Soils are composed of five main components mineral particles derived from rocks by weathering; organic materials - humus from dead and decaying plant material; soil water - in which nutrient elements are dissolved; soil air - both carbon dioxide and oxygen; and living organisms including bacteria that help plant decomposition. Soils differ in their fertility levels, because they have different proportions of these components and because the mineral particles have been affected to different degrees by weathering. Age of soil minerals, prevailing temperatures, rainfall, leaching and soil physico-chemistry are the main factors which determine how much a particular soil will weather (Sinha and Shrivastava, 2000).
Soil thus, is important to everyone either directly or indirectly. It is the natural bodies on which agricultural products grow and it has fragile ecosystem (Sinha and Shrivastava, 2000). South Africa ranks among the countries with the highest rate of income inequality in the world (Aliber, 2009). Compared to other middle income countries, it has extremely high levels of absolute poverty and food insecurity threat (FAO, 2009). As part of this, a potential contributor to food security might be small-scale agricultural production. Aliber (2009) indicated that input support targeting smallholder farmers could boost production and food security. Utilisation of uncultivated arable lands and subsistence agriculture might be one option to contribute to incomes and/or savings, as well as to encourage food diversification (Altman et al., 2009). Land with high agricultural suitability is considered to have greater long-term security with regards to both agricultural production and development. From a planning perspective, high agricultural flexibility is therefore considered an appropriate measure of high quality agricultural land that is highly productive and fertile.
Get your grade
or your money back
using our Essay Writing Service!
Only a small proportion of world's soils have a very good level of fertility, most of which have only good to medium fertility and some have very low fertility, and are often referred to as marginal soils (Ashman and Puri, 2002). Well-known fertile soils are deep alluvial soils formed from river mud, organic matter- rich soils on loess material, nutrient rich Vertisols and volcanic soils (Brady and Weil, 2004). Under poor management, soil fertility can be seriously depleted and soils may become useless for agriculture.
2.2. SOIL PHYSICO-CHEMISTRY
Soil is a natural medium on which agricultural products grow and it is dependent on several factors such as fertility to be considered productive (Shah et al., 2011). The fertility of the soil is depended on concentration of soil nutrients, organic and inorganic materials and water. These soil physico-chemical properties are classified as being physical, chemical and biological, which greatly influence soil fertility (Ramaru et al., 2000). To manage soil fertility, knowledge and understanding of these properties is required (as discussed below).
2.2.1. Physical soil properties
(i) Soil texture
Soil texture refers to the relative proportions of the various size groups of individual particles or grains in a soil (Rowell, 1994). It is dependent on the mixture of the different particle sizes present in the soil. Based on these different sizes, soil particles are classified as sand (0.05- 2mm), silt (0.002-0,5mm) and clay (<0,002mm) (Rowell, 1994). Soil texture is arguably the single most important physical property of the soil in terms of soil fertility, because it influences several other soil properties including density, porosity, water and nutrient retention, rate of organic matter decomposition, infiltration and cation exchange capacity (Møberg et al., 1999).
Clay particles hold larger quantities of water and nutrients, because of their large surface areas (Brady and Weil, 1999). This property causes the swelling and shrinking of clay soils, but only those with smectitic group of clay minerals. The large surface area of clay particles gives nutrients numerous binding sites especially when the surface charge density is high, which is part of the reason that fine textured soils have such high abilities to retain nutrients (Velde, 1995). The pores between clay particles are very small and complex, so movement of both air and water is very slow (Brady and Weil, 1999). Clay particles are negatively charged because of their mineralogical composition. Soils with such particles usually have high CEC and can retain water and plant nutrients; thus such soils are considered to be fertile and good for plant growth (Brady and Weil, 1999).
The knowledge of the proportions of different-sized particles in soils is critical to understand soil behavior and their management. Since sand particles are relatively large, so are the voids between them, which promote free drainage of water and entry of air into the soil (Brady and Weil, 2002). The implication of free drainage in sandy soil is that soil nutrients are easily washed down into the soil and become inaccessible for use by plants (Brady and Weil, 2002). Sandy soils are considered non-cohesive and because of their large size, have low specific surface areas and thus have low nutrient retention capacity (Rowell, 1994). Sand particles can hold little water due to low specific surface area and are prone to drought, therefore have a very low CEC and fertility status (Petersen et al., 1996).
Always on Time
Marked to Standard
The pores between silt particles are much smaller than those in sand, so silt retains more water and nutrients (Rowell, 1994). Soils dominated by silt particles therefore have a higher fertility status than sandy soils and provides favorable conditions for plant growth when other growth factors are favorable (Miller and Donahue, 1992).
(ii) Soil structure
The term soil structure refers to the arrangement of soil particles into aggregates (Six et al., 2000). Soil structure is affected by biological activities, organic matter, and cultivation practices (Rowell, 1994). It influences soil water movement and retention, erosion, nutrient recycling, sealing and crusting of the soil surface, together with aeration and soil's structural stability, root penetration and crop yield (Lupwayi et al., 2001).
Soil structure can be platy, prismatic, granular, crumbly, columnar and blocky (RCEP, 1996). An ideal soil structure for plant growth is often described as granular or crumb-like, because it provides good movement for air and water through a variety of different pore sizes and it also affects root penetration (RCEP, 1996). An ideal soil structure is also stable and resistant to erosion (Duiker et al., 2003). Organic matter and humification processes improve structural stability, and can rebuild degraded soil structures (Brady and Weil, 1999). Therefore it is vital to return or add organic material to the soil and to maintain its biological activity in order to enhance soil structure for plant growth. Favorable soil structure and high aggregate stability are therefore vital to improving soil fertility, increasing agronomic productivity, enhancing porosity and decreasing erodibility.
(iii) Water retention capacity
Water holding capacity refers to the quantity of water that the soil is capable of storing for use by plants (Brady and Weil, 1999). Soil water is held in, and flows through pore spaces in soils. Soil water can be described into the following stages: gravitational, capillary, and hygroscopic, based upon the energy with which water is held by the soil solids, which in turn governs their behavior and availability to plants (Rowell, 1994).
Water holding capacity is an important factor in the choice of plants or crops to be grown and in the design and management of irrigation systems (Brady and Weil, 1999). The total amount of water available to plants growing in field soils is a function of the rooting depth of the plant and sum of the water held between field capacity and wilting percentage in each of the horizons explored by the roots (Brady and Weil, 1999). Field capacity is the amount of soil moisture or water content held in soil after excess water has drained away and the rate of downward movement has materially decreased, which usually takes place within 2-3 days after a rain or irrigation in pervious soils of uniform structure and texture (Govers, 2002).
