Chapter VI CLAY MINERALOGY Chapter VI
CLAY MINERALOGY
Introduction
Because of the importance of clay materials in ceramics and other industries, in agriculture, in geology, and elsewhere, their investigation goes back far into antiquity.
From the very beginning, it has been observed by the various investigators, that clays and soils very widely differ in their physical and chemical properties. These variations are not in the amounts of the ultimate chemical constituents, but also in the way in which they are combined, or in the manner in which they are present in various clay materials.
In the older literature, a considerable number of concepts were suggested to protray the fundamental and essential components of all clay materials and to explain their variations in properties.
Until very recent years, there has been no adequate analytical tools to determine with any degree of certainity the exact nature of the fundamental building blocks of most clay materials. But during past few decades, considerable investigation of clay materials has been made by using the modern techniques such as spectrophotometric analysis, X-ray 104
diffraction, Infrared, Differential thermal analysis,
Scanning electron microscopy etc. These investigations have thrown more light on the presence of clay minerals, their crystal structures, chemical characters, water content, impurities present etc. which are responsible for physical properties, of clay materials which are mainly considered for their suitability in various industries.
In the present Chapter, the mineralogy of the clay samples from Sindhudurg district is presented. The results have been obtained by using X-ray diffraction, Infrared,
DTA, TG, and Scanning electron microscopy.
Definition of Clay :
The term 'clay' is being used as a rock term and also as a particle size term in mechanical analysis of sedimentary rocks, soils etc. for years together. In general the term clay implies a natural, earthy fine grain material which develops plasticity when mixed with water. The essential chemical components of clay are silica, alumina and water.
Iron, alkalis, and alkaline earths are nearly always present.
The term clay is used for material that has a variety of origin, such as i) product of weathering, ii) formed by hydrothermal action on pre-existing rocks or iii) sedime tary deposition in river or lake or sea. Wentworth (1922) asssigned clay grade to material less than 4 microns in lOS
size, whereas soil scientists have placed clay grade at
2 microns. But most of the clay fraction occurs with size less than 2 which appears to be a convenient limit.
During the earlier days, Kaolinite was considered as the essential clay mineral and the other material occuring as impurity. Soil scientists held the view that the essen tial component of all clay materials was a colloid complex.
Clay Minerals :
Clay minerals are phyllosilicates or layer silicates.
They consist of layers with two types of units involved in each layer, the tetrahedral and the octahedral. During the two decades 1920-1940, there were several contributions made towards the study of clay material on the basis of
X-ray diffraction analyses. Hadding (1923) and Rinne
(1924), regarded the clays as independent materials and not amorphous material or colloids. Microscopic and chemical study of clays by Ross and Shannon (1925, 1926) suggested that the components of clay materials are essentially crystalline which may be called as clay minerals. Ross
(1928) proposed a classification of clay minerals. Ross and Kerr (1931) and Correns (1936) gave widely accepted concept of clay mineral. According to this concept, clays are considered to be composed of extremely fine crystalline 106
particles, w~ich are essentially hydrou:; aluminium silicates.
AJ. kla 1 is and alkaline earths are present in some clay minerals wh ; l.!=: in some others, magnesiun1 or iron partly replace some of the aluminium. In addition to clay minerals, some of the non-clay minerals, organic matter and soluble salts also form important constituents of clays. Ross and Kerr (1931, 1934), Ross and Hendricks (1945) made detail study of kaolinite, halloysite and montmorillonite respecti vely. Hedricks and his co-workers (Hedricks 1938, 1941,
1942, 1945, Hendricks ~.al. 1936) made significant contri butions by way of giving the physico-chemical properties of different clays. Different aspects of clays have been studied by Grim, Bradley and their co-workers (Grim, 1947, 1948 , 1950, Grim e t. a l. 1935, 1937, Bradley, 1945).
The credit of cre ation of s ynthe tic clay minera ls in the laboratory for the first time, goes to Noll (1935). Orcel (1933) was the first to apply the techique of DTA in the study of cla ys. Brindley and Robinson (1946a, 1946b) studied in g reate r details the properties of kaolin minerals. Glaeser (1948), Mering et.al. (1950) studied ad s orption of various lons on clay mine rals and the ir
textures using electron microscope. Mukherjee et.al. (1946) and Chatte rj e e (1949) have studied the e l ectrochemistry
and chemistry of clays from India. 107
Since 1950, there has been a considerable addition of literature based on the various aspects of clays.
X-ray identification and crystal structure study by Brindley
(1951) and Brown (1961). Carroll (1970) published a guide to clay mineral identification using X-ray techniques.
Grim (1953), (1962, 1968) published books on 'Clay Mineralogy' and 'Applied Clay Mineralogy'. DTA investigations of clay edited by Mackenzie (1957), 'Geology of clays' by
Millet, (1970). 'Atlas of infrared spectroscopy of clays and their admixtures' and 'Atlas of electron microscopy of clays and their admixtures' by Vander Marrel and Beutel spacher (1968 and 1976) and 'Clay Minerals' (Nemecz, 1981).
Classification of clay minerals :
Several workers have attempted classification of clay minerals, mainly based on the structural characteristics as there is a wide range of chemical composition not only within a single group, but also within single mineral.
Caillare and Henin (1956) proposed a tabular classifi- cation of sheet silicates. This was later modified by
Caillere in 1960 by Millet (1970). It consists of six tables, one for the general classification of hydrated silicates, and kaolinites and serpentinites with real basal spacing of 7 ~' micas and dioctahedral montmorillonites 108
with basal spacing of 10 ~' micas and trioctahedral montmori llonites with basal spacing of 10 ~' chlorites having basal spacing of 14 ~' and for mixed layer complexes having varying basal spacing, are the other five tables classifying major groups of clays.
Deer, Howie and Zussman (1962, 1976) have classified clay minerals into five main groups, again on the basis of characteristic basal spacings.
1. Kandite group (7 ~) - kaolinite, dickite and nacrite, anaunite, halloysite, metahalloysite and allophane.
2. Illite group (10 ~) - illite, hyrdo-micas, phengite, brammallite, glauconite and celadonite.
3 . Smectite group (15 ~) montmorillonite, nontronite, hectorite, saponite and sauconite.
4. Vermiculite (14.5 ~).
5 • Palygorskite group palygorskite, attapulgite and sepiolite.
The clay minerals attapulgite and sepiolite from the palygorskite group have chain like crystal structures and are less common. However, the mixed layered minerals which occur very commonly in nature have no place 1n this 109
classification. Though there are few more classifications available, such as those by Franke-Kamenotskii (1961),
Jasmund (1955), the classification scheme for phyllosilicates proposed by AIPEA etc. The one proposed by Grim (1968) and reproduced below is more useful and takes into account not only structure but shape and also expandibility.
Classification of the Clay Minerals by Grim (1968)
I. Amorphous group
Allophane group II. Crystalline
A. Two layer Type
1. Equidimensional
Kaolinite group - kaolinite, nacrite etc. 2. Elongate
Halloysite group.
B. Three layer types 1. Expanding lattice
a. Equidimensional
Montmorillonite group - montmorillonite, Sauconite etc,. Vermiculite
b. Elongate Montmorillonite group - nontronite, saponite, hectorite 110
2. Non-expanding lattice Illite group c. Regular mixed layer types Chlorite group D. Chain - structure type Attapulgite
Sepiolite
Palygorskite
The important clay mineral groups relevant to the present work are described in brief below
The Kandite ·. gro~p : :
The kandite group include a group of minerals characte- rised by a basal spacing of 7 ~. Compared to the clay minerals from other groups, the kandites have a very restri- cted range of chemical composition. Kaolinite, diokite and nacrite and halloysite are described from this group.
