Correlation of physicochemical properties and sub-erosional landforms with aggregate stability variations in a tropical Ultisol disturbed by forestry operations

Chappell, Nick A.; Ternan, J. L.; Bidin, Kawi

doi:10.1016/s0167-1987(98)00196-2

Cited by 78 publications

(67 citation statements)

References 28 publications

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“…Within Alfisol soils of dry tropical Zimbabwe, Stocking (1981) observed that soil horizons with pipes have a higher ESP compared to nonpiped horizons. The study of Chappell et al (1999a) conducted within the humid tropics, demonstrated a similar relationship, with an ESP of 7Ð43% for the piped layer, compared to 2Ð58-4Ð14% for the layers higher in the profile.…”

Section: Local Increases In Erodibility Of Piped Stratamentioning

confidence: 72%

“…Alisol soils are associated with Acrisol soils but can be distinguished by cation exchange capacities exceeding 24 cmol C kg 1 clay (by 1 M NH 4 O Ac at pH 7). For example, the piped soils at Danum, East Malaysia (Table I) are classified as a Haplic Alisol (Chappell et al, 1999a). Globally, the Acrisol group is estimated to cover 1000 million hectares, while the Alisol group covers approximately 100 million hectares (Driessen et al, 2001).…”

Section: Reported Incidence Of Soil Piping In Humid Tropical Soilsmentioning

confidence: 99%

“…Such data are extremely limited for piped soils in the humid tropics. A small number of aggregate stability tests were, however, undertaken on a soil layer with active piping and on adjacent layers at one location in the Danum area (Chappell et al, 1999a). The piped layer at 0Ð94-m depth (in a profile surveyed by Bidin, 1995; Figure 5b) had a lower aggregate stability (i.e.…”

Section: Local Increases In Erodibility Of Piped Stratamentioning

confidence: 99%

“…2. As the resistance to flow within a large soil pipe is considerably less than the resistance to flow expected through the matrix (or even fine macropores) of the silt loam soil (Chappell et al, 1999a), the slower response is more likely to relate to the mechanism of recharge of the W3 pipe. The W3 pipe basin has an elongated headwater area, which extents to more than 60-m upslope of the pipe outlet (see Figure 2 in Sayer et al, 2006).…”

Section: Comparison Of Soil Pipe Outlet and Stream Time Constants Witmentioning

confidence: 99%

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Soil pipe distribution and hydrological functioning within the humid tropics: a synthesis

Chappell

2010

Hydrological Processes

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Abstract:Some of the most responsive runoff systems in the world are found within the humid tropics. These runoff responses are likely to be affected by the presence of natural pipes within the soil. This study provides a synthesis of the hydrological aspects of these phenomena within the humid tropics. Of the studies reporting the presence of soil piping within the humid tropics, most are associated with Ultisol soils, and, locally, most pipe outlets are observed on the lower sections of hillslopes. While the drainage role of pipes has been observed (providing faster and slower components of stream hydrographs), the mechanism of their recharge remains less clear. In part, this is because their spatial extent is poorly mapped within the hillslopes of the humid tropics. Further studies quantifying the length and recharge of soil pipe networks within the humid tropics are needed.

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Section: Local Increases In Erodibility Of Piped Stratamentioning

confidence: 72%

Section: Reported Incidence Of Soil Piping In Humid Tropical Soilsmentioning

confidence: 99%

Section: Local Increases In Erodibility Of Piped Stratamentioning

confidence: 99%

Section: Comparison Of Soil Pipe Outlet and Stream Time Constants Witmentioning

confidence: 99%

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Soil pipe distribution and hydrological functioning within the humid tropics: a synthesis

Chappell

2010

Hydrological Processes

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“…If expansive clays are present, these minerals will swell in the presence of water, and will shrink in dry conditions. Repeated shrink-swell cycles may destroy the clay aggregation and lead to further erosion (Chappell et al, 1999;Emami & Ghazavi, 2002;Bronick & Lal, 2004). Further, in dry conditions, clay can shrink, producing internal cracks which may facilitate tunnel or piping erosion.…”

Section: Porosity Hydraulic Conductivity Swelling and Erodibility Fmentioning

confidence: 99%

Erosion Related Changes to Physicochemical Properties of Ultisols Distributed on Calcareous

