chapter vi infiltration rates of soils for waters of...

CHAPTER VI

INFILTRATION RATES OF SOILS FOR WATERS OF DIFFERENT

SAR WITH DIFFERENT SALINITY LEVELS

The downward entry of water into soils is referred as

infiltration. The study of infiltration rates has special

significance in soil studies as it is influenced by many

factors such as chemical and physical status of the soil,

nature of the soil surface and profile. Infiltration rate

is defined as the volume of water passing into the soil per

unit of area per unit of time. It has the dimension of

-1 velocity (LT ).

When water, either from rain or irrigation,enters the

soil it immediately fills the uppermost layer of micropores.

At the same time some of the water is filled into the

continuous micropores by capillarity. Thus two types of

water movement, percolation (gravity flow) and capillarity,

work together in facilitating the irregular downward

penetration of water (67). If the infiltration is high the

soil interstices, both micro and macro,ultimately become

saturated to the full length of the profile until some

impervious layer is encountered. Under such circumstances,

the necessity of clearing off the micropores by drainage is

essential, otherwise the aeration conditions may

deteriorates. Certain factors further complicate the

percolation of water through soils,especially in the case

147

of saline-alkali and non-saline alkali soils. Clay

colloidal matter may clog not only the connecting channel,

but even the macropores, ultimately closing the smaller

pores. Secondly, entrapped air also impede the rate of

percolation.

In general, the finer the texture of the soil,slower

will be the rate of gravitational water flow. In sandy

soils the pores are large,amount of colloidal matter low

and flow will be easier. In heavy soils the pore spaces are

small and clogged with colloidal materials and the

contraction are many (34). The situation is further

aggravated in the case of a saline-alkali soil due to the

dispersion of the clay resulting from the hydrolysis of

exchangeable sodium in the soil matrix. Unless granulation

is encouraged by organic matter and other means,drainage in

such case will be slow and often ineffective.

According to Russell (61),plant growth on soils depends

directly on the presence of air,water and nutrients as well

as on suitable conditions of temperature and light. Under

normal circumstances, the soil complex contains sufficient

amount of nutrients which are released to the ·plant

gradually. The interspace between particles provides

sufficient water storage and at the same time permits

necessary aeration to the plant roots. When all conditions

are favourable the soil is known as a fertile soil. Wollny

(69) considered

physical properties

large

of

number

the soil.

of factors

According

influencing

to him, in

compact soil,the soil behaviour with regard to aeration and

148

availability of the air and water to the plants can be

considered poor. King (27) attempted to determine the

effective diameter of the pores by means of rate of flow of

air into a column of a soil. He also concluded from his

experiments

properties

colloidal

that clay and humus controlled the physical

of the soil due to high surface activity of clay

materials. The soil colloids will suffer either

dispersion

will form

due to the presence of high amounts of sodium or

large aggregates in presence of calcium or

organic matter. It is known that the stability of the clay

suspension is decided by the magnitude of the electric

charge (electric potential).

Wiegner (68),was the first to point out that the degree

of dispersion or stability of clay is determined by the

nature of the adsorbed cation. He showed that the stability

of the clay particles saturated with different cations

follows the Hofmester ion series:

L i > Na > K > Rb > Cs

In order to understand the factors influencing the

infiltration

the meaning

and allied

terminology

of America

rate and permeability,it is important to know

of the terms and the difference between these

terms. The report of the sub-committee on

has been published by the Soil Science Society

(55) in 1952. The downward entry of water into

the soil is known as infiltration. The infiltration rate

depends upon

of water in

physical condition of the soil and hydraulics

the profile,both of which may change rapidly

149

with time. The term infiltration velocity is the volume of

water moving downward into the soil surface per unit area

per unit time. The term infiltration velocity is close to

infiltration rate. However,infiltration velocities measured

with

the

small cylindrical infiltrometers will usually exceed

unless an adequate guard-ring infiltration rate

arrangement is used to control divergent flows in the soil

below the cylinder. Also,infiltration velocities measured

in water spreading

rate for the soil

operations may exceed the infiltration

if a considerable depth of water is

impounded. But if suitable controlled conditions are

maintained, infiltration rate and infiltration velocity will

have identical values.

