Cause And Effects Of Soil Erosion

Ca pulmonary tuberculosis And Effects Of nation ErosionThe Latin word erodere, typifying to jaw away is the origin of the word eroding (Roose, 1996). district Erosion is the somatogenetic removal of top body politic by various agents, including f completely(prenominal)ing raindrops, urine menstruum everywhere the injury profile and gravitational pull (Lal 1990). The Soil acquaintance Society of America defines corroding as the wearing away of the wreak coat by running wet, wind, ice or other geological agents, including such(prenominal) processes as gravitational creep (SCSA, 1982). Physical corrosion involves the dissolution and emigration of in irrigate-soluble alter particles (sand, silt and native matter). Removal of soluble real as dissolved substances is c wholeed chemical wearing and this maybe ca employ by get along flood or subsurface f scurvy where the body of water supply moves from i layer to some other within the background profile (Lal 1990). agree to ASCE, 1975, the carnal processes in blur eating away al funky in climb-down of modify particles, their ex listation and subsequent dethronement of s put forwarddal sedimentations down gear by raindrop pertain and flood over the defacement surface. Rain steady down is the about classical detaching agent (Morgan and Davidson 1986 Lal, 1990) fol lowed by over belt down accrue in entraining blur particles (Lal 1990).The process of acres eating away occurs in cardinal master(prenominal) steps, drug withdrawal of alter particles, merchant vesselsation and alluviation of earth particles down pitch by raindrop impact and overspill over the flaw surface (ASCE 1975 Morgan and Davidson, 1986, Lal 1990) followed by over inflict tend in entraining primer particles (Lal, 1990). Soil wear vehementuces stain productivity by physical sack of top flat coat, decrease in rooting depth and qualifying of water. In contrast spot, daub depletion means d ischarge or decline of state fertility collectable to jog removal or removal of nutrients by eluviations from water qualifying with the state profile (Lal, 1990). Sedimentation however, causes off site make interchangeable degradation of basins, accumulation of silts in water reservoirs and burial of sea-level productive beas and other problems (Lal, 1990). Sediments is the master(prenominal) cause of pollution and eutrophication (Lal, 1990). According to Lal 1990, fault degradation may be caused by accelerated soil corroding, depletion through intensive land use, deterioration in soil structure, changes in soil pH, leaching, salt accumulation, build up of toxic elelments such as atomic number 13 or zinc, excessive inundation leading to cut back soil disposes and low aeration.Soil Erosion is the most serious and least reversible reach of land degradation (Lal, 1977 El-Swaify, D tumbler and Amstrong, 1982). Soil eating away and soil evil , concord to Lal (1990) lead adverse fixs on market-garlairing because they deplete the soils productivity and diminish the resourse base.2.2 Soil Erosion ProcessGeologic erosion rotter be caused by a number of internal agents including rainwater, flowing water and ice, wind and the the mass movement of soil bodies under the action of gravitation which cause the loosened or dissolved earthy and rock materials to be removed from a place and eventually deposited to a new view (Lal,1990 Morgan and Davidson, 1986). The Soil Science Society of America (SCSA, 1982) draw geologic erosion as the normal or raw(a) erosion caused by geologic processes acting over long periods and passing in the wearing away of mountains, the grammatical construction up of flood plains, coastal plains. Etc. The slow and constructive natural soil erosion process has been significantly accelerated by adult male activities of poor do working practices, overgrazing, ground clearing for construction, logging and mining (Lo, 1990). quicken erosion not only affects the soil alone as well as the surround and is the primary cause of soil degradation (Lal, 1990). Agriculture has been identified as the primary cause of accelerated soil erosion (Pimentel, 1976).2.3 Soil Characteristics in the TropicsExtremes of climate and wide variety of p arnt materials cause immense contrast of soil properties in the tropics from soils in other restrained regions. In the tropics soils argon super variable and diverse like the phytology (Sanchez and Buoi, 1975 Van Wambeke, 1992). The main soil types argon alfisols, oxisols, ultisols and inceptisols (El-Swaify, 1990). Tropical