[MIS01-06] Relationship between the distribution of crevasse-splay deposits and the inundation distance of the October 2019 flooding of the Chikuma River, central Japan
Keywords:Flood deposit, Crevasse splay
We set up three river-perpendicular 1.4–2.2-km-long transects and investigated crevasse-splay deposits at about 100 m intervals together with the current direction and water depth along each transect. The measured elevation is lowering until 1.2 km from the levee and is getting higher from that point onwards. The crevasse-splay deposits were composed of a lower sand layer and overlying mud layer near the breached levee, but they were massive muddy sediments at the area distant from the levee. The thickness of the sand layer shows a thinning trend toward the foot of mountains, while the thickness of the mud layer varies in association with the topography rather than the distance from the levee. Along the 2.2-km-long transect from the breached levee, the sand layer extended to 0.8 km from the levee, whereas the mud layer was distributed until 1.6 km from the levee. The distribution of sand layer is affected by the distance from the breached levee, but not by water depth, indicating that the deposition of sandy sediments during a river flooding is affected by current velocity probably correlated with a distance from the breached levee. There were no sediments near the limit of the flooded area, between 1.7 and 2.2 km from the levee. This is probably because the stagnant floodwater took a relatively short time to recede at around the inundation limit since the elevation is higher than the area where the thick muddy sediments were observed.
The maximum limit of the sand and mud layers along three transects extended to 0–36% and 73–84% of the inundation distance, respectively. The maximum limit of the recent sandy tsunami deposits, in contrast, extended to over 90% of the inundation distance where the inundation distance is less than 2.5 km (Abe et al. 2012, Sedimentary Geology). The difference between the distribution of a sand layer by crevasse splay and tsunami is probably attributable to the difference in their hydraulic behaviors. It is considered that the crevasse-splay flow is too weak to transport sand grains to the area distant from the breached levee.