The ability of the soil to provide water for plants is an important fertility characteristic (RCEP, 1996). The capacity for water storage varies, depending on soil properties such as organic matter, soil texture, bulk density, and soil structure (RCEP, 1996). This is explained by the degree of soil compaction, where problems will arise if excessive compaction occurs which would results in increased bulk density, a decrease in porosity and aeration and poor water drainage (Gregory et al., 2006), all resulting in poor plant growth.
(iv) Electrical Conductivity (EC)
Soil electrical conductivity (EC), is the ability of soil to conduct electrical current (Doerge, 1999). EC is expressed in milliSiemens per meter (mS/m) or cm (cm/m). Traditionally, soil scientists used EC to estimate soil salinity (Doerge, 1999). EC measurements also have the potential for estimating variation in some of the soil physical properties such as soil moisture and porosity, in a field where soil salinity is not a problem (Farahani and Buchleiter, 2004). Soil salinity refers to the presence of major dissolved inorganic solutes in the soil aqueous phase, which consist of soluble and readily dissolvable salts including charged species (e.g., Na+, K+, Mg+2, Ca+2, Clâˆ’, HCO3âˆ’, NO3âˆ’, SO4âˆ’2 and CO3âˆ’2), non-ionic solutes, and ions that combine to form ion pairs (Smith and Doran, 1996).
Salt tolerances are usually given in terms of the stage of plant growth over a range of electrical conductivity (EC) levels. EC greater than 4dS/m are considered saline (Munshower, 1994). Salt sensitive plants may be affected by conductivities below 4dS/m and salt tolerant species may not be impacted by concentrations of up to twice this maximum agricultural tolerance limit (Munshower, 1994). Electrical conductivity is the ability of a solution to transmit an electrical current. The conduction of electricity in soil takes place through the moisture-filled pores that occur between individual soil particles. Therefore, the EC of soil is determined by the following soil properties (Doerge, 1999):
This Essay is
a Student's Work
This essay has been submitted by a student. This is not an example of the work written by our professional essay writers.Examples of our work
. Porosity, where the greater soil porosity, the more easily electricity is conducted. Soil with high clay content has higher porosity than sandier soil. Compaction normally increases soil EC.
. Water content, dry soil is much lower in conductivity than moist soil.
. Salinity level, increasing concentration of electrolytes (salts) in soil water will dramatically increase soil EC.
. Cation exchange capacity (CEC), mineral soil containing high levels of organic matter (humus) and/or 2:1 clay minerals such as montmorillonite, illite, or vermiculite have a much higher ability to retain positively charged ions (such as Ca, Mg, K, Na, NH4, or H) than soil lacking these constituents. The presence of these ions in the moisture-filled soil pores will enhance soil EC in the same way that salinity does.
. Temperature, as temperature decreases toward the freezing point of water, soil EC decreases slightly. Below freezing, soil pores become increasingly insulated from each other and overall soil EC declines rapidly.
Plants are detrimentally affected, both physically and chemically, by excess salts in some soils and by high levels of exchangeable Na in others. Soils with an accumulation of exchangeable Na are often characterized by poor tilth and low permeability and therefore low soil fertility status, making them unfavorable for plant growth (Munshower, 1994).
(v) Bulk Density (BD)
Soil bulk density is defined as the mass of dry soil (g) per unit volume (cm3) and is routinely used as a measure of soil compaction (Gregory et al., 2006). The total volume includes particle volume, inter-particle void volume and internal pore volume (Gregory et al., 2006). Bulk density takes into account solid space as well as pore space (Greenland, 1998). Thus soils that are porous or well-aggregated (e.g. clay soil) will have lower bulk densities than soils that are not aggregated (sand) (Greenland, 1998).
Plant roots cannot penetrate compacted soil as freely as they would in non-compacted soil, which limits their access to water and nutrients present in sub-soil and inhibits their growth (Hagan et al., 2010). Compacted soil requires more frequent applications of irrigation and fertilizer to sustain plant growth, which can increase runoff and nutrient levels in runoff (Gregory et al., 2006).
The bulk density of soil depends greatly on the soil's mineral make up and the degree of compaction. High bulk density usually indicate a poorer environment for root growth, reduced aeration and undesirable changes in hydrologic function, such as reduced infiltration (Brady and Weil, 1999). The presence of soil organic matter, which is considerably lighter than mineral soil, can help decrease bulk density and thereby enhancing soil fertility (Hagan et al., 2010).
2.2.2. Soil Chemical properties
Soil chemical properties which include the concentrations of nutrients, cations, anions, ion exchange reactions and redox properties, but for the purpose of this study focus will be based on properties that have an implication on soil fertility including:
(i) Soil pH
Soil pH is an important soil property that affects several soil reactions and processes and is defined as a measure of the acidity or alkalinity of the soil (Bohn, 2001). It has considerable effect on soil processes including ion exchange reactions and nutrient availability (Rowell, 1994). Soil pH is measured on a scale of 0 to 14, where a pH of 7.0 is considered neutral, readings higher than 7.0 are alkaline, and readings lower than 7.0 are considered acidic (McGuiness, 1993).
Most plants are tolerant of a pH range of 5.5-6.5 which is near neutral pH range (Bohn, 2001). Soil pH is one of the most important characteristics of soil fertility, because it has a direct impact on nutrient availability and plant growth. Most nutrients are more soluble in acid soils than in neutral or slightly alkaline soils (Bohn, 2001). In strongly acidic soils the availability of macronutrients (Ca, Mg, K, P, N and S) as well as molybdenum and boron is reduced. In contrast, availability of micronutrient cations (Fe, Mn, Zn, Cu and Al) is increased by low soil pH, even to the extent of toxicity of higher plants and microorganisms (Bohn, 2001).
The pH of a soil is also reported to affect so many other soil properties (Brady and Weil, 1999), including nutrient availability, effects on soil organisms, fungi thrive in acidic soils, CEC and plant preferences of either acidic or alkaline soils. Most plants prefer alkaline soils, but there are a few which need acidic soils and will die if placed in an alkaline environment (Brady and Weil, 1999).
(ii) Cation Exchange Capacity (CEC)
Cation exchange capacity is defined as the sum of the total of the exchangeable cations that a soil can hold or adsorb (Brady and Weil, 1999). A cation is a positively charged ion and most nutrients cations are: Ca2+, Mg2+, K +, NH4+, Zn2+, Cu2+, and Mn2+. These cations are in the soil solution and are in dynamic equilibrium with the cations adsorbed on the surface of clay and organic matter (Brady and Weil, 1999).