Kaolinite : It is chemically a hydrated Al silicate Silica tetrahedra are linked with the aluminium at their centers by a group forming a single layer. Several such layers are stacked together with a periodic spacing of 7 ~' this is clearly reflected in the X-ray diffractobands. On heating 550°C to 600°C, the structure co 11 a p s e s and the 7 ~ peak is lost in the diffractograms. These two features were also observed in lll
the present study in the clays from Sindhudurg district.
Dickite and Nacrite : These are the minerals usually found in hydrothermal deposits. They show chemical affinity with kaolinite but crystallise in monoclinic system in contrast to kaolinite. There lattice structures are different.
They show an intense pask at 7.1 ~but the structure remains stable after heating to 600°C.
Halloysite : It is known to occur in two forms with basal spacing 10 ~and 7 ~ in two forms, namely elongated tubes and spherical globules. The one with basal spacing
10 A is called halloysite and the one with 7 ~ metahalloysite. Recently, AIPEA (1980) has accepted that instead of calling hydrated and dehydrated or halloysite and endellite they should be termed simply as 'Halloysite 10 ~ and Halloysite
7 ~.
A slight deviation in the structure of halloysite occurs from kaolinite in the fact that a water layer is present separating the kaolinite layers.
Metamorillonite is a high alumina endmember of the montmorillonite group with some slight replacement of Al+J by Mg+3 and without any substantial replacement of
Si+4 by At3 At the beidellite end of the montmorillonite- 112
beidellite dioctahedral sheets. When ferric iron replaces aluminium, the dioctahedral nontronite - beidellite series r esults. Saponite, the octahedral mineral from this group contains Mg and Na occurring as interlayer cation.
montomorillonite - (Al, Mg) (0H) si o beidellite - 2 2 4 10
( Ca 2+ , Mg 2+ , Na + )
Illite Group : Illite is the most common clay mineral group occurring in nature. Minerals from the illite group have structures that are similar to those of micas differing onl y in the content of potassium ion which is less and is r e placed by water. Illites and montmorillonite both have same unit layer configuration, however, some of the si licons in illite are always replaced by aluminium and the resulting excessive negative charge is balanced by potassium in interlayer positions. 113
I n the illites, the characteristic 10 R diffraction l i ne 1n X-ray diffraction is often modified into a band bec a us e of the small particle size, variation in the inter l a ye r c a tion, and interlayer hydration. This band tails of f t ow ards the low ang le region. Polymorphs of illites a re a l so known t o occur. That may be distinguished from each o the r by the manner in which sheets stack together in the ' C' direction. They are indicated by a number and a l e tter. The numbers l, 2, 3, indicate layers in a unit c e ll and letters M or T suggest the crystal s y stem mo noc l i nic or triclinic.
I n ord e r t o have a qualitative and quantitative e s t i ma ti on of the major mineral constituents of the clay
samp l es und e r study, the different techniques such as
SEM -, XRD, IR, DTA and TG have been used. The results
thus ob t a ined a r e pre s e nt ed in the following paragr a phs.
Scanning Electron Microscopy
Th e scanning electron microscopy (SEM) is uniquely suited f or study ing clays because it affords a ma gnified,
three dime nsiona l v i ew of the unmodified (natural) clay s urface with g rea t depth of focus. Th e only sample preparation nece s sar y for clays is a thin meta llic coa ting , applied 114
in a v acuum evaporator, which serves to prevent a build up o f e lectrons on the surfaces of conducting away s tatic e l ec tricity.
An e lectron optical column, containing electro -mag n e tic lenses, demagnifies an electron source in order to focus a fine beam of electrons o n the specimen surface . This b eam is scanne d across the specimen surface in a rectang ular raster in synchronism with the spot of a cathode ray tube .
Th e sig n a l r e sulting from interaction of the beam with the specime n is col l ec t ed by a suitable electron detector a nd used to modulate the CRT brightness. In most applications, i t is the low-energy secondary electro ns which are thus us e d t o form a picture of the specimen on the CRT face.
Ma n y papers have been published on the applications o f the SEM, bu t o nly a few are concerned with c lay mi n e rals.
Bo r s t a nd Ke lle r ( 1969) studied 49 r eferen ce c l ays. Gillot
( 196 1 ) , Kel l er (197b, 1978 , 1982) , Bohor and Huges ( 1971) ,
Berner and Holdren Jr. (1977), Zalba (19i9) and many other a uthor s h ave inc luded a few SEM micrograph s of clays, but the ins t r um e nt h as not b een ex t e nsive l y applie d in c l ay mineralogi cal research. Bentelspacher and Van der
Ma r e l ( 1968) pulished an 'Atlas of Electron Microscopy o f Clay Mi n e rals a nd the ir Admixture s '. 115
Analytical Method
Two powdered clay samples from Tak and Januali were scanned using 'Cambridge Stereoscan - 150'. Each sample was scanned at different magnifications and only some areas sh owing t ypical and interesting features were photographed . Th e samples were mounted on stub and sputter coated by gold palladium thin film to a thickness of about 200 ~ under a -5 vacuum l ess than 10 em with 1.4 kv current and using a beam with 20 kv energy, fine stream of Argon is passed and coated for 4 minutes. The work was done a t NCL, Pune.
The general charac t ers of the samples studied are s umma ri zed below.
Th e kaolinisation of feldspar illustrated by scanning e l ec tron micrographs include a diverse group of mineral produc ts a nd processes. More than a single t ype of kaolin mi nera l may be formed from the same parent material. The mo rphologies of the kaolin mine rals produced are likewise d i ve rse.
In the present study, the micrographs 1 and 2 (Plate
14, photo l and 2) show fragments of feldspar with spikes of kaolin mineral ostensibly have ' grown' on a base of e tched a nd shattered micro-fragment of feldspar indicating earl y 116
s tage of chemical weathering. In the background, the e longate kaolin appears in scattered form. The microg raph o f clay sample from Tak show plates of dickite ( Plate 14, pho t o 13 ) and dark cavities with walls showing the spikes of kaolin (Plate 14, photo 4) are observed from clay samples fr om Janua li. Anothe r microg raphs of clay from Tak (Plate
15 , photo l) show honeycomb texture with platelets arrang ed on edge-edge cellular pattern. As Walker, et.al. ( 1978) have sugge sted, the y ma y have formed as a result of r eplacement and dissolution of some or all elements of the s i lic ate minerals. Both clay samples in their microg raphs s h ow sh e ave s of kaolinite plate s and 'flower' patte rn (Plate
15 , photo 2 and 3 ) . The pre sence of e longate kaolin ( Plate
15 , photo 4) may be indicative of alternative conditions including both we athe ring a nd hydro-thermal alte ration. On e a lte rnative during weathering is that almost all feldspar we athe rs, in the first stage, is an elongate kaolin mineral tha t later crystallise s to platy kaolinite, thus r e pre s e nting 'metastable' morpholog y. A second alternative i s tha t the e l ongate morpholog y is formed wh e n wea the ring occ urs i n a near- s urfa c e e nv ironment, or in a highland area unde r go ing surface erosion (K e ller, 19 79) . 117
Transmission Electron Microscopy : Th e transmission electron microscope is quite similar t o a normal optical microscope , except that the use of e l e ctrons instead of light for sample illumination results in much superior resolving power and correspondingly much g r e at e r magnification. IN TEM, r e solving power is usually e xpressed in angstrom (~) units, l x 10-8 ern. The TEM is very useful to understand the structure of the material.
