (Lopatin et al. 2006). Dendroclimatic analysis can be used to identify the major climatic factors that influence radial growth of tree species.

The largest administrative region of North-western Russia (forest area of Komi Republic is 33% of total North-western Russia’s forest area) was selected for the assessment of long-term forest growth trends. Komi is situated at the eastern boundary of the European part of Russia, in the boreal region where large areas of natural forest still exist. Borehole temperature measurements in Komi Republic indicate strong subsurface warming, reflecting changes in the trends of both surface air temperature and solid precipitation (Oberman & Mazhitova 2004).

The main objective of this research is to investigate the effect of climate change on radial growth of Siberian spruce (Picea obovata Ledeb.) and Scots pine (Pinus sylvestris L.) in north-western Russia (Komi Republic).

Climatically, Komi (Fig. 1) lies within the Arctic, Atlantic-Arctic and Atlantic-Continental provinces (Stolpovski 1997). Annual mean temperature varies between +1° C in the southern part of the republic and -6° C in the northern part, with the lengths of the growing season (days with mean temperature above +10° C) being 10 - 45 days. Annual rainfall decreases from 700 mm in the south to 450 mm in the north. Characteristic for the winter period, which lasts 130 - 200 days is accumulation of a thick snow cover (70-80 cm - Galenko 1983). The territory of Komi is characterized by surplus moisture. Mean annual evapotranspiration is significantly lower than annual rainfall (Tab. 1).

The vegetation cover of Komi is dominated by Middle and Northern taiga forests, with the exception of mountainous parts of the republic where forest-tundra and tundra ecosystems have developed (Larin 1997). Boreal vegetation is dominated by Scots pine (Pinus sylvestris L.), Siberian spruce (Picea obovata Ledeb.) and Siberian fir (Abies sibirica Ledeb.). Downy birch (Betula pubescens Ehrh.) forests are the first stages of post-fire succession, frequently with abundant aspen (Populus tremula L.).

Forests with Siberian spruce in Komi reach 16 mln. ha, i.e. 60% of the whole forest area. Siberian spruce in optimal conditions could reach a height of 35-40 meters and 90-110 cm diameter at breast height. Scots pine is distributed on 24% of the forest area and represents 23% of the total growing stock. The forest stands with high productivity are concentrated in the middle boreal zone of Komi. The mean heights are about 22-24 m, and the mean diameter is 28-30 cm with a growing stock of 160-190 m3 ha-1 (Kozubov & Taskaev 1999).

Komi is the most forest-rich region in north-western Russia. The forested area includes about 300 000 km2, making up 4.1% of Russian forested areas. The total stock of wood in the forests of Komi reaches 2855.8 mln. m3. The mean volume of wood is about 80-100 m3 ha-1. In southern regions the mean standing volume is 300 m3 ha-1.


Material and methods

Selection of sites and trees

The material was collected along a transect from the south of Komi (south taiga sub-zone of boreal forests) to the Arctic spruce timberline. The sampled stands were at similar altitudes. The study stands were grouped into “sub-zones” according to their geographical position in the taiga sub-zones of boreal forests. Totally 261 trees were collected in 5 sub-zones of taiga forests in Komi (Fig. 1, Tab. 2) and 696,929 tree rings were measured.

The sites were selected using GIS datasets of forest management units, old forest inventory maps and satellite images TERRA ASTER (scene size 60x60 km) with a spatial resolution of 15 m. In the procedure for site selection the main aim was to find the most common site types and at the same time exclude possible forest management or any other human impact from the past. Sites with a low productivity index (5 class, according to the classification system for Russian forest productivity) represents 70% of the forest area of Komi Republic (Kozubov & Taskaev 1999). The sites were selected to minimize the differences in exposure, soil properties, topography or vegetation development. To obtain information about changes in site productivity trees of different ages and comparable sites were selected. The trees were randomly sampled on sites of low fertility.

The stands were selected according the following criteria for site conditions:

In most of the regions in Komi the forest stands are multistoried. Therefore the sample trees were chosen from among trees not dominated by older trees but rather located in openings within the stand. The sample trees were expected to reveal homogeneity in their tree-ring pattern; they showed no obvious signs of near-neighbour competition or forest management. Trees were chosen from different diameter classes, healthy looking with straight, unbroken stems and regularly shaped crown. Mature dominant trees without visible signs of damage were selected as sample trees. The sample trees in the stands were expected to have a common growth trend, which was influenced by a large portion of the climatic effects and other factors which differ among individuals and from site to site. At each site an averaging process, during building chronology, helped to minimize the influence of other factors.

