salt range

Muhammad Waqas MansooriDepartment Of Geology, UOP.

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FIELD REPORT ONSalt Range

SUBMITTED TO:Mr. Haneef

Mr. Naveed Anjum

SUBMITTED BY:Muhammad WaqasBS (Part-2)Geology

Class No. 27

DEPARTMENT OF GEOLOGYUNIVERSITY OF PESHAWAR

(2008-09)


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.INTRODUCTION

The name of Salt Range was first use by ELPHISTON in 1813. The name isderived from the fact that area contains huge reserve of the common table salt.

The East-West trending fold belt compises the low rolling hills and valleys of theuplifted Kohat-Potwar Plateau, The Salt Range and its Westward extensions. It is 85 kmwide and extends for about 200 km. It is a discrete structural zone bounded in the northby the north-dipping Main Boundary Thrust (Sarwar et al. 1979; Yeats et al. 1984; Cowardet al. 1985). Southward the Salt Range Thrust, Kalabagh Fault and the Surghar Thrustfrom its southern boundary. West and eastward it is terminated by the N-S orientedKurramThrust and Jehlum Fault respectively (Kazmi and Raza 1982).

The Salt range is mainly divided into two parts. The area to the east of the riverIndus “Main Salt range” or “Cis-Indus Salt range” and the area to the west of river Indusis called “Trans-Indus Salt range”. The main Salt range is further divided into three parts:

Western Salt Range Central Salt Range Eastern Salt range.

Eastern Salt range is about 16km and its height about the sea level is 760m. Thewestern range is widens westward to the width of about 32km with highest attitude of1422m at Sakesar. Similarly central Salt range is more wider than eastern and western Saltrange.

The rocks in the Salt ranges are generally folded and are typically marked by largeand small scale faulting as well as local over-thrusting with movements towards south. Asedimentary sequence ranging from Pre-Cambrian to Recent is exposed in the Salt Range.It is also marked by several unconformities.

The Salt Range is essentially a complex salt anticlinorium. The Eocambrianevaporites are exposed in some of the over-folded and faulted anticlines. Along itssouthern margin, the Salt Range Thrust has pushed the older rocks of the Salt Range overthe less deformed Tertiary sequence of the south-lying Jehlum plain. Subsurface geo-physical data shows that the Salt Range and Potwar Plateau are underlain by a decollementzone within Eocambrian evaporites. The Salt Range is thus the surface expression of theleading edge of a decollement thrust (Lillie et al. 1987).

In our field visit, we have visited eastern and western Parts of Salt Range. In theEastern Salt range, we studied the Khewra Gorge, while in the western Salt range westudied the Nammal Gorge and Zaluch Nala section. We have studied the stratigraphy anddetailed lithology of the various formations exposed in the above said Gorges.


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STRATIGRAPHY OF THE REGION

The Salt Range rocks stratigraphic unit range in the age from Pre-Cambrian to theTertiary with the marked absence of Ordovician, Silurian, Devonian and Carboniferousage throughout the region.

Locally a given stratigraphic rock sequence pinches out laterally to the point ofvanishing e.g Mesozoic sequence is well developed in the western salt range and Trans-Indus ranges but the Triassic and Jurassic and perhaps all the cretaceous formations areconspicuously absent in the most of the central and eastern Salt range.

We have visited the following three Gorges in the Salt range during our field tothat region: Khewra Gorge (Eastern Salt range) Nammal Gorge (Western Salt range) Zaluch Nala (Western Salt range)

The description and Stratigraphy of the above three Gorges are explained as:


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VARIUOS GROUPS OF FORMATIONS THAT WE HAVE STUDIED INTHE SALT RANGE.

JEHLUM GROUPAge: CambrianFormations:

Baghanwala Fm.Jutana Fm.Kussak Fm.Khewra S.St.

NILA WAHANGROUP

Age: Early PermainFormations:Sardhai Clays.Warcha S.St.DandotFm.Tobra Fm.

ZALUCH GROUPAge: Late Permian

Formations:Chiddru Fm.Wargal L.St.Amb Fm.

SUR GHAR GROUPAge: Jurassic-Cretaceous

Formations:Lumshiwal Fm.Chichali Fm.

BAROUCH GROUP:Samana Suk Fm.

Shinwari Fm.Datta Fm.

MUSA KHEL GROUPAge: TriassicFormations:Kingriali Fm.Tredian Fm.Mianwali Fm.

MAKARWAL GROUPAge: PaleoceneFormations:Patala Fm.

Lockhart FmHangu Fm

RAWALPINDI GROUPAge: MioceneFormations:Kamlial Fm.Murree Fm.

SIWALIK GROUPAge: Miocene-Pliestocene

Fomations:Soan Fm.

Dhok Pattan Fm.Nagri Fm.Chinji Fm.

