To determine the California bearing ratio by conducting a load penetration test in the laboratory.
NEED AND SCOPE
The California bearing ratio test is a penetration test meant for the evaluation of subgrade strength of roads and pavements. The results obtained by these tests are used with the empirical curves to determine the thickness of pavement and its component layers. This is the most widely used method for the design of flexible pavement.
This instruction sheet covers the laboratory method for the determination of C.B.R. of undisturbed and remoulded /compacted soil specimens, both in soaked as well as an unsoaked state.
PLANNING AND ORGANIZATION
Types of equipment and tool required.
1. Cylindrical mould with inside dia 150 mm and height 175 mm, provided with a detachable extension collar 50 mm height and a detachable perforated base plate 10 mm thick.
2. Spacer disc 148 mm in dia and 47.7 mm in height along with the handle.
3. Metal rammers. Weight 2.6 kg with a drop of 310 mm (or) weight 4.89 kg a drop 450 mm.
4. Weights. One annular metal weight and several slotted weights weighing 2.5 kg each, 147 mm in dia, with a central hole 53 mm in diameter.
5. Loading machine. With a capacity of at least 5000 kg and equipped with a movable head or base that travels at a uniform rate of 1.25 mm/min. Complete with load indicating device.
6. Metal penetration piston 50 mm dia and a minimum of 100 mm in length.
7. Two dial gauges reading to 0.01 mm.
8. Sieves. 4.75 mm and 20 mm I.S. Sieves.
9. Miscellaneous apparatus, such as a mixing bowl, straight edge, scales soaking tank or pan, drying oven, filter paper and containers.
DEFINITION OF C.B.R.
It is the ratio of force per unit area required to penetrate a soil mass with a standard circular piston at the rate of 1.25 mm/min. to that required for the corresponding penetration of a standard material.
C.B.R. = Test load/Standard load X 100
The following table gives the standard loads adopted for different penetrations for the standard material with a C.B.R. value of 100%
Penetration of plunger (mm)
Standard load (kg)
2.5 5.0 7.5 10.0 12.5
1370 2055 2630 3180 3600
The test may be performed on undisturbed specimens and on remoulded specimens which may be compacted either statically or dynamically.
PREPARATION OF TEST SPECIMEN
Undisturbed specimen
Attach the cutting edge to the mould and push it gently into the ground. Remove the soil from the outside of the mould which is pushed in. When the mould is full of soil, remove it from weighing the soil with the mould or by any field method near the spot.
Determine the density
Remoulded specimen
Prepare the remoulded specimen at Proctors maximum dry density or any other density at which C.B.R> is required. Maintain the specimen at optimum moisture content or the field moisture as required. The material used should pass 20 mm I.S. sieve but it should be retained on 4.75 mm I.S. sieve. Prepare the specimen either by dynamic compaction or by static compaction.
Dynamic Compaction
Take about 4.5 to 5.5 kg of soil and mix thoroughly with the required water.
Fix the extension collar and the base plate to the mould. Insert the spacer disc over the base (See Fig.). Place the filter paper on the top of the spacer disc.
Compact the mix soil in the mould using either light compaction or heavy compaction. For light compaction, compact the soil in 3 equal layers, each layer being given 55 blows by the 2.6 kg rammer. For heavy compaction compact the soil in 5 layers, 56 blows to each layer by the 4.89 kg rammer.
Remove the collar and trim off the soil.
Turn the mould upside down and remove the base plate and the displacer disc.
Weigh the mould with compacted soil and determine the bulk density and dry density.
Put filter paper on the top of the compacted soil (collar side) and clamp the perforated base plate on to it.
Static compaction
Calculate the weight of the wet soil at the required water content to give the desired density when occupying the standard specimen volume in the mould from the expression.
W =desired dry density * (1+w) V
Where W = Weight of the wet soil
w = desired water content
V = volume of the specimen in the mould = 2250 cm3 (as per the mould available in the laboratory)
Take the weight W (calculated as above) of the mixed soil and place it in the mould.
Place a filter paper and the displacer disc on the top of the soil.
Keep the mould assembly in static loading frame and compact by pressing the displacer disc till the level of disc reaches the top of the mould.
Keep the load for some time and then release the load. Remove the displacer disc.
The test may be conducted for both soaked as well as unsoaked conditions.
If the sample is to be soaked, in both cases of compaction, put a filter paper on the top of the soil and place the adjustable stem and perforated plate on the top of filter paper.