soils low in weatherable minerals and basic cations (sodium, calcium, magnesium, and potassium) resulted from continuous weathering of parent materials (Lo, 1990). The ability of these soils to keep typeset nutrients is whoppingly dependent on the humus heart found in plant biomass and the organic matter (Rose,1993). The in action mechanism o f soil mineral constituents (kaolin and sesquioxides) in these soils, causes deficiency in set nutrients, refuses the cogency to hold open basic cations, limits busy race with organic matter and excessively immobilizes phosphates and related to anions, a coach which are toweringly toxic to plant roots (Lo, 1990). Crop drudgery in tropical soils are constrained by primarily aluminum- derived soil acidity and infertility save generally their physical properties are affirmative (El-Swaify, 1990). Tropic soils halt moderate to superior permeability under natural conditions, but susceptible to slaking and development of impermeable crust upon action of raindrops and as a result overflow join ons with continuous cultivation (Lal, 1982). This crusting cause unnoticeable reduction of filtration rate, increasing water flood which leads to acceleration of soil erosion (Falayl and Lal, 1979).It is important to note however that heavy and intense rains cause surd erosion in t he tropics (Morgan, 1974 Wilkinson 1975 Amezquita and Forsythe, 1975 Lal 1976 Aina, Lal and Taylor, 1977 Bois, 1978 Sheng 1982).2.4 Soil Erosion on sop up SlopeAccording to Lal 1990, Steeplands refer to lands with a careen gradient greater than 20%. It is important to note however that jejune undulating lands have a great potential for result production and agricultural development. Due to the hypothesis of soil erosion and the problem of mechanization, the steep areas are considered marginal for husbandry production (Lal, 1990).The difficult topography in steepland agriculture restricts mechanizations of operations thus, reducing all agricultural activities (land preparation, cultivation and harvesting), limiting the farmer in scale and efficiency. Inputs such as fertilizer and pesticides have to be carried manually by the farmer. As a resulted they are used scarcely. Observably any cast up in the use of these agricultural inputs willinging result in decline in he farm ers profits from the generally trim down agricultural field (Benvenuti, 1988). For all these reasons steepland farmers tend to concentrate in senior higher(prenominal) value crop production of limited scale (Ahmad, 1987 Ahmad 1990). It is important to note however that farmers prefer steep delivers imputable to cultural hold cultivation, planting and harvesting can be through in an upright fashion (Williams and Walter, 1988). Futher more subsistence farmers are found on steep set ups because of more favourable env bidmental conditions such as lower temperatures, reduced diseases and high reliability of rainwater. (Hurni, 1988).In the tropics, removal of forest vegetation causes excessive leaching and accelerated soil nutrient passing play. Being highly weathered soil types , their contained minerals generally have poor ability to retain sorbed nutrients against leaching. Clay soils with high residualmiron contents are considered superior in impedance to flood caused soil er osion thus, soils emanated from basic igneous rocks and red soils developed from calcareous rocks are strongly aggregated collectible to the cementing position of iron oxides, hence, soil erosion is expected to be slight than for most other soils. Also soils developed from fragmentary volcanic materials with andic properties are patient of to soil erosion (Sheng, 1986 Ahmad, 1987 Ahmad, 1990 Lal, 1990). Soils formed from shales, schists, phyillites and sandstones are considered highly erodible. Soils produced from these rocks are high in both sand or silt fraction, and corpse minerals and iron oxides are generally insufficient as cementing agents for a changeless-structured soil. These parent materials are generally rich in muscovite occurring in all soil particle-size fractions. Micah-rich soils are weak-structured, and thus raindrops can easily dislodged the weak aggregates, while the form fraction dispersed in water. The resulting mica flakes settling on their flat axes in the water film on the soil surface causes soil crusting. The formation of soil crusts further restricts water entry into the soil (Ahmad and Robin, 1971 Sumner, 1995), resulting to inclination of a much greater volume of runoff water, a condition which leads to further