An aly tical Technique : Very fine powdered clay samples from Tak and Harkul f r om Vengurla and Kankauli talukas r e spective l y we re used for transmission electron microscopy, with the Philips EM
30 1 electron microscope at RSIC, Powai, Bombay. The i n s trume nt ha s a resolving powe r of about 2004 ~' corresponding ly with magnifications as high as about SO O, OOOx .
Observations :
Microphotographs of clay samples from Tak (Plate 16, ph o t o l a nd 2) indicat e s the pres e nce of we ll-crystallised kao linite , while microg raphs of clay from Harkul indicate
the pr e sence of both we ll-c rys t a llised a nd non-crys tallised
(P l ate 16 , ph o to 3 and 4) ka olinite . 118
X-ray diffraction of clays : Clays are the mixtures of very fine particles. Clay mi ne ralogy 1n we athering studies is largely concerned with identification of clays, which forms a difficult task. The commonest techniques used in the study of clay minerals are
X-ray diffraction, SEM, TEM, infra red (IR) and diffe rential the rmal analysis (DTA). Out of these, X-ray diffraction r ema ins the major technique for clay mineral identification.
X-ray diffraction is concerned with determining the spacings between the different planes in the cry stal lattice and certain spacings are characteristic of certain minerals. In practice, a curve is usually obtained showing the s pacing s and intensity of lines. Peaks on the curve, reveal the various minerals present.
Clay minerals are layer silicates in which sheets of a t oms , of the s tacked one above another in various ways with diffe rent kinds of atoms lying b e tween the l ayers a nd holding them toge ther. As they have planar structure, the 'd' spacing s corresponding t o 001 reflections are important 1n the identification. Th e common me thod of sample packing in a window randomises all the r e flec tions. I t is observed tha t 119
i f by ~orne means, the clay particles are allowed t o lie flat on the subtrate, then in the X-ray diffraction only the 001 r e fl e ctions characteristic of the individual mineral would be enhanced. Variations in these 001 reflections also help in the study of interstification, if any.
Analytical method :
The clay samples from various localities have been s ubj e cted t o X-ray diffraction analysis to ide ntify the mine ralogy of the samples. In addition to clay minerals, som e other minerals associated 1n the clays are also ide ntified. The XRD data of various samples is given in Table Nos. 6.1 to 6.22.
Samples were crushed to 250 mesh ASTM sieve. For separation of clay fraction, 25 gm of each sample were soake d in wate r for 24 hours using NH40H as dispersing agent. The mixture was shaken for about l hour on shaking machine for better dispersion. From suspension, the clay frac tion has been collected by pipe tte a na l ysis. Th e s e s ampl e s were allowed to settle on a glass slide at normal
room temperature in order to get the oriented mount. 120
The following treatment was made
a. On air dried sample
b . Gl yco lated sample and c. Sample heated up to 550°C to 600°C for 2 hours
The samples were run at the laboratory of Geological
Survey of Iran (Tehran) on the X-ray diffractometer (Type
Siemens, West Germany) operated at 30 KW and 24 MA (Cu) and
28 MA (Co) using Nickel filter and Cu ~radiations of wave leng th 1.542 ~ and using iron filter Co Ka radiations of wa ve len g th 1. 79 · ~. The scanning speed was maintaine d at
1 ° e m per min linear chart accordingly, s tarting with 28 =
4 ° with both the radiations.
For the identification of different peaks, Hana~olt's met h od h as b een us e d, in which the peaks a r e compared with
ASTM cards.
Distribution of clay minerals :
In the following paragraphs, distribution of clay minerals from clay samples unde rstud y is given.
Kudal Taluka :
Kao linite is the dominating clay mineral seen in the samp l es from Kudal taluka. The most commonly associated 121
mineral with Kaolinite is Quartz. In some localities (Pat), a mixed l ayer of Kaolinite, illite and unaltered Potash feldspars are also seen. A f ew low intensity peaks of illite are a lso identified.
Vengurla Taluka :
In this taluka, almost in all the samples, a mixture of Kaolinite, Quartz and Potash feldspars is identified. However, the Kaolinite is abundantly present.
Kankauli :
In Kanka uli t aluka, kaolinite is dominantly present. In some localities, illite has been noted . Here, in this locality, the unaltered feldspars are very few.
Malvan : The important clay mineral in this locality is again
Kao linite, but in Malvan taluka, in addition to kaolinite, o ther minerals like micas (muscovite), a few quartz and illite are present.