Clay and organic matter are the main sources of CEC (Peinemann et al., 2002). The more clay and organic matter (humus) a soil contains, the higher its CEC and the greater the potential fertility of that soil. CEC varies according to the type of clay. It is highest in montmorillonite clay, lowest in heavily weathered kaolinite clay and slightly higher in the less weathered illite clay (Peinemann et al., 2002). Sand particles have no capacity to exchange cations because it has no electrical charge (Brady and Weil, 1999).
CEC is used as a measure of soil nutrient retention capacity, and the capacity to protect groundwater from cation contamination (Brady and Weil, 1999). It buffers fluctuations in nutrient availability and soil pH (Bergaya and Vayer, 1997). Plants obtain many of their nutrients from soil by an electrochemical process called cation exchange. This process is the key to understanding soil fertility (Rowell, 1994). Nutrients that are held by charges on a soil are termed 'exchangeable' as they become readily available to plants (Rowell, 1994).The higher the CEC of a soil, the more nutrients it is likely to hold and the higher will be its fertility level (Fullen and Catt, 2004).
Factors affecting cation exchange capacity
The factors affecting cation exchange capacity include the following (Brady and Weil 1999), soil texture, soil humus content, nature of clay and soil reaction.
Soil texture influences the CEC of soils in a way that it increases when soil's percentage of clay increases i.e. the finer the soil texture, the higher the CEC as indicated in Table 2. CEC depends on the nature of clay minerals present, since each mineral has its own capacity to exchange and hold cations e.g. the CEC of a soil dominated by vermiculite is much higher than the CEC of another soil dominated by kaolinite, as vermiculite is high activity clay unlike kaolinte which is low activity clay. When the pH of soil increases, more H+ ions dissociate from the clay minerals especially kaolinite, thus the CEC of soil dominated by kaolinite also increases. CEC varies according to the type of soil. Humus, the end product of decomposed organic matter, has the highest CEC value because organic matter colloids have 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.
Table 2.1: CEC values for different soil textures (Brady and Weil, 1999)
CEC range (meq/100g soil)
Clay, clay loam
(iii) Organic Matter
The importance of soil organic matter in relation to soil fertility and
physical condition is widely recognized in agriculture. However, organic matter
contributes to the fertility or productivity of the soil through its positive
effects on the physical, chemical and biological properties of the soil (Rowell, 1994), as follows: physical - stabilizes soil structure, improves water holding characteristics, lowers bulk density, dark color may alter thermal properties; chemical - higher CEC, acts as a pH buffer, ties up metals, interacts with biological - supplies energy and body-building constituents for soil organisms, increases microbial populations and their activities, source and sink for nutrients, ecosystem resilience, affects soil enzymes. Soil organic matter consists of a wide range of organic substances, including living organisms, carboneous remains of organisms which once occupied the soil, and organic compounds produced by current and past metabolism of the soil (Brady and Weil, 1999).
Soil organic matter plays a critical role in soil processes and is a key element of integrated soil fertility management (ISFM) (Brady and Weil, 2004). Organic matter is widely considered to be the single most important indicator of soil fertility and productivity (Rowell, 1994). It consists primarily of decayed or decaying plant and animal residues and is a very important soil component. Benefits of Organic matter in soil according to Ashman and Puri, (2002) include: increasing the soil's cation exchange capacity and acting as food for soil organisms from bacteria to worms and is an important component in the nutrient and carbon cycles.
Organic matter, like clay, has a high surface area and is negatively charged with a high CEC, making it an excellent supplier of nutrients to plants. In addition, as organic matter decomposes, it releases nutrients such as N, P and S that are bound in the organic matter's structure, essentially imitating a slow release fertilizer (Myers, 1995). Organic matter can also hold large amounts of water, which helps nutrients move from soil to plant roots (Mikkuta, 2004).
An important characteristic of organic matter in soil fertility is C: N ratio. The C: N ratio in organic matter of arable surface horizons commonly ranges from 8:1 to 15:1, the median being near 12:1 (Brady and Weil, 1999). The C:N ratio in organic residues applied to soils is important for two reasons: intense competition among the micro-organisms for available soil nitrogen which occurs when residues having a high C:N ratio are added to soils and it also helps determine their rate of decay and the rate at which nitrogen is made available to plants (Brady and Weil, 1999).
(iv) Plant Nutrients
Plants require 13 plant nutrients (Table 2.2) (micro and macro nutrients) for their growth. Each is equally important to the plant, yet each is required in vastly different amounts (Ronen, 2007).
Essential elements are chemical elements that plants need in order to complete their normal life cycle (Scoones and Toulhim, 1998). The functions of these elements in the plant cannot be fulfilled by another, thus making each element essential for plant growth and development (Scoones and Toulhim, 1998).
Essential nutrients are divided into macro and micronutrients as illustrated in Table 3. Macronutrients are those that are required in relatively high quantities for plant growth and can be distinguish into two sub groups, primary and secondary ones, (Uchida and Silva, 2000). The primary macro-elements are most frequently required for plant growth and also needed in the greatest total quantity by plants. For most crops, secondary macro nutrients are needed in lesser amounts than the primary nutrients. The second group of plant nutrients which are micronutrients are needed only in trace amounts (Scoones and Toulhim, 1998). These micronutrients are required in very small amounts, but they are just as important to plant development and profitable crop production as the major nutrients (Ronen, 2007).
