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Clay mineral(mineralogy)
1. DEPARTMENT OF APPLIED GEOLOGY
DR. HARISINGH GOUR VISHWAVIDYALAYA
SAGAR, M.P
( A CENTRAL UNIVERSITY)
CLAY MINERALS
Under The Guidance Of:- Presented By:-
Dr. G.C. Gautam Lavkush Maurya
Assistant Professor M.Tech 1st Sem.
Dr. H.S.Gour V.V. Sagar Reg.No.- Y18251014
2. Chemically ,clay minerals are hydrous aluminium phyllosilicates ,sometimes they
occur with variable amounts of calcium,magnesium,iron ,sodium and potassium.
Clay mineral are usually ultra fine grained normally considered to be less than
2μm in size on standard particle classification.The upper limit of clay size is 4µm.
Because of size it require special technique for study. These include X-ray
diffraction,electron diffraction and various spectroscopic methods
Clay is a naturally occurring material composed primarily of fine grained
minerals, which shows plasticity through a variable range of water content and
which can be hardened when dried or fired.
INTRODUCTION
8. (a)1:1 clay structure
CLASSIFICATION OF CLAY
All clay minerals are made of different combinations of two sheets-tetrahedral sheet and
octahedral sheet.
Ex-kaolinite ,halloysite
O
Al
Si
9. (b)2:1 clay structure
CLASSIFICATION OF CLAY
All clay mineral are made of different combinations of two sheets-tetrahedral sheet and
octahedral sheet.
Ex- montmorillonite, illite and vermiculite
O
Al
Si
10. KAOLINITE
1:1 phyllosilicate mineral(platy shape)
There is no
interlayer swelling
Low cation exchange
capacity
Kaolinite is a pure, white
firing clay
It also contains
quartz,ilmenite,rutile and
haematite.
Bonding between the layers
are vanderwaals forces and
hydrogen bonding
12. OCCURRENCE
Kaolinite are as primary residual deposits formed by weathering or low
temperature hydrothermal alteration of feldspar,muscovite and other Al
rich silicates usually in acid rocks.(granites,rhyolites,quartz,diorite ,etc.)
2KAlSi3O8 +3H20 Al2Si2O5(OH)4+4SiO2+2K(OH)
In secondary deposits, parent minerals have been transported under
suitable non-alkaline condition and deposited in deltaic,lagoonal or other
non-marine environment.
13. 2:1 Structure
It is most
expendable of all
place
Layers are weakly
bounded by weak o-
o bonds or cation
oxygen bond
High cation exchange
capacitiy
SMECTITE
15. ILLITE
2:1 Structure
Non-expanding
Cation-exchange capacity
of illite is smaller than that
of smectite but higher
than that of kaolinite
Interlayer spacing of
structure are filled by K
cations resulting non-
expanding nature
It is product of early
alteration of Mica
17. VERMICULITE
2:1 Structure
Moderate to high expandable
High cation exchange capacity
Vermicullite is weathered product of micas in
which K+ ions between molecular sheets are
replaced by Mg+2 and Fe+2 ions
19. PARAGENESIS
SMECTITE AND ILLITE: In the burial diagenesis of mudrocks,
increasing depth and temperature facilitate the conversion of di
octahedral smectite to illite, and tri octahedral smectites to chlorite.
VERMICULLITE: These are formed by alteration of
phlogopite/biotite,chlorite,pyroxene,etc resulting in ultrabasic and
basic rocks.
20. USES
In ceramics( it is main component of porcelain)
In paint it is used to extend titanium dioxide white pigment and modify gloss levels
In cosmetics(pre-work skin protection and barrier creams)
In paper industry
KAOLINITE
SMECTITE
In drilling of Water & oils wells
Stopping leakage
As lubricant
21. VERMICULITE
In fireproofing of structural steel and pipes
Exfoliated vermiculite provides a low density material with excellent thermal
and acoustic insulation properties
In seed germination
22. REFERENCE
MINERALOGY-DEXTER PERKINS
INTRODUCTION TO MINERALOGY-WILLIAM
D.NESSE
AN INTRODUCTION TO ROCK FORMING
MINERALS-J ZUSSMAN
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