Prior to felling, for visual assessment of the tree ring pattern, a core from each tree was extracted with an increment borer. This allowed exclusion of those trees affected by competition in the past. Siberian spruces and Scots pines were sampled at breast height (1.3 m above the ground). In most cases, discs were cut using a chain saw. If it was difficult to cut discs, cores were extracted from trees with the increment borer from two radii per tree (the first one oriented to the north, the others at 900 -1200 to the first). Geographical coordinates of sample trees were measured using GPS.

Meteorological data

Monthly precipitation sums and air temperature means from 5 climate stations (WMO numbers 22996, 23804, 23711, 23412, 23219) were obtained from the Center of Meteorology and Environment Monitoring of Komi Republic (Fig. 1, Tab. 2) and the public archives (Razuvaev et al. 1995 Vose et al. 1992). Climate records were checked for consistency and homogeneity (Razuvaev et al. 1995). Meteorological data were used for identification of dendroclimatic relationships and long-term trends in climate change. To identify long-term trends in climate, the deviations in absolute units from the long-term mean were calculated for the common period. The deviations were then smoothed with a 30-year running mean.

Chronology development

Radial increments were measured to an accuracy of 0.01 mm. During the process of measurement, the raw measurements of tree rings were cross-dated using visual control, by comparing the series graphically. Cross-dating and data quality were assessed using the computer program COFECHA (Grissino-Mayer et al. 1997, Holmes 1999).

To maximize the climatic signals in tree ring series, other factors should be minimized. For example, a typical sample might display exponentially declining growth with age, the classic biological growth curve. Standardizing the sample using a spline curve results in data values that represent a departure from the “expected” value for a given year. This departure from the expected mean value is then used to interpret a proxy environmental signal in the data. The above-mentioned procedure usually is an attempt to remove the growth trends due to normal physiological ageing processes and changes in the surrounding forest community. Therefore individual ring-width series were indexed using spline curves of 60 years with a frequency response of 50%. This approach was selected due to the high amount of variance in the dataset because of using the trees from different age cohorts for chronology building.

The common interval (1954 - 2003) adjusted for order of the pooled autoregressive model was used for analysis of climate-growth relationships. Indices were further prewhitened using Box Jenkins methods of autoregressive and moving average time series modelling (ARMA - Box & Jenkins 1976, Cook 1985, Monserud 1986). The order of the autoregressive-moving mean process was determined by Akaike Information Criteria (Akaike 1974, Cook 1985). Prewhitening allows us to transform autocorrelated series into a series of independent observations by extracting residuals from the modelled process. Chronologies were produced by averaging the annual values of indices. The software ARSTAN (Grissino-Mayer et al. 1997, Holmes 1999) was used to calculate chronologies from tree-ring measurement series by detrending and indexing (standardizing) the series, then applying a robust estimator of the mean value function to remove the effects of endogenous stand disturbances.

Residual ARSTAN chronologies containing high frequency variation were used to examine climate-growth relationships on an interannual basis.

Chronology confidence was determined using statistics of Expressed Population Signal (EPS - Wigley et al. 1984). EPS was computed as a function of mean inter-tree correlation and sample size. In general, it can be assumed that values of EPS equal to or greater than 0.85 are indicators of reliable chronology (Cook & Kairiukstis 1990). Here EPS was computed over the time window of 50 years (1954-2003).

Statistical analysis of growth-climate relationships

Response function analysis (Cook & Kairiukstis 1990) was applied to determine which monthly weather variables significantly affected high frequency variation in radial increment of Scots pine and Siberian spruce. The monthly mean air temperature and monthly sums of precipitation were used to analyse the response of trees to current and previous years. The DENDROCLIM2002 software was applied for the analysis, using bootstrapped confidence intervals to estimate the significance of both correlation and response function coefficients and testing their significance at the 0.05 level. The temporal stability of dendroclimatic relationships was illustrated using correlation coefficients of significant (p


Results

Site chronologies

Using collected samples 9 site chronologies of Scots pine and Siberian spruce radial increments were constructed for 5 sites. The expressed population signal (EPS) of chronologies was calculated for the common interval (1954 - 2003). Five of nine chronologies (Tab. 3) are within the well-accepted EPS threshold of 0.85 (Cook & Kairiukstis 1990). However some of the chronologies are covering longer time interval, starting from 1786, and this time interval cannot be used for the extraction of common climatic signal due to the fact that prior 1954 EPS statistics were worse. Therefore the only 5 site chronologies (Fig. 2), that are representative of the true population during the common period, were selected for the dendroclimatic analysis.

