Peatlands play an important role in the global carbon cycle, despite the fact that they cover less than 3% of the global land area. With an estimated 270–547 Pg carbon (C) stored as peat (Clymo et al. 1998; Turunen et al. 2002; Yu et al. 2010) – i.e. 50–500 kg C m−2 – peatland ecosystems comprise over one-third of the global soil carbon pool (Gorham 1991; Lappalainen 1996; Rydin and Jeglum 2013). Peatlands are largely located in the northern hemisphere, almost 80% can be found in the boreal and subarctic zones (Smith et al. 2007; Yu et al. 2010), 10% in the tropics and Southeast Asia, and 10% in the temperate zone (Lappalainen 1996; Frolking et al. 2011).

Peatlands have for long been considered as economically useful sources of carbon (Kirkinen et al. 2007, 2010), but recently the attention shifted towards their conservation due to their role in the global carbon cycle, affecting global climate (Frolking et al. 2011). Their functioning as carbon sink, however, relies both on temperature and hydrology (Fekete et al. 2010), which in turn affects the groundwater table, and indeed these are the main drivers controlling C fluxes in peatland ecosystems (Gunnarsson 2005; Limpens et al. 2008; Lund et al. 2010; Waddington et al. 2015). However, various disturbances affect the C sink potential, most often implying changes in soil microbial activities (Strack and Waddington 2007; Dorrepaal et al. 2009; Dieleman et al. 2015; Robroek et al. 2015; Pullens et al. 2016) or plant community composition (Dorrepaal et al. 2003; Buttler et al. 2015).

Increase global warming is an important driver of change in the carbon balance of these ecosystems (Alm et al. 1999). Over the period of 1906–2005, global air temperatures increased by about 0.7 °C (IPCC Working Group 1 et al. 2013). Notably, the last decade of that period was the warmest on record (IPCC Working Group 1 et al. 2013). Further, general climate models predict temperature to increase by additional 2–8 °C, depending on the region, by the end of the twenty-first century (Christensen et al. 2007). As reported by NASA and NOAA, 2016 was the warmest year on record globally (Northon 2017). Additionally, IPCC predicts patterns in precipitation to change, with more intensive (extreme) rainfall periods that alternate periods of drought (IPCC Working Group 1 et al. 2013). Together, these changes in climate conditions will alter the hydrological conditions in peatlands and will modify processes related to the carbon cycle. Understanding the importance of biotic and abiotic controls on carbon fluxes from peatlands is, therefore, crucial to infer the role of climate change on the feedback of carbon to the atmosphere (Turetsky et al. 2002; Limpens et al. 2008). Additionally, water table drawdown, and long periods without rain, can thus significantly impact the structure of the microbial community (Jaatinen et al. 2007) and the functioning of peatlands (Weltzin et al. 2003; Bragazza 2008), which then can (temporarily) shift from C sinks to C sources (Lafleur et al. 2005; Lund et al. 2012).

The potential of northern peatlands to accumulate carbon (C) is largely determined by the balance between carbon uptake by its vegetation (i.e. through photosynthesis) and carbon release from the peat soil (Alm et al. 1997). Increase global warming, such as the increased temperature and resulting water table drawdown, may imbalance peatland carbon cycles, resulting in a large feedback to the global climate. Results from a recent gradient study have identified reduced peat moss production and increased ecosystem respiration as the main cause of the reduced C uptake by alpine peatlands subjected to the increased temperature and long periods without rain (Bragazza et al. 2016). The authors noted that the increased uptake by the vascular plant community could not compensate for the negative effects of the ecosystem respiration.

Ecosystem respiration (RECO) is usually defined as the sum of autotrophic and heterotrophic respiration (Giardina and Ryan 2000; Valentini et al. 2000). Dorrepaal et al. (2009) have shown that in peat soils, 70% of RECO is accounted by heterotrophic respiration (i.e. decomposition). Therefore, RECO seems mainly driven by abiotic conditions, such as soil moisture and temperature (Komulainen et al. 1999; Dorrepaal et al. 2009). However, the relative importance of temperature and hydrological conditions for RECO is unclear and seems to depend on their relative effect on autotrophic and heterotrophic pathways, which might be decoupled (Lafleur et al. 2005). Remarkably, the effect of vegetation on heterotrophic respiration seems to be larger than the effect of temperature (Ward et al. 2015) or water table (Turetsky et al. 2008), highlighting the importance of these biotic controls on peatland carbon fluxes.

