SEEFOR 11(2): 135-144
Article ID: 2011
ORIGINAL SCIENTIFIC PAPER
Tree Growth Variability of Pinus heldreichii at Tree-Line Locations in Kosovo**
Faruk Bojaxhi1*, Ervin Toromani2, Nehat Çollaku2
(1) University of Prizren, Forestry and Environment Faculty, Rruga e Shkronjave, nr.1, 20000 Prizren, Kosovo**;
(2) Agricutural University of Tirana, Faculty of Forestry Sciences, Koder Kamez, AL-1029 Tirana, Albania
* Correspondence: e-mail: email@example.com
Citation: Bojaxhi F, Toromani E, Çollaku N, 2020. Tree Growth Variability of Pinus heldreichii at Tree-Line Locations in Kosovo. South-east Eur for 11(2): 135-144. https://doi.org/10.15177/seefor.20-11.
Received: 7 Mar 2020; Revised: 14 Jun 2020; Accepted: 19 Jun 2020; Published online: 21 Sep 2020
** This designation is without prejudice to position on status, and is in line with UNSC 1244 and the ICJ Opinion on the Kosovo declaration of independence.
It is well-known that tree growth at the upper treeline is controlled by low temperatures and limited seasonal growth. The study’s objective was to investigate the climate warming effects on Bosnian pine (BP; Pinus heldreichii Christ.) growth during the 20th century. We hypothesized that, like all the other drought-stressed conifers growing on tree-line locations, BP responds significantly to climate factors that control their growth. Three natural forest stands of BP were selected in Prevalla, Decan and Koritnik. The cores were taken from 98 dominant and co-dominant BP trees at breast height with no sign of human interference. The tree-ring widths were measured at 0.001 mm precision, with a LINTAB 6 (RINNTECH, Heidelberg) system and TSAP-Win Scientific software. A set of three BP tree-ring width chronologies were developed by trees spread on a typical mountain slope at elevations ranging from 1815 to 1945 m above sea level. The tree-ring chronologies from three sites showed significant correlation and this agreement decreased with the distance between sites. The length of the master chronologies varies among sites ranging from 176 years (Koritnik) to 541 years (Decani). The tree growth was controlled by a common climatic signal (local temperatures) and drought during midsummer across the investigated sites. These results confirm the assumption that tree growth at tree-line sites is controlled by low temperatures and drought conditions during the midsummer.
Keywords: Bosnian pine; tree line; SPEI; Forward Evolutionary Interval Analysis
Bosnian pine (Pinus heldreichii Christ., Hereafter "BP") is one of the main conifer species growing in Kosovo. The species inhabits high elevations (over 1500 ma.s.l) within the Western, South and South-Western Kosovo (Figure 1). Despite its limited distribution in the Balkans and southern Italy, the species has been widely used in dendroclimatic studies. Previous studies have been conducted in Bulgaria (Panayatov et al. 2009, 2010), Greece (Branders 2007, Griggs et al. 2007), and Albania (Seim et al. 2012), exploring climate–growth relationship of this high-elevation species. Moreover, summer temperature was reconstructed (1768–2008), based on maximum latewood density measurements of P. heldreichii trees from a high-elevation stand in the Pirin Mountains in Bulgaria (Trouet et al. 2012). In Albania, a 1391-year tree-ring width chronology (617–2008) was developed and maximum density measurements were acquired on living and dead P. heldreichii trees (Seim et al. 2010).
The overall forest area covered by P.heldreichii in Kosovo amounts to 2150 ha, mostly mixed with species like silver fir (Abies alba Mill.). Some natural forest stands of this species exist in Kosovo, situated in Prevalla, Koritnik and Decani regions respectively, but only two dendroclimatic studies have been conducted to date (Bojaxhi and Toromani 2016, 2017). The high conservational value of such taxa additionally increases the importance of tree-ring width-based studies that allow a better understanding of the climate – radial growth relationship as well as eco-physiological requirements of trees.