Put annular weights to produce a surcharge equal to the weight of base material and pavement expected in actual construction. Each 2.5 kg weight is equivalent to 7 cm construction. A minimum of two weights should be put.
Immerse the mould assembly and weights in a tank of water and soak it for 96 hours. Remove the mould from the tank.
Note the consolidation of the specimen.
Procedure for Penetration Test
Place the mould assembly with the surcharge weights on the penetration test machine. (Fig.).
Seat the penetration piston at the centre of the specimen with the smallest possible load, but in no case in excess of 4 kg so that full contact of the piston on the sample is established.
Set the stress and strain dial gauge to read zero. Apply the load on the piston so that the penetration rate is about 1.25 mm/min.
Record the load readings at penetrations of 0.5, 1.0, 1.5, 2.0, 2.5, 3.0, 4.0, 5.0, 7.5, 10 and 12.5 mm. Note the maximum load and corresponding penetration if it occurs for a penetration less than 12.5 mm.
Detach the mould from the loading equipment. Take about 20 to 50 g of soil from the top 3 cm layer and determine the moisture content.
Observation and Recording
For Dynamic Compaction
Optimum water content (%)
Weight of mould + compacted specimen g
Weight of empty mould g
Weight of compacted specimen g
Volume of specimen cm3
Bulk density g/cc
Dry density g/cc
For static compaction
Dry density g/cc
Moulding water content %
Wet weight of the compacted soil, (W)g
Period of soaking 96 hrs. (4days).
For penetration Test
Calibration factor of the proving ring 1 Div. = 1.176 kg
Surcharge weight used (kg) 2.0 kg per 6 cm construction
Water content after penetration test %
Least count of penetration dial 1 Div. = 0.01 mm
If the initial portion of the curve is concave upwards, apply correction by drawing a tangent to the curve at the point of greatest slope and shift the origin (Fig. 40). Find and record the correct load reading corresponding to each penetration.
C.B.R. = PT/PS X 100
where PT = Corrected test load corresponding to the chosen penetration from the load penetration curve.
PS = Standard load for the same penetration taken from the table I.
Penetration Dial
Load Dial
Corrected Load
Readings
Penetration (mm)
proving ring reading
Load (kg)
Interpretation and recording
C.B.R. of the specimen at 2.5 mm penetration
C.B.R. of the specimen at 5.0 mm penetration
C.B.R. of the specimen at 2.5 mm penetration
The C.B.R. values are usually calculated for penetration of 2.5 mm and 5 mm. Generally, the C.B.R. value at 2.5 mm will be greater than at 5 mm and in such a case/the former shall be taken as C.B.R. for design purpose. If C.B.R. for 5 mm exceeds that for 2.5 mm, the test should be repeated. If identical results follow, the C.B.R. corresponding to 5 mm penetration should be taken for design.
Compaction is the process in which sediment is squeezed and in which the size of the pore space between sediment grains is reduced by the weight and pressure of overlying layers.
Cementation is the process in which sediments are glued together by minerals that are deposited by water.
Unified
soil classification system is adopted by ASTM D-2487-98 and IS:
1498-1970 for classification and identification of soils for general
engineering purpose.
Soils are broadly classified into three divisions:
Coarse grained soils: In these soils, 50% or more of the total material by weight is larger than 75micron IS sieve size.
Fine grained soils: In these soils, 50% or more of the total material by weight is smaller than 75 micron IS sieve size.
Highly organic soils and other miscellaneous soil materials:
These
soils contain large percentage of fibrous organic matter, such as peat,
and the particles of decomposed vegetation. In addition, certain soils
containing shells, cinders and other non-soil materials in sufficient
quantities are also grouped in this division.
1. Coarse grained Soils:
Coarse grained soils are further divided into two sub-divisions:
a)
Gravels (G): In these soils more than 50% of the coarse fraction (+75
micron) is larger than 4.75 mm sieve size. This sub-division includes
gravels and gravelly soil, and is designated by symbol G.
b) Sands
(S): In these soils, more than 50% of the coarse fraction is smaller
than 4.75mm IS sieve size. This sub-division includes sands and sandy
soils.
Each of the above sub-divisions are further divided into four groups depending upon grading and inclusion of other materials.
W : Well Graded
C : Clay binder
P : Poorly graded
M : Containing fine materials not covered in other groups.