Function in plant growth
Deficiency symptoms and toxicities
Chlorophyll and Protein formation
Air/Soil, applied fertilisers
Slow growth, stunted plants, chlorosis, low protein content
Photosynthesis, Stimulates early growth and root formation, hastens maturity
Soil and applied fertilisers
Slow growth, delayed crop maturity, purplish green coloration of leaves
Photosynthesis and nzyme activity, starch and sugar formation, root growth
Soil and applied fertilisers
Slow growth, Reduced disease or pest resistance, development of white and yellow spots on leaves
Cell growth and component of cell wall
Weakened stems, death of plants' growing points, abnormal dark green appearance on foliage
Enzyme activation, photosynthesis and influence Nitrogen metabolism
Interveinal chlorosis in older leaves,
curling of leaves, stunted growth,
Amino acids, proteins and nodule formation
Soil and animal manure
Interveinal chlorosis on corn leaves, retarded growth, delayed maturity and light green to yellowish color in young leaves
Photosynthesis, chlorophyll synthesis, constituent of various enzymes and proteins
Interveinal chlorosis, yellowing of leaves between veins, twig dieback, death of entire limp or plants
Enzyme activation, metabolism of nitrogen and organic acids, formation of vitamins and breakdown of carbohydrates
Interveinal chlorosis of young leaves, gradation of pale green coloration with darker color next to veins
Enzymes and auxins component, protein synthesis, used in formation of growth hormones
Mottled leaves, dieback twigs, decrease in stem length
Enzyme activation, catalyst for respiration
Stunted growth, poor pigmentation, wilting of leaves
Thickened, curled, wilted and chlorotic leaves; reduced flowering
Nitrogen fixation; nitrate reduction and plant growth
Stunting and lack of vigor (induced by nitrogen deficiency), scorching, cupping or rolling of leaves
Root growth, photosynthetic reactions
Wilting followed by chlorosis, excessive branching of lateral roots, bronzing of leaves
Constituent of carbohydrates and photosynthesis
Air/ Organic matter
Maintains osmotic balance and constituent of carbohydrates
Constituent of carbohydrates and necessary for respiration
Air/Water/ Organic matter
Table 2.2: Essential plant elements, their sources and role in plants (Ronen,2007)
Deficiency of any of these essential nutrients will retard plant development (Brady and Weil, 2004). Deficiencies and toxicities of nutrients in soil present unfavorable conditions for plant growth, such as: poor growth, yellowing of the leaves and possibly the death of the plant as illustrated in Table 3 (Ahmed et al., 1997). Therefore proper nutrient management is required to achieve maximum plant growth, maximum economic and growth response by the crop, and also for minimum environmental impact.
In addition to the nutrients listed above, plants require carbon, hydrogen, and oxygen, which are extracted from air and water to make up the bulk of plant weight (Brady and Weil, 1999). Achieving balance between the nutrient requirements of plants and the nutrient reserves in soils is essential for maintaining soil fertility and high yields, preventing environmental contamination and degradation, and sustaining agricultural production over the long term.
2.2.3. Soil Biological properties
(i) Soil organisms
Soil organisms include mostly microscopic living organisms such as bacteria and fungi which are the foundation of a healthy soil because they are the primary decomposer of organic matter (Brady and Weil, 1999). Soil organisms are grouped into two namely soil microorganisms and soil macro organisms (Table 2.3).
Table 2.3: Soil Macro and microorganisms and their role in plant and soil (Brady and Weil, 1999)
Function in plant and/or soil
Decomposition of organic matter
Soil surface and humus particles
Source of protein and enhance soil fertility
Surface layers of grass lands
Fix atmospheric nitrogen and enhance soil fertility
Soil (without organic matter)
Add organic matter to soil, improve aeration of swamp soils, and fix atmospheric nitrogen
They can be applied to crops in large quantities as a biological insecticide
Soil and plant roots
Enhance soil fertility and structural stability
Ants and termites
Dominant in tropical soils
Soil can contain millions of organisms that feed off decaying material such as old plant material, mulch & unprocessed compost (Ashman and Puri, 2002), Microorganisms constitute < 0.5% of the soil mass yet they have a major impact on soil properties and processes. 60-80 % of the total soil metabolism is due to the microflora (Alam, 2001). Micro-organisms, including fungi and bacteria, affect chemical exchanges between roots and soil and act as reserve of soil nutrients (Kiem and Kandeler, 1997).
Soil organic matter is the main food and energy source of soil microorganisms (Ashman and Puri, 2002). Through decomposition of organic matter, microorganisms take up their food elements. Organic matter also serves as a source of energy for both macro and micro organisms and helps in performing various beneficial functions in soil, resulting in highly productive soil (Mikutta et al., 2004).
Macro-organisms such as insects, other arthropods, earthworms and nematodes live in the soil and have an important influence on soil fertility (Amezketa, 1999). They ingest soil material and relocate plant material and form burrows. The effects of these activities are variable. Macro-organisms improve aeration, porosity, infiltration, aggregate stability, litter mixing, improved N and C stabilization, C turnover and carbonate reduction and N mineralization, nutrient availability and metal mobility (Amezketa, 1999; Winsome and McColl, 1998 and Brown et al., 2000).
The various groups of soil organisms do not live independently of each other, but form an interlocked system more or less in equilibrium with the environment (Brady and Weil, 1999). Their activity in soil depend on moisture content, temperature, soil enzymes, dissolution of soil minerals and breakdown of toxic chemicals. All have a tremendous role in the development of soil fertility (Alam, 2001). Their actions involve the formation of structural systems of the soils which help in the increase of agricultural productivity (Alam, 2001).
2.3. SOIL CLAY MINERALOGY
The clay fraction of soil is dominated by clay minerals which control important soil chemical properties including sorption characteristics of soils (Dixon and Schulze, 2002). Minerals are naturally occurring inorganic compounds, with defined chemical and physical properties (Velde, 1995). Minerals that are formed in the depths of a volcano are called primary minerals (Pal et al., 2000). Feldspar, biotite, quartz and hornblende are examples of primary minerals. These minerals and the rocks made from them are often not stable when exposed to the weathering agents at the surface of the earth (Dixon and Schulze, 2002). These rocks are broken down (weathered) continuously into small pieces by exposure to physical and chemical weathering processes (Dixon and Schulze, 2002).
Some of the elements that are released during weathering, reform and crystallise in a different structure forming secondary minerals (Melo et al., 2002). Secondary minerals tend to be much smaller in particle size than primary minerals, and are most commonly found in the clay fraction of soils (Guggenheim and Martin, 1995). Soil clay fractions often contain a wide range of secondary minerals such as kaolinite, montmorillonite and aluminum hydrous oxides, whereas the sand or silt particles of soils are dominated by relatively inert primary minerals. The clay fraction is usually dominated by secondary minerals which are more chemically active and contribute the most to soil fertility (Melo et al., 2002). Two major secondary mineral groups, clay minerals and hydrous oxides, tend to dominate. These groups can appear in various mixtures often in association with soil organic matter (Brady and Weil, 2004).
Clay minerals are hydrous aluminium phyllosilicates, sometimes with variable amounts of iron, magnesium, alkali metals, alkaline earth metals and other cations, (Joussein et al., 2005). They are derived from weathering of rocks and are very common in fine grained sedimentary rocks such as shale, mudstone and siltstone and in fine grained metamorphic slate and phyllite (Van der Merwe et al., 2002). There are also non-clay minerals such as quartz and calcite which are derived from weathering of igneous rocks, (Van der Merwe et al., 2002).
Clay minerals are essential phases in soil chemistry and play extremely important roles in ion exchange reactions (Brigatti et al., 1996; Barrow, 1999). Soils which are texturally and chemically similar may differ in productivity or fertility due to the presence or absence of small amounts of particular clay minerals (Van der Merwe et al., 2002). For example, smectite clays are versatile and strong cationic exchangers and their presence can greatly influence the mobility of potentially toxic elements. Vermiculite has been widely used in the study of short- to medium-term variations (seasonal and annual) in soil processes (Monterroso and Macias, 1998).
