Water Recharge in a Soil with Shrinkage Cracks

Blake, G. R.; Schlichting, E.; Zimmermann, Udo

doi:10.2136/sssaj1973.03615995003700050014x

Cited by 55 publications

(30 citation statements)

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“…A theoretical model for the behaviour of tritiated water in soils was subsequently developed by Zimmermann and co-workers (Zimmermann et al, 1966;Blume et al, 1967;Zimmermann et al, 1967). The basis of this model is rapid, lateral molecular exchange between 'stationary'and 'mobile' water on a scale of the order of grain size in a homogeneous soil ( N 1 s for particle size 0.05 mm, using a self-diffusion constant of water D = 2.13 x m2 s-' at 25°C (Simpson and Carr, 1958)).…”

Section: Introductionmentioning

confidence: 99%

Vertical soil water movement in a tropical rainforest catchment in northeast queensland

Bonell

Cassells

Gilmour

1983

Earth Surf Processes Landf

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In a tropical rainforest catchment, shallow piezometers respond almost instantaneously to rainfall, but the dominant groundwater recharge mechanisms are not well understood. To improve understanding, the downward movement of soil water on a runoff plot was traced using tritiated water injected at 0.20 m below the surface which marks the lower boundary of active subsurface storm flow. The tritium pulse was translated slowly down the profile, apparently dominated by interstitial piston flow on the lines described by Zimmermann's theoretical model. This recharge mechanism accounted for about 35 per cent of rainfall or 50 per cent of throughfall. The pulse's advance may have also been delayed by the upward movement of soil water indicated by the distribution of hydraulic potential under different hydrological conditions. The result was an increase in soil water transit time particularly below 1.0 m. There was also evidence in the tracer profiles for rapid by-pass flow but the volumes concerned could not be quantified in this experiment.

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Section: Introductionmentioning

confidence: 99%

Vertical soil water movement in a tropical rainforest catchment in northeast queensland

Bonell

Cassells

Gilmour

1983

Earth Surf Processes Landf

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“…The most recognized PF mechanisms in the unsaturated zone are: crack flow, burrow flow, finger flow, and lateral flow Roulier and Schulin 2006). Crack flow (CF) refers to PF along continuous cracks in soils (Blake et al 1973); burrow flow (BF) to flow through channels created by soil fauna such as earthworms (Domı´nguez et al 2004); finger flow (FF) to flow through fingers starting at a fine-over-coarse soil interface (Starr et al 1978); and lateral flow (LF) to lateral movement over an inclined hydraulically restrictive layer (Weyman 1973;Weiler and McDonnell 2007). The rapid transport of water through PF pathways may be important for water recharge and for decreasing surface runoff, especially in clayed soils.…”

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confidence: 99%

Development of a method for estimating the likelihood of crack flow in Canadian agricultural soils at the landscape scale

Dadfar¹,

Allaire²,

Jong³

et al. 2010

Can. J. Soil. Sci.

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Development of a method for estimating the likelihood of crack flow in Canadian agricultural soils at the landscape scale. Can. J. Soil Sci. 90: 129Á149. Indicators of risk of water contamination by agricultural pollutants are developed in Canada to assess sustainability of agriculture. Crack flow (CF), a key pathway for sub-surface contaminant transport, is part of the transport-hydrology algorithm used in two of these risk indicators. The objective was to develop a methodology for predicting the likelihood of CF in Canadian agricultural soils at the landscape scale. The algorithm considers soil clay content, crack development followed by a runoff event based on water budget, tile drainage, and crops. More than 40% of Canadian farmlands had moderate to very high likelihood of CF, mainly in Manitoba, Ontario and Quebec, due to frequent runoffs on cracked clay soils potentially contributing to groundwater contamination. In Ontario and Quebec, farmlands with high CF likelihood correspond to regions under intensive tile drainage, which increases the risk of lateral translocation of contaminants to surface water bodies. Besides being a component of risk indicators of water contamination by phosphorus and coliforms, the CF algorithm and maps can be used to identify areas at risk of subsurface water contamination. Best management practices, adapted to reduce CF can then be targeted to these areas.

