My Thesis

Origin and Occurrenceof Soapstone in Sherwa,
Abbottabad, Hazara Division, KPK.
RAJA JABIR CIIT/FA10-ERS-057/ATD
MUNIM AYAZ CIIT/FA10-ERS-016/ATD
EHTISHAM KHURSHEED CIIT/FA10 -ERS-099/ATD
HAIDER KHAN CIIT/FA10 -ERS-072/ATD
Department of Earth Sciences COMSATS Institute
of Information Technology Abbottabad –
Pakistan
Spring 2014

COMSATS Institute of Information Technology
Origin and Occurrenceof Soapstone in
Sherwan, Abbottabad, Hazara Division, KPK.
A thesis presented to
COMSATS Institute of Information Technology, Abbottabad
In partial fulfilment
Of the requirement for the degree of
BS Earth Sciences
By
SALMAN AHMAD CIIT/FA10 -ERS-063/ATD
Spring 2014
i

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Origin and Occurrenceof Soapstone in
Sherwa, Abbottabad, Hazara Division, KPK .
An undergraduate thesis submitted to the department of Earth Sciences as a partial
fulfilment of the requirement for the award of Degree of BS in Earth Sciences.
Name Registration Number
SALMAN AHMAD CIIT/FA10-ERS-063/ATD
HAIDER KHAN CIIT/FA10-ERS-072/ATD
Supervisor
Mr. Ayaz Mehmood
HOD, Department of Earth Sciences,
COMSATS Institute of Information Technology (CIIT) Abbottabad.
Co-Supervisor
Dr. Muhammad Zahid
Department of Earth Sciences,
COMSATS Institute of Information Technology (CIIT) Abbottabad.

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Final Approval
Origin and Occurrence of Soapstone in
Sherwan, Abbottabad, Hazara Division, KPK.
By
SALMAN AHMAD CIIT/FA10 -ERS-063/ATD
Has been approved
for the COMSATS Institute of Information Technology Abbottabad
External Examiner:
Dr. Mohammad Ishaq Ghaznavi
(Department of Geology, University of Haripur)
Supervisor:
Mr.Ayaz Mehmood
(Department of Earth Sciences / Abbottabad Campus)
Head of Department:
Mr. Ayaz Mehmood
(Department of Earth Sciences / Abbottabad Campus)

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Declaration
We Raja Jabir, Munim Ayaz, Salman Ahmad and Haider Khan hereby declare that we
have produced the work presented in this thesis, during the scheduled period of study.
We also declare that we have not taken any material from any source except referred to
wherever due that amount of plagiarism is within acceptable range. If a violation of
HEC rules on research has occurred in this thesis, we shall be liable to punishable
action under the plagiarism rules of the HEC.
Date:
Raja jabir
CIIT/FA10-ERS-057/ATD
Munim ayaz
Salman Ahmad
Haider Khan

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Certificate
It is certified that Raja Jabir, Munim Ayaz, Salman Ahmad and Haider Khan have carried
out all the work related to this thesis under my supervision at the Department of Earth
Sciences COMSATS Institute of Information Technology, Abbottabad and the work
fulfils the requirement for award of BS degree.
Date: 14 – July – 2014
Supervisor
Mr Ayaz mehmood
HOD, Department of Earth Sciences
Head of Department:
Mr.Ayaz Mehmood

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DEDICATION
To Almighty ALLAH and the Holy Prophet Muhammad
(P.B.U.H)
&
My Loving Family

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ACKNOWLEDGEMENT
‘I only desire your betterment to the best of my power;
And my success in my task can only come from ALLAH;
In Him I trust and unto Him I look;’
(Surah-e-Hud, Verse 88, Chapter 11)
First of all, we would like to thank ALLAH Almighty for giving us the capability,
perseverance, courage and determination to accomplish this venture.
Darood-o-Salam to the personage (SAWW) for whose sake Gracious ALLAH created
this universe.
We are immensely thankful to our supervisor, Ayaz Mehmood, for his valuable guidance
and encouragement.
We are also indebted to the management and faculty of the Department of Earth Sciences
especially Dr. Muhammad Zahid, Dr. Allah Bakhsuh Kausar, for their support.
Last but not the least; we give our heartfelt thanks to our parents for bearing with our
endless hours of work and for fully supporting us, also we thank our friends and siblings
for being with us all the way through.
Raja jabir
Munim Ayaz
Salman Ahmad
Haider Khan

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Abstract
The present studies deal with soapstone deposits of the Sherwan area, Hazara. Sherwan is
located 35km to the northwest of Abbottabad city. The purpose of the present work is to
understand the petrography and occurrence of Sherwan soapstone. The overall relief of the
area is moderately high. The study area consists of different types of lithologies, which
constitute the Abbottabad Formation, Tanawal Formation and Hazara Formation. Hazara
Formation underlies the Tanawal Formation. It dominantly consists of slate and phylite.
Tanawal Formation consists mainly of quartzose schist, quartzite and schistose rocks. It
underlies the Abbottabad Formation which consists mainly of dolomitedolomitic
limestone, quartzose sandstone and limestone. Dolomitedolomitic limestone is grey to
dark grey in colour. It is medium to thin bedded. Quartzose sandstone is mostly jointed and
fractured and is brown in colour. It is medium bedded an coarse grained, limestone over
lies quartzose sandstone, it is thin to very thin bedded. Veins of calcite are also prominent
at places. Dolomitedolomitic limestone, member of the Abbottabad Formation host most
of soapstone deposits. The soapstone occurs as irregular shaped bodies warped in dolomite
beds.
Based on the field, geology, petrography and mineralogy of the Sherwan
soapstone deposits, it is concluded that Sherwan soapstone deposits are formed due to
both, i.e: Syngenetic and epigenetic. In origin syngenetic deposits probably represent
either metamorphosed silicious dolomite rocks or formed due to reaction between
dolomitic and quartzitic beds. During metamorphism the epigenetic class includes
deposits which owe their origin to a metasomatic process addition of silica to a relatively
pure Dolomitic rock. The additional silica could be released from dolomitic rock during
hydrothermal activity. The source of these hydrothermal fluids could be Mansehra
granite.