Using an innovative approach of water table manipulation, combined with the use of open-top chambers (OTC’s) to increase air and peat temperature, we studied the effect of the water table drawdown and increased temperature on the RECO. By experimentally raising or elevating 1 × 1 m ‘intact soil monoliths’ within their surrounding soil, thus maintaining a hydrological connection with the surrounding peat matrix, we were able to manipulate the water table, without any concomitant change in the plant and microbial community (as generally seen in micro-topographical gradient studies) (Lamentowicz et al. 2016). We hypothesized that the increased temperature and decreased water table level would result in the increased loss of carbon by respiration, and that the effects of both are additive. Furthermore, we hypothesized that seasonality in respiration rates should follow the patterns in monthly temperature, yet that these relationships are expected to be higher in dry conditions as compared to wet conditions.

Materials and Methods

Study Site

The experimental site, Linje mire (53°11′15”N, 18°18′34″E), is located in northern Poland (Fig. 1), at 91 m a.s.l. The site (approx. 6 ha) is classified as a poor fen with ombrotrophic vegetation in the central part (Kucharski and Kloss 2005). It was drained in the past (dysfunctional drainage ditches are still visible on the peatland surface - Boński and Bońska 2004), but it has been under protection since 1901. The climate is mild oceanic to mild continental (Kottek et al. 2006); mean annual air temperature is approx. 8.0–8.5 °C, and annual precipitation varies between 500 and 550 mm (1971–2000) (Lorenc 2005; Hałas et al. 2008).

Fig. 1
figure 1

Linje mire location and experimental design

The dominant plants species in the experimental area is Sphagnum fallax (H. Klinggr.). The vascular plant community is dominated by the tussock cottongrass (Eriophorum vaginatum L.) and the common sedge (Carex rostrata Stokes), which are accompanied by the common cranberry (Oxycoccus palustris L.), the pine (Pinus sylvestris L.) and the marsh tea (Rhododendron tomentosum Stokes). Endemic to the site, and a glacial relict, is the dwarf birch (Betula nana L.) (Kloss 2005; Kloss and Żurek 2005).

Within the experimental area, we selected 28 1 × 1 m plots with homogeneous plant species assemblage and comparable water table depths. A boardwalk was constructed to prevent damages caused by trampling during the measurements and maintenance works. Half of the plots were covered with open-top chambers (OTCs) that served to increase air temperature. The remaining half of the plots served as ambient controls (CTL). Within both treatments (OTC and CTL), in three plots water table depth was increased (dry – D), whilst in the other three plots water table depth was decreased (wet – W). Further, three plots were assigned as control treatments, and as such water table remained non-manipulated. For simplicity, these plots are hereafter referred to as ‘cut’ water table plots (cut – C). The wet plots were constructed by cutting and removing three 50 × 50 × 30 (l × w × h) blocks of peat including vegetation. We then removed 10 cm of the underlying peat, after which the earlier removed blocks were carefully replaced. This resulted in water table depths under the peat surface in the plots to be decreased by 10 cm, without losing the hydrological connection with the surrounding peat matrix. This whole procedure was repeated for the dry plots, but in this case the 10 cm of peat that earlier was removed from the wet plots was added to the plots before replacing the peat block plus vegetation. This procedure resulted in plots where the water table was manipulated without changing the hydrological context, but with the increased water table depths of 10 cm. The plots with non-manipulated water table received exactly the same treatment, but no peat was removed or added before placing back the peat blocks plus vegetation. The whole procedure led to triplicated plots with all combinations of increased temperature (OTC) or ambient temperature (CTL), and reduced water table depth (wet – W), ambient water depth (cut – C), and increased water table depth (dry - D) (Fig. 1). All 18 experimental plots were bordered with plastic sheeting (15 cm height) so as to maintain the structure of the moss carpet. To control the effect of cutting, the remaining 10 plots – which had intact (uncut) peat soil – only received either the OTC (OTC, n = 5) or remained non-covered (CTL) (Lamentowicz et al. 2016). OTCs were constructed according to the ITEX protocol (Shaver et al. 2000), and consisted of transparent polycarbonate hexagonal chambers (50 cm high, 1.7 m top-width, 2.4 m base-width). OTCs allow quasi-natural transmittance of visible wavelengths, and minimize the transmittance of re-radiated infrared wavelengths (Marion et al. 1997). All OTCs were raised 10 cm above the peat surface to allow air circulation (Lamentowicz et al. 2016).

