versión On-line ISSN 0718-2791
R.C. Suelo Nutr. Veg. v.8 n.1 Temuco 2008
R.C. Suelo Nutr. Veg. 8 (1) 2008 (1-13) J. Soil Sc. Plant Nutr. 8 (1) 2008 (1-13)
EFFECT OF BULK DENSITY ON HYDRAULIC PROPERTIES OF HOMOGENIZED AND STRUCTURED SOILS
Efecto de la densidad aparente sobre las propiedades hidráulicas de los suelos homogenizados y estructurados
1 Instituto de Ingeniería Agraria y Suelos, Universidad Austral de Chile, Casilla 567, Valdivia, Chile.
In order to determine the effect of bulk density and soil structure on their hydraulic behaviour, undisturbed samples were collected and disturbed samples were prepared from a Luvisol. The experimental field, located in Harste/Goettingen, Germany, was cultivated with sugar beet (Beta vulgaris). The water retention curve (WRC) and saturated hydraulic conductivity (Ks) were measured on undisturbed samples and homogenized samples prepared at different bulk densities (1.2 -1.4 and 1.6 Mg m-3). To determine the effect of soil shrinkage on the unsaturated hydraulic conductivity (k/Ψ) ,the vertical deformation of the repacked samples was measured and relative water content differences (dθ)were determined. The hydraulic properties of soils with identical texture depend on bulk density (dB) and structure. The increasing bulk density not only induces changes in the pore-size distribution but also affects the ability of soil to shrink and to conduct water under unsaturated conditions. Greater shrinkage was observed for samples with lower dB as a consequence of reduction of coarse pores. The water content differences increase with decreasing bulk density, inducing an increasing error in the estimation of k/Ψ.
Keywords: Water retention curve, soil shrinkage, soil structure
Con el objetivo de determinar el efecto de la densidad aparente y estructura del suelo sobre su comportamiento hidráulico, muestras no disturbadas fueron recolectadas y muestras disturbadas fueron preparadas a partir de un Luvisol. El campo experimental, ubicado en Harste/Goettingen, Alemania, fue cultivado con remolacha (Beta vulgaris). La curva de retención de agua (WRC) y la conductividad hidráulica saturada (Ks) fue determinada en muestras no disturbadas de suelo y en muestras homogenizadas preparadas a distintas densidades aparentes (1.2 -1.4 y 1.6 Mg m-3). Para determinar el efecto de la contracción del suelo sobre la conductividad hidráulica no saturada (K/Ψ), se midió la deformación vertical de las muestras ensambladas y a partir de ello se determinó la diferencia en el contenido volumétrico de agua.
Palabras clave: Curva de retención de agua, contracción suelo, estructura suelo
Soil hydraulic properties like the retention capacity and hydraulic as well as gas conductivity have agronomical and ecological implications. Drainage, evaporation and water-uptake by roots are just few examples where the knowledge about the rate of water flow through the soil plays an important role (Plagge et al., 1990; Kutilek and Nielsen, 1994).
The relative proportion of the three phases (water, gas and solid) of the soil is influenced by properties like texture, structure, biological activity, weather and soil management (Hillel, 1998). In these terms the porous media can be characterized in their volume and function which is of great relevance to understand processes related to water, air and heat transport in soils (Oschner et al., 2001; Dorner and Horn, 2006).
Soil volumes are affected by mechanical stresses (e.g. tillage-induced soil compaction, Blackwell et al., 1986; Horn et al., 1991; Horn et al., 1995; Ball et al., 1997; McNabb et al., 2001) and internal forces (e.g. wetting and drying cycles, Peng and Horn, 2007; Bartoli et al, 2007). The magnitude of volume changes are controlled by the mechanical stability of the soil or by the level of the actual in comparison with previous internal stresses. The internal stresses in soils containing more than 12% of clay induce aggregate formation, which results firstly in a prismatic structure with a dominant vertical pore function orientation. Repeated swelling and shrinkage creates tensile and shear induced crack formation in blocky and thereafter in a subangular blocky structure (Horn and Smucker, 2005).