Previous dendroclimatic studies conducted in Kosovo found that BP growing in high elevation locations is sensitive to summer drought stress and the magnitude of sensitivity was higher in young trees. The negative effect of summer drought stress on BP radial growth is expected to be more pronounced with climate warming in the coming years.
In order to enhance our understanding of climate warming effects on BP growth during the 20th century, we aimed to pursue this study following these objectives: (i) assessing the cross-dating potential of BP growing on various sites; (ii) investigating the potential relationships between climate and BP growth, and (iii) elucidate temporal and spatial variability in relationships identified between climate and BP. We hypothesized that, like the other drought-stressed conifers growing on tree-line locations, BP responds to climate factors that influence moisture availability. An improved perspective of the dendroclimatic potential of BP could enhance our understanding of climate effects in natural ecosystems and strengthen the spatial and temporal resolution of the tree-ring record in Kosovo.
MATERIALS AND METHODS
The study area includes natural ecosystems located close to the upper distribution limit of BP at Prevalla (hereafter, PRE) - (42°11'N, 20°57'E; 1945 m a.s.l), Decan (hereafter DE) - (42°36'N, 20°14'E; 1830 m a.s.l), and Koritnik (hereafter, KO) - (42°04'N, 20°31'E; 1815 m a.s.l) in western and southern Kosovo (Table 1, Figure 1).
Soil types formed on limestone bedrocks are dominated by leptosols (rendzinas) and brown soils and have slight differences among sites. At all sampled sites BP is the dominant species, while the ground vegetation comprises species such as Sesleria autumnalis Ard., Brachypodium sylvaticum Huds., Carex humilis Leyess., Thymus balcanus L., Fragaria vesca L., Festuca heterophylla Lam., Dactylus glomerata L., etc. These forest stands are growing under the effect of continental climate with some influences of the Mediterranean climate in southern Kosovo. The mean annual temperature varied among sampled sites and ranged from 8.0°C (PRE) to 8.3°C (KO). The average annual precipitation ranged from 791 mm (DE) to 1029 mm (KO) (CRU TS. v 3.22 dataset by Jones 2014, period 1901-2013) and is bimodally distributed with a pronounced maximum during May and a secondary peak in November (Figure 2). The growing season at all three sites lasts 5 months, from May to September. The natural forest stands of BP grow on sites with different slope aspects ranging from NW for DE and KO sites to SW for PRE site.
Field and Laboratory Methods
The collection of samples took place from July to September 2014. In total, 89 trees were sampled, and two cores per tree were extracted at breast height (ca 1.3 m from ground) with an increment borer, but only 85 sampled trees were used to build chronologies at three sites. Dominant and co-dominant BP trees with umbrella-like crowns growing on shallow and poor soils were cored to obtain a sensitive chronology. Increment cores were dried fixed onto wooden mounts with cells vertically aligned (Stokes and Smiley 1996) and sanded. All cores were surfaced using progressively finer sandpaper beginning with ANSI 120-grit and finishing with ANSI 400-grit. Some cores could not be included in our dendroclimatological analyses due to ring anomalies associated with the lobate growth form, twisted stems, and predominance of false rings that mimicked true rings (Schweingruber 1993). Annual tree-ring widths were measured to an accuracy of 0.001 mm using a LINTAB 6 (RINNTECH, Heidelberg) system and TSAP-Win computer software. Cores were visually cross-dated and cross dating was statistically verified with COFECHA software (Holmes 1983). Each measured radius was processed by COFECHA as an individual time-series subdivided into 40-year segments sequentially overlapped by 20 years. We used the ARSTAN program (Cook 1985) to standardize all series applying a double detrending procedure to remove adverse growth effects from age-related growth trends, autocorrelation, and possible natural or anthropogenic influences that could interfere with the climate signal within the growth rings. First, detrending was conducted using a negative exponential curve and then second detrending was done by using cubic smoothing spline curves of 30 years in order to preserve the common climatic signal. The actual ring measurement was then divided by the predicted value to produce a dimensionless index of growth for that year (mean=1.0).A final master chronology was created for each site from the tree-ring data by averaging all indices of tree growth for each year across all series (Cook 1985).Chronology quality was estimated using Rbar and Expressed Population Signal statistics (EPS) with a limit value of 0.85 (Wigley et al. 1984).Rbar is a measure of the strength of the common growth "signal" within the chronology (Briffa and Jones 1990), while the EPS is an estimate of the chronology’s ability to represent the signal strength of a chronology on a theoretical infinite population (Briffa and Jones 1990). Three chronologies (standard, residual and arstan) were developed by the program ARSTAN, and we used the residual chronologies in our additional analyses.
