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Article

Climate-Growth Relations of Abies georgei along an Altitudinal Gradient in Haba Snow Mountain, Southwestern China

by
Mei Sun
,
Jianing Li
,
Renjie Cao
,
Kun Tian
,
Weiguo Zhang
,
Dingcai Yin
and
Yun Zhang
*
National Plateau Wetlands Research Center, Southwest Forestry University, Kunming 650224, China
*
Author to whom correspondence should be addressed.
Forests 2021, 12(11), 1569; https://doi.org/10.3390/f12111569
Submission received: 26 September 2021 / Revised: 11 November 2021 / Accepted: 11 November 2021 / Published: 15 November 2021
(This article belongs to the Special Issue Long-Term Productivity and Landscape Processes of Mixed Conifer Forests)
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Abstract

:
Climate warming has been detected and tree growth is sensitive to climate change in Northwestern Yunnan Plateau. Abies georgei is the main component of subalpine forest in the area. In this study, A. georgei ring width chronologies were constructed at four sites ranging from 3300 to 4150 m a.s.l. in Haba Snow Mountain, Southeastern edge of Tibetan Plateau. We analyzed the relationship between four constructed chronologies and climatic variables (monthly minimum temperature, monthly mean temperature, monthly maximum temperature, monthly total precipitation, the Standardized Precipitation-Evapotranspiration Index, and monthly relative humidity) by using response function analysis, moving interval analysis, and redundancy analysis. Overall, the growth of A. georgei was positively affected by common climatic factors (winter moisture conditions, autumn temperature, and previous autumn precipitation). At low and middle-low sites, May moisture condition and previous December precipitation controlled its radial growth with positive correlations. At middle-high and high sites, previous November temperature was the key factor affecting tree growth. The result of moving interval analysis was consistent with correlation analyses, particularly for May moisture at low altitudes.

1. Introduction

Effects of climate change on forest ecosystems have been widely concerned [1,2,3], particularly for those forests at high altitudes where trees are more susceptible to climate warming [4,5]. Climate change directly affects tree regeneration, growth, and migrating abilities, and consequently influences forest dynamics [6,7,8]. Tree rings often contain an amount of climate information and have long been used as a valid tool to detect long-term climate-growth relationships [9,10], and to further evaluate future impacts of climate change on forest ecosystems [11,12].
Altitude is an important ecological factor, which often causes the redistribution of hydrothermal conditions affecting the tree radial growth [13]. It is generally believed that the radial growth is mainly affected by temperature in high altitudinal areas, while moisture conditions control tree growth at low altitudes [14,15]. However, due to the difference in the rate of climate change along the altitudinal gradient, this rule is not applicable in all cases [16,17], some research has also showed that the same tree species respond consistently to climate variables at different altitudes [17]. Studying climate-growth relations across species distributional range could help to learn how tree growth responds to climates in an area, and therefore to better understand forest dynamics and formulate proper management strategies under climate change scenarios.
The central Hengduan Mountain (HM) is located in the Southeastern edge of Tibet Plateau, with a complex topography, vertical climate belts, rich forest resources, and small human disturbances, and is considered as a climate sensitive area where a warming trend has been observed during the past decades (0.3 °C/decade) [18]. This provides excellent conditions for studying the altitudinal trend of climate-growth relationships [19,20]. In recent decades, dendrochrological techniques have been widely applied in detecting climate-growth responses of conifer species at different sites in HM. Like Picea likiangensis, Picea brachytyla, Tsuga dumosa, Abies ernestii, and Abies georgei in Baima Snow Mountain [21,22]. P. brachytyla in Meili Snow Mountain and Geza [23,24]. A. georgei, P. likiangensis, Pinus densata, and Larix potaninii in Shika Snow Mountain [12,25]. P. likiangensis and T. dumosa in Yulong Snow Mountain [26,27]. These studies showed that both temperature and precipitation influenced tree radial growth in HM, but growth response to climate varied with tree species and sites. Haba Snow Mountain (HSM) is a typical snow mountain in the central HM with a well-preserved forest ecosystem, however, little is known about impacts of climate change on tree growth in the area [28], particularly in altitudinal trends of climate-growth relationships. Recently, growth responses of A. georgei to climate factors at the upper distributional limit in HSM (data also used in this paper) has been detected [29].
A. georgei is a high-altitude conifer widely distributed in HM and is known as the main tree species compositing subalpine forests. Prior studies have revealed that higher temperatures in the previous November–December and current June–August stimulate the species radial growth at its upper distributional limit in HM [23,29], while current June and September precipitation limit its growth [29]. However, studies on climate-growth relationships of A. georgei along the altitudinal gradient in HM are rather scant [25]. Therefore, the aim of this study is to identify the main climatic factors influencing A. georgei growth at different altitudes in HSM and to evaluate the temporal stability of the climate-growth relationship. Given that high-altitudes with low temperature in HSM and temperature decrease as altitudes increase, we expect that A. georgei growth is temperature-limited and this sensitivity is more obvious at higher altitudes.