The Darcy flow equation

V = K i2

expresses the proportionality between the flow velocity and

the

I K I

driving

in this

force in terms of the hydraulic gradient. The

practical unit

equation (the Darcy K) is commonly used as a

for expressing the permeability of soil to

water by soil scientists and engineers. The value of 1 K1

for a porous medium depends both on the nature of the

medium and the physical properties of water. The early

workers thought permeability as a property of medium alone.

A lot of confusion has been made regarding permeability and

its dependence or non-dependence on the fluid medium.There

are so many physical mechanisms and processes involved in

the flow of water in soil that,it is not clear as to how to

150

take into account all the variables in the fundamental

equation for soil permeability. For example,a change of a

few hundred parts per million in soluble electrolytes can

change the water flow rate in some agriculture soil by a

factor of 300. For media which have stable pore structure,

the permeability (intrinsic permeability) is the same for

liquid and gases.

Experience indicates that the infiltration rate of a

given soil can be high or low,depending on physical status

and management history. Infiltration rate is often

critically influenced by surface soil conditions, but

subsurface layers also are sometimes limiting. Water

distribution in the profile and depth of water applied are

modifying

high or

factors. The infiltration rate can be undesirably

undesirably low. It is the low end of the range

that may be a critical limiting factor in the agricultural

use of alkali soils. It is difficult to specify a boundary

limit between satisfactory and unsatisfactory infiltration

rates at the low end of the range,because so many factors

are involved,including the patience and skill of the farmer.

However, if the infiltration rate is less than 0.25 cm/hr

special water-management problems are involved that may

make an irrigation enterprise unprofitable for average

farmers.

~ow the chief problem of study by various soil

scientists has been the improvement of the saline alkali

soils. Alkali soils often have a dense block single grain

structure; they are hard to tili when dry and have low

151

hydraulic conductivity when wet. Reeve and co-workers (51)

have shown that, the ratio of air permeability to water

permeability for soils is an useful index of stability of

soil structure.Hendrick and co-workers (23) have shown that

dispersed soils may be effectively improved by synthetic

polyelectrolytes applied at the rate of 0.1 percent on the

dry soil basis.

The external surface area of most soils lie in the

range of 10-15 2 m l&m, whereas the internal surface area

varies to a greater extent. It is nil in soils that contain

inter-layer swelling mineral dnd as high as 1500 m2/gm no

or more in soils containing minerals of expanding-lattice

type. It is also known that the soils of arid region

contain clay fraction which contain higher proportion of

montmorillonite and illite and lower proportion of

kaolinite.

The leaching requirement is a ratio of the equivalent

depth of the drainage water to the depth of irrigation

water.

Leaching requirement = Dd /D. W lW

( 1,. R. )

Under the conditions of aerial application of

irrigation water, when no rainfall movement of salt in the

harvested crop and no precipitation of soluble constituents

in the soil takes place,then the leaching requirement can

be correlated as follows:

152

L.R. = Dd /0. = ECd /EC. W lW W lW

Where EC = electrical conductivity of the

respective waters

For irrigation waters with conductivity of 1,2 and 3

mrnhos/cm respectively,the leaching requirements will be 13,

25 and 38 percent·when EC . ' dw = 8 mhos/em for food crops,1s

the tolerable limit. In addition,rainfall,removal of salts

by the crops and precipitation of salts like caco3

or

gypsum will be the additional factors which will reduce the

value of leaching requirement. Leaching practice may vary

from region to region and hence different methods of

leaching may be required for different areas.

It has been found that the curves for a soil,relating

vapour pressure to moisture content, are affected by the

amount and nature of the colloids and the type of the

exchangeable cations on the surface of the clay. At a

relative humidity of 99.8 per cent hygroscopicity increases

according to the series.

L i > Na > H > Ba > Ca > K

At a relative humidity of 74.9%, this order is -

H > Ca > Li > Na > Ba > K

Kuron ( 2 9 ) has obtained similar data for clay from

Gabersdorf.At low vapour pressures,the adsorption series is

H > Mg > Ba > Ca > Na > K

At higher vapour pressures, the sodium saturated clay

adsorbs maximum water. Kuron (29) attributes such a

153

behaviour to the hydration of exchangeable cations. The

peculiar

that at

contains

entrance

behaviour of sodium ions is explained on the basis

low vapour pressure, the dehydrated sodium clay

a large number of pores that are too small for the

of water molecule;calcium clay,on the other hand,

is more open and is able to adsorb more water.

Jenny (26) considers that relative size of the ion is a

contributing factor in the hydration of alumino-silicates.

