(^eotl^emttal B>tnUti of t^t $f)odpl^orite IBtpofiitsi ^rounb Mmnt^ iHata, ^baipur Mi&txitt,

DISSERTATION SUBMITTED IN PARTIAL FULFILMENT FDR THE

AWARD OF THE DEGREE OF

jlaster of l^Ulo&opW IN

GEOLOGY

AALE NABI

DEPARTMENT OF GEOLOGY ALIGARH MUSLIM UNIVERSITY

ALIGARH (INDIA)

1988

DS1431

ALffiARN MUSLm (IMVEftSfTy, AU6ABH

Dr. LIAQftT A.K, RAO M.Sc.,M.Phil.,Ph.D. P.G.Dip.Hydrogeology Dip.Statistics (Alig)

Lecturer

Dtrrr. OF GEOLOGY ALIGARH - 2 0 2 0 0 1 (India)

Dated 2,0-1-\9^^

This is to certify thar Mr. Aale Nabi has

completed his research work under my supervision

for the degree of Master of Philosophy of the

Aligarh Muslim University, Aligarh. This work is

an original contribution to our knowledge of the

phosphorite deposit around Nimuch Mata, Udaipur

district,. Rajasthan, and has not been published

anywhere.

He is allowed to submit the work for the

M.Phil, degree in Geology of the Aligarh Muslim

University, Aligarh.

(LIAQAT A.K. RAO) Supervisor

THIS WORK IS DEDICATED TO MY REVEREND PARENTS

FOR I WILL BE NEEDING THEIR PRAYERS TODAY,

TOMORROW AND ALL TIMES TO COME.

TO tfY PARENT'S FAMILY WITH ALL MY LOVE

INDEX OF CONTENTS

Table of Contents - - - - _ - j

List of figures - _ - - _ - v

List of tables - _ _ - _ - vi

Chapter I - - - - _ « 1-14

C h a p t e r I I 1 5 - 2 6

C h a p t e r I I I _ - _ - - - . 2 7 - 2 8

C h a p t e r IV 2 9 - 3 3

C h a p t e r V 3 4 - 3 7

C h a p t e r VI - - _ _ . _ _ 3 8 - 5 1

C h a p t e r VII - - - - - _ 5 2 - 6 0

Chapter VIII 6 1 - 6 6

Bibliography - - _ - _ _ 6 7 - 7 8

Explanation of Plates - - - -_-. 79 -81

TABLE OF CONTENTS

PAGE No,

Chapter I INTRODUCTION 1

General statement 1

Location and accessibility 1

Climate 1

Topography 2

Drainage and vegitation 2

Status of Nimuch Mata phosphorite 2

Previous work 3

Purpose of the work 5

Methods and presentation of work 6

ACKNOWLEDGEMENT 14

Chapter II STRATIGRAPHY AND GEOLOGICAL SET UP 15

Sequence and lithology of rock types 2 2 around Nimuch Mata

Phyllites 23

Dolomitic limestone 24

Orthoquartzite 24

Post Aravalli granite and ?5 quartzvein

Stiructure 25

Non-Tectonic structures 25

Bedding plane 25

Axial plane foliation 26

i i

T e c t o n i c s t r u c t u r e s

J o i n t s

F o l d s

F a u l t s

26

26

26

26

C h a p t e r I I I NATURE AND MODE OF OCCURENCE OF PHOSPHORITE

Nature of phosphorite

Colunmar stromatolitic phosphorite

LaminatecS/stratiform stromatolitic phosphorite

Mode of occurence of phosphorite deposit

27

27

27

28

28

Chapter IV STROMATOLITES

General statement

Occurence and characteristic

Collenia columnaris

Minjaria colceolata

Collenia baicalica

29

29

29

30

30

31

Compound s t r o m a t o l i t e s s t r u c t u r e 31

D i s c u s s i o n 32

Chapter PETROMINERALOGY

Phosphorite

Cellophane

34

34

34

iii

Quartz 35

Calcite and dolomite 35

Accessory minerals 36

Dolomitlc limestone 36

Quartzite 36

Chapter VI GEOCHEMISTRY AND DISTRIBUTION OF MEJOR OXIDES

38

General s t a t e m e n t 38

D i s t r i b u t i o n of major oxides 38

Alumina 38

S i l i c a 40

F e r r i c ox ide 40

Ferrous ox ide 40

Titanium 40

Manganese 40

Lime and magnesia 41

Phosphorus 41

Soda and p o t a s h 41

Loss of i g n i t i o n 41

Carbon-d i -ox ide 4 2

Composition and mutual r e l a t i o n s h i p of s i g n i f i c a n t ox ides 42

Mutual r e l a t i o n s h i p of s i g n i f i c a n t 44 ox ides

iv

Chapter VII GEOCHEMISTRY AND DISTRIBUTION OF TRACE ELEMENTS 52

Copper

Cadmium

Chromium

Cobalt

Nickle

Zinc

Lead

Rubidium

53

55

55

57

57-

58

59

59

Chapter VIII SUMMARY AND CONCLUSION 61

B I B L I O G R A P H Y 67

E X P L A N A T I O N OF P L A T E S 79

LIST OF FIGURES

1. Location map of phosphate deposits around Udaipur, Rajastahan ( India ),

2, Geological map showing the phosphate occurences around Udaipur district. Rajasthan ( India ) ,

3, Histograms of frequency percent distribution of major oxides in Nimuch Mata phosphorite.

4. Relationship of Po^S ^^^ ^•^^2' • ®2°3' ^^^' MnO, CaO and MgO. CaO + Po^B ~ ^^2* CaO/PjOc - HjO in Nimuch Mata phosphorite.

5. Triangular diagrams showing compositional variation of major oxides in Nimuch Mata phosphorite.

6. Histograms showing the relative distribution of certain trace elements in Nimuch Mata phosphorite.

7. Relationship of ^2^5 ^ * » * » ^ » *^' Ni, Zn, Pb and Rb in Nimuch Mata phosphorite.

v i

LIST OF TABLES

G e n e r a l s t r a t i g r a p h i c framework of t h e A r a v a l l i m o u n t a i n r a n g e .

I I G e n e r a l i z e d s e q u e n c e of t h e A r a v a l l i r o c k s a l o n g D e b a r i - U d a i p u r r o a d .

I l l C l a s s i f i c a t i o n of t h e P r e c a m b r i a n r o c k s of U d a i p u r .

IV The s t r a t i g r a p h i c s u c c e s s i o n of t h e p h o s p h o r i t e b e a r i n g s h e l f d e p o s i t s .

G e n e r a l i z e d s e q u e n c e of A r a v a l l i r o c k s a r o u n d Nimuch Mata p h o s p h o r i t e .

VI Chemica l c o m p o s i t i o n of Nimuch Mata p h o s p h o r i t e , U d a i p u r ' d i s t r i c t . R a j a s t h a n .

VII C o r r e l a t i o n m a t r i x of f o u r t e e n Nimuch Mata p h o s p h o r i t e s a m p l e s f o r t w e n t y one v a r i a b l e s .

V I I I S i O j / A l j O j , MgO/AljOj, F e 2 0 3 / A l 2 0 3 ,

Fe203/FeO, CaO/PjOg, CaO/MgO, Na^O/KjO

and CO2/P2O5 r a t i o s f o r Nimuch Mata

p h o s p h o r i t e .

IX R e c a l c u l a t e t o 100 %rt36 o f t h e b u l k coH^xjaewts o f MgpO, ^ 2 % ^'^ C a o .

vii

X Recalculated to 100 wt% of the bulk components of MgO, ^.0+ and SiOj*

HjO"*", CO2 an(

phosphorite.

HjO"*", CO2 and Pj^S ^" Nimuch Mata

XI Comparision of the abundance of trace elements in phosphorites.

XII Trace analysis of Nimuch Mata phosphorite samples.

LOCATION MAP OF PHOSPHATE DEPOSITS AROUND

UDAIPUR,RAJASTHAN( INDIA)

75°A3' 45'

24« 30

FIG.1

C H A P T E R - I

I N T R O D U C T I O N

G e n e r a l S t a t e m e n t :

The phosphorite deposits of Udaipur district,Rajas-

than were first reported from the Precambrian Aravaili meta-

sediments at Kharwaria, Kanpur, Matoon and Dakan Kotra by the

Officers of Geological Survey of India in early 1967 and at

Jhamar Kotra, Neewania, Sisarma, Badgaon and ' imuch Mata by

the personnel of the Rajasthan State Government^Deaprtment of

Mines and Geology in 1968 (Fig.l). Inspite of their geological

as well as economic interest the deposit of the area have drawn

little attention of the earlier workers. The present investi­

gation may therefore be considered as the first serious attempt

to deal with the geo-chemistry of the Nirauch Mata Phosphorite

deposit of Udaipur district, Rajasthan.

Location and accessibility :

The phosphorite deposit of Nimuch Mata (24 37* N

lattitude and 73° 41'E longitude) is located at a distance of

about 4 km, north-west of Udaipur city and included within the

toposheet number 45 -. of the Survey of India. The area is

easily approachable by a metalled road,

01 iraate :

The c l i m a t e of t h e Udaipur r e g i o n i s s e m i a r i d w^ith an

average aiiaual r a i - a f e l l of 62S t o 7S0 HBR, con f ined between J a l y

« ^ Se4it:eBdoer, The msmlemmt t e s ^ i e r a t a r e d u r i n g fSDe-aiseEt ocaa psri'Oia^

'goes s?pt:o %9^C. The Oiooxal ^emp&xatwpe flwctusstiaa i s s^me-ttme

as high as 22°C. Temperature in the month of December and

January goes below 5 C,

Topography :

Physiographically, Rajasthan is divided into four

main regions viz*, (i) Western desert plain (ii) Aravalli mountain

range, (iii) xiastern plain (iv) Vindhyan plateau to the South-

iiast. The Aravalli mountain range of Rajasthan is considered

to be the oldest Precambrian mountain chain of India, made up

essentially of folded rock typical of geosyncline. The highest

north-western part is about 1500 meters above m.s.l. sloping

down gradually to the north-east end south-west axes of the two

Aravalli ranges. The phosphorite deposit of Nimuch Mata is

located on an isolated hillock which trends north-west - south­

east rising upto nearly 776 m above m.s.l.

Drainage and Vegetation ;-

The Nimucn Mata area is mainly drained by seasonal

streams and a small nala which flows in northern direction. The

vegetation is confined to the soil covered ground and includes

mostly, Thar (Suphoriba Nivalis),Babool (Acacia Arabica),Dhak

(Butegtron dosa) and Neem (Azadivacleete). Cultivation is

only confined to the low lying areas, mostly in the north and

north-eastern portions of Nimuch Mata,

Status of Nimuch Mata phosphorite :

The discovery of a unique stromatolitic Precambrian

Arawaili j^Msp^MTi-te tfe osili, ti»a w^ fixst wade in 19€T faf

t&et QeoLeigfijaal Smrvey ci€ Ii iia < Kakfctaaffch id Sant V,H*^tagT}

from Kanpur, Matoon, Kharwaria and Dakan Kotra areas of Udai-

pur district/ encouraged a widespread exploration for phospho­

rite in Rajasthan, This was followed by discovery of phospho­

rite deposits near Jhamar Kotra, Sisarma, Nimuch Mata and Bad-

gaon in Udaipur district by the State Directorate of Mines

and Geology, Government of Rajasthan.

The search for phosphorite deposits in the region

was based mainly on their typical litho-association of dark

shale, chert and carbonate rocks as well as the existence of

a geosyncline (continental shelf area)bordering the craton which

is considered to be the most favourable areas for phosphate

deposition.

The phosphatic horizon near Nimuch Mata is treceable

over a strike length of 700 m and it extends impersistently

5 to 6 km in the areas of Badgaon in the north and Sisarma in

the South. The thickness of phosphoritic horizon varies from

0.5 to 10 metres. The phosphatic material is mainly confined

to algal structure and occurs mainly as well defined stromato-

litic bodies in dolomitic limestone. The P20cConcentrations

vary from 5 to 10 percent and the reserve was estimated at

about 0.33 million tonnes by the Geological Survey of India,

Previous work ;

Hacket, C«A.(1881) was the f i r s t to propose the name

Aravai l i system t o the rocks composing the Arava l l i mountalu

r^Ege l a i a j a » t i » a , ffe pi^^are«J a geological m^ «jd c l a r i ­

f i e d t ^ naci® iaeloagijag t o t h e Arewalli system, eaq^osed armmi

Udaipur district, Rajasthan.

In the present century the systematic geological map­

ping in the parts of Rajasthan were carried out by Latouche,

T.H.D. (1902), Middlelemiss, C.S.(1922), Heron,A.M.(1935,1936

and 1953). The systematic studies carried out by Heron (1953)

indicates a four-fold classification of the Precambrian rocks

of Rajasthan on the basis of three prominent unconformities

viz: (i) Banded geneissic complex, comprising mainly of granite

and gneisses. (ii) Aravalli group of rocks, consisting mainly

of phyllites, schist, dolomite, marble and quartzite. (iii)Railos,

consisting mainly of schist and limestone, (iv) Delhi system,

comprising of quartzite, schist, limestone,etc.

In th3 recent year a large part of Rajasthan has been

mapped on 1:63,360/1:50,000 scale, and some of the mineralized

belts have been covered by large scale mapping, by the personnels

of the Geological Survey of India (Gupta, B.C. 1934, Poddar,B.C,

and Mathur, R.K, 1965, Raja Rao, C.S. at alvl97l).

Since the discovery of phosphorite deposits in Udaipur

district of Rajasthan, valuable contributions regarding phospho­

rite were made by Muktinath (1967), Muktinath and Sent,V.N.(1967)

Muktinath et al-, (1969), Roy, A.B. (1978), Banerjee, D.M. (1971),

Roy, A.B. et alv(1980) and Roy and Paliwal (1981), who gave the

summary of the work done on various phosphorite deposits of Udai­

pur district^ Rajasthan,

EeceiEtly the geology of tiie uaaifHir regiosn^iadiislve

(1971) and Roy et al., (1981).

Tte systematic studies regarding the stromatolites of va­

rious phosphorite deposits of Udaipur region have been carried out

by Muktinath and Sant (1967), Raja Rao, Iqbaluddin and Mathur(1968),

Chauhan, D.S.(1970,1973 and 1980),Banerjee (1971,1974),Verma,K.K.

and Barman,G,(1975), Barman et al.,(1978), Rao, L.A.K.,(1982)and

Rao, L.A.K. and Akhungi, R.A.(1983).

Petro-minerological studies of some of thj i^hosphorite,

deposits of Udaipur district were carried out by Chaudhari, R.et al.,

(1968), Chatterjee, P.K. and Mukherjee, D.S.(1971), Rao, N.K. and

Rao, G.V.U.(1971) and Banerjee, et al.,(1981). Mineralogical studies

of the Matoon and Kanpur phosphorite by Chaudhari, et al,,(1968) and

of Dakan Kotra by Rao, L./ ,K. and Rasul,^,H, (1985) indicate that

caroonate flourapatite and carbonate hydroxyl flourapatite are the

most common phosphate minerals.

Geochemical studies from some of the phosphorite deposits

of Udaipur region were carried out in the past by Banerjee, et al.,

(1981), Pandya, M. K. et al., (1981),Rao,(1982-1984),Rao and Rasul

(1984), Contribution regarding the genesis of various phosphorite

deposits of Udaipur district, Rajasthan, were published from time

to time by Pandya and Chauhan (1976), Banerjee/et al.,(1980),Verma

and Barman( 1975), Chauhan and Sisodia (1981) and Rao (1982).

PURPOSE OF THE WORK

Purpose;

The present investigation has been planned after revie­

wing carefully the previous work azid certain existing problems

Off -t.^ ^fyeis^ix33^i^se ct^tos^tv ia ti^- PSalsxsr jreglco of SaJ sstbaax,

An a^txnpt^s^s liee E »aae fegp td» iscesesrt aozt ear t:o st-wdj the

litho-stratigraphy, stromatolitic assemblings,petromineralogy

and geochemistry of the phosphorite deposits of Nimuch Mata.

The purpose of the present work is also to investigate in some

details of the mode of occurrence, mineralogy and geoQrhemistry

of the phosphorite deposit of the study area in order to throw

some light on tlie physico-chemical environmental conditions

under which the phosphorite of Nimuch Mata were formed.

METHODS AND PRESENTATION OF WORK

In order to achieve the required objectives the fo­

llowing scheme of investigations were carried out.

Field investigations :

The field investigations, interalia, included cons­

truction of a geological map of the Nimuch Mata area. The va­

rious types of phosphorite and stromatolitic form species were

recorded and representative samples of phosphorite as well as

other associated rocks were collected for petro-minerological

and geo-chemical studies.

LABORATORY INVESTIGATIONS

The laboratory investigation involves :

i. Microscopic Studies : About fifty thin sections of

representative phosphate rock samples and other asso­

ciated rock units were prepared and studied under the

petrological microscope*

^^^ Analytical Studies : Fourteen phosphorite samples

wear© sheeted ^smgL fcalysed cijea jcail - f ^ the ^ ^ j ^

t i ta^^ «iet »iaafcic», o€ maj«: cstiifes aad trm^

elements following the p rocedure outlined by Shapiro, L,

and Brannock, W.VJ. (1962).

Powdering of the Samples:

The rock samples were powedered to about 300 mesh size

in centrifugal ball mill in the geo-chemical laboratory of the

Geology Department and the solutions 'A* and 'B* were prepared

for the determination of major oxide as well as for the trace

elements.

