A dendrochronological analysis of maximum summer half-year temperature variations over the past 700 years on the northeastern Tibetan Plateau

Absence of late-summer warming trend over the past two and half centuries on the eastern Tibetan Plateau

“…Particularly in the growing season, these forests could reduce surface heating by discharging excess heat through evapotranspiration of water, which further leads to atmospheric cooling by increasing cloud cover (Betts, 2000). The absence of warming trend in summer or increasing trend in tree-ring growth was also reported in other studies from Changdu region (Bräuning and Mantwill, 2004;Linderholm and Brauning, 2006) and eastern Tibetan Plateau (Collins et al, 2002;Gou et al, 2008;Liang et al, 2009;Fan et al, 2010). Absence of warming trend in summer does not mean the same in other seasons.…”

“…However, warm-season minimum temperature played strong roles on the process of MXD formation in high latitude regions (Mervi, 2005;Frank et al, 2007;Kirdyanov et al, 2008). As indicated by observed meteorological data, the minimum temperature was rising much more rapidly than maximum temperature during the recent warming on the Tibetan Plateau (Gou et al, 2008;Fan et al, 2009), Asia (Tabari and Talaee, 2011), North America (Zhang et al, 2000;Wilson and Luckman, 2003) and the globe (Easterling et al, 1997;Stone and Weaver, 2002). Tree-ring density studies in northern high latitudes showed long-term warming trend in summer temperature since Industrial Revolution (Luckman and Wilson, 2005;Büntgen et al, 2006;Grudd, 2008;Briffa et al, 2013).…”

Temperature changes on the Tibetan Plateau during the past 600 years inferred from ice cores and tree rings

“…The Tibetan Plateau (TP), one of the Earth's most imposing geomorphic features, is a climatically very important region due to its influence on large-scale atmospheric circulation patterns over Asia, including the summer monsoon over South Asia and the South China Sea (Ding, 1992;Li and Yanai, 1996;Webster et al, 1998). During the past decades, a great number of paleoclimatic records covering the last centuries were derived from ice cores Liu et al, 1998;Thompson et al, 1993Thompson et al, , 2000Thompson et al, , 2003Thompson et al, , 2006aWang et al, 2006;Yao et al, 1997;, tree rings (Bräuning, 1999;Bräuning and Mantwill, 2004;Cook et al, 2003;Zhang et al, 2003a,b;Shao et al, 2005;Fan et al, 2008Fan et al, , 2009Gou et al, 2006Gou et al, , 2008Sheppard et al, 2004;Liu et al, 2006a,b;Esper et al, 2002Esper et al, , 2003aTreydte et al, 2006), lake sediments (Herzschuh et al, 2006;Wu et al, 2001;Zhang et al, 2003a,b;Zhang et al, 2004;Liu et al, 2006a,b;Zhao et al, 2007Zhao et al, , 2008Zhao and Herzschuh, 2009) and glacier fluctuations (Bräuning, 2006;Yang et al, 2007) on the TP and adjacent areas (Yang et al, 2003;Ge et al, 2007;Wang et al, 2007). However, it is difficult to compare the results obtained from different proxy data due to lack of calibration ...…”

An attempt to dendroclimatic reconstruction of winter temperature based on multispecies tree-ring widths and extreme years chronologies (example of Upper Silesia, Southern Poland)

“…The concept that a clear climate signal can be found in the tree species growing under limiting conditions have been used in many reference dendroclimatological studies in recent decades, concerning the reconstruction of thermal (e.g., Jacoby and D'Arrigo 1989; Vaganov et al 1996;Rolland et al 2000;Cook et al 2003;Esper et al 2003;Barber et al 2004;Büntgen et al 2005;Gou et al 2008) and moisture conditions (e.g., Douglas 1914;Schulman 1956;Stockton and Meko 1975;Lara et al 2001;Cook et al 2004;Esper et al 2007). However, research on past climate changes based on the use of proxies are of great importance in other regions, too.…”