According to Jenny (26),different clays would be hydrated

according to the following scheme:

Li > Na > K

H >

Mg > Ca > Ba

Since Mg and Li ions are of the same size,Mg-system should

be more highly hydrated because there will be one half as

many ions

Ca-system

found that

present in the Mg as in the Li-system. Similarly

should be more hydrated than Na-system. It was

for Putnam clays (Beidellite),swelling varies

with the nature of the adsorbed cations as follows:

Li > Na > Ca > Ba > H > K

On the other hand, the order of swellingfor bentonite is:

Na > Li > K > Ca = Ba > H

Lutz ( 32) has found that lateritic colloids

(halloysite) do not swell,irrespective of the nature of the

adsorbed ion on the complex. The swelling of Li and Na

clays increases with increase in concentration of these

154

ions on the complex. Maximum swelling is reached at about

60% saturation of the exchange complex with Li ions. On the

other hand there is a continuous decrease in swelling as

the percentage of K-ions in the system increases.

Difference in strength with which these ions are held on

the surface, is not sufficient to explain a high degree of

variation in the swelling. Again the differences can not be

interpreted directly in terms of hydration of ions. The

Li-colloid attracts water molecules very strongly even to

the point of complete dispersion of aggregated system. The

K ions appear to hold the sheet like particles with much

energy than Li or Na ions. Hand Ca-clays do not swell much.

The relative swelling for the various systems is 1,1.7,1.8,

8 and 10 percent for K,Ba,Ca,Na and Li respectively.

The high swelling of bentonites suggests that the

bentonites attract large amount of water as a result of

forces associated with an inner layer of the colloidal

surface. Thus i t seems possible to interpret the

differences in swelling and hydration to variations in the

a t t r a c t i v e f or c e s o f t he 1 aye r a n d t he r e s u 1 t i n g i n c•r e a sed

mobility of the adsorbed ions, which causes measurable

osmotic type of swelling.

Terzaghi (64) has studied the swelling of elastic

systems with soil (porous structure). He has interpreted

that the swelling in this system is due to the combined

action of the surface tension of water in this system and

the elasticity of the solid component.

The flocculating power of active ions increases with

155

valency. Jenny and Reitemeir (26),have studied in detail

the significance of exchange reactions on the stability of

the clay systems, and have helped to clarify relations

between flocculating potential and ionic exchange. When KCl

is added as an electrolyte to a sodium clay,ion exchange

will take place and the lowering of potential is obtained

through exchange; while if KCl is added to K-clay,then

potential is lowered through repression as well as ion

exchange. In both the situations flocculation results.

It has been found by Myres (40),that H-humate forms

more stable aggregates with clays than Ca-saturated humus.

This result brings out the fact that flocculation is not

the same as granulation. In order to have stable

granulation there must be cementation of the flocculated

particles. It is obvious that adsorbed calcium is n~ cementing agent. Most of the cementing agents in the soil

are irreversible or slowly reversible inorganic and organic

colloids. Stable aggregate formation cannot take place

sands or silts in absence of colloids. The soil colloid

material may be divided into atleast three distinct groups

as far as its cementation effects are concerned.

1. Clay particles themselves

2. Irreversible or slowly reversible inorganic colloids

such as oxides of iron and aluminium

3. Organic colloids.

Russell (60),has suggested that the aggregate formation

is dependent on an interaction between exchangeable cations

on the clay particles and the dispersion liquid. According

- --- --------------------------------------------------------------------------------------

156

to him, formation of aggregates is limited to particles

smaller than 1 \.l in diameter and it is a property of those

clays which have a relatively high base exchange capacity

and is brought about only by those liquids whose molecules

have an appreciable dipole moment. Russell (60) presents

the following theory about the mechanism of aggregate

formation. Each particle is surrounded by electrical double

layer, the outer one being diffused and consisting of

cations, while the inner layer consists of negative charges

presumably adsorbed on the surface of the particles. The

cations in the diffused layer move about in the water in

the same way as they do around a complex anion,as in the

Debye-Huckel theory of strong electrolytes. Since water

molecules possess dipole moment they tend to be oriented

along the lines of electric force,radiating from each ion

into the diffused layer and from each free charge on the

surface of the clay particle. A linking system is thus set

up consisting of: particle-oriented molecules cation

oriented wetting molecules particle.

