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Soil structure describes the arrangement of the solid parts of the soil and of the pore space located between them. It is determined by how individual soil granules clump, bind together, and aggregate, resulting in the arrangement of soil pores between them. Soil structure has a major influence on water and air movement, biological activity, root growth and seedling emergence.

Contents

OverviewEdit

Soil structure describes the arrangement of the solid parts of the soil and of the pore spaces located between them (Marshall & Holmes, 1979).[1] Aggregation is the result of the interaction of soil particles through rearrangement, flocculation and cementation. It is enhanced by:[1][2] the precipitation of oxides, hydroxides, carbonates and silicates; the products of biological activity (such as biofilms, fungal hyphae and glycoproteins); ionic bridging between negatively charged particles (both clay minerals and organic compounds) by multivalent cations; and interactions between organic compounds (hydrogen bonding and hydrophobic bonding).

The quality of soil structure will decline under most forms of cultivation—the associated mechanical mixing of the soil compacts and shears aggregates and fills pore spaces; it also exposes organic matter to a greater rate of decay and oxidation In the form of pudia

(Young & Young, 2001). A further consequence of continued cultivation and traffic is the development of compacted, impermeable layers or pans within the profile.

The decline of soil structure under irrigation is usually related to the breakdown of aggregates and dispersion of clay material as a result of rapid wetting. This is particularly so if soils are sodic; that is, having a high exchangeable sodium percentage (ESP) of the cations attached to the clays. High sodium levels (compared to high calcium levels) cause particles to repel one another when wet, and the associated aggregates to disaggregate and disperse. The ESP will increase if irrigation causes salty water (even of low concentration) to gain access to the soil.

A wide range of practices are undertaken to preserve and improve soil structure. For example, the NSW Department of Land and Water Conservation, (1991) advocates: increasing organic content by incorporating pasture phases into cropping rotations; reducing or eliminating tillage and cultivation in cropping and pasture activities; avoiding soil disturbance during periods of excessive dry or wet when soils may accordingly tend to shatter or smear; and ensuring sufficient ground cover to protect the soil from raindrop impact. In irrigated agriculture, it may be recommended to: apply gypsum (calcium sulfate) to displace sodium cations with calcium and so reduce ESP or sodicity, avoid rapid wetting, and avoid disturbing soils when too wet or dry.

Impacts of improving soil structureEdit

The benefits of improving soil structure for the growth of plants, particularly in an agricultural setting include: reduced erosion due to greater soil aggregate strength and decreased overland flow; improved root penetration and access to soil moisture and nutrients; improved emergence of seedlings due to reduced crusting of the surface; and greater water infiltration, retention and availability due to improved porosity.

It has been estimated that productivity from irrigated perennial horticulture could be increased by two to three times the present level by improving soil structure, because of the resulting access by plants to available soil water and nutrients (Cockroft & Olsson, 2000, cited in Land and Water Australia 2007). The NSW Department of Land and Water Conservation (1991) suggests that in cropping systems, wheat yields can be increased by 10 kg/ha for every extra millimetre of rain that is able to infiltrate due to soil structure .

Hardsetting soilEdit

Hardsetting soils lose their structure when wet and then set hard as they dry out to form a structureless mass that is very difficult to cultivate. They can only be tilled when their moisture content is within a limited range. When they are tilled the result is often a very cloddy surface (poor tilth). As they dry out the high soil strength often restricts seedling and root growth. Infiltration rates are low and runoff of rain and irrigation limits the productivity of many hardsetting soils.[3]

DefinitionEdit

Hardsetting has been defined this way: "A hardsetting soil is one that sets to an almost homogeneous mass on drying. It may have occasional cracks, typically at a spacing of >0.1 m. Air dry hardset soil is hard and brittle, and it is not possible to push a forefinger into the profile face. Typically, it has a tensile strength of 90 kN m<sup>–2</sup>. Soils that crust are not necessarily hardsetting since a hardsetting horizon is thicker than a crust. (In cultivated soils the thickness of the hardsetting horizon is frequently equal to or greater than that of the cultivated layer.) Hardsetting soil is not permanently cemented and is soft when wet. The clods in a hardsetting horizon that has been cultivated will partially or totally disintegrate upon wetting. If the soil has been sufficiently wetted, it will revert to its hardset state on drying. This can happen after flood irrigation or a single intense rainfall event."[4]

See alsoEdit

ReferencesEdit

  This article incorporates public domain material from the United States Government document "http://www.nrcs.usda.gov/wps/portal/nrcs/detail/soils/ref/?cid=nrcs142p2_054253".

  1. ^ a b Dexter, A.R. (June 1988). "Advances in characterization of soil structure". Soil and Tillage Research. 11 (3-4): 199–238. doi:10.1016/0167-1987(88)90002-5. 
  2. ^ Masoom, Hussain; Courtier-Murias, Denis; Farooq, Hashim; Soong, Ronald; Kelleher, Brian P.; Zhang, Chao; Maas, Werner E.; Fey, Michael; Kumar, Rajeev; Monette, Martine; Stronks, Henry J.; Simpson, Myrna J.; Simpson, André J. (16 February 2016). "Soil Organic Matter in Its Native State: Unravelling the Most Complex Biomaterial on Earth". Environmental Science & Technology. 50 (4): 1670–1680. doi:10.1021/acs.est.5b03410. 
  3. ^ Daniells, Ian G. (2012). "Hardsetting soils: a review". Soil Research. 50 (5): 349–359. doi:10.1071/SR11102. 
  4. ^ Mullins, CE (1997). "Hardsetting". In R Lal; WH Blum; C Valentin; BA Stewart. Methods for assessment of soil degradation. Boca Raton, FL: CRC Press. p. 121. ISBN 9780849374432. Retrieved 18 August 2016. 
  • Cockroft, B & Olsson, KA 2000, Degradation of soil structure due to coalescence of aggregates in no-till, no-traffic beds in irrigated crops,
  • Australian Journal of Soil Research, 38(1) 61 – 70. Cited in: Land and Water Australia 2007, ways to improve soil structure and improve the productivity of irrigated agriculture, viewed May 2007, <http://www.npsi.gov.au/>
  • Department of Land and Water Conservation 1991, "Field indicators of soil structure decline", viewed May 2007
  • Leeper, GW & Uren, NC 1993, 5th edn, Soil science, an introduction, Melbourne University Press, Melbourne
  • Marshall, TJ & Holmes JW, 1979, Soil Physics, Cambridge University Press
  • Soil Survey Division Staff (1993). "Examination and Description of Soils". Handbook 18. Soil survey manual. Soil Conservation Service. U.S. Department of Agriculture. Retrieved 2006-04-11. 
  • Young, A & Young R 2001, Soils in the Australian landscape, Oxford University Press, Melbourne.
  • Charman, PEV & Murphy, BW 1998, 5th edn, Soils, their properties and management, Oxford University Press, Melbourne
  • Firuziaan, M. and Estorff, O., (2002), "Simulation of the Dynamic Behavior of Bedding-Foundation-Soil in the Time Domain", Springer Verlag.

External linksEdit

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Types of soil structure

Prismatic, Platy, Columnar, Blocky and Spheroidal.