disintegration of soil aggregates and get off of colloidal soil material (Ahmad, 1987 Ahmad 1990). Soil crust restricts gaseous exchange leading to anaerobic soil conditions, denitrification, toxic do due to ethylene production, and mechanical impedance to seedling maturation (Ahmad 1987 Ahmad, 1990).Steep slope cultivation can cause authorized unstableness in the ecological system with both onsite and offsite detrimental impacts (El-Swaify, Garnier and Lo, 1987). Soil, climate, land use and farming systems affect the point and the point of moroseness of soil erosion. However, unheeding of soil and climatic conditions, intensively used steeplands in densely be regions experience severe soil erosion problem. vote down use influences the degree of severity of soil erosion on steeplands. Uncontrollable grazing or over grazing, exensive and abusive cultivation, diversified cropping are responsible for severe soil erosion in unprotected arable lands (Roose, 1988 Liao et al 1988). Ahmad (19871990) reportd soil loss of approximately 120 t0 180 tonnes per hectare in Tobago Trinidad. In Australia, annual soil loss of 200 t/ha to 328 t/ha has ben account from sloping sugar cane plantations in central and north Queensland (Sallaway, 1979 Mathews and Makepeace 1981). on that point are 2 types of soil erosion associated with the Caribbean region, land slipping and gullying. Land slipping is a manifestation of mass movement associated with steepland agriculture and the severity being strongly influenced by the parent materials. Land clearing (example deforestation) and crop production can influence land slipping particularly in the early portion of the ladened season when the cleared soil wets red-hot due to saturation of the soil above rock. Serious dislocations, crop loss and destruction of any mechanical anti erosion devices can result from this form of mass movements. Due to drastic changes in hydrological conditions experienced by land naturally prone already to slipping and cleared for agriculture for the first time land slippage would be of roughhewn experience (Ahmad 1987 Ahmad 1990).Gullying is another common form of soil erosion that occurs on steep land bcause of the terrain involved. This is more common on sandy soils, volcanic soils and vertisols, which are all porous materials. Soils easily attain saturated conditions upon the rapid entry of water, so severinging the material and ultimately, leading to the formation of gullies. Agricultural activities enables this soil erosion in steeplands by allowing rapid soil wetting upon the start of the wet season. Farming activities though unsuitably oriented field boundaries, foot tracks and the miss of provision for disposal of surface water are some main causes of gullying, even on soils not prone to this tpe of steepland soil erosion (Ahmad 1987Ahmad 1990).Since steeplands are traditionally considered marginal for agricultural crop production, most research on soil erosion and soil conservation has been done on each flat land or rolling land with a upper limit slope of about 20%(Lal, 1988).2.5 Factors Affecting Soil ErosionThe causes of soil erosion have been intensively discussed during the past 40 years. Soil erosion is a natural process that is enhanced by human activity (Richter, 1998) and occurs in all landscapes and under different land uses. In rise to condition to human activities, soil erosion processes are similarly caused by morphometric characteristics of the land surface, the erosive forces of pelting and the erodibility of soils and soil surfaces.When rainwater reaches the soil surface it will either enter the soil or run off. Runoff occurs when the rainwater tawdr iness exceeds the percolation capacity of the soil. Water erosion is the result of the scattering action of rain drops, the transporting power of water and also the vulnerability of the soil to dispersion and movement (Baver and Gardner, 1972). The effects of soil erosion is also classified definition of gullies and explanation of gully development is given by Morgan (1996), as surface as Hudson (1995) who additionally focuses on individual episodes of the development of gullies. Toy et al (2002) give detailed definitions of soil erosion features and processes such as tabloid erosion and inter-rill erosion, rill erosion, as well as ephemeral and immutable gully erosion.Rill erodibility depends both directly and indirectly on soil properties such as bulk density, organic carbon and clay content, clay mineralogy, cations in the exchange complex, soil pH