2. Materials and Methods

2.1. Study Area

Haba Snow Mountain (HSM) is located in the Northwestern Yunnan and the Southeastern edge of the Tibet Plateau (Figure 1). The highest point of HSM is 5396 m a.s.l., and the lowest point is 1550 m a.s.l. near beside Jinsha River. From the Jinsha River valley to the peak of HSM, different vertical climate zones are formed successively, such as the sub-tropical zone (1550–1800 m a.s.l.), northern subtropical zone (1800–2100 m a.s.l.), warm temperate zone (2100–2500 m a.s.l.), moderate temperate zone (2500–3100 m a.s.l.), cold temperate zone (3100–4100 m a.s.l.), cold zone (4100–4700 m a.s.l.), and permanent ice and snow zones (above 4700 m a.s.l.) [30,31]. The type of forest vegetation corresponding to the vertical climate zone has been formed. Below 2100 m a.s.l., the dry and warm river valleys is dominated by shrub species such as Ziziphus mintana, Terinalia franchetii, and Caryopteris forrestii. Between 2100 and 2850 m a.s.l., a warm and temperate coniferous forest is dominated by Pinus yunnanensis and Pinus amandii. From 2900 to 3200 m a.s.l., P. densata is the dominant species and formed a coniferous forest. At altitudes of 3300–4100 m a.s.l., it is a cold-temperate coniferous forest with P. likiangensis, Larix potaninii, and A. georgei as the major species. Altitudes above 4200 m a.s.l. are alpine meadows and alpine screes sparse vegetation [31].
A. georgei is a shade-tolerant and shallow-rooted species, adapted to humid climate, and grown in the gray-brown forest soil, which is generally founded at altitudes of 3200–4100 m a.s.l. According to the results of the “Comprehensive Scientific Investigation of the Haba Snow Mountain Nature Reserve in Yunnan”, the total forest area is 11,391.8 hm2, while the A. georgei forest area is 4121.7 hm2, accounting for 36.18% of the total forest area.
The HSM is affected by a South-Asian monsoon climate, which is characterized by distinct wet and dry seasons [31]. According to the climate data of 1951–2016 from the Lijiang meteorological station (Figure 2), the annual average temperature is 12.9 °C, the coldest in January with an average temperature of 6.2 °C, and the hottest in June with an average temperature of 18.2 °C. The average annual precipitation is 959.37 mm. The precipitation is mainly concentrated in the rainy season (June–October). The precipitation is 842.40 mm, accounting for 87.81% of the annual precipitation.

2.2. Tree-Ring Sampling and Chronnology Development

In 2017, we collected tree-ring samples at four altitudes (3317 m, 3682 m, 3967 m, and 4152 m), spanning the altitudinal distributional range of A. georgei. When sampling, large, healthy, and undisturbed trees were selected. After sampling, we used a branch to block the hole caused by drilling to prevent insects entering, which may be helpful for wound securing and avoiding diseases. For each tree, two cores parallel to the contour line at breast height were taken. We placed the obtained cores into a plastic straw and numbered them. The altitude deviation was controlled within 10 m at each altitude to keep the consistency of climatic signal. In total, 128 trees and 230 cores were collected at four altitudes (Table 1).
The samples were brought back to the laboratory and were treated in accordance with the standard process of dendrochronological techniques [32]. After the samples were naturally air-dried, they were fixed and polished. Each core was placed under a binocular microscope for preliminary dating, and then scanned at high resolution (2400 dots per inch) on an EPSON Scan (Expression 11000XL, Seiko Epson Corporation, Nagano, Suwa, Japan) scanner. Ring widths on each scanned image were measured at an accuracy of 0.001 mm by using the software CooRecorder version 9.3 and cores from the same tree were cross-dated by using the software CDendro version 9.3 [33]. Dating results of ring width series were checked by using the program COFECHA [34]. The cores that had low correlations with the main sequence were eliminated. Finally, 124 trees and 216 cores remained and were selected for next analysis.
To maximally retain the climatic signals, ring width measurements were developed by using the ARSTAN program [34]. Ring-width series were standardized to remove the biological growth trend, as well as any other low-frequency variations induced by stand dynamics. The detrending procedure assumed a 50% frequency response over a 100-year frequency band. This detrending method allows maximizing the common signals among individual tree-ring series. To reduce the influence of outliers in the computation of the mean chronologies, all detrended series were averaged on a site-by-site basis by using the bi-weight robust mean. Residual chronologies were produced to remove any auto-correlation effects and were used for further analyses. The quality of chronologies was evaluated by several statistics, such as mean sensitivity, signal-to-noise ratio, and expressed population signal.

