eChapters

Manychemicalreactions innature,particularlyinlivingsystems,occur inaqueous solutions. Reactions are often carried out in the laboratory in aqueoussolution becausethese aregenerallymore rapid in solutionthanwhen puresolid reactions are mixed. Analysisof substancesmaybe qualitative or quantitative in nature. A quantitative analysisis one inwhich the amountor concentrationof a particular species in a sample is determined accurately and precisely.

1.1 Volumetric Analysis

Volumetric analysis is a quantitative analysis. It involves the measurement of the volume of a known solution required to bring about the completion of the reaction witha measuredvolume of the unknown solution.

The reaction used in volumetric analysis must fulfil the followingconditions;

Advances in analyticalchemistry and instrumentalanalytical chemistry in the pastfew decades have significantlyimproved, makingelemental determinations in soil extracts and water samples easier, faster and less challenging for the analyst. For most of the elemental analysis procedures, the more traditional wet chemistryprocedures havebeenreplaced byvarious analytical instrumental procedures that employ either emission or absorption spectrophotometry. The elemental concentration in prepared soil extracts and water samples can be determined by a number of instrumentalanalyticalprocedures.

The trend today is toward greater analytical sophistication, to multielement computer controlled analytical instrumentation, resulting in a less ended understandingof the analytical principlesinvolved, and “black box” concepts of instrument calibration, maintenance, and operation. Preparation of the analyte and suitable adaptation for a method of analysis requires an understanding, by the analyst, of the principle of the method as well as its requirements and limitations. Adequate testing is usually required before putting the method to use, following procedures such as those that have been adapted by the Association of Official Analytical Chemists (AOAC).

It is not possible to cover in adequatedetail every method of analysissuitedfor the elemental concentration determination in soil extracts and water samples. Therefore, the objective here is to provide sufficient background information about the instrumentalprinciples to guide the reader.

3.1 Concepts of Soil Sampling

Samplinginvolvesthe selection fromthe total populationof a subset ofindividuals upon which measurements will be made. The measurements made on this subset (or sample) will then be used to estimate the properties (or parameters) of the total population.Samplingisinherent toanyfield research programinsoilscience because the measurement of the total population is impossible for any realistic study.

Samplingdesign involves theselection of the mostefficient method forchoosing the samples thatwill be used to estimatethe properties of the population. The definition of the population to be sampled is central to the initial formulation of the research study. The sampling design defines how specificelementswill be selected from the population, and these sampled elements form the sample population.

Pedogenetic and soilgeomorphic studies focus on determining the processes thatformed the soilproperties or landscapes under study and the environments that controlled the rates of these processes. Pedonscale studies are closely associated with thedevelopmentof soil taxonomic systems andfocus onvertical, intrapedon processes. Soil geomorphic studies are the interface between quaternary geologyand soil science and soil geomorphologistsfocus on lateral transferprocesses and the historical landscape evolution. Hence sampling is difficult for a particular population and is differentfor differentstudy.

The influence of water quality on the soil and plant growth is related to the chemical and physicalproperties of the soil, the salt tolerance of the crop, the climaticregime of the area and the method,frequencyand the amount of irrigation water applied. Irrigation water quality refers to its suitability and sustainability for use in agricultural crops. The problems thatresultfrom the use of a particular irrigation water, vary both in kind and degree, and are modified by soil, climate and crop as well as by the skill and knowledge of the water user. As a result there is no set limiton water quality, rather itssuitability for use is determined by the conditions of use which affects the accumulation of water constituents andwhichmayrestrictcrop yield.The soilproblems mostcommonlyencountered and used as a basisto evaluate water quality are those related to salinity, water infiltrationrate,toxicityanda group of other miscellaneous problems. Numerous guidelines are available for evaluation of water quality. Time to time some of theseguidelines has been updated with modification of some criteria like SAR to Adj. SAR and the Adj. R_Na and development of new concepts like water qualityIndex (WQI) whichhave increasedour predictability. Thenewguidelines are relied heavily on old ones.The modified guideline by Ayers and Westcot (1985) was foundto be themost reliabletopredict thewaterqualityforirrigation.

