Sediment transport by overland flow over an area of net deposition

Beuselinck, L; Govers, Gérard; Steegen, An; Quine, T. A.

doi:10.1002/(sici)1099-1085(19991215)13:17<2769::aid-hyp898>3.0.co;2-x

Cited by 52 publications

(60 citation statements)

References 25 publications

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“…Size-selectivity during the depositional process is directly related to the degree of (micro-) aggregation of the transported sediment. If sediments are fully dispersed, deposition is highly selective and the fine fraction will almost completely be removed (Beuselinck et al, 1999). However, as sediments are transported in (micro-)aggregated form, most of the fine fraction is (re-)deposited after the transport phase .…”

Section: Sediment and C Depositionsupporting

confidence: 75%

Catchment-scale carbon redistribution and delivery by water erosion in an intensively cultivated area

et al. 2010

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Section: Sediment and C Depositionsupporting

confidence: 75%

Catchment-scale carbon redistribution and delivery by water erosion in an intensively cultivated area

et al. 2010

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“…Stream power calculations were used to ascertain whether entrainment in the overland flow contributed to soil erosion (Beuselinck et al, 1999;Kinnell, 2005). According to Beuselinck et al (2002) for loamy soils the critical stream power above which entrainment occurs is in the range 0.15-0.20 W m -2 .…”

Section: Overview Of the Experimentsmentioning

confidence: 99%

Rain splash soil erosion estimation in the presence of rock fragments

Jomaa

Barry

Brovelli

et al. 2012

CATENA

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Rain splash soil erosion in the presence of rock fragments and different initial conditions was tested in laboratory flume experiments under controlled conditions. The aim of the experiments was to ascertain whether cumulative soil erosion is proportional to the area of soil exposed to raindrop detachment under the condition of constant and uniform precipitation. The surface area exposed to rain splash erosion was adjusted by placing rock fragments onto the surface of identically prepared soil in laboratory flumes. The laboratory results showed that the eroded cumulative mass depended on the cumulative runoff, and that soil erosion was proportional to the soil surface area exposed to raindrops, in situations where an initially dry, ploughed and smoothed soil surface were ensured. The results showed that this relationship was controlled to a smaller extent by the soil's initial moisture content, bulk density and soil surface characteristics.When the initial conditions were more complex, soil erosion was proportional to the area exposed only at steady state. Then, sediment concentrations during the first part of the erosion event were instead more sensitive to the initial state of the soil surface, whereas at steady state it was observed that the concentrations of eroded sediments were controlled mainly by the effective rainfall and area exposed to raindrops. Previously published field data on rain splash soil erosion were analyzed to ascertain whether the same behavior was evident under field conditions. For this case it was found that rain splash erosion is in general not proportional to the area exposed. In contrast to the controlled laboratory experiments, the field experiments were characterized by non-uniform initial surface roughness, surface soil aging and heterogeneous rock fragment size and spatial distribution. However, the presented laboratory results showed clearly that, for soils with negligible surface roughness, erosion depends on (i) the area of soil 3 exposed to rainfall and (ii) the cumulative runoff, and that it is only slightly dependent on other soil variables.Keywords: Soil erosion experiment, Area exposed, Flume experiment, Cumulative discharge, Cumulative eroded mass, Soil initial conditions. IntroductionOver several decades, attention has been given to the effect of the soil surface characteristics (such as surface roughness, crop residues, organic mulches, vegetation cover and rock fragment coverage) on runoff generation, infiltration and soil erosion rates Poesen et al., 1999;Li, 2003;Gyssels et al., 2006;Smets et al., 2008;Knapen et al., 2009;Guo et al., 2010;Zavala et al., 2010). Numerous studies have pointed out the role played by surface rock fragments on erosion as well as on the hydrological response of soils (such as infiltration rate, surface ponding, runoff generation) (Adams, 1966;Poesen et al., 1990Poesen et al., , 1998Poesen et al., , 1999 Parsons, 1991, 1994;Bunte and Poesen, 1994;Ingelmo et al., 1994;Poesen and Lavee, 1994;Torri et al., 1994;van Wesemael et al., 19...

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“…If the local stream power ( ) is less than a critical threshold ( cr ), re-entrainment does not occur and deposition of size class i is a function of its specific settling velocity (Beuselinck et al, 1999;Hairsine et al, 2002). If the local stream power exceeds this threshold value, a shielding factor H is calculated to decide whether net erosion or deposition occurs (Hairsine and Rose, 1992a):…”

Section: Modelling Erosion and Depositionmentioning

confidence: 99%

“…The grey area represents the range of possible settling velocities related to different proportions of primary particles or soil aggregates. Right y axis shows the settling velocity classes as implemented in the model for primary particles and aggregates (based on particle size distribution measurements conducted by Beuselinck et al, 1999). Luvisols, with a clay, silt and sand content of 14, 82, and 4 %, respectively (Desmet and Govers, 1997).…”

Section: Model Implementationmentioning

confidence: 99%

“…Following detachment, the model simulates the transport and deposition of primary particles or aggregated soil based on the erosion type of detachment that they underwent. The particle size distributions of primary particles and aggregated soil were taken from direct measurements (n = 81) in the Belgian loess belt conducted by Beuselinck et al (1999). The grain size distribution for aggregated soil represents the relative difference between fully dispersed and non-dispersed soil in 10 different diameter classes.…”

Section: Model Implementationmentioning

confidence: 99%

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Modelling a century of soil redistribution processes and carbon delivery from small watersheds using a multi-class sediment transport model

2017

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Abstract.Over the last few decades, soil erosion and carbon redistribution modelling has received a lot of attention due to large uncertainties and conflicting results. For a physically based representation of event dynamics, coupled soil and carbon erosion models have been developed. However, there is a lack of research utilizing models which physically represent preferential erosion and transport of different carbon fractions (i.e. mineral bound carbon, carbon encapsulated by aggregates and particulate organic carbon). Furthermore, most of the models that have a high temporal resolution are applied to relatively short time series (< 10 yr −1 ), which might not cover the episodic nature of soil erosion. We applied the event-based multi-class sediment transport (MCST) model to a 100-year time series of rainfall observation. The study area was a small agricultural catchment (3 ha) located in the Belgium loess belt about 15 km southwest of Leuven, with a rolling topography of slopes up to 14 %. Our modelling analysis indicates (i) that interrill erosion is a selective process which entrains primary particles, while (ii) rill erosion is non-selective and entrains aggregates, (iii) that particulate organic matter is predominantly encapsulated in aggregates, and (iv) that the export enrichment in carbon is highest during events dominated by interrill erosion and decreases with event size.

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Sediment transport by overland flow over an area of net deposition

Cited by 52 publications

References 25 publications

Catchment-scale carbon redistribution and delivery by water erosion in an intensively cultivated area

Catchment-scale carbon redistribution and delivery by water erosion in an intensively cultivated area

Rain splash soil erosion estimation in the presence of rock fragments

Modelling a century of soil redistribution processes and carbon delivery from small watersheds using a multi-class sediment transport model

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