2.3. Climate Data

We collected monthly minimum temperature, monthly mean temperature, monthly maximum temperature, monthly precipitation, and relative humidity in the period between 1951 and 2016 from the Lijiang meteorological station (27°50′ N, 99°42′ E, 3276.7 m). To further detect the effect of moisture condition on tree growth, the Standardized Precipitation-Evapotranspiration Index (SPEI) [35] was also applied and datasets (1951–2016) were obtained from a CRU grid (CRUTS4.03, https://spei.csic.es/database.html (accessed on 11 November 2021).

2.4. Climate-Growth Relationships

Since climate has a lagging effect on tree growth [36], climate variables from previous September to current October were selected for the correlation analysis by using program DendroClim2002 [37]. To detect accumulation effects of climate on tree growth, we also selected seasonal data, i.e., the post-growing season (September–October) of the previous year, the dormant season (January–March), the early growing season (April–May), the growing season (June–August), and the post-growing season of the current year. The response function first extracts the principal component of the climate variables and then performs regression analysis, which can more accurately reflect the extent to sample data affected by environmental factors. Therefore, we use correlation coefficients of the response function to reflect the relationship between tree growth and climate factors.
We also assessed the temporal stability of climate-growth relationships by using evolutionary and moving response functions module in DendroClim2002. Evolutionary intervals were calculated using forward and backward selection with a window period of 22 years.
To further explore climate-growth relationships, we applied redundancy analysis (RDA) by using the program CANOCO4.5 [38]. In RDA correlation matrix, residual chronologies were the response variables, years were the samples, and climate variables were the explanatory variables. Significant (p < 0.05) climate variables were selected after applying forward selection using a Monte Carlo permutation test based on 999 random permutations [38].

3. Results

3.1. Tree-Ring Chronologies

The length of A. georgei residual chronology of the four sampling sites (Figure 3) increased from low to high altitudes (Table 2). Each statistical characteristic value did not show a clear trend along the altitudinal gradient, but all had higher mean sensitivity (MS) and higher expressed population signal (EPS) with a value above 0.90, indicating that the chronologies had a high quality and could represent the characteristics of tree-ring width in the area, and that they could be used in this dendrochronological study. Tree-ring chronologies from adjacent sites showed significant and positive correlations over the common period 1951–2016 (Table 3), indicating the similarity in the growth sensitivity to climate signals at four altitudes.

3.2. Relationship between Ring width Index and Climate Variables

The results of response function (Figure 4) showed that the radial growth of A. georgei at low altitudes (L and ML) was more affected by moisture condition than temperature. May moisture availability was consistent at both L and ML, by showing negative correlations with Tmean and Tmax (Figure 4a) and positive correlations with humidity (Figure 4b). At L, previous October and December precipitation and SPEI, and current June relative humidity and SPEI positively influenced tree growth. While precipitation in previous October and current January positively affected tree growth at ML. At high altitudes (MH and H), the radial growth of A. georgei was significantly and positively correlated with the previous November temperature.
For the result of seasonal analysis, moisture condition before current growing season was important in tree growth at the L site, by showing significant correlations of precipitation, SPEI, and relative humidity with PPG, DG, and EG (Figure 4b), temperature negatively and positively affected tree growth in EG and PG, respectively (Figure 4a). At the ML site, temperature negatively influenced tree growth in EG, while relative humidity and precipitation positively affected tree growth in DG. No significant correlations were found at two high altitude sites.