Major Oxides :

Solution 'A* was used for the determination of SiO_

and Al^O-f about 0,1 gm of the sample and standards were decom­

posed with NaOH (16 pellets) for five minutes in a nickle cruci­

ble. Some water was added after the m^lt cooled down at room

temperature and allowed to stand overnight till the melt dis-

integrated completely. Contents of each cn-cible were trans­

ferred to one litre volumetric flask and solutions were acidi­

fied with 20 ml 1:1 HCl and made up the volume.

Solution VB* was used' for the determination of Fe^O^,

CeO, MgO, TiO^/MnO, Na20, and K-O, The powdered sample (0,5 gm)

was moistened in a platinum crucible with one or two drops of

concentrated H2SO- and 20 to 30 ml of Hydrochloric acid. The

crucible was kept with lid over a steara-bath. After one hour

the lid was removed and sample was allcswed to be dried completely.

The residue was transferred to a 400 ml beaker aad added water,

T,he laeafaegr was placai aa. a iasot plate and lieafced till the faaes

of SO^ were driven off completely. About 10 ml of HNO^ was

added and beaker was replaced on a hot plate. Each beaker was

allowed to be heated till strong fumes evolved and any colour

due to organic matter was removed by adding four drops of HCIO.-

HNO^ (1:1) mixture. Hydrazine sulphate (0.2 %) was used to remove

the brown precipitate of MnO„. Solutions were cooled to room tem­

perature and transferred to 250 ml volumetric flasks and diluted

to the volume.

Silica (SiO-) was determined by 5 ml of 'A' reagent

blank solution, 5 ml of each standard solution and 5 ml of each

sample solution, placed in a 100 ml volumetric flask. One ml of

amraoniiim raolybdate solution was added to the solution and it was

allowed to stand for about 10 minutes. Tartaric acid solution

(10 per cent ) four ml and one ml reducjing solution (0.7 gm of

sodiiom-sulphite in 10 ml of water 0,15 mg of 1- amino-2-nephthol-

4-sulphonic acid were mixed and dissolved (A) 9 gm of sodium-bi­

sulphite in 90 ml of water (B), then (B) was added to the solu­

tion (A) and mixed thoroughly. The content was diluted to

volume, raixed well, and allowed to stand for about 30 minutes.

The transmittance at 640 mu was determined and calculated to

SiO- percent.

Alumina was determined by measuring the transmittance

at 475 rnu about 15 ml of *A' reagent blank solution, 15 ml of

each standard solution and 15 ml of each sample solution were

placed ia a sreries of evaporating dishes. The content was eva-

iJacafcesd to drjaess osa a st£i:sm. hsttM and to €sacfa d,is±i.* 25 idL c^

solution 'A* reagent blank solution was added and heated for a

few minutes on a steam bath to dissolve the salts. The contents

were placed in a series of 100 ml volumetric flasks and 2 ml of

calcixim chloride solution, one ml of hydroxylamine hydrochloride •

solution (10 percent) and 2 ml of thio-glycolic acid (4 percent)

were added and allowed to stand for five minutes. 10 ml of buffer

solution (100 gm of sodium acetate in water 30 ml of glacial ace­

tic acid diluted with 500 ml of water) were added to each flask,

mixed and allowed to stand for about 10 minutes and 10 ml of

alizarin red S-solution (0,05 per cent) was added to each flask

and allowed to stand for about an hour. The percent transmit-

tance at 4 75 mu for each solution was determined using the blank

solution as reference.

Total iron was determined by 5 ml of standard iron

solution and 5 ml of each sample solution of 'B' in a series

of 100 ml volumetric flasks. An additional flask was used for

the preparation of reagent blank solution, 5 ml hydroxylamine

hydrochloride (10 percent) was added to each flask and allowed

to stand for 10 minutes. To each flask 10 ml of sodium citrate

of 1:10 phenonthroline solution (0,1 percent) end 10 ml of sodium

citrate (10 percent) were added and diluted to 100 ml with water.

ftfter an hour the percent transmittance at 560 mu was measured.

Titanium Oxides (TiOj) was determined by taking equal amounts

of solation 'B' and reagent (50 ml of 1:1 H^SO^ + 50 ml of phos­

phoric acid and 400 ml of hydrogen per oxide). The transmittance

was ffle:atsuxed: at 4fK) wti bel ew 26®C tjesaper sticpe*

Kasagparaease (BoO) svas itfeteradx i by pladaag 20 ml t^ St-emidsjoA soitt-

i:4cxB« W atl €)£ each. Siaqples soJt&ttxm *B* ±n a series of 1Q& col

10

beakers. Phosphoric acid 0,5 ml, sulphuric acid 25 ml (1:9)

and 2 grn of potassiiim periodate were taken in a beaker and heated

on sand bath till pink colour appeared. The content was cooled

down and made upto volume (100 ml). The transmittance was mea­

sured at 525 mu.

Potassium Oxide (KjO) and sodiTim oxide (Na^O) were determined

by using the flame photometer where lithium was used as an inter-

nal standard. v;ith the help of pipette 25 ml of solution 'B*

was placed to a beaker, 25 ml of water and 50 ml of internal

standard solution containing 200 ppm. of litiiium were added.

.iwOCk solution of Kcl and NaCl of 0.5 to 10 percent were prepared-

The recorded readings by ^lame photometer are proportional to the

concentration cZ ,:>t_ .ium in wtendard and sample solution. The

ccacencrdtion of pot-- ;iium as K_0 was caa.v- ' ^*-^d. Na.n was deter-

'lalo*© in the same way as that for KJ!),

Calcium (CaO) was determined volumetrically in which

SMA solution was used. 25 rol of sample solution 'B', 25 ml of

Standard solution and 25 ml of blank solution were placed in a

series of conical fla-ks,. Hydrochloric acid (1:1) 25 ml, Trie-

thanolamine (1;1) 5 ml, 2/3 drops of polyvinyl alchohol (one

percent) and screen-d indicator, 20 to 50 mg, were added and dil­

uted to approximately 200 ral, 5 ml KOi: ( 30 percent) was added

to the content and titrated with the EDTA solution (0.01 N) with

constant stirring till the colour changed from greenish blue to

imrple. The CaO percent was calculated i^ using formula

1 CaE»-= - V:. X. s/ii ^ 3^22m

11

where,

a « mg of CaO equivalent to 1 ml of JiDTA

V^= £DTA used in titrating 25 ml of solution 'B'

w = Weight of sample (gm) 25 ml of solution 'B'

Magnesium (MgO) was also determined volumetrically by the solu­

tion 'B',10 ml of sample solutions 'B' were placed in a series of

conical flasks and 20 ml of ammonium chloride containing methyl

red (15 percent) soluti on was a dded and nutralised with ammonium

hydroxide till the pink solution turned yellow. The content was

diluted to 25 ml and allowed to stand for about 15 minutes, fil­

tered tne precipitated and in the 25 ml filtrate, first 100 ml of

water and then 10 ml of buffer solution (66 gm of ammonivim chlo­

ride in one litre of (1:1) ammonium hydroxide) were added. Using

eriochrome black-T indicator titrated against EDTA till it turned

greenish blue. MgO percent was calculated by using the formula.

MgO % = ( 25 V2 -v.) X 0.4032

V, = Volume of EDTA for CaO+MgO

V. = Volume EDTA for CaO.

Phosphorous-pentoxide (^2^5^ ^^^ determined vo lumet r ica l ly . 0.5 gm

of sample powder was taken in a 25 0 ml of volumetric f lask and

HNO was added, bo i led , f i l t e r e d and d i lu ted t o the mark, when

ammonium molybdate so lu t ion was added t o the 50 ml so lu t ion , a

yellow p r e c i p i t a t e of phospho-ammonium molybdate was formed. The

p r e c i p i t a t e was f i l t e r e d aad washed with cold water and t i t r a t e d

agaixist M/10 Hi^H using ptoenolphthaline soluticaa. The exact voluaae

o£ HaOH consuraed was i ad l ca t ad isgr pA«* coLtjor of t m so lu t ion ^diicb

12

Ferrous iron (FeO) was determined volumetrically in

wnich standard dichronie solution with diphenlamine sulphonic acid

was used as indicator. 0.5 gm of sample was placed in a platinum

crucible and 10 ml of H2SO,(1:3) and 5 ml of HF were added and

the solution was heated for about 10 minutes on a sand bath. The

content of crucible was then transferred in a one litre beaker

containing about 10 gm of boric acid, 20 ml of H2SO. (1:3), 15 ml

of indicator and 5 ml of spike solution. The content was thoro­

ughly mixed and titrated against potassium aichromate (2.728 gm

K-Cr^O^) in two litres of water till the solution turned to pur­

ple colour,

Carbondioxide (CO2) was determined volumetrically. In a series

of 250 ml beaker, 0.5 gm of calcium carbonate £S standard and

0.5 gm of the powdered sample were placed, 25 ml of hydrochloric

acid ( 0.5 N ) was added to each beaker and allowed to remain

over night. The remaining acid in the beaker was titrated with

sodium hydroxide ( 0.35 N ) and bromophenol blue was used as an

indicator, which gave yellow to blue end point. The calculation

of CO2 in percent was made es given below :

1. Calculated the acid alkali ratio

25

Volume of NaOH for blank

2. Multiplied each of NaOH titration values by the acid-

alkali ratio,

3 . Substracrted each f igure obtained in s tep 2 from 25 HCl,

This gave HCl i n m l l l i - l i t r j ^ s constamed by carbonate*

13

4, A factor v/as obtained on the basis of titration of

the standard CaCO-.

5. Multiplied each sample value for HCl consumecl as

obtained in step (3) by the factor to obtain CO-

in percentage.

Analysis for the determination of trace elements were

carried out a G.B.C, model No. 902 Atomic Absorption Spectropho­

tometer, The trace elements viz. Cu,Ni, Co, Cr, Pb, Zn, Rb and

Cd were quantitatively determined and the wavelength used for

individual element is given below;

j::L£Mi::NTS VVAVE Li^NGTM (nm)

Cu 324.7

Ni 232.0

Co 24 0.7

Cd 228.8

Cr 357.9

Pb 283.3

Zn 213.9

Rb 780.0

After the chemical analysis, the data were fed by

VAX - 11, 780, computer for calculation of the correlation

co-efficient between major and trace elements and the element

ratio of petrogenetic significance.

]-1

A C K N O W L E D G E M E N T

I wish to express my profound gratitude to my supervisor Dr. Liaqat A.K. Rao, Lecturer, Department of Geology, Aligarh Muslim University, Aligarh, for his excellent guidance, constant support and trust throughout the course of this study.

I am highly thankful to Prof. S.M. Casshyap, Chairman, Department of Geology, A.M.U., Aligarh, for his persistent interest and providing me research facilities.

I am grateful to Drs. S. Ahmad Ali, Shadab Khursheed, Mohd. Ajmal, A. Wahid Israili and Ajaz Ansari for their valuable suggestion and encouragement at all levels.

A token of deep appreciation to all my friends for their inspiring assistance and offered time are, Messers. M. Rehan Azmi, Mazher Abbas, M.J.A. Siddiqui, Zafer Kaleem, Amirul Hasan, Suhail Ahmad, Sajid Raza and Miss T.N. Kazmi.

My everlasting thanks to my closest friend cum brother •Muinuddin, for his caring companionship, constant, unfailing source of encouragement, help and inspiration throughout the completion of this dissertation.

Unqualified praise is due to my brother Muzahir Hussain for his constant persuation to continue my higher studies.

I am also thankful to Mr. Firoz Javed for his valuable assistance in the analytical work and Mr. Zakir Husain for provi­ding books and literatures.

Thanks are due to Mr. Shafqat Ali for typing this manuscript and Mr. Saleemuddin Ahmad for excellent cartographic work.

The whole story will remain incomplete if I donot express the indebtedness to my parents, who, as I believe will be the happiest souls on this earth to see my work completed. I know their affection, love, guidance and patience can never be paid back by mere thanks.

LE NABI

GEOlO^iCAL HAP Smmm^ THE PHOSPHATE QCCUREHCES A

ARomm mmtp\m B^imci, UAJASXHAHinmy^

(7*J: 'JHAMAR KOTRA " ^ ^L\7', K>f\'J' 1.6 0 1.6 3.2 KmV

I I I i { BASED ON HERON, 1953)

IVg^ POST ARAVALLI GRANITE AND COMPOSITE GNEISS

~ I 1 PHYLLITES AND GRAYWACKE

CARBONACEOUS PHYLLITE

^ ^ DOLOMITIC LIMESTONE

ID ORTHOOUARTZITF

[ f - I ARKOSE AND CONGLOMERATE

' - ( ^ 3 PflOSPMORlTE OCCURENCE f ^ ^ BANDED GNEISSIC COMPLEX

FIG. 2

C H A P T E R - II

STRATIGRAPIiY AND GEOLOGICAL SiiT UP

The Aravalli Mountain Range, whicn fringes the north­

western margin of the Peninsular Indian Shield, runs for more

than 700 Km from Delhi in the north to north of Ahmedabad in

the south. It is helieved to be one of the most ancient moun­

tain ranges in the world. The major part of the mountain range

falls in the State of Rajasthan and it continues in the States

of Haryana and Delhi in the north and Gujarat and Madhya Pra­

desh in the south and south-east respectively. The chief geo­

logical features encompassing the foundation of this great moun­

tain include several unconformities separating several metasedi-

mentary and meta-voloanic units laid successively over an ancient

basement of plutonic rocks end para-gneisses.

The term Aravalli System was first introduced by Hacket

(1881) to designate a group of low grade metamorphic rocks occu­

rring in parts of Rajasthan. The Aravalli System is composed

mainly of quartzite, phyllites, greywakes, slate,impure lime­

stone, mica-schist and composite gneisses. These rocks are well

exposed around Udaipur and parts of Chittorgarh district,

Rajasthan.

Heron (1935,1953) recognised the Aravalli System as

the oldest precembrian formation overlying the Banded Gneissic

Complex and the Bundelkhand Gneiss (renamed by Pascoe,i:.S,1950 as

t±3^ Beracb Gtaaiii^), BdractLUSSil} n^^ped tte formeticais e3E±Easl.\feiy

tA

16

in Rajasthan and suggested a four-fold classification of the

precambrian rock formations of Rajasthan. These rock for­

mations are separated by the three prominent erosional un­

conformities. The general stratigraphic framework of the

rocks forming the Aravalli mountain range,following Heron

(1953), is given in the following table - I

T A B L E -

Delhi System

Ajabgarh Series

Alwar series

Railo series

Upper phyllites

Limestones.

Biotitic limestones and

calc-gneisses,

Calc-schist.

Phyllites,biotite-schists

and composite gneisses.

Quartzites.

Arkose grits and conglome­

rates.

Garnetiferous biotite-

schist.

limestone(marble).

Local basal grit.

Aplo-granite,epidiorite

and harnblende-schists,

ultrabasics.

Aravalli System

Banded Gneissic Complex.

17

Impure limestones, quartzites,

phyllites, biotite-schists,

composite gneiss.

Quartzites, grits and

local soda-syenites.

Conglomerates.

Local amygdalolds and tuffs.

Pegmatites, granites,

aplites and basic rocks.

Schists, gneisses and compo­

site gneiss.

Quartzites.

Mathur (1964) mapped the area of about 200 sq Km aroiind

Udaipur between 24° 30' and 24° 45' N latitude 73° 30'

and 73 37' E longitude. Table II represents the genera­

lized sequence of the Aravalli rocks along Debari - Udaipur

road,

T A B L E - II

Post Aravalli

Aravali Super Group

Quartz vein, amphibolites

(intrusive granite and migma-

tlte into the Aravalli).

Phyllites, conglomerate, arkose

and reddish phyllites.

Phyllites, slate, carbonaceous

pfajfliit s witii iiitereal afcory

18

Aravalli Super Group

r" bodies of dolomite and quartzite,

Basic volcanics with inter-stra­

tified qucirtzite, greywakes

and phyllites.

Ortho-quartzite, quartz pebble,

conglomerate and qu jrtz grit.

Greywackes and phyllites with

intercalatory bodies of dolo­

mite and interformational

conglomerates.

Phyllites with intercalatory

bodies of carbonaceous phylli­

tes, dolomite,calcareous quar­

tzite and quartzite.

Red to buff Orthoquartzite with

intercalatory phyllites.

Coarse grained to pebbly arkose

sub-arkose and felspathic quart­

zite,

Arkosic qiiartz, pebble conglome­

rate. Green-schist with inter-

stratified Orthoquartzite and

dolomite.

Buff Orthoquartzite.

Pebbly talc quartz rock and talc

l_ schist*

_^Batoslcmal ancagi forgi ty

19

Banded Gneissic Complex

Chlorite and biotite-schist,

amphibolite schist,composite

gneisses, aplite, pegmatite

and quartz vein,

Banerjee (1971) classified the Precambrian rocks of

Udaipur area into Udaipur Formation, Matoon Formation and

Debari Formation (Table III). In his classification, the

phosphorite bearing horizons are confined to the Matoon For­

mation, whereas rocks of the Debari and the Udaipur Formations

are devoid of any phosphorite horizon.

UDAIPUR FORMATION

MATOON FORMATION

T A B L E - III

Lithic quartzite, flaggy qusrtzite and current-

bedded ortho-quartzite.

Sandy phyllite, calcareous phyllite,biotite-

schist and carbonaceous phyllite.

Ortho-qurrtzite, brecciated calcareous quart­

zite, marble and carbonaceous phyllite.

Impure marble, dolomitic limestone with rolled

and rewashed fragmental phosphorite with bio-

hermal phosphorite,

Sandy phyllites and schists.