Irrigated agriculture is playing a major role in enhancing food and livelihood security of a country. Supply of fresh water which is an importantinput for the sustainable and economic development of agriculture are not enough to meet the requirement of all sectors of economy. Reduced water availability to agriculture from the present share of 85% of country’s water resources to about 70-75% by 2020AD wouldaffect the capacity of the country to meet the food production target, unless supplies are augmented from unconventional sources. For future agriculture there are no alternatives but to rely on non conventional sources for partial alleviation of the forecasted water scarcity. Amongthese sources extraction of marginal quality groundwater and the waste water generatedfromurban and industrial activities have thepotential to augment the water supplies. Many associatedsoil, plant and environmental problems come up when these sources of water are directly used for irrigation. For addressing theseproblems and to get more benefit from thesesourcesof water, the first step is to understand how an irrigation water source affects the soil plantsystem.Thereforeknowledge of irrigationwaterqualityiscriticaltodevelop appropriate site and crop specific comprehensive short term and long term management programs.

Most of the DNA of an living organism is packaged and organized in a chromosome as well as in mitochondria and cell organelles (Feulgen and Rossenbeck 1924). DNA is not found on its own but rather is structured in long strands wrapped around protein complex called nucleosome consisted of a protein called histone. During most of the duration of cell cycle a chromosome consists of long double helix DNA molecule (with associated proteins)During S phase the chromosome gets replicated resulting in X –shaped structure (chromatids) and still attached to a single centromere. The basic role of the chromosome is to provide a frame work which allows each linear segment of the genome to replicate and segregate efficiently. Failure in either of processes cause chromosome imbalance in daughter cells. Three specific cis-acting sites are required for stable chromosome maintenance, i.e., an origin of replication, a centromere and telomeres.

Classical studies of the morphologyof individual chromosomesof the plant species begun by S. Nawaschin 1910-16 and continued by Taylor (1925), Sharp (1929) and Mc Clintock (1929-30). And eventually it was possible to set up working models which account for the internal structure and chemistry of the chromosome and the genetic material as well as genetical facts. The use of aceto-carmine with iron (Belling, 1921) and application of heat greatly improved the staining differentiation of chromosomes. Smears have practically replaced the paraffin techniques of studying chromosome. The gross morphology of chromosomes is generally worked out either at prophase stages of meiosis or metaphase in somatic tissues. The chromosomes may differ in thickness, total length, position of centromere or spindle fiber attachment region, chromomere pattern and number and position of secondary constriction. The total length of chromosomes at metaphase also differs in different tissues of a species and also in certain tissues chromosome present may be very different in appearance. Figure 1 shows various morphological features of a eukaryotic chromosome

The relationship between gene and chromosome was suspected at the time of rediscovery of Mendelian^, Laws. During that period Montgomery (1901) and Walter Sutton (1902) working on grasshoppers showed that chromosomes occur in distinct pairs, often of recognizable shape and size, and that synapsis involves the union of maternal and paternal chromosomes, while Winiwarter (1901) concluded from his studies in rabbit ovaries that bivalents in the first meiotic division resulted from the chromosome pairing side by side and not end to end as believed by some other workers of that time . Theodor Bovery (1902) showed from his work on polyspermy in the fertilization of sea urchin eggs that the chromosomes of an individual were not equivalent (genetic information) to one another and hence a full chromosomal complement is essential for normal development of cell. Correns (1902) and Cannon (1902) pointed out close parallelism between Mendelian segregation and chromosome reduction during meiosis and concluded that genes are located on chromosomes but they, like de Vries, supposed that maternal and paternal chromosomes move to opposite poles during meiosis. In the same year Guyer established an understanding that random assortment between different pairs of chromosomes would give the independent assortment of genes required by Mendel. Ultimately Sutton (1903) brought together the ideas from cytology and genetics to clearly show the role of chromosomes in heredity and hence to establish the field of cytogenetics. Boveri also through his work, advanced many of the same ideas and thus the hypothesis correlating genes and chromosome transmission was established, which is known as the “Sutton-Boveri Hypothesis or chromosome theory of inheritance”.