3.3. Dynamic Relationships between Radial Growth and Climatic Change

The climate-growth relationship (Table 4) was stable at the L site, particularly for May (temperature, precipitation, SPEI and relative humidity) by showing significant correlations at all years. For previous October and December precipitation, significant correlations were found at most years. The relationship of SPEI was more stable in previous December than in previous October and current March, by showing more significant years. The October temperature showed a quite stable relationship with tree growth by showing significant correlations in some years. At ML, significant correlations were found at all years for May temperature and most years for May relative humidity, January and previous October precipitation, indicating a stable relationship. The stability was good at MH by showing significant correlations at most studied years, while it was poor at H by showing several years with significant correlations.

3.4. Redundancy Analysis between Climatic Factors and Residual Chronologies

According to RDA results (Figure 5), the moisture condition played a more important role in tree growth at low altitudes (L and ML), indicated by a smaller angle between their chronology vectors and moisture vectors (March and May relative humidity, and previous December precipitation) than two temperature vectors. Vice versa, tree growth was more affected by temperature at high altitudes (MH and H) by showing closer relationships with temperature in previous November and current September.

3.5. Altitudinal Trends of Growth Responses

The strength in responses of the May moisture condition decreased with increasing altitudes (Figure 6a). The effect of previous November temperature turned from negative to positive towards higher altitudes, while the impacts of an early growing season (negative) became weak as the altitude increased (Figure 6b). Previous December precipitation turned from positive to negative with increasing altitudes, while there was no significant trend in DG SPEI (Figure 6c). The coefficients of PPG precipitation decreased with increasing altitudes, but the trend was not significant (Figure 6d).

4. Discussion

Our results revealed that the radial growth of A. georgei was more affected by the moisture condition at a lower distributional range while by temperature at higher altitudinal sites in HSM, which supported one of our hypotheses that the strength of temperature impacts enhanced as altitude increased, but rejected another hypothesis that low temperature was the main factor controlling tree growth across the altitudinal distributional range. Consistent to our findings, the importance of moisture (temperature) decreased (increased) with increases in altitudes has been reported in nearby central Himalaya [39,40].

4.1. Climate-Growth Relationships along the Altitudinal Gradient

May moisture condition is a dominant factor influencing the radial growth of A. georgei at low altitudes. Since May is relatively dry in the studied area with high temperature and low precipitation (Figure 2), A. georgei start growing and growth may suffer from drought stress due to insufficient water supply caused by increased plant transpiration and soil water evaporation [41], consequently limiting tree early growth. In addition, the soil in HSM is poor in water retention and holding capacity, which easily leads to drought stress when water is insufficient [30]. However, the temperature is lower with less evapotranspiration at high altitudes, therefore drought stress was not detected at high altitudinal sites. Similar results have also been reported in Southeastern Tibetan Plateau [42,43], Central Tibetan Plateau [44,45,46], and Western Himalayas [47].
More precipitation in previous December could enhance A. georgei growth at lower sites, since more precipitation in winter can provide higher water reserve availability for tree growth at the beginning of the growing season in the next year, particularly for those lower sites under May drought stress (as discussed in above paragraph). The positive effects of previous December precipitation on tree growth at the lower limit was also reported for P. densata at HSM [48]. However, it became weak (coefficients) and turned into negative correlation at higher sites, reflecting that precipitation was not limiting at the species upper distributional limit.
Previous November temperature was found to be important in determining tree growth at high altitudes. November is the season for dormant bud formation, if the temperature is too low, the number of dormant bud formation will be reduced [49,50]. Furthermore, low temperature would cause needle leaves die due to the leaf tissue frozen, thereby reducing photosynthesis production and restricting tree growth in the next year. The relationship turned into slightly negative (not significant) at the lowest site, the temperature was higher at the lower site, and the precipitation gradually became more important. Positive effects on subalpine tree growth were also reported at Central Austrian Alps and Slovakia [36,51].