These symbols used in combination to designate the type of grained soils. For example, GC means clayey gravels.
2. Fine grained soils:
Fine grained soils are further divided into three sub-divisions:
a) Inorganic silts and very fine sands: M
b) Inorganic clays: C
c) Organic silts and clays and organic matter: O.
The
fine grained soils are further divided into the following groups on the
basis of the following arbitrarily selected values of liquid limit
which is a good index of compressibility:
i) Silts and clays of low compressibility:
Having a liquid limit less than 35 and represented by symbol L.
ii) Silts and clays of medium compressibility:
Having a liquid limit greater than 35 and less than 50 and represented by symbol I.
iii) Silts and clays of high compressibility:
Having a liquid limit greater than 50 and represented by a symbol H.
Combination
of these symbols indicates the type of fine grained soil. For example,
ML means inorganic silt with low to medium compressibility.
Unified Soil Classification System and Symbol Chart:
Fig: Unified soil classification system for coarse grained soils
Fig: Unified soil classification system for fine grained soils
Fig: Soil Plasticity chart as per Unified soil classification system
Subgrade is one of the most crucial part of embankment fills or natural surface just below the sub-base or lower sub-base of road pavement and shoulder. The surface above the subgrade is known as the formation level or finishing level. Subgrade is the in situ material upon which the pavement structure is placed or constructed at selected location.
Formation level is defined as the final level of soil surface after completion of earthworks and when trough the process of compaction, stabilization and reinforced. The subgrade main function is to withstand the loading of road pavement (sub-base, base, etc.) above it.
Although there is a tendency by looking at the pavement performance in terms of pavement structure and mix design alone, the subgrade can often be the overriding factor in pavement performance.
Unsuitable Materials for Subgrade
The soil number one enemy is water which effect the quality
Not every soil is suitable of becoming filing or embankment materials in road construction. Some consideration should be made in terms of specification and observation in choosing the right soil.
Unsuitable soil materials for subgrade (or embankment fills) are as follows:
Clay soil which contains the value of Liquid Limit more than 80% and/or Plasticity Index more than 55%,
Having the value of Lost On Ignition (LOI) more than 2.5%,
It is flammable materials (oily), and organically clay soil,
Contain lots of rotten roots, grass and other vegetation,
Considered as unstainable soil or toxic and categorized as peat soil,
Soil which is soft and unstable because it is too wet or dry which makes it difficult to compact properly.
Testing for Subgrade
The Casagrande Apparatus
There are several testing method that were used
to test the subgrade layer and also embankment layers. The notable and most recommended test (among others) to be carryout are as follows:
California Bearing Ratio (CBR), as accordance to: BS 1377: Part 4 1990, ASTM D1883-05 or AASHTO T-193
Compaction Test, as accordance to: BS 1377: Part 4 1990, ASTM D-698 or AASHTO T-99
Liquid Limit (LL) and Plastic Limit (PL)test, as accordance to: BS 1377: Part 2 1990, ASTM D-4318 or AASHTO T-89
Lost On Ignition (LOI) test, as accordance to: BS 1377: Part 3 1990 or AASHTO T-267
Performance of Subgrade The subgrade’s performance generally depends on two interrelated characteristics: Load Bearing Capacity The subgrade must be able to sustain loads transmitted from the pavement structure. The load bearing capacity is frequently affected by the types of soil, moisture content, and degree of compaction. A subgrade that can sustain a highly sum of loading without an excessive deformation was considered good quality.
The types of soil especially from gravel type considered the best and from peat type considered as the worst material. Moisture content of soil is also important and determine by conducting the soil compaction test at lab as to find out which type contains more water. The degree of compaction normally reflect to the method of compaction used at construction site, by means of machinery and the numbers of passes.
Changing in Volumes In most cases, soils will undergo some amount of changes in volume when exposed to excessive moisture, rise in temperature or in freezing conditions. For instance, some clay soils would shrink and swell depending upon its moisture content, whereas soils with excessive fines may be susceptible to frost heave in freezing areas.
As a conclusion, the subgrade must be form properly to prevent any possible damage to the road pavement. Factors of choosing the right or suitable materials, affecting the strength, materials specification, materials classification, and method of testing is vital for the road construction especially in earthworks stage.
Soil erosion by water, wind and tillage affects both agriculture and the natural environment. Soil loss, and its associated impacts, is one of the most important (yet probably the least well-known) of today's environmental problems.