Responses to mean monthly temperatures and monthly precipitations sums

In western part of Middle taiga zone the statistically significant positive response of Scots pine to the monthly mean temperatures of November year prior to growth and May of the current growth season was found (Fig. 3B). There was no other significant response to temperature (Fig. 3A, C, D, E).

Response function analysis showed positive (Fig. 3A, D) and negative (Fig. 3B, C) response of the radial increment to the monthly sums of precipitation. Radial increment of Siberian spruce was influenced by November precipitations of the year prior to growth in eastern part of Middle taiga zone (Tab. 2, site 4) and June precipitations in eastern part of Middle taiga zone. Radial increment of Scots pine was influenced by September precipitations of the year prior to growth in eastern part of Middle taiga zone and June precipitations in eastern part of Middle taiga zone (Tab. 2, site 4). In western part of Middle taiga zone (Tab. 2, site 3) the response of Scots pine and Siberian spruce to the precipitations was opposite (Fig. 3 B, D).The increase in precipitation positively affected the radial increment of Spruce and negatively the radial increment of Pine. The similar difference between Pine and Spruce in response to the monthly sums of the autumn precipitations of the year prior to growth was found in eastern part of Middle taiga zone (Fig. 3A, C). The difference in response to the monthly sums of precipitations within the Middle taiga zone is explained by the geographical position of the sites (Fig. 1).

No statistically significant responses to temperatures and precipitations were found for Scots pine in Southern taiga zone (Fig. 3E). The lengths of growing season and annual evapotranspiration (Tab. 1) is longer here, comparing with Middle taiga zone. This is also confirmed by the smallest amount of variance explained by climate (Tab. 4).

The variance explained by the mean monthly temperature varied from 26% to 48% (Tab. 4). The highest explained variance by temperature is in most northern site chronology of Scots pine, the lowest in Southern taiga. The variance explained by the monthly sums of precipitations varied from 26% to 44%. The variation of radial increment explained by the precipitations is highest for both species in eastern part of the Middle taiga zone. There is a clear gradient of increasing amount of variance explained by monthly precipitation sums from south to north (Tab. 4). The total amount of variance in radial increment explained by climate varied from 43% to 70%.

Temporal stability of growth-climate relationships

The variables identified in dendroclimatic analysis as significant for the radial increment of Scots pine and Siberian spruce in Middle taiga zone were retested for the temporal stability of the relationships using 25-year window correlation. In this step we were looking to disprove (p>0.05) a correlation bet­ween a monthly climate parameters and ring-width chronologies for a given 25-year period if r

The statistically significant changes in correlations between climate variables and radial increment were identified for Siberian spruce (Fig. 4). In eastern part of the Middle taiga zone the correlation between precipitations of November year prior growth changed since 1987 and was significantly non stable years after 1987. The relations to temperature of June also changed in the western part of Middle taiga zone in 1987. The dendroclimatic relationships of Scots pine were also changing over the time, but those changes were statistically not significant.

The amount of variance of radial increment explained by the monthly mean temperatures and monthly precipitation sums changed over the period 25 years from 14% to 20% (Tab. 5). In western part for Siberian spruce and eastern part of Middle taiga zone for Scots pine the amount of explained variance increased on 7% and 14%. But other 3 chronologies showed decrease in explained amount of variance from 2% to 20%. Therefore using those ring-width chronologies and monthly climate data for the period from 1954 to 2003 it is not possible to make conclusion on changes in dependency of the radial increment from climate.

Climate change analysis

Fig. 5 shows the deviation in degrees C from the long-term mean (70 years) temperature and in millimetres from the mean annual sum of precipitation at the 3 meteorological stations included here with the longest period of observation. There is clear evidence during recent decades that the climate in the Komi Republic has changed. During the last 20 years the mean annual air temperature has increased, and over the last 40 years the annual precipitation sum at meteorological stations has also increased. But the impact of each month on the annual result differs over time (Fig. 6).