Soil clay mineralogy plays a vital role in soil fertility since mineral surfaces serve as potential sites for nutrient storage (Tucker, 1999). However, different types of soil minerals hold and retain differing amounts of nutrients (Velde, 1995). Therefore, it is vital to know the types of minerals that make up a soil so as to predict the degree to which the soil can retain and supply nutrients to plants.
Knowledge of the clay mineralogical composition and the different clay minerals present in soil is important in understanding use, and management of the soil, and in determining the agricultural potentials of soils.
2.3.1. Occurrence of clay and clay minerals
Clays and clay minerals occur under a fairly limited range of geologic conditions (Velde et al., 2003). The environments of formation include soil horizons, continental and marine sediments, geothermal fields, volcanic deposits, and weathering rock formations (Joussein et al., 2005). Most clay minerals form where rocks are in contact with water, air, or steam (Hillier, 1995). Examples of these situations include weathering boulders on a hillside, sediments in sea or lake bottoms, deeply buried sediments containing pure water, and rocks in contact with water heated by magma (molten rock) (Hillier, 1995).
A primary requirement for the formation of clay minerals is the presence of water. Soil clay minerals' formation occurs in many different environments, including the weathering environment, the sedimentary environment, and the digenetic-hydrothermal environment (Brady and Weil, 1999). Clay minerals composed of the more soluble compounds e.g. smectites are formed in environments where ions can accumulate (e.g. in a dry climate, in a poorly drained soil, in the ocean, or in saline lakes) (Velde 1995). Clay minerals composed of less soluble compounds (for example, kaolinite and halloysite) form in more dilute water such as that found in environments that undergo severe leaching (for example, a hilltop in the wet tropics), where only sparingly soluble elements such as aluminum and silicon can remain (Brady and Weil, 1999). Illite and chlorite are known to form abundantly in the diagenetic-hydrothermal environment by reaction from smectite (Brady and Weil, 1999).
2.3.2. Weathering of minerals
The minerals' parent materials form in the crystallisation of molten rock material: these are known as primary minerals, and include olivine, quartz, feldspar and hornblende. Primary minerals are not stable when exposed to water, wind and extremes of temperature (Hillier, 1995). Some of the elements that are released during weathering reform and crystallise in a different structure: these are the secondary minerals, and include vermiculite, montmorillonite and kaolinite (Hillier, 1995). Secondary minerals tend to be much smaller in particle size than primary minerals, and are most commonly found in the clay fraction of soils. As minerals weather, they lose silicon (as soluble silicic acid), leading to increasing proportions of aluminates in weathered clays, such as kaolinite. Aluminium hydroxide species are amphiprotic.
The rate and nature of the weathering process very much depends on climatic conditions. Intense weathering produced in a hot and moist climate can lead to major changes in mineral structure and the conversion to hydrous oxides. There are four phases to be considered in the system that model the formation of clay minerals by the weathering of granitic rocks as the clays have a definite composition: K-feldspar, Muscovite (illite), Kaolinite and gibbsite:
3KAlSi3O8) +2H+ +12H2O ï‚«2K+ +6Si (OH)4 +KAl3Si3O10(OH)2
(K- Feldspar) (Illite) ............... [Eqn. 2.1]
2KAl3Si3O10 (OH)2 + 3H2O + 2H+ ï‚«2K+ + 3Al2Si2O5(OH)4
(Illite) (Kaolinite) ............. [Eqn. 2.2]
Al2Si2O5+ (OH)4 5H2O ï‚«ï€ 2Si(OH)4 + 2Al (OH)3
(Kaolinite) (Gibbsite) ...................... [Eqn. 2.3]
2.3.3. Structure of clay minerals
The structure of clay minerals is developed by the formation of sheets, which are "flat" layers of silicate tetrahedral or aluminate octahedral units (Brady and Weil, 1999). Tetrahedral sheets are sheets of horizontally linked, tetrahedral-shaped units that serve as one of the basic structural components of silicate clay minerals. Each unit consists of a central four-coordinated atom (e.g. Si, Al, or Fe) surrounded by four oxygen atoms that, in turn, are linked with other nearby atoms (e.g. Si, Al, or Fe), thereby serving as inter-unit linkages to hold the sheet together (see Figure 2.1a).
Octahedral sheets are sheets of horizontally linked, octahedral-shaped units that serve as one of the basic structural components of silicate clay minerals (see Figure 2.1b). Each unit consists of a central six-coordinated metallic atom (e.g. Al, Mg, or Fe) surrounded by six hydroxyl groups (OH) that, in turn, are linked with other nearby metal atoms (e.g. Al, Mg, or Fe), thereby serving as inter-unit linkages to hold the sheet together.
Silica tetra hedra with shared oxygen
Figure 2.1a: Si-Tetrahedral layer
Source: Wilson (1999)
Aluminum octahedra with shared oxygen
Figure 2.1b: Al-Octahedral layer
Source: Wilson (1999)
In clay minerals, these sheets stack on top of each other, and are held together by hydrogen bonding or electrostatic attraction (Olis et al., 1990). On the basis of the number and arrangement of tetrahedral and octahedral sheets contained in the crystal units or layers, silicate clays are classified into two different groups (Brady and Weil, 1999) i.e. 1:1 type minerals and 2:1 type minerals:
(i) 1:1 Clay Minerals
The 1:1 type minerals are made of one tetrahedral sheet and one octahedral sheet bonded together to form a layer (Figure 2.2) (Brady and Weil, 1999). In soils, kaolinite is the most prominent member of this group, which includes halloysite, nacrite and dickite. No expansion ordinarily occurs between layers of these minerals when wetted, because the structure is fixed, cations and water do not enter between structural layers and there is also a little isormophous substitution (Van der Merwe et al. 2002). In contrast with other silicate groups, kaolinite exhibits less plasticity, stickiness, cohesion, shrinkage or swelling (Brady and Weil, 1999). Kaolinite-containing soils are easy to cultivate for agriculture and with some nutrient supplementation from manure and fertilizer, can be very productive (Brady and Weil, 1999).