Ortho-quertzite, brecciated quertzite, dolomite

marble, rolled fragmental phosphorite and bio-

hermal phosphorite,

Isi^woe raaxi^e^ caart sBactaaBS p^llit.e vJLizh .small

20

DEBARI FORMATION

BANDi:;D GNEISSIC COMPLEX

specks of garnet and manganiferous dolomite

intruded by post Aravalli (?) aplogranite.

Buff to reddish brown ortho-quartzite with inter­

calated phyllites and chlorite-schist, meta-

conglo merate and petromictic arkose.

Meta-arkose,

Meta-conglomerate and felspathic quprtzite.

Local shear Fault

Gneisses, granite, mica-schist,marble,dolomite

and quartzite.

In the vicinity of Udeipur, the Aravalli rocks, dis­

tributed along two parallel belts, exhibit distinctly different

facies sequences that reflect near-shore and deep sea environ­

ment respectively (Roy and Paliwal 1981), The stratigraphic

succession of the phosphorite bearing shelf de_osit is given

in table IV following Roy and Paliwal (1981).

21

•y A B L £ - IV

O ai o QJ Cd CU

to

H

i j

< 5

D4

O

o

W

FORMATlON-C Conglomerate, arkose and qua r t z i t e .

Greywacke and p h y l l i t e s .

o oi o H

3 %

Lul

FORMATION-B

FORMATION-A

Carbonaceous slate, phyllites,Dolo-

stone, ferrugenous quartzite and

phosphorite quartzite.

Minor conglcanerate, quartzite,

carbonate mixite.

Quartzite, minor conglomerates

with green schist and pockets of

white mica-schist.

Unc onf Qrmity_

BASEMENT ROCK: Granites, gneisses, araphibolites, mica-

sciiist and roeta-sediments.

22

Attempts have been made from time to time to classify

and correlate the phosphorite horizons of India. Muktinath

(1974) classified the major phosphorite deposits which are asso­

ciated with the Precambrian, Palaeozoic, Jurassic, Cretaceous

and Tertiary terrain of Rajasthan, Uttar Pradesh, Madhya Pradesh,

Gujarat, Tamil Nadu, Assam, Jammu & Kasl-imir and Himachal Pradesh.

Many valuable contributions regarding the various phosphorite

deposits of India have been made in the past such as I'-iuktinath

(1967) and Sant (1967,1969), Banerjee (1971 a,b,c, 1981), Baner-

jee and Sahgal, N. (1987,1988), Basu, P.C. et al.,(l981). Cha­

tter jee and Mukherjee (1971), Chauhan (1970,1973,1979),Choudhari

and Balasubramaniam (1980), Choudhari and Roy (1986), Patwardhan,

A.M. (1973,1975), Pandya, M.K., Srivastfva, S.B.L. and Dwivedi,

C.S. (1984), Rao and Rao (1971) ' V , . Val-

dio, K.S, (1969 a,b) and Verme and Berman (1975).

SEQUENCE AND LITHOLOGY OF ROCK TYPES AROUND NIMUCH MATA :

According to the vievs expressed by some earlier wor­

kers viz. Fodder and Mathur (1965) , Damle and Sharma ( 1970 ),

Banerjee (1971) and Roy and Paliwal (1981), the older dolomitic

limestone on the east of Udsipur city, occuring more or less

close to the basal sequence of the Aravallis, encloses the

Jhamarkotra, Matoon, Kanpur, Kharwaria and Dakan Kotra

phosphorite deposits, while on the west of Udai^>ur city, the

younger dolomitic limestone comprises Sisarraa, Nimuch Mat.?., and

Badgaon phosphorite deposits ( Pig, 2). The phosphorite deposits

23

of Nimuch Mata, that occur in close proximity to the algal

stromatolites, form a thick succession of rocks belonging to

the Matoon Formation of the Aravelli Super Group.

The rock units, encountered from the east to the west

of the study area, include Lower phyllitea. slate, greywake,

phyllites, Wpper dolomitic limestone with phosphorite horizon,

orthcQquartzite and Upper phyllites.

The general strike trend of all the rock units is

north-west to south-east and dip moderately towards the west

or south-west. The following stratigraphic sequence in Nimuch-

Mata (Table V) has been established by the author on the basis

by his field observations and mapping :

POST-ARAVALLI

ARAVALLI SUPER GROUP

T A B L £ - V

Quartz vein and Granite (Intrusives)

Upper Phyllites

Upper dolomitic limestone with

Phosphorite horizon.

Orthoquartzite.

Lower phyllites, slate,

Greywacke,phyllites,

Phyllites i-

The upper and lower p h y l l i t e s are s t e e l grey t o gree-

nish black in colour, and a re exposed in the north-west and

eastern pa r t s of Niimich Mata, The p h y l l i t e s are c h l o r i t i c

24

and carbonaceous. Tlrie minute flaky minerals, constituted of

biotite, muscovit^' and chlorite. Quartz occurs in angular to

subangular shape and its size is fine to medium grained. Rock

cleavages are well-developed and at places bedding planes are

defined by compositional colour contrasts. Phyllites are mainly

confined to the low-lying areas in the form of small isolated

outliers,

Dolomitic limestone :

Dolomitic limestone is light bluish-grey in colour

and essentially composed of calcite, dolomite, and fewer sub-

rounded grains of quartz with minor amounts of ferruginous

matter. Phosphorite occurswithin the dolomitic limestone /

marble in association of algal stromatolites, Dolomitic lime­

stone which is massive and fine-grained, exhibits varying deg­

rees of crystallization and is exposed mainly in the northern

part of the study area. Thj rock is generally silicified and

sometimes appear ferrnaginous. At places, the carbonates are

re .laced by chert.

Orthoquartzite :

The orthoquartzite which appear dirty white to buff

and brownish yellow in colour, is exposed in the northern part

of the area. It is essentially composed of quartz with minor

and variable amounts of calcite, dolomite, feldspar and ferru­

ginous matter. The qufirtzite is hard, roas-sive and medium-grained

in size.

25

Post Aravalll Intrusive granite and vein yiartz :

The Post-Aravalli intrusive granite and vein quartz

could be seen in the north and north-western portions of the

area. The post-Aravalli grani:;e has been intruded mainly into

the dolomitic limestone with occasional intrusion of the vein

quartz. In the ortho-quartzite, the intrusion of vein quartz

more common particularly, in the northern part of the area.

Structure :

The Precambrian rocks belonging to the Aravalli Super

Group show a high degree of structural complexity comparable in

scale and complexity with the most strongly deformed erogenic

belts of the world. Atleast there are four distinct phases of

erogenic deformations that have affected the rocks of the Udai-

pur region and they are designated as AF-, 2 ' ^3 ^^^ ^ 4 •'•"

chronological order producing folds and a host of other asso-ROY »'^i

c i a t e d s t r u c t u r e . ( P a l i w a l , 1981 ) .

The d i f f e r e n t s t r u c t u r a l e l e m e n t s i n t h e Nimuch Mata

a r e a of Uda ipur d i s t r i c t have b e e n i d e n t i f i e d and d e s c r i b e d b e l o w .

NON-.TgCTONIC STRUCTURES

Bedd ing P l a n e ( S . ) : The p r i m a r y b e d d i n g p l a n e s a r e

p r o m i n e n t l y d i s p l a y e d t h r o u g h c o l o u r o r c o m p o s i t i o n a l c o n t r a s t s

i n q u a r t z i t e . The d o l o m i t i c l i m e s t o n e i s a l s o t h i c k l y bedded

w i t h a l i t t l e f o i i a t i c m d e v e l o p e d p a r a l l e l t o t h e b e d d i n g p l a n e .

The gfecteral s t r i k e t r e n d of t h e bed i n t h e a r e a of i n -

t e t r e s t i s S - S ±20 m^-Sxl w i t h i^Taal d i p a f 4 5 ^ t o 5S® towasEst

oar 5Qeat:iiF'Mest«

26

Axial plane foliation :-

The axial plane foliation (S2) is we11-developed in

the phyllitcs and quartzitic rocks, where it is marked by the

parallel arrangement of flaky minerals like chlorite, bioiite,

etc.

TECTONIC STRUCTURES

Joints :- Joints are well-developed in dolomitic limestone

and quartzite. Three different sets of joints viz,. Strike,

dip and oblique joints have been identified.

Folds :- The mesoscopic folds can be seen at most of the places

around Nimuch Mata area. The fold axes strike 10° to 12° NNE-

SSW with their plunges in different directions.

Faults :- Some minor faults have affected the Nimuch Mata

phosphorite and they are visibly marked by silicification.

C H A P T I : : R . - Ill

NATURE AND MODE OF OCCURRENCE OF I'HOSPHORITE

The phosphorite deposits of Nimuch i\ata occur exclusively

associated with the stromatolites. The nature and mode of occur­

rence of phosphorite in this region is mainly governed by the

morphological variations, shown by the stromatolites/ which have

gone under erosional processes and subsequent deformation of the

biostroraal/biohermal deposits.

NATURE OF PHOSPHORITE

Out of six distinct types of stromatolitic phosi)horites

(Banerjee,1971, Chauhan, 1979, Rao 1982 ) viz., (a) Laminated

stromatolitic phosphorite (b) Silicified fragmental phosphorite

(c) Columnar stromatolitic phosphorite (d) Massively bedded phos­

phorite (e) Nodular phosphorite (f) Pelletal Phosphorite, only the

colximnar and laminated/stratiform stromatolitic phosphorite were

identified and recognised in the study area. A brief description

of these phosphorites is given below :

Columnar stromatolitic phosphorite :

The columnarstromatol itic phosphorites are typically bluish-

grey in colour and occur as ill-defined tabular unbranched columns

with the convex laminae upward in the dolomitic ground mass and

show concentration of Pp^B ''•'•y ^^ ^^^ algal columns. Phosphorites

associated with the coluirmar algal structures are very common in

the north - western part of Nimuch Mata <P1 -1 Fig.- 1 ) . The inter-

coirairoer spaces of tias pfeospftiafce bearii^ stxacEatalltie consJjst asariaiy

27

28

Of clastogenic materials. The columnar algal stromatolites vary

in height ranging between 8 and 4 0 cm., and their basal diamaters,

1,5 to 8 cm. The algal structure occurs more or less at right

angles to the bedding plane of dolomitic limestone,

Laminated/Stratiform stromatolitic phosphorite ;

The laminar stromatolitic phosphorites occur in the

north-eatern ^ art of the Nimuch Mata area. The thickness of

individual lamina varies from 1 nun to 1 cm. These laminated

stromatolites are essentially composed of alternate laminae of

dark grey phosphatic material and whitish to greyish and fine

to medium grained carbonate materials with some silt size quartz,

and show conformabl- relationship with the hostrock. The indi­

vidual phosphate as well as carbonate lamina varies considerably

both in thickness as well as in outline.(PI -I,Fig,2).

Mode_cfoccurrence of Phosphorite deposit :

The phosphorite horizon, which is traceable over a

strike length of about 700 metres, extends impersistently 5 to

6 km, in the adjacent areas of Badgaon on the north and Sisarma

on the south. Its thickness varies from 0.5 to 10 ra and the

horizon pinches and swells along the stike of the band. The

P Oc concentration is entirely dependent on the composition and

density of stromatolite population. The richest portion (nor­

thern and central parts) is confined to the thickly populated

stromatolites. It is ccmposed of laminated phosphorites which

became columnar stroraatalitic towards the north-western portion

of the area. The •arafeBraacfetag tjgae of algae Is- -s sry camixm^

C H A P T E R - I V

S T R O M A T O L I T E S

General Statement :

The stromatolites, being biogenic and soft sedimen­

tary carbonate structures, are produced by the lime secreting

and carbonate precipitating activities of some unicellular alga

like cvanophycae (blue-green algae), chlorophycean (green algae)

and Rhodophycea (red algae). The stromatolites occur in rocks

of nearly all ages extending from Precambrian to Recent. They

are one of the important evidence of ancient life and are also

found growing today. But they are more predominant in the rocks

older than Ordovician, particularly in the upper Precambrian.

Ancient stromatolites are rvjgarded as the close precursor to

the modern algae forms. They have been successively used as

stratigraphic marker beds for the regional and local correlation

in the Urals and Siberia (USSR), USA, Canada and in the lesser

Himalyas and the Vindhyan Formations of India,

Occurrence and characteristic :

The various stromatolitic form species from the Pre­

cambrian Arevalli meta-sediments of Rajasthan were identified

and recognised by Banerjee ( 1971 b ), Chauhan ( 1973,1979 ) ,

Barman et al,, (1978), The present study deals mainly with the

identification and classification of various stromatolitic form

species of the Nimuch Mata area of Udaipur district, Rajesthan,

The strcsnatolitic form species identified and recognisad from

tiae axes of iaafcerest eLoseiy a essBtfiLe those c^ Cf^llf^j^

Cc^gaarxs, (Fei^an & F^atop?. Hijaj-aria calceolata. (Korolyixk).

30

Collenia balcallca ( Maslov ) and the compound structures were

designated as SK - LLH and LLH - SH (Logan,B.W, et al.,1964).

^ brief description of these stromatolitic form species identi­

fied is given below :

Collenia columnaris : (Fenton and Penton)

This form species resembles those described by Fenton

and Fenton (1937) and Valdiya, K.S. (1969). It occurs as un-

branched discrete vertical columnar structure which normally

grows perpendicular to the bedding plane, T le individual lamina

is dome-shaped, closely spaced and broadened towards the top.

The columns are generally ellipsoidal in cross section and ra­

rely rounded. Thickness of the individual lamina varies from

3 to 4 cm. The colvunn ranges from 10 to 30 cm. in height and

1 to 5 cm, in diameter (PI - II, Fig.l), Collenia columnaris is

a silicious and non-phosphatic form and confined mainly to the

eastern portion of the area,

Minjaria calceolata : (Korolyuk)

The colonies of Minjaria calceolata species appear

sub-cylindrical and often coliimnar and resemble KorolyuJ^'s (1960)

form species. The columns appear vertical or tilted. The la­

teral margins are generally smooth. The height of the alga co­

lumns varies from 5 to 30 cm, and the width ranges from 2 to

5 cm. The form species contains, collophene and dahllite as

phosphatic minerals in very fine micro-lamination while the

clastic carbonate and deterltal gucxtz occur as its bindiiag

flKEtaeri^is C PI - H , F±4§»2}*

31

Collenia baicalica : (Maslov)

This form species is characterized by dichotomous

branching columns and resemble those described by Maslov(1937)

and Krylov(1960). The branches grow at its base and rapidly

expand upwards, forming a club-shaped structure. This form is

round to oval-shaped in cross section. The thickness of indi-

vidual lamina varies from 1 to 3 mm. The height of the column

varies from 6 to 20 cm. and its diameter, from 2 to 7 cm.

(Pl-11, Fig.3).

Compound stromatolitic structure :

The compound stromatolitic stiructures in the Nimuch

Mata phosphorite deposit are quite frequent. In these structure

two or more discrete columns may be linked by an inter-connec­

ting bridge or a stratiform structure may differentiate upward

into discrete colximn. They can be easily compared with those

described by Logan et al., (1964) and designated as SH - LLH -

SH - LLH - SH ( S H = vertically stalked hemispheroid),(LLH=

Laterally linked hemispheroid). The phosphatic laminae appear

as unerv^ and discorinected bodies and more or less alternate

with the carbonate laminae ( Pl-II, Fig.4 ).

32

D I S C U S S I O N

The present study of stromatolite from Nimuch Mata

area reveals the presence of Collenia columnarls^ Collenia

baicalica/ Minjaria calceolata and compound forms of stromato­

lites. These stromatolitic form species are phosphatic in

nature except collenia columnaris. Phosphate minerals usually

occur as sheaths around the columnar structure and within the

frame work of their uneven laminae.

The variation in the morphology of the stromatolites

and the nature of the associated material suggest considerable

variation in the hydrodynamic conditions in the Nimuch Mata

basin. The frequent occurrence of compound form indicate tur­

bulent water conditions, characteristics of an intertidal en­

vironment (Logan 1961, Logan et al., 1964). The phosphatic

intraclasts occupying the inter-columnar spaces of stromato­

lites seem to have been derived from the strong tidal wave

action. On the eastern flank of Fatehsagar lake in the vicinity

of the Nimuch Mata deposit, mud cracks, ripple marks (Pl-III,

Fig. 1 £t 2 ) and cross ripple laminations support the existence

of a supertidal to inter-tidal environment in the Nimuch Mata

area.

It seems possible that tidal current had influenced

most of the shapes of the stromatolites of Nimuch Mat« area.

The columnar structures must have been developed in the inter­

tidal areas as indicated by the inconsistency in the morphology

of st:ra«atoiltes^ irfaeiae tiiial current were powerxul mxcmg^ to

33

prevent spreading of the algal mat(laminated algal stromato­

lites). Only small isolated laminated algal stromatolitic

phosphorite suggest the shallow sub-tidal environmental

conditions.

C H A P T E R

P E T R O M I N E R A L O G Y

About one hundred and twenty samples were collected

from the phosphorite deposit of Nimuch Mata area in order to

study the phosphate and other associated minerals and rocks

under petrological microscope. It has been observed that the

phosphate minerals occur in almost all the samples in varia­

ble amounts and are associated with gangue minerals viz :

quartz, calcite, dolomite, sericite, feldspar, chert and some

opagues as well as pyrites.