In some months the trends are positive, and others have some negative trends. As shown above for the boreal zone, the radial growth of trees could be attributed to certain months. Deviations from means in temperature, which are significant for radial increment of pine and spruce in Komi, are shown on Fig. 6. In our study the significance of those climatic parameters for radial increment was identified by response function analysis. The decrease in temperature of May in western part of the Middle taiga zone most probably was compensated by increase of temperature in November of the year prior to growth and increase in precipitations of June (Fig. 6). The positive response of Siberian spruce in the western part of Middle taiga zone to the precipitations of June was reflected in tree ring width (Fig. 5, Fig. 6).


Discussion

The limit of this study is its spatial representativeness of the selected stands for different sub zones of taiga (Lopatin et al. 2006). It is important to understand changes in forest productivity not only on a temporal scale, but also in spatial terms. Currently, due to the low accessibility and huge size of the territory, it is impossible to create systematic sample plots in Komi Republic. Therefore, to make conclusions about spatial response distributions other methodological approaches need to be used.

Another limit of this study for the climate reconstruction is the potential bias due to the different ages of the sampled trees. It was shown that the climatic signal is maximized in older trees and the higher amount of noise present in younger trees (Carrer & Urbinati 2004). But from the standpoint of forest management, for the purpose of understanding factors influencing radial increment of trees in the forest, represented by different age classes, this bias is not important.

The statistical relationships of Siberian spruce growth to climate in Middle taiga zone of Komi have changed over the last century. This is due to changes in temperature and precipitation or to changes in the sensitivity of trees to climate. The changes in tree-ring sensitivity could be attributed to ultraviolet radiation (Briffa et al. 1998), increased atmospheric CO2, nitrogen deposition (Kellomaki et al. 1997, Kellomaki & Vaisanen 1997, Kellomaki & Wang 1997a, Kellomaki & Wang 1997b), ozone exposure (Bartholomay et al. 1997, Wager & Baker 2003), pollution, and cycles in sunspot activity (Raspopov et al. 2004).

The method of analysing the factors influencing growth trends through the building chronology with standardization of raw tree ring measurements for the whole sub zone of taiga contains some limiting factors. At present it is impossible to find an ideal curve that removes variation in the radial increment caused by ageing, competition, stand dynamics and other factors reflected in tree rings and at the same time preserving the long-term growth trend. Furthermore, it is even more difficult to find an individual curve for each separate factor. However, the method could be used in case of a large number of sampled trees, and those limits could be minimized due to the process of averaging. In this study the low-frequency variation caused by the above-mentioned factors was removed, but with the understanding that standardization partly removes long-term growth trends, which belong to low- and medium-frequency growth variation, i.e. periods more than 30 years.

In Boreal forests, the climate change scenarios imply a great rise in temperature and in precipitation, especially in winter. Higher precipitation in summer may compensate for the enhanced evapotranspiration, making sufficient amounts of water available for forests. Longer growing seasons reduce the soil frost. In northern Europe under warmer conditions the Siberian spruce and Scots pine are likely to invade the tundra region and higher elevations (IPCC 2001). Therefore, it is probable that climatic warming will stimulate early initiation of photosynthesis in spring, resulting in better utilization of solar radiation and increased productivity.

On most of the studied sites there are increasing long-term trends in total monthly precipitation and mean monthly air temperatures that are important for radial growth. This increase could be attributed to a factor that causes increasing site productivity in Komi. But due to the big difference in climate conditions through the Komi Republic, there is no one single or clearly identified group of monthly climate parameters that affected the growth at all sites.

The analysis of the variables for the other months showed the increase in temperature and precipitation was due to the trends in months that are significant for radial increment. The importance for radial increment months with positive trends is higher.

The absence of statistically significant response (pFig. 4A, C, D, E) in dendroclimatic analysis to the air temperature does not show the absence of relation between radial increment and temperature, because relatively big amount of variance could be explained by the monthly temperature (Tab. 4). The absence of response in several chronologies testes using DENDROCLIM 2002 could be due to the possible non-linear relationships between temperature and radial increment or relatively short period (50 years) used for calculation response function coefficients.

The amount of variance explained by the temperature is larger than the amount explained by precipitations (Tab. 4) except for Siberian spruce in the eastern part of Middle taiga zone. However, the territory of Komi is characterized by surplus moisture; mean annual evapotranspiration is significantly lower than annual rainfall (Tab. 1). It was shown on pine growth in Sweden (Jonsson 1969) that response of ring-width to this parameter might be non-linear and therefore might be difficult to evaluate using methods assuming a linear weather-growth relationship (as for example, response function analysis - Drobyshev et al. 2004). In boreal regions the potential impact of precipitation is related to temperature.