Most of the 1:1 type minerals are considered to exhibit the properties of low activity clays (Van der Merwe et al. 2002). Low activity clays e.g. kaolinite, are more highly weathered due to their lesser surface area as they have a lower capacity to retain and supply nutrients (Kahr and Madseni, 1995). Low activity clays can also have anion exchange capacity (AEC), depending upon the pH of the soil. The AEC causes these clays to retain and supply nutrients, such as phosphate, sulfate, and nitrate, rather than the base cations, under acidic conditions (Brady and Weil, 1999). In order to provide adequate amounts of the base cations, proper management of pH is crucial, i.e. if soil pH is low, additions of lime and/or organic matter may increase the CEC for soils high in low activity clays (Brady and Weil, 2002). Soils containing 1:1 clay minerals, since they are not highly fertile would perform better in agriculture if the soil is carefully managed and necessary nutrients added.
kaolinite molecular model
Figure 2.2: Clay mineral [Kaolinite: Al2Si2O5 (OH)4] with 1:1 layering (tetrahedral - octahedral sheets)
Source: Wilson (1999)
(ii) 2:1 Type Minerals
The crystal units of 2:1 type minerals are characterized by an octahedral sheet sandwiched between two tetrahedral sheets as illustrated in Figure 2.3 (Brady and Weil, 1999). This crystal structure is comprised of four general groups, two of them which are smectite and vermiculite and are also expanding- clay minerals; the other two are fine-grained micas (illite) and chlorite and are relatively nonexpanding clay type minerals (Brady and Weil, 1999). Most of the 2:1 type minerals exhibit the properties of high activity clays (Van der Merwe et al. 2002). Generally, soils with large amounts of high activity clays are not highly weathered (Van der Merwe et al. 2002). High activity clays have a high CEC, due to their large surface area (Brady and Weil, 1999). These clays thus have a great capacity to retain and supply large quantities of nutrients, such as Ca, Mg, K, and NH4 and tend to produce highly fertile soils (Brady and Weil, 1999).
Smectite Molecular model
Figure 2.3: Clay mineral (Montmorillonite) with 2:1 layering
Source: Wilson (1999)
Expanding and nonexpanding 2:1 clay minerals
Examples of these expanding clay minerals are montmorillonite, vermiculite, illite and mica (Brady and Weil, 1999). Some high activity clays such as montmorillonite have a shrink and swell potential (Mathe et al, 2007). This clay minerals (especially smectite), are noted for interlayer expansion, which occurs by swelling when minerals are wetted as water enters the interlayer spaces and force the layers apart (Brady and Weil, 1999).This means that the clays will expand and swell when wet and shrink and crack when dry. With little additions of nutrients, these soils may be very productive. However, the shrink and swell potential will result in poorer drainage and resulting in soil aggregates to being too hard to till because of dryness, and so, proper management of irrigation is required (Van der Merwe et al. 2002).
Micas and chlorites are examples of nonexpanding clay minerals (Brady and Weil, 1999). Weathered minerals similar in structure to these micas are found in the clay fraction of soils and they are called fine-grained micas (Brady and Weil, 1999). The major source of charge is in the tetrahedral sheet, where about 20% of the silicon sites are occupied by aluminum atoms (Olis et al., 1990). To satisfy this charge, potassium ions are strongly attracted in the interlayer space (Brady and Weil, 1999). The potassium being strongly attracted to the adjacent sheets, acts as a binding agent, preventing expansion of the crystal (Brady and Weil, 2002). Hence, fine-grained micas are quite non-expansive. Such properties as hydration, cation adsorption, swelling, shrinkage and plasticity are much less intense in fine-grained micas than in smectites (Brady and Weil, 2002).
In comparison, soil fertility is generally high in high-activity clays such as smectites and other 2:1 clay minerals. 2:1 clay minerals are associated with high CEC, large surface areas and high soil organic matter (SOM). Soil fertility is thus low in low activity clays such as kaolinites and other 1:1 clay minerals. 1:1 clay minerals have low CEC and small surface area, thus they tend to decrease aggregate stability and therefore soil fertility (Leinweber and Schulten, 2000 and Six et al., 2000). The characteristics of these minerals are briefly summarized in the Table 2.4 below.
Table 2.4: Summary of 1:1 and 2:1 clay minerals characteristics (Brady and Weil, 2008)
Interlayer condition / Bonding
Specific surface area (m2/g)
Basal spacing (nm)
1 : 1 (non-expanding)
lack of interlayer surface, strong bonding
3 - 15
5 - 20
2 : 1 (expanding)
very weak bonding, great expansion
80 - 150
700 - 800
0.98 - 1.8 +
2 : 1 (expanding)
weak bonding, great expansion
500 - 700
1.0 - 1.5 +
2 : 1 (non-expanding)
partial loss of K, strong bonding
10 - 40
50 - 200
2 : 1 : 1 (non-expanding)
moderate to strong bonding, non-expanding
10 - 40
2.4. SOIL FERTILITY
Soil fertility refers to the ability of the soil to supply essential plant nutrients and soil water in adequate amounts and proportions for plant growth and reproduction in the absence of toxic substances which may inhibit plant growth (Havlin et al., 2005). Soil fertility is a complex quality of soils that is closest to plant nutrient management, (Gruhn et al., 2000). It is the component of overall soil productivity that deals with its available nutrient status, and its ability to provide nutrients out of its own reserves and through external applications for crop production. It combines several soil properties (biological, mineralogical, chemical and physical), all of which affect directly or indirectly nutrient dynamics and availability (Eghball, 2002). Soil fertility is a manageable soil property and its management is of utmost importance for optimizing crop nutrition on both a short-term and a long-term basis to achieve sustainable crop production (Havlin et al., 2005).
Soil productivity is the ability of a soil to support crop production determined by the entire spectrum of its physical, chemical and biological attributes (Ashman and Puri, 2002). Soil fertility is only one aspect of soil productivity but it is a very important one (Brady and Weil, 2004), for example, a soil may be very fertile, but produce only little vegetation because of a lack of water or unfavourable temperature or even other factors. Even under suitable climatic conditions, soils vary in their capacity to create a suitable environment for plant roots (Fullen and Catt, 2004). Good natural or improved soil fertility is essential for successful cropping (Fullen and Catt, 2004), and it is the foundation on which all input-based high-production systems can be built.
Soils vary in their fertility level as a result of differences in their properties (Foth and Ellis, 1997). Soils that are highly weathered like ultisols and oxisols are characterized by differences in stable aggregate due to differences in clay mineralogy (Hassett and Banwart, 1992). Ultisols and oxisols usually forms very stable aggregates and drains well, although nutrient additions may be necessary for the soils to perform better (Brady and Weil, 2002). Highly weathered soils are considered to be more fertile and are dominated by shrinking and swelling clays, than less weathered soils such as luvisols. Soils that primarily consist of partially decomposed organic matter (Gruhn et al., 2000) have high organic matter content and consequently tremendous water holding capacity, which enables them to perform well in agriculture (Mathe et al., 2007).
