## 2 Materials and Methods
### DIMONA Platform and Model
#### 2.1.2. DIMONA Process-Based (PB) Model
For each soil layer i of the unsaturated soil profile, soil air availability, \(f_{\rm{GR,i}}\) (Equation (S4.4.1.3)), is estimated from the ambient soil water content available for the root/rhizoid water uptake, \(\theta_{\rm{i}}\), soil total porosity, \(\theta_{\rm{TP,i}}\), soil macroporosity, \(\theta_{\rm{MP,i}}\) (if any), and soil water content at field capacity, \(\theta_{\rm{FC,i}}\), of that soil layer, as follows:  
Figure 7:3  
with \(f_{\rm{GR,i}}\) acting in a similar way to \(f_{\rm{GR}}\) above. When soil approaches field capacity, \(\overline{\rm{\theta}}=\overline{\rm{\theta}}_{\rm{FC}}\), \(f_{\rm{GW}}=1\) in Equation (8) (Equation (S4.4.1.1)) and \(f_{\rm{GR}}=1\) in Equation (9) (Equation (S4.4.1.2)); hence, \(f_{\rm{\theta}}=(1+f_{\rm{\theta A}})/(1+f_{\rm{\theta A}})=1\) in Equations (2a,b) (Equation (S4.2.1.a,b,c,d)) and \(f_{\rm{\theta}}=1\) in Equation (3) (Equation (S4.2.1.2a,b)). Also, \(f_{\rm{R}}=(1+f_{\rm{\theta A}})/(1+f_{\rm{\theta A}})=1\) in Equation (4) (Equation (S4.3.1.1a,b)) and \(f_{\rm{R}}=1\) in Equation (5) (Equation (S4.3.1.2a,b)), \(f_{\rm{U,i}}=(1+f_{\rm{\theta A}})/(1+f_{\rm{\theta A}})=1\) in Equation (6) (Equation (S4.3.1.3a,b)) and \(f_{\rm{U,i}}=1\) in Equation (7) (Equation (S4.3.1.4a,b)). Thus, consistent with other studies [20; 21], there are no hydrology limitations on plant growth, root/rhizoid respiration, and nutrient uptake when soil is at field capacity in the model. The Effect of Air Availability on Plants from Adaptations to Wetland Soil Conditions  
The modifier for the effect of air availability on plant productivity and growth, root respiration, and nutrient uptake from adaptations to wetland soils, \(f_{\rm{\theta A}}\) (Equations (S4.5.1.1) and (S4.5.1.2)), is  
Figure 7:4 Figure 7:5  
where \(\rm{d}_{\rm{SL}}\) is the depth of the entire soil profile (unsaturated and/or saturated). Thus, when \(\rm{d}_{\rm{WT}}=0\), then \(f_{\rm{\theta A}}=1\), indicating plants with adaptations to wetland soils. When WT recedes down the soil profile, i.e., \(\rm{d}_{\rm{WT}}>0\), and increases with WT drawdown while \(\overline{\rm{\theta}}>\overline{\rm{\theta}}_{\rm{FC}}\), then \(f_{\rm{\theta A}}\) increases above unity, reflecting improved root activity, with receding WT and with adaptations to wet soils. When the soil becomes less wet, with \(\overline{\rm{\theta}}\leq\overline{\rm{\theta}}_{\rm{FC}}\), often accompanied by WT receding further down, then \(f_{\rm{\theta A}}\) also decreases, reflecting a diminishing role of adaptations with improved soil aeration, proportionally to \(\rm{d}_{\rm{WT}}/\rm{d}_{\rm{SL}}\). Thus, \(f_{\rm{\theta A}}\to 0\) with WT approaching the bottom of the soil profile, or disappearing, i.e., with \(\rm{d}_{\rm{WT}}\to\rm{d}_{\rm{SL}}\), reflecting no need for adaptations in the well-earated soil. Soil Hydrology  
Previously, the hydrological module for peat in the _DIMONA_ PB model (i.e., the PHM model) was applied to the Mer Bleue bog to simulate \(\theta\) at various peat depths at a daily time step driven by observed d\({}_{\rm WT}\)[26] and near-surface \(\theta\)[27]. It is from these studies that the above modifiers were estimated at an hourly time step.