Nandi¹,

Luffman²

2012

JSD

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Water induced soil erosion, relating to improper land management, is a serious land degradation problem in Ultisols that results in rill and gully erosion. The extent of land degradation depends largely on the severity of erosion, which modifies the soil's physical and chemical properties. A detailed understanding of eroded soil properties is essential for assessment of future land management and soil-water conservation. The aim of this research is to evaluate the changes in physico-chemical and mineralogical properties of ultisols associated with gully erosion in East Tennessee. The study area is located in the southern Appalachian Valley and Ridge province, where a thick sequence of red colored clay rich soil (soil series is the Collegedale-Etowah complex) is found on dolomite and limestone bedrock. Four one-meter long soil cores and fifty-two bulk samples were collected from sites of active gully erosion (two cores) and from adjacent non-gullied soil (two cores). The physico-chemical properties assessed for each sample included clay mineralogy using X-ray diffraction (XRD), scanning electron microscopy (SEM) with energy-dispersive X-ray (EDX) methods, pH, cation exchange capacity (CEC), nitrogen, potassium, and phosphorus, particle size distribution (PSD), Atterburg limits, bulk density, moisture content, porosity, saturated hydraulic conductivity (Ks), soil erodibility factor, and swelling potential. According to the USDA, soil texture was classified as silty clay loam and silty clay. Significant differences (p<0.05) existed between eroding and non-eroding soils for the following factors: clay and silt content; porosity Ks, K; Atterberg limits, and swelling potential. Statistically significant correlations were established between clay content and Atterberg limits, bulk density, Ks, and swelling potential. Furthermore, results of X-ray diffraction indicated the presence of quartz, chlorite, illite, kaolinite, kaolinite -smectite expansive clay, hematite and ferrihydrite. Relic crystals of calcite were found in the saprolite horizon. Overall result indicated that selected physico-chemical properties can be used as an indicator of gully erosion in southern Appalachian Ultisols.

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Spatial and temporal variation in two rainfall simulators: implications for spatially explicit rainfall simulation experiments

Lascelles

Favis‐Mortlock

Parsons

et al. 2000

Earth Surf. Process. Landforms

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Rainfall simulators are widely used yet there is little evidence in the literature to show that their spatial and temporal variability has been adequately taken into account. For experiments that are concerned only with some aggregate or mean effect of simulated rain then such variations may be unimportant. However, where rainfall simulation is being used to study (and perhaps model) small-scale processes that are themselves spatially variable (such as rill initiation) then knowledge of the simulator's inherent variability is vital. A first aim of this paper is therefore to examine this variability, and to appraise methodologies by which it may be quantified. A second aim is to evaluate the implications for spatially explicit rainfall simulation experiments.Two simulators were used, a portable drip-screen simulator and a laboratory-based full-cone nozzle simulator. Neither produced a spatially uniform distribution of rainfall depth: both produced distributional patterns that were fairly consistent despite varying intensities and run times. Small-scale, apparently random variations were superimposed on these more deterministic patterns. However, despite this marked spatial variability, calculation of uniformity coefficients (1ÀSD/mean) resulted in high values. Thus it appears that the uniformity coefficient gives little real indication of the spatial uniformity of simulated rainfall, despite its established usage in the literature. Additionally, spatial distributions of raindrop size ±and hence kinetic energy ±were calculated for the full-cone nozzle simulator. These show that zones of high rainfall amount do not necessarily relate to zones of high energy reaching the surface.The presence of such variability raises a number of issues for spatially explicit rainfall simulation experiments. While there has been little work on the spatial variability of natural rainfall at field scale and smaller, it appears that the spatial heterogeneity of simulated rainfall depths observed in this study does not differ greatly from that of natural rain. But since a major attraction of rainfall simulation experiments is additional control over rainfall's many variables, the spatial non-uniformity of depth observed in this study is unwelcome. The existence of an apparently deterministic component to this non-uniformity nonetheless suggests that it can, at least in principle, be corrected by calibration. Less easily handled is the discrepancy between spatial distributions of rainfall depth and energy, since this will certainly affect rainfall simulation experiments that are, for example, concerned with erosion processes due to raindrop impact.

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Correlation of physicochemical properties and sub-erosional landforms with aggregate stability variations in a tropical Ultisol disturbed by forestry operations

Cited by 78 publications

References 28 publications

Soil pipe distribution and hydrological functioning within the humid tropics: a synthesis

Soil pipe distribution and hydrological functioning within the humid tropics: a synthesis

Erosion Related Changes to Physicochemical Properties of Ultisols Distributed on Calcareous

Spatial and temporal variation in two rainfall simulators: implications for spatially explicit rainfall simulation experiments

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