4.2. Consistent Effects among All Sites

Cambial activity is generally slow in the post growing season with low temperature [52,53], although September and October are in the post growing season and cambial activity is weak, high temperature can still promote the photosynthesis to produce nutrients for tree growth and extend the growing season, consequently forming wide ring width in the current year [45]. Similar results have been proved in conifer trees of neighboring areas [46,54].
The moisture condition during winter (January to March) positively affected tree growth. On the one hand, A. georgei is a shallow-rooted tree species, and the dormant season precipitation is mainly snowfall. Snowfall can form a thermal insulation layer on the ground, which can prevent the root system from being damaged by the low temperature during the winter, which is conducive to tree growth in the cold weather. The same conclusion has been reported for conifer trees at Tianshan Mountain in Northern China and high elevation sites in Northern Patagonia of Argentina [55,56]. On the other hand, snowfall during the dormant period is conducive to maintaining good soil moisture and increasing the water reserve in the early growing season [57]. The effects of winter snowfall on tree growth have the same results in previous studies, such as the subalpine in Northwestern Yunnan [26], the Northeastern subalpine in China [58], the subalpine in Central Japan [59], and Quebec [60].
Our results have revealed that precipitation during the previous post growing season (mainly October) is also a critical factor that positively affected tree growth across the altitudes, particularly at two low sites. Adequate precipitation in the post growing season of the last year would keep the soil in a good moisture condition and may increase the accumulation of carbohydrates, which is beneficial to tree growth of the coming year [61].
In addition, high temperatures in the early growing season had negative impacts on tree growth, suggesting that moisture conditions in spring was important for tree growth. Significant correlations only presented at two low sites (Figure 4a) and correlation coefficients decreased with increasing altitude (Figure 6b), the finding supported the result of May moisture condition impacts, indicating that drought stress was more obvious at low sites than at high sites.

4.3. Temporal Stability in Climate-Growth Relationships

The stability by moving interval analysis supported the results of correlation analyses by response function and RDA. Those climatic factors with significant correlations of tree growth were presented at many time scales, particularly for May climatic conditions (temperature, precipitation, SPEI and relative humidity) at the L site, indicating the key effect of the May moisture condition on the species growth at low altitude. At the ML site, the negative effects of May temperature on tree growth was similar to site L, suggesting drought stress on tree growth at low altitudes. The stability of previous November temperature at MH and H site was relatively weak by showing less significant years as compared to other climatic factors, but it still proved the importance of temperature on the species radial growth at high altitude. There were no obvious increases in the years showing significant correlations since 1980s or 1990s, and it is likely that the warming may not reach the threshold to affect tree growth.

5. Conclusions

The radial growth of A. georgei responded differently to climates along the altitudinal gradient in HSM, generally showing moisture sensitivity at lower altitudes (L and ML sites) and temperature control at higher altitudes. Current May moisture condition and previous December precipitation played an important role in affecting tree growth at low altitudes, while the previous November temperature was the key factor at high altitudes. More precipitation in winter and early spring and higher temperature in the late growing season would stimulate tree growth in the area. The stability analysis supported the results of two correlation analyses, and it can provide more accuracy information for the understanding of the climate-growth relationship dynamics.

Author Contributions

M.S. finished the manuscript, J.L. and R.C. analyzed the data, K.T. put forward the idea of the article, D.Y. and W.Z. helped field sampling, Y.Z. modified the article. All authors have read and agreed to the published version of the manuscript.

Funding

This work was funded by the National Natural Science Foundation of China (31600395) and the Plateau Wetlands Science Innovation Team of Yunnan Province (2012HC007).

Data Availability Statement

The data presented in this study are available on request from the corresponding author.

Acknowledgments

We thank Lei Wang with help in improving the quality of the figures. We thank Raphael Chavardes and Igor Drobyshev for their continuous support throughout this project.

Conflicts of Interest

The authors declare no conflict of interest.