Phosphorite :

Phosphorite usually contains more than one apatite

minerals like pedolite, dahllites, francolite, stoffelite,

kurskite,gradnolite, welkite, ellestadite and mornite. Such

mineralogical variations are very common, hence it is conven­

ient to use cellophane as a generic term for the phosphate

minerals,

A brief description of the minerals identified and

recognised in the studied phosphorites is given below,

Collop'nane :

Cellophane, a c ryp toc rys t a l l i ne mineraloid having

composition 3Ca3(PO^)^ Ca(C03 F20)H20 i s the dominant phos­

phate mineral i den t i f i ed and recognised In the phosphori te

depos i t of Nimuch Mata. Collophaiie^that occurs as f ine a»d

irregpaaLaar ^racKles* oaaesstjed lay calcariagias aad c&arfcy laateactal

34

35

varies in colour from light grey to grey, and yellow brown to

brown ( Pl-IV,Fig.l ). The average size of phosphatic granu­

les ranges from 0.02 to 0.05 mm. Collophane chiefly occurs in

the form of random grains arranged in linear bands, disconti­

nuous clusters and as dissiminated individuals (Pl-IV,Fig.2).

Quartz :

Quartz is the most dominant gangue mineral in the

phosphorite. The grain diameter ranges in size from 0.22 to

2.16 mm ( PI - IV, Fig.3 ) and show oblique to slightly undu-

lose extinction. Quartz occurs mainly in association with co­

llophane, mostly as tiny inclusion in collophane that can be

measured on micron scale ( PI - IV, Fig.4 ) and also as coarse

grained crystallized quartz forming the matrix of phosphate

mineral.

Calcite 'and Dolomite i

Calcite and dolomite are the chief gangue minerals

of stromatolitic phosphorite. In general, calcite is colour­

less having three sets of cleavages, rhombohedral in shape

and vary in size from 0.25 to 1.25 mm. Coarse-grained calcite

that occurs as groundmass, exhibits well developed cleavages

( PI - V, Fig. 1 ) whereas fine to medium grained calcite found

in the intercolumnar spaces of stromatolite occurs as a cemen­

ting material. Dolomite also exhibits almost the same optical

properties vary in size frcro 0,30 to 1.69 mm and mainly occurs

as ground mass ( PI - v. Pig.2 )•

36

Accessory minerals ;

The accessory minerals identified in the phosphorites

of the study area are constituted mainly of carbonate minerals

together with minor amounts of mica, sericite and chert. Chert

is fine grained, crypto-crystalline and colourless to faintly

brownish in colour.

The other minerals identified include, feldspar, mus-

covite and sericite, that usually occur as shapeless plates and

elongated laths ( PI - V, Fig. 3 & 4 ). Sericite and muscovite

are generally colourless to yellowish wriite in colour. Secon­

dary limonite and limonitised pyrite occur sporadically.

Dolmitic limestone :

The rock is medi\im to fine grained. The major mine­

ral assemblage in these rocks are mainly dolomite and calcite

and quartz with ferruginous coatings, Calcite grains' are gene­

rally colourless to greyish in colour v;ith two sets of cleava­

ges ( PI - V, Fig. 2 ). The arrancement of calcite grains gives

the appearance of mosaic dolomite, occurs mainly as fine grained

matrix, quartz occurs in several forms. Many rocks s-mples

show rounded clastic grains of quartz. Sometimes euhedral crys­

tals of quartz partially replace calcite and dolomite. There

are also veins of quartz associated with ferruginous chert

( PI - VI, Fig, I ),

Uuartzite ;

The <3uar-trl±» i s malaily Qampxased of guart2: vi±th m i a a r

dmxMUTks a£ crartJOBaEfces,, 'Sae c^aeait ing laaEberrial i s a -sery f l o e

g r a i n e d q u a r t z w i t h scrae iroai oacldes and c l^ j r t < PI - VI , P i g , 2 ) ,

37

Quartz generally occurs as monocrystalline grain and shows clear

appearance except a few with dustyincluslon. Some strained

quartz occurs in the form of polycrystalline grains with sutured

boundaries (PI - VI, Fig, 3 ), Quartz often has inclusion of

minerals like apatite, tourmaline, etc.

C H A P T E R - VI

GdOCHjfiMISTRY AND DISTRIBUTION OF MAJOR OXIDES

General Statement :

Fourteen phosphorite samples from Nimuch Mata deposit

were analysed chemically for the quantitative determination of

the major oxides viz., Al-O,* ^^^2* F^-O-zFeO, MnO, MgO, CaO,

PjOc/ Na-O, K 0, CO, and H^O " by weight percent. The analy­

tical results are presented in table ( VI ) and discussed on

the following lines :

1) Abundance and distribution trends of each major oxides

in the phosphate rocks,

2) Uuantitative variation tends of the significant oxides

in the phosphorite and their mutual relationships.

The statistical treatment of geochemical data of Nimuch

Mata phosphorite has been carried out in order to determine their

ranges of variation and frequency percent distribution. The

frequency distribution of major oxides in the phosphorite is

given in Fig. 3.

Distribution of Major Oxides :

The distribution (wt % ) , variation range and mean

(Wt %) of the various major oxides, in the phosphorites are

stimmarised and given in table-VI and discussed as follows :

Alinnina (Al^0_) :

The qumxt±tB:t±^^ -^rarijatdaoB. txeaicljs G£ -^Jii- isx Mimach.

Mata pi ios^K«: l t« l i e iba Isetweeaa 0*39 aaad 3.55 perosBEt wdtii am

a v e r a g e c o n c e n t r a t i o n of 1»82 j ^ r c e n t . The f requency i^rcaaat

?e

- B

39

[fiJ :fi 1*^1 ' « ' ' • i 1 I, i i - i ,i I i-l..i iteLjail I I i i I 1 1 1 I .1

IJ - AljOj V.

0 SiOj V.

^ g 1 1 I i-.-iu^

f«ov.

F.jOjV.

. F

ITI

•LJ}^ ' • ' ' ' '

IJS L*l..i-j, i i..i.i :i„i..,i,.i 1..I i , i - x , i 1 1 ,1-t •

MgOV.

t f ' ' ' ' * ^ ' ' '

M

..n n

[{•L fflfl

b o o o o o M20 V.

si

EEUOfl,[l O *n o i* O t^ 0 0 —^"^"^ rr»J'«>r.»«»2 ~ C 2 i ; S 2 2

FIG 3 HISTOGRAMS SH0W1M6 FREQUENCY ( PERCENU DISTRIBUTION OF MEJOR OXIDES M WMUCH MATA P H C £ P W » H

40

distribution exhibits bimodal nature of AI2O2 (Fig. 3-A) in

the phosphorite.

Silica (SiO^) :

The quantitative variation trends of silica in Nimuch

Mata phosphorite vary from 34.73 to 50.13 percent with an ave­

rage of 44,40 percent. The frequency percent distribution shows

unimodal positively skewed nature in the phosphorite ( Fig. 3-B ).

Ferric oxide (Fe^Q^) i

The quantitative variation trends of ferric oxide in the

study area vary fron 0.28 to 4.58 percent with an average of 1.48

percent. Frequency percent distribution (Fig, 3-C) exhibits bimo­

dal nature of Fe 0. in the phosphorite.

Ferrous oxide (FeO) :

Ferrous oxide in the Nimuch Mata phosphorite ranges bet­

ween 0.25 and 4.17 percent with an average of 1.33 percent. The

frequency percentage histogram indicates bimodal nature of FeO

distribution (Fig. 3-D).

Titanivtm (TiO^) : ' 2

The variation trends of TiO^ in Nimuch Mata phosphorite

are from 0.23 to 1.58 percent with an average of 0,47 percent.

The frequency percent histogram shows unimodal positively skewed

nature of Ti02 in the phosphorite (Fig. 3-E),

Manganese (MnO) :

The qttapti.tat.3nge -gar la t lam tpeiaas c^ m£) i n tiae pho^pfa©-

r l t s raxiges between Q«l£l aead iS«Q3 peasxsesxt ti^th a c a^verage of &,Xi2

41

percent. The frequency percent histogram indicates a unimodal

positively skewed nature of MnO ( Fig. 3-F).

Lime and Magnesia (CaO and MqO) :

The variation trends of CaO and MgO in Nimuch Mata

phosphorite are from 0.67 to 4.70 percent and 17,00 to 36.31

percent respectively. The average concentration of CaO is

2.86 and MgO/ 28,48 percent. The frequency percent distribution

of both CaO and MgO in Nimuch Mata phosphorite shows bimodal

nature of distribution. (Fig. 3 G & H).

Phosphorus pentoxide ( 2 ^ *

' he quantitative variation trends of ^o^s ^^ ^^® study

area are from 6,30 to 10,02 percent with an average of 7,85 per­

cent. The frequency percentage histogram (Fig. 3-1) shows uni­

modal positively skewed nature of ^2^^ " ^ ^^ Nimuch Mata

phosphorite.

Soda and Potash (Na O and K^O);

The quantitative variation trends of Na20 and K2O in

Nimuch Mata phosphorite range between 0.23 and 2,40 percent and

0,07 and 0.73 percent respectively. The average concentration

of Na20 is 0.08 percent and K2O is 0,31 percent. The frequency

percent distribution of Na^O exhibits bimodal nature whereas

K2O shows unimodal positively skewed nature of distribution

(Fig. 3-J-K).

I»os3 of IgnltxoD ^^jQ ) »

The c^axrtltMtXvs -spariatifioa tr&ads c£ M.p'*' iLOI) in Niaaaacfc

42

Mata phosphorite range between 0.01 and 0,79 percent with an

average of 0.15 percent. The frequency percent histogram shows

unitnodal positively skewed distribution of H-O in the phospho­

rite ( Fig. 3 - M).

Carbon-dioxide (CO^) :

The carbon-dioxide (CO2) content in the phosphorite

ranges from 3.20 to 18.60 percent with an average of 9.4 per­

cent (i'ig. 3 - L) shows bimodal distribution of CO2 in the

phosphorite,

COMPOSITION AND KUTUAL RELATIONSHIP OF TIIE SIGNIFICAKTT OXIDES

v;ith a view to find out the compositional characteristic

and mutual relationships of the significant oxides^ the correla­

tion co-efficient among the various major oxides (Table VII) and

the concentration plots of P Oc and other oxides were^orked ©ut

(Fig,4), The results of the chemical analyses reveal that the

phosphorite deposit of Nimuch Mata is characterised by a low to

medium concentration of P-jOc and CaO, a higher concentration of

Si02# MgO, CO- and a low concentration of AI2O3/ Fe202/ FeO, MnO,

Na20, K2O and H20"*".

It is well known that all naturally occuring phosphates

are monophosphates get easily hydrolised in water because of the

P-O-P bond. Therefore,phosphate minerals are most conveniently

classified on the basis of cation polyhydra and their ccaidensation.

In phosphate, the oxygen atoms teicaag either to PQ^ or to Ir droa l

gxaere© ear to «a^er molexroles.

r - - 0 22

80

60

o

40

20

•I}-

0 I I I ' I I I _l 1 1 0

r = 0.I9

^ ^ I I I I I

10 )5 PjOj

10 C

r= 0 20

20 25 0

010

0 08

10 15 20 25 P2O5

o c Z

0 0 6

0 04

002

2 • T* I' r % o

D r=0 32

• • • • •« • ' I I I ' I I I ' '

4 6 P2O5

10

2 -

E r = 0 53

6 10 0 2

50

40

30 o 2

20

10

• • • t I " % I J ' ' I 1 1 0

6 8 P2O5

F r = - 0 2A

10 12

I ' l l 1 I 1 • ' ' 10 15

P2O5 20

10

o o

25 0

010

008

' 0 05

' 004

002 -

10

H

20 30 P2O5

40 50

0 I ' t I I I 1 t 1 1 i Q Q l I » Z m% I I I i I r

0 2 X. 6 8 «i 0 0L2 a* as o« to C02 t laa/PjOg

0«)d«« i«p«tc«n-t

43

FJG. A RELATIOWSHIP OF PjO^ WITH S102 ' ^"^^3 ,FeO,MnO,CQO AND M9O. CaO • P 2 % - C O j , C a a / P j ^ s - ^ 2 0 Pt0TS FOfi N^CKWMAIA

ptmsPHomm

44

Moreover, the mineral apatite is named gen rally accor­

ding to the proportions of F, Cl, CO2 and OH in a unit cell. How­

ever, (Mcconnel 1938) restricted the term flourapatite having

less than one percent each of C0„ and H2O and more than three

percent of flourine. The minerals of apatite series have the

general formula Ca ^^^4^6 (F^OH^Cl)^- The chemical composition

of Nimuch Mata phosphorite deposit shows higher contents of the

the oxides of Si, Mg, Fe and Al. On the other hand flourine is

not determined in any of the samples whereas significant amount

of CO and H»0 is of considerable importance. These constitu­

ents support the possibilities of carbonate hydroxyl apatite com­

position of the Nimuch Mata phosphorites,

MUTUAL RELATIONSHIP OF SIGNIFICANT OXIDES

The phosphorite has slightly higher concentration of

Al-O- than that of the phosphorite deposits of Matoon, Kanpur "

and Dakan Kotra, etc, P-Or- and CaO shows a weak but positive

relationship with Al-O- (Table - VII). A strong positive rela­

tionship also exists when Al O-, is correlated with CO^ and H^O 2 3 2 2^

whereas ^^0^, Fe-O^r MgO and MnO are antipathetically related

to A1202. The exceptionally high Si02/Al202/ MgO/Al202 ratios

(Table - VIII) and negative relationship of AI2O2 with Si02/ MgO and 'E^J:^^ suggest that probably 12* 3 ' ^® phosphate minerals

were replaced by silicate minerals either by silica solution

or through secondary silicification. The variable MgO/Al-O, ratio

seems to be due to acctKnulation of some terrigenous impurity,

TiK pcBElt;±ve reiatioasixlfi feefcweea Al_0- aod Ite O and K-O indicates

45

that concentration may be due to presence : of soda and potash

feldspar.

The relationship between SiO^ and P-jO which is graphi­

cally illustrated in (Fig. 4-A), indicates that there is an in­

crease in silica percentage with the decrease of P Oc content.

The inverse relationship between SiO„ and P Oc clearly indicates

that silica and phosphate have been precipitated under controlled

and mutually dependent conditions. The high concentration of sili*

ca in these phosphorites appears to be largely one of the dilution

of the amount of CaO and PpOc. The close similarity between

Si "*'(0,4 2A°) and P " (0.35A°) clearly indicates that these two

cations may be capable of co-polymarization with the tendency of

4+ 5 +

Si substituting P , Silica in the phosphate rock occurring

in the form of chert and quartz, appeared to be either detrital

or precipited under controlled pH condition. The presence of

detrital silica indicates the pro'xiraity of basin near the shore

line ( see Khan, H.H, et al.,1979.).

The relationship between ferric and ferrous oxides with

^2^5 ® graphically illustrated in Fig. 4{ B & C ). Both Fe203

and FeO show a positive relationship with P Oc though the rela­

tionship is very weak. Their positive relationship possibly

suggest that the phosphate minerals are somewhat ferruginous and

the phosphate precipitation took place under fairly oxidizing

condition ( Rao 1982). The iron oxides are antipathetically rela­

ted to magnesia. Their negative relationship may be due to the

rs jklaoesaeasst of Be S^ «g * C -aee laaewer *I,X..* lSFm>,

46

The Fe202/Al_0, ratio, which lies between 0.12 and 5,10,

(Table VIII) is higher than that found in aluminosilicate minerals.

It clearly indicates that iron oxides are not related to the alu-

mino-silicate minerals. Furthermore, the dominance of Fe^O^ over

FeO and nearly constant FeJO^/FeO ratio can be interpreted as an

indication of fairly oxidizing condition at the site of deposition.

Titanium oxide is antipathetically related to o'-'s ^ well

as to CaO. A sympathetic relationship of TiO- with Al-O^ suggests

a close association of geochemical association between the two

oxides though the geochemical coherence is very weak. A strong

positive relationship betv/een titanium oxide and iron oxide

( Table VII ) clearly indicates that much of the titanium in these

phosphorites is possibly due to the presence of titani\im bearing

minerals like rutile and anatase.

The concentration of manganese in these phospharites is

found to be very low that is in the order of 0,01 to 0,08 percent.

The plot and computed correlation co-efficient of MnO content

against P2^5 ^ Fig, 4 - D ) shows a sympathetic relationship, A

similar sympathetic relationship also exists when MnO is correla­

ted with iron oxides ( Table Vil ), The variable Mn/Fe ratio

(Table VIII) in these phosphorites indicates that manganese and

iron were delivered at the site of deposition in different propor­

tion and co-precipitated under fairly oxidizing condition where

2+ iron was more easily oxidized than manganese and Fe stablised as

2+ P^2^Z °^ ^^ (-OH)^, whereas Mn oxidized to MnO- or Mn(0H)2. ^he

ae^!t;±v^ relatloaship Q £ tSaO «giti2 CaQ m^ bet iixtex sreted as sxi^ss—

tt:t»ticm ci .^ by Hu in calcite lattice eai ^acaa^mt x^ close

47

similarity in the ionic radii of Mn "*" (o.90A°) and Ca "*" (0.99A°),

The positive relationship of 2^5 ^^^ ^^ ^^ ^^® phos­

phorite is illustrated in (Fig. 4 - E) and the correlation co­

efficient is given in table VII, The strong positive relation

between CaO and P Oc suggests co-precipitation of lime and phos­

phate forming stable calcium phosphate under suitable alkaline and

shallow marine water condition and probably of the photosynthe-

sizing blue-green algae playing the role of catalytic agent.