As removal of water proceeds,an increasing proportion

of cations share their water envelope with the clay

particles and so the number of links increases. The links

also become stronger because they become shorter. In

consequence, the cohesion of the clay particles i.e. the

hardness of the crumb,increases. The main weakness in the

Russell hypothesis is the emphasis that is placed upon the

cation as the connecting link between the particles. The

same phenomenon can be explained on the basis of the

157

orientation of liquid molecules on colloidal surface as

developed by Langmuir and Harkins. The tenacity of the

bonds between clay and sand increases with decreasing

particle size. Sideri (63) considers that the tenacity does

not depend upon the naure of the adsorbed bases. Water is

considered to be bonded between the oriented particles.

Organic colloids cause a high degree of aggregation of

clay particles. Experience in the chemistry of Fe (OH) 3 has

shown that this hydrated colloid becomes almost completely

irreversible upon dehydration. There is sufficient evidence

to suggest that this irreversibility of colloidal Fe (OH) 3

is an important factor in the production of stable

aggregates in certain soils. Aggregation depends on the

climatic conditions e.g. the percentage aggregation in

Canada is 73% while it is only 25% in Texas. This is due to

the fact that there is a high percentage of organic matter

in Canada and a lower percentage in Texas. It may be

concluded that the aggregate formation in soils in

reclamation of saline-alkali soils depends upon:

1. The ·coagulation of flocculation of the colloidal

particles

2. The presence. of small primary particles that may be

aggregated

3. The cementation of the coagulated material into stable

aggregates.

The movement of soil water,through a given volume of

soil, must take place through the soil pore-space. Movement

of water through these pores is brought about by the action

158

of gravity or capillary pull,either alone or in combination.

According to the dominance of the moving force,the type of

water movement may be discussed from two points of view:

1. Water which moves in the larger pores primarily

through the action of gravity or movement in a

saturated soil, and

2. Water,which moves thorugh the action of capillary

forces from surface to surface, or in small pores

in the presence of numerous air-water interfaces

or movement in an unsaturated soil.

Soil moisture movement under unsaturated soil

conditions are compared with older concepts of capillarity

and the more recent analogies to the flow of heat or

electricity.

The flow of water in a soil may be expressed according

to Darcy•s equation:

V = - K Grad ¢

where Grad ¢ represents the change in the total water

moving forces per unit distance and K is the specific

conductivity or the amount of water which will flow in one

second across a unit cross-sectional area of soil

perpendicular to the direction of flow,when the value of <I>

changes at the rate of one unit per· centimeter.

The texture and the structure of the soil affect

capillary conductivity, as they influence the number,size

and continuity of the pores.

The capillary conductivity depends upon the kind of

159

soil, its state of packing and the moisture content. Those

particular soil properties that affect capillary movement

are included in the evaluation of K.

In general, the capillary permeability of different

textured groups are:

Sand < fine sand < loam < light clay < clay

For saturated flow the order of permeability is

reversed. These results point out that the water films in

sands become discontinuous of much lower tensions or

moisture contents than in clays. This is due to the fact

that clays possess a larger number of (larger) pores than

in sands.

The movement of capillary water downward takes place

under the combined influences of the gravitational

potential gradient (Grad$ and the capillary potential

gradient (Grad IV).

Philip ( 44) developed a method to calculate the

cumulative infiltration I in terms of power series.

00

I(t) = l: Jn ( e ) t n/2 ( 1 ) n=l

in which the coefficient Jn (0) are,again,calculated from

K(O) and 0(0), and coefficientS is called the sorptivity.

Differentiating above equation with respect to t,we get the

series for the infiltration rate i(t);

( 2 )

160

In practice, it is generally sufficient for an approximate

description of infiltration to replace equations (1) and

(2) by two parameter equations of the type

I(t) = St~ +At

I ( t ) = 1 St-~ + A 2 ( 3 )

where t is not too large. In the limit,as t approaches

infinity, the infiltration rate decreases monotonically to

its final asymptotic value i( <1> ).

However, at very large times,it is possible to represent

above equation (3) as:

~ . 1 St-~ + k I = St + Kt, l = 2 ( 4 )

where 'K' is the hydraulic conductivity of soil's upper

layer which in a uniform soil under ponding, is

approximately equal to the saturated conductivity Ks.

The effect of profile st~atification on infiltration

has been studied by Hanks and Bower (22),Miller and Gardner

(39). Hillel and Gardner (24) recognized three _stages

during transient infiltration into crust-capped profile.