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Forests 12 01569 g001 550
Figure 1. Location of the study area, the sampling site, and the meteorological station.
Figure 1. Location of the study area, the sampling site, and the meteorological station.
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Figure 2. Climate date from the Lijiang meteorological station (1951–2016). Monthly minimum temperature (Tmin), monthly mean temperature (Tmean), monthly maximum temperature (Tmax), and total precipitation (Prec) (a). Relative humidity (b). Trends of annually mean temperature (c). Trends of annually total precipitation (d).
Figure 2. Climate date from the Lijiang meteorological station (1951–2016). Monthly minimum temperature (Tmin), monthly mean temperature (Tmean), monthly maximum temperature (Tmax), and total precipitation (Prec) (a). Relative humidity (b). Trends of annually mean temperature (c). Trends of annually total precipitation (d).
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Figure 3. Residual chronologies and sample depth at four altitudes. The residual chronology of low altitude (L). The residual chronology of Middle–Low altitude (ML). The residual chronology of Middle–High altitude (MH). The residual chronology of High altitude (H).
Figure 3. Residual chronologies and sample depth at four altitudes. The residual chronology of low altitude (L). The residual chronology of Middle–Low altitude (ML). The residual chronology of Middle–High altitude (MH). The residual chronology of High altitude (H).
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Forests 12 01569 g004a 550Forests 12 01569 g004b 550
Figure 4. Relationships between residual chronologies and climatic factors. * p < 0.05. Correlation coefficients of Tmin, Tmean and Tmax computed by response function (a). Correlation coefficients of Prec, SPEI and relative humidity computed by response function (b). PPG indicates the previous post growing season (September–October); DG indicates the dormant season (January–March); EG indicates the early growing season (April–May); G indicates the growing season (June–August); PG indicates the post growing season (September–October); p indicates the previous year.
Figure 4. Relationships between residual chronologies and climatic factors. * p < 0.05. Correlation coefficients of Tmin, Tmean and Tmax computed by response function (a). Correlation coefficients of Prec, SPEI and relative humidity computed by response function (b). PPG indicates the previous post growing season (September–October); DG indicates the dormant season (January–March); EG indicates the early growing season (April–May); G indicates the growing season (June–August); PG indicates the post growing season (September–October); p indicates the previous year.
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Figure 5. Redundancy analysis between climatic factors and residual chronologies (1951–2016). Only significant climatic factors (p < 0.05) are shown. The longer vector of climate factor indicates the greater contribution; correlation coefficients between the climatic factors and the chronologies are illustrated by the cosine of the angle between the two vectors. Vectors pointing in the same directions indicate a positive correlation, and in opposite directions indicate a negative correlation. Numbers represent the corresponding months, T represents temperature; P represents precipitation; RH represents relative humidity. The letter P before number represents previous year. L indicates the residual chronology of low altitude; ML indicates the residual chronology of Middle–Low altitude; MH indicates the residual chronology of Middle–High altitude; H indicates the residual chronology of high altitude.
Figure 5. Redundancy analysis between climatic factors and residual chronologies (1951–2016). Only significant climatic factors (p < 0.05) are shown. The longer vector of climate factor indicates the greater contribution; correlation coefficients between the climatic factors and the chronologies are illustrated by the cosine of the angle between the two vectors. Vectors pointing in the same directions indicate a positive correlation, and in opposite directions indicate a negative correlation. Numbers represent the corresponding months, T represents temperature; P represents precipitation; RH represents relative humidity. The letter P before number represents previous year. L indicates the residual chronology of low altitude; ML indicates the residual chronology of Middle–Low altitude; MH indicates the residual chronology of Middle–High altitude; H indicates the residual chronology of high altitude.