The climate-growth relationship was assessed by means of bootstrap correlation analysis estimated by Dendro-Clim 2002 program (Biondi 1997, Biondi and Waikul 2004). Due to the lack of representative meteorological data for the whole period covered by our chronologies, we used datasets from the Climate Research Unit (CRU) for mean temperature and total precipitation. The chosen climate data were derived from the nearest points of the CRU grid with the sampled sites and were used in the climate-growth relationship. We also used the Standardised Precipitation-Evapotranspiration Index (SPEI) at 1- and 3-months’time scale in the period 1901-2013. The SPEI is a multiscale drought index based on the monthly precipitation and potential evapotranspiration from the CRU datasets (Vicente-Serrano et al. 2010).
Tree-ring chronologies were calibrated against instrumental climate records obtained from the CRUTS3.22 dataset (http://www.cru.uea.ac.uk/), for the period 1901-2013 with a spatial resolution of 0.5×0.5° (Mitchell and Jones 2005), using correlation and response functions analysis. Correlation analysis was performed to quantify the relationship between the residual chronologies from three sites and monthly mean temperature, total precipitation (Fritts 1976) and drought index (SPEI) for 1 and 3 months.
Correlation coefficients were deemed statistically significant at the P<0.05level, as shown by bootstrapped confidence intervals. The considered window for exploring the relations between climate and tree growth were from May of the prior year of growth to October of the current year of growth, assuming that the cambial activity of BP continues during the winter months and studying the role of climate during the previous year on the current radial growth (Fritts 1976, Grissino-Mayer 1995).
Then we applied forward evolutionary interval analysis (FEI) to provide a complementary assessment of temporal stability for significant monthly climate-growth relationships. Our objective was to elucidate temporal variability in the relationships identified between climate and BP radial growth (Biondi 1997, Biondi and Waikul 2004). FEI begins with the earliest year in common to all variables, from which forward evolutionary intervals are progressively enlarged by adding one year to a base interval length at each iteration (Biondi and Waikul 2004). Persistent relationships between climate variables and tree growth over the 20th century would further substantiate the results of correlation analysis and suggest the suitability of BP tree-ring data for use in dendroclimatic reconstructions.
The length of the master chronologies varies among sites. The DE chronology was the longest with 541 years, spanning the period 1474-2014 with a replication of more than 34 trees from 1770 onwards. The KO chronology was the shortest, 176 years long, with a sample replication of 25 trees, while the PRE chronology was 243 years long, spanning the period 1776-2014 with a samples replication of 25 trees from 1901 onwards (Figure 3, Table 2). The maximum value of inter-annual variability, expressed by the mean sensitivity (MS), was found in the KO, while the minimal value was found in the PRE chronology. High values of the first-order autocorrelation found at all chronologies indicated that BP growth strongly depends on the climate conditions of the previous growing year.
Figure 3. Tree-ring width chronologies of BP (P. heldreichii Christ.) from Decan (DE), Prevalle (PRE) and Koritinik (KO). The upper part in each graph shows the raw tree-ring width chronology, while the lower part shows tree replication in respective site chronologies.