The difference in response of spruce growth in different sub-zones is explained by the difference in climatic parameters, climate change trends and differences in the ecological characteristics of different provenances. The changes in air temperatures in Komi Republic are not distributed equally over the territory. The response to the temperatures in the western part of Middle taiga zone could be attributed to the increasing length of the growing season due to increasing temperature in May and November. We are assuming that during the recent decades cambial activity already started at the first weeks of May, because the temperature in this period was often above + 5°C.

The response of high frequency variation in radial increment of pine to summer temperatures was reported for different sites in Northern Europe (Helama et al. 2002, Kalela-Brundin 1999, Kirchhefer 2001, Linderholm et al. 2003, Lindholm 1996, Lindholm & Eronen 2000, Miina 2000). This pattern was also found in our study (i.e. Scots pine in western part of Middle taiga zone), but without the strongest response to the July temperature. The possible explanations are the selection of sites in multistoried forests and the influence of continental climate. In the Komi Republic there is a continental climate (Tab. 1) with more extreme climate conditions than those in Finland, Sweden and Norway, which are greatly influenced by the Gulf Stream.

The general decrease in amount of variance explained by climate is in accord with the findings on reduced correlations between growth and temperature in subarctic Eurasia (Vaganov et al. 1999).


Conclusions

A clear long-term trend in climate change was identified. At all meteorological stations the air temperature increased during the last 20 years, and total precipitation started to increase 40 years ago. This is reflected in the radial growth increment of Siberian spruce and Scots pine. Thus, climate change could partly explain the increased site productivity.

The total variance explained by temperature varies from 26% to 48% and precipitation from 26% to 44%. The climate factors influencing increased radial increment of Siberian spruce differ from those in Scots pine. The higher temperatures allow enhancement of evapotranspiration, which is why both temperature and precipitation affected radial increment positively. The temporal stability of dendroclimatic relationships has changed for radial growth of Siberian spruces in western and eastern parts of Middle taiga zone. The statistically significant climatic parameters influencing radial increment of spruce and pine in Komi were identified. The increased radial increment of spruce and pine in Komi is attributed primarily to the increase in temperature. But the correlation of precipitation sums and air temperature with radial increment of Siberian spruce in Middle taiga zone changes over the time. Climate change is causing increasing site productivity, but its direct influence, identified by means of response function analysis, explains only part of the high frequency variations in radial increment. Taking into account the correlation with climate variables and their temporal stability, it is possible to simulate the future development of forest resources in Komi under the changing climate. For purposes of forest management, new climate-sensitive growth models should be developed.

Acknowledgements
This study was supported by a CIMO fellowship grant TM-04-2734, NorFA grant “Network for Dendrochronological Research in Northern Europe”, travelling grants from the Graduate School in Forest Sciences (University of Joensuu), the project Intensification of forest management and improvement of wood harvesting in North West Russia in the research programme Russia in flux funded by the Academy of Finland, Russian Foundation for Basic Research (project 06-04-48792). Thanks to Dr. Hans-Peter Kahle for critical comments that helped to improve this manuscript. Mekrijarvi Research Station provided excellent facilities for measuring the discs and cores from Russia. Dr. Bruce Miche helped improve the language of the manuscript.