The process of infiltration under rain sprinkler

irrigation was studied by Rubin (58, 59). The exact

relationship between porosity and soil permeability is yet

in the experimental stage. There are sufficient evidences

l

161

that the size, density of packing and hydration of the

particles have great effects upon permeability. Lutz (33)

has demonstrated that the permeability of clays increases

as hydration of the particles decreases. The relative

permeability of Davidson, Iredell, putnum and bentonite

colloids were found to be approximately 100,50,32 and 2

respectively. The relative degrees of hydration of these

systems were 0, 10, 35 and 100 respectively. These

differences are due to the nature of colloids since the

silica-sesquioxide ratio of these systems increases in the

same manner as the hydration. Basically,non-saline alkali,

saline-alkali, and saline non-alkali soils have different

physical properties. Soils differ in texture, levels of

salinity, amount of Caco 3 ~ amount of gypsum,type of clay

minerals as well as availability of different types of

waters in nature: hence there is a need for studying

infiltration rates and permeability of different types of

soils.

In the last twenty years ~normous development has taken

place in the field of study of infiltration,permeability

and the physical and chemical properties of the soil.

Studies on soil structure and the physical properties

of soil have been carried out by McGeorge and Breazeale

(36) and Reeve (52). The behaviour of soil in relation to

the percolating solution and its electrolyte content has

been critically observed by a large number of workers

including McNeal and co-workers (37,Reeve and Doering (53),

Gardner, Bower and co-workers (18),Elirc (13),Philips and

162

Farrell (48), Pack and his co-workers (43),Philip (44,45),

Reeve and Tamoddoni (54),Quirk (50),Brooks and Goertzen (8),

Agassi, Shainberg and Morin (1),Shainberg and Singer (62).

The infiltration behaviour of soils in relation to the

clay type and the associated swelling has been studied by

Klages (28), Gill and Sherman (19),Dettman (10),Aylmore and

Quirk (6), Norrish and Quirk (42),Michaels and Lin (38),

Norrish (41), Quirk (49), Agrawal et. al. (3),Ambergaonkar

(5). The problem of dispersion of soil and the role of

exchangeable sodium in relation to infiltration has been

brought out by Leland (30),Demnead (9),Reeve and Brook (51),

Richards (56) and Eaton and Horton (12).

be

According

hindered

to Agassi et. al. (1,2) infiltration may also

by aggregate destruction from rain drop impact

and resultant crust formation. In many areas of the world

which are characterized by high intensity rains and sodium

affected soils, both mechanisms, which are interrelated

operate to reduce soil water intake.

Agrawal and Ramamoorthy (4) have studied the effect of

saline irrigation water (Ec = 2250 umhos/cm,SAR = 14) on

soils of varying texture and observed that heavy textured

soils (montmorillonitic) showed more of salinity hazard as

compared (to Kaolinitic and Illitic) light textured soils,

whereas the reverse was the case for sodium hazard.

Phillip

concept of

has given a purely mathmatical

infiltration. It can be

treatment to the

said that the

infiltration theory incorporating the various aspects of

soil moisture, water movement and water depth have been

163

fully treated by Phillip (45, 46,47). The improvement in

infiltration rate on application of amendments and the

aggregation of soil particles has also been studied

extensively by Hendricks and co-workers (23), Letey and

co-workers (31), Bower (7),Marshell (35). Side by side the

techniques of measuring infiltration rate,permeability and

hydraulic conductivity have been revised from time to time.

This includes the work of Richards (55),Vries (65,66),Peck

an~ Talsma (43), Fireman (14), and Gardner (15, 16). In

addition some important applications have also been studied;

e.g .. the engineering aspects of the reclamation of sadie

soils with high salt waters has been critically studied by

Doering and Reeve (11). The application of the infiltration

theory to hydrology has been made by Gardner (17).

The Sodium Adsoption Ratio (SAR) is given by,

SAR

+ Na

This equation is used for evaluating the Exchangeable

Sodium Percentage (ESP) in the soil:

ESP = 10 ESF = 100 (Na)/CEC

Where ESF is the exchangeable sodium fraction. The

equilibrium exchangeable sodium fraction of soil that has

been equilibrated with water having a given SAR may be

approximated as:

164

ESF = SAR/(1/K + SAR)

However, on

depending

both SAR

upon

and

diluting

the SAR

the

a water the ESF will change,

and the extent of dilution. Thus,

salinity level will govern the

infiltration rates in soils.