Sawa ntwadi : Kaolinite is dominantly occurring clay mineral of sampl e s collected from this taluka. He re, kaolinite is associated with f e ldspars, quartz a nd a few illite . Table ().l 1XRO Data Locality S!I'W&nt.,.adi 11 (Sa... ant..,adi 1!1lu~•)
( 6. 097)
) , e d-spacing Relative Remarks Intensity
5.09 10.08 6.09 Illite 7. 17 7.16 45.11 Kaolinite 7.93 6.48 4.57 Hie roc line 11.59 4.45 3.&5 Kaolinite 11.85 4.35 3.96 Kaolinite 12.14 4.25 43.89 Quartz 12.44 4.15 3.65 Kaolinite 13.05 3.95 6.82 Hicroclina 13.54 3.82 3.29 Kaolinite 14.05 3.68 3.29 Hicrocline, Illite 14. 51 3.57 32.!:)1 Kaolinite, Hie roc line 14.89 3.48 56.70 Hicroc1ine 15.51 3.34 100.00 Kaolinite, Quartz, Hicrocline, Illite 15.77 3.28 12.19 Hie roc line 16.04 3.23 18.65 Hie roc line 17. 19 3.02 6.70 Hie roc line 17.60 2.95 G. 70 , Hicroc1ine 17.95 2.90 4.26 Hicroc 1ine 18. 76 2.78 2. 13 Hicrocline 20.00 2.61 4.14 Hicrocline, Illite 20.20 2.59 2.74 Hie roc line 20 .47 2.55 4 . 26 Kaolinite 20.78 2.52 4.57 Kaolinite, Hie roc line, llli te 21.36 2.45 12.80 Quartz 22. 55 2.33 13.53 Kaolinite, Hie roc line 23.0':) 2.28 18.29 Kaolinite, Quartz Hie roc line, Quartz 23.57 2.23 10.97 Kaolinite, 24.48 2.15 15.24 Hicrocline, Illite Quartz 24. 8& 2. 12 12.80 Kaolinite, Quartz, Illite 1.6.85 l. 98 7. 92 Kaolinite, 27.66 1. 92 4.38 Kaolinite Quartz 29.46 1. 81 69.50 Kaolinite, 30 .36 1. 76 8.53 Kaolinite Quartz 32.35 1. 67 35.45 Kaolinite, Quartz, Illite 35.45 1. 54 20.72 Kaolinite,
Quar tz are Al pha-Qua rtz. Table 6.2 XRD Data Locality Talawade (Sawantwadi Taluka)
( 5.319)
Sr.No. e d-spacing Relative Remarks Intensity
l. 7. 10 7.19 19.68 Kaolinite 2 . 11.58 4.46 3. 19 Kaolinite 3. 11. 80 4.37 2.65 Kaolinite 4. 12.14 4.26 30.85 Microcline, -Quartz 5 . 13. 00 3.97 3.45 Microcline 6. 13.55 3.84 8.35 Microcline, Kaolinite 7. 13. 90 3. 74 2.65 Microcline, Kaolinite 8. 14.50 3. 57 12.76 Microcline, Kao 1 in it e 9. 14. 92 3.47 6. 11 Microcline
10 . 15 . 51 3.34 100. 00 - Quartz + Kao 1 in it e + Microcl ine 1 l . 15.76 3 . 29 2. 76 Mi l: roc1ine 12. 15. 99 3.24 28 .72 Microcline 13. 17.20 3.02 2.12 Microcline 14. 17.52 2 .95 3.19 Microc 1ine 15. 17. 97 2.89 3.82 ! 6. 18 . 93 2 . 7 5 l. 59 Kaolinite, Mi croc line 17. 19.97 2.62 2.65 Mi croc line 18 . 20.95 2 . 56 2 . 28 Kao linite 19. 20. 13 9 2.50 l. 06 Microcline 20 . 21. 34 2 . 45 9.20 - Quart z 21. 21.60 2 .42 2. 12 Microc line Mi croc line 22 . 22.45 2. 34 4.25 Kaolinite, Kaolinite 23 . 23. 07 2. 28 2. 76 - Quartz, Microcline 24. 23 . 57 2.23 2. 12 - Qua rt z , Microcline 25 . 24 . 47 2. 16 3. 72 Kaolinite 26 . 24 . 9 1 2. 12 2.92 - Qua rt z , - Quartz, Kao linite 27. 26 . 85 1. 98 4. 25 - Ouart z , Kaolinite 23 . 29 . 46 l . 81 20.74 2') . 2 CJ . 77 1. 80 2. 12 - Quart z , Kaolini te 30 . ~l 2 . :; 5 l. 6 7 2 . 92 - Qu;lrtz , Kao linite :J l. J ::, . 4 ~ 1. 54 3 . 29
. ,. l 7. • Table 6.3 XRD DatA Locality Qtavane (Sawnntwndl Talukil )
(5.063)
Sr.No . e d-spacing Relative Remarks Intensity
1. 7. 1 7 7.15 75.94 Kaolinite
2 0 11.50 4.45 4.55 Kaolini te 3 0 11. 86 4.35 2.43 Kaolinite
4 0 ~ 2 0 ll· 4.24 29.87 Qua rtz 5 0 12. 3 7 4 0 16 l. 51 Kaolinite 6 . 13.43 3 . 84 3 . 03 Kaolinite 7 0 14. SQ 3. 57 42.52 Kaolinite
8 0 15 . 5Q 3.34 lOO.QQ Quartz , Ka o linite , ~1 i c r n c l in e 9. 17. 16 3.Q3 2.Q2 Microcl i ne 10. 20.45 2 .55 4.05 Kaolinite
11. 21. Q3 2.49 7.59 Ka o linite 12 0 21.35 2 . 45 10.63 Quartz
J 3 0 22 . Q8 2 . 3 7 3 . 54 Ka o linite
14 0 22.50 2.33 9.87 Kaolinite 15 0 22.98 2 . 29 1. 51 Kaolinite 16 0 23 . 1 Q 2.27 18 .47 Quartz Quartz J 7. 23 . 57 2 .23 14 .68 Ka o linite , Qua r t z 18 . 24 . 86 2 . 12 7.08 Kao lin it ~ , quartz 19 . 26.84 l. 98 6 . Q7 Ka o linitf', f) uart z 20 . 29 . 47 l. 81 11. 13 Ka o lin ite , Quar t z 21. 32. 38 l. 6 7 4. 55 Ka o l ini t e , (Ju a r t z 2 2 0 35.4 5 l. 54 18 . 2 2 4. Q) Ka o lin ite 23 . 37 . QQ 1. 48
All Quart z are Alpha-Qua rt z . Table b.:. : XRD Data Locality Sawantwadi Poo l ( Sawantwadi Taluka)
(8.928)
S r. No. e d-spacing Relative Remarks Intensity
l. 3. 05 14.47 42 .85 Ch l orite
2 . 4 . 3 7 10 . 10 9.37 llli te
J . 6. 13 7. 21 13.39 Kaolin ite
4. 6 . 8 5 6.4 5 8.92 Hie r oc line 5 . 9 . 12 4.85 35.71 Chlori t e
b . 10 . 32 4.29 45.53 Quartz
7 . 10 . 95 4.05 16.07
k . 11. 43 3 . 88 8 . 03 Hie r oc line
g. 11 . 70 3.79 9.82 Chlori te 10 . 12 . 10 3.67 10.44 Illite, Microcline
11. 12. so 3 . 55 11. 16 Kaolinite, Hicrocline
1 2 . 1 3. 2 5 3. 3 5 100.00 Kaolinite, Illite, Microcline Quartz
l 3 . J 3. 7 J 3 . Z~ 94.63 t_licroc line
1 4. 14 . 30 3. 11 8.92 Kaolinite
J 'i. 15.02 2.97 6.69 Microcline