Measurements of Meteorological Variables

Soil temperature sensors (5TM; Decagon Devices, USA) were installed in all plots at 5 cm depth below the peat moss surface. These sensors registered the peat temperature (Ts) at 5 s intervals, after which 2-min average values were logged (CR1000, Campbell Sci., U.S.A.). These data were used to calculate mean daily soil temperature. Simultaneously, air temperature (Ta) was recorded using HOBO U23 Pro v2 data loggers (Onset Computer Corporation, USA). The sensors were installed at the height of 30 cm above the soil surface to monitor the microclimate in each plot. These parameters were measured every 10 min and used to calculate mean daily Ta.

To record water table depths (WTD), HOBO U20–001-01 pressure data loggers (Onset Computer Corporation, USA) were installed in four wells (5 cm diameter and 2 m long PVC wells) around the experimental site. These loggers were set to record pressure every 3 h and data were averaged to calculate daily values. WTD within each plot was then calculated using experimental treatment (−10 cm, 0 cm and +10 cm) relative to the averaged water table depth across the experimental site. These calculated values were calibrated by manual measurements conducted from time to time in the pipe placed in the center of each plot for hydrochemistry measurements.

Precipitation was recorded continuously 1 m above the soil surface using a tipping bucket Rain Gauge Smart Sensor (S-RGB-M002) with a resolution of 0.2 mm. This sensor was connected to HOBO U30 USB Weather Station Data Logger (Onset Computer Corporation, USA) and the interval of measurements was 10 min.

Measurements of CO2 Exchange

At each plot, CO2 efflux was measured using a dynamic closed chamber system (darkened net canopy assimilation chamber; PP-Systems CPY-4) and an infrared gas analyzer (PP-Systems EGM-4) in a Sphagnum dominated surface where the collar of 20 cm diameter was inserted into the soil to 10-cm depth. During the experiment, the collars were kept free of vascular plants. The CO2 concentration was recorded at 4-s intervals for 2 min. The measurement campaigns were carried out every two weeks during the growing season (April–November). At each campaign field, measurements were performed repeatedly during a full day, using three analyzers and a stochastic sampling scheme for the path of plot measurements. Fluxes are expressed in μmol CO2 m−2 s−1.

Data Analysis

Initially, basic statistical characteristics (mean, minimum, maximum) have been calculated for each variable collected in each plot for different time intervals (30 min, day, month and year) in order to check the data on quality prior to further statistical use. The collected data were categorized according to the manipulative treatments in order to analyze their effect on micrometeorological variables such as daily mean Ts, daily mean Ta, daily mean WTD and RECO. Some missing Ts data in 2013 were calculated using a neural network (Chambers and Hastie 1992). The weights used for these networks were obtained on the basis of training with the data series from 2014. Then we analyzed the distribution of each meteorological variable (Ta, Ts and WTD). Since they did not pass the Lilliefors normality tests, adapted for large data sets (≥ 5000 data entries), we continued using parametric tests. To test for the differences between CTL and OTC treatments for the whole measurement period, we used the one-way ANOVA with P ≤ 0.05 significance threshold. The impact of treatments on RECO values was also tested using a mixed effects model to describe the repeated measures analysis. Treatment is treated as a random variable in the model. (Chambers and Hastie 1992) while Tukey’s post hoc tests were used to determine the differences between treatments (Tukey HSD).