CHERAT GROUPAge: EoceneFormations:Chorgali Fm.Sakesar Fm.Nammal Fm.


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KHEWRA GORGE

Khewra Gorge is present in the Eastern Salt Range. It is located about a distanceof 1km from the Khewra town, After this town it is named as Khewra Gorge. “KhewraGorge is known as the Museum of Geology.”

In this Gorge we have studied, Salt range formation which is of Pre-Cambrian age,Jehlum group rocks which are of Cambrian age, it includes Khewra Sandstone, Kussakformation, Jutana formation and Baghanwala formation.

Disconformity (major) between Baghanwala formation and Tobra formation iscalled Permo-Cambrian unconformity.

SALT RANGE FORMATIONNOMENCLATURE:

Wyyne (1878) named this formation as “Saline Series”, Gee (1945) called the sameunit “Punjab Saline Series”. The Present Name “Salt Range Formation” has beengiven by Asrar Ullah(1967).

TYPE LOCALITY:Khewra Gorge in eastern Salt Range.

THICKNESS:The thickness of Salt Range Formation is more than 800m at type locality.

LITHOLOGY:The lower part of the formation comprises beds of marl and gypsum with

bitminous shales and dolomites. The base of the formation is not exposed. The middlepart of the formation contains an alternation of gypsum, dolomite, shale, siltstone with oil-shale layers, particularly in the western Salt Range. The top of the formation is formed by agypsum layer containing high-grade oil-shale or a layer of highly altered volcanic rockknown as Khewra Trap.

The Salt Range has been divided into three mambers; Billianwala Salt Marl Member: It is largely compsed of hematitic, dull red,

gypsiferous marly beds with thick seams of salt. Its base is not exposed. Bhandar Kas Gypsum Member: It is comprised of massive gypsum,

dolomite and marl.It overlies the Billianwala member. Sahiwal Marl Member: This member overlies the Bhandar Kas Member

and is comprised of an upper bright marly unit and a lower unit containingdull red marls.

CONTACTS: Lower contact of the Salt range formation is not exposed. Upper contact with the Khewra sandstone is conformable.

AGE:The Salt Range has assigned the age of Late-Proterozoic.

ENVIROMENT OF DEPOSITION:Environment of deposition is restricted basin condition with high rate of

evaporation and climate is hot and arid.


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Salt Range Formation

KHEWRA TRAP:The Salt Range contains thin flows of an ultrapotassic rock. Commonly known as

Khewra Trap. It is purple, reddish brown, orange to buff, rarely dark green rock.It is frequently mottled very fine-grained, porphyritic and vesicular to

amygdaloidal.The phenocrysts are euhedral to skeletal spinifex, and commonly grownradially. The Khewra Trap is so unique that Mosebach (1956) assigned it a new name-Khewrite.

KHEWRA SANDSTONEKhewra formation is the first member of the Jehlum group. Jehlum group

represents the Cambrian strata of the Salt range.HISTORY:

“Khewra group” by Noetling (1894), “Purple Sandstone Series” by Wynne (1878)is named as “Khewra Sandstone” by Fatmi (1973). Khewra Gorge is the type locality ofthe Khewra sandstone.

LITHOLOGY:This formation mainly consists of sandstone. Sandstone is thin to thick bedded and

the color is purple to brown or yellowish brown. Massive sandstone is also present whichis of maroon color. The grain size of the sandstone is also varying in this formation. Fewintercalations of brown shale are also present.The Sandstone is characteristically cross-bedded.

THICKNESS:


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The Khewra sandstone is widely distributed throughout the Salt range and Khisorrange. The thickness of this formation 150m at the type locality in Eastern Salt Range and80m in the Khisor Range.

CONTACTS: Lower contact is conformable with Salt Range Formation. Upper contact with Kussak formation is gradational and conformable.

AGE:Khewra sandstone hass assigned the early Cambrian age.

Ripple Marks in Khewra Sandstone

Ball and Pillow Structures in Khewra Sandstone


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KUSSAK FORMATIONIt is the second member of the Jehlum group.

HISTORY:Obolus beds of “Wynne” (1878), neobolus beds of “Wyyne” (1885), Kussak group

of “Noetling” (1894) is now named as Kussak Formation by the Stratigraphic Committeeof Pakistan.

TYPE LOCALITY:Kussak Fort (Eastern Salt Range).

LITHOLOGY:Kussak formation consists of greenish to dark grey color shale, sandwiched

between upper and lower grayish sandstone and siltstone member. Sandstone ismicaceous, gray in color and fine to medium grained. This color is due to the presence ofglauconitic and iron sulphide. Silt stone is mainly thin bedded while sandstone is mediumbedded with few dolomite beds.