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Table of Contents
Chapter No1 Introduction.
1.1 General Statement..........................................................................................................1
1.2 Soapstone in Pakistan ....................................................................................................1
1.3 Soapstone deposits of Hazara Division..........................................................................1
1.4 The study area ...............................................................................................................2
1.5 Relief and Climate. ........................................................................................................2
1.6 Nature and Scope ..........................................................................................................4
1.7 Objectives .....................................................................................................................4
1.8 Methodology .................................................................................................................4
Chapter No 2 Regional Geology
2.1 Tectonic of north Pakistan ............................................................................................5
2.2 The Himalayas ..............................................................................................................5
2.2.1 The sub Himalayas..........................................................................................5
2.2.2 The lesser Himalayas ......................................................................................6
2.2.3 The high Himalayas ........................................................................................6
2.3 Geology of Hazara Area ................................................................................................6
2.3.1 Salkhala Formation.........................................................................................9
2.3.2 Hazara Formation............................................................................................9
2.3.3 Tanawal Formation.........................................................................................9
2.3.4 Abbottabad Formation ....................................................................................9
3.3.5 Datta Formation ............................................................................................10
2.3.6 SamanaSuk Formation..................................................................................10
2.3.7 Chichali and Lumshiwal Formation..............................................................10
2.3.8 Kawagarh Formation ....................................................................................10
2.3.9 Kala chitta Group..........................................................................................11
2.3.10 Murree Formation .......................................................................................11
2.3.11 Manshera Granite........................................................................................11
2.4 Mineral deposits of Hazara..........................................................................................12

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2.4.1 Iron ore..........................................................................................................12
2.4.2 Phosphate......................................................................................................13
2.4.3 Magnesite deposit .........................................................................................14
2.4.4 Soapstone......................................................................................................14
Chapter No 3 Local Geology
3.1 General Statement........................................................................................................15
3.1.1 Hazara Formation..........................................................................................15
3.1.2 Tanawal Formation.......................................................................................16
3.1.3 Abbottabad Formation ..................................................................................17
3.2 Description of lithological units...................................................................................18
3.2.1 Quartzite........................................................................................................18
3.2.2 Phyllite ..........................................................................................................19
3.2.3 Dolomitic Limestone ....................................................................................19
3.2.4 Quartzose sand stone.....................................................................................19
3.2.5 Thin bedded Lime stone................................................................................19
3.2.6 Fleshly coloured Quartzose sand stone.........................................................19
Chapter No 4 Economic deposits of Sherwan
4.1 Soap stone deposits of Sherwan...................................................................................20
4.1.1 Bandi Mines..................................................................................................20
4.1.2 Chelethar Mines............................................................................................21
4.1.3 Khandakhu Mine 1........................................................................................21
4.1.4 Khandakhu Mine 2........................................................................................23
Chapter No 5 Petrography, Wet Chemical Analysis and XRD
5.1 Petrography..................................................................................................................24
5.2 X-Ray Diffraction ........................................................................................................25
Chapter No 6 Discussion and Conclusion
6.1 Discussion and Conclusion…………………………………………………….27
References………………….……………………………………………………….30

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LIST OF FIGURES
Fig.1.1 Circle showing study area........................................................................................3
Fig 2.1 Geological map of Hazara Kashmir Syntaxes (after Greco, 1991) .........................7
Fig: 3.1 Hazara Formation ................................................................................................15
Fig: 3.2 Tanawal Formation...............................................................................................16
Fig 3.3 Abbottabad formation ...........................................................................................17
Fig 4.1 First mine at Chaleter ...........................................................................................21
Fig 4.2 Talc deposit in Chaleter mine................................................................................22
Fig 4.3 Shaft Mine at KhandaKhu.....................................................................................22
Fig 4.4 Tunnel of shaft mine at KhandaKhu No 2 ............................................................22
Fig.5.1 XRD of Sample No 1.............................................................................................26
Fig.5.2 XRD of Sample No 2.............................................................................................26

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LIST OF TABLES
Table 2.1: Stratigraphy of the Hazara Area ........................................................................8
Table 3.1: Stratigraphy of the Sherwan Area ....................................................................18
Table 5.1: Chemical analysis of major element of talc......................................................25
Table 5.2: Result of XRD ..................................................................................................25

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1.1General Statement
Talc is an industrial raw material used in many industrial applications because of its unique
physical and chemical features. It is a layered, hydrous magnesium silicate with chemical
formula of Mg3(Si2O5)2(OH)2 and the theoretical chemical composition of 63.5 wt.% of SiO2,
31.7 wt.% of MgO, and 4.8 wt.% of H2O (Grim 1968). Talc is an industrial mineral, which is
composed of hydrated magnesium sheet-silicates with theoretical formula of Mg3Si4O10(OH)2
that belongs to the phyllosilicate family (Fuerstenau and Huang, 2003; Ozkan, 2003; Yehia and
AL-Wakeel, 2000; Boghdady et al, 2005). Talc may have white, apple green, dark green or
brown colours, depending on its composition. It is the softest among Mohs hardness scale
ranging from (1–1.5) and a greasy feel (Boghdady et al. 2005). The specific gravity of talc is
about 2.75; it is relatively inert, and water repellent (Engel and Wright, 1960). Talc extracted
from various localities shows different mineralogical, chemical, and physical properties; these
features depend on their parent rock types, and origins play a key role in their usability. Based on
their origins, talc deposits can be classified into 5 groups:
i) Ultramafic-related talc deposits, ii) Talc deposits within dolomites, iii) Metamorphic talc
deposits, iv) Talc deposits related to banded iron formations, and v) Secondary talc deposits
(Prochaska 1989). Talc/Soapstone is used in many industries such as paper making, plastic, paint
& coating, rubber, foods, pharmaceuticals, cosmetics and ceramics etc.
1.2Soapstone in Pakistan
In Pakistan deposits of soapstone are reported at Sherwan (Abbottabad, Hazara), Jamrud and
Landikotal (Khyber Agency), Parachinar (Kurram Agency), Zhob (Balochistan) and various
other localities (Zaki 1969).
1.3 The Soapstone Deposits of Hazara Division
In the Hazara division, soapstone deposit occurs around Sherwan, to the northwest of
Abbottabad. These are probably the largest and economically viable soapstone deposit of the
country which is being exploited at several localities in the area around Sherwan for the last
several years. In local language the soapstone is called “Glass Mora”.

