Disparte ( 1987) measured an increase of infiltration with higher rooting density after decomposition of roots. 2005), thereby facilitating water transport through the soil (Gish and Jury 1983 Murphy et al. These pores have high connectivity (Pagliai and De Nobili 1993 Whalley et al. 1995 Wuest 2001 Horn and Smucker 2005 Ghestem et al. After root decay, bio-macropores and root-induced micropores are formed (Cresswell and Kirkegaard 1995 Mitchell et al. ( 1993) measured reduced infiltration rates as long as plants are actively growing and their roots block pore channels. These effects are depending on the lifespan of roots. Micro-fissures and cracks are structural pores formed in the root zone of transpiring plants by more intense wetting-drying (e.g. Scanlan ( 2009) suggested that root in-growth results in the division of larger into smaller pores. Temporal pore clogging occurs due to roots growing into pre-existing pores (e.g. Several pathways of root influence on soil hydraulic properties have been described. ( 2011) demonstrated that contrary to the usual assumption of higher depletion in vicinity of roots (Gardner 1960), soil water content is higher in rhizosphere soil compared to bulk soil over a wide range of pressure heads, indicating a significant change of the water retention curve in vicinity of plant roots.
Roots are a key element in plant related effects on soil structure and soil hydrology (Gregory 2006 Bengough 2012 Logsdon 2013). Among the various driving factors of soil structural porosity, vegetation is playing a dominant role. retention and hydraulic conductivity, in the saturated and near-saturated range (Cresswell et al. Beside texture, soil structure is the main property to shape the fundamental relations for soil water flow, i.e.
Soil hydraulic properties are the common result of particle size distribution (texture) and aggregation (structure).
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