All chronologies were significantly correlated with each other for the common period 1840-2014. The degree of agreement and similarity appears to be higher between PRE and KO chronology (R=0.61; p<0.01), but slightly lower among DE and PRE chronologies (R=0.25; p<0.05), implying that the degree of correlation appears to be related to the vicinity between sites (Table 3).
Relationships Between Climate and Tree Growth
The correlation between DE chronology and temperature was not significant at the study site, but significant relationships were found with October precipitation of the previous years of growth and summer months of the current growing year.
In addition, significant negative correlations were found between BP radial growth for KO site and monthly mean temperature for the previous July, August, September and current June. Moreover, BP radial growth in this site was negatively correlated with current May, but a positive correlation was found with previous August precipitation.
Bootstrapped correlation analysis between PRE chronology and climatic variables showed a positive relationship with current January – February temperatures, as well as with May and October precipitation of the previous years and July precipitation of the current growing year. An opposite relationship was found with previous June and current April precipitation (Figure 4).
Figure 4. Bootstrap correlation coefficients between residual chronologies with temperature (left) and precipitation (right) from May of the year prior to growth to October of the current year of growth. Asterisks on the top of the bars indicate statistically significant correlations (p<0.05) and the horizontal dashed lines represent the 95% confidence interval.
The results of this analysis indicate that precipitation during the growing season is not the only limiting factor. Considering the number of significant coefficients of temperatures with a negative relation to growth, our analysis showed that this number was higher than those with a positive relation.
The results of the Pearson correlation between BP chronologies and SPEI in 1 to 3 months’ time scales were different between sites (Figure 5). DE chronology had the highest positive correlation frequency with SPEI than the two other sites. These results indicate that young (PRE) and middle-aged (KO) trees are less sensitive to drought than old trees.
Figure 5. Correlation coefficients (y-axis) showing the relationship between the BP residual chronology and monthly SPEI from the previous May to the current October for period 1951–2013. The horizontal dashed lines indicate the relationships between BP growth and SPEI values for a significance level of p
Thus, BP growth at DE site was positively correlated with SPEI values from June to August of the current year for 1 month time scale and from July to October of the current growing year for 3 months’ time scale. Positive significant correlation between BP growth with July SPEI values was attained for two other sites. PRE chronology was the only one where 1 month time-scale SPEI was negatively correlated with BP growth and current April, implying that the low amount of rainfall during this month may delay the initiation of BP radial growth. Positive correlations found between SPEI and BP growth during July at all three sites show the impact of midsummer drought on trees’ growth.
FEI suggested that these relationships were not all persistent during the period of inquiry. However, FEI indicated a sustained negative relationship between radial growth and current June monthly mean temperatures for PRE and KO sites, as well as a continuous positive relationship between growth and current January-February temperatures. FEI also indicated a persistent positive relationship between BP growth and previous May, July and August monthly precipitation at KO site and current June at DE site. Positive correlations found between SPEI and BP growth during July at all three sites show the impact of drought on trees’ growth.
Figure 6. Results for forward evolutionary interval analysis (1951–2013) between monthly mean temperature and the BP chronology (32-year base interval). Monthly climatic variables are shown on the y-axis, beginning with the previous May and ending with the current October. The last years of the forward intervals are listed on the x-axis. Significant positive (p<0.05) correlations are shown with colors ranging from brown to cherry, while significate negative (p<0.05) correlations are shown with color from green to purple.