References

  1. Akaike H (1974). A new look at the statistical model identification. IEEE Transactions on Automatic Control AC-19: 716-723.
  2. Bartholomay GA, Eckert RT, Smith KT (1997). Reductions in tree-ring widths of white pine following ozone exposure at Acadia National Park, Maine, USA. Canadian Journal of Forest Research - Revue Canadienne de Recherche Forestiere 27: 361-368.
  3. Box GEP, Jenkins GM (1976). Time series analysis: Forecasting and control (revised edition). San Francisco, Holden-Day.
  4. Briffa KR, Schweingruber FH, Jones PD, Osborn TJ, Shiyatov SG, Vaganov EA (1998). Reduced sensitivity of recent tree-growth to temperature at high northern latitudes. Nature 391: 678-682.
  5. Carrer M, Urbinati C (2004). Age-dependent tree-ring growth responses to climate in Larix decidua and Pinus cembra. Ecology 85: 730-740.
  6. Cook ER (1985). A time series analysis approach to tree-ring standardization. University of Arizona, Tucson, pp. 171.
  7. Cook ER, Kairiukstis LA (1990). Methods of dendrochronology. Applications in the environmental sciences. International Institute of Applied System Analysis, Kluwer Academic Publishers, Dordrecht, The Netherlands.
  8. Da Motta RS (2004). Sustainable forest management and global climate change: Selected case studies from the Americas. Environment and Development Economics 9: 272-276.
  9. Drobyshev I, Niklasson M, Angelstam P (2004). Contrasting tree-ring data with fire record in a pine-dominated landscape in the Komi republic (Eastern European Russia): Recovering a common climate signal. Silva Fennica 38: 43-53.
  10. Galenko E (1983). Phytoclimate and ecological factors of increasing productivity of boreal forests in Russian European North. Nauka, Leningrad.
  11. Grissino-Mayer H, Holmes R, Fritts H (1997). International tree-ring data bank program library manual. Tucson, Arizona, Laboratory of Tree-Ring Research, University of Arizona.
  12. Helama S, Lindholm M, Timonen M, Merilainen J, Eronen M (2002). The supra-long Scots pine tree-ring record for Finnish Lapland: Part 2, inter-annual to centennial variability in summer temperatures for 7500 years. Holocene 12: 681-687.
  13. Holmes R (1999). Dendrochronology program library. User’s manual. Tucson, Arizona, USA, Laboratory of Tree-Ring Research, University of Arizona.
  14. IPCC (2001). Climate Change 2001: The Scientific Basis. Contribution of Working Group I to the Third Assessment Report of the Intergovernmental Panel on Climate Change (Houghton JT, Ding Y, Griggs DJ, Noguer M, van der Linden PJ, Dai X, Maskell K, Johnson CA eds). Cambridge University Press, Cambridge, United Kingdom and New York, NY, USA, pp. 881.
  15. Jonsson B (1969). Studier över den avvä derleken orsakade variationen i å rsringsbredderna hos tall och gran i Sverige. 16, 1-279. Rapporter och Uppsatser, Institution for skogsproduction, Skogsh ö gskolan.
  16. Kalela-Brundin M (1999). Climatic information from tree-rings of Pinus sylvestris L. and a reconstruction of summer temperatures back to AD 1500 in Femundsmarka, eastern Norway, using partial least squares regression (PLS) analysis. Holocene 9: 59-77.
  17. Kellomaki S, Vaisanen H (1997). Modelling the dynamics of the forest ecosystem for climate change studies in the boreal conditions. Ecological Modelling 97: 121-140.
  18. Kellomaki S, Vaisanen H, Kolstrom T (1997). Model computations on the effects of elevating temperature and atmospheric CO2 on the regeneration of Scots pine at the timber line in Finland. Climatic Change 37: 683-708.
  19. Kellomaki S, Wang KY (1997a). Effects of elevated O3 and CO2 on chlorophyll fluorescence and gas exchange in Scots pine during the third growing season. Environmental Pollution 97: 17-27.
  20. Kellomaki S, Wang KY (1997b). Photosynthetic responses of Scots pine to elevated CO2 and nitrogen supply: Results of a branch-in-bag experiment. Tree Physiology 17: 231-240.
  21. Kirchhefer AJ (2001). Reconstruction of summer temperatures from tree-rings of Scots pine (Pinus sylvestris L.) in coastal northern Norway. Holocene 11: 41-52.
  22. Knowlton K, Rosenzweig C, Goldberg R, Lynn B, Gaffin S, Hogrefe C, Civerolo K, Ku JY, Solecki W, Small C, Oliveri C, Cox J, Rosenthal J, Kinney PL (2004). Evaluating global climate change impacts on local health across a diverse urban region. Epidemiology 15: S-100.
  23. Kozubov GM, Taskaev AI (1999). Forestry and forest resources of Komi Republic. Dik Publishing House, Moscow, Russia (in russian).