The effects of soil compaction on soil structure have been investigated by many authors (Blackwell et al., 1986; Horn et al., 1995; Ball et al., 1997; McNabb et al., 2001). It is also well known that soils are able to shrink and swell (Peng et al., 2006). However, with respect to the calculation of hydraulic properties, it is always assumed that soils behave like a rigid body. Soil shrinkage can be characterized by the shrinkage curve, which relates the volume changes as a function of the water content changes. The shrinkage curve generally presents a typical sigmoidal shape; with linear and curvilinear parts determining successive phases of shrinkage. Bronswijk (1990) defined these phases from the wet to the dry side as: structural shrinkage, normal shrinkage, residual shrinkage and zero shrinkage. These zones differ between each other from the relative proportion of water losses and volume decrease being both proportional in the normal shrinkage but not in structural and residual shrinkage, where the water losses exceeds volume decrease.
Soil structure is changing continuously due to external and internal forces affecting consequently soil porosity and its functions. In order to describe the hydraulic behaviour of structured and disturbed soils with different compaction level, the objectives of this work were to determine: (1) the effect of bulk density on the water retention curve, (2) soil shrinkage and (3) its consequences on the hydraulic conductivity.
MATERIALS AND METHODS
Soil material and management
The investigation was conducted on arable soils in a slightly undulating area in Northern Germany. The soil is described as Stagnic Luvisol (FAO, 1998) derived from Loess with two tillage treatments: Conservation (Mulch-M) and Conventional (Plough-P). Mulch defines the treatment when the soil is loosened with a field cultivator to a depth of 8-10 cm, while Plough means ploughing and complete converting down to 30 cm depth. Before 1992 the whole field was uniformly ploughed to 30 cm depth. At the sampling time the soil was cultivated with sugar beet (Beta vulgaris). Some physical properties of the studied soils are shown in Table 1.
Collection of undisturbed soil samples
The soil sampling . took place in November 2003, directly after sugar beet harvesting. Undisturbed soil samples were taken at a depth of 15-19 cm in metal cylinders with 6 replications. Afterwards, the soil samples were put into plastic bags and boxes to avoid evaporation and mechanical disturbances.
Preparation of repacked soil samples by three bulk densities
In addition, from the sieved soil (<2 mm) repacked soil samples with three different bulk densities (dB) were prepared: 1.2, 1.4 and 1.6 Mg m-3 (ten replications for each bulk density prepared with 20% gravimetric water content). To ensure uniform bulk densities, the soil was packed into cylinders at carefully controlled densities by means of a "Load frame" device.
In order to determine the effect of bulk density on hydraulic properties four samples were used to measure the water retention curve (WRC) and shrinkage (S), and six to measure the saturated hydraulic conductivity (Ks). First all samples were slowly saturated by capillary rise from beneath. The saturation took at least three days.
Determination of the water retention curve and soil shrinkage
The water retention curve (WRC) was determined at 8 different water suctions. The saturated samples were drained at-10, -20 and -30 hPa on sand tanks. The drainage of the samples at water tensions of -60, -150, -300, -500 hPa occurred on ceramic plates and of -15000 hPa in a pressure chamber. When the samples attained equilibrium with the applied vacuum, the gravimetric water content was determined. At the end, samples were dried in an oven at 105 °C for 16 hours (Hartge and Horn, 1989) to determine and to control the bulk density and volumetric water content. To determine the total porosity, a particle density of 2.63 Mg m-3 was used resulting from the dominant quartz.
The shrinkage of the repacked samples was measured during the determination of the WRC. To estimate the vertical shrinkage of the soil their actual height was measured with a calliper at 6 defined points (1 on the middle and 5 on the sides) as was proposed by Peng and Horn (2005).
Determination of the saturated hydraulic conductivity
The saturated hydraulic conductivity (Ks) was measured with a permeameter under instationary conditions. The water flow was measured three times for each soil sample and the arithmetical mean was calculated. The Ks values were log-transformed because oftheir non-normal distribution (Hartge and Horn, 1989).
Correction of the water retention curve after shrinkage
In order to consider the shrinkage effect on the water retention curve, the vertical shrinkage was used to correct the volumetric water content at each matric potential. Additionally, the structural changes caused by shrinkage were expressed by differences in water content (dθ) with and without consideration of shrinkage, in relation to the volumetric water content at saturation as follows:
where Φrs means the volumetric water content of rigid soil [vol%],Φdt is the volumetric water content corrected by shrinkage [vol%] and Φs is the volumetric water content at saturation [vol%].