In the present work, soil samples of different clay

types from Ahmedabad (CLAY TYPE:Kaolinite-Montmorillonite),

Amreli (CLAY TYPE: Montmorillonite) and Kutch (CLAY TYPE:

Kaolinite-Illite) district of Gujarat State were used

for infiltration studies. Waters with different SAR and

different salinity levels were used for infiltration study.

Infiltration rates were measured by using the modified

Dettman Emersion technique.

Table 6.1 shows composition of different SAR waters

varying in concentration.

Results for infiltration cates are presented in Table

No.6.2-6.6.

l

165

TABLE 6.1

COMPOSITION OF DIFFERENT SAR WATERS VARYING IN SALINITY LEVELS

SALT CONCENTRATION (Meq/Litre) TOTAL

SAR SALINITY NaCl CaCl 2 MgC1 2

(PPM)

15 75 25 25 9518

15 60 16 16 6793

15 30 4 4 2575

15 20 1. 7 5 1. 7 5 1529

30 150 25 25 13906

30 120 16 16 10303

30 90 9 9 7112

30 60 4 4 4330

45 200 19.79 19.79 15761

45 180 16 16 13813

45 90 4 4 6085

45 50 1. 23 1. 23 3177

60 240 16 16 17323

60 180 9 9 12377

60 120 4 4 7840

60 60 1 1 3715

75 225 9 9 15009

75 150 4 4 9595

75 90 1.44 1. 44 5560

75 50 0.44 0.44 3015

TABLE 6.2

INFILTRATION RATE (Cm/Hr) OF DIFFERENT SOILS OF DIFFERENT CLAY TYPES WITH DIFFERENT SAR WATER

SOIL : NORMAL SAR WATER 15

TOTAL SALINITY LEVEL (PPM)

TIME 9518 6793 2575 1529 (MIN. ) K-M M K-I K-M M K-1 K-M M K-1 K-M M K-1

1 318 96 132 420 132 138 252 96 96 294 108 84

2 84 42 30 180 48 54 156 24 24 78 24 36

3 108 36 30 - 24 12 60 36 24 90 18 30

4 48 36 30 24 12 60 12 18 36 1 8 1 8

5 - 30 12 24 6 - 18 12 - 12 12

6 18 18 12 18 12 12 12 6

7 18 6 36 6 18 12 18 12

8 12 18 18 12 12 6 24 6

9 12 24 18 12 12 12 18 G

10 12 24 12 12 6 24 18 6 ..... O'l O'l

TABLE 6.3

INI•'II.TR/\TION RATE {Cm/Hr) OF DIFFERENT SOILS OF DIFFERENT CLAY TYPES WITH DIFFERENT SAR WATER


TOTAL SALINITY LEVEL (PPM) TIME

13906 10303 7112 4330 (MIN. ) K-m M K-I K-M M K-I K-M M K-I K-M M K-I

1 276 72 144 300 138 108 252 108 96 240 102 120

2 132 36 18 196 72 12 126 36 18 172 42 18

3 60 18 18 114 30 24 84 24 30 102 30 6

4 90 18 12 66 18 18 72 18 18 106 24 12

5 30 24 12 30 24 18 60 6 12 liO 18 12

6 18 30 18 18 12 6 12 12

7 12 24 18 12 12 12 12 12

8 6 18 12 12 12 6 18 12

9 6 18 18 12 - 6 18 6 .....

10 6 18 12 6 12 - 12 12 0)

-..:)

----------------------- I

TABLE 6.4



TOTAL SALINITY LEVEL (PPM) TIME

(MIN. ) 15761 13813 6085 3177

K-M M K-I K-M M K-I K-M M K-I K-M M K-I

1 300 126 102 264 102 66 240 96 142 204 120 144

2 184 36 30 96 54 48 120 42 124 196 112 42

J 96 36 24 50 30 44 60 30 36 120 74 34

4 48 30 12 60 24 36 48 36 18 48 36 32

5 72 18 12 40 24 24 42 24 18 42 42 24

6 36 12 24 24 18 36 24 24 30 24 6

7 24 30 30 24 12 30 12 12 18 24 6

8 24 18 30 24 18 18 16 18 6

9 18 12 30 18 6 18 12 18 6

10 12 12 12 12 18 6 12 6

~

O'l 00

TABLE 6.5




TIME 17323 12377 7840 3715 (MIN. )