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The Sherwan deposits in Hazara District are found in zone that is 10 miles long and 1 mile
wide extending from Hariala westward across the Siran River to Kharan. Although there are
as many as 50 soapstone mines in the Sherwan area, most of the production comes at the
following four localities:
 Bandi
 Chelethar
 KhandaKhu
 Kangrora
Total production of soapstone from the Sherwan area during the year 2000 is reported to be
55,000 metric tons (MT). All the mine owners are from the private sector. About 1500 labourers
are engaged in the excavation and transportation of soapstone in the area. Thus the mining and
supply of soapstone has been a source of income and employment for the local people. Besides
the Government of Pakistan also gets monetary benefits from this natural resource in the form of
royalty and excise duty as well as other taxis are levied both on the raw material and on its
products.
1.4 The Study Area
As mentioned above several large deposits of occur in the Sherwan area of Abbottabad, Hazara.
These are being mined at a number of places and have been producing good quality soapstone
for the last several decades. A detailed geological investigation of these deposits is the subject of
present study. The location of study area is Chelethar (sherwan) and the distance of chelethar is
42km from Abbottabad. Geographical coordinates of the area are 34o
11'0.6.53"N and
73o
02'26.74"E (Fig 1.1).
1.5 Relief and Climate
The overall relief of the study area is moderately high. The slopes are generally steep. Locally
thick covers of alluvium have not only reduced gradient of the slopes greatly but have also
resulted in the formation of relatively low plains. Notable difference in lithology, structure
and texture of the component rocks have led to the formation of many escarpments in the area
under discussion.

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Climatic conditions of the area are more or less similar to those in Abbottabad however the
hot weather starts a little later and ends a little earlier in the study area. The result is that the
summers are relatively short and winters long in the Sherwan and adjoining areas.
The annual average rainfall in the Sherwan area is about 23”. Although the winters are not
altogether dry, most of the rainfall takes place during the hotter month of the year with July
and august recording maximum rainfall.
Fig.1.1: Circle showing study area.

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1.6. Nature and Scope
Large deposits of soapstone occur at a number of places in the Sherwan area of Abbottabad,
Hazara. Despite their economic importance geological details of these deposits especially their
petrographic and mineralogical characteristics are largely unknown. Detailed studies of such a
nature are needed not only for their affective utilization but also to know about their genesis.
The current study is initiated to furnish such information about the Sherwan soapstone.
1.7 Objective
The major objective of the current investigation is to study in detail the geology, petrography
and mineralogy of the Sherwan soapstone. The result from these studies is utilized to discuss
the origin of these deposits.
1.8. Methodology
1.8.1 Fieldwork
A detailed fieldwork was carried out in the study area. The study includes, measuring
thickness of the formation, marking contact between soapstone and Abbottabad Dolomite and
taking samples from different locations.
1.8.2 Laboratory Techniques
All the collective rock samples were cut and made into thin sections. Detailed petrographic
examinations were carried out under the polarizing microscope. Mineralogically, most of the
investigated rocks are carbonate-rich, i.e .Consisting of calcite and /or dolomite. Petrographic
distinction between calcite is not possible because of their almost identical optical properties.
Therefore, most of the collected samples were grounded and made into powder pallets for
running through the XRD machine for better understanding of their mineralogical
composition, especially the type of carbonate they contain.

2.1 Tectonics of North Pakistan
In Pakistan, the Indian and Eurasian plates are separated by the rocks of the Kohistan Island arc.
Kohistan was sutured to the Asian plate along the northern, or shyok, suture at about 100 ma
(Pudsey et al. 1985; Trelor et al. 1989) well before the onset of Himalayan collision, Himalayan
collision in Pakistan was thus between Kohistan and India with Kohistan Thrust southwards onto
the Indian plate along the Main Mantle thrust MMT, which is the true westwards continuation of
the Indus-Tsangbo Suture zone (Fig2.1).
2.2 The Himalayas
The Himalayas, consisting of a series of Enechelon mountain ranges with extensive intervening
valleys form a 2500 Km long and 160-400 Km wide mountain belt that extends along the
northern margin of the Indo-Pakistan crustal plate Continental collision of India with Eurasia is
believed to have formed this vast mountain range with a thick mass of Proterozoic casement
events. The geology of the Himalayas is the quite complicated (Kazmi& Jan 1997)
Continued convergence of the Indian plate with the Eurasian and other minor plates has
produced several distinct tectono metamorphic terrains to the south of the MMT from south to
north these include (Spenser 1993) .
1. The Sub Himalayas
2. The Lesser Himalayas
3. The Higher Himalayas
2.2.1 The Sub Himalayas
The sub Himalayas delimited to the north by the main boundary thrust (HBT) locally called the
Murree Fault. Geometrically, the fault plane cuts the steeply dipping molasse beds on its footwall
and carries northeast dipping lesser Himalayas schists and gneisses on its hanging wall.