At the used water tensions (till -500 hPa) horizontal cracks were not clearly observed in the investigated soils. Additionally, regarding the complicated and irregular geometry of soil cracks, the quantitative and feasible measurement of horizontal shrinkage is more difficult as of the vertical (Peng et al., 2006). Therefore, our investigations were concentrated only on the vertical changes. Such restriction can be justified by the initial dominance of vertical cracks during shrinkage, as it is described in Hartge and Horn (1999). In order to show the effect of the bulk density and soil shrinkage on the water movement under unsaturated conditions, the hydraulic conductivity as function of the water tension was estimated using the equation (2) proposed by van Genuchten (1980), with and without consideration of the soil deformation as follows:
where K/Ψ means the unsaturated hydraulic conductivity [cm s-1], h is the water pressure [hPa], Ks is the saturated hydraulic conductivity [cm s-1] and a, n, m are the van Genuchten parameter of the WRC [-].
Averages for each soil horizon were calculated. In order to proof the effect of bulk density and structure formation on pore-size distribution and Ks, statistical analysis was performed by analysis of variance (p≤0.05). The differences of means were assessed by the Tukey-Test (p≤0.05).
Effect of the bulk density on the water retention curve and soil shrinkage
The development of the WRC depends on the soil density as well as on soil structure (Fig.1) . As expected, the saturated water content (8s) decreases with increasing bulk density (Tab. 2). The development of the WRC for the structured samples (Ps and Ms) differs from that of the homogenized material (Ph and Mh), even if they have a nearly similar water content at saturation. It is noticeable that the undisturbed soil samples (both for P and M) start to loose water at higher pF-values (pF 1,78) than the disturbed ones. Those differences can be seen especially in the amount of medium pores (MP).
The shrinkage curves show the relation between water content and soil volume changes (Fig.2). Generally, the void ratio (e) and the moisture ratio (-0) at saturation decrease with increasing dB. Additionally, with increasing dB the shrinkage curves become shorter and smoother. The residual shrinkage predominates in all investigated samples, i.e. volume decrease is lower than water losses, which can be explained by high bulk density and the used water tension (till -500 hPa).
Although the soil does not present a great shrinkage at the applied water tensions (Fig. 2) some structural changes due to water menisci formation take place. These changes can be evaluated through the relative water content difference (d8), understood as the difference between the volumetric water content with and without consideration of the shrinkage in relation to the volumetric water content at saturation (Fig. 3). The dashed line represents the situation for the soil assumed as a rigid body, when no changes in the volumetric water content due to shrinkage take place. As the bulk density decreases, a greater deviation of dθ from the dashed line is observed (it becomes more negative) showing that structural changes due to shrinkage become larger. By the lower dB, the greater deviation of d8 occurs near saturation (till -20 hPa), showing the greater error in the determination of the volumetric water content.
Effect of the bulk density on the hydraulic conductivity
The saturated hydraulic conductivity decreases with increasing bulk density as a response of the smaller volume of coarse pores in the disturbed samples (Table 2).
Ks for Ps and Ph (1.4) do not present statistically significant differences, but Ps has a greater bulk density, which normally coincides with a smaller Ks value. The same values for Ks can be explained by the higher continuity between soil aggregates of the undisturbed pore system at a given bulk density. The undisturbed samples collected from Mulch (Ms) present the same dB and wCP as shown for Mh (1.4). However, Ks of Ms is significant higher than Mh (1.4), showing the pore-continuity effect of the undisturbed material. In fact, Ms is comparable inKs with Mh (1.2) even considering the higher dB of Ms. As the soil drains, k/ψ curve decrease (Fig. 4). However, the intensity of these changes differs depending on the bulk density and pore-size distribution. Differences in k/ψ observed in Ph at pF=3.0 reach almost one order of magnitude depending on dB, while for Mh this situation was not observed as a result of the faster decrease of k/ψ at dB=1.4 than at 1.2 Mg m-3.
If the volumetric water content is corrected by soil shrinkage, the estimated values of unsaturated hydraulic conductivity increase (Fig. 5). Thus it can be seen that if the soil does not behave as a rigid body, errors in the estimation of the volumetric water content can be made, even in the residual shrinkage range. These discrepancies increase with decreasing bulk density (Fig.3) and have consequences on the estimation of the unsaturated hydraulic conductivity (Fig. 5).