K-M M K-I K-M M K-I K-M M K-I K-M M K-I

1 336 102 78 318 96 120 258 90 102 240 96 96

2 90 42 30 160 36 24 90 36 42 84 30 24

3 96 30 24 102 24 24 90 42 24 84 30 12

4 90 30 18 90 24 12 60 30 24 72 24 12

5 18 18 18 24 12 48 30 18 GO 24 12

6 12 18 18 12 12 12 60 18 12

7 12 24 18 6 12 12 18 12

8 12 6 12 6 12 18 18 12

9 12 18 12 12 18 12 12 12

10 12 18 12 6 12 12 12 12 ...... en c.o

TAULE 6.6




TIME 15009 9595 5560 3015 (MIN. ) K-M M K-I K-M M K-I K-M M K-I K-M M K-I

1 240 96 72 246 84 72 240 60 96 246 108 78

2 120 76 30 90 24 30 102 30 30 108 24 18

3 78 48 24 84 18 24 78 30 24 90 24 18

4 no 24 18 60 18 24 90 18 18 72 12 24

5 78 24 12 54 6 1 2 60 18 18 48 12 18

6 12 12 54 6 12 60 18 24 1 8 1 8 18

7 12 18 6 12 18 1 2 18 12

8 18 12 12 6 12 6 18 6

9 12 12 6 6 12 6 6 12

10 12 12 6 6 12 6 12 12 f-lo

-...J 0

I lnfi!tr!l1101'l r!IIEO [ Qn!Hr I ~r----------------------

Clay Type K-M

SA A 15 300

:t i 0~'------~----~------~------~----~

2 3

Trme rn mnts. 4 0

ll 0- 96l8 pam -+- e 1 oo pam -+- Zfl 1 f> pam

Grapn No - 6.1

lnfil1r!11i0n r111e [ On/Hr ]

1001

:t ... -........ . __ .Clay _ _Type SA A 15

Ml

~~- --

:r ·-· oL-----L-----~----L-----~------~~--~ o z • e a 10

T rme rn mnts.

- Q61S ppm -+- 67QG pgm ..... ?576 pnwn -- 162Q pgm

Grap> No. - 6.2

lntll1r!l110f"l r!lle [ On/Hr I '200~--------------------------------~

4 6

Clay Type K-1

SA A 15

8 10

Trme rn mnts

~ W61B pgm -+- S7Qu pnwn ~ ~676 ppm ~ 162Q pgm

Grap> No. - 6.3

I I

171

:('"""'~·:tow~--.. ~Clay Type K-M I

l ~""' S A R 3 0

'Q .:.""

~I ~~-~~-- ·-. ............ '·

I] ~~~

l 0 2

l1me ~~ rnnts. 4 6

- 1SGO!I ppm -+- 10000 ppm --¥- 7112 ppm -- • 330 ppm

8llh NO. - C.•

r------------------------------------------------. I

lnliltreiiOn rille I On/Hr J 200,.--------------------------------------, Clay Type M

SA R 3 0

0 8 10

11me 1n ITI1tS.

~ 16006 ppm -+- 10606 ppm --¥- 7112 ppm -- •680 ppm

Gra!'fl No. - C-6

lnloltrelion rete I On/Hr l ~---------------------------------------.

160

100

Clay Type K-1 SA R 3 0

oi~----~----L-----~-

-. -i I

o • 0 0 •o 1unc 1n rnnts.

- 16006 ppm -+- 10000 ppm --¥- 7112 ppm -Q... •330 ppm

Grapn No. - C.O

172

r-1

lnfiltrctlon r!llg I On/Hr I

<00[ ---·-··----

Clay Type K-M 300 '

·~··· SAR 45

200

100 "~ '··

--+-0

0 2 4 6 a 10 12

T1me 1n mnts.

Gtepn NO - !I 7

lnfiltrctKJn rille I On/Hr ] 1~.---------------------------------------~

-- C~y TYf?e M SA R 4 5

00

()L------L---~-----~-

0 6 8 10

T 1me 1n mnts.