According to Pascoe (1959), at the base of Kussak Formation there is a veryregular and characteristic grit and conglumerate not more than a foot thick. Theconglumerate consists of a matrix of well-rounded, medium to coarse sand grains ofyellowish brown colour, in which are embedded rounded pebbles of white and yellowishquartzite, dark grey-green and black slate and dark quartzite.

This conglumerate is almost parallel and represent a time gap, Para-conformity.ENVIRONMENT OF DEPOSITION:

Environment of deposition of Kussak formation is continental shallow marineenvironment.

THICKNESS:Kussak formation is widely distribution the Salt range. It varies in thickness form

25ft to 71ft.CONTACT:

Lower contact with underlying Khewra Sandstone is conformable. Upper contact with overlying Jutana Dolomite is conformable.

FOSSILS:The fossils which are found in this formation are brachiopods, trilobites’ trails,

Granulata, Redlichia etc.AGE:

Middle Cambrian age.DEPOSITIONAL ENVIRONMENT:

Marine depositional environment.


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Kussak Formation

JUTANA FORMATIONIt is the third member of the Jehlum group.

HISTORY:The magnesian sandstone beds by “Fleming”, Jutana stage by “Noetling” (1894), is

called as Jutana formation by the Stratigraphic Committee of Pakistan.TYPE LOCALITY:

Near Jutana Village, in Eastern Salt Range.LITHOLOGY:

This formation mainly consists of yellowish white or cream colored, partly sandydolomites and dolomitic sandstone with few shale intercalations. Dolomite is thin to thickbedded and in the upper part it is also massive and brecciated. Fractures are also present inthe dolomite.

THICKNESS:Its thickness is 75-90m in Eastern Salt Range and 45m in Khisor Range.

CONTACTS: Lower contact is conformable with underlying Kussak formation. Upper contact is conformable with overlying Baghanwala formation.

FOSSILS:The fossils which are found in this formation are brachiopods, Gastropods and

trilobites.AGE:

Early to Middle Cambrian age.BAGHANWALA FORMATION

It is the fourth and last member of the Jehlum group.HISTORY:


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“Psuedomorph salt crystal zone” by Wynne (1878), “Baghanwala group” byNoetling (1894) is now called as Baghanwala formation by Stratigraphic committee ofPakistan.

TYPE LOCALITY:Near Baghanwala village, in Eastern Salt Range.

LITHOLOGY:The Baghanwala consists mainly of reddish-brown shales and platy to flaggy

sandstone characterised by an abundance of Salt Pseudomorphs. Ripple marks and mudcracks are common.

Salt Pseudomorphs in Baghanwala Formation

ENVIROMENT OF DEPOSITION:Environment of deposition of this formation is Non-marine, lagoonal and arid

environment.THICKNESS:

Thickness of this formation in the type locality is 100-116m while in the Khewragorge its thickness is 40m.

CONTACTS: Lower contact with Jutana formation is conformable Upper contact with Tobra formation is Unconformable.

AGE:Age assigned to this formation is Middle Cambrian.


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Baghanwala Formation

DISCONFORMITY BETWEEN BAGHANWALA AND TOBRAFORMATIONS: (Permo-Cambrian Boundary)

This boundary lies between Baghanwala formation of Cambrian age and overlyingTobra formation of Permian age, while whole remaining sequence of Ordovician, Silurianand Carboniferous ages are missing between the two formations indicating a large time gapas it is a major unconformity (Disconformity). At that time where there was a period oferosion and/or Non-deposition. It is also known as “Permo-Cambrian Unconformity”.


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NAMMAL GORGE

Nammal Gorge is present in the western Salt range. It is located close to theMianwali-Rawalpindi highway. There is a small town called Nammal nearby, so this gorgeis called as Nammal Gorge.

In this Gorge we studied: ZALUCH GROUP rocks which are of Upper Permian age. It includes Amb

formation, Wargal limestone, and Chiddru formation. The Permo Triassic Boundary between Chidru formation and Mianwali

formation. MUSA KHEL GROUP rocks which are of Triassic age. It includes Mianwali

formation, Tredian formation, and Kingriali formation. SURGHAR group rocks which are of Jurrasic and Cretaceous age. It includes

Datta formation, Shinawri formation, Samana Suk formation, Chichalli formation,Lumshiwal formation and Kawagarh formation.

K.T boundary or Cretaceous-Triassic boundary. MAKARWAL GROUP rocks which are of Paleocene age. It includes Hangu

formation, Lockhart formation and Patala formation. CHERAT GROUP rocks which are of Eocene age. It includes Nammal

formation, Sakesar formation and Chorgali formation.

AMB FORMATIONIt is the first member of Zaluch Group. Zaluch group represents the Upper

Permian strata of the Salt range.HISTORY:

“Amb sandstone beds” by Waagen (1891), “Amb formation” by Teichert (1966) isnow called as Amb formation by stratigraphic committee of Pakistan.