I b. I 5 . I 0 2.95 5.35 ~ hl o rite
I 7 . I 7 . 40 2 . 57 J 0. 71 Kao linite, Microcline
l .~ . 18 .20 2 . 46 29.0 1 Qua rtz
l ':J . 18 . 77 2 .39 7. 14 Kaolinite, Microcline
20. 19.68 2 . 2 8 15. l 7 Kaolinite, Quartz
2 1 . 20 .09 2.24 10 .71 Kaolinite, Quartz
L.'L . 2 1 . 19 2. l3 22 .32 Kaolinite, Quartz
L. 3 . 22 . 82 l. 98 12.49 Kaolinite, Illite, Quartz .C hl orite 24. 23.07 1. 96 6.24 25.00 l. 82 28.56 Kaolinite, Quartz
LL . 1 s. 56 l. 7 8 7. 14 Kaolinite Kaolinite, Illite, Quartz '!.7 . 27 . 46 l. 6 7 10.26 Kaolinite, Quartz 2tl . 2'!.90 l. 54 25.89
:\ 1 1 ({ll :, ,·u. ;,ce A1pha-Quart:t. fable 6.) : XRD Data Locality Mumras (Sawantwadi !eluka)
(&.25)
Sr.No. e d-spacing Relative Remarks Intensity
I. 4.26 12.06 11. 8 7 Sepoli te 2. 5. 10 10.00 10.25 Illite
3. 7.14 7.19 68.75 Kaolinite 4 . 10 . 37. 5.00 3.75 Illite
"J . 11 . 55 4.4& 7.50 Kaolinite, Sapolite, Illite 6. 12. 13 4.25 53.75 Quartz 7. 12 .73 4.06 2.50 Sepolite 8. 12.96 3.98 4.50 Sepolite 9 . 13. 30 3.89 3. 12 Sepolite 10. 14.49 3.57 37.50 l'aolinite, Sepolite
11. 15.47 3.35 100.00 Kaolinite, Quartz, Sepolite, Illite
i 2 . 16 .30 3. 18 3. 7 5 ~!lite 13 . 16 . 94 2.91 3. 75 Sepoli te 14. 19 .47 2.68 5.62 Sepolite
1 5. 20 .05 2.61 1. 87 Illite, Sepolite 16. 20 .48 2. 55 .. 6.25 Kaolinite, Sepolite I 7 . 21. 36 2 .46 17. so Quartz 18 . 22.08 2.38 5.31 Kaolinite 19. 22.46 2.34 5.62 Kaolinite Sepolite 20. 23.10 2. 2 7 9.06 Kaolinite, Quartz, 21. 23.57 2.23 9.06 Sepolite Illite 22 . 24.49 2. 15 4.37 Kaolinite, Quartz, Sepolite 23. 24.35 2.12 14.37 Kaolinite, Illite 24. 26.85 1. 98 6.87 Kaolinite, Sepolite, Quartz 2S. 29.48 1. 81 2 3. 12 Illite 26 . 32 .29 1.67 6.25 Kaolinite 27. 32.65 1. 65 2.50 Kaolinite 28 . 33.52 1. 61 4.68 Kaolinite 29. 35.45 1. 54 20.62 Kaolinite 30 . 36.80 l. 49 5.00
All Quar tz are Alpha-Quartz. Teble 6.(,: XRD Data Locality Nemale (Sawantwadi Tnlukll)
(6.451)
Sr.No. e d ·spacing Relative Remarks Intensity
1. 4.39 10.06 3.22 Illite 2. 6.16 7. 16 11.61 Kaolinite 3. 6. . 82 6.48 4.83 Microcline 4. 10.00 4.43 2.25 Kaolinite 5. 10.44 4.26 56.44 Quartz 6. 11. 17 3.97 12.90 Microcline 7. 11.64 3.82 19.99 Kaolinite 8. 12.03 3.69 10.32 Microcline, .Illite 9. 12.40 3.58 7.09 Kaolinite, Microcline l 0. 12.77 3.48 22.25 Micro<.. line ll. 13.28 3.34 100.00 Kaolinite,_ Microcline, Illite, Quartz 12. 13.73 3.24 63.21 Microcline 13. 14.34 3.10 11.61 Kaolinite
1L. . 14.71 3.02 10.32 l'\ic.roc.line 15. 15.10 2.95 9.67 Microcline 16. 15.38 2.90 9.99 Microcline 17. 16.08 2. 77 6. 77 Microcline, Kaolinite 18. 17. 12 2. 6i" 10.64 Microcline, llli te 19. 17.50 2.56 9.35 Kaolinite, Microcline 20. 17. 77 2.52 9.48 Microcline, Illite 21. 18.28 2.45 16.12 Quartz 22. 18.49 2.43 5.16 Illite 23. 19.27 2.33 5.80 Kaolinite, Microcline 24. 19.72 2.28 18.06 Kaolinite, Quartz 25. 21. 12 2.23 9.67 Microcline 26. 20.87 2.16 14.83 Microcline, Illite 2 7 . 21.21 2. 12 12.90 Kaolinite, Quartz 28 . 21. 7o 2.07 3.87 Kaolinite Kaolinite, Quartz, Illite 29. 22.89 1. 98 13.86 30. 23.55 1.92 4.51 Kaolinite Kaolinite 31. 24.48 l. 86 7.74 Quartz 32. 25.05 1. 81 30.31 Kaolinite, Kaolinite, Quartz 33. 25 .23 l. 80 9.35 Kaolinite, Quartz, Illite 34. 27.43 1. 67 8.38 Kaolinite, Quartz 35 . 27 . 70 l. 65 3.67
;, t l (;11art7 a r e Alph (8.333) Sr.No. e d-spacing Relative Rema r ks Intensity l. 4.35 10. 15 7.91 Illite 2. 6.09 7.26 51.66 Kaolinite 3. 9.95 4.45 6.83 Kaolinite 4. 10.35 4.28 37.49 Quart z 5. 10.59 4.19 5.83 Kaolinite 6 . 12.44 3.57 51.66 Kaolinite, Hicrocline 7. 13.23 3.36 100 . 00 Kaolinite, Quartz, Hicrocline, Illite 8. 13.65 3.26 13.33 Hicrocline 9. 14.29 3.12 22 . 49 Kaolinite 10 . 3.02 3.02 7.49 Hicrocline 11. 17.46 2.56 11.66 Hie roc line 12 . 18 . 18 2.46 15.83 Quartz 14. 18.84 2.43 6.83 Hicroc line, I 11 i te 15. 19.07 2.35 8.33 Kaolinite, ~lie r oc line 15. 19.64 2.29 18.83 Kaolinite, Quartz 16 . 20.05 2.24 11.66 Hicrocline, Quartz 17. 20.65 2. 18 4.99 Kaolinite 18. 21. 15 . 2. 13 10 . 83 Kaolinite, Quartz 19 . 22.84 1. 98 7.49 Kaolinite, Illite, Quartz 20. 24.97 l. 82 28.33 Kaolite, Quar t z 21. 27.38 1.67 29.16 Kao linite, Illite, Quartz 22. 28.90 1. 59 4.99 Kaolinite, Quartz Quartz 23. 29.90 1. 54 17.49 Kaolinite, Illite, All Qua rtz are Al pha-Quartz . Table 6.8 XRD Data. Locality Kankauli, Taluka Kankau1i. Sr.No. e d-spacing Relative Remarks Intensity 1. 5.06 10.16 7 . 18 Illite 2. 7. 15 7. 1d 13.07 Kaolin! te 3. 7.92 6.49 9.80 Microcline 4. 12.12 4.26 66.66 Quartz 5. 12 . 96 3.98 11.76 Microcline 6. 13.47 3.83 16.99 Kaolinite 7. 13.96 3.70 13.07 Microcline 8. 14.21 3.65 8.49 Microcline, Illite 9. 14.45 3.58 6.536 Kaolinite 10. 14.86 3.48 23.52 Microcline 11. 15.45 3.34 100.00 Quartz, Kaolinite, Hicrocline, Illite 12 . 