and experimental conditions such as moisture content, aging of prewetted soil and quality of eroding water (Rapp,1998). Gover s (1990) found that runoff erosion resisitance of a loamy material was extremely sensitive to rendering in the initial moisture content and to a lesser extent to changes in bulk density.The process of water erosion can be separated into two components, rill and interrill erosion (Young and Onstad, 1978). Interrill erosion (sheet erosion) is mainly caused by raindrop impact and removes soil in a thin almost incognoscible layer (Foster, 1989). In interril erosion the flow of water is generally unconfined, shut mingled with soil clods and covers much of the soil surface. As the velocity of flow maturations the water incises into the soil and rills forms (Evans,1980).Rill erosion begins when the eroding capacity of the flow at some point exceeds the ability of the soil particles to rebarbative detachment by flow (Meyer cited by Rapp, 1998). Soil is detached by headcut recruit from knickpoints (De Ploey, 1989 Bryan, 1990), rill slide sloughing and hydraulic trim stress (Foster ci ted by Rapp, 1998) as well as by slumping by undercutting of side walls and scour hole formation (Van Liew and Saxton, 1983). These processes are usually combined into a detachment prediction comparability as a function of average shear stress (Foster cited by Rapp, 1998). When the rills develop in the landscape, a three to five dollar bill fold increase in the soil loss commonly occurs (Moss, light-green and Hutka 1982 and Meyer and Harmon 1984).2.5.1 Vegetative FactorsThe effects of vegetation can be classified into three catergoriesThe interception of raindrops by the canopy (DHuyvetter, 1985). Two effects are associated with this. Firstly, part of the intercepted water will evaporate from the leaves and stems and thus reduce runoff. Secondly, when raindrops strike the vegetation, the vigor of the drops is dissolute and there is no direct impact on the soil surface. The interception lot depends on the type of crop, the growth stage and the number of plants per unit area.A well distributed, close growing surface vegetative cover will slow down the rate at which water flows down the slope and will also reduce concentration of water (DHuyvetter, 1985). As a result, it will decrease the erosive action of running water.There is also the effect of roots and biological activity on the formation of stable aggregrates, which results in a stable soil structure and increased infiltration that reduces runoff and decreases erosion (DHuyvetter, 1985). Increased permeability also reduces erosion as a result of in increased water percolation due to better drainage. Stables aggregrates in the topsoil also counteract crusting.2.5.2 Rainfall FactorsRaindrop size, precondition, time of a storm and wind speed interactions controls the erosive power of rainfall (DHuyvetter, 1985). The erosivity of rainfall is expressed in terms of energising energy and is moved(p) by various factors.According to Wischmeier and Smith (1965), the intensity of rainfall is most related tot e kinetic energy, according to the regression equalityE = 1.213 + 0.890 log IWhereE = the kinetic energy (kg.m/m2.mm)I = rainfall intensity (mm/h)Raindrop size, statistical distribution and shape all influence the energy momentum of a rainstorm. Laws and Parson (1943) reported an increase in median(prenominal) drop size with increase in rain intensity. The relationship between mean drop size (D50) and rainfall is given byD502.23 I 0.182 (inch per hour).The median size of rain drops increases with low and medium intensity fall, but declines slightly for high intensity rainfall (Gerrard, 1981). The kinetic energy of an rainfall event is also related to the velocity of the raindrops at the time of impact with the soil (DHuyvetter, 1985). The distance through which the rain drop must fall to maintain terminal velocity is a function of drop size. The kinetic energy of a rainstorm is related to the terminal velocity according to the equationEk = IV2/2Where Ek = energy of the rain st ormI = IntensityV= Velocity of raindrop before impactEllison (1945) developed an equation showing that the relationship between the soil detached, terminal velocity, drop diameter and rainfall intensityE = KV4.33 d1.07 I0.63Where E = relative amount of soil detachedK = soil constantV = velocity of raindrops (ft/sec)d = diameter of raindrops (mm)I = rainfall intensity2.5.2.1 Effect of rainfall intensity on runoff and soil lossAccording to Morgan (1995), soil loss is closely related to rainfall partly through the detaching power of raindrops striking the soil surface and the contribution of rain to runoff. If rainfall intensity is less than the infiltration capacity of the soil, no surface runoff occurs and the infiltration rate would equal the rainfall intensity (Horton, 1945) as sited by Morgan (1995). If the rainfall intensity exceeds the infiltration capacity, the infiltration rate equals the infiltration capacity and the excess rainfall forms surface runoff.According to Morgan (1 995), when the soil is unsaturated, the soil matric potential is negative and water is held in the capillaries due to matrics suction. For this reason, under saturated conditions sands may produce runoff truly quickly although their infiltration capacity is not exceeded by the rainfall intensity. Intensity partially controls hydraulic conductivity, increasing the rainfall intensity may cause conductivity to rise so that although runoff may have formed rapidly at relatively low rainfall intensity, higher rainfall intensities do not always produce greater runoff (Morgan, 1995). This mechanism explains the reason why infiltration rates sometimes increase with rainfall intensities (Nassif and Wilson, 1975).2.5.3 Soil FactorsAccording to Baver et al, (1972), the effect of soil properties on water erosion can be in two ways Firstly, certain properties determine the rate at which rainfall enters the soil. Secondly, some properties affect the resistance of the soil against dispersion and erosion during rainfall and runoff.The particle size distribution is an important soil property with regards to erodibility. Generally it is found that erodible soils have a low clay content (DHuyvetter, 1985). Soils with more than 35% clay are often regarded as being cohesive and having stable aggregates which are resistant to dispersion by raindrops (Evans, 1980). Evans also taked that sands and coarse loamy sands are not easily eroded by water due to its high infiltration rate. In contrast soils with a high silt or fine sand fraction are very erodible.Erodibility of soil increases with the proportion of aggregates less than 0.5mm (Bryan, 1974). Factors which contribute to aggregate stability include organic matter content, root secretions, mucilaginous gels formed by break down of organic matter, the binding of particles by sesquioxides and the presence of a high Ca concentration on the exchange sites of the colloids instead of a high sodium content (DHuyvetter, 1985).The depth of erosion is fit(p) by the soil profile (Evans, 1980). According to Evans soil horizons below the A horizon or plough layer are often more compact and less erodible. The texture and chemical composition of the sub surface horizon can also have an adverse effect. Normally deep gullies can be cut if the parent material is unconsolidated. If resistant bedrock is near the surface only rills will develop. Soil rich in surface stones are less susceptible to erosion (Lamb, 1950 and Evans, 1980). Stones protect the soil against erosion and also increase the infiltration of the flowing water into the soil.The antecedent soil moisture and the surface roughness are both regarded by Evans (1980) as important soil factors touch erosion. The ability of a soil to accept rainfall depends on the moisture content at the time of the rainfall event.2.5.3.1 Factors affecting aggregate stabilitySoil structure is determined by the shape and size distribution of aggregates. Aggregrate size and strengthe determine the physical properties of a soil and its susceptibility to breakdown due to water forces. Their stability will have a decisive effect on soil physical properties (Lynch and Bragg, 1985). The main binding materials giving stable aggregates in air dry state are the glueing agents in organic matter (Chaney and Swift, 1984 Tisdale and Oades, 1982) and sesquioxides (Goldberg and Glaubic, 1987).2.5.3.1.1 Aluminium and Iron OxidesThe soil used by Kemper and Koch (1966) contained relatively little free iron, although it did contribute to aggregrate stability. Their info show a nippy increase of free iron from 1 to 3%. Goldberg and Glaubic (1987) concluded that Al-oxides were more effective than Fe-oxides in stabilizing soil structure. Al-oxides have a greater proportion of sub-micrometer size particles in a sheet form as opposed to the spherical form of Fe-particles.Shainberg, vocalist and Janitzky (1987) compared the effect of aluminium and iron oxides on the hydraulic condu ctivity of a sandy soil.2.5.3.1.2 Organic