2.2.2 The Lesser Himalayas
The Lesser Himalayas is composed of folded and thrusted rock formation ranging in age from
Pre-Cambrian to Eocene. It is delimited to the south by the Tertiary molasse along the main
Boundary Thrust and to the north by the Higher Himalayan crystalline rocks along the Main
Central Thrust. The metamorphism in this element is of very low to low grade.
2.2.3 The High Himalayas
The Tectonic limits of this sequence are represented by the Mylonites of the Main Central Thrust
zone at the base, and by the ultramafic rocks of the Ophiolitic melange and or of the root zone of
the Kohistan sequence along the MMT (Greco & Spencer 1993), it is a zone of Precambrian and
Mesozoic rocks metamorphosed during the climax of the Himalayan deformation. The
relationship between deformation and metamorphism is very complex in Higher Himalayas. The
rocks include marbles, metapelite, amplibolite, quartzite, ortho gneisses and para gneisses.
2.3 Geology of the Hazara Area
The Hazara area covers 2000 square miles in the southern foothills of the Himalayas between the
Jhelum River on the east and Indus River on the west. Rugged mountains and deep canyons
characterize most of the area altitude range from 11,00 fee near Turbella to more than 16,000
feet on the Kashmir divide; the Indus Siran Kunhar, Kishan Hangu and Jehlum river all flow in
deep gorges.
According to the tectonic subdivision outlined above, the Hazara area is a part of the lesser
Himalayas rocks of the Hazara area range from Precambrian to Quaternary in age (Table. 2.1)
and include sedimentary, igneous and metamorphic types (Calkins et al. 1975).

Fig 2.1 Geological map of Northern part of Pakistan (after Greco, 1991)
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Table 2.1: Stratigraphy of the Hazara Area.
Formation Age
Murree Formation Oligocene to Miocene
Kala Chitta Group Paleocene to Eocene
Kawagarh Formation Upper Cretaceous
Lumshiwal Formation Upper Jurassic to Lower Cretaceous
Chichalii Formation Upper Jurassic
Samanasuk Limestone Jurassic
Datta Formation Lower Jurassic
Mansehra granite Cambrian
Abbottabad Formation Cambrian
Tanawal Formation Cambrian
Hazara Formation Precambrian
Salkhala Formation Precambrian

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2.3.1 Salkhala Formation
The oldest know rocks in the Hazara region are the metamorphic rocks of the Salkhala
Formation of Precambrian age. This formation is widely exposed in the Balakot and Mahindra
areas the formation consists largely of quartz schist, marble, graphite schist and quartzo-
feldspathic gneisses
Quartz schist constitutes a large proportion of the formation chlorite and muscovite make up 20
to 40% of the schist and the remainder is quartz minor amounts of chinozoisite, garnet, magnetite
and biotite are present at places. Calcite or graphite as lamina and disseminated grains, appears
the schist adjacent to larger of marble or graphite schist.
2.3.2 Hazara Formation
The various names given to the thick widespread sequence of black and brown slate phyllite and
little metamorphosed graywacke include “Attack Slates” (Waagen et al. 1872) “Slates series of
Hazara” (Middlemiss, 1896) “Hazara Slate formation” (Marks and Ali, 1961). The Hazara
Formation occupies large parts of an accurate belt as much as 12 miles wide which together with
the overlying younger rocks, extends southwards from the vicinity of Ghari-Habibullah through
Abbottabad and then westward to Tarbela.
2.3.3 Tanawal Formation
The term Tanawal Formation is used for a sequence of quartzose schist that overlies the Hazara
formation in the area north and east of Tarbella Wynne (1879) originally named these rocks as
“Tanawal Group” Middlemiss (1896) called these rocks “Tanawal Quartizites” and believed that
they form the lower part of the overlying “Infra-Trias” or “Kingriaili Formation” in the area
between Sherwan and Indus river. The Tanawal Formation overlies the Hazara Formation and
underlies the Abbottabad Formation.
2.3.4 Abbottabad Formation
Marks and Ali (1962) proposed the name Abbottabad Formation for a part of the tightly folded
belts that extend from the northeast of Sirban Hill near Abbottabad, to Ghari Habibullah. Other

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main areas of its outcrop include the belts between (1) Sherwan and the Indus river. (2)
Muzaffarabad and Balakot and (3) the MandaKuchha syncline
2.3.5 Datta Formation
Waagen et al. 1972 were the first who observed the rocks of the Datta Formation on Sirban Hill
near Abbottabad. This formation is exposed in parts of the Kohat (Meissner et al . 1973 and Dera
Ismail Khan areas (Hemphill &Kidwai 1973), the Kala Chitta Hills and the Hazara area.
In the Hazara area, the Datta Formation consists of a thin but highly persistent sequence of red
and brown shale and quartzose beds that crop out in the tightly folded belt east and northeast of
Abbottabad.
2.3.6 Samana suk Limestone
The Samana suk limestone is in disconformable contact with the underlying Datta Formation the
Samana suk limestone is essentially clastic. This formation extends southward to Deraismail
Khan and eastward through Kohat and the Kalachitta Hills, as far as the Hazara area in the
Hazara region the Sammana suk Limestone underlies the Daulatmar peak and parts of the area
between Abbottabad and Ghari Habibullah.
2.3.7 Chichali and Lamshiwal Formations
The Chichali and Lamshiwal Formation are discussed together because they are not very thick in
the Hazara area in many places, the thickness of both these units is as less as 150 feet.
The Chichali and lamshiwal Formations have widespread distribution in Pakistan Exposure of
the rocks belonging to these units occur over a vast area that extends form DeraIsmial Khan ,
though Kala BaghKohat and Kala Chitta Hills, to Hazara.
2.3.8 Kawagarh Limestone
Although Waagen et al (1872) have noted the occurrence of Kawagarh Limestone in the Hazara
area such rocks have never been named or mapped as a separate unit the limestone occupies the
core of a south plunging synclinal structure which extends southward to Kakul. The Kawagarh
Limestone is thick to thin bedded and has a fine even grained nearly lithographic texture.