The chromosomes provide physical basis by which genetical stability and continuity of individuals and populations are maintained in each generation. Chromosomes also play an important role to generate variation which is an essential component of evolutionary process. Although crossing over during meiosis is responsible for generation of variability, but structural changes in chromosome too are important for causing variation and evolution, since genetic and cytological analysis of individuals of related species or isolated populations within the species have shown that they may differ by various kinds of changes in their chromosomal structure. The structural changes usually may result from spontaneous chromosome breakage. But under normal condition/s such breakage is an rare event and its frequency is dependent upon environmental conditions, i.e., temperature, various high energy radiations (e.g. X, λ and β-rays) and some chemicals. Chromosome breakage is reported to be higher in some hybrids and in presence of particular genes. Certain chromosomes and chromosomal segments (centromeric and other heterochromatic regions) are more likely to undergo breakage. But stability and continuity of structural changes in the chromosomes depend on the behavior of the broken ends. There is no change if broken end rejoins at the same chromosome but a change may occur if it rejoins with the end of other chromosome or if remains unattached. In case of a pair of homologous chromosomes if one chromosome has any structural change and other one is normal we customarily call it a structural hybrid.

The intervarietal chromosome substitution lines of wheat (T. aestivum) are utilized to study the effects of individual whole chromosome/s on agronomic characters of interest to improve crop plants to be selected for preferred traits (Law and Worland 1973). The common method to develop subsitutiion lines involves development of monosomics lines first of that variety which are used later as recipient variety or recurrent parent for substitution. Presently monosomic lines of several wheat varieties are available. However, the development of substitution lines for a specific chromosome by using monosomics sometimes may be erroroneus due replacement of specific monosome by another one of the 21 chromosome set from the donor to the recipient and consequently monosomic becomes monosomic for another chromosome or a recombined chromosome (univalent shift.). Therefore, to maintainand confirmthe identityof a chromosome involved in monosomy are tagged with either genetic marker/s or confirmed cytologically or with the help of molecular markers.

The newly synthesized autopolyploids, having few or more undesirable features, e. g; meiotic instability, low seed setting and late maturity etc, are usually not suitable for immediate commercial use, are known as raw polyploids. This is specifically more applicable for those sexually propogated polyploids which are developedfor seed. In early generations due to polyploid chromosome constitution and polysomic inheritance they predominanantly do not breed true. Further more, due to meiotic instability chromosome number in their progeny is not always constant or equal to as in synthesized autotetraploid which may vary from few more to few less than the standard autotetraploid. The raw polyploids usually reverts back to diploid parental constitution due chromosome elimination (Randolph and Fischer, 1939). The mechanism responsible for reverting back to diploid status is similar to that of which give rise haploids from diploids. Presently cases are known where either spontaneously or due to specific treatments the chromosome number was reduced to half in somatic tissues. The phenomenon causing such chromosomal reduction is termed as somatic reduction or reduced mitosis Earlier reports suggested it probably to be caused due to spindle organizer abnormalities or some other unknown mechanism/s. The treatment of seed or seedling by colchicine, chloramphenicol and paraflurophenylalanine are reported to have induced chromosome reduction and production of haploids.