DISCUSSION AND CONCLUSION
Radial growth trends shared between BP at the three sites indicate the influence of local climate conditions on species’ growth. Significant correlations between BP chronologies and monthly climate data support our approach that BP growing on the studied sites is suitable for dendroclimatic analyses. A significant positive relationship between indexed BP growth and SPEI emerges during July in the current growing year. It suggests that the lack of precipitation during July is limiting the BP radial growth for the rest of the growing season. Thus, temperature rising and the lack of available water during July or summer months will lead to physiological dehydration and physiological drought in BP trees (Zhang et al. 2018). Drought stress will directly affect the transpiration and respiration of trees, leading to a reduction of the photosynthesis rate and eventually producing narrow tree-rings (Trugman et al. 2018). The severity of drought stress on individual trees closely depends on tree age. The drought in the study areas caused by temperature rising and lack of water availability, especially during July, has a strong limiting effect in trees of different age. In particular, the DE chronology composed by older trees, compared to other sites, showed more significant positive correlations with drought index (SPEI) than younger and middle-aged chronologies from PRE and KO sites. Older aged BP trees from DE site have bigger crown size, directly influencing the water balance through a higher evapotranspiration leading to a greater water consumption. This finding is consistent with the results of other studies indicating that age indirectly affects the trees’ response to environmental factors due to photosynthesis efficiency, hydraulic conductance and nutrient transport (Vieira et al. 2009).
Jiao et al. (2017) reported that tree age could interfere with the expression of environmental signals related to radial growth and that the age effect is not completely eliminated from the developed chronologies. The KO site was the only one where1-month timescale SPEI (current April) was negatively correlated with BP growth, implying that the low amount of rainfall during this month may delay the initiation of BP radial growth. The decrease in available moisture during the beginning of the growing season could decrease the photosynthetic rate and cause trees to allocate fewer carbohydrates for radial growth (Fritts 1976, McDowell et al. 2008).
We found strong relationships between KO tree-ring chronology and temperatures of the year prior to the growth. In tree-line locations, the growing period is relatively short and most active tracheid’s formation occurs at the beginning of the summer (Rossi et al. 2006). The inverse relationship between annual radial growth and monthly mean temperature during the previous late summer and early fall indicates that high monthly mean temperatures would increase evaporation rates and decrease the amount of water stored from summer rains. It is well-known that evaporation increases as monthly mean temperature increases, restricting the amount of water available for photosynthesis (Fritts 1976, McDowell et al. 2008). At PRE site a positive correlation with January and February temperatures was noted, implying that mild winters may have a positive influence on snow melting and soil moisture. From a physiological point of view, winter temperatures cannot directly influence cambial activity since the trees are dormant. However, during warmer winters, more precipitation falls as rainfall, rather than snow (IPCC 2007). In our case, it is more probable that precipitation in cases with warmer winter temperatures is in the form of wet snow, which on its side is less prone to wind transport and immediate sliding along steep slopes and therefore could contribute to a deeper snow cover. This can provide more soil moisture after snowmelt and could be a prerequisite for increased cambial activity given that other conditions are favorable.
Several possible explanations exist for the temporal instability of climate-growth relationships at the three sites. Climate is not the only environmental variable that affects the widths of tree-rings (Fritts 1976). It is possible that other non-climatic factors are responsible for erratic-ring patterns noted in all BP chronologies. Although there is no information about the anthropogenic activity, the presence of young trees especially in KO and PRE sites is a good indicator of silvicultural management treatments and this may partly explain the temporal variability in the relationships between radial growth and local climate. We noticed trunk scars and wounds on some trees at all three sites. These injuries were the result of lightening activity and might affect their growth. Therefore, biotic factors and anthropogenic activity, during the past and present, may partially explain the temporal instability of climate-growth relationships at all sampled sites.
It is projected that Kosovo will have increasingly warmer temperatures and a higher irregularity of precipitation in the future. Taking into account the role of drought during the summer season and temperatures on BP growth, their impact will likely become more important in the global warming scenarios.
ET, FB carried out the field measurements, laboratory measurements and performed the statistical analysis, while SB and BB conducted the sample preparations. Both authors contributed to data collection and manuscript writing.
This research was conducted in the framework of the PhD thesis and no external funding has been used.
The authors would like to thank the reviewers for their valuable comments in manuscript improving.
Conflict of Interest
The authors declare no conflict of interest.
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