  24. Larin V (1997). Forests, their exploitation and regeneration. In: Republic of Komi. Komi Publishing House, Syktyvkar, Russia, pp. 34-40.
  25. Linderholm HW, Solberg BO, Lindholm M (2003). Tree-ring records from central Fennoscandia: the relationship between tree growth and climate along a west-east transect. Holocene 13: 887-895.
  26. Lindholm M (1996). Reconstruction of past climate from ring-width chronologies of Scots pine (Pinus sylvestris L.) at the northern forest limit in Fennoscandia. University of Joensuu, pp. 7-169.
  27. Lindholm M, Eronen M (2000). A reconstruction of mid-summer temperatures from ring-widths of Scots pine since AD 50 in northern Fennoscandia. Geografiska Annaler Series A-Physical Geography 82A: 527-535.
  28. Lopatin E, Kolstrom T, Spiecker H (2006). Determination of forest growth trends in Komi Republic (northwestern Russia): combination of tree-ring analysis and remote sensing data. Boreal Environment Research 11: 341-353.
  29. Makinen H, Nojd P, Kahle HP, Neumann U, Tveite B, Mielikainen K, Rohle H, Spiecker H (2003). Large-scale climatic variability and radial increment variation of Picea abies (L.) Karst. in central and northern Europe. Trees-Structure and Function 17: 173-184.
  30. Mauro G (2004). Observations on permafrost ground thermal regimes from Antarctica and the Italian Alps, and their relevance to global climate change. Global and Planetary Change 40: 159-167.
  31. Menzel A, Fabian P (1999). Growing season extended in Europe. Nature 397: 659.
  32. Meyneeke JO (2004). Effects of global climate change on geographic distributions of vertebrates in North Queensland. Ecological Modelling 174: 347-357.
  33. Miina J (2000). Dependence of tree-ring, earlywood and latewood indices of Scots pine and Norway spruce on climatic factors in eastern Finland. Ecological Modelling 132: 259-273.
  34. Miller CE (2003). Satellite observations of global climate change. Abstracts of Papers of the American Chemical Society 226: U23.
  35. Monserud RA (1986). Time-Series Analyses of Tree-Ring Chronologies. Forest Science 32: 349-372.
  36. Oberman NG, Mazhitova GG (2004). Permafrost dynamics in the north-east of European Russia at the end of the 20th century. Norwegian Journal of Geography 55: 241-244.
  37. Raspopov OM, Dergachev VA, Kolstrom T (2004). Periodicity of climate conditions and solar variability derived from dendrochronological and other palaeoclimatic data in high latitudes. Palaeogeography Palaeoclimatology Palaeoecology 209: 127-139.
  38. Razuvaev VN, Apasova EG, Martuganov RA (1995). Six- and Three-Hourly Meteorological Observations from 223 USSR Stations. ORNL/CDIAC-66, NDP-048. Carbon Dioxide Information Analysis Center, Oak Ridge National Laboratory, Oak Ridge, Tennessee, USA.
  39. Spiecker H (1999). Overview of recent growth trends in European forests. Water Air and Soil Pollution 116: 33-46.
  40. Spiecker H (2000). Growth of Norway Spruce (Picea abies (L.) Karst.) under changing environmental conditions in Europe. In: Spruce Monocultures in Central Europe: Problems and Prospects (Klimo E, Hager H, Kulhavy J eds). European Forest Institute. European Forest Institute Proceedings 33, pp. 11-26.
  41. Spiecker H (2002). Tree rings and forest management in Europe. Dendrochronologia 20: 191-202.
  42. Stolpovski PM (1997). Republic of Komi. Komi Publishing House, Syktyvkar.
  43. Vaganov EA, Hughes MK, Kirdyanov AV, Schweingruber FH, Silkin PP (1999). Influence of snowfall and melt timing on tree growth in subarctic Eurasia. Nature 400: 149-151.
  44. Vose RS, Schmoyer RL, Steurer PM, Peterson TC, Heim R, Karl TR, Eischeid JK (1992). The Global Historical Climatology Network: Long-term monthly temperature, precepitation, sea level pressure and station pressure data. ORNL/CDIAC-53, NDP-041. Carbon Dioxide Information Analysis Center, Oak Ridge National Laboratory, Oak Ridge, Tennessee, USA.
  45. Wager DJ, Baker FA (2003). Potential effects of ozone, climate, and spruce budworm on Douglas-fir growth in the Wasatch Mountains. Canadian Journal of Forest Research - Revue Canadienne de Recherche Forestiere 33: 910-921.
  46. Wigley TM, Briffa KR, Jones PD (1984). On the average value of correlated time series, with applications in dendroclimatology and hydrometeorology. Journal of Climate and Applied Meteorology 23: 201-213.
  47. Zagreev VV (1992). General yield tables for normal stands. In: Forest Inventory Handbook, all union rules and regulations for the forest inventory. Kolos, Moscow, pp. 298-231.