Wide hybridization (interspecific/intergeneric) is basically attemped to introduce new genetic variability from wild or distantly related species into cultivated ones or to synthesize new plant type/s like Triticale and Raphanobrassica. Majority of the commercial crop plants are usually deficient for one or the other desirable traits which are usually available in their wild relatives. However, crossability between commercial varieties and their wild relatives is very limited which is naturally imposed by certain genetically controlled reproductive barriers. These reproductive barrier/s usually operate either at pre or post fertilization stage/s in plant species (Stebbins1958). Since a species is constituted of individuals who share a common gene pool, reproduce among themselves only / exchange genes and share a common habitat. Hence at natural level gene flow remains strictly confined only among members of a particular species otherwise among the members of unrelated species a genetic barrier exists to create reproductive isolation. Therefore, wide crossing basically requires the overcoming of such barriers whch are imposed by temporal and spatial isolation of parents. The reproductive isolation consists of premating and post mating isolation mechanisms like habitat isolation or geographical isolation, sexual isolation and mechanical barrier depending upon incompatibility or mismatching of ganitalia (animals). Sexual isolation in animal kingdom is usually enforced by type of sexual displays and mating calls which are attractivce only to particular members of a species , however other potential intermating species also do exist in the same habitat or locality at that particular period of time.

Soil is a mass of large variability and thus its sampling is the most challenging problem for any soil analyst. Practically, soil sampling is a two step process which includes (i) collection of soil from homogeneous unit and (ii) processing which in turn includes drying, grinding, sieving, mixing, partitioning and storing.

2.1 Particle Size Distribution Analysis

Soil is composed of inorganic particles and organic molecules of varying size and shape. The expression of the proportion of the different size inorganic particles is termed as ‘soil texture’. It is one of the most important basic characters being little changed by cultivation or other practices. Particles are arbitrarily distinguished into following groups on the basis of their diameters.

3.1 Determination of Bulk Density of Soil

3.1.1 Determination of Bulk Density of an undisturbed Soil

Bulk density of soil is expressed as the ratio of the mass (weight) of soil particle to their total volume including the pore space between the soil particles. Alternately, it is the weight of unit volume of dry soil. It is usually expressed in the unit of gram per cubic centimeter (g/cc) or mega gram per cubic meter (Mg/m³). In fine textured soil bulk density varies from 1.00 to 1.60 g/cc, whereas in coarse textured soil from 1.20 to 1.80 g/cc.

4.1 Determination of Specific Surface Area of Soil

Specific surface area of a soil is defined as surface area per unit weight of soil and is expressed as m² g^-1. The specific surface of soil greatly influences the physical and chemical properties such as retention of water at high suction, swelling, plasticity, soil strength, cation exchange capacity and availability of nutrients. The basic principle of determination of specific surface is based on the amount of gas or polar liquid required to form a monomolecular layer on the soild. Knowledge of molecular size (diameter) and the mass of the adsorbate enables one to calculate specific surface of the adsorbent.

Principle

Dyal and Hendricks (1950) introduced a method for estimating specific area based upon the adsorption of ethylene glycol (EG) to form a monomolecular layer over the entire soil surface. The method involves adding EG to pretreated soil or clay sample and evaporating the excess EG in an evacuated system. The quantity of EG retained at the moment the evaporating rate decreases is proportional to the surface area. Later on Carter et al. (1965) suggested the use of ethylene glycol monoethyl ether (EGME) having high vapour pressure at room temperature than EG for determining surface area of the layer silicate minerals and soils.

In natural condition primary soil particles cohere to each other to form a cluster or an aggregate through the cementing action of various agents like organic matter, carbonates, oxides of iron and aluminium, etc. Aggregate analysis tells one about the structural status, pore geometry which in turn influences the movement of air and water in soil, amount of water stable secondary particles (aggregate) as well as the extent of finer particles aggregated to the coarser particles and the erodibility status of surface soil against wind and water.

6.1 Determination of Soil Moisture

6.1.1 Determination of Soil Moisture Content by Gravimetric Method (Direct method)

Traditionally, water content in soil is expressed as the ratio of the weight of water present in the soil to the weight of dry soil. When this ratio is multiplied by 100, it becomes the percentage of water in the soil sample on dry weight basis.