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Figure 6. Altitudinal trends in correlation coefficients of A. georgei with significant climate factors between 1951 and 2016. May moisture condition (temperature, precipitation, and relative humidity) (a). Temperature (previous November, current early growing season, and post growing season) (b). Precipitation in previous December and SPEI in dormant growing season (c). Dormant growing season and previous post growing season (d).
Figure 6. Altitudinal trends in correlation coefficients of A. georgei with significant climate factors between 1951 and 2016. May moisture condition (temperature, precipitation, and relative humidity) (a). Temperature (previous November, current early growing season, and post growing season) (b). Precipitation in previous December and SPEI in dormant growing season (c). Dormant growing season and previous post growing season (d).
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Table
Table 1. The information of sampling sites.
Table 1. The information of sampling sites.
SitesAltitude/m a.s.l.Longitude/ELatitude/NNo. (Tree/Core)
Low altitude (L)3317100°04′54.78″27°20′19.86″26/52
Middle–Low altitude (ML)3682100°04′19.62″27°20′25.37″33/60
Middle–High altitude (MH)3967100°05′31.25″27°20′39.71″35/62
High altitude (H)4152100°05′51.48″27°20′48.90″34/56
Table
Table 2. Statistics of residual chronologies and common interval analysis.
Table 2. Statistics of residual chronologies and common interval analysis.
Residual ChronologiesLMLMHH
No. (tree/radii)26/5130/5234/5734/56
chronology length1933–20161923–20161831–20161737–2016
Mean sensitivity0.210.140.150.11
Statistics of common interval analysis (1950–2016)
Variance in first eigenvector/%49.33%32.18%34.79%36.20%
Standard deviation0.180.130.120.10
Signal-to-noise ratio6.776.2522.2026.81
Expressed population signal0.870.860.960.96
Table
Table 3. Pearson correlation coefficients among four chronologies of A. georgei for the common period 1951–2016. Significance level: **, p < 0.01.
Table 3. Pearson correlation coefficients among four chronologies of A. georgei for the common period 1951–2016. Significance level: **, p < 0.01.
LMLMHH
L1.000
ML0.367 **1.000
MH0.0760.348 **1.000
H0.0270.363 **0.494 **1.000
Table
Table 4. Analyses with moving intervals between the residual chronologies and the monthly climatic variables.
Table 4. Analyses with moving intervals between the residual chronologies and the monthly climatic variables.
Sampling SiteInterval PeriodClimatic VariableSignificant Year
L1953–2016Previous October precipitation1953–1970 (+), 1974–1990 (+), 2012 (+), 2014–2016 (+)
Previous December precipitation1953–1985 (+), 1992–1993 (+), 1995 (+), 1999–2016 (+)
Current May precipitation1953–2016 (+)
Previous October SPEI1953–1963 (+), 1968–1969 (+), 1980 (+), 1993–2009 (+), 2014–2016 (+)
Previous December SPEI1953–1990 (+), 2002 (+), 2007 (+), 2009 (+), 2011 (+), 2013–2016 (+)
Current March SPEI1953–1965 (+), 1967 (+), 1969 (+), 1986–1987 (+), 1999 (+), 2002–2016 (+)
Current May SPEI1953–2016 (+)
Current May relative humidity1953–2016 (+)
Current May temperature1953–2016 (−)
Current October temperature1953–1967 (+), 1972–1976 (+), 1998 (+), 2000–2001 (+), 2003–2013 (+), 2015–2016 (+)
ML1953–2016Previous October precipitation1953–1963 (+), 1966–1967 (+), 1980–1986 (+) 1990–1994 (+), 2006–2007 (+), 2009–2016 (+)
Current January precipitation1953–1969 (+), 1973–1975 (+), 1989–1990 (+), 2003 (+), 2006–2016 (+)
Current May relative humidity1953–1970 (+), 1972–1975 (+), 1978 (+), 1980–1985 (+), 2004 (+), 2007–2016 (+)
Current May temperature1953–2016 (−)
MH1953–2016Previous November temperature1953–1967 (+), 1974 (+), 1980–1981 (+), 1983–1996 (+), 2000 (+), 2003 (+), 2011–2016 (+)
H1953–2016Previous November temperature1953–1965 (+), 2014–2016 (+)
Note: (+) indicates a significant and positive correlation; (−) indicates a significant and negative correlation.
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Sun, M.; Li, J.; Cao, R.; Tian, K.; Zhang, W.; Yin, D.; Zhang, Y. Climate-Growth Relations of Abies georgei along an Altitudinal Gradient in Haba Snow Mountain, Southwestern China. Forests 2021, 12, 1569. https://doi.org/10.3390/f12111569

AMA Style

Sun M, Li J, Cao R, Tian K, Zhang W, Yin D, Zhang Y. Climate-Growth Relations of Abies georgei along an Altitudinal Gradient in Haba Snow Mountain, Southwestern China. Forests. 2021; 12(11):1569. https://doi.org/10.3390/f12111569

Chicago/Turabian Style

Sun, Mei, Jianing Li, Renjie Cao, Kun Tian, Weiguo Zhang, Dingcai Yin, and Yun Zhang. 2021. "Climate-Growth Relations of Abies georgei along an Altitudinal Gradient in Haba Snow Mountain, Southwestern China" Forests 12, no. 11: 1569. https://doi.org/10.3390/f12111569

APA Style

Sun, M., Li, J., Cao, R., Tian, K., Zhang, W., Yin, D., & Zhang, Y. (2021). Climate-Growth Relations of Abies georgei along an Altitudinal Gradient in Haba Snow Mountain, Southwestern China. Forests, 12(11), 1569. https://doi.org/10.3390/f12111569

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