The CaO/P-Oc ratio ( Table VIII ) varies only within

narrow limits and its mean value ( 0.37) is less than 1,31, which

is expected for carbonate apatite. Moreover, the low CaO/P„Oc

values indicate the presence of different phosphate minerals possi­

bly aluminium or alumino-calcic as also evident from the positive

correlation between P.Oc- and Al^O-.

The relationship of MgO with P^^S* ^^ illustrated in

(fig. 4 - F). PjOc shows an antipathetic correlation with MgO.

A sympathetic relationship between CaO and MgO ( Table VII )

2+ suggests, that Mg J.nhibits the precipitation of apatite and

2+

s u b s t i t u t e s Ca in the a p a t i t e s t r u c t u r e (see Bachra, B.N, e t a l , ,

1965; Marten, C.3. and Har r i s s , R.C. 1970). The experimental work,

ca r r i ed by Marten and Harriss (1970), a lso suggests t h a t there

was probably a threshhold of Ca/Mg above which a p a t i t e could

p r e c i p i t a t e . The magnesian ions seem to r e t a rd the s a l i n i t y when

CaO/MgO (Table VIII) r a t i o approaches 4.5 to 5 .2 . The very low

Ca/Mg r a t i o (0.04 to 0,18) poss ib ly suggests replacement of magne-

sL&a, c a l c i t e b carboacttg aisat±t3e%. "Snia dert£S3slne(i aa gxiBEssliBB secsss

•to iae j^resent in tlje form (3£ fRa^cfeesiao: carbooat^ as well as Hydra-

^ed Kta^poesiuiB carbonate as iSKlicated hj tise positi'^ra co r r e l a t ion

48

of MgO with CO2 and ^j^^' Furthermore, the variable MgO/Al O^

ratio ( Table VIII ) suggests that Mg is also included in the

clay fraction.

The phosphorite deposit of ^imuch Mata shows that ^2^5

as well as CaO are antipathetically related to Na^O and K-O

(Table - VII). The negative relationship of Na^O with P2^5 ®"^

CaO suggests that bulk of Na-O present in these phosphorites may

be as a com^^ensatory cation in a coupled substitution pair of

2+ 2+ Na for Ca amd for PO. to preserve electronutrality (see Gul-

brandsen, R.A, 1966), The higher concentration of Na-O in these

phosphorites indicates that the formational environment was of

high salinity.

The concentration of potassiiam varies with P-,0 as well

as CaO. These phosphorites show low concentration of K_0 as com­

pared to Na^O. Soda and potash show close coherence with alxunina

which seems to be possibly due to the presence of some soda and

potash feldspars in these phosphorites.

PurtDerraore, the prepondrence of Na-,0 over K_0 and vari­

able Na20/K20 ratio ( Table - VIII ) suggest their derivation from

argillaceous sediments and the product seems to be controlled by

alumina, titanium, potassium, sodium and magnesia as well as

oxides of iron in slightly reducing to fairly oxidizing condition.

The results of the chemical analyses show that the pre­

sence of CO, in some of the sample is too high to be explained

«s coadaonate iapttrities* Ttae plots of CCLy ag- iast CaD + ^ 2 % ^^

sbomi ±a < Fig 4 - G >, iaSteatat that 002 * ^ *= ' ^ inm&ases v±th

49

the increase of CaO+P-Oc content. It indicates that basic phos­

phate mineral is the carbonate apatite. The negative correlation

co-efficient of C0„ with P^O^ suggests substitution of P by C,

The positive correlation between CO^ and MgO as well as CO^ and

CaO ( Table - VII ) indicates the formation of calcium/magnesium

carbonate.

The CO2 / P2°5 ^ " io (Table - VIII ) in these phospho­

rites was found to be very near to that of carbonate apatite ( see

Sandell et al., 1939), In some of the samples the higher CO„/P„0£.

-3 -2

ratio indicates the possibilities of PO. substitution by CO^

and compositionally, it approaches very near to carbonate hydroxyl

apatite.

The concentrat ion p l o t and co r r e l a t i on co -e f f i c i en t

values of H O with P^Oc and CaO show an a n t i p a t h e t i c r e l a t i o n ­al z b

ship among these c o n s t i t u e n t s . The CaO/P-Oc r a t i o p lo t t ed against

H2O content ( Fig 4 - H ) i nd i ca t e s t h a t samples having higher

the Ca0/P20c r a t i o are a l so high in HO values and vice ve r sa , ,

i nd i ca t ing thereby s u b s t i t u t i o n of (OH), by (P0-) . The excess

water s u b s t i t u t e s both Ca and P, poss ib ly in the form of H O and

H^O^ (Rao, 1982).

of phosphorites The geochemical characterstics/are discussed with the

help of triangular diagrams as follows :-

The triangular diagram (Fig. 5 - A) for MgO-CaO-P-Oc shows

that P_Oc and CaO decrease with addition of MgO in the Nimuch Mata 2 5

phosphorite. From the nature of calcite, dolomite and phosphate

aasocLat±o«i, it aay iae: st-ate-d. tJaart there were two gt.-aage's le-sUaig to

icbe foosaticm sf phosphorite viz., 1) decrease of CaO/p20u ratio

50

toe

FfG. 5 TRIAhfGULAR DIAGRAMS SHOWmO COMPOStTtOWAi • RiAftOW OF HAJim ©jaB£S »IIJ«H«JCHMA«k.PI^SPHO»J€

51

with increase of MgO and 2) decrease of CaO/MgO ratio with increase

of PoOc. Thus it probably appears that MgO controlled the stability

of CaO and P^^S'

Fig. 5 - B shows that MgO is sympathetically related to CaO

and CO- in the MgO-CaO-CO- system. The higher concentration of MgO

and CO- with respect to CaO content indicates that the constituents

in Nimuch Kata have undergone partial to complete dolomitization

as also indicated by lower CaO/MgO ratio.

The diagram K-O - Al-O- - Si02 (Pig.5 - c) illustrates that

the principal group of major constitutents not related to apatite

are those forming quartz silicate group of minerals. The K-O/Al-O-

and SiO- / Al-O- ratio reflect the insignificant amounts of admixed

alumino-silicate minerals. Another significant feature is the asso­

ciation of silica with the other constituents in substantial quantity

The diagram MgO.- SiO- - H20'*'(Fig. 5-D) indicates that there

is an increase of silica with the decrease of MgO. It has been

observed that samples having lower Ca/P+C ratio also have lower

H-O content and vice versa.

The P2O5 - ^2^^ " " 2 <^^39^^^ (Fig. 5 - E ) shows that

CO- + OH found to increase with the decrease on P2O5 ^ i" vice versa.

It indicates that manner of substitution might be PO. >• CO^OH as

well as the possibility of PO^v~" " ^(OH)^ substitution. The degree

of PO^ substitution by CO3OH seems to be low as compared to

^^4 % — (OH)^ substitution.

C H A P T E R - VII

GEOCHr:MISTRY AND DISTRIBUTION OF TRACE ELEMENTS

The recognition of trace elements in the rock body is

not of recent origin but many earlier workers particularly in

the begining of twentieth century have worked on the trace ele­

ments, kvashington, H.S., (1913) has stated that the minor ele­

ments were not related only to the rock type but to the major

elements constituting the rocks.

Goldschimidt, V.M., (1937) made certain useful observations on

elements distribution in the rocks as well as in the minerals

and proposed a geochemical classification on the basis of their

chemical affinity. Goldschimidt (1937) also stated that the

distribution of chemical elements in different phases depends

on the electronic configuration of the atoms. Subsequently

Mason, B., (1958), Tauson, L.V.,(1965), Nockolds (1966), etc.,

added further valuable information of the trace element studies.

Accordingly, the elements that indicate their presence into an

iron phase, sulphide phase and silicate phase are known as side-

rophile, chalcophile and lithophile elements respectively.

Ringwood, A.E,, (1955 a) applied electro-negativity to the dis­

tribution of trace elements. According to him whenever mutual

replacement between two elements possessing appreciably different

electro-negativity in a crystal is possible, the element with

lower electro-negativity will be preferentially incorporated

laecaaise it. forms a wore strong ioaic bond than cetisers. This

xsiie is -^api*©^ s«t isf act or tiy *«i::re d.i££ereEBee In eiecrtro-Bega-

tivlty is more than one. Graf, D.L. ClS'S©} suggested the

53

following five forms in which minor and trace elements occur

in carbonates :

i) Solid solubility in the individual minerals,

ii) In detrital minerals,

iii) as authigenic precipitate,

iv) as by-products of re-crystallization and

v) elements or their compound adsorbed by the different­

iation of elements during sedimentation.

However, no serious effort (except Rao, 1982,1984) has

been made by earlier workers to study the trace elements of the

phosphorite deposit of Udaipur district, Rajasthan. An attempt

has been made to present and discuss the geochemical abundance

and distribution of trace elements associated with the phospho­

rite deposit of Nimuch Mata, Udaipur districts, Rajasthan,

The concentration trend of various trace elements occu-

ring in the phosphorites of the study area have been compared

with the average values of trace elemints as determined by

Krauskopf, K.B., (1955), Gulbrandsen, R.A.,(1966) and also with

the average trace elements computed by Tooms et al.,(l969). The

concentration trends are also compared with the values computed

by Rao (1984) and given in Table - XI. The concentration of trace

elements in the Nimuch Mata phosphorite is given in Table - XII

and their relative distribution is shown in Fig. 6,

copper (Cu) :

Copper i s a s t r o a g cimlcpphile element in i t s gpeoctae-

« ^ c ^ Ssejaanrxenar, The a n a l y t i c a l r e s u l t s i ad l ca t e t h a t

54 fOO

80

G 60

( 0

2 0

1 XJLMJLJL

eoo

o 600

200

0 L J IIIIJJJLL 1 100

eo

«o

40

20 llllmiiiJii I 1000

800

600

<00 -

200

luiijlJl L. <3 _ fv

imuulillu

3 6

u^ ^ r CD c^

l l j J j J l . . l . ^ l fsj. («v s* d\ ui r^ m V*

Samtptri: Ho.

rre- € KRSTW3W(#*s smwww T«EiREijm*c fHsiweatrow of ctwwuw iwacs ELEMENTS

55

concentration of copper in the phosphorite varies from 2,4 ppm

to 70.7 ppm with an average of 11.7 ppm (Table - XII). A plot

of copper against Po^s ^^^^' "• ^ indicates inverse relation­

ship. The inverse relationship may possibly due to the ionic

substitution of copper in apatite lattice during diagenesis.

Furthermore, the negative correlation of Cu with CaO (Table-VII)

2+ may indicate the possibilities of replacement of Ca by Cu in

the apatite lattice. It is also known that under deduce physico-

chemical condition the algae was responsible for the removal of

Cu from stromatolites and copper concentrated in the rock adja­

cent to the algae matter ( Raha, P,K., 1978 and Verma, K.K.,1978),

Cadmium (Cd) i

The concentration of Cd in Nimuch Mata phosphorite

ranges between 1,10 ppm and 6,0 ppm, with an average of 2.61 ppm,

(Table - XII ), Cadmium shows significant sympathetic relation­

ship with P2* 5 ^®" plotted against the latter ( Fig, 7-B ).

Cadmium is also sympathetically related to CaO ( ' andel, E.B., and

Goldich, S.S., 1943, and Rankama and Sahama, 1950), Cadmium is

closely related to CaO owing to their near-identical ionic radii,

Cd( 0.97A* ) and Ca " (0,99A*^).

Chromium (Cr);

Chrcxnium c o n t e n t i n t h e Nimuch Mata p h o s p h o r i t e r anges

Very widely between 2 ,1 ppm and 9.89.9 ppm. wi th an average of

266.77 ppm. (Table - X I I ) , An i n v e r s e r e l a t i o n s h i p between Cr

and P2°5 ^^^9* 7-C) s u g g e s t s t h e non-coherence of chromiuni w i th

ptao^phorcKis. Cr SJSOSES c l o s e coiaereaKse wrth sooe eieasesEts reXa4:e^

.0009

.0007

= 0005

• 0003

.0001

-

1 -

A

r = -0 .25

• I 1 1 1 1 L

56

B

r = 0.17

• • • I * M •

I I I • I I I I I J

.09

07

o 05

.03

01

c r : - 0 0 5

I « • •

I 1 I 1 1 1 I I I I

D f x0.t9

J I I I I I I I — I — I I

.009

.007

.005

.003

.001

-- E

r:

.t.

- 0 18

.1 1 1

•

1..

•

• • • •

1 • • •

I 1

•

•

1 t

F r = - 0 0 2

• • • .

-1 I 1 • I I L 1 1 1 1

09

07

J3

a. .05

03

Qt

G r : 0.01

• •

• . •

• J 1 J I t I I t r

H

r = 0.12

• •• *• _ t I t I t < i t—t—t •

I- tor Ptxcnvt •

W

-\

57

to silicate and carbonate minerals as evident by its positive

correlation co-efficient with Si02/Ti02#Fe202/CaO and MgO

iTable - VII). Most likely much of Cr, present in the sili­

cates is entrapped by the fossil algae forming stromatolites.

Cobalt (Co) :

Cobalt is a siderophile element in its geochemical

behaviour and closely related to nickle (Goldschimidt 1929),

The concentration of Cobalt in Nimuch Mata phosphorite varies

from 100,9 ppm to 857.0 ppm with an average of 363,24 ppm.

(Table - XII). The plot (Fig, 7 - D) indicates that Co and

P2OC are sympathetically related with each other although

the relationship is very weak ( r = 0,19 ), The analytical

data shows that Co has close coherence with Ni, Fe and Mg

(Table - VII), The positive correlation of Co with CO2

suggest that cobalt content in thife phosphorite is possibly

due to presence of strcxnatelites,

Nickle (Ni) I

Nickle is a siderophile element in its geochemical

behaviour and occurs associated with iron. The concentration

of nickle in the carbonate rocks has been reported by many ear­

lier workers^ 4 ppm. to 200 ppm. by Gulbrandsen (1966),143 ppm,

and 14 ppm to 32 ppm in Hatoon and Dakan Kotra phosphorites

respectively, by Rao,(1984) (Table - XI),

Nickle content in the Nimuch Mata varies from 14 ,9 ppm

to 71,4 p£^ witii an asresrage of 3S.S2 fipa (TCaiaLe - XIXJ. Tlae

58

relationship between Ni and P2O5 is antipathetic as shown in

( Fig. 7 - E ).

The geochemical relationship among the elements in a

Mg - Ni - Fe phase as suggested by Ringwood ( 1955, 1956 ) that

2+ FeO bond is weaker than NiO bond and Fe is more mobile than

Ni "*", Therefore Fe is easily replaced by Ni , The present

study also indicates a negative correlation co-efficient

( Table - VII ) between nickle and iron and which suggests the

2+ 2+ replacement of Fe by Ni , The positive correlation between

Ni and MgO ( Table - VII ) suggest that Ni was retained along-

with Mg in sediments under favourable physico-chemical conditions,

Moreover, Ni content seems to be absorbed by the organic matter

during their life activity ( see Nicholls, G.D, and Loring,

D.H. 1962 ).

Zinc (Zn) :

Zinc is predominently a chalcophile element. Clark,

F.W., and Washington, H.S., ( 1924 ) reported 40 pFwn Zn in the

upper lithosphere.

The concentration of Zinc in the phosphorite ranges

between 13,4 ppm and 56 ppm with an average of 26.78 ppm.

( Fig. 7 - F ) shows an antipathatic relationship between ^2'^^

and Zn. The distribution of Zinc in these phosphorites indi­

cates that Zinc is mainly lost from the phosphates probably

during weathering and subsequently being taken up by the are-

59

Lead (Pb) ;

Lead is a chalcophile element and occurs mainly as

2+ Pb in phosphate and silicate minerals. The Pb concentration

in carbonate rocks has been reported to be fairly variable e.g.

5 to 10 ppm by Rankama and Sahama (1950). Rao (1982) reported

that the concentration of Pb in Dakan Kotra and Matoon phospho­

rites is from 24 - 56 ppm and 310 ppm respectively (Table-XI),

The present study reveals tha.t the concentration of

Pb in the Nimuch Mata phosphorite ranges from 258.8 ppm to

962.7 ppm with an average of 539 ppm (Table-XII). Tne posi­

tive relation of Pb with P OcCir'ig. 7 - G) possibly suggests

that Pb was separated from its original host mineral during

weathering and transported in the form of soluble stable com­

pound in association v/ith phosphate as well as carbonate mine­

rals to the site of deposition and accumulated in the algae

forming stromatolites.

Rubidium (Rb);

Rubidium is a lithophile element. It has close rela­

tionship with potassium and sometime it replaces potassium

(Hortman, £.L., 1959),

i'he CO.icentration of rubidium in Nimuch Mata phospho­

rite varies from 0-513 ppm wiuh an average of 170 ppm (Table-XII)

The concentration of Rb with phosphorite is appreciably higher

than its value reported by Rao, (1984)from the Matoon (4-14 ppm)

aad -tiie Dakctn. Kotra phospiacirites (1-4 pp©)*

60

The sympathetic relationsliip between Rb and P jOj.

(Fig. 7 - H ) clearly indicates that bulk of Rb seems to be

related with phosphate mineral and their fixation might be

controlled by the biogenic activity of algal stromatolites

as evident by the positive correlation of Rb with CaO and MgO

(Table - VII).

C H A P T E R - VIII

SU^iKARY AND CONCLUSION

The purpose, .of present investigation has been to investi­

gate the geocheniical nature of the phosphorite deposit of Nimuch

Mata area of Udaipur district, Rajasthan. Considerable attention

has be _n given to study the mode of occurrence, stromatolitic assem-

lages, petro-mineralogy and geochemistry of these phosphorites.