Soill fertility is also greatly influenced by the presence nutrient elements classified as macro and micro elements (Gruhn et al., 2000). The major and micro or trace elements are made available to plants by breakdown of the mineral and organic matter in the soil (Havlin et al., 2005 and Shah et al., 2011). Availability of these nutrients depends on how much is present, the form in which it is present in the soil (Table 2.5) , the rate at which it is released from organic matter or mineral particles and the soil pH i.e. its acidity or alkalinity.
The proportion of nutrients held on the clay and humus particles influence deficiencies (Shah et al., 2011) e.g. K, Ca and Mg are held on the surface of clay particles and are directly taken up by plant roots or from the soil solution. An excess of K can create a deficiency of Ca or the reverse can occur. Acid soils high in Mn often cannot supply enough Co for rhizobium bacteria with a consequent effect on N fixation by legumes. Also on very acid soils Mn and Fe make P unavailable to plants by 'fixing' it in insoluble complexes. The chemical relationships influencing soil fertility are complex and affected by the parent material from which soil develops, the type of clay present, the proportions of different sized particles, e.g. sand, silt, clay, which also have important effects on soil structure.
Table 2.5: Essential nutrient elements showing element, symbol and primary forms used by plants (Shah et al., 2011).
Primary Forms Used by Plants
HPO42- , H2PO4-
B(OH)3O (Boric acid)
2.5. INFLUENCE OF SOIL PHYSICO-CHEMICAL PROPERTIES ON SOIL FERTILITY
In summation of all factors affecting soil fertility, fertile soil can be described as one that is: rich in the nutrients which are necessary for plant nutrition, including nitrogen, phosphorus and potassium (N-P-K); contains appropriate concentration of trace elements which are also critical for plant nutrition, but are needed in much smaller quantities than N-P-K nutrients, these include boron, cobalt, copper, iron and several others; contains good levels of organic matter, which improves soil structure and its ability to hold water; the soil pH (an indicator of acidity or alkalinity) is balanced; has good soil structure; has a good CEC in available forms for plants; contains a range of macro-organisms (earthworms, termites, etc.) and micro-organisms (fungi, bacteria, etc.) and that help support plant growth and health; contains high-activity clays such as smectites, montmorillonites and other 2:1 type clay minerals. Clay minerals play a key role in determining the capacity of a soil to retain nutrients and moisture. They are therefore of great importance in fertilization and irrigation management. For this reason, recommendations on the type of fertilizers and the method of application for a particular crop are based to a large extent on soil clay mineralogy.
SOM is largely dependent on soil characteristics (e.g. clay mineralogy) that control the affinity of soil mineral particles for binding with SOM compounds. For example, 2:1 clay minerals (e.g. illite), dominant in the clay fraction of most temperate soils, and SOM can mutually interact with positively charged metal ions due to the net negative charge of SOM at field pH and the permanent negative charge of 2:1 clay minerals (Dixon, 1989). Due to its important role, the clay mineralogy must be taken into consideration for fertilizer management. Another important implication of soil clay minerals especially illite and vermiculite is their ability to fix certain nutrients over others, thus rendering them unavailable to crop roots.
Heavily clayed soils called vertisols are moderately weathered and characterised by high cation exchange capacity and contain montmorillonite as the dominant mineral (FAO, 2001). Vertisols are generally more fertile than other soil types, but careful management of irrigation may be required as they are heavy clayey soil with high proportion of swelling clays (Parker and Rae, 1998). They are also naturally high in organic matter and are therefore well suited for agricultural use (Brady and Weil, 2002).
Cation exchange capacity and anion exchange capacity (AEC) are properties that can help differentiate soil minerals (Landon, 1991). Cation exchange capacity and AEC values are important measurements that provide important information regarding the soil's ability to retain and supply certain nutrients to the plant (Landon, 1991). In addition to nutrient retention, CEC and AEC help in predicting the leaching potential of certain nutrients in areas with high rainfall (Brady and Weil, 1999). When the soil has a very high CEC, negatively charged nutrients such as nitrate are not retained by the soil (Hassett and Banwart, 1992). Instead, nitrate leaches through the soil profile in areas with high amounts of precipitation. Likewise, soils with high AEC experience leaching of positively charged nutrients, such as calcium and potassium (Hassett and Banwart 1992). Ion exchange occurs when the loosely held cations or anions on the clay mineral surfaces are replaced by ions of the same charge (sign and magnitude) in solution (Brady and Weil, 2002). Cation exchange is by far the most common, and is necessary for soil fertility (Landon, 1991).
Different cations in soils are adsorbed more or less easily than others and the tightness with which the soil holds cations varies (Brady and Weil, 1999); it is greatest for hydrogen and aluminum cations and decreases for other cations in the following order: Al > H > Ca > Mg > K > Na . It is not just the total number of a particular nutrient ion adsorbed in the substrate which determines its availability to plants, but also the fraction of the CEC occupied by that ion. Cation exchange capacity varies according to the type of clay mineral whereby it is usually highest in highly weathered clay minerals such as smectite, lowest in heavily weathered clay minerals such as kaolinite and slightly higher in the less weathered illite, (Bergaya and Vayer, 1997). The existence of kaolinite as the secondary mineral may have implications with regards to the agricultural potential of the land mainly because of its low CEC, (Ekosse et al., 2011). Higher CEC implies the reduced leaching of nutrients even ion fertilizer application. However, it may also mean retention of contaminants. Physico-chemical and clay mineralogical properties of soil therefore clearly interact to influence soil fertility. This interaction varies with soils because of the differences that exist in soil orders.
2.6. INFLUENCE OF SOIL CLAY MINERALOGY ON SOIL FERTILITY
Soil clay minerals play a very important role in the chemical reaction of soil and influence the movement and retention of contaminants, metals, and nutrients in the soil (Tucker, 1999). Soil clay minerals influence agricultural land use, soil fertility and productivity (Ekosse et al., 2011). They influence the physico-chemical, physical and chemical properties of soils and have a strong bearing on their usage in agriculture (Ekosse et al., 2011). The magnitude of the contribution of clay minerals to soil CEC, buffer capacity, cation fixation, and various physical and chemical properties depends upon the nature and amount of the various mineral species present (Pal, 2000). Secondary clay minerals are extremely important in soil as they provide a mechanism for retaining essential nutrients through ion exchange therefore enhancing soil fertility (Dixon and Schulze, 2002), and they also buffer the soil against rapid changes in acidity or alkalinity and help create soil structure (Wilson, 1999).