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2.3.9 Kala Chitta Group
The KalaChitta Group in Hazara ware known for many years as the Nummulitic Formation
Waagen et al (1872) used this name for the outcrops of formation limestone and calcareous shale
on Sirban Hill near Abbottabad.
A greater part of the Kala Chitta group composed of grey poorly bedded generally nodular
limestone and dark grey calcareous shale. The shale commonly contains nodules of clayey
limestone some of the beds are to a large degree bio-clastic containing abundant fossils,
especially Foraminifera.
2.3.10 Murree Formation
Wynne (1874) reported the occurrence of a sequence of red shale and sandstone found along the
foothills of the Himalayas. He turned these rocks as the “Mari Group” after the “Mari Hill
station” 35 miles northeast of Rawalpindi “Mari” is now spelled as Murree subsequent
designations for this sequence have been Murree beds (Lydekker& Richard 1876) and “Murree
series” (Pilgrim 1910 Wadia 1928) this unit is now known as Murree Formation by the
geological survey of Pakistan.
The Murree Formation consists of red, thinly laminated siltstone and shale, thick-bedded red
mudstone and subordinate green grey and maroon fine to medium grained grey wake most of the
Murree formation contains enough interstitial carbonate produce effervesce with dilute acid
2.3.11 Mansehra Granite
The name Mansehra granite was given by Shams (1961) to the non-foliated granite found locally
in and around the Mansehra town. He also distinguished a foliated granite which he called the
Hakale granite (Shams 1961) in a later paper Shams stated that these various granites are
genetically related differing only in their location and level of emplacement (Shams and Rehman
1966) in the Mansehra area of field has combined all the three varities into one unit called the
Mansehra granite and Of fields usage is followed here.
The Mansehra granite is believed to represent the southern fringes of the extensive granite
intrusions in the axial zone of the great Himalayas, That are known as “Central Himalayas

12
gneisses” (Stoliczka& Ferdinand 1865) Middlemiss (1896) termed the granitic rocks of the
Hazara area as “gneissose granites” These intruded rocks are of Cambrian age (cf. Mehmood &
Shah 1998) the Mansehra granite is highly foliated at Susalgali.
2.4 Mineral Deposits of Hazara
2.4.1 Iron Ore
Sedimentary iron and manganese deposits which are part of the red bed sequence of Cambrian
age, are found along a northeast trending belt that extends from Kabul through Galdanian to
Chure-Gali. Similar deposits just east of Abbottabad probably the southern extension of this
beds. Although the red bed sequence seems to be continuous between Kakul and Chure-Gali, i.e.
distance of eight miles it is of economic significance only at places because of wide variation in
its ore-forming elements.
Previous investigations include a brief study by Kleiber (1958) in connection with the survey of
iron resources of Pakistan, and a more detail study by Quraishi and Imam (1960) The Galdanian
area is underlain by a thick series of carbonate rocks and quartzites which trend northeast. At
least two red bed formations are intercalated in the carbonate-quartzite series, and one of them
contains significant concentrations of the iron and manganese mineral. The underlying dolomite
belongs to the Abbottabad Formation. Kleiber (1958) briefly examined the chure Gali area and
Quraishi and Abdullah (1960) mapped it is a considerable detail. The red bed sequence with its
manganese iron-rich beds at Chure Gali extends south westward for a known distance of three
fourths of a mile and they are very likely the northeastward continuation of the red-bed
formation at Galdanian. The stratigraphic sequence is broadly similar to that at Galdanian, i.e.
dolomite at the base followed by quartzite, then red bed and finally limestone at the top. The
occurrence of iron and manganese of economic interest is largely restricted to iron manganese
rich lenses mostly near the top of the red bed sequence.
Khan (1951) studied an iron rich formation just each of Abbottabad. It forms a linear zone
extending from Shekhal Bandi southwestward toward Mannum Gali i.e. a distance of about 3
miles. Except for the lack of dolomite the general fological setting is similar to the deposits at
Galdanian and ChureGali. The general strike of the beds is northeast and the formation may
correlate with that at Galdanian. The red bed sequence is about 60 feet thick and consists of

13
lenticular beds of hematitic siltstone and clay stone. The iron-rich beds are 7 to 30 feet thick.
Only the upper part of the red beds seems to be of ore grade Khan (1951) estimated 633,000 tons
of iron ore averaging 20 iron per feet of depth for the area studied.
A layer of hematite occurs near langrial which lies along the all-weather Haripur-Lora road
Northeast from Langrial the hematite layer extends in a discontinuous fashion for 16 miles to
point near Kalabagh cantonment. Continues Lenses moderately rich in oolitic hematite are
scattered along a partly red zone which is a much as 100 feet thick at places
2.4.2 Phosphate
Deposits of phosphorite occur in the Kakul Mirpur area, which I located at a distance of 9.5 km
to the north of Abbottabad. These deposits are spread our an area of 13 km. the main and most
promising deposit is located near the Kakul village (Nasir at al 1989).The area containing the of
slightly metamorphosed sedimentary rocks of Cambrian age. These include sandstone limestone
dolomite greywacke quartzite conglomerate shale phyllite and siltstone of the Abbottabad
formation.
2.4.3 Mangnesite Deposits
Deposits of mangnesite are being mined around the Kumhar village lies to the west of
Abbottabad .The grey dolomitic limestone of the Abbottabad formation hosts the Kumhar
mangnesite deposit. As many as 14 mangnesite lenses of different sizes have been so far
discovered in the area (Alam 1972).
2.4.4 Soapstone
Deposits of soapstone occur in area around Sherwan. Most of the deposits are confined to the
dolomite member of the Abbottabad Formation Soapstone forms irregular bodies in host rock
(Tayyab et al. 1964). Only the small showing at Haripur is in quartzose rocks of the Tanawal
Formation. A detailed investigation of some of these deposits in the major objective of the
current studies. The details regarding their geological setting and other Characteristics are
included in the chapters 4-5.

15
3.1 General Statement
As mentioned in the chapter on introduction the present studies deal with the soapstone deposits
of the Sherwan area Hazara Sherwan is located at a distance of 35 km to the northwest of
Abbottabad. The study area consists of different types of lithologies which constitute the
following three formation (Alam 1972) and shown in Table 3.1.
o Abbottabad Formation
o Tanawal Formation
o Hazara Formation
3.1.1 Hazara Formation
This formation is of Precambrian age ( Shah 1977) underlying the Tanawal Formation it
dominantly consists of slate and phyllite with minor amounts of metamorphosed limestone and
carbonaceous layers slate and phyllite are green to dark green and black but are rusty brown on
weathered surfaces (Fig.3.1). Some thick bedded fine to medium grained sandstone is also
present limestone beds and a sequence of phyllite and gypsum are found in the southern parts of
Hazara and Kashmir within this formation lendicular bends of carbonaceous matter have been
converted to graphitic schist because of low to medium grade metamorphism.
Fig: 3.1 Hazara Formation

16
3.1.2 Tanawal Formation
This formation consists mainly of quartzone schist quartzite and schistose conglomerate it is well
exposed along the southern and southeastern margin of the Mansehra granite and in a narrow belt
to the northwest to the south of Mansehra granite, the Tanawal Formation mainly consists of
medium grained quartzite and fine grained mica schist (Fig. 3.2). The Tanawal Formation
underlies the Abbottabad formation and overlies the Hazara Formation (Shah 1977)
At quite a few places e.g just south of Abbottabad along the Haripur-Abbottabad road, the
Tanawal Formation is missing and the Hazara Formation directly underlies the Abbottabad
Formation the Contact between the Abbottabad Formation and a boulder bed known in the
literature as Tanaki boulder bed (Calkins et al. 1969) Habibullah, lower contact of Tanawal
Formation with the underlying Hazara Formation seems to be gradational and marked only by a
lithological change from slate below to quartzite above. In the northeastern Salkhala Formation
along an unconformity. The thickness of Tanawal Formation is difficult to measure due to
structural complications.
The Tanawal Formation is devoid of fossils. However, from the contact relationship discussed
above, it follows that the Tanawal Formation in younger than the Hazara Formation but older
then the Abbottabad Formation. Therefore the Tanawal Formation is most probably late
Precambrian in age.
Fig:3.2. Tanawal Formation

17
3.1.3. Abbottabad Formation
The Abbottabad Formation consists mainly of dolomatic limestone quartzose sandstone and
shale with many lithological changes and interchanging facies from place to place (3.3). For
example in the Turbella area the main constituents of the formation are thin shale and
conglomerate at the base it followed upward by quartzose sandstone dolomite and again
quartzone sandstone which caps the formation in the Abbottabad area, the lower shale unit is
replaced by conglomerate followed by alternating is overlain by quartzone sandstone followed
upward by alternating dolomite and limestone. The Sherwan soapstone deposits occur within the
Abbottabad Formation.
In the Sherwan area the Abbottabad Foramtion is in unconformable contact with the underlying
Tanawal Formation Locally the presence of a boulder bed marks the unconformity. Elsewhere
however only a lithological change marks this contact. In the eastern part of southern Hazara
across the Punjal fault, the Tanawal Formation is missing and the Abbottabad Formation rests
unconformable over the Hazara Formation. The thickness of the formation is above 6,00 meters
at the type section near Abbottabad. The age assigned to it is lower Cambrian (Latif 1974).
Fig 3.3 Abbottabad Formation

18
Table 3.1: Stratigraphy of the Sherwan Area (Muhammad 1993)
Age Formation Lithology
Late Precambrian Tanawal Quartzite, schist, quartzite & phyllite
`Lower Combrian Abbottabad
Dolomitic limestone , freshy coloured
quartzose sandstone Thin bedded
limestone & quartzose sandstone
Trust Fault
Late Precambrian Tanawal Phyllite, quartzite, schist & quartzite
Unconformity
Precambrian Hazara Slates
3.2 Description of lithological units of the Abbottabad and Tanawal formation
Sherwan area.
The following is a detailed account of the various rock units, which are exposed in the Sherwan
area. They belongs to the Tanawal and Abbottabad Formation (Alam 1972).
3.2.1. Quartzite
Striking NEN to SWS and dipping northwest its southeastern most extremity can be traced near
the village SindhoGali, 15 mile stone along the Abbottabad Sherwan road at places due to
weathering the pinkish and yellowish brown tints. The quartzite is fine to medium grained
granular and commonly xenoblastic to hypidoblastic. The larger grains are most of quartz while
the smaller grains are of feldsper and mica it is medium bedded and exhibits prominent cross
bedding. Locally the quartzite is highly fractured and jointed.

19
3.2.2 Phyllite
The phyllite strikes in the NEW to SWS direction and dips at an angle of 45 towards NW
phyllite overlies the quartzite but due to its pinching and swelling character the contact with
quartzite is not persistent and at places which changes into light brown colour on weathered
surfaces, it is sandy in nature and occasionally very thin of quartz are encountered running
irregularly, phyllite is very fine grained hard but not very compact mostly it is thin bedded to
laminated and shows platy structure. Fractures are developed oblique and nearly perpendicular to
the bedding laminations.
3.2.3 Dolomitic limestone
As mentioned above the dolomatic limestone occurs above the phyllite unit and where the latter
is missing it is directly in contact with the underlying quartzite. Generally the dolomatic
limestone strikes in the NEN to SWS direction and dips.
Dolomitic limestone strikes in the NEN to SWS direction and dips at 46 to 50 towards north.
This unit mainly consists of limestone with thin interbeddings of shale phyllite. The limestone is
light grey in colour. It is fine grained and argillaceous in nature. Thin irregular veins of calcite
are also developed. Mostly the in it under discussion is thin to very thin bedded and highly
fractured and jointed the fracture and units are at places so close that they break the limestone
into small pieces.
3.2.4 Freshly-Coloured Quartzose Sandstone
Overlying the thin-bedded limestone this marker unit is readily recognizable in the field due to
its peculiar colour and granularity. It trends in the NEN to SWS and dips at 46 to 51 toward
northwest. Quartz is the major constituent of the unit and, at place thin {up to 6 think} veins of
quartz also occur. This sandstone is coarse grained. Mostly it is medium bedded, hard and
compact. Fracture and joints are scarce. Thickness of this unit ranges from 5 to 20 feet.

Chapter No 4
Economic Deposits of Sherwan

4.1 Soapstone deposits of Sherwan
In the area around Sherwan, soapstone constitutes an important type of the lithological unit that
constitute the Abbottabad Formation. The Sherwan soapstone deposit are distributed in a n 80 w
Trending, 10x1-1/2 miles belt, which stretches from Bundi to Kangar Dhaka on the western side
of Siran River All the important soapstone deposits are restricted to the dolomite unit of the
Abbottabad Formation within the Sherwan syncline. Only one small showing at Hariala, 2 miles
southeast of Sherwan, occurs in association with a quartzose rock of the Tanawal formation.
Dolomite makes up 10% to 50% of the mined material which is easily removed through band
sorting at the mine portal. Most of the Sherwan soapstone production comes from the following
mines
 Bandi Mines
o Chelethar Mines
o KhandaKhu Mines
o Panjkulian Mines
o Kharan Mines
Four mines from three of the areas, listed above, are located within the study area and are
important in terms of their reserves and production. These are briefly described below:
4.1.1 Bandi Mines
The Bandi Mine is located about a quarter of a mile south of Bandi village, and 3 miles
southwest of Sherwan . An unmetalled 3 miles king road connects the mine with Hal village. The
mine is presently producing about 10 tons of soapstone per day.
The mine area is underlain by a thick sequence of bedded dolomite, which strikes N80 E and
dips 70 NW. A large body of massive pale green soapstone 50 feet thick is oriented parallel to
the bedding. No fault are noted in the mine area.
The soapstone body has been intersected by the adits and, therefore, has a proven length of 50
feet vertically, the body extends at least from level of the mine adit up dip to the surface, a
distance of about 100 feet but assuming a thickness of 10 feet, a trapezoidal body of soapstone
weighting 39,000 tons is blocked out. A part of it has been mined out from the existing workings
(Tayyabet al.1964).

4.1.2 Chelethar mines
The mine is four to ten km east of chelether village access is by road an area of about 200 acers.
Underground working of the mine consist of two adits driven into the hillside and connected
inside by a cross drift. Small cuts have been given off the drifts. The soapstone body dips almost
vertically and trends about N70W. it is about 100 feet thick (Fig.4.1 &4.2) .
Fig.4.1 First mine at Chaleter
Fig.4.2. Talc deposit in Chaleter mine.

4.1.3 Khandakhu mine No 1
This khandakhu mine is located quarter of a mile southwest of khandakhu village, just north of
the main trail accessible by a good road to village. The surface cut was open on a vertical vein of
good quality, creamy white soapstone as much as 14 feet thick (Fig.4.3). The vein appears to end
abruptly against sandstone at the eastern end of the cut and is 4 feet thick at the western end of
cut. Fracture cleavages parallel to the vein are common in the dolomite. The fault or shear, which
localizes the vein has little or no vertical displacement at the surface and is market by a 6 inches
thick zone of dolomite breccia with a rusty weathering siliceous matrix (Tayyab et al. 1964).
Fig.4.3.Shaft Mine at KhandaKhu
4.1.4 KhandaKhu Mine No 2
Another soapstone is half mile southwestern of KhandaKhu, and a quarter of mile southwestern
of mine area # 1 .access is by good road (Fig.4.4). The mine consists of gently dipping dolomite

and quartzose sandstone beds, fracture zone and closely spaced joints. The strike of the bedding
at the outcrop is N800
W and dip 84NE (Tayyabet al.1964).
Fig.4.4.Tunnel of shaft mine at KhandaKhu No 2.

Chapter No 5
Petrography and XRD

5.1 Petrography
Talc dolomite and quartz can be recognized in thin sections of soapstone. Talc in these thin
sections is very fine grained and are most colourless in plane polarized light. The relatively
coarser variety of talc is very flaky and fibrous displaying spherulitic appearance. In most of
cases talc replaces dolomite at the edge of the grains of dolomite forming a closed network of
replacing veins and can be considered as stock work. Cross cutting relationship between the
replacing talc and the host dolomite can also be identified. The replacement of the coarse grain
dolomite with fine grain talc along the fractures and at the edges of the dolomitic grains indicate
the hydrothermal activity in the area. It seem that silica rich hydrothermal fluids of possible
granitic origion may have replaced dolomite with the following reaction.
Dolomite +silica +water talc + calcite+ carbondioxide
3ca Mg (SO3)2 +4SiO2+H2O Mg3Si4O10 (OH) 2+3CaCO3+3CO2
No deformational phases are metamorphic events have been observed in these thin sections,
however the coarser flaky and fibrous variety of talc could be formed during metamorphism . we
would like to note here that the talc, pyrophylite closely resemble with muscovite and it is very
hard to distinguish among them in the thin section. Since, muscovite and pyrophyllite have been
not reported by XRD result. Therefore we assume the fibrous and flaky variety is a
metamorphosed talc.
Because of fine grain nature of the talc it is very difficult to distinguish between talc and
dolomite.Talc can also be formed via a reaction between dolomite and silica, which is typical of
skarnification of dolomites via silica-flooding in contact metamorphic aureoles;
Dolomite + silica + water talc + calcite + carbon di oxide
3CaMg + 4Si + M 3CaC + 3C
5.2 X- Ray Diffraction:
Mineralogically, most of the investigated rocks are carbonate-rich, i.e . Consisting of calcite or
dolomite. Petrographic distinction between calcite is not possible because of their almost

identical optical properties. Therefore, most of the collected samples were ground and made into
powder pallets for running through the XRD machine for better understanding of their
mineralogical composition, especially the type of carbonate they contain. The XRD data are
presented in the Table 5.1.The XRD pattern of the samples is illustrated in Fig. 4.2-4.6. Most of
the peaks belong to magnesite and dolomite whereas the others belong to some minor minerals.
This confirms the occurrence of magnesite and dolomite in the investigated area.
Table 5.1. Result of XRD
Sample No Minerals Formulas
1 Talc Mg3Si4O10(OH)2
2
Silicon oxide, SiO2
Dolomite CaMg(CO3)2
Fig.5.1 XRD of Sample No 1