Effect of soil structure on hydraulic properties
Since the soil texture between undisturbed and disturbed samples is identical, differences in the relation between pore volume and pore function are related to the bulk density and soil structure formation. The differences between pore size distributions (or WRCs) of homogenized (repacked) and undisturbed samples are the consequence of soil aggregation. If repacked and undisturbed soil samples collected in Mulch are compared, differences in the WRC at the same dB were assessed. Remarkable is the higher amount of medium pores in e.g. Ms than in Mh(1.4) which dominates in the conservation tillage persisting over longer periods. This differences tend to decrease (but are in some cases still significant) with increasing drainage, showing the increasing effect of textural pores. This latter effect was confirmed by measurements made by Tuli et al. (2005). Disturbed soil samples were only once wetted and dried and, consequently no real aggregation occurs. On the other hand, the structure of the undisturbed soil is a consequence of soil management and successive swelling-shrinkage processes. As Horn and Smucker (2005) suggested, the aggregate formation and strength depend on swelling and shrinking process and on biological activity and kinds of organic exudates as well as on the intensity, number and time of swelling and drying events. The greater differences observed between Mh and Ms are probably related to the conservation of soil structure avoiding the aggregate destruction. This implies, that the pore continuity under Mulch is not interrupted allowing a more intensive water transport. This can be confirmed by investigations made by Buczko et al. (2006), who observed higher hydraulically active macropores and higher macropore connectivity under conservation than conventional tillage treatment. Lower macropore connectivity in cultivated soils were amongst others described by Bodhinayake and Si (2004).
Tuli et al. (2005) investigated and compared hydraulic properties of undisturbed and disturbed (repacked) soil samples. With respect to the WRC, they found out that repacked soil samples present higher air-entry pressure values than the undisturbed ones, showing the lack of macropores in the disturbed samples. In our results, the volume of macropores (wCP) is the same for Ms and Mh (1.4) but higher for Ps than Ph (1.6). They measured also the air and water permeability. For both investigated properties, undisturbed soil samples showed higher values. This illustrates the contribution of more continuous macropores to water and air permeability for the undisturbed samples. In the same direction, Blackwell et al. (1986) mentioned that differences in permeability data between disturbed and undisturbed samples are mostly governed by soil structure and macroporosity. Generally, the amount of macropores, are responsible of the permeability of soil to water near saturation (Iversen et al., 2001). However, the continuity of these pores can not be neglected. The greater Ks for the undisturbed soil in M (Ms>Mh (1.4)) is influenced by the pore continuity reached during the aggregate formation, which does not take place in the disturbed material.
An increasing bulk density in the homogenized material implies a decrease of coarse pores and an increase in middle and fine pores. It is well known that this behaviour induces changes on hydraulic conductivity as assessed in structured soil by Ankeny et al. (1990), Fuentes et al. (2004), Horn and Smucker (2005). This phenomenon appears as a result of the reduction of structural pores (the large pores are reduced at first, as mentioned by Richard et al., 2001) and the destruction of pore continuity developed during aggregate formation. Saturated hydraulic conductivity for soils with different amount of macropores (and pore continuity) was also described by Cameira et al. (2003), Fuentes et al. (2004) and Buczko et al. (2006). They investigated different soil types under two tillage treatments and assessed lower Ks for conventional than conservation treatment responding to a lower soil aggregation (Six et al., 1999; Pinheiro et al., 2004) and higher disturbance of macropores continuity (Osunbitana et al., 2005). Improvement of pore continuity with increase of macropores was also noticed by Currie (1965) who investigated gas transport in highly developed natural aggregated soils. He pointed out that preferentially gas transport in soil profile occurs through the inter-aggregate pore system (more continuous than zones of aggregated or crumb pores) formed by macropores, being reduced in compacted soils. The same trends were also described by Fujikawa and Miyazaki (2005) for alluvial soils.
Effect of bulk density on shrinkage
Regarding the importance of water for all processes in soil, their hydraulic properties are often investigated and well understood if we assume a rigid pore system. Soils, however, are no rigid bodies which results in changes in their properties as a result of internal and external forces. If we want to understand the effect of shrinkage on hydraulic properties, measurements on disturbed and repacked soil samples can give a good insight in the effect of non rigidity on hydraulic functions. However, the possibility of extrapolation to in situ conditions can be rather restricted because of the exclusion of water uptake effects through roots on soil structure formation but at least it represents the seedbed conditions. Peng and Horn (2005) mentioned that soil homogenization due to repeat ploughing always results in an altered shrinkage pattern in comparison with the identical soil without any intermediate homogenization. The ability of soil to shrink decreases exponential with increasing dB, as far as the soil particle/aggregates get closer. Horn et al. (1991) showed that at a given dehydration stresses, less structured soils were easy to deform. If soils are compacted the amount of contact points between particles and soil strength increases (Hartge and Horn, 1999), which results in a reduced mobility of particles to rearrange (Hartge, 2000). Consequently, a more negative suction is needed to regain structural changes. As the soil drains the water menisci formation induce shrinkage affecting the volume of medium and fine pores (Peng and Horn, 2007) and the volumetric water content (Figure 3). The later is underestimated and consequently the simulation of k/Ψ with the van Genuchten is underrated as well. The underestimation depends on the rigidity of the pore system (determined by the cohesion between particles and the angle of the internal friction) and the applied water suction (or intensity of drainage).