15.75 3. 29 12.41 Microcline 13. 15.92 3.24 97.38 Hicrocline 14. 16.15 3. 19 5 . 22 Illite 15. 17. 16 3.02 9.80 Hie roc line 1 G. 17.59 2.96 16.34 Hie roc line 17. 17.94 2.90 16 . 34 Hie roc line 18 . 18 .91 2. 7 5 5.88 Kaolinite, Hicrocline 19. 19.92 2.62 5.22 Hicrocline, Illite 20 . 20.79 2.52 5.22 Kaolinite, Hicrocline, Illite 21. 21.31 2.46 22.87 Quartz 2 2 . 22 . 50 2.33 5.22 Kaolinite, Hicrocline 23. 23.06 2. 28 39.21 Quartz, Kaolinite 24 . 23 . 56 2.23 16.34 Quartz, Kaolinite, Microcline 25. 24 . 44 2.16 18.30 Kaolinite, Hicrocline, Illite 26. 24.85 2.12 14.37 Quartz, Kaolin! te 2 7 . 26.84 l. 98 14.37 Quartz, Kaolinite, Illite 28. 28.76 l. 85 8.49 Kaolinite 29. 29.45 1. 81 39.86 Quartz, Kaolinite 30 . 32.33 l. 67 13 . 07 Quartz, Kaolinite 31. 35.45 :.54 43.79 Quartz, Kaolinite, I 11 ite All Quartz are Alpha-Quartz. Table 6.9 XRD Data. Locality Janauli II, Kankauli Taluka. (7.812) Sr.No. 0 d-spacing Relative Remarks Intensity 1. 3 .09 14 .28 19. 53 Chlorite 2. 6. 18 7. 15 47.65 Kaolinite 3. 6.8S 6.45 7. 81 Microcline 4. 9 .35 4.74 15.62 Chlorite 5 . 10.40 4.26 63.66 Quartz 6. 11.00 4.03 14.06 Chlorite 7. 11.55 3.84 13.67 Kaolinite 8. 11. 96 3.71 6.24 Microcline 9 . 12. 50 3. 55 22.65 Kaolinite 10. 12.7 5 3.49 11.71 Microcline I I . 13.27 3.35 100 . 00 Quartz, Kaolinite, Hicrocline 1 2 . 13.70 3. 2 5 60.93 Hie roc line 13. 14.73 3.02 8.59 Hicrocline 14. 15. 08 2.95 13.67 Hicrocline 15. 16.20 2. 76 3.12 Kaolinite, Microcline 16. 17.26 2.59 5.07 Hicrocline 1 7 . 17.45 2.56 8.59 Kaolinite 18 . 17.70 2.53 5.46 Kaolinite 19. 18 .23 2.46 35.93 Quartz 20 . 18.75 2.39 6.01 Kaolinite, Microcline, Chlorite 21. 19. 24 2.33 3.90 Hicrocline, Kaolinite, Chlorite 22. 19.70 2.28 22.26 Quartz, Kaolinite 23. 20. 12 2.23 7.03 Quartz, Kaolinite, Hicrocline, Chlorite 24. 20.87 2.16 14.68 Kaolinite, Hicrocline 25. 21.20 2. 12 21.48 Quartz, Kaolinite 26. 21. 79 2. 07 4.68 Kaolinite 27. 22.36 1. 98 12 .10 Quartz, Kaolinite 28. 23.54 1. 92 3. 12 Kaolinite 29. 24.04 1. 89 9. 37 Kaolinite 30. 24.55 1. 85 3.51 Kaolinite 31. 25.02 1. 81 35.93 Quartz, Kaolinite, Chlorite 32. 25.25 1. 80 7. 81 Kaolinite 33. 25.53 l. 78 7.42 Kao 1 in i te 34. 26.62 1. 72 6.09 Kaolinite 35. 2 7. 4 2 1. 6 7 5.85 Quartz, Kaolinite 36. 29.30 1. 57 7.42 Kaolinite 37. 29.94 1. 54 32.02 Quartz, Kaolinite All Quartz are Alpha-Quartz. I 'I I • \ r I ,, \" ' \Rr f ':1 1_tl I .• r 'I} it y K11 mhh"r'" ''t t 7 (~In I , ..111 I .1 ! 11L1) (5.263) S r. No. d-spacin~ Relative Remarks Intensity I. :, . 13 9.98 t14. 7 3 ~1uscov i le 7. . 7. I 'j 7. 18 I 2. 4 7 Kaolinite 3. 10 .34 4.98 20.52 Muscovite 4. II. 54 4 . 47 7.36 Muscovite '!. I 2. 12 4.26 59.99 -Quartz b . I .1 . .1 4 3.87 5.26 Muscovite 7 . 13. 87 3 . 73 3. 15 Muscovite, Kaolinite 8 . 14. 46 3.58 5 . .52 Kaolinite 9 . 14 . 8 5 3.49 7.10 Muscovite 10 . 15 . 49 3.34 100.00 -Quartz, Muscovi le, Kaolinite 11. 16.23 3.20 7.89 Muscovite 12. I 7. 39 2.99 ll. 97 Muscovite 13. 18. 24 2.85 7.36 ~1uscovi te 14. 18.69 2. 79 5. 70 Muscovite l ~~ . 20 . 19 2. 59 l. 57 Muscovite 16 . 20 .40 2. 56 7.36 Muscovite, Kaolinite l 7. 21. 03 2 . 49 2. 10 Muscovite, Kaolinite 18 . 21 .34 2.45 19.47 Muscovite, - Quartz 19. 22.07 2. 37 2.63 Muscovite, Kaolinite 20 . 23 . 06 2. 2 8 13. 15 - Quartz, Kaolinite 21. 23.56 2.23 13.05 Muscovite, - Quartz 22. 24 . 26 2. 12 l 0. 52 - Quartz, Kaolinite 23 . 26 . 65 1. 99 13. 15 Muscovite, Kaolinite 24 . 26.84 1. 98 3.68 Muscovite, - Quartz 25 . 29.46 l. 81 15.26 - Quartz, Ki!olinite 26 . 32.32 1. 6 7 3. 15 -Quartz, Kaolinite 2 7. 32.60 1. 66 2. 10 Muscovite, Kaolinite 28. 32.93 1. 64 2. 10 ~1uscovi te Kaol i nite 29 . 35 .44 l. 54 13 . 15 Muscovite, -Quartz, All Quartz are AI plw-Quar tz . Table b.!!: XRD Data Locality Kumbharmatt 3 (Mal van Taluka ) (5.208) Sr. No . e d-spacing Relative Remarks Intensity 1. 5.16 9.96 16.14 Muscovite/Illite 2. 7. 19 7. 15 44.78 Kaolinite 3. 10 . 35 4.97 6.24 Illite/Muscovite 4. 11.60 4 . 44 3.64 Kaolinite 5 . 12. l 3 4.26 54. 16 -Quartz 6 . 12.36 4.16 1. 56 Kaolinite 7. 14.50 3.57 27 . 08 Kaolinite 8. 15 . 50 3.34 100.00 -Quartz, Kaolinite, Illite/~~s ccv ite 9. 16.25 3. 19 2.08 Muscovite/ Illite l 0 . 17.4 2.98 3 . 12 Muscovite/Illite 11. 18 . 2 5 2.85 2.08 Muscovite/Illite 12. 18 .7 3 2. 77 l. 82 Muscovite/Illite 1 3 . 20 . 4 1 2.56 5.20 Kaolinite / ~scoyj_te 14. 20 . 70 2. 52 1. 56 Kaolinite- Illite I S . 21. 02 2.49 4.68 Kaolinite 16 . 2 1. 34 2.45 20.83 -Quartz 1 7. 22.011 2. 38 2 . 2 3 Kaolinite 18 . 22 . 50 2.33 4.24 Kaolinite 19 . 23 . 08 2. 28 20. 31 Kaolinite, -Quartz 20 . 23 .5 7 2.23 5. 72 Quartz, Muscovi te 21 . 24.85 2. 21 14.32 Kaolinite, -Quartz Illite 22. 26.6fl 1. 99 6.24 Kaolinite- 2 J . 26 . &4 1. 98 3. 12 - Quartz 24 . 29 .4 5 1. 82 21.87 Kaolinite, -Quartz 25 . 32.34 1. 6 7 7.20 -Quartz, Illite/Muscovite Muscovite 26 . 32.62 1. 65 l. 56 Kaolinite, -Quartz, Muscovi te/llli 27 . 3 5 . 1,4 l. 54 12 .49 Kaolinite, -Quartz, All f Jtld r t z '' r e Alpha - Quortz. TA b lef-.12: XR!l [)at a Locality Kumbharmatti 4 (M a l vAn Tnluka) ( 5. 319) Sr.~ o . e d-spacing Relative Remarks Intensity l. 5. 16 9.94 57.9 7 Muscovite 2 . 7. 21 7. 12 18.61 Kaolinit e 3 . 10. 36 4.97 17.02 Muscovite 4. 11. 57 4.46 6.38 Kaolinite + ~1uscov it e 5. 12. 13 4. 26 63.56 -Quart z 6 . 13. 34 3.87 4. 78 Muscovite 7. 13.88 3. 72 5.31 Kaolinite 8 . l ~. 4 7 3.58 9.57 Ka olinite 9 . 14.85 3.49 5.85 Muscov ite 10 . 15. 50 3. 34 100.00 - Quartz, Kaolinite, Musco v ite l I . 16.26 3. 19 7.44 Mus covite 12 . 1 7. 4 5 2 . 98 9. 57 Mus covi t e 13 . 18. 26 2.85 7.97 Mu scovit e jt,. 18 . 7 2 2. 78 5.31 Musc ovite 15 . 20. 18 2.59 1. 59 Mus cov ite 16 . 20 . 44 2.56 6.91 Ka o linite + Muscovite l 7 . 21.04 2.49 3. 72 Kaolinite + Muscovite 13 . 21 . 36 2.45 13.56 - Qua rtz, ~1uscovi te 19 . 22. 10 2.37 2. 12 Muscovite, Kaolinite 20 . 23. 08 2. 28 14. 62 Kaolinite, - Qua rtz 21. 23.59 2 .23 6.91 Mu scovite , - Quartz 22 . 24 . 86 2.1 2 20. 21 Kao linite , - Quartz 2 3 . 26.67 l. 99 12. £3 Muscovite 2,, . 26.90 l. 98 6.38 - Qua rt z , Ka o linite - Quartz, Muscovite 2j , 29 . 47 I. 81 20.90 Ka o linite, - Quartz, Mus covi t e 2<> . 32 . 35 1. 67 6.91 Kao linite , Ka o linite, - Quartz , Mus covi te ~7 . 35 .46 l. 54 9.73 All r; uilr t z n r e Al pha-Ouar tl. 1 Tablehol : XRD Oat a Locality Han:;~,aon (Kudal Taluka) (6.535) Sr.No. e d-spacing Relative Remarks Intensity l. 4.34 10. 17 2.61 llli te 2. 6.07 7. 28 9.80 Kaolinite 3. 6.75 6.55 3. 92 Microcline 4. 7.41 5.97 3.92 Microc line 50 9.92 4.47 2.94 Kaolinite, Illite 6. 10.38 4.27 89.85 Quartz 7. 11. 10 4.00 5.88 Microcline 8. 11. 51 3.86 18.95 Microcline 9. 11.94 3. 72 8. 16 Kaolinite 10 . 12. 09 3.67 4. 57 Illite 11. 12 .33 3.60 8. 16 Kaolinite, Microc line 1 2. 12.75 3.49 18.62 Microcline 13. 13.25 3.36 100.00 Kaolinite, Illite, Quartz, Microc line 14. 13 .67 3. 25 92.79 Microcline 15. 14.30 3.11 93.45 Kaolinite 16 . 14. 7 5 3.02 10.45 Microc line 17. 15. 04 2.96 14.37 Microcline 18 . 15 . 35 2.90 14.05 Mi c r oc line 19 . 16. 1 fl 2.76 2.94 Microcline 20 . 17. 08 2.62 3.92 Microcline, Illite Microcline 21. 17.40 2.57 4.57 Kaolinite, Mi c rocline 22 . 17.70 2.53 4.70 Kaolinite, Quartz 23 . 8 . 20 2.46 30.71 Kaolinite, Microcline 24. 18.77 2.39 4.05 Kaolinite, Microcline 25 . 19. 20 2.34 7. 18 Kaolinite, Qua rtz 26 . 19 . 68 2.28 32.67 Kaolinite, Microcline, Quartz 27. 20 . 08 2.24 11. 76 Microc line, I llite 28 . 20 . £5 2. 16 17.97 Kaolinite, Quartz 29 . 21. l g 2.13 28.10 Kaolinite, I llite, Quartz 30 . 22 . 85 l. 98 13.07 Ka o l inite 31. 24 . l 5 1. 86 6 . 53 Ka o linite, Qu a rtz 32 0 2 5. 00 l. 82 33.98 Kno lini.te , Qu artz 23 0 27.38 l. 6 7 13. 7 2 Kao lini te , Qua rtz ., 2 7. 6 7 1. 65 4.24 ~· 0 ~;J •J li n it c , l! J i t e , Qua rt z 2) . 29 . 92 1. 54 L3 . 19 ------·- · 1 . ~ ~ - ( f\. I ~- ,r- .t - • 1 1.1 r· t. : . l.ocil l i ty (5o649) 5 r . ~, ·' . d-spncin,: fh •l iltive Rt->lll it rk s Int e nsity l. s 0 14 lOoOO 3 o95 Illite 2. 7 . I 3 7 0 l 7 4 0 ) I Kaolinite 3 . 7 . ') 7 6o46 II o29 Microc iine " . II olll> 4.42 6. 21 Kaolinite 5 . I 2 . 1 11 4.24 33.89 Quartz 6o 1 2.~6 4.02 7.34 Microcline 7. l 3 . (J l 3.97 3.95 Microcl ine 8 . 3 .82 4.68 Microcline + Kaolinite 'J . I :. 0 I 3 3.66 :l2 . 03 Microc line 10 . 14 . % 3.46 19.48 Microcline 11. I 5 o') 3 3.34 100.00 Kaolinite + Quartz -+ Illite U. I 'i . rlO 3.28 22.59 Microcline 13 . 1 h . n I 3.24 77.95 Microcline l b 0 l i 3. 18 14. 12 Illite I 5o l 7 . l ') 3.02 18.64 Microcline I 6. l 7 o '•U 2 .97 11. 86 Microcl ine I 7 o I I o 'J ~ 2.89 6. 77 Mi croc line + lll i t e 1 h . I h 0 .lt > 2o84 4. 18 19. l K. 'J ,., 2. 7 5 5.60 Kaolinite + Microcline 20. :!() .U L 2.6I II. 29 Microcline , Illite 21. 2.56 3.95 Kaolinite, Hicrocline Kaolinite + Microc line n . l( l . 17 2 .52 3.38 9.60 Quartz 23 . 2 I o .lll 2o45 5.08 Microcline, Illite 24 0 L I o h >: 2o42 Kaolinite + Hicrocline 25. 21. .57 2. 32 5.08 Quartz, Ka o li nile 26 . 2 l. l I 2.27 16.94 n. 2023 6. 21 Mi crocline , Quartz Microcline, Illite 28. 24.4 K 2. 16 13. 55 19. 20 Kaolinite + Quartz 29. 24 0 )l 'J 2 ol 2 Kaolinite + Quartz + I llite 30. I. 97 9.03 --· ------ Al l llll,iil · ' " ' . \ ~jt!I ( I- 1/I J . ill/ . Table 6.1':1 XRD Data LocalitY Pat Red (Kudal Taluk11) (S.376) Sr.No. e d-spacing Relative Remarks Intensity 1. 7. 18 7. 15 53.76 Kaolinite 2. 11. 55 4.46 2.68 Kaolinite 3. 12.12 4.2& 39.24 Quartz 4. 14.45 3.58 51.60 Kaolinite 5. 15.48 . 3. 35 100 . 00 Kaolinite + Quartz 6. 21.00 2.49 4.30 Kaolinite 7. 21.33 2.45 21.07 Quartz 8. 22.06 2.38 4.83 Kaolinite 9. 22.40 2.34 5.91 Kaolinite 10. 23.07 2.28 17.20 Quartz + Kaolinite 11 23.57 2.23 5.91 Quartz + Kaolinite 12. 24.36 2.12 8.60 Quartz + Kaolinite 13. 26 . 84 1. 98 10.75 Kaolinite + Quartz 14. 29.44 1. 81 30.64 Kaolinite + Quartz 15. 32.32 1.67 6.98 Kaolinite + Quartz Kaolinite + Quartz 1& . 32.5& 1.66 4.30 Kaolinite + Quartz 17. 33.45 1.62 2.68 All Quartz are Alphii·Ouartz. Table 6.16 XRD aata. Locality Kasal, Taluka Kudal. Sr. No. d-spacing Intensity Remarks Relative 1. 7.13 7.18 47.65 Kaolinite 2 . 11.62 4.44 5.70 Kaolinite 3 . 12.11 4.26 71. 18 Quartz 4 . 14.51 3.57 25.88 Kaolinite 5 . 15.49 3.34 100.00 Kaolinite, Quartz 6 . 20.41 2.56 2.94 Kaolinite 7. 21.34 2.45 17.06 Quartz 8 . 23.08 2.28 4.29 Kaolinite, Quartz g . 23.58 2.23 4.70 Quartz 10 . 24.85 2.12 6.47 Kaolinite, Quartz 11. 26.87 1. 97 5.88 Quartz 12 . 29.46 1. 81 14.70 Kaolinite, Quartz 13 . 32.33 1. 77 3.82 Kaolinite 14. 35.46 1. 54 8.23 Kaolinite, Quartz 15 . 36.90 1. 48 2.05 Kaolinite All Quartz are Alfa-Quartz. Table 6.1J, XRD Data Locality Tak 1 (Vengurla Taluka) (5.55) Sr.No. e d-spacing Relative Remarks Intensity 1. 7. 14 7.18 100.00 Kaolinite 2. 11.55 4.45 4.44 Kaolinite 3 . 11. 81 4.36 9.43 Kaolinite 4. 12.07 4.27 3.60 Kaolinite 5. 12.30 4.19 8.32 Ka o linite 6. 13.41 3.85 3.88 Kaolinite 7. 14.46 3.57 66.60 Kaolinite 8 . 15.49 3.34 2. 77 Kaolinite 9 . 20.40 2.56 6.10 Kaolinite 10 . 20.64 2.53 3.88 Kaolinite ll. 20.96 2.50 9.43 Kaolinite 12. 22.06 2.38 4.44 Kaolinite 13. 22.44 2.34 19. 14 Kaolinite 14 . 22.93 2. 29 7.21 Kaolinite 15. 23.94 2.20 2.22 Kaolinite 16 . 26.67 1. 99 5.27 Kaolinite 17. 32.45 1. 66 3.88 Kaolinite 18 . 33.35 1. 62 2.22 Kaolinite Tabl( ll.l'-. XR D Da La Locality Tak 2 (Ven ~o; ur1a Ta1 uka) (5. 31 Sr.!\o. 8 d-spacing Relative Remarks Intensity l. 7. 13 7.14 100.00 Kaoliuite 2 . l 1 . 57 4.45 5.31 Kaolinite 3 . I 1. 86 4.34 15.42 Kaolinite 4 . 12 .43 4. 15 20.21 Kaolinite ) . I 3. 15 3.93 2.65 Kao linite 6. I 3 . 50 3. 83 7. 97 Kaolinite 7 . 13 .84 3.73 3.98 Kaolinite 8 . 14.46 3.57 98.40 Kaolinite C) , 14 .92 3.47 3. 72 Kaolinite I U. 15 .4 () 3.36 6.91 Ka o l inite 11. 16 .47 3. 13 2.65 Ka o l inite 1! . 16 . 80 3.09 2.65 Kaolinite l l. 18.96 2.61 3.72 j.,. 20 . 4 'J 2.55 6.91 Ka o linite I '>. 20 . 67 2.53 4 .25 Kaolinite 1l> . 21.04 2.49 7. 97 Kaolinite I 7 . 21. 59 2.43 3. 19 1 "· . 22 . 07 2. 38 27.65 Kaolinite 1') . 22 . 50 2.33 18. 08 Kaolinite 2U. 22 . 97 2.29 10. 63 Kaolinite L I . 23. 4CJ 2. 2 5 1. 59 . ' 26 . 6 ) 1. 99 5.85 Kaol inite ~ L ' .: ·. . .! t 1 . BU I. 98 5.85 Ka o linite Ka o linite ~ 4. '27 . 50 l. 93 3.98 Kaolinite 2 c., . 2 B. I S l. 89 3. 19 Kaolinite 2b . 2 9 . I 5 l. 83 3.72 Kao1 ini te i• 'l . 1U . OO 1. 78 12. 23 Kaolinite 2!:!. 31.00 1. 7 3 1. 59 Kaolini te :.!9 . 32 . 55 1.66 6.91 Kaolinite 30. 33.53 l. 61 5.05 Kaolinit• 3 1 . 34 . 35 l. 58 1. 96 1. Kaolinite l2 . 35. 35 l. 54 59 ------· All ()\1 o r l L. a r e Alj,lw-Quar lL. Table 6.\Q : XRD nata I IIC illlty Mahapan (Ven11,urla Tnluka) ('i .J7L) .> r. No . d-spnc in>; Relative Remarks In.tensi ty 1. 7.17 7. 16 15.96 l':aolinite 2. 7.91 6.49 2.68 Hie roc line 3. 11.61 4.44 3. 22 Kaolinite 4. 12. 17 4.24 31. 71 -Quartz, Hie roc line 5 . 12.40 4. 16 2.90 Kaolinite 6. 13. 10 3.97 4.83 Hicrocline 7. 13.55 3.81 2. 15 Microcline 8 . 14.03 3.69 2.95 Hicrocline 9 . 14 .4 7 3. 57 8.60 Hi c rocline + Kaolinite 10 . 1/o 94 .1 .46 4.56 Hicrocline I I . IS. 53 3.34 100.00 -Quartz, Micn•c.. line, Kaolinite I 2. 15.77 3.28 11.98 Hicrocline 13 . 16.03 3 .24 50.53 Hicrcc line 11·. 17.30 3.00 2.68 Kao 1 in it e I 5. 17. 50 2.97 2.68 Hie roc line I G. 17. 97 2.89 6. 18 Hicroc 1ine I 7 . 18. 87 2. 76 3. 8 7 Hicrocline 1 q . 20. t, 5 2. 56 7. 25 Hicrocline + Kaolinite l 9 . 21. 04 2.49 1. 7 2 Hicrocline + Kaolinite 20 . 21. 39 2.45 2. 79 - Quartz 21. 21.63 2.42 3. 76 ~licro c line Mi c roc 1ine + Kaolinite f. "l 22 . so 2.33 4.83 - Quartz + Kaolinite 1. 3 . 23 . 08 2. 27 5. 37 Mic r oc line 2 4. 23 . 57 2.23 6.98 Microc line 25 . 24 . 4 5 2. 16 4.03 Ka o linite + - Quart z :::, . 24. 138 2 . 12 4.30 Kao lini t e + - Qua rt z 26 . fl l 1. 98 3 . 76 9.40 K.:~o linite B . 29.46 1. 81 Ka o linite, -Quartz 29 . 3 2 . 31, 1. 6 7 3. 2 2 6 . 7 2 Kao linite, - Quartz. 30 . 35 . 45 l. 54 ,\ l l l)ua rtz are Al pha-Ou;H t z . Table 6oXl: XRD Data Locality Adeli (V engur1a Ta1uka) ~ 6o250~ 12o195 SroNoo d-spacing Relative Remarks Intensity