Chapter No 6
Discussion and conclusion

27
6.1 Discussion and Conclusion
A detailed survey of the general geological occurrences, field/ textural relationships, lithological
association and detailed reading of the relevant published literature suggests that talc; the most
abundant constituent of Soapstone deposit, can originate in three different ways:
1. Alteration and metamorphism of pre-existing ultramafic rocks lead to the formation of talc-
rich assemblages. Hydration of the originally ultramafic rocks (e.g. Dunite) produces
serpentinite rocks dominantly composed of serpentine. Assuming olivine as reactant, the
relevant chemical reaction for serpentinization would be:
(Mg, Fe)2 SiO4 + H2O Mg3Si2O5 (OH)4 + Fe3O4
(Olivine) (Water) (Serpentine) (Magnetite)
A further addition of carbon dioxide would convert the serpentinite formed as a result of the
reaction, mention above into a talc-magnesite assemblage according to the following reaction:
2Mg3Si2O5(OH)4 + 3CO2 Mg3Si4O10(OH)2 + 3MgCO3 + 3H2O
(Serpentine) (Talc) (Magnesite)
Depending upon the composition of the fluid phase and total pressure, the equilibrium
temperature for such a reaction vary between 300 C and 550 C (Greenwood 1967; Evans &
Trommsdorff 1974). According to Johannes (1969), at a fluid pressure of 2 Kb, the
asseblages talc + magnesite is stable between about 350C and 550C and at 7Kb about 490C
and 660C. The result of recent studies (e.g Schandl & Naldrett 1992; Schandl & Wicks
1993), however, show that the talc-carbonate and quartz-carbonate assemblages may also
originate at slightly lower temperature (250-300C). It follows, therefore, that the talc-
magnesite assemblages may form in the temperature range of 250-550C.
2. A largely isochemical prograde metamorphism of a suitable sedimentary precursor, i.e
Siliceous dolomite may also yield talc-bearing rocks:
3CaMg(CO3)2 + 4SiO2 + H2O Mg3Si4O10(OH)2 + 3CaCO3 + 3CO2
(Dolomite) (Quartz) (Talc) (Calcite)

28
Metamorphic conditions for such a reaction are assumed to be 400-500C temperature and 2-
5 Kb pressure (Puhan 1983).
The formation of talc is limited, since Mg-trioctahedral montmorillonite forms rather than
talc when either the solids to water ratio is low (4g/l.) or the gas pressure is low (Pco2= 1
bar).
3. Talc-rich assemblages may also form as a result of metasomatism of pre-existing reactive
rocks by fluids containing appropriate chemical components, for example, when siliceous
hydothetrmal solutions invade a dolostone. The relevant reaction will be essentially the
same as given for case 2 above. The only difference being the source of silica, which is
indigenous in case 2, but extraneous in case 3.
Since the investigated soapestone deposits are intimately associated with sedimentary rock
and, perhaps even more importantly ultramafic rock are totally lacking in the Sherwan area
the first possibility for these genesis is not applicable. In other words, only the last two
mechanisms may be considered to explain the genesis of the Sherwan soapstone.
Petrographic features and minerological composition of the country rocks and of the
deposits themselves also suggest a greater probability of the second and third genetic
models, mentioned above.
The carbonate country rocks display features, that suggest they have under gone prograde
metamorphism. These include (i) Marbel-like sugary texture (ii) Development of Phisibility
and (iii) The presence of minerals.
4. The coarse grained flaky and fibrous varity of talc along with spheralitic talc indicate a
metasomatic origin. Moreover muscovite and talc closely resemble and cannot be
distinguished in the thin section. Furthermore, the attitude of at least some of the studied
Soapstone bodies is concordant with that of a country rocks and, therefore, their formation
cannot be attributed to a metasomatic phenomenon, which is likely to produce discordant
rather than concordant bodies. Hence the source of silica for such concordant Soapstone
bodies seems to be indigenous. There are two further possibilities:(i) The Silica either comes
from the parent rocks, i.e it was a siliceous Dolomite.(ii) The precursor was a relatively pure

29
Dolomitic rock that reacted with the adjacent quartose beds during metamorphism to form
the Soapstone deposit.
Since some of the talc cross cut the country rock. So the cross cutting relationship with host
rock, stockwork appearance of the talc and the formation of talc along the grain boundaries
all, envisages that some talc is metasomatic in origin or in other words hydrothermal
alteration has reconsolidated the talc deposits at places. As pointed out in the third chapter,
some of the Soapstone occurs as veins (fracture-fills) or is distributed along shear and
brecciated zones within the dolomitic member of the Abbottabad Formation. This type of
soapstone mineralization is definitely epigenetic and the source of silica in this particular
case must be external or of possible granitic origin.
From the discussion given above, it follows that the Sherwan Soapstone deposits include
two different genetic types, i.e (1) Syngenetic and (2) Epigenetic. The syngenetic deposits
probably represent either metamorphosed Siliceous dolomitic rocks or metamorphic
reaction zones between adjacent dolomitic and quartitic beds. The epigenetic class include
deposits, owe their origin to a metasomatic activity in the study area.

30
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