Equipments and Materials

Soil auger, aluminium moisture box with air tight lid, balance, oven and desiccator

7.1 Determination of Hydraulic Conductivity of Saturated Soil Laboratory Methods

Hydraulic conductivity of a saturated soil indicates the ease with which water is transmitted through the soil pores. If a constant water head (h) is maintained on a saturated soil column of length (L) and the volume of water (V) percolating per unit time (t) through per unit cross sectional area (A) to the other end, then according to Darcy’s Law, the rate of flow of liquid or flux (q) is proportional to the hydraulic gradient (ÄH/L) across the length of soil column.

Soil consistency is a term used to designate the manifestation of different physical forces acting within the soil at various moisture levels. The consistency limits, also known as ‘Atterberg Limits’ (Atterberg, 1911; 12) are defined by the water content of the soil to create specified degree of consistency. These limits are – (i) Liquid limit or upper plastic limit, (ii) Plastic limit or lower plastic limit and (iii) Sticky limit.

8.1 Determination of Liquid Limit or Upper Plastic Limit

Equipments and Materials

Liquid limit device (Casagrande, 1932) and accessories, spatula, dish, oven, moisture box, balance, desiccator

9.1 Determination of Oxygen Diffusion rate (ODR) of Soil

The rate of movement of oxygen from atmosphere to respiring plant root cells is important for root respiration and thereby the growth and development of plant. While diffusion through the air-filled pores maintains the exchange of gases between the atmosphere and soil, diffusion through water films maintain the supply of oxygen and disposal of carbon dioxide from active root tissues which are typically hydrated.

Principle

Lemon and Erickson (1952) introduced a method for measuring oxygen diffusion in soil with the help of platinum electrode. The process measures the extent of chemical reduction of oxygen by the platinum electrode maintaining a constant potential of 0.65V with a reference electrode.

Temperature is a fundamental property of usually used to characterize the thermal condition of a system. The growth of any biological system is optimal within certain ranges of temperature and inhibited or ceased beyond this boundary. In addition to plant growth, the significance of temperature on agriculture can be ascertained by its role on physical, chemical and biological processes occurring in soil. Therefore, to study these soil properties intensively measurement of soil temperature is essential.

10.1 Measurement of Soil Temperature

Temperature of any system cannot be directly measured. It can only be estimated by its influence on some properties (thermometric properties) which respond to the variation in the intensity of heat of that system. These thermometric properties include volume, pressure, length, electrical resistance, thermal emf of the matter. Instruments built to take the advantage of any of these thermometric properties of the matter are called thermometer.

11.1 Determination of Penetrability of Soil

Penetrability of a soil is usually assessed by the penetration resistance, which a measure of soil strength and thereby the soil compaction. Penetration resistance is the capacity of the soil in its confined state to resist penetration by a rigid object. Besides soil strength, the penetration resistance also depends on the size, shape and orientation of the axis of the penetrating probe. The penetrating probe may be a finger, pencil, stick, root or any specially designed object having a specified geometric shape and a device to measure the resistance as it is pushed into the soil.

Soil penetrability is intimately related to agriculture because of its adverse impact on draught requirement during ploughing, root development and crop yield, to civil engineering due to its relation to settlement, stability and ground water flow.

Soil penetrability is a measure of the ease with which an object can be pushed or driven into the soil. Any device designed to measure the resistance to penetration may be called penetrometer. There are several types of penetrometers: (i) pocket penetrometer, (ii) proctor penetrometer, (iii) cone penetrometer, and (iv) split-spoon penetrometer. Here, we will discuss about two most commonly used penetrometers viz. pocket penetrometer and cone penetrometer used for agricultural purposes.

Thermal Analysis

Physical and chemical properties of any soil are governed largely by the mineralogical make up of the soil, and more specifically by the clay fraction. Identification, characterization and an understanding of properties of different minerals are important in evaluating soils in relation to classification, agronomic practices and engineering purposes.