The temperature dependence of soil respiration is commonly expressed by Q10 value. Q10 values were determined for each manipulation treatment. This parameter is the rate of RECO change determined by the interval of Ts equal 10 °C (Winkler et al. 1996; Fang and Moncrieff 2001). Q10 values were calculated as Q10 = (R2/R1)10/(T2-T1), where R2 and R1 are respiration rates found at temperatures T2 and T1, respectively.

All statistical tests were performed with R software version 3.1.2 using the agricolae, car, doBy, lawstat, FactoMineR, fBasics, flux, nortest, xts, zoo packages (Jurasinski et al. 2014, Gastwirth et al. 2015, Gross and Liggers 2015, Mendiburu 2015, R Core Team 2014).


Micrometeorological Conditions in the Experimental Site

The mean Ta of each measurements period from April to November was 13.3 °C and 14.0 °C, respectively (Fig. 2b). The mean Ts in 2013 (12.1 °C) was 0.7 higher than in 2014 (11.4 °C) (Fig. 2a). In the first year, the mean daily Ta reached a maximum on June 20th (25.7 °C) while the mean daily Ts was the highest on August 7th (24.6 °C - Fig. 2b). In 2014 the highest mean daily Ta was observed on July 8 (26.4 °C) and the mean daily Ts on August 2nd (23.8 °C). In 2013 the highest maximum Ta value was found on August 8th (38.4 °C), while in 2014 this extreme was observed on July 28th (38.3 °C). With respect to the WTD (Fig. 2c), the mean value of measurement period was higher in 2013 (−7.4 cm) than in 2014 (−21.2 cm). The WTD during the second half of 2014 was much lower than in the corresponding period of the previous year. In the summer 2014, the WTD was more than 20 cm lower than in summer 2013 and this resulted in annual WTD amplitudes in 2013 (18.0 cm) lower than in 2014 (37.4 cm). Such fluctuations in groundwater levels may be the result of the combination of higher Ta (increasing evapotranspiration) and lower precipitation in 2014. Indeed, the annual total precipitation in 2013 (477.6 mm) was higher than in 2014 (408.7 mm).

Fig. 2
figure 2

Daily mean values (n = 28) of peat temperature - Ts (a), air temperature - Ta (b) water table depth - WTD (c) in Linje mire (2013 - solid red line; 2014 - dashed blue line)

The Effect of Warming and Water Table Manipulation on Microclimate

On average for over two years, OTCs increased Ta by 0.3 °C, which is in the range of results found in other works (e.g. Buttler et al. 2015). Mean values of monthly Ta over two years were not different between OTC (8.4 °C) and CTL (8.1 °C) plots (P = 0.498). But mean monthly maximum Ta during this period was higher in the OTC treatments (16.1 °C) as compared to the CTL treatments (14.9 °C) (P < 0.001). Furthermore, mean monthly Ts over the two years were significantly lower at OTC plots than at CTL plots (P = 0.004). Mean values of monthly Ts were equal between the OTC (7.1 °C) and CTL (7.4 °C). If one considers only the two growing seasons, the mean of daily maximum Ta in OTC plots was increased by 1.1–1.2 °C and 1.6–1.8 °C during the growing seasons of 2013 and 2014, respectively. Manipulation of the water table showed that the mean of monthly WTD for both years was statistically different between the three variants of water table treatments (P < 0.05), which confirms the effectiveness of the applied manipulation. Over the two years, the water level manipulation did not impact the mean of monthly Ta (P = 0.689), but it did affect the mean of monthly Ts (P = 0.003).

Separate Effects of Cutting, Warming and Water Table Manipulation on RECO

The difference between daily maximum Ta in OTC and CTL plots (max delta was approx. 4 °C) determined conspicuous differences in the observed RECO values (Fig. 4). OTC treatments had a significant impact on Reco in 2013 (P = 0.006). Additionally, differences in water level treatments had a significant impact on mean daily RECO values in 2013 (P = 0.003) and 2014 (P = 0.016). The impact of cutting on RECO (i.e. CTL vs CCTL) was found negligible (P > 0.05). In 2014, there was an interaction between OTC and cutting (P < 0.01). These tests showed also an interaction between OTC and WTD in 2014 (P = 0.003).

Overall Comparison of RECO Between Treatments

In 2014, there was also a significant interaction between warming, cutting and water level. The values of RECO during the measurement period of 2013–2014 were in the range between 0 and 4.9 μmol CO2 m−2 s−1 (Fig. 3). The mean RECO during the growing season in 2013 (0.58 μmol CO2 m−2 s−1) was approximately 0.2 μmol CO2 m−2 s−1 lower than in 2014 (0.76 μmol CO2 m−2 s−1).

Fig. 3
figure 3

The ecosystem respiration (RECO) in relation to soil temperature (2013 black dots, 2014 - red dots)

The highest of mean daily RECO values over the two growing seasons 2013–2014 was 0.93 μmol CO2 m−2 s−1 (DOTC), while the lowest was 0.53 μmol CO2 m−2 s−1 (WCTL). If each year is considered separately, in 2013 the lowest mean daily RECO value was observed at OTC plots (0.51 μmol CO2 m−2 s−1), whereas in 2014 it was at COTC (0.65 μmol CO2 m−2 s−1). In contrast, the highest values of mean daily RECO were in both years in DOTC plots (0.80 μmol CO2 m−2 s−1 and 1.16 μmol CO2 m−2 s−1 in 2013 and 2014, respectively).

Mean values of daily RECO in wet plots (0.54 μmol CO2 m−2 s−1 and 0.80 μmol CO2 m−2 s−1, in 2013 and 2014, respectively) were lower than RECO values found in dry plots (0.72 μmol CO2 m−2 s−1 and 0.91 μmol CO2 m−2 s−1 in 2013 and 2014, respectively). Also, wet plots had the lowest mean of maximum daily RECO values in 2013 (2.92 μmol CO2 m−2 s−1), while in 2014 it was at control plots (3.42 μmol CO2 m−2 s−1). The dry conditions determined higher CO2 effluxes (Fig. 3).

Tukey test indicated two significantly different groups of RECO treatments (letters A and B in Fig. 4). In both years mean RECO values in DOTC treatment were significantly higher than the values obtained in CTL, OTC and WCTL treatments. In 2013, the CCTL belonged also to this last group, and in 2014 it was COTC.

Fig. 4
figure 4

Tukey test comparison for mean values of RECO in all treatments for the growing seasons 2013 (a) and 2014 (b). The central bars indicate the median values, points indicate the mean values, the box limits indicate the first and third quartiles and the whiskers show the minimum and maximum values. Capital letters indicate significant differences

Q10 Value

In our study Q10 coefficients varied between treatments and years, ranging from 2.0 (DOTC and COTC in 2013) to 6.1 (WOTC in 2014) (Fig. 5). The pairwise comparisons, where CTL, DCTL, CCTL and WCTL are compared with OTC, DOTC, COTC and WOTC, respectively, show that in most cases the OTC treatment increased Q10 value in 2013 and 2014 except the dry treatment in 2013 (DOTC, decrease of 0.2) and the wet treatment in 2013 (WOTC, decrease of 0.6). The mean Q10 value for the period of April to November 2014 was 3.3, while for the same period in 2013 it was 3.0, and for both years it was 3.1.

Fig. 5
figure 5

Mean Q10 values for each combination of treatments in 2013 (grey) and 2014 (dark grey). Error bars represent standard deviation (Control uncut plots: N = 5, dry, cut and wet plots: N = 3)


Additive Effect of Warming and Lowering of WTD on C Cycling

Many studies documented that main factors impacting soil respiration (RECO) and therefore carbon emissions are air temperature (Bubier et al. 1998; Bortoluzzi et al. 2006; Davidson et al. 2006; Chojnicki et al. 2010; Heijmans et al. 2013) or peat temperature (Chapman and Thurlow 1996; Silvola et al. 1996; Lafleur et al. 2005; Juszczak et al. 2013; D’Angelo et al. 2016). Approximate 1 °C temperature increase at subarctic peatlands resulted in increases of RECO values and mobilization of carbon that was located in deeper peat layers (Dorrepaal et al. 2009). Chivers et al. (2009) stated that despite different water levels observed at their sites, there was no impact of WTD on RECO. Although, according to Lafleur et al. (2005), a variability in WTD has a major impact on the peatland respiration if the water table is close to the surface.