1. Structural changes affect the porous media in their volume and fiinction. These changes get larger with decreasing bulk density.
2. Structural changes take place due to internal (shrinkage) and external forces (compaction) and affect the hydraulic behaviour of these soils.
3. The aggregation of the soil is more intense in undisturbed soil samples due to successive wetting and drying cycles prefer the creation of new pores.
4. The structural changes due to water loss can be represented by d8 Without consideration o dθ the values of k/Ψ can be underestimated.
ANKENY, M. D., T. C. KASPAR, R. HORTON. 1990. Characterization of tillage and traffic effects onunconfined infiltration measurements. Soil. Sci. Soc. Am. J. 54: 837-840. [ Links ]
BALL, B. C, D. J. CAMPBELL., J.T. DOUGLAS., J. K. HENSHALL, AND M. F. O'SULIVAN. 1997. Soil structural quality, compaction and land management. Eur. J. of Soil Sci. 48: 593-601. [ Links ]
BARTOLI, F., J. C. BEGIN, G. BURTIN AND E. SCHOULLER. 2007. Shrinkage of initially very wet soil block, cores and cods from a range of European Andosol horizons. Eur. J. of soil Sci. 58: 378-392. [ Links ]
BLACKWELL, P. S., J. P. GRAHAM, J. V. ARMSTRONG, M. A. WARD, K. R. HOWSE, C. J. DAWSON AND A. R. BUTLER. 1986. Compaction of a silt loam soil by wheeled agricultural vehicles. I. Effect upon soil conditions. Soil Tillage Res. 7: 97-116. [ Links ]
BODHINAYAKE, W. AND B. C. SI. 2004. Near -saturated surface soil hydraulic properties under different land uses in the St. Denis National Wildlife Area, Saskatchewan, Canada. Hydrol. Processes 18: 2835-2850. [ Links ]
BRONSWIJK, J. J. 1990. Shrinkage geometry of a heavy clay soil at various stresses. Soil. Sci. Soc. Am. J. 54: 1500-1502. [ Links ]
BUCZKO, U., O. BENS AND R. F. HÜTTL. 2006. Tillage effects on hydraulic properties and macroporosity in silty and sandy soils. Soil. Sci. Soc. Am. 170: 1998-2007. [ Links ]
CAMEIRA, M. R., R. M. FERNANDO AND L. S. PEREIRA. 2003. Soil macropore dynamics affected by tillage and irrigation for a silty loam alluvial soil in southern Portugal. Soil Tillage Res. 70: 131-140. [ Links ]
CURRIE, J. A. 1965. Diffusion within soil micro structure a structural parameter for soils. Soil Sci. 16: 278-289. [ Links ]
DÖRNER, J. AND HORN, R. 2006. Anisotropy of pore functions in structured Stagnic Luvisols in the Weichselien moraine region in N Germany. J. Plant. Nutr. Soil Sci. 169: 213-220. [ Links ]
FAO. 1998. World Reference Base for Soil Resources. World Soil Resources Report 84, Food and Agriculture Organization of the United Nations, Rome. [ Links ]
FUENTES, J. P., M. FLURRY AND D. F. BEZDICEK 2004. Hydraulic properties in a silt loam soil under natural prairie, conventional till, and no-till. Soil. Sci. Soc. Am. J. 68: 1679-1688. [ Links ]
FUJIKAWA, T., T. MIYAZAKI. 2005. Effect of bulk density and soil type on the gas diffusion coefficient in repacked and undisturbed soils. Sol Sci. 170 (11): 892-901. [ Links ]
Hartge, K. H. and R. Horn. 1989. Die physikalische Untersuchung von Boden. Stuttgart, Enke, 177 P. [ Links ]
HARTGE, K. H. AND R. HORN. 1999. Einführung in die Bodenphysik. Enke, Stuttgard, 304 S. [ Links ]
HARTGE, K. H. 2000. The effect of soil deformation on physical soil properties. A discourse on the common background. P. 32-43. In R. Horn et al. (ed) Subsoil compaction-distribution, processes and consequences. Catena Verlag. Reiskirchen, Germany. [ Links ]