A summery of present investigation and the conclusion

drawn, are presented as follows :-

The phosphorite deposit of Nimuch Kata (24 37' : 73 41*)

of Udaipur district is locat-d within a thick succession of Frecam-

brian rocks of Rajasthan. Stratigraphically, the Precambrian rocks

of Udaipur region, referred to as Aravalli Supergroup are divisible

into three Formations viz., Debari Formation (lower), Matoon Forma­

tion (Middle) and Ldaipur Formation (Upper).

The rocks encounterea rrorr> east to west in the area of

interest include Lower phyllites, Up er dolomitic limestone with

phosphorite horizon, orthoquartzite and Upper phyllites, belonging

to the Katoon Formation of the Aravalli supergroup. Granite and

vein quartz occurrence in the northern portion of the area are post-

Aravalli intrusive bodies in the dolomitic limestone as well as in

the orthoquartzite.

The general strike trend of the rock units is N-S to

MW-S£ and dipping a-t €5° to 55° toward the west or saixtix^w-'St^

61

62

Joints are quite cornrTion in dolomitic limestone and quartzite. Some

minor folds and faults occur in the area.

The rock units, encountered in the study area comprise

mainly of dolomitic marble, quartzite, phosj^horite/ phyllites and

greywacks which are the products of low grade regional metamor-

phism which is comparable to the chlorite-schist facies.

The phosphorite dejt-osit of Nimuch Mat a reported from the

dolomitic limestone and often from quartzite, classified as

columnar algal stromatolitic phosphorite and

laminated algal stromatolitic phosphorite.

The phoSi^horite deposit occurs as a single horizon and

is traceable over a strike length of about 700 metres in Nimuch

Mata and extends impersistantly beyond upto 5 to 6 Km in the adja­

cent Badgaon and Sisarma area in the north and south respectively.

Its thickness varies from 0.5 to 10.0 metres. The P Oc- - rich

portion of the deposit, ( > 10% o^S^ """ confined to the central

part of Nimuch Mata.

The various stromatolitic form species identified resemble

those of Collenia columnaris (Fenton and Fenton), Minjaria dalceolata

(Korolyuk), Collenia baicalica (Maslove) and compound form of stro­

matolitic structure designated as SH-LLK-iiHrLLH-SH, These stroma­

tolitic form species are phosphatic in nature except Collenia

columnaris which is poorly phosphatic. However, all the form species

suggest a shallow sub-tidal to shallow inter-tidal environm^rntal

condition.

T'l^e phospisarites iia?»e colI<^h^3e and dahllifce as t t e

cboPBiaant phoSi-hate mixierals. C a l c i t e , dolcraite and quartz are

63

the dominant gangue constituents. The other minor associated gangue

minerals include^ chert, feldspar, muscovite,sericite and some

ferruginous matter.

Representative samples of Nimuch Mata phosphorites were

chemically analysed for the quantitative determination of their

major oxides viz., 120^/ SiO-* ^^o^S' ^^^' MnO,Ti02, CaO, MgO, ^205.

Na_0, K 0, H O and CO^ by weight percent. The deposits are cha­

racterised by low to moderate concentration of CaO and P-jO . and

somewhat higher concentration of SiO^, KgO and CO-.

The sympathetic relationship between CaO and i pOj. clearly

indicates the formation of stable calcium phosphate minerals. The

2+ presence of Hg and its positive relationship with CaO rather in­hibits the growth of apatite crystallites and possibly substitutes

2+

Ca in the apatite structure. The negative relationship of MgO

with P2O5 suggests the replacement of magnesium calcite by calcium

phosphate. The excess of CO^ and sympathetic relationship of CO2

with CaO + ^2^5 suggest that the basic composition of the phosphate

minerals is carbonate apatite. The higher CaO/P^Oc ratio suggests -3 -2

the possibilities of PO- substitution by CO^ and vice versa.

Moreover, the positive relationship between CO- and H2O suggests

that the substitution might have taken place in the manner: PO . . ^CO^OH. The h igher CaO/P-Oc va lues a r e a l s o high in 1 20"*"

v a l u e s i n d i c a t i n g t h e s u b s t i t u t i o n of (OH), by (PO^). The sympa­

t h e t i c r e l a t i o n s h i p of ^IpO^ wi th CaO and P^Oc sugges t s t h e f o r ­

mat ion of a lumino-phosphate mine ra l and t h e r e a c t i o n may be as

fo l lows t

^ 2 ^ 2 % ^ ° " ^ 4 * 2fS^4"^ ^ 2A1PG^. 2H2O + 2Si02 + H^O

64

The except!onall^i low values of CaO/i'205 ^"^ the nor­

mal CO^/P^Oc values in these phosphorites suggest the possibili-

-3 -2

ties of PO, substitution by CO^ and the composition approaches

very nearly that of carbonate hydroxyl apatite. The positive rela­

tionship between PpOj- and iron oxides bear testimony to the fej^ru-

ginous nature of these phosphorites. The dominance of Fe-O^/FeO

ratio possibly suggest fairly oxidizing condition at the site of

deposition.

The principal oxides viz., 3i0„, TiO , ^'^^2' ^^o*^' ^7^

etc.,which are not related to apatite, may have association with

the silicate group. The nigh SiO^/Al-O^ and the lev; K O/Al-O^

and MgO/Al„0^ ratios signify the presence of quartz and alumino-

silicate minerals in these phosphorite. The excessively high

Si02 content might have possibly derived from secondary silici-

fication and possibly caused by the dilution of PoOc. The oxides

of K and Ti seem to be strongly associated with clays, Na is

possibly distributed between clays and apatite.

The phosphorites of Nimuch Kata are strikingly united

in their trace element suite compared to that of other phosphorite

deposits of Udaipur region, such as Matoon, Dakan Kotra (Rao,1984),

Jhamar Kotra, Kanpur ( Banerjee, et al., 1981). Only Rb concentra­

tion in Nimuch Kata phosphorite is in notable quantity. Some of

the variation in concentration may be due to the presence of car­

bonates and silicates.

The trace elements viz., Cu, Cd, Cr, Co, Ni, Pb and Rb.

in the phosphorite of Niraiich ftfeta hatve been defcexmlned

65

quantitatively. The elements like Cd^ Co, Pb, Rb and Cr seems

to be related to apatite. Zn, Cu and Ni are probably associated

with the carbonate as well as with the silicate minerals. The

trace element distribution in these strcmatolitic phosphorites

suggest that the fixation of Cu, Ni, Co, Cd, Pb, Rb and Cr was

geochemically controlled by the biogenic activity forming fossil-

algae, Elements adsorbed by clay, alumino-silicate and carbonate

minerals include Cu, Ni, Co, Pb, Zn and Rb, The general trend

of trace element dispersion in the Nimuch Mata phosphorite appears

to be somewhat similar to the concentration trends as reported

from the shallow marine sediments by Keith, K,L. and Degens, E.T.

1959. It may, therefore, be suggested that the environment of

deposition of Nimuch Mata phosphorites was shallow marine water.

The formation of phosphorite may be due to chemical

precipitation phenomenon controlled by the physico-chemical condi­

tions of tne medium such as Eh-pH and supply of the materials,

SiOp, P-pOc and CaO were brougi.t to .the depositional basin by the

chemical decay of the pre-existing terrestrial rocks ( Banded

Gneissic Complex ) containing minexi-ls like apatite^ quartz,

feldspar and some ferromagnesian minerals, etc. Most probably ,

Marine upwelling caused the concentration of phosphate minerals

over the shelf areas of the Aravalli basin. Due to luxurent

growth of blueish-green algal flora in the warm and sunny shallow

marine environment, the phosphatic sediments might have accumu­

lated initially with the specific communities of algal structure,

39se fa'Vour^xLe geocijanicai ^ivixQEcmeat acccmps^yliig actiis ity of

66

algal matter mutually interacted under a set of shallow inter-

tidal to shallow sub-tidal environmental condition at the time

of deposition of phosphorite. The precipitation of phosphate

was however essentially dependent upon the Eh-pH conditions,

partial pressure of CO^, temperature, photosynthesis and replace-

ment process.

B I B L I O G R A P H Y

Baner jee , D.M., 1971 a . . Or ig in of Precambrian sed imen ta ry

phospho r i t e s of Rajas than, I n d i a , Proc, 58th I n d .

S c i , Congr. I l l (V), p . 297.

Baner jee , D.M., 1971 b , , Precambrian s t r o m a t o l i t i c p h o s p h o r i t e

of Udaipur, G e o l . Soc. Amer, B u l l . V. 82, No. 8,

p p . 2319 - 2330.

Baner jee , D.M,, 1971 c , A r a v a l l i s t r o m a t o l i t e s from Udaipur ,

Ra jas than . J o u r . Geol . Soc. I n d i a . V. 12 (4) ^ 5^9- '? '55-

Baner jee , D.M. 1974. , M i c r o f o s s i l s from l a t e Precambrain

phospha t i c A r a v a l l i s t r o m a t o l i t e s of Udaipur,

Rajas than , I n d i a . I n . V.K. ( e d . ) , Rec. Research in

g e o l . Delhi Hindustan Pub. Corp. 1, pp . 263 - 268.

Baner jee , D.M. Basu, P .C, and S r i v a s t a v a , N. , 1980^, P e t r o l o g y ,

Mineralogy, Geochemistry and o r i g i n of the Precambrian

A r a v a l l i p h o s p h o r i t e d e p o s i t s of Udaipur and Jhabua,

I n d i a . Econ. G e o l . 75 (8 ) , p p . 1181 - 1199.

Baner jee , D.M., Sahgal , G . C , Neeta S r i v a s t a v a and Khan, M.W.Y.,

1 9 8 1 . , Element v a r i a t i o n p a t t e r n in t h e Precambrian

phospho r i t e s and count ry rocks of Udaipur, R a j a s t h a n .

P r o c , 4 t h I n t . Sem, on p h o s p h o r i t e I , G . C , P . p r o j e c t -

156^ tJ^rtigrrr^ JjssSia^ I Q e i ,

6 7

68

Banerjee« D.M, and Sahgal , N, , 1987, , P ro te rozo ic p h o s p h o r i t e of

I n d i a , Updated in format ion p a r t I I . Geochemistry,

Mem. Geol . Soc, I n d i a , No. 6, p p . 487 - 510.

Baner jee , D.M. and Sahgal , N, 1988. A s t u d y of p r o t e r o z o i c

phosphor i t e from Chelima Pachcher l a a r e a , Kurnool

d i s t r i c t , A .P . I n d i a . J o u r . G e o l . Soc. I n d i a . V. 32,

p p . 32 - 39,

Barman, G. Verma, K.K. and P u r i , S . N . . , 1978, , B i o - s t r a t i g -

raph ic zona t ion of the s t r o m a t o l i t e s bea r ing hor izons

in the A r a v a l l i s of Udaipur, d i s t r i c t , Ra ja s than ,

J o u r , Geol , Soc, I n d i a . V. 19, No. 6, pp . 264 - 267.

Basu, P . C , Sood, N,C. and Venkatesh, V, 1 9 8 1 . , Precambrian

, phosphor i t e of Cuddapah b a s i n - A phosphogenic model.

( A b s t r a c t ) . 4 t h I n t . F i e l d workshop and seminar on

p h o s p h o r i t e . Vol . of A b s t r . p . 39 .

C h a t t e r j e e , P.K., and Mukharjee, B, 1 9 7 1 , , Mineralogy of

phosphor i t e from Udaipur, R a j a s t h a n , Proc , 58th Ind ian ,

S c i . Cong, I I I ( V ) , p , 236 ( A b s t . ) .

Chaudhuri , R. Chakrabor ty , A.K. and Ghosh, S.K,, 1968. , S tud i e s

on Indian p h o s p h a t e s . Pa r t I , Technology, V, 5, No. 4,

p p . 285 - 293 .

69

Chaudhuri, R. and Balasubramanian, N,, 1980,, Grade d i s t r i b u t i o n

pa t te rn and i t s bearing on the formation of high and

low grade in Jhamar Kotra phosphorite depos i t . Udaipur,

Rajasthan, Ind. Jour . Earth Sc i , V. 1, No. 1, pp.89-93.

Chaudhuri, R, and Roy, A.B., 1986., Proterozoic Cambrian

phosphorite deposi t s of Jhamar Kotra^ Rajasthan,

India . In , cook, P . J , and Shergold, J.H. ( Eds.) :

Phosphate depos i t s of the world, V.I . Cambridge

un ive r s i t y . P ress , 386 p .

Chauhan, D.S., 1970,, Phosphorite bearing s t romato l i t es from

Araval l i s of Rajasthan, 5th Himalyan geology sem.

Chandigarh, p , 10 ( Abstract ) ,

Chauhan, , D.S., 1973., S t romatol i tes from the Precambrian

phosphorite bearing stratum of the Araval l l region of

Udaipur, Rajasthan. Dokl. Acad. Nauk. U.S.S.R. 208,

pp. 1429 - 1431.

Chauhan, D.S., 1979,, Phosphate bearing s t romato l i t es of the

precambrian Arava l l i phosphorite deposite of Udaipur

region, t h e i r environmental s igni f icance and genesis

of phosphori te . Precamb. Research V. 8 pp. 85 - 128.

Chauhan, DL,S., 1980 a , . S t romatol i tes of Nimuch Mata and

Badgaon phosphori te deposi ts and genesis of rock

i?4io :feaebe* Proc , Moz^es^of} stroflBafetiolites Ja®, 191B,

H^aipeuv Bajastla^x, Xi^^a. C saX» Sarv« Ixsaia. mit^c*

i ^ b , 44, pp . 314 - 329.

70

Chauhan, D.S,, and Sisodia, 1981., Matire of Udaipur phospho­

rite and its genetic implication, Proc. 4th Int. Sem.

on pyK>sphorite I.G.C.P. Project - 156, Udaipur, India.

Clark, F.W. and Washington, M.S., 1924., The composition of

the earth crust. U.S.G.S. Prof, paper 127.

Damle, G.V. and Sharma, B.L,, 1970., The nature and sedimentary

structure in Aravalli rocks around Udaipur, Rajasthan.

West commemoration V, Sagar Univ. Sagar. pp. 470 - 484.

Drever, J.I., 1971., Magnesium iron replacement in clay

minerals in anoxic marine sediments. Science, V. 172.

pp. 1334 - 1336,

Fenton, C.L. and Fenton, M.A,, 1937., The belt series of the

North : Stratigraphy, sedimentology and Palaeontology,

Geol. Soc. Amer, Bull, V. 48, pp, 1873 - 1970.

Goldschimidt, V.K,, 1929., Die Natur geschichte der Eisenfamilie.

Stahl u. Eisen, Heff, 18.

Goldschimidt, V.M., 1937., The principles of distribution of

chemical elements in minerals and rocks. Jour. Chem.

Soc, for 1937, p. 655,

Graf, D.l*,, I960,, Geochemistry of carbonate sediments and

sedinjentary carbonate rocks, I* IV^ Illinois state

Geoi. Sarv. Clre* ^ 7 , 2J9B, 3^1, 3158, p^ 250.

71

Gupta, B.C. , 1934. , The geology of c e n t r a l Mewar. Mem. Geol .

Surv . I n d i a . V. 65, p t . 2, pp . 107 - 169.

Gulbrandsen , R.A., 1966. , Chemical compos i t ion of p h o s p h o r i t e s

of phosphor ia format ion, Geochim. e t . Cosmochim, Acta,

V. 30, pp . 769 - 778.

Hacket, C.A., 1881 . , Geology of A r a v a l l i r eg ion . C e n t r a l and

E a s t e r n . Rec. Geol . Surv. I n d i a . V. 1 4 ( 4 ) .

pp . 297 - 303.

Heron, A.M., 1935. , Synopsis of t h e Fre-Vindhyan geology of

Rajputana . T r a n s . Nat . I n s t . S c i . I n d i a , V. 1, p t . 2,

p p . 17 - 33 ,

Heron, A.M., '1936. , Geology of the South - Eas te rn Mewar,

Rajputana . Mem, Geol , Surv. I n d i a . V. 48 p t . 1,

p . 90.

Hteron, A,M,, 1953 . , The geology of C e n t r a l Ra jpu tana , Mem,

Geol , Surv . I n d i a . V. 79, p t . 1, p p . 1 - 389,

Horstman, E .L . , 1959, , The d i s t r i b u t i o n of L i , Rb and Cesium

i n igneous and sedimentary r o c k s , Geochin, e t ,

Cosmochim Acta , V. 12, No, 1 - 2 , p p . 1 - 2 8 ,

Krylov, I . N , , I 9 6 0 , , The developitient of columiiar b ranch ing

stx<j«Batolites ^axia^ Seip^ean t imes in S o u t b e r a U r a l s ,

K G * . A k a ^ »a«tea* S*S,S»a, ¥ • 132* J^EU 39S - 8SB.

72

Krauskopf, K,B. , 1955 . , Sedimentary d e p o s i t s of r a r e m e t a l s .

Eco. Geo l . 50 th Anniversary Vol. pp . 411 - 463 .

Ke i th , M.L. and Degens, E . T . , 1959, , Geochemical i n d i c a t o r s

of marine and f r e s h w a t e r s e d i m e n t s . I n , P.H. Abelson

( E d i t o r ) , Researches i n geochemis t ry , Wllley, New York.

N,Y, p p . 38 - 6 1 .

Khan, H.H,, 1979, , An a p p r a i s a l of Precambrian p h o s p h o r i t e

of Jhabua, M.P. I n d i a . I n . Cook, P . J . Shergold, J . H ,

( e d s . ) , P r o t e r o z o i c ~ Cambrian phosphor i t e , Canberra

Pub. and P r i n t . Co. Ltd . Canberra , pp. 42 - 8 3 .