Clay minerals are increasingly recognized as an important fraction in soils influencing the nutrient retention capacity and their mobility in specific environments (Boonfueng et al., 2005). The influence of common clay minerals such as kaolinite (Zhou and Gunter, 1992), smectite (Jongmans et al., 1998), and illite (Post and Borer, 2002) on soil properties including CEC (Asadu et al., 1997), organic matter content (Peinemann et al., 2000) and dispersivity (Singer et al., 1992) have been studied in details. Clay minerals are very important natural metal ion adsorbents in soils (Mareschal et al., 2011). As the adsorption capacity depends on the crystal structural features, clay mineral transformation processes may affect the adsorption properties of the soil itself (Mareschal et al., 2011).
According to Bain and Griffen (2002), the clay fraction of the soil and in particular the kind and amount of the respective clay minerals present, determines in large measure the chemical and physical properties of the soil. The physical effects manifest themselves in soil structure, and in the movement and retention of soil moisture (Brady and Weil, 2002). By reason of its predominant role in cation and anion exchange, the clay fraction is the primary factor which controls soil acidity and alkalinity, and as such must be taken into account in any program of reclamation of alkaline and saline soils (Bohn et al., 2001). To the extent that it influences the ease or difficulty of release of plant nutrient ions, the clay fraction is important in plant nutrition (Tucker, 1999).
Majority of clay minerals have exchangeable cations (Pal et al., 2000). These cations generally are held on the surface of the clay, and are not strongly held (Pal et al., 2000). They can be exchanged for other cations in an equilibrium process. As soils weather, they lose CEC and fertility and as minerals weather, they lose silicon (as soluble silicic acid), leading to increasing proportions of aluminate in weathered clays, such as kaolinite (Parker and Rae, 1998). Aluminium hydroxide species are amphiprotic i.e. they can accept or lose protons. As a consequence, soils dominated by oxides of aluminium (and other metals) can have positive sites, allowing anion exchange (Parker and Rae, 1998). The reaction of soils that greatly influences soil fertility is determined by its clay fraction, especially the mineralogical composition (Douglas, 1989). Studies by Parfitt et al. (1997) have revealed that soil clay mineralogy influences organic matter dynamics in soils, sorption and ion reactions and fixation of nutrients. These effects of the clay minerals are enhanced or compromised by interaction with other soil properties such as pH and electric conductivity.
2.7. SOIL FERTILITY STATUS OF ARABLE LANDS
In agriculture arable land is land that can be used for growing crops (Sheffrin, 2003). It includes all land under temporary crops (double-cropped areas are counted only once), temporary meadows for mowing or market and kitchen gardens and land temporarily fallow (less than five years). Data for arable land are not meant to indicate the amount of land that is potentially cultivable (FAO, 2010). As such, it has to be distinguished from agricultural land, which, according to Food and Agriculture Organization's (FAO) definition, additionally includes land under permanent crops as well as permanent pastures. In 2008, the world's total arable land amounted to 13,805,153 kmÂ², whereas 48,836,976 kmÂ² was classified as "agricultural land" (FAO, 2010)
The challenge for agriculture over the coming decades will be to meet the world's increasing demand for food in a sustainable way. Declining soil fertility and mismanagement of plant nutrients have made this task more difficult (Gruhn et al., 2000). The overall strategy for increasing crop yields and sustaining them at a high level must include an integrated approach to the management of soil nutrients, along with other complementary measures (Gruhn et al., 2000). An integrated approach recognizes that soils are the storehouse of most of the plant nutrients essential for plant growth and that the way in which nutrients are managed will have a major impact on plant growth, soil fertility, and agricultural sustainability. Farmers, researchers, institutions, and government all have an important role to play in sustaining agricultural productivity.
The effects of declining soil fertility on yield growth are particularly visible in Africa, where the most serious food security challenges exist and lie ahead (Badiane and Delgado 1995; Rosegrant, Agcaoili-Sombilla, and Perez 1995). The low level of chemical fertilizer use, decline in soil organic matter, and insufficient attention to crop nutrient studies contribute the most to the loss of soil fertilityMin the region (Kumwenda et al. 1996). In comparison to the rest of the world, fertilizer use in Sub-Saharan Africa is low and declining. In 1996, Sub-Saharan Africa consumed only 1. million tons of fertilizer, (equivalent to 8.9 kilograms per hectare of arable land) (Figure 2.4). By comparison, global fertilizer use reached approximately.
Declining soil fertility and mismanagement of plant nutrients have made the task of providing food for the world's population in 2020 and beyond more difficult. The negative consequences of environmental damage, land constraints, population pressure, and institutional deficiencies have been reinforced by a limited understanding of the biological processes necessary to optimize nutrient cycling, minimize use of external inputs, and maximize input use efficiency, particularly in tropical agriculture (Kumwenda et al. 1996).
Figure 2.4: Fertilizer consumption in Sub-Saharan Africa and the world, 1961-96 (FAO 1998 and 1999.)
Over the past 40 years, approximately 30% of the world's cropland has become unproductive (World Summit on Sustainable Development 2002). About 2 million hectares of rainfed and irrigated agricultural lands are lost to production every year due to severe land degradation, among other factors (Figure 2.5) (Primental and Giampietro, 1994; World Bank). It takes approximately 500 years to replace 25 millimeters (1 inch) of topsoil lost to erosion. The minimal soil depth for agricultural production is 150 millimeters. From this perspective, productive fertile soil is a non-renewable, endangered ecosystem (Primental and Giampietro, 1994; Pimental, 2000).
Figure 2.5: Amount of Irrigated agricultural land in the world (1961-2002)
Source: UN FAO Stat Irrigation (http://faostat.fao.org/faostat/)
In 1960, when the world population numbered only 3 billion, approximately 0.5 hectare of cropland per capita was available, the minimum area considered essential for the production of a diverse, healthy, nutritious diet of plant and animal products like that enjoyed widely in the United States and Europe (US GAO report, 2003).
C:\Users\Joey\AppData\Local\Microsoft\Windows\Temporary Internet Files\Content.IE5\0KCVT2GI\africa-arable-land-01.jpg
Figure 2.7: Map showing arable lands in Africa (www.mapsoftheworld.com)
The increase in world population means that pressures on land will continue to be acute, particularly in Africa and Asia (ADB, 2001). The increased needs for food and other agricultural products must be met mainly by raising and sustaining crop and livestock yields and by more intensive land use (ADB, 2001; FAO, 2001). However, current projections also assume an expansion of the arable area in developing countries, although at half the rate of the previous 30 years (FAO, 2001). By 2030, FAO estimates suggest that an additional 57 million ha will be brought into cultivation in Africa, and 41 million ha in Latin America, increases of 25 per cent and 20