HILLEL, D. 1998. Environmental Soil Physics. Academic Press, London, 771 P. [ Links ]
HORN, R., BAUMGARTL, TH., KÜHNER, M. UND KAYSER, R. 1991. Zur Bedeutung des Aggregierugsgrades für die Spanungsverteiligung in strukturierten Boden. Zeitschrift für Pflanzenernahrung und Bodenkunde 154: 21-26. [ Links ]
HORN, R., H. DOMZAL, A. S•OWI •SKA-JURKIEWICZ, C. VAN OUWERKERK. 1995. Soil compaction processes and their effects on the structure of arable soils and the environment. Soil & Till. Res. 35: 23-36. [ Links ]
HORN, R. AND A. SMUCKER. 2005. Structure formation and its consequences for gas and water transport inunsaturated arable and forest soils. Soil & Till. Res. 82: 5-14. [ Links ]
IVERSEN, B. V., P. MOLDRUP, P. SCHJØNNING, AND P. LOLL. 2001. Air and water permeability in differently textured soils at two measurement scales. Soil Sci. 166: 643-659. [ Links ]
KUTILEK, M AND D. R. NIELSEN. 1994. Soil hydrology. Catena Verlag, 38162 Cremlingen-Destedt, Germany. ISBN 3-923381-26-3. [ Links ]
MCNABB, D. H., A. D. STARTSEV, AND H. NGUYEN. 2001. Soil wetness and traffic effect levels on bulk density and air- field porosity of compacted boreal forest soils. Soil. Sci. Soc. Am. J. 65: 1238-1247. [ Links ]
OSCHNER, T. E., R. HORTON, AND T. REN. 2001. A new perspective on soil themal properties. Soil Sci. Soc. Amer. J. 65: 1641-1647. [ Links ]
OSUNBITANA, J. A., D.J. OYEDELEB AND K.O. ADEKALUA. 2005. Tillage effects on bulk density, hydraulic conductivity and strength of a loamy sand soil in southwestern Nigeria. Soil and Till. Research 82: 57-64. [ Links ]
PENG, X. AND HORN R. 2005. Modelling soil shrinkage curve across a wide range of soil types. Soil Sci. Soc. Amer. J. 69: 584-592. [ Links ]
PENG, X., HORN R., S. PETH AND A. SMUCKER. 2006. Quantification of soil shrinkage in 2D by digital image processing of soil surface. Soil and Till. Research. 91: 173-180. [ Links ]
PENG, X. AND HORN R. 2007. Anisotropic shrinkage and swelling of some organic and inorganic soils. Eur. J. Soil. Sci. 58: 98-107. [ Links ]
PINHEIRO, E. F. M, PEREIRA M. G.AND L. H. C. ANJOS. 2004. Aggregate distribution and soil organic matter under different tillage systems for vegetable crops in a Red Latosol from Brazil. Soil and Tillage Research. I: 79-84. [ Links ]
PLAGGE, R., RENGER, M. AND CHRISTIAN H. ROTH. 1990. A new laboratory method to quickly determine the unsaturated hydraulic conductivity of undisturbed soil cores within a wide range of textures. Zeitschrift für Pflanzenernähr. und Bodenk. 153: 39-45. [ Links ]
RICHARD, G., COUSIN, I., SILLON, J. F., BRUAND, A., GUERIF, J. 2001. Effect of compaction on the porosity of a silty soil: influence on unsaturated hydraulic properties. Eur. J. Soil Sci. 52: 49-58. [ Links ]
SIX. J., E.T. ELLIOTT AND K. PAUSTIAN. 1999. Aggregate and soil organic matter dynamics under conventional and no-tillage systems. Soil. Sci. Soc. Am. J. 63: 1350-1358. [ Links ]
TULI. A., J. W. HOPMANS, D. E. ROLSTON, AND PER MOLDRUP. 2005. Comparison of air and water permeability between disturbed and undisturbed soils. Soil Sci. Soc. Am. J. 69: 1361-1371. [ Links ]
VAN GENUCHTEN, M. TH. 1980. A closed - form equation for predicting the hydraulic conductivity of unsaturated soils. Soil Sci. Soc. Amer. J. 44: 892-898. [ Links ]