## 3 Results
### Net Radiation, Energy Balance, Bowen Ratio and Water Balance  
Site-specific energy balance components are shown in Figure 4. Net radiation (R\({}_{n}\)) was greater in the pine forest than in the larch forest due to a 2.5 weeks longer growing season and \(\sim\)20% higher values of summer months, which resulted in totals R\({}_{n}\) = 1415 MJ m\({}^{-2}\) vs. R\({}_{n}\) = 1200 MJ m\({}^{-2}\) in the growing season respectively. Net radiation at our forest sites was compared to that at two actinometric stations, Eniseisk (near the pine forest) and Tura (near the larch forest), and showed their reasonable correspondence. The surface albedo difference of 5%-10% between the forest (at our sites) and grass (at weather stations) explained the difference in R\({}_{n}\) measured at our sites and the weather stations: the darker forest surface absorbed more short-wave radiation than the lighter grass surface [49]. Maximal values of R\({}_{\rm n}\) were \(\sim\)120 W m\({}^{-2}\) above the larch forest and \(\sim\)150 W m\({}^{-2}\) above the pine forest in June-July. Figure 3: Temperature of the air (**upper**) and soils at 5 cm (**middle**) and soil temperature isopleths at various depths (**lower**) for one season in the Gmelin larch (**left**) and Scots pine (**right**) ecosystems for the growing season. Figure 4: Energy balance components and Bowen ratio (positive 7-day running averages) in the Gmelin larch (**left**) and Scots pine (**right**) ecosystems for the growing season (May–September, V–IX): R\({}_{\rm n}\)–Net radiation (filled dots are data from actinometric stations Tura (near the Gmelin larch forest) and Eniseisk (near the Scots pine forest); H–sensible heat, and \(\lambda\)E—Latent heat; Bowen ratio. Partitioning of the radiation balance into sensible heat flux (H) and latent heat flux (LE) expressed through both absolute values and Bowen ratio (\(\beta\) = H/LE) in both forests are shown in Figure 4.  
Soil heat flux (G) in the non-permafrost pine forest was \(\sim\)3%-5% of R\({}_{\rm n}\)[33]. G was not measured in our larch forest, but it was expected to be much greater because of permafrost thawing. [PERSON] (1984) [50] estimated soil heat flux could reach 30% of R\({}_{\rm n}\) during the thawing process in spring and 50% in fall. Sensible heat flux was the larger term in the radiation balance and followed the R\({}_{\rm n}\) pattern in both forests. In the Gmelin larch forest, H was maximal 40-80 W m\({}^{-2}\) at the beginning of the growing season, in late May-early June, before leaves came out and after decreased continuously. In the pine forest, with its evergreen habit, H stayed high till August and was 60-100 W m\({}^{-2}\). Latent heat flux was governed by both available energy and rain. Maximal LE reached 40-60 W m\({}^{-2}\) also in the mid-summer in both ecosystems. All LE extremes (maxima and minima) were related to flash rain events, such as in July of 2007 and in August of 2008 in the larch forest or little rain in the pine forest in July of 1998 (Figures 3 and 4). Bowen ratio. In both our pine and larch forests, \(\beta\) stayed between 1 and 2 during the growing season and only in early spring was high and reached 10 (Figure 4). Compared to our pine forest, in a closely located but moister spruce-fire forest and a mixed birch-confer forest \(\beta\) was -1 and in a birch forest \(\beta<1\) during the growing season ([PERSON] et al. 2002) [51]. [PERSON] et al. (2004) [10] also indicated that in their Cajander larch forest in central Yakutia, \(\beta\) remained 1-2 when the forest was physiologically active and raised to 10 when it was not. [PERSON] et al. [52] showed that in a sparse Cajander larch forest also in Yakutia \(\beta\) varied between 10-20 in early spring before leaves came out and then dropped to 1 during the full foliage in the mid-summer and raised again in the fall. [PERSON] (1984) [50], though, gave lower \(\beta<1\) in both pine and larch forests in central Yakutia and \(\beta>1\) only in early spring. Water balance.