LITHOLOGY:This formation consists of thin to medium bedded sandstone and limestone. Thin

beds of shale are also present. In some portion limestone and sandstone are mixed. Whenlimestone is less then sandstone, then it is called as Limy sandstone. Limestone is light greyon fresh surface and grey to brown on weathered surface. Fractures are also present inlimestone. Thin layers of organic shale are also present in this formation.

ENVIROMENT OF DEPOSITION:Environment of deposition of this formation is Shallow marine to palludal.

THICKNESS:This formation is well developed in the western Salt range and thin out east wards.

Thickness of this formation is 80m in type locality and 47 m in Khisor range.CONTACTS:

Upper contact with Wargal limestone is conformable lower contact with Sardhai formation is also conformable but not present

in the Nammal gorge.FOSSILS:

This formation is highly fossiliferrous. Amb Formation contains abundant floralremains, including Glossopteris and Gangamopteris and a rich fauna including


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foraminifera, bryozoans, brachiopods, pelecypods, gastropods, cephlopods and ostrocods.The fusilinids Monodiexodina Kattaensis and Codonofusiella laxa are important.

AGE:Due to presence of these fossils the age assigned to this formation is Upper

Permian.

WARGAL LIMESTONEIt is the second member of the Zaluch group.

HISTORY:“Wargal group” by Noetling (1901), “Middle Productus limestone” by Waagen

(1879), is now called as Wargal limestone by stratigraphic committee of Pakistan.LITHOLOGY:

The Formation mainly consists of grey, medium or thick bedded to massive, partlysandy limestone and dolomite with few, thin intercalations of dark-grey to black shale.

It is easily recognisable from a distance because of its cliff-forming massivelimestone.

ENVIRONMENT OF DEPOSITION:The paleoenvironment is interpreted as generally shallow marine, with the

exception of few strata which might have been deposited under deep water conditions.THICKNESS:

This formation is well distributed in the Salt range and Khisor range. Its thicknessin Zaluch Nala is 182m.

CONTACTS: Lower contact with Amb formation is sharp and conformable Upper contact with Chiddru formation is also transitional and

conformable.FOSSILS:

This formation is highly fossiliferous. Various fossils found are Brachiopods,Gastropods, Ammonoids, trilobites etc. Index specie Productus (brachiopod) is also foundabundantly in this formation.

AGE:Due to presence of these fossils age assigned to this formation is Late Permian

(Late Murgabian to Early Dzhulfian).


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Fossil fragments in Wargal Limestone

CHIDDRU FORMAITONThis formation is third member of Zaluch group.

HISTORY:“Chiddru beds” by Waagen (1891), “Chiddru Group” by Dunbar (1932) is now

called as Chiddru formation by the Stratigraphic Committee of Pakistan.LITHOLOGY:

It consists of dark-grey sandy shales at the base, overlain by calcareous sandstoneand sandy limestone. The top of the formation is formed by a characteristic whitesandstone layer as muchas 5m thick.

ENVIRONMENT OF DEPOSITION:Environment of deposition of this formation is shallow marine, littoral to palludal.

THICKNESS:This formation is well distributed in the western Salt ranges and Trans Indus

ranges. Its average thickness at the type locality is 64m.CONTACTS: Lower contact of this formation with Wargal limestone is conformable and

transitional. Upper contact with Mianwali formation is disconformable.

FOSSILS:The Chiddru Formation contains abundant brachiopods and gastropods, and

subordinate microfossils.AGE:

Due to the presence of these fossils age assigned to this formation is Late Permian.

THE PERMO-TRIASSIC BOUNDARY(The passage of Marine Permian to Marine Triassic)


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The Permian rocks located in the Salt Range have richness of fauna and havingrelationship with the rocks of Triassic system, the strata near the Permo-Triassicboundary are marine and having conformable relationship but there is significant breakin the fauna at the contact.Kummel and Teichert in 1966 referred to the body as Paraconformity showing sub-Arial exposure at the end of the Permian time. In support to this view, they thoroughlystudied the contact throughout the Salt range to find out the lithological and texturalchanges across the boundary. Their wotk is briefly summarized as under.

The upper most lithological unit of Chiddru formation is sandstone bed called aswhite sandstone bed. The sandstone is fine to medium grained, thinly bedded withinterbeds of shale while the upper contact with Kathwai member of Mianwaliformation is dolomite.

The Permo-Triassic boundary is marked by the following properties:There is abrupt change in the lithology at the boundary of the two system i.e.

white sandstone of Upper Permian and dolomite at the base of Triassic.The upper most sandstone bed shows decrease in faunal contents which indicate

change in depositional environment during the deposition of white sandstone bed.Kathwai member on the other hand also lack fossils, indicating shallow intertidalenvironment.

The variation in thickness of white sandstone bed indicates time gap betweenPermian and Triassic rocks.

