## 4 Discussion  
### Carbon Dioxide Fluxes and Phytomass  
According to the literature data, the ecosystem respiration (R\({}_{\rm eco}\)) in the swamp ecosystems of the boreal zone with similar ecological conditions varies from 38 in the _Sphagnum_ bog [47] up to 132 \(\pm\) 49 in shrub communities of ombrotrophic bogs [49; 50] and 194 \(\pm\) 96 mgC m\({}^{-2}\) h\({}^{-1}\) in the rrams [38; 51]. The measurements made on the bog massif studied by us earlier in the ridge-hollow complex showed R\({}_{\rm eco}\) varying from 56 to 132 in ridges and from 28 to 75 mgC m\({}^{-2}\) h\({}^{-1}\) in hollows [6]. The minimum R\({}_{\rm eco}\) values obtained because of the current study were observed in the S.hollow (hollow with the dominance of _Scheuchzeria palustris_ L.) in early June and amounted to 11 (median; 9-1Q, 17-3Q), and the maximum values were observed in the Tall ryam at the end of July and reached 581 (572, 587) mgC m\({}^{-2}\) h\({}^{-1}\). At the same time, the median R\({}_{\rm eco}\) in these areas from the end of May to the end of July was 55 and 182 mgC m\({}^{-2}\) h\({}^{-1}\), respectively (Table 2). In general, our results are consistent with the available estimates: the R\({}_{\rm eco}\) values obtained by us in Tall ryam may seem somewhat overestimated. These measurements were carried out in areas where the stocks of aboveground phytomass of vascular plants (148 \(\pm\) 67 g/m\({}^{2}\)) and litter (145 \(\pm\) 31) did not practically differ from the literature data (128 \(\pm\) 42 and 189 \(\pm\) 114 g/m\({}^{2}\), respectively [52; 53; 54]). It is likely that such R\({}_{\rm eco}\) values at the Tall ryam, Ridge and S.hollow sites may be due to the coincidence of two other factors favoring an increase in the intensity of respiration processes: (1) a significant decrease in WTL by the end of 2 July (2) the maximum temperature of the surface of the peat layer, which was observed at the Tall ryam during the same period (Figure 2). Given the relatively small temporal variability of phytomass stocks from late May to late June, we suggest that WTL and soil temperature were the most important drivers of R\({}_{\text{eco}}\) flux variability not only in space (both between and within different sites) but also in time, as it was found out in [46; 47; 48]. The intensity of carbon dioxide assimilation, GEE (from \(-86\) in Ryam to \(-200\)--\(220\) mgC m\({}^{-2}\) h\({}^{-1}\) in Ridge and Open bog), seems to be somewhat higher in comparison to the literature data. For example, on similar ridges in an oligotrophic bog in European Russia, GEE varied between \(-185\)--\(84\) mgC m\({}^{-2}\) h\({}^{-1}\), in hollows and pools here \(-150\)--\(46\) mgCm\({}^{-2}\)h\({}^{-1}\)[50; 55; 56]; and on the current object of study according to earlier measurements, [6] \(-157\)--\(50\) mgC m\({}^{-2}\) h\({}^{-1}\). In an oligotrophic bog in the middle taiga [9], the rate of carbon assimilation did not exceed \(-50\) mgC m\({}^{-2}\) h\({}^{-1}\), in an ombrorophic bog in Finland around \(-80\)--\(106\) mgC m\({}^{-2}\) h\({}^{-1}\)[57]. Thus, our results are closer to the upper limit (the highest absorption of carbon dioxide) of the GEE estimates according to the literature data. We assume that the reason for this is the method of organizing the measurements that we used: all of the measurements were taken during the period when the sun was high above the horizon (from 10 am to 4 pm local time), and mostly in cloudless weather. Accounting for diurnal GEE variability and taking measurements under more varied lighting conditions would not only provide a more adequate average GEE estimate but also better parameterize the GEE-PAR relationship in Models 1-5.