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Many applications in watershed management, forestry, agriculture, and horticulture require hydrologically feasible estimates for assessing the rate at which water infiltrates and percolates through the soil, and how much of that is either taken up by the vegetation or passes through the ground until entering flow channels and streams further below in the landscape. In the literature, there are many approaches to do this, ranging from direct field measurements to numerical and theoretical constructs (Di Frederico and Tartakosky 2000; Pachepsky and Rawls 2005; Sudicky et al. 2010). Field measurements focus on, e.g., (i) direct measurements regarding the rate of infiltration, (ii) hydraulic gradients and hydraulic conductivities along hillslopes and aquifers, and (iii) stream discharge. Theoretical means infer soil and subsoil water retention and hydraulic conductivities from basic soil properties such as soil texture, organic matter content, and density. In turn, these estimates can then be used to determine temporal changes in soil moisture and soil moisture flow within fields (or hydrological response units), along hill slopes and across catchments, by way of simple trickle-down models (e.g., Church 1997), or complex geographically distributed hydrology models (Kim et al. 2008). The most elaborate models generate atmosphere-vegetation-soil transference fluxes based on empirical Eddy correlation techniques (Kuchment et al. 2006), while the simpler models use weather records involving precipitation and air temperature to assess daily changes in soil moisture and water flow (Balland et al. 2006; Murphy et al. 2009). This chapter (i) presents a generalized framework for estimating soil hydraulic conductivities at saturation, i.e., Ksat, at the soil-layer level, and (ii) applies this framework for modelling water retention and stream discharge for six wellstudied forest catchments across Canada, from east to west. Within this framework, special attention is given to ensure that i. soil moisture content at field capacity (FC) is always smaller than soil moisture content at the saturation point (SP), ii. the permanent witting point (PWP) is always smaller than FC,

Determining Hydraulic Conductivity from Soil Characteristics with Applications for Modelling Stream Discharge in Forest Catchments