MIANWALI FORMATIONIt is the first member of the Musa Khel group. Musa Khel group represents the

Triassic strata of the Salt range.HISTORY:

“Lower part of Mianwali series” by Gee (1959), “Top most limestone and dolomitebeds” by Waagen (1879) was named as “Mianwali formation” by Kummel in (1969).

LITHOLOGY:This formation is mainly composed of limestone, siltstone, dolomite, shale and

sandstone. This formation is divided into three members: Kathwai member: It is the lower most part of the Mianwali formation and

mainly consist of crystalline dolomite and interbedding of Shale. Mitti wala member: It is the middle part of the Mianwali formation and

consists of green shale beds with sandstone and limestone interbedded. Narmia member: It is the lower most member of the Mianwali formation and

mainly consists of sandy dolomite, and dark gray to brown color limestone.Sandstone interbeds are also found in this part.

ENVIRONMENT OF DEPOSITION:Environment of deposition of this formation is open marine to deltaic


Thickness of this formation is 127m.CONTACTS: Lower contact with Chidru formation is marked by Paraconformity Upper contact with overlying Tredian formation is sharp, well defined and

conformable.


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FOSSILS:The various fossils found in this formation are ceratites (cephalopod), brachiopods,

and conodonts.AGE:

Due to the presence of these fossils the age assigned to this formation is LowerTriassic.

TREDIAN FORMATIONIt is the second member of the Musa Khel group.

HISTORY:“Kingriali Sandstone” by Gee (1948), is called as “Tredian formation” by Kummel

and Gee in 1966.LITHOLOGY:

This Formation consists of a non-marine sequence of thin to thcik bedded,varigated, micaceous sandstone with ripple marks and slump structures, interbedded withshale in the lower part. The upper part of the Formation contains massive to thick-beddedsandstone, interbedded with thin dolomite beds in the upper part.

ENVIRONMENT OF DEPOSITION:Environment of deposition of this formation is shallow marine to deltaic.

THICKNESS:The thickness of this formation in Zaluch Nala is 76m.

CONTACTS: Lower contact with Mianwali formation is sharp, well-defined and

conformable. Upper contact with Kingriali formation is also gradational and


This formation contains spores, pollens and wood fragments.AGE:

Due to the presence of these fossils the age assigned to this formation is MiddleTriassic.

Contact between Tredian and Kingrilai Formations


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KINGRIALI FORMATIONIt is the third and last member of the Musa Khel group

HISTORY:“Kingriali Dolomite” by Gee (1943) is named by Gee again in 1945 as “Kingriali

formation”.LITHOLOGY:

This Formation contains thin to thick-bedded or massive, grey dolomite anddolomitic limestone with dolomitic shale and marl.

ENVIRONMENT OF DEPOSITION:Environment of deposition of this formation is shallow marine environment.

THICKNESS:The average thickness of this formation is 76-106m.

CONTACTS: Lower contact of this formation is with Tredian formation and is

conformable. Upper contact is with Datta formation of Jurassic age and the contact is

Disconformable.FOSSILS:

Fossils are rare though some brachiopods, bivalves and crinoids have beenreported.

AGE:Age assigned to this formation is Late Triassic.

DATTA FORMATIONThis formation is the first member of the Surghar Group. Surghar group

represents the Jurassic and Cretaceous strata of the Salt range.HISTORY:

“Variegated stages” by Gee (1945), “Lower part of Samana beds” by Davies (1930)is named as “Datta formation” by Danilchik in1961.

LITHOLOGY:Variegated beds of sandstone, siltstone and shale of different colors are present in

this formation. Sandstone is red to maroon, grey, green and white in color. Shale, siltstoneand mudstone are irregularly distributed. In the upper part thick beds of maroon shale arealso present. Sulpher is mostly present in this formation indicating swamp or deltaicenvironment.

ENVIRONMENT OF DEPOSITION:Environment of deposition of this formation is very shallow marine to deltaic and

alluvial plains.THICKNESS:

Thickness of formation at its type locality is 212m.CONTACTS: Upper contact of this formation with overlying Shinawari formation is

gradational and conformable. Lower contact with underlying Kingriali formation is disconformable.

FOSSILS:This formation is poorly fossiliferrous but some petrified wood is present there.

AGE:


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Age assigned to this formation is Early Jurassic.

Datta Formation

SHINAWARI FORMATIONThis formation is the second member of the Sur Gher group.

HISTORY:“Lowest Samana Beds” by Davies (1930), “Lower part of Kyoto Limestone” by

cutler (1933), is named as Shinawri formation by Fatmi in 1961.LITHOLOGY:

This Formation consists mainly of thin-bedded grey limestone, nodular marl, shaleand sandstone. Current beddings and ripple marks are present.

ENVIRONMENT OF DEPOSITION:Environment of deposition of this formation is shallow marine, deltaic, tidal flats

and estuarine environment.THICKNESS:

Thickness of this formation at type locality is 400m.CONTACTS: Upper contact of this formation is with overlying Samana Suk formation and is

transitional and conformable . Lower contact with underlying Datta formation is also Conformable.

FOSSILS:Various fossils found in this formation are Ammonoites, Brachiopods and corals.

AGE:Age assigned to this formation is Early-Middle Jurassic.


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SAMANA SUK FORMATIONThis formation is third member of Sur Gher group. Few beds of this formation are

present in Nammal gorge but it is undifferentiated from the Shinawri formation.HISTORY:

“Bared limestone” by Gee, “Upper part of Kyoto limestone” by Cutler (1933) isnamed as Samana Suk formation by Davies in 1930.

LITHOLOGY:Main lithology of this formation is medium to thick bedded limestone of gray to

dark gray color. This limestone is oolitic with shale beds with subordinate marl andcalcareous shale.

ENVIRONMENT OF DEPOSITION:Environment of deposition this formation is shallow marine shelfal to supertidal


Thickness of this formation at type locality is 186m.CONTACTS: Lower contact of this formation with underlying Shinawri formation is

conformable upper contact with overlying Chichali formation is disconformable.

FOSSILS:Various fossils found in this formation are Brachiopods, bivalves, Gastropods and

Crinoids.AGE:Age assigned to this formation is Upper Jurassic.

CHICHALI FORMATIONThis formation is the fourth member of the Sur Ghar group.

HISTORY:Gee (1945) named it as “Belemnite beds”.The name has been since formalized as

“Chichali Formation” by Danilchik (1961).TYPE LOCALITY:

Near Chichali Pass in Surghar Range.LITHOLOGY:

It is comprised of a lower sandy glauconitic, phosphatic shale member, a middlesandstone member and an upper glauconitic sandstone member.

THICKNESS:Thickness varies from 12m to 17m .

CONTACTS: Upper contact of this formation is with overlying Lumshiwal formation and is

conformable (gradational) . Lower contact with underlying Samana Suk formation is Dis-Conformable.

FOSSILS:Cephalopods such as Perisphinctes, Mayaites, Aspidoceras, Belemnopsis gerardi

have been found in this formation.AGE:

Age assigned to this formation is Late Jurassic to Early Cretaceous.


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LUMSHIWAL FORMATIONThis formation is the fifth member of the Sur Ghar group.

HISTORY:Davies (1930) named this formation as “Main sandstone series”. Gee (1945)

suggest the name “Lumshiwal sandstone”. The name has been since formalised asLumshiwal Formation by the Stratigraphic Committee of Pakistan.

LITHOLOGY:It is mostly grey, thick bedded to massive, current-bedded, feldspathic and

ferroginous sandstone, but contains silty, sandy glauconitic shale towards the base.Northward and eastward, the formation grades into a mostly marine sequence ofsandstone, siltstone and shelly limestone.

THICKNESS:Thickness ranges from 38m to 194m.

CONTACTS: Upper contact of this formation is with overlying Kawagarh formation and is

disconformable . Lower contact with underlying Chichali formation is gradational and

Conformable.FOSSILS:

Abundant moulds of barchiopods, bivalves, gastropods, ammonoids, belemnitesand echiniods occur in this formation.

AGE:Age assigned to this formation is Middle Cretaceous.

KAWAGARH FORMATIONThis formation is the sixth member of the Sur Ghar group.

HISTORY:Davies (1930) → Sublithographic LimestoneFatmi and Khan (1966) → Darsamand LimestoneKhan and Ahmed (1966) → Durban LimestoneLatif (1970) → Chanali LimestoneDay → Kawagrah MarlsStratigraphic committee of Pakistan has given the name Kawagarh Formation.

LITHOLOGY:The formation consists mainly of dark marl, calcareous shale and nodular,

argillaceous limestone.THICKNESS:

Its thickness ranges from 40m to 200m.CONTACTS: Lower contact is disconformable with Lumshiwal Formation. Upper contact is disconformable with Hangu Formation.

FOSSILS:This formation contains Glabotruncana lapparenti, G. fornicata, G. concavta

carinata, Heterohelix reussi, H. globulosa, Rugoglobigerina rugosa and Globorotalitesmultisepta.(Latif 1970a, 1970c)

AGE:


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The age of the formation is Late Cretaceous.(Coniacian to Campanian)CORRELATION:

It may be correlated with the Parh Limestone, Mughal Kot Formation and PabSandstone in the Suliman-Kirthar fold belt.

K.T BOUNDARY(Cretaceous-Tertiary Boundary)

At the end of the Mesozoic era and before the beginning of the Cenozoic era,there was a major Disconformity in geologic history. If we study the rocks of thePaleocene age, we find a total displacement of almost all the life on earth. The dinosaurs,plants, invertebrates etc all are disappeared. This major Disconformity is seen all over theworld. It is represented in Pakistan in the form of the laterite bed at the bottom of theHangu formations as we go from Kawagarh formation within Hangu formation. In thelower Indus basin, it is represented between the Moro group and Ranikot group.

Scientists all over the world have presented their ideas on this matter out of whichthree are well known.

Meteorite impact theory: According to this a meteorite stuck the earth near theGulf of Mexico. As a result a huge cloud rose which block the sun rays fromreaching the earth’s surface. As a result all living creatures died due to theirdependence on sunlight as a primary source of energy.

Volcanic activity: According to this theory, during this period repeated volcanicactivity cause the formation of the huge dust clouds. Eventually blockingsunlight and other sources, thus causing the death of the living creatures on theearth.

Change in the earth’s Magnetic field: According to this theory, the suddenreversal of the earth’s magnetism distributed the living systems, which couldnot adjust to the new magnetic field and thus resulted in the death of all theliving organisms.

HANGU FORMATIONThis formation is the first member of the Makarwal group. Makarwal group

represents the Paleocene strata of the Salt range.HISTORY:

The “Hangu Shale” and “Hangu Sandstone” by Davies (1930) have beenformalized by the stratigraphic committee of Pakistan as Hangu formation.LITHOLOGY:

This formation consists of dark grey, rarely variegated sandstone, shale,carbonaceous shale, and some nodular argillaceous limestone. The sandstone is white, lightgray, and reddish brown, weathers dark rusty brown, fine to coarse grained and medium tothick bedded.

THICKNESS:In the Salt range area this formation is 40 to 45m thick.

CONTACTS: Upper contact of this formation is with Lockhart formation and this contact is

transitional and conformable. Lower contact of the formation is unconformable with Lumshiwal Formation.


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FOSSILS:The various fossils found in this formation are foraminifera with some corals,

gastropods and bivalves.AGE:

Age assigned to this formation is Early Paleocene.

LOCKHART FORMATIONThis formation is the second member of the Makarwal Group.

HISTORY:Davis (1930) introduced the term Lockhart Limestone for a paleocene limestone

unit in the kohat area.LITHOLOGY:

Grey to dark gray, medium to thick massive bedded, brecciated limestone. Thelimestone displays very well developed nodularity. The nodularity may be caused by any ofthe following four reasons.

Organic activity Differential compaction Pressure solution Stretching

ENVIRONMENT OF DEPOSITION:The Lockhart Limestone is interpreted to have been deposited under stable, broad

shelf/ramp setting.THICKNESS:

In the Samana Range the formation is 60 meter thick.CONTACTS: Upper contact with Patala formation is transitional and conformable. lower contact is with Hangu formation and the contact is also conformable.

FOSSILS:The limestone contains abundant foraminifers, corals, mollucs, Echinoids and

algea.AGE:

On the basis of these fossils the age of the formation is assigned as MiddlePaleocene.

PATALA FORMATIONThis formation is the third member of Makarwal group.

HISTORY:Davies and Pinfold (1937) named it as Patala shale which later was renamed as the

Patala Formation by the Stratigraphic Committee of Pakistan.LITHOLOGY:

It is comprised of shale and marl with subordinate limestone and sandstoneinterbeds. The shale is dark greenish grey, carbonaceous as well as calcareous, and friablewith selenite crystals distributed throughout. The limestone is light to dark grey in color,medium bedded and nodular, whereas the sandstone is yellowish brown and is located inthe upper part of the formation. In Salt Range, it contains coal seams.

ENVIRONMENT OF DEPOSITION:


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The environment of deposition is transitional marine environments.THICKNESS:

Type locality is in Patala nala located in the salt range area, where the thickness ofthe formation is 90 meters.

CONTACTS: Upper contact with overlying Nammal formation is transitional and

conformable. Lower contact is with Lockhart formation and it is also transitional and


The formation is richly fossiliferrous and contains abundant foraminifera andmollusks.

AGE:On the basis of the above mentioned fauna, the age assigned to this formation is

Late Paleocene.

NAMMAL FORMATIONThis formation is the first member of the Cherat group. Cherat group represents

the Eocene strata of the Salt range.HISTORY:

“Nammal limestone and shale” by Gee (1935), “Nammal Marl” by Danilchik andShah (1967), is named as Nammal formation by Stratigraphic Committee of Pakistan.

LITHOLOGY:Main lithology of this formation is shale, marl and limestone alterations. Shale is

gray to green and fossiliferrous. Lime stone is gray to bluish, argillaceous and highlyfossiliferrous. Marl is light gray to bluish gray and is also fossiliferrous.

