Cation-exchange capacity: Difference between revisions
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==CEC with Soil pH== |
==CEC with Soil pH== |
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[[File:EffectiveCECsoilpH.jpg|thumbnail|100px|Effective CEC with Soil pH]] |
[[File:EffectiveCECsoilpH.jpg|thumbnail|100px|Effective CEC with Soil pH]] |
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| ⚫ | Many soils' CEC is dependent upon the pH of the soil. As soil acidity increases (pH decreases), more H<sup>+</sup> ions are attached to the colloids and push other cations from the colloids and into the soil solution (CEC decreases). Inversely, when soils become more basic (pH increases), the available cations in solution decreases because there are fewer H<sup>+</sup> ions to push cations into the soil solution from the colloids (CEC increases).<ref>{{cite book|last=Havlin, Tisdale, Beaton, Nelson|title=Soil Fertility and Fertilizers|year=2011|publisher=PHI|location=New Delhi}}</ref> |
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Many soils' CEC is dependent upon the pH of the soil. This is due mostly to the [[lyotrophic]] series, which describes the relative strength of various cations' adsorption, and is generally as follows: |
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| ⚫ | As soil acidity increases (pH decreases), more H<sup>+</sup> ions are attached to the colloids and push other cations from the colloids and into the soil solution (CEC decreases). Inversely, when soils become more basic (pH increases), the available cations in solution decreases because there are fewer H<sup>+</sup> ions to push cations into the soil solution from the colloids (CEC increases).<ref>{{cite book|last=Havlin, Tisdale, Beaton, Nelson|title=Soil Fertility and Fertilizers|year=2011|publisher=PHI|location=New Delhi}}</ref> |
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*'''Factors affecting cation exchange''' |
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**1. Soil pH – determines how many exchange sites will be occupied by H+ rather than cations |
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**2. Cation concentration – low concentration will make it harder for plants to get cation nutrients |
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==CEC with Soil Depth== |
==CEC with Soil Depth== |
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Revision as of 02:20, 17 December 2013
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In soil science, cation-exchange capacity (CEC) is the maximum quantity of total cations, of any class, that a soil is capable of holding, at a given pH value, available for exchange with the soil solution. CEC is used as a measure of fertility, nutrient retention capacity, and the capacity to protect groundwater from cation contamination. It is expressed as milliequivalent of hydrogen per 100 g of dry soil(meq+/100g), or the SI unit centi-mol per kg (cmol+/kg). The numeric expression is coincident in both units.
Clay and humus have electrostatic surface charges that attract the solution ions, and hold them. This holding capacity varies for the different clay types and clay-blends present in soil, and is very dependent of the proportion of clay+humus that is present in a particular soil. One way to increase CEC is to favor the formation of humus.
In general, the higher the CEC, the higher the soil fertility.
Calculation of CEC
The CEC is the number of positive charges that a soil can contain. It is usually described as the amount of equivalents necessary to fill the soil capacity. In soil science, an equivalent is defined by the number of charges in terms of a given number of hydrogen ions. As hydrogen ions have only one positive charge (H+), this makes calculations relatively simple. An equivalent of Al3+ would have one third as many ions for the same amount of charges, and Ca2+ would have half as many ions.
Translation from meq/100g to an every day unit, like lb/acre of available nutrients, can be made via calculation, that considers the atomic weight, the ion's valence, and by estimating the soil depth and its density. Mengel gives the following correspondence for 1 meq/100g:[1]
Calcium, 400 lb/acre
Magnesium, 240 lb/acre
Potassium, 780 lb/acre
Ammonium, 360 lb/acre
Base saturation
Closely related to cation-exchange capacity is the base saturation,[2] which is the fraction of exchangeable cations that are base cations (Ca, Mg, K and Na). It can be expressed as a percentage, and called percent base saturation. The higher the amount of exchangeable base cations, the more acidity can be neutralised in the short time perspective. Thus, a soil with high cation-exchange capacity takes longer time to acidify (as well as to recover from an acidified status) than a soil with a low cation-exchange capacity (assuming similar base saturations).
The base-cation saturation ratio (BCSR) is a method of interpreting soil test results that is widely used in sustainable agriculture, supported by the National Sustainable Agriculture Information Service (ATTRA)[3] and claimed to be successfully in use on over a million acres (4,000 km²) of farmland worldwide.
CEC of Mineral Soils
Many heavily weathered or oxidized soils, especially in the wet tropics, have a high concentration of Al+3. Since aluminium is toxic in high quantities for most plants, there are certain advantages and disadvantages to this. For one, due to the relatively high adsorption rate of aluminium to soil colloids, it is taken out of the soil and the plant cannot use it. On the other hand, because it has 3 positive charges, it takes up a large amount of charge in a CEC. For example, Al+3 fills the same space as three NH4+ ions. This makes many aluminium heavy soils relatively infertile. There is no easy way to remove Al ions from the soil colloid and free the CEC for other ions.
CEC of Organic Matter
Organic materials in soil increase the CEC through an increase in available negative charges. As such, organic matter build-up in soil usually positively impacts soil fertility. However, organic matter CEC is heavily impacted by soil acidity as acidity causes many organic compounds to release ions to the soil solution.
CEC with Soil pH
Many soils' CEC is dependent upon the pH of the soil. As soil acidity increases (pH decreases), more H+ ions are attached to the colloids and push other cations from the colloids and into the soil solution (CEC decreases). Inversely, when soils become more basic (pH increases), the available cations in solution decreases because there are fewer H+ ions to push cations into the soil solution from the colloids (CEC increases).[4]
- Factors affecting cation exchange
- 1. Soil pH – determines how many exchange sites will be occupied by H+ rather than cations
- 2. Cation concentration – low concentration will make it harder for plants to get cation nutrients
- 3. Strength of adsorption of cations on colloids- this is due mostly to the lyotrophic series: Al3+ > H+ > Ca2+ > Mg2+ > K+ = NH4+ > Na+
CEC with Soil Depth
Anion exchange capacity
Similar to the CEC, the anion exchange capacity is a measurement of the positive charges in soils affecting the amount of negative charges which a soil can adsorb. There are relatively few anions that are restrictive in agriculture, but they are important, such as sulfur or phosphorus. The anion lyotrophic series is:
H2PO4- > SO4-2 > NO3- > Cl-
In contrast to CEC, AEC generally will increase when pH drops and decrease when pH rises.
Laboratory determination
There are two standardised International Soil Reference and Information Centre methods for determining CEC:
- extraction with ammonium acetate; and
- the silver-thiourea method (one-step centrifugal extraction).
There exist slightly conflicting ideas on which mechanisms to include in the term, "cation exchange", in soil chemistry. From a theoretical point of view, one should distinguish cation exchange from ligand exchange, and exchange of diffuse layer adsorbed cations. On the other hand, from a practical point of view, e.g. in forest and agricultural management, what is important is the soils' ability to replace one cation with another rather than the exact mechanism by which this replacement occurs. What is included in the term, "cation exchange", in soil science thus varies with the scientific context.
Standard values
| Kaolinite | 3-15 |
| Halloysite 2H2O | 5-10 |
| Halloysite 4H2O | 40-50 |
| Montmorillonite-group | 70-100 |
| Illite | 10-40 |
| Vermiculite | 100-150 |
| Chlorite | 10-40 |
| Glauconite | 11-20+ |
| Palygorskite-group | 20-30 |
| Allophane | ~70 |
These are the values reported by Carroll (1959)[5] for the cation-exchange capacity of minerals in meq./100g at pH of 7.
See also
References
- ^ Mengel, David D., Department of Agronomy, Purdue University. "Fundamentals of Soil Cation Exchange Capacity". Retrieved 2011-05-03.
{{cite web}}: CS1 maint: multiple names: authors list (link) - ^ Turner, R.C. and Clark J.S., 1966, Lime potential in acid clay and soil suspensions. Trans. Comm. II & IV Int. Soc. Soil Science, pp. 208-215
- ^ NCat Soil Management
- ^ Havlin, Tisdale, Beaton, Nelson (2011). Soil Fertility and Fertilizers. New Delhi: PHI.
{{cite book}}: CS1 maint: multiple names: authors list (link) - ^ Carroll, Dorothy (1959). "Ion exchange in clays and other minerals". Geological Society of America Bulletin. 70 (6): 749‐780. doi:10.1130/0016-7606(1959)70[749:IEICAO]2.0.CO;2.
- ISRIC (International Soil and Reference Information Centre)
- Robert Lippert, Clemson University Extension Service
- David B. Mengel, Department of Agronomy, Purdue University
- "One Hundred Harvests Research Branch Agriculture Canada 1886-1986". Historical series / Agriculture Canada - Série historique / Agriculture Canada. Government of Canada
- "A study of the Lime Potential, R. C. Turner, Research Branch, Canadian Department of Agriculture, 1965