Temporal and spatial variation of infilling processes in a landslide scar in a steep mountainous region, Japan

• Published in: Earth surface processes and landforms 2015-04, Vol.40 (5), p.642-653
• Main Authors: Imaizumi, Fumitoshi, Sidle, Roy C., Togari-Ohta, Asako, Shimamura, Makoto
• Format: Article
• Language: English
• Subjects: Creep (materials); dry ravel; Geographic information systems; infilling; landslide; Landslides; Landslides & mudslides; Satellite navigation systems; Scars; sediment flux; Sediment transport; Sediments; Slope gradients; Soil (material); soil creep
• ISSN: 0197-9337; 1096-9837
• DOI: 10.1002/esp.3659

The duration of the soil‐depth recovery needed for reoccurrence of shallow colluvial landslides at a given site in humid regions is much longer than the return period of rainfall needed to generate sufficient pore water pressure to initiate a landslide. Knowledge of the rate of change in soil depth in landslide scars is therefore necessary to evaluate return intervals of landslides. Spatial variation in sediment transport at the Kumanodaira landslide scar in central Japan was investigated by field observations. Spatial distribution of the rate of change in soil depth was estimated using sediment transport data and geographic information system (GIS) analysis. Observations revealed that the timing of sediment transport differed for shallow and deep soil layers. Near‐surface sediment transport (mostly dry ravel and some shallow soil creep at depths ≤0·05 m) measured in sediment traps was active in winter and early spring and was affected by freezing–thawing; soil creep of subsoil (i.e. >0·05 m), monitored by strain probes, was active in summer and autumn when precipitation was abundant. Near‐surface sediment flux was estimated by a power law function of slope gradient. Deeper soil creep was more affected by relative location to the landslide scar, which influences soil depth, than by slope gradient. Our study indicated that the rate of soil‐depth recovery is high just below the head scarp of the landslide. Abrupt changes in the longitudinal slope topography immediately above, within and just below the head scarp became smoother with time due to degradation proximate to the landslide head scarp and flanks, as well as aggradation just below the head scarp. Copyright © 2014 John Wiley & Sons, Ltd.