Korolyuk, I , K . , I 9 6 0 . , S t r o m a t o l i t e s of lower Cambrian and

P r o t e r o z o i c of t h e I r k u t s k a m p h i t h e a t r . Tr , I n s t . Geo l ,

Razrab Goryuch, I skop , Akad, Nauk, U.S.S.R, V, I ,

pp . 112 - 161 .

Latouche, T.H.D,, 1902 , , Geology of wes te rn Rajputana, Mem. Geo l .

Surv , I n d i a , 3 5 ( 1 ) , p p . 1 - 116.

Logan, B,W,, 1 9 6 1 , , c ryptozoan and a s s o c i a t e d s t r o m a t o l i t a s

from r e c e n t Shark Bay, wes te rn A u s t r a l l i a , J o u r , G e o l ,

V, 69, p p . 517 - 5 3 3 .

Logan, B.W., Re^ak, R. and Gioslxtrg, R.N,, 1964,, C l a s s i f lcat : lo .

and e invi ronmeata l s i g n i f i c a n c e of a l g a l s t i a o m a t Q i l t e s .

73

Maslov, V.P . , 1937. , On t h e Pa leozo ic rock b u i l d i n g a l g a e of

Eas t S i b e r i a , Mascow Univ. P a l a e n t . Lab. , Pub.

Problems of Pa laeon to logy , V. 17, pp . 335 - 339.

Mason, B . , P r i n c i p l e s of Geochemistry , 3 rd . e d . . New York :

John Wiley & Sons, 1966, 329 pp .

Mathur, R.K., 1964., Sys temat i c g e o l o g i c a l mapping in p a r t s

of Udaipur, Ra j a s than . Prog . Rep. F . S . 1963 - 6 4 .

Geol . Surv. I n d i a , ( Unpublished ) .

Mathur, R.K,, 1965, , A no te on r e p e t i t i o u s sequence of

g r a y w a c k e - s l a t e - p h y l l i t e s i n t h e A r a v a l l i System

around Udaipur, Ra ja s than . B u l l , Geol , Soc, I n d i a ,

V. 2, pp . 84 - 8 8 .

Middlemiss , C . S . , 1922. , Geology of I d a r s t a t e , Mem. Geo l . Surv.

I n d i a . 4 4 ( 1 ) , p . 166.

Mukt ina th , 1967. , Phosphate d e p o s i t s i n Rajasthan^ Ind i an

M i n e r a l s . V, 21 , No, 2, pp , 83 - 101 ,

Muktinath and San t , V.N,, 1967, , Occurence of a l g a l p h o s p h o r i t e

i n t h e Precambrian rocks of R a j a s t h a n . Cur r , S c i ,

V, 86, No, 23, p , 638,

Muktinath and San t , V.N., 1969. , P h o s p h o r i t e i n Precambrian

rocks of Udaipiir a r e a , Rajas^thaa. P r o c . 56 th Irad,

S e t . Ooragr, &ssct*, p t » 4^ £ ^ . ^ - 9a .

74

N i c h o l l s , G.D, and Lor ing , D.H., 1962, , The geochemis t ry of

some B r i t i s h ca rbon i f e rous s e d i m e n t s . Geochim, e t ,

Cosmochim. Ac ta . V. 26, pp . 181 - 223.

Pandya, M.K. and Chauhan, D .S . , 1976 . ,Or ig in of rock

phosphate d e p o s i t of Jhamar Kot ra , Udaipur, Rajas than ,

Semi. Develop. Rock phosph, and p y r i t e s . Udaipur ,

p p . 1 9 - 4 0 .

Pandya, M.K. S r i v a s t a v a , S.B.L. and Dwivedi, C .S . , 1984 . ,

Pet rography and geochemis t ry of t h e Jhamar Kotra

p h o s p h o r i t e d e p o s i t s , Udaipur, Ra ja s than . S p e c i a l

Pub. Geol . Su rv . I n d i a . No. 17, pp . 117 - 127.

Pandya, M.K., S r i v a s t a v a , S.B.L. and Dwivedi, C . S . , 1 9 8 1 . ,

Pe t rography and geochemist ry of t h e Jhamar Kotra

p h o s p h o r i t e d e p o s i t , Udaipur, Ra ja s than . P r o c . 4 t h

I n t . Sem, on p h o s p h o r i t e , I . G . C . P , P r o j e c t - 156,

Udaipur, I n d i a ,

Patwardhan, A.M., 1 9 7 3 . , A n o t e on t h e o r i g i n of Mussorie

p h o s p h o r i t e i n t h e lower Himalya, I n d i a , and i t s

Pa l aeo -geograph ic i m p l i c a t i o n s . Mineral . Depos i t a ,

V. 8, pp . 369 - 387.

Raha, P.K. , 1978 . , S t r o m a t o l i t e s and t h e i r b e a r i n g on t h e

geiiesijs of t b e magaes i t e aakd a s s o c i a t e d sailpii ide

Jaasema^ Workshcyp cm stiXOTtttciltes iselS cm Jaai . 9 - 12,

a t Udalpaxr^ £ ( a j a s t h ^ «

75

Patwardhan, A.M., 1975 . , More evidence i n favour of t h e b i o ­

chemical o r i g i n of the Mussorie p h o s p h o r i t e , Kumaon,

lower Himalya, I n d i a , Mineral . Depos i t a . V. 10,

pp . 261 - 265 .

Raja Rao, CS,, I qba ludd in and Mathur R.K., 1968. , Algal

s t r u c t u r e s from A r a v a l l i beds nea r Dakan Kotra .

Udaipur d i s t r i c t , Ra ja s than . Cur r . S c i , 37(19) ,

pp . 560 - 5 6 1 .

Raja Rao. C . S . , 1 9 7 1 . , Precambrian s t r a t i g r a p h y of R a j a s t h a n .

A review. Rec. Geo l . Surv . I n d i a , 101(2) , pp . 6 0 - 7 9 .

Rankama, K. and Sahama, T.G. , 1950, , Geochemis t ry . U n i v e r s i t y

of Chicago P r e s s .

Ringwood, A.E. , 1955 ft,. The p r i n c i p l e s , governing t h e t r a c e

element d i s t r i b u t i o n dur ing magmetic r e c r y s t a l l i z a t i o n .

P a r t I . The e a f l u e n c e of e l e c t r o n e g a t i v i t y , Geochlm.

e t . Cosmochim.Acta. V. 10, p p . 297 - 303.

Rao, L.A.K., 1982, , Or ig in of p h o s p h o r i t e d e p o s i t s around

Matoon, Dakan Kot ra , Udaipur d i s t r i c t , R a j a s t h a n .

Ph.D. Thesis A.M.U., A l l g a r h .

76

Rao, L.A.K. and Akhunjee, R.A., 1983,, Algal stromatolites

phosphorite and its palaeo-environmental significance

In the Precambrian Aravalli rocks formation of Kanpur

area, Udaipur, Rajasthan. Proc, X Ind. Coll. Micropal.

and Strat. Ill - 118.

Rao, L.A.K, and Rasul, S.H., 1984., A recent observation

on the geochemistry and genesis of some Precambrian

phosphorite of Rajasthan state, 27th Int. Geol. Cong.

Moscow. U.S.S.R. 7, ( Section 13 - 16 ) 294 - 300.

Rao, L.A.K,, 1984., Trace element studies of the Pre­

cambrian stromatolitic phosphorite of Udaipur,

Rajasthan. Chem. Geol, 45, pp, 17 - 31,

Rao, L,A,K, and Rasul, S,H,, 1985., A carbonate bearing

hydroxy1 fluorapatite from the Precambrian Matoon

Formation around Dakan Kotra, Udaipur, Rajasthan,

Ind, Jour, Earth Sci, V. 12, No. 3, pp. 187 - 192,

Rao, N,K, and Rao, G.V.U., 1971,, Petrographic study of

some Indian phosphorites. Jour. Geol, Soc, Ind,

12(4), pp. 356 - 367.

Roy, A,B., 1978., Report on the structural analysis of the

rock phosphate bearing of the Jhamar Kotra mines,

Udaipur* Rajasthan, Unpublished Rep, Subm, to R.S,

77

Roy, A.B. and P a l i w a l , B . S . , 1981 . , Evolu t ion of lower

P r o t e r o z o i c e p i c o n t i n e n t a l d e p o s i t s . S t r o m a t o l i t e s

b e a r i n g A r a v a l l i rocks of Udaipur, Rajas than , I n d i a ,

Precambrian Res, V, 14, pp, 4 9 - 74.

Roy, A.B. Nagor i , D.K., Golani , P .R. , Dhakar, S .P , and

Chaudhuri , R,, 1980. , S t r u c t u r a l geometry of t h e

rock phospha te -bea r ing A r a v a l l i rocks around Jhamar

Kotra mines a r e a , Udaipur d i s t r i c t , Ra jas than , Ind ian

J o u r . Ear th S c i . , V. 29, No. 1, pp . 21 - 25 .

S a n d e l l , E .B . , and Gold ich , S . S . , 1943 . , The r a r e m e t a l l i c

c o n s t i t u e n t s of some American Igneous irocks. P t , I

J o u r , Geol . V, 5 1 , No. 2, pp , 527 - 537,

Shap i ro , L,* and Brannock, W,W,, 1962, , Rapid a n a l y s i s of

s i l i c a t e , c a r b o n a t e and phosphate r o c k s . U . S . G . S .

Prof, Paper . 1144 - A, pp , A 1 - A 56,

Taiison, L.V, and Kravchenko, L.A., 1965 , , C h a r a c t e r i s t i c of

Pb and 2n d i s t r i b u t i o n in Minerals of Calcedonlan

g r a n i t o i d s of t h e Sauanyr b a t h o l i t h i n C e n t r a l

Tian - Shan, Geokhimiya, No, 8, pp , 819 - 824 ,

Tooms, J . S , Siirmtjerhayes, C.P, and Cronan, D , S . , 1969 . ,

Geochemistry of roari«e phosphate and manganese

d e p o s i t s , Oceonogr, Mar» Blol,^ Aim> Rev,* V, 7,

HP, 49 ~ 1(K). ,.v^J^S5^,^;^. . r

AccN«. • >

V^i

78

Valdiya, K,S., 1969 a.. Stromatolites of the lesser Himalyan

carbonate formations and the Vindhyans, Jour, Geol,

See. India^ 10 : pp. 1-25.

Valdiya, K.S,, 1969 b,, A new phosphorite horizon in late

Precambrian calc zone of Pithoragarh Kumaun Himalya.

Curr. Sci. 38(17) : 415 - 416.

Verma, K.K. and Barman, G,, 1975., On the Origin of phosphorite

rocks of Rajasthan, India. Semi. On Rec. Adv. in

Precamb. Geol. of Udaipur, Rajasthan.

Verma, K.K., 1978., Mineral deposits related to stromatolites.

Proc. Workshop on stromatolites, Jan. Udaipur,

Rajasthan.

Washington, H.S., 1913., The distribution of elements in igneous

rocks, ore deposits,. Am. Inst, Min. Met. Engg.

EXPLANATION OF PLATES ancJ

M i c r o p h o t o g r a p h s of t h i n s e c t i o n s

PLATE - I

F i g , 1 Columnar a l g a l s t r u c t u r e showing t h i c k s h e a t h s of p h o s p h a t e ( b l a c k ) and c a r b o n a t e (wh i t e t o l i g h t g r e y ) , N o r t h - W e s t of Nimuch Mata .

F i g , 2 L a m i n a t e d / s t r a t l f o m i a l g a l s t r o m a t o l i t l c p h o s ­p h o r i t e ( d a r k ) c e m e n t e d w i t h c a r b o n a t e ( w h i t e ) , a l s o showing t h r e e co lumnar s t r u c t u r e

one a t b o t t o m composed of c a l c i t e ( w h i t e ) , two a t t o p , t h e r i g h t one i s composed m a i n l y of c a r b o n a t e and has t h i c k s h e a t h of p h o s p h a t e w h i l e t h e l e f t one i s composed p a r t l y of c a r b o n a t e and p a r t l y o f p h o s p h a t e ( N o r t h - E a s t of Nimuch Mata ) ,

PLATE - I I

Fig. 1 Feebly phosphatic ( black ) collenia columnaris associated with dolomite ( light grey ) ( East of Nimuch Mata ),

Fig, 2 Minjarla calceolata showing distinct laminae of phosphate ( dark grey ) and carbonate ( light ) ( North of Nimuch Mata ).

Pig. 3 A colony of Collenia balcllca showing branching, traversed by quartz vein (white), ( North-West of Nimuch Mata ),

Fig, 4 Block diagram of Compound structure ( SH LLH SH LLH — SH ) showing uneven phosphate laminae < black ) disconnected and more or less alternate with carbonate laminae ( white ), ( Ue&t of Miimach Mata ),

79

80

PLATE - I I I

Fig« 1 A r g i l l i t e s showing mud-cracks ( West of Nimuch Mata ) ,

F i g . 2 A r g i l l i t e s showing r i p p l e marks a t t he Eas t e rn f lank of Fateh Sagar l a k e .

PLATE - IV

Fig, 1 Irregular granules of cellophane ( dark brown ) cemented by calcareous materials, ( Crossed nicols, X 25 ),

Fig, 2 Collophane showing linear bands in clustered form embedded in quartz, ( Crossed nicols, X 25 ),

Fig. 3 Quartz exhibiting oblique to undulose extinctions ( Crossed nicols, X 25 ),

Fig, 4 Fine grained quartz-vein surrounded by the collophane granuled ( dark ). ( Crossed nicols, X 25 ),

PLATE - V

F i g . 1 Rhombohedral g r a i n s of c a l c i t e i n p h o s p h o r i t e ( Crossed n i c o l s , X 25 ) .

P i g . 2 Doloroite ( l i g h t ) p a r t i a l l y r ep laced by co l lophane ( dark l i n e a r bands ) . ( Crossed n i c o l s , X 25 ) .

81

Fig, 3 Phosphorite showing feldspar with laminar twinning, sericite and quartz. ( Crossed nicols, X 25 ).

Fig. 4 Pyrite crystal enclosed by quartz and dolomite crystals. ( Crossed nicols, X 25 ),

PLATE - VI

Fig. 1 Dolomitic limestone showing quartz vein ( l i gh t ) with ferjrugenous cher t ( d a r k ) ( Crossed n i c o l s , X 25 ) .

F ig . 2 Quartzi te showing quartz with iron oxides and che r t ( Crossed n ico l s , X 25 ) .

Fig. 3 Quartzi te showing metamorphosed quartz with sutured boundaries ( Crossed n i co l s , X 25 ) ,

PLATE-1

FlG.l

FIG. 2

PLATE-II

I

FIGJ F1G.2

riG.4

PLATE- I !

FIG. 1

FIG. 2

PLATE-IV

FIG. 1 {*n4C.,X25)

FIG. 2 ( * n i c ^ X 2 5 )

FIG. 3

( *n i c . ,X25 ) FIG. 4

( • n i c . , X 2 5 )

PLATE-V

FIG. 1 ( • n i c . , X 2 5 )

FIG. 2 ( • n i c . X25)

( •n ic . ,X25 )

PLATE-V I

FIG. 1 ( + n i c . , X 2 5 )

( + n i c . , X 2 5 )

FIG,3

(*n ic . ,X25)

A P P E N D I X

>

1

u -1 ©

< H

C « c *t m

4J

-P 0)

(0 •0

% 01 0) +>

o 0* <o 0

(0 *i

£ o 3 e •H 25 «w 0 C

o •H

-H 0)

§• e o 0

10

o <0 x: u

1 s ? <

•

^ •-I

fO T-«

CM •H

fH -»

O r-»

cr>

CO

r-

\D

in

^

o

f4

T-l

«» a ••

» •

'« t «

«

tjQ

r-fV

o tn

tH

00 r-t

r-l

\o r-•

CM

CO r-o

m in

n

-(5v- ' tn • o

o in

r-»

o M

TH

vO ro

M

vO t

M

<» r» o

o w «-•

<*>

o CM ^ <

O ^ *

<» tfi

o o •

xa in

in

ro rH

o in

• *

(N

•^ r-l •

CO CO

o\ r« CO • ^

•"S" T-i

CM •<4<

in in *

in •<t

VO t

•<*

in in

in Tj-

CM vO

CO

r* ^ CO

o a\ CM

O VO

in

CM

o •H CO

m • > *

• T*

<& m

* o

r<

r-o

CD (N

o

a\ <*>

o

in CD • o

CO o\ ro

CM ^

O

(Ti in • o

CM a\

o

n ^

o

t »n TH

n VO

"*

in t-4

r^

00 lO

•«»

ro o CM 0) P>4

«n CO

• «-l

tf) CN • o

•* so o

in CM

o

in CO

o

r-' r * o

00 in

CO

00 CO

o

CO in • o

CO CO

o

o CO

o

o\ CO

»-«

r* »H

•*

•'1'

o tH

CM t-«

•<»•

o a> fk

r-• ^

« o

D Z

CO CM

O

CO CM

o

CO CM

o

p 2

CO CM

O

in • *

o

in • ^

• o

in •*

o

CO CM

o

o as

o

CO m tH

c vO

o

o C7\

o

CM O •H f*

CM O « o

n o • o

«-» o o

r-l

o o

»-t

o o

• *

o * o

00 o o

t-l

o o

CM o • o

• f

o o

CM o o

r-t

o o

CM O

O

»-l

o o

T-t

o o

o c m

«0 ^ •

w CM

cr» CO •

VD CM

O O

in CM

o o

o o

CM

O O •

CO CM

c «-<

CO r-t

o o r« CM

•<<•

CM •

•5<>

CO

ON .H

CM CO

O O

CO CO

CO CO

CO

o o rH CO

f-4 CO

vO CO

o CM

CM

O » S

10 CO •

CM

o r-• •

• « »

CO

CO

t VO

O

in Tf

CO

CM o •

CM

CM O

CM

O 00

CO

o 00 •

CO

CM i-t

CO

CM tH

CM

o CM

r-t

VO

o CO

(Ti 00

CO

O 00

CM

O (0 u

»n 00 •

f-

o GO •

Cf\

o CM

CO

o CM

CO

o CO

r

o o t

CO

CM

o o .-)

o •<t

00

o 00 •

VO

o o r>

o o r

o f~-

t-»

o o r-*

o o GO

O o t

in

o CM Ck

00 o •

»H

**i CO « o

CO CM

O

o VO

»-l

o CM

CM

(n CM • o

r CM

o

o in

r-l

•<* a\ • o

vO CM

O

o •'I'

iH

o •'J'

CM

CO

o CM

tn CM

o

o m »-i

O CM

(0 2S

T H CO

• o

"*p CM • o

•«1' r-t

o

a\ CM

o

o CO

o

o\ r-t • o

r rH

o

tn CM

o

CO CO • o

CO CO

o

CO CO

o

1-1 in

o

CO

r-o

'* •"J*

o

r» o o

o CM X

o ^ •

CO

o (T> »

VO

O r> CM

o VO

CO iH

o c ^

o \o •

CO 1-1

o r» in f-i

o o ^ r-t

O CO •

in

o ^

(7\

• *

ro

CO

O CM

CO

O 00

vO

o C7>

CO

o tn

CO

CM

O U

tfV «H

• o

a» o • o

CM r-t

o

r-o o

in rH

o

r-« t-l • o

o\ o o

CO o o

CTv CO • o

TH

O

° 1 ro O

O

o\ r-o

CM vt

o

CO

o O

TH

o o

•f

o CM X 1

•

^\ a\ •

00

CO VO

c CO 00

00

o in

00

en T-«

r-l •

OS

o as CM

o CO as r4

o CO 00 •

CO c in CO

a\ as

rt> o o o in as as as

CO vO

00 en r~ CO

as as

as «*

00 (7*

H •

O

' •

.