"The threat of nuclear weapons and man's ability to destroy the environment are really alarming. And yet there are other almost imperceptible changes - I am thinking of the exhaustion of our natural resources, and especially of soil erosion - and these are perhaps more dangerous still, because once we begin to feel their repercussions it will be too late." (p144 of The Dalai Lama's Little Book of Inner Peace: 2002, Element Books, London)
It isn't easy to find comprehensive information on erosion, however. To a large extent this is because soil erosion does not fit neatly under any one heading: it is studied by geomorphologists, agricultural engineers, soil scientists, hydrologists and others; and is of interest to policy-makers, farmers, environmentalists and many other individuals and groups.
The Soil Erosion Site brings together reliable information on soil erosion from a wide range of disciplines and sources. It aims to be the definitive internet source for those wishing to find out more about soil loss and soil conservation.
What is soil erosion?
Soil is naturally removed by the action of water or wind: such 'background' (or 'geological') soil erosion has been occurring for some 450 million years, since the first land plants formed the first soil. Even before this, natural processes moved loose rock, or regolith, off the Earth's surface, just as has happened on the planet Mars. In general, background erosion removes soil at roughly the same rate as soil is formed. But 'accelerated' soil erosion — loss of soil at a much faster rate than it is formed — is a far more recent problem. It is always a result of mankind's unwise actions, such as overgrazing or unsuitable cultivation practices. These leave the land unprotected and vulnerable. Then, during times of erosive rainfall or windstorms, soil may be detached, transported, and (possibly travelling a long distance) deposited. Accelerated soil erosion by water or wind may affect both agricultural areas and the natural environment, and is one of the most widespread of today's environmental problems. It has impacts which are both on-site (at the place where the soil is detached) and off-site (wherever the eroded soil ends up). More recently still, the use of powerful agricultural implements has, in some parts of the world, led to damaging amounts of soil moving downslope merely under the action of gravity: this is so-called tillage erosion. Soil erosion is just one form of soil degradation. Other kinds of soil degradation include salinisation, nutrient loss, and compaction.
Soil Erodibility
Soil erodibility is an estimate of the ability of soils to resist erosion, based on the physical characteristics of each soil. Generally, soils with faster infiltration rates, higher levels of organic matter and improved soil structure have a greater resistance to erosion. Sand, sandy loam and loam textured soils tend to be less erodible than silt, very fine sand, and certain clay textured soils.
Tillage and cropping practices which lower soil organic matter levels, cause poor soil structure, and result of compacted contribute to increases in soil erodibility. Decreased infiltration and increased runoff can be a result of compacted subsurface soil layers. A decrease in infiltration can also be caused by a formation of a soil crust, which tends to "seal" the surface. On some sites, a soil crust might decrease the amount of soil loss from sheet or rain splash erosion, however, a corresponding increase in the amount of runoff water can contribute to greater rill erosion problems.
Past erosion has an effect on a soils' erodibility for a number of reasons. Many exposed subsurface soils on eroded sites tend to be more erodible than the original soils were, because of their poorer structure and lower organic matter. The lower nutrient levels often associated with subsoils contribute to lower crop yields and generally poorer crop cover, which in turn provides less crop protection for the soil.
Slope Gradient and Length
Naturally, the steeper the slope of a field, the greater the amount of soil loss from erosion by water. Soil erosion by water also increases as the slope length increases due to the greater accumulation of runoff. Consolidation of small fields into larger ones often results in longer slope lengths with increased erosion potential, due to increased velocity of water which permits a greater degree of scouring (carrying capacity for sediment).
Vegetation
Soil erosion potential is increased if the soil has no or very little vegetative cover of plants and/or crop residues. Plant and residue cover protects the soil from raindrop impact and splash, tends to slow down the movement of surface runoff and allows excess surface water to infiltrate.
The erosion-reducing effectiveness of plant and/or residue covers depends on the type, extent and quantity of cover. Vegetation and residue combinations that completely cover the soil, and which intercept all falling raindrops at and close to the surface and the most efficient in controlling soil (e.g. forests, permanent grasses ). Partially incorporated residues and residual roots are also important as these provide channels that allow surface water to move into the soil.
The effectiveness of any crop, management system or protective cover also depends on how much protection is available at various periods during the year, relative to the amount of erosive rainfall that falls during these periods. In this respect, crops which provide a food, protective cover for a major portion of the year (for example, alfalfa or winter cover crops) can reduce erosion much more than can crops which leave the soil bare for a longer period of time (e.g. row crops) and particularly during periods of high erosive rainfall (spring and summer). However, most of the erosion on annual row crop land can be reduced by leaving a residue cover greater than 30% after harvest and over the winter months, or by inter-seeding a forage crop (e.g. red clover).
Soil erosion potential is affected by tillage operations, depending on the depth, direction and timing of plowing, the type of tillage equipment and the number of passes. Generally, the less the disturbance of vegetation or residue cover at or near the surface, the more effective the tillage practice in reducing erosion.
Conservation Measures
Certain conservation measures can reduce soil erosion by both water and wind. Tillage and cropping practices, as well a land management practices, directly affect the overall soil erosion problem and solutions on a farm. When crop rotations or changing tillage practices are not enough to control erosion on a field, a combination of approaches or more extreme measures might be necessary. For example, contour plowing, strip cropping, or terracing may be considered.
Erosion processes
Soil may be detached and moved by water, wind or tillage. These three however differ greatly in terms of:
where and when they occur
what happens to the area that is being eroded (on-site impacts)
how far the eroded soil is moved, and
if the soil is moved away from the place where it was eroded, what happens as a result (off-site impacts).
Rainsplash
Rain may move soil directly: this is known as 'rainsplash erosion' (or just 'splash erosion'). Spash is only effective if the rain falls with sufficient intensity. If it does, then as the raindrops hit bare soil, their kinetic energy is able to detach and move soil particles a short distance.
Because soil particles can only be moved a few centimetres at most by this process, its effects are solely on-site. Although considerable quantities of soil may be moved by rainsplash, it is all merely redistributed back over the surface of the soil (on steep slopes, however, there will be a modest net downslope movement of splashed soil). Thus a more descriptive term might be 'rainsplash redistribution'.
Because rainsplash requires high rainfall intensities, it is most effective under convective rainstorms in the world’s equatorial regions. Rainsplash is relatively ineffective where rain falls with a low intensity (e.g. because the rainfall is of frontal origin), such as in the north-west of the USA or in northern Europe.
Rill and gully erosion
Rainfall may also move soil indirectly, by means of runoff in rills (small channels) or gullies (larger channels, too big to be removed by tillage). In many parts of the world, rill and gully erosion is the dominant form of water erosion.
That fraction of the rainfall which does not infiltrate (soak into) the soil will flow downhill under the action of gravity; it is then known as runoff or overland flow. Runoff may occur for two reasons. Firstly, if rain arrives too quickly (i.e. with too high an intensity) for it to infiltrate: the runoff which results is then known as infiltration excess runoff, or Hortonian runoff. Secondly, runoff may occur if the soil has already absorbed all the water it can hold (i.e. because it is fully saturated, or if the soil is frozen). Runoff which results from this situation is known as saturation excess runoff.
As runoff moves downhill, it is at first a thin diffuse film of water which has lost virtually all the kinetic energy which it possessed as falling rain. Thus it moves only slowly, has a low flow power, and is generally incapable of detaching or transporting soil particles.
The microtopography (i.e. small-scale pattern of irregularities) of the soil’s surface tends to cause this overland flow to concentrate in closed depressions, which slowly fill: this is known as ‘detention storage’ or ‘ponding’. Both the flowing water, and the water in detention storage, protect the soil from raindrop impact, so that rainsplash redistribution usually decreases over time within a storm, as the depth of surface water increases. There are, however, complex interactions between rainsplash and overland flow.
If rain continues, the increasing depth of water will eventually overtop the microtopographic depressions. Overland flow that is released in this way is likely to flow downhill more quickly and in greater quantities (i.e. possess more flow power as a result of its kinetic energy), and so may be able to begin transporting and even detaching soil particles. Where it does so, the soil’s surface will be lowered slightly. Lowered areas form preferential flow paths for subsequent flow, and these flow paths are in turn eroded further. Eventually, this positive feedback results in small, well-defined linear concentrations of overland flow (‘microrills’ or ‘traces’).
In many cases, individual microrills become ineffective over time due to sedimentation. A subset, however, grow further to become rills; and a smaller subset may go on to develop into gullies. This process of ‘competition’ between microrills and rills leads to the self-organized formation of networks of erosional channels (dendritic on natural soil surfaces; constrained by the direction of tillage on agricultural soils), which form efficient pathways for the removal of water from hillslopes. It is in such erosional channels that water erosion also operates most effectively to detach and remove soil by its kinetic energy. In most situations erosion by concentrated flow is the main agent of erosion by water.
The flow-dominated erosional channels are separated by interrill areas where the dominant processes are rainsplash and diffuse overland flow; however, boundaries between rill and interrill areas are both ill-defined and constantly shifting.
In some circumstances subsurface flow may be important in determining where channel erosion will begin and develop (e.g. at the base of slopes, and in areas of very deep soils such as tropical saprolites). Meltwater from thawing snow operates in a broadly similar way to rain-derived overland flow, detaching and transporting unfrozen soil in areas of concentrated flow. Snowmelt erosion is, though, less well studied and less well understood.
As erosional channels increase in size (i.e. grow to become large rills and gullies), processes such as gravitational collapse of channel walls and heads increase in importance. Runoff and sediment from rills and gullies may be moved into ditches, stream and rivers, and so transported well away from the point of origin. However, sediment may also be deposited within the rill or gully, or beyond the rill or gully’s confines in a depositional fan, at locations where the gradient slackens. Here it may be stored for a variable period of time, possibly being reworked by tillage activity, until a subsequent erosion event is of sufficient size to re-erode the stored sediment. It may then be redeposited further downstream, or make its way into a permanent watercourse and thence to lake or ocean.
Soil erosion in the past
Erosion of soil by water and wind has been occurring naturally since the first land plants formed the first soil, during the Silurian Period. Accelerated erosion is, from a geological perspective, of very recent origin; yet on a human timescale, accelerated erosion is old. There is considerable archaeological evidence from many parts of the world that accelerated erosion by water (in particular) is often associated with early agriculture.
In a scientific context, water erosion’s association with unwise agricultural practices was first noted within during the early decades of the 20th century by pioneers of soil conservation such as Hugh Hammond Bennett in the USA, and subsequently by workers in other parts of the globe.
During the period of colonialism, the imposed adoption of European agricultural methods frequently led to accelerated erosion in developing countries. There, the problem often continues to the present day.
In the last few decades of the 20th century, there was a worlwide move towards intensive agricultural technologies. These frequently leave the soil bare during times of heavy rainfall. As a result, previously problem-free areas of the world, such as north-west Europe, began to experience notable increases in water erosion.
The extent of soil erosion
Despite the global nature of the problem of erosion by water, even today we do not have good information regarding the global extent of erosion by water. Data on the severity of erosion is also often limited. The GLASOD study estimated that around 15 per cent of the Earth's ice-free land surface is afflicted by all forms of land degradation. Of this, accelerated soil erosion by water is responsible for about 56 per cent and wind erosion is responsible for about 28 per cent. This means that the area affected by water erosion is, very roughly, around 11 million square km., and the area affected by wind erosion is around 5.5 million square km. The area affected by tillage erosion is currently unknown. Because soil is formed slowly, it is essentially a finite resource. The severity of the global erosion problem is only now becoming widely appreciated.
Ways of Preventing Soil Erosion
1.Prevent soil erosion by planting vegetation, trees, ground cover, shrubs and any other plants. The roots from these plants will help hold the soil in place. Soil will not be easily blown away by wind, or washed away by the rain.
2.Create windbreaks, which are Hedges or fences of trees designed to reduce erosion, especially wind erosion. Plant them on different plots of lands.
3.Grow crops on farm lands. When land is not being used, use cover crops because they help prevent soil erosion by wind or rain. Beans are often used as cover crops.4.Apply mulch, which is; a protective covering of rotting vegetable matter spread to prevent soil erosion. The topsoil is will not be likely washed or blown away, when it’s covered by mulch.
Soil Erosion Prevention
Contour farming is another method that’s useful in preventing and controlling soil erosion by water runoff. It’s done by planting along the slope of a hill, following the natural contours of the land, instead of straight up and down or across.
Another method is that you could plant a cover crop when your land is not in use. Besides providing protection for your land, many cover crops are nitrogen-fixers, which mean they absorb nitrogen from the air and deliver it back to the land.
If you have a problem with wind erosion, try planting a windbreak. A windbreak can be a row of trees, bushes or even a plastic snow fence. Anything that will keep high winds from sweeping across your land can help prevent wind erosion.
Keeping your soil healthy is a very important step to take in preventing soil erosion. Soil that is rich in organic matter has better structure and is less susceptible to being washed or blown away. To keep your soil healthy, add plenty of compost each year and don’t over-till when you are planting.
Preventing soil erosion is always preferable to attempting to control or reverse it later. Once an area of land has been eroded, it’s sometimes impossible to correct it.
Soil Erosion Prevention Methods
There are many ways to prevention soil erosion from occurring on your land. There are also many products to assist you with this process. Before home or land owners choose a soil erosion prevention method they should accurately asses the soil erosion carefully before deciding on using a prevention product or methods. We will now discuss 4 top soil erosion prevention methods which will definitely help solve all soil erosion problems at a low cost.
Prevention Method 1: Planting Vegetation
One of the most common ways to prevent soil erosion on residential landscaped gardens and vegetation and crop properties is to plant flowers, trees and crops over the affect soil. Plants act as protective shields to the soil lessening the impact of rainfall, wind, excessive watering and ice melt. The plants will also help stabilize the soil and prevent it from becoming prone to soil erosion. Some popular soil erosion prevention plants are: wild flowers, crop veggies, small trees and herbs. Plants which crawl up and spread instead of growing upwards are also great soil erosion prevention plants.
Prevention Method 2: Matting
Soil erosion prevention products are available in many styles. One of the most common products which are most commonly used on residential properties, vegetation crops and vacant land is matting. Matting is available in wood fibres which make it environmentally friendly and biodegradable. The matting will be placed on the soils surface and prevent erosion from occurring. The matting will allow plants, crops and trees to grow through it and the soil will be healthy and stabilized. Matting can be cut to size to suit your property.
Prevention Method 3: Mulch/Fertilizer
Another soil erosion prevention method which is beneficial to the soil and plants which live in it, is applying a layer of mulch and fertilizer over the soil. The mulch and fertilizer layer will assist the soil to soak in water slowly and it will also lessen the impact of rainfall as it penetrates through to the soil. The mulch and fertilizer layer will also stabilize the affect soil by regaining its PH levels to be healthy and neutralized. Any type of mulch or fertilizer can be used to prevent soil erosion.
Prevention Method 4: Retaining Walls/Edging
Wet patches or mud puddles on your driveway, or any hardscaped area are a sign of soil erosion runoff. This is generally caused by water erosion. Water erosion is affecting the soil and making it expand and travel to different areas of the yard such as the driveway. You can prevent this from occurring by building a small retaining wall around your garden beds.
The retaining wall will act as a shield for the soil and prevent soil erosion from occurring. The wall will also keep water retained in the garden bed so that the soil will slowly soak it in. if used in conjunction with other soil erosion prevention methods this method can be very rewarding to your property.
A GIS-based model of soil erosion and transport
Soil erosion is a natural process that occurs when the force of wind, raindrops or running water on the soil surface exceeds the cohesive forces that bind the soil together. In general, vegetation cover protects the soil from the effects of these erosive forces. However, land management activities such as ploughing, burning or heavy grazing may disturb this protective layer, exposing the underlying soil. The decision making process in rural catchment management is often supported by the predictive modelling of soil erosion and sediment transport processes within the catchment, using established techniques such as the Universal Soil Loss Equation [USLE] and the Agricultural Nonpoint Source pollution model [AGNPS]
Wind Erosion Control
Management practices to control wind erosion are critical on sandy, muck, or peat soils, and should also be considered on clay or silty soils. Maintaining good soil structure and residue cover provides good resistance to wind erosion. Where little or no residue is left on the soil surface, (e.g., corn silage), a cover crop of winter rye may be sown to protect the surface of wind-susceptible soils until spring. Fencerows and snowfencing also provide good protection. Strip cropping, or even planting crops at right angles to prevailing winds is a method of controlling wind erosion on land susceptible to strong winds.
Tree windbreaks should be planted along the north and west boundaries of fields, and may be planted all around fields where wind erosion is a particular problem. On very steep slopes or areas where blowouts or rills/gullies frequently occur, permanent sod or tree cover should be maintained, and may in fact provide better financial returns.