Clay fractions of soils are usually composed of mixture of one or more secondary phyllosilicate minerals along with primary minerals inherited from the parent materials. Identification of minerals species as well as their quantitative estimation in such polycomponent system require application of several qualitative and quantitative analysis.

The methods used for identification and quantification have steadily been improved over the last 50 years. Among the several methods often used for this purpose three are very common, e.g. (i) differential thermal analysis (DTA), (ii) x-ray diffraction analysis (XRD), and (iii) infrared spectroscopy (IR).

Thermal analysis is a term covering a group of analyses that determine the changes of some physical parameters, such as weight, energy, dimension and evolved volatile substances with change in temperature. Many soil constituents undergo various thermal reactions upon heating, which can be utilized as a diagnostic tool for qualitative identification and quantitative estimation of the substances. These reactions may be exothermic or endothermic, and phase change or crystal change may take place during reactions. Whatever be the reactions, if properly measured, they give some valuable information to identify the substance under consideration.

Among the several methods available for thermal analysis, three methods are frequently used in soil research: differential thermal analysis (DTA), differential scan calorimetry (DSC), and thermogravimetry (TG). Among these, DTA and TG will be discussed here.

The total energy of a molecule consists of translation, vibrational, rotational and electronic energies. Transition among different types of energy levels occurs in different regions of electromagnetic spectrum. Transitions between rotational and vibrational energy levels of the ground state molecules give rise to absorption bands throughout the infrared region of the electromagnetic spectrum. Organic molecules are characterized by possessing bonds and groups that vibrate independently of each other. Thus, initially infrared spectrometry was used for identification of functional groups of organic molecules. There is lot of ambiguity in the interpretation of infrared spectra of organic matter preparations due to complexity and diversity of the components of soil organic matter. But if used carefully it can provide information on: (i) nature, reactivity and structural arrangement of oxygen-containing functional groups, (ii) presence of protein and carbohydrate constituents, (iii) presence or absence of inorganic impurities (metallic ions, clays, etc in humic fractions), (iv) the amount of different soil organic matter components, and (v) interaction of organic components with pesticides, herbicides, fertilizers, etc.

On the contrary to organic molecules, minerals tend to have few isolated vibrating groups. It can be used for mineralogical analysis when used in conjunction with x-ray diffraction and other similar techniques.

Infrared spectrometry is used in the identification of inorganic compounds including minerals which have well-defined absorption bands in determining- (i) whetherlayer silicate isdioctahedral or trioctahedral in composition, (ii) in studying isomorphous substitution, (iii) hydration of minerals, and (iv) in quantitative analysis. Infrared spectrometer provides information about nature and identify of inorganic compounds that are amorphous in x-ray diffraction analysis.

14.1 Principles of X-ray Diffraction

Any crystalline structure is characterized by a regular and systematic arrangement of atoms (or ions) in a three-dimensional array. Since crystals are composed of regularly spaced atoms or ions, each crystal contains planes of atoms or ions separated by a constant distance which is the characteristic of that crystalline species.

X-rays are essentially electrostatic and electromagnetic fields oscillating in planes perpendicular to each other and to the direction of propagation in periodic cycles. X-rays having wavelengths in the order of 10^-3 to 10¹ nm, are produced within a vacuum x-ray tube by bombardment of a metal anode with high-velocity electrons. High-velocity electrons transfer their energy to the electrons of metal anode causing their elevation to higher energy level (excited state). Excited electrons of metal atom soon come back to the vacant shell and each electron transfer from higher to lower energy state results release of a quantum of energy (x-ray photon) equivalent to the difference in energy between these two levels. The energy and the wavelength of emitted x-ray photons are finite and characteristic of the particular atoms of the metal anode used in x-ray tube. Usually, photons generated due to electron transfer from L-shell to K-shell are used for x-ray diffraction analysis.