>

I

»^

<

in 0)

H

•H ;<

>

c o >. +> c %

o

0}

H

01

4)

•H

O

p. 0} o •a OS +> to

o

i

c 0) 0)

• p

o 1-!

o

(Q

a

c o

• H - P «J

H <U

o o

cc:

a.

O

u o

s

3 o

o

CNJ O

o

o CNJ

O

(0

in O

(\j 0.

o (0 u

o

CM O • H EH

O 0)

O CM

CM O • H CO

O CM

CM O

O

? ? O

o

in O <f O tr\ • •

o o

t n CM CM

o o g

00 o

CO in r-

i n

? ? ? ? in CM

vo m • ?

CM O

CM in

• o

in rn

c T—

• o

"S

eg

o ? J! !3 5 5 8

• • • • • * o o o o p <«•

'mimil>mmmnli»mmmm

o o 8 r- 00 00 ^ Q

r- CM t- CM O • • • • *

? ? ? vo

O I

ON in

in in

in o • o I

o CM

o

CM O

o 1

o o • o I

vo in

in CM

00

?

-4- c^ CO f»- CM o vO ^ O r- r- O • • • • • • O O O O O t-m^mm*f,mmmfmmmmmmf

o • o I

CM CM • O

in o 00 O

O

in o •

o

in CM o I

00

o f

CO

tn

o

CM

O

CM CM O •

O I

o hr> t^ o b* tn o • • • O O t- M«MMiNli^MNiN*<MMM

in in

in CO

o o CM

CM m o CM CM

tn OS c

o

o in CM

00 in

(M T-

Q O

o CM ? -

CM rn o I

r-

O d r-

d CO

o ON

o -d- <t in o o o o CM

CM •3' CM

MMhtMMMkfMwMM

in O

o o o I

o I ? ? o

I mmmiifmmmim^0m'm

in vo in in CM o o 1

o CD

r-

CD

-a- in o d

o o O T-

00 m r- in

CM in in

O r- tn CO

o o o in CM

? ? ? ? KN

o vo •

o

vo O

o

fn o o

? -•^MMMMMMMMiMMaa

in o •

o

rn O

o I

vo O O

o CM

O

VO tn

o CM

o J

CM O tn o

CM 8

•*««a«i<k»««iii^#awMi

tn in

00 oo CM CM 00 ^

00 o CM

O O

O I

o I

o I

o I

o I

III IHillMIIWIMW»*WI

o -Cl­i n

•4-

d tn

d CO vo

vo CM K fn t- in o T- 3! ? ° ? ?

CO o O T-

o I

i n <»•

O d

O in

in rn t« vD <f T- f m

o o

o I

o I

o I

CM CM

CM CM *

O I

c o CM

vo o o I

CM -d-m CM • •

o o I

m o in o

r-

O

CM T -

• o I

r-m

o I

•4-

O I

CM

O I

fn O

o I

CO

m

CM in c m o

o I

o I

o o

vo CM

o o vo

rn ? ?

CO

m o

cr> o I

o o

•l-P«M«»>««)«MMM

o vo in

00

vo o

vo vo

• o

o o

CM 00 CM

c ^ c ^

? ?

o o

rn

o I

c ^ CM

o I

o o

5 o I

o o

o o

m o

CM CM

o CO

tn o CM o

at

CM O O O

i n O

CM cu

o CM

(0 2 ;

o CM Ui

CVJ o o

o CM X

3 U •rt

o u o o * O 5 £ S

H H H >

u

CQ

c «

o CM

\ o M

(0

z

(0

o IT)

o (M

\ o u o \ o 0)

n O

< \

ro O

<M 0>

CM

O

O oi

<

O •H to

• 0)

0 JC

0

10

fO S

x: o 3

z u 0

M O •H +> (0 l

in O CM

C>4

CM

o o

O M

P4 \ C4

O D O fM

(0 z o en

o (0 o in o CM 0«

o u o 0)

ro O cv» 0) ( ro O OJ

i-t

< CO

o (M

fO

O CM •-i

< O

ro O CM

o

CO

•

CO

:

:

^ • o

ro If

CM

o rH

O

O •'I' • o

t-H

<N CO ro

r lO

CM CM

O o •

CO ro

«-»

0\ Tf • o

r* in

o

rH i-«

O

a\ •>* • o

CM

r-'Sj'

ri

<N ro

vO •*

O O •

in in

CM

r-a\ • o

00 f^

CM

c o o

•«* • • o

r-t

00 vO tH

ro CM

TH

r-l

00 in •

CM rH

ro

CVJ ^ • o

ri

t • < *

• > *

o o

VO t-t

• o

CM

in

\o o

in in

^ rH

CO ^ •

CO T-^

• < *

ON T-t

• «-•

•f CM

•<1«

VO O

O

o ro • O

o

vD ro O

in

r* CM

VO <3\ •

ro

in

<* ro •

r^

00 VO

O

c o o

in '<* • o

CM

r~t

VO

p

VO '* iH

CM

«H in •

00 CM

VO

'* 00 • o

in 00

CM

r-t .H

O

o VO • o

1-i

tH

in

TH

o\ r* r* CO

a\ r* •

VO T-l

r*

r VO • «-•

o o VO

5J« rH

O

in >* • o

CM

<NJ T-4

o

VO

r»

r» 00 •

«-»

00

f-in •

TH

o\ in

T-l

1-1 T-l

o

o CM • o

»H

o r-l

in

00 ro

ro CM

in in •

CM VO

Oi

fO ro •

OJ

r-l CM

T-l

r-o o

in CM • o

o

TH CO

o

•<»'

r-l

O ri

CM 00 •

ro f-i

O

r-VO • o

fO ro

r-

(N r-»

o

r«-•<t

• o

rH

ro ro

O

00 in

•* CM

ro r-«

Tl<

tH

r-CM •

CM

CM in

in

• *

o o

00 o • o

CM

< rH

o

ro ro

T-t

TH

CM ^ «

ro ro

CM

in in •

r-i

Tj-

VD

rH

ro r-l

o

o •* • o

CM

VO CM

o

VO o ON

o in •

VO rH

fO

o r-• o

00 ro

r-l

CO TH

O

00 ^ • o

ro rH

o

vO in

c

ro O •

rH

^

c 10

o 6 T3 C (0

eg

8 o en

^ (n • <N

%

X H

1

u ^ OQ

<

f<

O (0

u •0

c 10

in O

CM Cki

% U s <w o w • ^J 0) fl +> a> -H c w 0 O a j3 E Q. 0 « O 0

£ X 0, •-i 9 <0 ^ -p

«J V S Xi +» J3

o «w St-

o g •H

^ z 4> C > -H

o o O <N ^ i4 0 TJ •P C

« <0 19 m •> O « c«

' ^ l ^ O

t - » • •

« «•

n

CM

O CM

Ui

O CM

CN O

to

O (0 u

CM O O

•A o Pi

0»

t ^ c ^ o o o l r > ^ - ^ • * ^ ^ H < ^ m a ) o o ' • o \ o \ r » c o o o t ^ i o c n u i i n m c M ^

i r ^ O ^ ^ O O O O O O O O O O O

C M X D I ^ I ^ ^ V O ^ C M v O x f i n f - c M o m f ^ o o t ^ i n ' *

CM 00 ON CM CO CO U> CM

c M T H f ^ t r » c M r o o r ~ * - « r - < M C M i n c n

O C O U > C M i / > C O ^ C ^ < 7 * ^ 0 0 » n o c M c o o o t » - t - ' ' * r > o o o v n o o v o r * o c o v o « r > o o « H o o c M r * v D ^ ' *

i n c M o o O N r ^ r ^ v o o o c M i n r o ^ c o r * r o c O ' * O Q O O ^ r ^ r l < v O T H C M O O » H r o

a ) o o r ' < ^ ^ v o o o c o ' n ^ < ^ » - < o o c M

« * ' ' * - « * ' v o c n c M r M i n c M i n < < C O V O C M » - » O C M ( N r > - C M

«-( CD • ^ <0 rH CM 0» TH

00 ^ 00 0> f-H T-t TH CM

C7» CO vO CO CO 0 » CO CO 0 0 VO CTv <J\

C M r H f O O O C O t - t O C O » - i c o T » < c o r ^ i n n » - i

o ^ M v o i n v o c o o v ' ^

« - « c M m c o m t - t a v o o r ^ r ^ ^ o o ^ o o c o r - o o r - t ^ r » « o « n m r » ' * v o u )

r - o o r ^ c M i n t ^ c o < J ^ v o t n o o f M O \ t - »

f - t 9 t ^ r - t r - < ^ O C M r l > 5 j > \ 0 0 \ < < > > 0

< ^ l f > o o o » O l ^ » c M ' ( | • ^ ^ o < * > ^ ^ o v

oo\or'r»«>\0'>*»-«fo»-«oO'-«cMc<> r - ( < - 4 r 4 < - l r - l * - t t - 4 r M C O C M r - i r O C 4 < M

4-icoovf-i«4iooc4r^t^^<4>f-««-«cn • » • • • • • • • • • • • • c ^ t o i n c i v ( 9 4 0 r - a > o ( * » M t n o S ' ^

im : 'V «• <« « «»- (» «« «4

• • • 1 *tt *v #

c (0

fM

o •H CO •O C O

o X

CM

u

aq

(0 •P

a •

c +> O H a. M e o O JC o Q,

0) M O

a, (0 •p (0

u 3 E •H 2

3 43

0)

•p

<4-l

o

-p ^

o o o 4J

tn o 04

•0 V « c •p «

3 O o y

o o

m o CM

w <M o u

tN

CN

(0

o

O

o f^

^ 0 ^ - O l D » ^ > < ^ l < ^ l r - 0 0 0 ^ 0 ^ o 0 ^ C 0

00 CM 00 fO

00 r~ rf r^ 5* CM uo ir>

CM o c^ <?\ o\ o •-< vO VO VO CO \£) VD •«J"

O N t r ) \ o i n o \ \ o m i n T j ' r H < H v o t ^ r o O f ^ O O t - « - « o c M r o r o ^ C M r M a o i n

O O O ^ O O f O O O O i - t O O O

CM CO ^ 0> VO \0 TH t^ ro a» o CM 00 r> m CD. in ^ c

c M ^ c M i r ) r - t ^ o o o c M r » c M ^ 5 i < < n v o i n u o m i n m u o v o r ^ i n ^ o t ^ v o v o

T - t r O O O O ' ^ » - « C 7 \ C M 0 0 * - t O Q O - * » - »

CM

o o o

CO r c o t^ r^ r-l r-l r-i r-t T-i

o o o o o o o o o o

i n c M r > < ^ 0 \ ^ ^ o o c M v o c ^ 0 ^ t > • T ^

c ^ m r " r o » - » c M T H < y \ r « . r M v o i n i n t n r O T j « « a < ^ ' * x ) < r a < c o c M ^ r o r M f o r o

c M c o T j « i n v o r * o o < ^ o •-• o* f^ ^

T A B L E - XI

t- comparision of the abundance of t r ace elements in phosphor i tes .

Elements

Cu

Cd

Cr

Co

Ni

Zn

Pb

Rb

I

19.00

5.00

102,00

1.43

23.28

118.8

80.33

7.76

II

22.47

5.18

57.7

4.76

24.40

60.23

32.40

13.35

III

2.4-70.7

1.1- 6.0

2.1-989.8

100,9-857

19.5-71.4

13.4-56

258.8-962.7

0.0-513.9

IV

4-40

-

30-400

-

4-200

10-200

-

•*

V

100.00

-

1000.00

-

100.00

300

«»

•"

VI

0.6-394

1.0-10.0

7.0-16 00

0.6-11.8

1.9-30

4.0-345

0.0-100

0.0-100

I * -

I I * -

III-

IV-

V -

VI -

Average.of twenty-one phosphorites from Matoon

Average of seventeen phosphorite sample from Dakan Kotra

Average of fourteen phosphorite sample from Nimuch Mata

Average computed by Krauskopt (1955)

Threshold values for phosphoria formation according

to Gulbrandsen (1966).

Average computed by Tooms et al (1969) usihg dat

compiled by Swaine (1962).

Average cMsputed by Rao ( 1984 ),

10

a;

e (0

CO 0) •P

H H X

1

u 1^

CQ

<

H

V4 0 x: 0. 0)

o Xi (X

It , -p 1 ro

X

JC

o 3 E •H 2

o

(0 « (0 > 1

(0

c

o m

•

o> « t4

: « ; > , • <

.

r-4

<n r-f

CM

o

ON

CO

p-

VO

in

•*

m

CN

(H

•

: •

o r-•

rt »-•

'

•

110 «

ro

CS • ^

r« n fM

CO •

v£)

r-•

in

VO

a\

en • •«t

><* •

CM

o •

VO

r-t

• CO

n •

ro

r-• o r

o •

•«i' T-t

00 •

in

d CJ

rH VD •

IM

1-t

• ro

r-t •

rM

O^

r-l

O •

CM

rt •

CM

CO

CM

1-1

» CO

T-t

• tH

Ov •

tH

O •

CM

r • ro

O •

VO

O •

eg

O • ro

XJ O

wi

r-•

*o VO <rj

TH

« r-• *

T-»

• CM

a> r-r-iH

CO •

ON 00 ON

ro •

tH

CM

ro

'S* O CM

in •

•"J* ON tH

CM •

VO

r>-

^ •

•<f ON CM

in •

in

CM

in • o o tH CM «

ON ro CM

VO •

in VO CM

• *

• VO tn vO

M O

^ CM • cn NO **J

o •

VO ro CM

r-» • r-<JN in

00

ro tH

»H

in •

tH

CO tH

ON • ro ro

ON

O

o tH ro • ro ro in

r«j • r> o

iH

• r-vo tH

in •

00

o TH O • r in CO

00 •

in 00 ro

ON *

ON ro iH

VO • ro (M in

0 U

CM CO • m ro

0\ •

• ^

tH

tH

• CM CM

ro

o • *

•t

• tH

r~

ro •

VO CM

in

tH

<*

CM •

•l* CM

in •

o\ tH

VO •

ON • *

in •

•>3' CO

t • o •<*

CM •

VO ro

^ • r« *)•

CT\ •

CM CO

•H 25

r-r~ 9

»o CM

^ •

VO CM

•* •

ro tH

vO

rH CM

O •

VO tH

in • r-tH

ON

o CM

00 •

ro tH

VO • ro CM

o •

ON ro

ro •

in tH

in •

f>* CM

o •

vO in

CM • o» •«»•

r-•

ON ro

C i>J

tH

r •

(f> en m

r •

CM VO ON

00 •

CO in CM

00

ON vD in

tH

• ro in ro

CO • o

o tH

•<* ro ON •

O CM

ro O • r ro

O •

in VO

tH

• ON CM CO

r-•

(N 00 ro

ro •

CM ON in

VO • o en in

r-•

r-CM in

JQ 04

o r • o r>-•tH

o •

CM

o tH o • r-vo

o tH

<N

ro •

C7N CJN

VO • ro •>*

•l-

ON in

CM • o tH tH

ro •

in

tH

CM • ro ro

in •

CM VO tH

ON • ro »H in

p-•

00

o ro 00 •

CM O

Q Z

JQ en i

: