Cation exchange capacity (CEC) is a measure of the soil’s ability to hold positively charged ions. It is a very important soil property influencing soil structure stability, nutrient availability, soil pH and the soil’s reaction to fertilisers and other ameliorants.
The clay mineral and organic matter components of soil have negatively charged sites on their surfaces which adsorb and hold positively charged ions (cations) by electrostatic force. This electrical charge is critical to the supply of nutrients to plants because many nutrients exist as cations (e.g. magnesium, potassium and calcium). In general terms, soils with large quantities of negative charge are more fertile because they retain more cations (McKenzie et al. 2004) however, productive crops and pastures can be grown on low CEC soils.
The main ions associated with CEC in soils are the exchangeable cations calcium (Ca2+), magnesium (Mg2+), sodium (Na+) and potassium (K+) (Rayment and Higginson 1992), and are generally referred to as the base cations. In most cases, summing the analysed base cations gives an adequate measure of CEC (‘CEC by bases’). However, as soils become more acidic these cations are replaced by hydrogen (H+), aluminium (Al3+) and manganese (Mn2+), and common methods will produce CEC values much higher than what occurs in the field (McKenzie et al. 2004). This ‘exchange acidity’ needs to be included when summing the base cations and this measurement is referred to as effective CEC (ECEC).
Different laboratories use various methods to measure CEC, and can return contrasting results depending on the fraction of the soil measured. In Australia, some laboratories measure CEC directly and others calculate it as CEC by bases. CEC is commonly measured on the fine earth fraction (soil particles less than 2 mm in size).
Measuring CEC involves washing the soil to remove excess salts and using an ‘index ion’ to determine the total positive charge in relation to original soil mass. This involves bringing the soil to a predetermined pH before analysis. Methods, including pre-treatment, for measuring CEC and exchangeable cations are presented by Rengasamy and Churchman (1999) and described in detail by Rayment and Higginson (1992).
CEC is conventionally expressed in meq/100 g (Rengasamy and Churchman 1999) which is numerically equal to centimoles of charge per kilogram of exchanger (cmol(+)/kg).
The CEC of soils varies according the clay %, the type of clay, soil pH and amount of organic matter. Pure sand has a very low CEC, less than 2 meq/100 g, and the CEC of the sand and silt size fractions (2 µm/2 mm) of most soils is negligible.
Clay has a great capacity to attract and hold cations because of its chemical structure. However, the different clay types occurring in Tasmanian soil have different CECs (table 1). It is highest in montmorillonite clay, found in black soils. It is lowest in heavily weathered kaolinite clay, found in Ferrosols and slightly higher in the less weathered illite clay. Humus, the end product of decomposed organic matter, has the highest CEC value because organic matter colloids have a large surface area and large quantities of negative charges. Humus has a CEC two to five times greater than montmorillonite clay and up to 30 times greater than kaolinite clay, so is very important in improving soil fertility. A higher CEC usually indicates more clay and organic matter is present in the soil and so high CEC soils generally have greater water holding capacity than low CEC soils.
Table 1: Cation exchange capacity of different soil particles.
100 – 300
Smectites (black swelling clays
60 – 150
Kaolinite (white potters clay)
2 – 15
Iron and aluminium oxides (from Ferrosols)
Source: McLaren and Cameron (1996)
A CEC above 10 meq/100g is preferred for plant production (Table 2). The five exchangeable cations are also shown in soil test results as percentages of CEC. The desirable ranges are: calcium 65 – 80% of CEC, magnesium 10 – 15%, potassium 1 – 5%, sodium 0 – 1% and aluminium 0%.
Table 2: Management implications of soil CEC.
Soils prone to leaching and nutrient loss; maintaining organic matter is essential. Low water holding capacity.
10 – 15
Typical range for loams. Moderate nutrient and water holding capacity.
Typical of heavy clay soils and organic peats. High nutrient status soils and high water holding capacity.
Soils dominated by clays with variable surface charge are typically strongly weathered. The fertility of these soils decreases with decreasing pH which can be induced by acidifying nitrogen fertiliser, nitrate leaching and by clearing and agricultural practices (McKenzie et al. 2004). Soil pH change can also be caused by natural processes such as decomposition of organic matter and leaching of cations. The lower the CEC of a soil, the faster the soil pH will decrease with time. Liming soils (see Soil Acidity fact sheet.) to higher than pH 5 (CaCl2) will maintain exchangeable plant nutrient cations.
Soils with a low CEC are more likely to develop deficiencies in potassium (K+), magnesium (Mg2+) and other cations while high CEC soils are less susceptible to leaching of these cations (CUCE 2007). Several factors may restrict the release of nutrients to plants. Some groups promote the controversial idea of managing cation ratios, claiming ideal ratios for Ca:Mg or Ca:K. For plant nutrition, a more critical factor is whether the net amount of Ca or K in the soil is adequate for plant growth. The addition of organic matter will increase the CEC of a soil but requires many years to take effect.
Figure 1 illustrates how CEC can change with depth. The sum of the base cations provides an estimate of the CEC of each soil layer. The surface 10 cm has a CEC of 4.6 meq/100 g because of a high organic content. At 10 – 30 cm depth, the organic content of the sand is very low, hence the low CEC. The CEC of the subsoil layers are governed by clay content, 61 %, 51 % and 34 % respectively. The dominant clay in this soil is kaolinite so CEC values remain low.
Figure 1: Sandy duplex soil, with clay at 40 cm. Note the high CEC of the clay below 40 cm, and the impact of organic matter on the sand’s CEC.
Cornell University Cooperative Extension (CUCE) (2007) Cation Exchange Capacity (CEC). Agronomy Fact Sheet Series # 22. Department of Crop and Soil Sciences, College of Agriculture and Life Sciences, Cornell University.
McKenzie NJ, Jacquier DJ, Isbell RF, Brown KL (2004) Australian Soils and Landscapes: An Illustrated Compendium. CSIRO Publishing: Collingwood, Victoria.
McLaren RG, Cameron KC (1996) Soil Science: An introduction to the properties and management of New Zealand soils. Oxford University Press, Auckland.
Rayment GE, Higginson FR (1992) Electrical Conductivity. In ‘Australian Laboratory Handbook of Soil and Water Chemical Methods’ Inkata Press: Melbourne.
Rengasamy P, Churchman GJ (1999) Cation Exchange Capacity, Exchangeable Cations and Sodicity. In Soil Analysis an Interpretation Manual. (Eds KI Peverill, LA Sparrow and DJ Reuter). CSIRO: Melbourne.
Author: Bill Cotching (Tasmanian Institute of Agriculture), Katharine Brown (The University of Western Australia) and Jeremy Lemon (Department of Agriculture and Food, Western Australia).
The National Soil Quality Monitoring Program is being funded by the Grains Research and Development Corporation, as part of the second Soil Biology Initiative.
The participating organisations accept no liability whatsoever by reason of negligence or otherwise arising from the use or release of this information or any part of it.