Our study provides experimental evidence that both warming and WTD impacted RECO, but more importantly that a combination of the increased temperature and lower WTD resulted in an additive effect on loss of carbon by respiration. The most striking differences were found at dry plots with warming (DOTC), most likely due to the enhanced aerobic conditions in the acrotelm (Chambers et al. 2011). Despite inter-annual climate variability, RECO values observed at DOTC plots were significantly different from RECO in other treatments, in both years. This supports the statement that the impact of a single factor alone is less effective than a combined effect. Indeed, in our experiment, the warming by means of OTCs and the lowering of water table had the largest impact on soil respiration.

Our results correspond well to findings in other experimental studies. Samaritani et al. (2010) showed that the strongest differences in soil respiration were observed during the warmer and drier periods. Long periods without rain may result in a sharper transition between unsaturated and saturated peat layers (Hornibrook et al. 2008) and change diffusion coefficients and water saturation within the peat, which can slow down the transport of gases and solutes in the peat profile (Waddington and Roulet 1997; Fraser et al. 2001; Limpens et al. 2008). Our results show that the peatland carbon flux can be modified by even small changes in environmental conditions such as those induced by our treatments. Since processes related to carbon losses are related to temperature and hydrology, which are dynamically interrelated, the application of combined temperature and WTD treatments has the potential to simulate more reliably the impact of climate change on the functioning of peatland than single factor manipulative experiments.

Cutting Impact on RECO

Since the cutting may have affected the vegetation functioning and e.g. transpiration rates can be modified by this intervention, therefore we did not notice differences between control and cutting treatments in both measurement years. Also indirectly cutting decreased Q10 in 2013 (Fig. 5) by interrupted connection structures in peat monoliths, however dry and warmer year of 2014 caused increasing Q10 values (Fig. 5). So far many studies showed that clipping and removing the aboveground parts of plants decreased RECO, because this reduces soil respiration by decreasing the input of labile carbon to soil (Wan and Luo 2003; Bahn et al. 2006) and/or by weakening the assimilation supply from photosynthesis (Bahn et al. 2008). It is widely known that the cutting causes slower regeneration of plants (Silvola et al. 1996).

High Yearly and Seasonal Variation of RECO

The respiration fluxes obtained during the two-field campaigns show that higher RECO values were recorded in 2014, which also had warmer mean annual Ta as compared to 2013. Thus, the Ts measured at 5-cm depth was probably less influential on mean annual RECO values and the fact of temperature drop at OTC sites suggests that heat induced CO2 emission was mainly determined in upper layers of peat profile. Our results showed a significant difference in the Ts between CTL and OTC treatments, however mean Ts at OTC’s was lower than CTL’s. This result may be explained by the fact that OTCs did not affect the temperature as measured with the sensors placed 5 cm below the surface (Chivers et al. 2009). However, the impact of OTC may be noticeable during the freeze-thaw and extremely high temperature events (Bokhorst et al. 2013). Indeed, we have found significant effects of OTC on plots’ microclimate using maximum daily Ta. Thus, the significant effect of warming on monthly RECO values is most likely the result of the increase in the Ta inside the chamber during hot and sunny summer days (Fig. 3) (Lamentowicz et al. 2016). In these extreme conditions, the OTC can effectively change the heat balance at the peatland surface (Lamentowicz et al. 2016) - an effect which can decline rapidly with depth. The advection of relatively warm air mass during the winter time increases the speed of snow melting at the peatland surface but the OTC presence can restrict the heat transport via reduction of the wind speed over the vegetation canopy (the sensible heat flux reduction). Furthermore, the presence of snow caused thermal insulation as well as increased the albedo. Both phenomena reduced the amount of heat at the surface of the peatland. This observation corresponds well to what was described by other authors (Marion et al. 1997; Johnson et al. 2013). Seasonality in respiration rates in our study is following the monthly Ta patterns, however CO2 emission strongly depended on peat moisture. Nijp et al. (2014) presented the opinion that in many situations warming does not increase RECO because of the water access limitation. Our results seem to be in contradiction to this statement since the CO2 emission in 2014 was higher (0.2 μmol CO2 m−2 s−1) than in 2013 with the lower water level during the second measurement season. Most probably the increase of acrotelm thickness triggered the increase of CO2 emission from the deeper peat layers.