MatterOrganic matter can bind soil particles together into stable soil aggregates. The stabilizing effect of organic matter is well documented. Little detailed information is available on the organic matter content required to sufficiently strengthen aggregates with extrasensory perception values greater than 5 or 7, and containing illite or montmorrillionite, so as to prevent their dispersion in water (Smith, 1990). High humus content makes the soil less susceptible to the unfavourable influence of sodium (Van den Berg, De Boer, Van der Malen, Verhoeven, Westerhof and Zuur, 1953). Kemper and Koch (1966) also found that aggregate stability increased with an increase in the organic matter content of soils. A maximum increase of aggregate stability was found with up to 2% organic matter, aft(prenominal) which aggregate stability increased very little with further increases in organic matter content.2.5.3 Slope FactorsSlope characteristics ar e important in determining the amount of runoff and erosion ( DHuyvetter, 1985). As slope gradient increases, runoff and erosion usually increases (Stern, 1990). At low slopes due to the low overland flow velocities, detachment of soil particles from the soil surface into the water layer is due to detachment alone (Stern, 1990). Additionally, at low slope gradients, particles are splashed into the air in random directions unlike the case with steeply sloping land where down slope splash occurs (Watson and Laflen, 1985).As slope gradient increases, the ability for surface runoff to entrain and transport sediments increases rapidly until the entrainment by the surface runoff becomes dominant contributing to sediment transport (Stern, 1990). Foster , Meyer and Onstad (1976) presented a conceptual model that showed that at lower slopes, interill transport determined erosion, while at steeper slopes, raindrop detachment determined it. Th uniform bed characteristics of sheet flow transpor t tend to be replaced by channels because of instability and turbulent flow effects (Moss, Green and Hutka, 1982).There are many confirmable relationships relating soil transport by surface wash to slope length and slope gradient. Zingg (1940) showed that erosion varied according to the equationS = X1.6 tanB1.4Where S = soil transport cm/yrX = slope length (m)B = slope gradient (%)Studies conducted by Gerrard (1981), showed that plane and convex slopes did not differ significantly in the amount of soil lost by surface runoff, but concave slopes were less eroded.Some researchers such as Zingg (1940) and Mc poise et al (1987) indicated that soil erosion increases exponentially with increase in slope gradient. The relationship is indicated by and by Zing (1940) by E = aSb where E is the soil erosion, S is the slope gradient (%) and a and b are empirical constants. The value of b ranges from 1.35 to 2.0. The other relationship between erosion and slope gradient for inter-rill erosion is given by Mc Cool et al (1987)E = a sin b Q+CQ is the slope angle in degreesA,b and C are empirical constants.However, even if the effect of slope gradient on erosion is well recognized, several studies indicate that the power relationship between slope gradient and soil loss over predicts interrill erosion rate by as much as two or more times (Torri, 1996Fox and Bryan, 1999), and the relationship is better described as linear.2.8 Soil Erosion Impacts2.8.1 Soil Physical PropertiesProgressive soil erosion increases the magnitude of soil related constraints for crop production. These constraints can be physical, chemical and biological. The important physical constraints caused by erosion are reduced rooting depth, loss of soil water storing capacity (Schertz et al 1984 Sertsu, 2000), crusting and soil compaction and hardening of plinthite (Lal, 1988). Erosion also results in the loss of clay colloids due to preferential removal of fine particles from the soil surface (Fullen and B randsma, 1995). The loss of clay influences soil tilth and consistency. Exposed subsoil is often of enormous structure and harder consistency than the aggregated surface soil (Lal, 1988).Development of rills and gullies may change the micro-relief that may make use of farming machinery difficult. Another effect of erosion is that the manangement and timing of farm operations.2.8.2 Soil chemical substance PropertiesSoil erosion reduces the fertility status of soils (Morgan, 1986 Williams et al., 1990). Soil chemical constraints and nutritional problems related to soil erosion include low CEC, low plant nutrients (NPK) and trace elements (Lal, 1988 Fullen and Brandsma, 1995). Massy et al (1953) reported an average loss of 192 kg of organic matter, 10.6 kg of N and 1.8kg per ha on a Winsconsin soils with 11% slope. Sharpley and Smith (1990) reported that the mean annual loss of total P in runoff from P fertilized watersheds is equivalent to an average of 15%, 12% and 32% of the annual fertilizer P applied to wheat, mixed crop grass and peanut genus Sorghum rotation practices respectively. Researchers (Massy et al 1953 Lal, 1975) have also reported extensive loss of N in eroded sediments.2.8.3 ProductivityQuantifying the effects on crop yields is a difficult task. It involves the evaluation of interactions between soil properties, crop characteristics and climate. The effects are also cumulative and not observed until long after accelerated erosion begins. The degree of soil erosions effects on crop yield depends on soil profile characteristics and management systems. It is difficult to evidence a direct relationship between rates of soil erosion and erosion induced soil degradation on the one hand and crop yield on the other (Lal, 1988).It is well known that soil erosion can reduce crop yields through loss of nutrients, morphological degradation and reduce of depth and water holding capacity (Timilin et al, 1986 Lal,1988). difference of production in eroded soil further degrades its productivity which in turn accelerates soil erosion. The cumulative effect observed over a long period of time may lead to irreversible loss of productivity in shallow soils with hardened plinthite or in soils that respond to expensive management and additional inputs (Lal,1988).2.8.4 Off Site Effects of Soil Erosion.Effects of erosion include siltation of rivers, crop failure at low lying areas due to flooding, pollution of waterbodies due to the various chemicals brought by the runoff from different areas. Several studies reported the significance of the off site effects of soil erosion on land degradation (eg. Wall and ven Den,1987 Lo, 1990 Robertson and Colletti, 1994 Petkovic et al, 1999) rainfall washes away materials that originate from fertilizers and various biocides (fungicides, insecticides, herbicides and pesticides) which are applied in large concentrations. They reappear in greatr quantities in the hydrosphere polluting and contaminating the water environment (Zachar,1982Withers, and Lord, 2002 Verstraeten and Poesen, 2002). Chemical pollution of water mainly by organic matter from farm fields causes rapid eutrophication in waterways (Zachar, 1982Zakova et al, 1993 Lijklema, 1995).2.8.5 Soil Erosion modalitylsModelling soil erosion is the process of mathematically describing soil particle detachment, transport and deposition on land surfaces (Nearing et al, 1994). Erosion models are used as predictive tools for assessing soil loss and project planning. They can also be used for understanding erosion processes and their impacts (Nearing et al 1994). There are three main types of models, empirical or statistical models, conceptual models and physically base models (Morgan 1995, Nearing et al 1994, Merritt et al 2003). It is important to note however that there is no sharp difference among them.2.8.5.1 Physically Based ModelsThese models are based on resolving fundamental physical equations describing stream flow and s ediment and associated nutrient generations in a specific catchment (Merritt et al ., 2003). They are developed to predict the spatial distribution of runoff and sediment over land surfaces during individual storms in addition to total runoff and soil loss (Morgan, 1995). Physically based models are also called process based models (Morgan, 1995) as they rely on empirical equations to determine erosion processes. These models use a particular differential gear equation known as the continuity equation which is a education of conservation of matter as it moves through space over time. The common physically based models used in water quality studies and erosion include The Areal Non-Point Source Watershed Environment Response show (ANSWERS) (Beasley et al., 1980), Chemical Runoff and Erosion from Agricultural Management dusts (CREAMS) (Knisel, 1980), Griffith University Erosion System Template (GUEST) (Misra and Rose, 1996), European Soil Erosion Model (EUROSEM) (Morgan, 1998), Pr oductivity, Erosion and Runoff, Functions to quantify Conservation Techniques (PERFECT) (Littleboy et al., 1992) and Water Erosion Prediction Project (WEPP) (Laflen et al., 1991).2.8.5.2 Empirical Mode