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“…This is in agreement with the presence of well developed pedality, cracks, and slickensides in the upper profiles of the Laewest in our study area promoting non-Darcian by-pass flow. By-pass flow under these conditions diminishes the movement of water to ped interiors where they remain oxygenated (Blake et al, 1973;Anderson and Bouma, 1977a, b;Bouma et al, 1977;Bouma and Lovejoy, 1988;Lin et al, 1999). By-pass flow can penetrate to depths of greater than 2 m in a matter of days without saturating overlying zones even in subhumid to humid Vertisols (Blake et al, 1973;Lin and McInnes, 1995).…”

Section: Hydropedological Formation Of Vertisolsmentioning

confidence: 99%

“…By-pass flow under these conditions diminishes the movement of water to ped interiors where they remain oxygenated (Blake et al, 1973;Anderson and Bouma, 1977a, b;Bouma et al, 1977;Bouma and Lovejoy, 1988;Lin et al, 1999). By-pass flow can penetrate to depths of greater than 2 m in a matter of days without saturating overlying zones even in subhumid to humid Vertisols (Blake et al, 1973;Lin and McInnes, 1995). This is consistent with recent work showing that 77% of the water is carried by only 3% of the porosity defined as >0.5 mm pore diameter in some Vertisols (Lin et al, 1997).…”

Section: Hydropedological Formation Of Vertisolsmentioning

confidence: 99%

Hydropedological model of vertisol formation along the Gulf Coast Prairie land resource area of Texas

Nordt

Driese

2009

Hydrol. Earth Syst. Sci.

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Abstract. Vertisols are clayey soils containing slickensides and wedge-shaped aggregates formed by shrink-swell processes in seasonally wet climates. The dynamic distribution of macro-and microvoids as a by-product of this unique pedoturbation process, accompanied by microtopographic lows and highs (gilgai), mitigate our ability to make accurate and precise interpretations of aquic and hydric conditions in these problem soils. We studied Vertisols across a subhumid to humid climosequence to assess the formation of redoximorphic features on shallow, linear (nondepressional) landscape positions in response to varying levels of rainfall. Approximately 1000 mm of mean annual precipitation (MAP) is required to form soft iron masses that then increase in abundance, and to shallower depths, with increasing rainfall. Soft iron masses with diffuse boundaries become more abundant with higher rainfall in microlows, whereas masses with nondiffuse boundaries become more common in microhighs. Most soft iron masses form in oxygenated ped interiors as water first saturates and then reduces void walls where iron depletions form. In contrast, at least 1276 mm of MAP is needed to form iron pore linings in both microlow and microhigh topographic positions. Iron depletions do not correlate with rainfall in terms of abundance or depth of occurrence. The quantity of crayfish burrows co-varies with rainfall and first appears coincidentally with soft iron masses in microlows near 1000 mm of MAP; they do not appear until nearly 1400 mm of MAP in microhighs. Dithionite-citrate extractable and ammonium-oxalate extractable iron oxides increase systematically with rainfall indicating more frequent episodes of iron reduction and precipitation into pedogenic segregaCorrespondence to: L. C. Nordt (lee nordt@baylor.edu) tions. The sum of our data suggests that Vertisols forming in the Coast Prairie of Texas with MAP greater than 1276 mm should be classified as aquerts because of the presence of aquic conditions. These same soils may also meet the definition of hydric as one criterion for the identification of Federally-protected wetlands. However, there is a considerable disjunct between protracted periods of saturation and limited periods of reduction in these soils. Based on the distribution of redoximorphic features in the study area, regional water table data, and recent electrical resistivity data from a nearby upland Vertisol, non-Darcian bypass flow is the principle mechanism governing the flux of water through deep cracks where water first accumulates and then persists in microlow bowls at depths of 1 to 2 m.

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Water Recharge in a Soil with Shrinkage Cracks

Cited by 55 publications

References 0 publications

Vertical soil water movement in a tropical rainforest catchment in northeast queensland

Vertical soil water movement in a tropical rainforest catchment in northeast queensland

Development of a method for estimating the likelihood of crack flow in Canadian agricultural soils at the landscape scale

Hydropedological model of vertisol formation along the Gulf Coast Prairie land resource area of Texas

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