~ 16761 ppm -+- IS81S ppm ....,.._ 6086 ppm -- Sin ppm

Grat:n NO. - 6 8

"''('""•'~ <do I On!H• I

1.')0 r a

100

00

Clay Type K -I

SA R 4 5

12

ol_--~~-~~~~~~-~-~~~--__j o 2 4 e 8 10 12 1

L..G_r_a., __ N0 __ -_"-_~~ __ ~_6_76_1_"""' ___ -+-__ I_~_:_:oo_"""'_'_n_mr_..,._~~_:_· ·_86_ppm ____ -__ :._•7_7_"""'_j

173

\ I

I

- 17::123 epm

Gr•pn No - 6.10

: ('"''"'~ ·~• I ""'"' I

00~ 60

Clay Type K-M I I

SA R 6 0

QL-----~----~------~----~------~----~ 0 2 4 0 8 10

Time 1n mnts.

- 171!128 epm -+- 12877 epm -+- nwo ppm -a-- s 7\6 ppn

Gr•pn No. - a 11

lnftlt<llltQn rille ( On/Hr I ~~----------------------------------------~

9lay _Type K -I SA R 6 0

100

80

4 6 a 10

T 1rne 1n mnts.

I ~ 1rS2S ppm ~ 9716 ppn

L Grapn No.- al:!

174

175 r------------------------------------------------~

lnflltr11tkJn rllte ( On/Hr I ~-------------------------------~ Clay Type K-M :260

SA A 7 5 200

'o ol____----~--------~------~~------~

0 2 .. 0 8

T1me tn mnts - I600G ppm -+- Q6Q6 ppm ..... 66CO ppm -- 3016 ppm

Gralll'l No - CI.IS

lnflltr~tllan rl!le ( On!Hr I 1ror---------------------------------------~

Clay Type M 100

SA A 7 5 ao

20

OL'----~~----J------J------~----~----~

0 2 4 0 8 10

Time m mnts. - liSOOII ppm -+- gcjQC ppm ....... !lOGO ppm -- !10l6 ppm

Gr~ No.- Cl.14

lnflllr~tlian rl!le I On/Hr }

~----------------------------------------~

100 Clay Type K -I

SA R 7 5 ao

60

40 --

20 --- .. . 0

0 2 .. 0 8 10 12

L Gr~_N_o_. --_e -_,; __ •60<_JO_ppm __ -+-___ Q6_Til6_,rr_:n :'~ ----~-~·:_J

DISCUSSION

At the first sight it appears that Sodium Adsorption

Ratio (SAR) will be directly reflected as the base

saturation of a soil with Na+ with respect to Ca++ and Mg++

and we use the SARin the same context. But infiltration

rate studies indicates that the built up ratio ++ ++

"' +JCa + Mg answered as ESP is different for differer,t l' a , 2

type of clay soils. For example,in the present study it is

noted that the infiltration rate for the

Kaolinite-Montmorillonitic Ahmedabad soil is distinctly

very high for all the SAR ratio waters (15,30,45,60 and 75),

compared to Montmorillonitic Amreli soil and

Kaolinite-Illite Kutch soil. Thus the built up Na controls

the infiltration rate. Electrolyte concentrations also

somewhat affects infiltration rate, yet the pronounced

effect is from the clay mineralogy of the soil.

In the case of Kaolinite-Illite soils the infiltration

rates are not very high for SAR 15 and 30, but are

definitely higher for SAR 45 and again lower infiltration

rate for SAR 60 and 75. It is inferred from these results

that with SAR 15 and 30 waters there is going to be base

saturation + by Na ion. With SAR 45 water electrolyte effect

is slightly prominent. Again with SAR 60 and 75 waters the

base saturation with + respect to Na is higher,which lower

down the infiltration rates.

In the case of Montmorillonitic soil infiltration rates

177

are not very high for SAR 15 waters,but definitely higher

for SAR 30 and SAR 45 water. Again for SAR 60 and SAR 75

infiltration rates decreases. I~ is inferred that high SAR

leads to higher ESP. Higher build up ESP will decrease the

infiltration rates. Higher salt concentration will lead to

increase in infiltration rates due to electrolyte effect.

For this reason even sea-water can be used to reclaim

(saline-alkali) soils.

Considering the results in Table 6.2 to 6.6 we find

that with increasing SAR there is decrease in infiltration

rates, which is more so after the 3rd and 4th minute,because

the 1st and 2nd minute reading are of the uppar part of

column which might contain small amounts of air,the lower

part being filled intact and would have less amounts of atr

vojds.

On comparing the infiltrat1on rates of all three sails

it is concluded that infiltration rates of:

K-M > M > K-I

1. Ag ass i , M. , I .

electrolyte

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chapter vi infiltration rates of soils for waters of...

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