# Heat Capacity of Drained Peat Soils  
[PERSON]  
1 Department of Environmental Management, Institute of Environmental Engineering, Warsaw University of Life Sciences-SGGW, 02-776 Warsaw, Poland; grzegorz_,[EMAIL_ADDRESS] (G.K.); [PERSON]AIL_ADDRESS] (J.S. )1  
[PERSON]  
2 Department of Chemistry, Institute of Food Sciences, Warsaw University of Life Sciences-SGGW, 02-776 Warsaw, Poland; ewa_,ostrowska_,[EMAIL_ADDRESS] (J.S. )2  
[PERSON]  
3 Department of Engineering, University of Cambridge, Cambridge CB2 1 PZ, UK; [EMAIL_ADDRESS]  
[PERSON]  
1 Department of Environmental Management, Institute of Environmental Engineering, Warsaw University of Life Sciences-SGGW, 02-776 Warsaw, Poland; grzegorz_,[EMAIL_ADDRESS] (G.K.); [EMAIL_ADDRESS] (J.S. )2  
[PERSON]  
1 Department of Environmental Management, Institute of Environmental Engineering, Warsaw University of Life Sciences-SGGW, 02-776 Warsaw, Poland; grzegorz_,[EMAIL_ADDRESS] (G.K.); [PERSON]AIL_ADDRESS] (J.S. )2  
[PERSON]  
3 Department of Engineering, University of Cambridge, Cambridge CB2 1 PZ, UK; [EMAIL_ADDRESS]  
[PERSON]  
1 Department of Environmental Management, Institute of Environmental Engineering, Warsaw University of Life Sciences-SGGW, 02-776 Warsaw, Poland; grzegorz_,[EMAIL_ADDRESS] (G.K.); [EMAIL_ADDRESS] (J.S. )2  
[PERSON]  
1 Department of Environmental Management, Institute of Environmental Engineering, Warsaw University of Life Sciences-SGGW, 02-776 Warsaw, Poland; grzegorz_,[EMAIL_ADDRESS] (G.K.); [EMAIL_ADDRESS] (J.S. )2  
and autotrophic (root) respiration. Although these two sources are difficult to separate, they often are additive and treated as a total soil respiration [8]. The measured amount of the CO\({}_{2}\) efflux in peat soils depends on soil temperature, groundwater level position [9], and soil moisture content [10]. The empirical investigation proved that greenhouse gases modeling, besides other environmental factors, depends on the soil temperature dynamics [11]. The volumetric heat capacity (\(C_{\text{\tiny{p}}}\)) is a complex soil property which is used in the studies of soil temperature and heat flow. It includes knowledge about soil thermal status but also incorporates information about soil physical properties (soil bulk density and volumetric moisture content). Thus, \(C_{\text{\tiny{p}}}\) is often expressed in the form of a mixing model as the sum of volume fractions of thermal capacities of the individual soil components, i.e., solid, liquid, and gaseous [12]. In practical applications the \(C_{\text{\tiny{p}}}\) value can be estimated by neglecting the gaseous phase and by considering only two soil constituents, i.e., solid and water phases [13]. Because the specific heat capacity and density of water (\(c_{\text{\tiny{w}}}\) and \(\rho_{\text{\tiny{w}}}\), respectively) are commonly known, to determine \(C_{\text{\tiny{v}}}\) using a mixing model the specific heat capacities (\(c_{\text{\tiny{p}}}\)) for solid particles should be measured independently. The \(c_{\text{\tiny{p}}}\) values for soil mineral constituents are in the range of approximately 0.718 to 0.939 J g\({}^{-1}\) K\({}^{-1}\)[13; 14; 15]. The published data of [PERSON] (1963) [12] show that for organic soils the \(c_{\text{\tiny{p}}}\) values range from 1.738 to 1.994 J g\({}^{-1}\) K\({}^{-1}\) with a value of 1.925 J g\({}^{-1}\) K\({}^{-1}\) at an average particle density 1.300 g cm\({}^{-3}\). In studies on investigation of the heat transfer in the boreal bog, the \(c_{\text{\tiny{p}}}\) values for organic soils were between 1.380 and 2.000 J g\({}^{-1}\) K\({}^{-1}\)[16]. For the past four decades the most widely used technique for studying specific heat capacity as a function of temperature has been the modulated differential scanning calorimetry (MDSC) method. This method has been developed by combining the conventional differential scanning calorimetry (DSC) and the temperature modulated calorimetry (TMC) techniques.