Diffraction of x-ray involves scattering of x-rays by planes of atoms of the crystal separated by definite distance and reinforcement of scattered rays in definite direction away from the crystal. Reinforcement of scattered rays is quantitatively related to the distance of atomic planes in a crystal as defined by Bragg’s equation:

15.1 Law of Mass Action

Gulberg and Waage, the two Norwegian chemists in the year 1864 stated the law of mass action in this form: ‘The velocity of any chemical reaction at any instant at a given temperature is proportional to the active mass of each of the reactants at that instant present in the system, the active mass in a homogeneous system is defined as the number of gram molecule of the substance present per unit volume i.e., the molar volume’.

16.1 Balance and Weighing

16.1.1 Principle of Functioning of a Balance

It is one of the important tools used in the laboratory and one should have thorough knowledge aboutitsassembly, use and care,otherwise it may be the initialstep for introducing error in any physical or chemical analysis. Every balancehas its maximum load limit and sensitivity depending upon its construction.

Essentially balance may be regarded as a rigid beam, BC having a central fulcrum, O and two arms of equal length, d₁, d₂ (Fig.16.1). Theboth ends of beam have prism edges upon which the balance pans are suspendedby means of suitable suspension.

17.1 Determination of Soil pH

The soil pH value is the measure of hydrogen or hydroxyl ion activity in the soil solution and it indicates whether the soil is acidic, neutral or alkaline in reaction. The pH is the most important property of soil as it controls the availability of plant nutrients, microbial activity and physical condition of soil. Since crop growth is affected both under very low (strongly acidic) and very high (strongly alkaline) soil pH, reclamation of these soils are necessary. Soil pH in fact indicates the extent of active acidity (activity of hydrogen ion in soil solution) of soil. Depending upon the purpose of measurement and soil condition, soil pH is measured in several soil-water or soil-salt solution ratios. The saturated paste is used for identifying specific soil problems like degree of acidity or alkalinity. For making fertilizer recommendation, 1: 2 soil-water suspension is generally adopted. To mask the variability in salt content of the soil, the pH is measured in soil-CaCl₂ suspension (1:2 soil-0.1 M CaCl₂ solution). The soil pH value is independent of dilution over a wide range of soil-salt solution ratio, thus more reproducible than those obtained with soil-water suspension.

18.1 Determination of Electrical Conductivity of Soil Solution

The conductivity or more precisely the specific conductance of a soil at a given soil-water ratio is the reciprocal of the specific resistance offered by the solution at 25ºC between the electrodes of 1 sq cm cross section kept 1 cm apart. Thus, the electrical conductivity of any solution depends on the amount of soluble salt present in it. Knowledge on the extent of salinity is important for management of saline soil including the choice of the crop suitable for that soil. Soluble salt content in saturation extract is more reliable index of salinity level than in soil: water ratio of 1: 2 or 1: 2.5, because it simulates the extent of salinity experienced by crop in field moisture condition.

Salinity class of soil is based on the electrical conductivity (EC) of saturation extract at 25ºC. However, EC of water extract from 1:2 soil-water suspension can be transformed into the EC of saturation extract following the formula (except for soil containing gypsum).

Carbon may be present in soil in four different forms:

1. Carbonates: Mainly as CaCO₃ and MgCO₃, active CO₃ ^2- and HCO₃ ^- ions and gaseous CO₂.
2. Highly condensed elemental organic form: Charcoal, graphite.
3. Completely decomposed resistant organic residues: Humus.
4. Undecomposed and partially decomposed organic residues.

The latter three fractions constitute the total organic carbon of which last two are chemically active form.