Coral Reef Tells The History Of Soil Erosion
Coral reefs, like tree rings, are natural archives of climate change. But oceanic corals also provide a faithful account of how people make use of land through history, says Robert B. Dunbar of Stanford University. As per a research findings reported in the Feb. 22 issue of Geophysical Research Letters, Dunbar and colleagues used coral samples from the Indian Ocean to create a 300-year record of soil erosion in Kenya, the longest land-use archive ever obtained in corals. A chemical analysis of the corals revealed that Kenya has been losing valuable topsoil since the early 1900s, when British settlers began farming the region. "We observed that soil erosion in Kenya increased dramatically after World War I, coinciding with British colonialism and a series of large-scale agricultural experiments that provoked a dramatic change in human use of the landscape," said Dunbar, a professor of geological and environmental sciences. "Today, the Kenyan landscape continues to lose topsoil to the Indian Ocean, primarily because of human pressure". Erosion is a serious threat, he noted, because the loss of fertile soil often is accompanied by a decrease in food production. As per one recent study, soil erosion is a global problem that has caused widespread damage to agriculture and animal husbandry, placing about 2.6 billion people who are at risk of famine. "This is especially worrisome in East and sub-Saharan Africa, where per capita food production has declined for the last half-century," Dunbar said. Coral bands For the study, Dunbar and colleagues donned scuba gear and dove to the Malindi coral reef near the mouth of the Sabaki River, the second longest river in Kenya. Draining about 11 percent of Kenya's landmass, the Sabaki transports sediments to the sea.
The scientists took core samples from two large coral colonies, each more than 12 feet tall and about 15 feet wide. To find out how sediment flux has varied over the years, Dunbar's team measured the ratio of two elementsbarium and calciumin the coral skeleton, which is composed of calcium carbonate. "It turns out that there is a lot of barium in soils," Dunbar said. "So whenever something changes the landscape and causes the soil to erode and wash into the rivers, the soil is delivered to the sea. And with that soil comes the barium".
The corals then incorporate the barium in well-developed bands that provide a record of annual growth, similar to tree rings, he added. To measure barium levels in the corals, Dunbar's team applied an innovative technique that quickly vaporizes the carbonate, then analyzes its chemical composition with a mass spectrometer.
"In the past we used a dentist drill," Dunbar said. "We drilled out a little bit of powder, and then we dissolved the powder and took it to the lab, where we measured the barium with a wet chemical technique. It was a very slow process, very painful. It took forever to get data." The new method, developed by scientists at the Australian National University, "increased the speed at which we could collect data by a factor of 50," he noted.
Agricultural Soil Erosion Is Not Adding to Global Warming
Agricultural soil erosion is not a source of carbon dioxide to the atmosphere, as per research published online today (October 25) in the journal Science. The study was carried out by an international team of scientists from UC Davis, the Catholic University of Leuven in Belgium, and the University of Exeter in the U.K. Carbon emissions are of great concern worldwide because they, and other greenhouse gases, trap heat in the Earth's atmosphere and are a major cause of global climate change. "There is still little known about how much carbon exactly is released, versus captured, by different processes in terrestrial ecosystems," said Johan Six, a professor of agroecology at UC Davis and one of the study's authors. "We urgently need to quantify this if we are to develop sensible and cost-effective measures to combat climate change". In their new study, the scientists observed that erosion acts like a conveyor belt, excavating subsoil, passing it through surface soils and burying it in hollows downhill. During its journey, the soil absorbs carbon from plant material; when the soil is buried, so is the carbon. Erosion, therefore, creates what can be described as a "sink" of atmospheric carbon. The team improved prior estimates of the amount of carbon being sunk. Said lead author Kristof Van Oost of the Catholic University of Leuven, "Some academics have argued that soil erosion causes considerable emissions of carbon, and others that erosion is actually offsetting fossil-fuel emissions. Now, our research clearly shows that neither of these is the case". They observed that erosion captures the equivalent of about 1.5 percent of annual fossil-fuel emissions worldwide. Earlier studies suggested a broad range of erosion's effects, from a sink equaling 10 percent of fossil-fuel emissions, to a source equaling 13 percent. Even without major carbon impacts, the scientists said, erosion is a problem that must be addressed, because it has a detrimental effect on agricultural productivity and the surrounding environment.
Soil erosion: what we still don't know
Greater understanding of the occurrence, processes and impacts of soil erosion by water, wind and tillage is needed. Why? Both directly, in order to enhance mankind's ability to tackle the resulting environmental problems; and indirectly, in order to learn more about the processes of erosion and the conditions under which it occurs.