Figures

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Fig. 1 - Sampled stands and sub zones of taiga boreal forests. Borders of vegetation complexes according to Kozubov & Taskaev ([23]). Numbers refers to the zones, see table 2.

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Fig. 2 - Standardized tree-ring chronologies of Siberian spruces smoothed with a 10-year moving average, shown as a deviations from the mean (n = number of trees).

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Fig. 3 - Response function analysis tree-ring chronologies for common interval 1954-2003. Lower case “p” denotes months in the year previous to the current year growth season. Filled bars of response function coefficients are significant at p

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Fig. 4 - Temporal stability of dendroclimatic relationships estimated for the common interval of 50 years (1954-2003). Lower case “p” denotes months in the year previous to the current year growth season. Upper case “T” and “P” denotes temperature and precipitation of the months. Confidence intervals are showed with dashed lines.

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Fig. 5 - Deviation in degrees C from long-term mean annual temperature and in mm from mean long-term annual sum of precipitation on analysed meteorological stations, smoothed using 30-year running mean.

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Fig. 6 - Absolute deviations from long-term means for mean monthly temperature (A) and monthly sums of precipitations (B, C) that are significant for radial increment of pine and spruce in Komi smoothed with the 30-years running mean.

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Tables

Tab. 1 - Climatic characteristics in different taiga sub zones in Komi ([10]).

Sub zone of taiga boreal forest Vegetation period, days Precipitation, mm Annual
evapotranspiration, mm
May -
October
October - April
Northern forest - tundra transition zone 117 235 190 125
Northern taiga 143 290 190 175
Middle taiga 158 330 260 200-250
South taiga 177 370 250 300

Tab. 2 - Tree ring data collected in Komi Republic in 2003-2005. (§) The Scots pine trees not found in forest-tundra transition zone.

Site Forest zone Location
coordinates
Siberian spruce Scots pine Distance to
meteo-
station,
km
Meteo-station,
analysed period
n trees Time Span Min-Max Mean n trees Time Span Min-Max Mean
1 Forest - tundra transition zone(§) 66°41’260” N
56°49’142” E
16 1812
2005
71-192
115.6
- - - 125 Khoseda - Khard,
1933-1995
2 Northern taiga zone 65°59’697” N
57°48’820” E
16 1878
2005
37-126
75.3
20 1924
2005
52-80
69.3
42 Ust-Usa,
1936-2003
3 Middle taiga zone (west) 61°44’834” N
50°34’910” E
40 1779
2005
38-225
104.3
45 1786
2005
34-218
93.6
30 Syktyvkar,
1896-2004
4 Middle taiga zone (east) 63°25’294” N
57°57’597” E
51 1826
2005
27-176
91.3
21 1842
2005
142-163
152
130 Troitsko-Pechersk,
1893-2004
5 South taiga zone 60°33’615” N
49°26’945” E
30 1917
2005
18-89
52.8
22 1877
2005
28-127
73
38 Objachevo,
1944-2004
Total: 153 - - 108 - - Mean
73
-

Tab. 3 - Expressed population signal of chronologies for the period 1954 - 2003.

Site Forest
zone
Siberian
spruce
Scots
pine
1 Forest - tundra transition zone 0.41 -
2 Northern limit of the Northern taiga zone 0.63 0.71
3 Middle taiga zone (east) 0.85 0.85
4 Middle taiga zone (west) 0.86 0.85
5 South taiga zone 0.85 0.61

Tab. 4 - Amount of variance (R2) explained by temperature (T) and precipitations (P) for the period 1954-2003.

Site Forest zone Siberian spruce Scots pine
P T P and T P T P and T
3 Middle taiga zone (east) 0.416 0.390 0.641 0.446 0.484 0.646
4 Middle taiga zone (west) 0.402 0.413 0.652 0.220 0.386 0.702
5 South taiga zone 0.220 0.264 0.435 - - -

Tab. 5 - Temporal stability of the amount of variance (R2) explained by temperature and precipitations for 2 subsequent 25-years periods.

Forest
zone
Time
span
Siberian
spruce
Scots
pine
Middle taiga zone (east) 1954-1978 0.649 0.574
1979-2003 0.727 0.388
Middle taiga zone (west) 1954-1978 0.309 0.228
1979-2003 0.292 0.370
South taiga zone 1954-1978 0.639 -
1979-2003 0.420 -


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