20.1 Exchange Capacity

Soil colloidal particles carry both negative and positive charges on their surface which attract and hold equivalent amount of oppositely charged ions to their surface. The total number of negative charges present on a given mass of soil or capacity of a given mass of soil to exchange cations or total number of cation held by a given mass of soil is termed as cation exchange capacity (CEC). Similarly, the capacity of a soil to retain anions is known as anion exchange capacity (AEC). The ion exchange capacity of a soil depends upon the type and amount of colloidal particle (clay and organic matter) present in the soil. Ion exchange capacity (CEC/AEC) is expressed as milliequivalent ion (cation/ anion, respectively) per 100 g of soil (meq/100g). It is also expressed as centimoles of charge (positive/negative) per kg of soil [cmol (±) / kg]. Meq/ 100g = cmol (±) / kg of soil.

20.1.1 Determination of Cation Exchange Capacity of Soil Principle

Soil is first saturated with normal ammonium acetate (pH 7.0). Excess ammonium (NH₄⁺) ions and displaced cations are then removed by washing with alcohol. The amount of NH₄⁺ ions retained by the soil is measured by steam distillation of NH₄-saturated soil with MgO. During distillation evolved ammonia is absorbed in a boric acid solution as ammonium borate and the amount ammonium borate formed is determined by titration with standard sulphuric acid in presence of mixed indicator.

21.1 Determination of Total Nitrogen in Soil (Modified Kjeldahl Method)

Nitrogen mostly present in soil in organic form. Relatively small amount of nitrogen usually occurs in ammonium and nitrate form, the available form. The Kjeldahl method of total N determination includes both organic and ammonium forms and with modification nitrate form of N can also be included.

Principle

When soil is digested with concentrated sulphuric acid organic nitrogen is converted to ammonium sulphate. To speed up the reaction a digestion mixture composed of sodium (or potassium) sulphate (to raise the boiling point of H₂SO₄) and cupric sulphate (CuSO₄) - selenium powder (catalyst) is used.

Phosphorus is present in soil both in inorganic form and organic form. The inorganic P can be divided into different pools. The major active inorganic forms are: P bound to aluminium (Al-P), iron (Fe-P), calcium (Ca-P) and silicate minerals and relatively less active forms are occluded and reductant soluble forms of P. On the other hand, the principal organic P compounds present in soil are (i) inositol phosphate, (ii)phospholipids, (iii)nucleicacid and other unidentified esters and phosphoproteins.

22.1 Determination of Available Soil P

The availability of soil P to plant varies greatly depending upon the reaction, minerological composition and amount of the soil colloid. Very little P is present in the soil solution except in recently fertilized or sodic soils. The type of phosphate ions present in the soil solution depends on the soil pH. In soils of neutral to slightly alkaline pH, HPO₄^2-ion is the dominant form. In slightly or moderately acidic soils, both HPO^-and HPO^2-ions prevail. At strongly acidic soil HPO 244 24 ion tends to dominate, while above pH 9.0, the PO₄^3-ion becomes more important - than H₂PO₄ .

As the P is drawn from soil solution largely through diffusion by the plant, it is replenished from solid phase pool of available P. P fertilizer is added to recharge this pool.

23.1 Forms of Soil K

Ignoring potassium (K) in soilorganism, total K in soilmaybe classified as (i) water soluble K, (ii) readily exchangeable K (exchangeable K), (iii) slowly exchangeable K (non- exchangeable or fixedK) and (iv) mineral or lattice K. Thedifferentforms are in dynamic equilibrium with one another.

Sulphur (S) occurs in soil in both organic and inorganic forms. Inorganic S fraction may occurs as sulphate (SO₄^2-) and compounds of lower oxidation state such as sulphide (S^2-), polysulphide (S_n^2-), thiosulphate (S₂O₃^2-) and elemental sulphur (S⁰). In well drained soils inorganic S usually present as sulphate. Under anaerobic condition (reduced or waterlogged soil) inorganic S mainly occur as sulphide and under extreme condition as elemental S form. Estimation of S is carried out in two steps:

1. Extraction of different forms of S from soil by suitable extractant.
2. The filtrate is then analysed for S by the turbidimetric method.

The turbidimetric method is the most widely used one because of its simplicity and rapidity.