Q10 Values Describe the Dynamics of RECO

The differences of peat Q10 values between treatments support previous findings that temperature and moisture have a direct influence on Sphagnum productivity (Turetsky et al. 2012) and microbial communities (Peltoniemi et al. 2015), and this is reflected in RECO. The higher temperatures elevate CO2 respiration and may also stimulate plant productivity, especially in cold regions (Rustad et al. 2001). Results of field experiments show the increased Sphagnum productivity with warming (Robroek et al. 2007), as long as there was sufficient water (Dorrepaal et al. 2003). In Linje mire, the noticeably lower Q10 values found in the dry treatment can be explained by changes in microclimate conditions that affect the microbial community (Luo et al. 2001; Allison et al. 2010; Crowther and Bradford 2013) and particularly by the lower peat moisture (Silvola et al. 1996; Suseela et al. 2012). These findings follow the results presented by other authors, Q10 parameters was also described by other authors and for wetlands have been reported as values between 2.2 and 4.2. (Lafleur et al. 2005) and from 2.0 to 8.9 (Hirota et al. 2006), 2.9–9.4 (Acosta et al. 2017). The values of this parameter in our case was ranging from 2.0 to 6.1. Q10 values depended on the depth where soil temperature was measured. High Q10 values were related with soil temperature at 10 cm and they considered that it reflects the influence of the low temperature range (Acosta et al. 2017). Kirschbaum (1995) suggested that high Q10 can be attributed to low soil respiration under low temperature. Here, we demonstrate that the OTC generally increased the respiration Q10 values, however in wet conditions, Q10 increased strongly with OTC (WOTC = 6.1), indicating a high reactivity of respiration rate when the organic matter got exposed to aerobic conditions.

Estimated Yearly Carbon Loss

The estimated values of the cumulated RECO at Linje mire for both years (113.7 g C-CO2 m−2 yr−1) are smaller than at Degerö Stormyr poor fen in the middle of Sweden (404.0 g C-CO2 m−2 yr−1) (Nillson et al. 2008; Wu et al. 2013). On the other hand, similar values of cumulated RECO were measured at Mer Bleue raised bog (Roulet et al. 2007) and at Stordalen mixed mire (Bäckstrand et al. 2010), specifically 230.0 and 150.0 g C-CO2 m−2 yr−1, respectively. These differences may be dependent on the type of peatland (Jaatinen et al. 2007), although inter-annual variability of temperature (Pullens et al. 2016) and moisture (Turetsky et al. 2012) may strongly modify the carbon balance of the compared mire ecosystems.


We report on the first experimental study in a Central European peatland aiming at assessing the effect of projected climate change on RECO.

  1. 1.

    Our results show that OTCs changed micrometeorological conditions by the increase of Ta near the ground.

  2. 2.

    We show that the combined warming and lowering of water table had an additive effect on the increased peatland RECO. Respiration rates were highly seasonal and followed patterns in mean monthly temperature values.

  3. 3.

    Our experimental study confirms that peatland RECO is a sensitive indicator, even of very subtle changes of micrometeorological conditions. Such sensitivity has an important implication to monitor the carbon sink function of Central European poor fens.

  4. 4.

    Q10 value very well describes the dynamics of RECO since this parameter reacted to both changes in temperature and WTD.