ENVIRONMENT OF DEPOSITION:Environment of deposition of this formation is shallow marine to lagoonal


Thickness of this formation at its type locality is 100m.CONTACTS: Upper contact of this formation is with overlying Sakessar formation and is

transitional and conformable. Lower contact of this formation is with underlying Patala formation and this

contact is also conformable.FOSSILS:

Various fossils found in this formation are Foraminifera and mollusks.AGE:

Due to the presence of these fossils, age assigned to this formation is EarlyEocene.

SAKESAR FORMATIONThis formation is the second member of the Cherat Group.

HISTORY:“Sakesar Limestone” by Gee in 1935 was accepted by the Stratigraphic committee


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of Pakistan.LITHOLOGY:

Bulk of lithology of this formation is limestone which is cream to light gray incolor, nodular, and massive in the upper part and also highly fossiliferrous. Light graycolored Marl is also found in the top most part and having Chert nodules.

THICKNESS:Thickness of this formation in Salt range is from70-150m.

CONTACTS: Upper contact is with Chorgali formation and this contact is transitional and

conformable. Lower contact is with Nammal formation and it is also conformable.

FOSSILS:Various fossils found in this formation are Foraminifera, Mollusks and Echinoids.

AGE:Due to the presence of these fossils, the age assigned to this formation is Early

Eocene.

CHORGALI FORMATIONThis formation is the third member of the Cherat Group.

HISTORY:Pascoe (1920) → Chorgali bedsStratigraphic committee of Pakistan has given the name Chorgali Formation.

LITHOLOGY:In Salt Range, The formation is divisible into two parts.The lower part consists of

shale and limestone, while the upper part is mainly limestone. The shlae of the lower partis greenish grey and calcareous, and the limestone is light grey and argillaceous. In its upperpart, the limestone is white bor cream, porcellainous and well-bedded.

ENVIRONMENT OF DEPOSITION:The formation is interpreted to be deposited in an intertidal to supratidal

environment during a regressive phase (Jurgan and Abbas, 1991). Gill (1953) suggests thatit was deposited in an open-shelf/ramp setting.

CONTACTS: Lower contact is with Chorgali formation and this contact is transitional and

conformable. Upper contact is with Kamlial Formation and is unconformable.

FOSSILS:The Chorgali Formation is richly fossiliferous and contains foraminifera, molluscs

and ostrocods. (Latif 1970)AGE:

The formation has assigned the age of Early Eocene.CORRELATION:

The Formation correlates with the Lora formation (Latif, 1970) in Hazara area andShekhan Formation in Kohat region.


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ZALUCH NALA :Zaluch Nala is located in the western Salt range. It is the type locality of the Zaluch

group rocks.In this Nala we have studied: Lei Conglomerate which are Quaternary deposits. NEELA WAHAN group rocks which are of Lower Permian age. It includes

Tobra formation, Dandot formation, Warcha Sand stone and Sardhaiformation.

LEI CONGLOMERATELei conglomerates are quaternary deposits. The name “Lei Conglomerates” was

introduced by Gill in 1952 but it was earlier named as “Boulder Conglomerate” by Pilgrimin 1910.

This conglomerate consists of poorly sorted pebbles and boulders of mostlyEocene rocks, with a small proportion of older sedimentary rocks, quartzites and igneousrocks. The conglomerate is intercalated with beds of soft sandstone and siltstone of palebrown to dark brown color.

This conglomerate is different from the conglomerate of the Tobra formation insense that there are no bedding planes in Lei Conglomerate but they are present in Tobraformation.

Lei conglomerates are known as FANGLOMERATES because the environmentof deposition of this formation is Fluvial.

TOBRA FORMATIONThis formation is the first member of the Neela Wahan group. Neela Wahan group

represent the Lower Permian strata of the Salt range.HISTORY:

“Talchir boulder beds” by Gee and “Talchir stage” by Pascoe in 1959 was nownamed as Tobra formation by stratigraphic committee of Pakistan.

LITHOLOGY:Main lithology of this formation is conglomerate, sandstone and shale.

Conglomerate of this formation is polymictic which means that clasts of this formation arederived from various sources. Pink colored Granite clasts are very common in theseconglomerates which are the part of the “Nager Parker granite” in Sindh. Metamorphicslates are also present in this formation. Striations are also present in this formation whichindicates Glacio-Fluvial environment of deposition of this formation.

ENVIRONMENT OF DEPOSITIION:Environment of deposition of this formation is Glacio-Fluvial and Fluvial


Thickness of this formation is 20m in type locality but 133m in the western Saltrange.CONTACTS: Upper contact of this formation is with Dandot formation which is transitional

and conformable. Lower contact of this formation in Zaluch Nala is with Lei conglomerate

which is an unconformable contact.


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FOSSILS:Various fossils reported from this formation are pollens, spores etc.AGE:Age assigned to this formation is Lower Permian.

Tobra Formation

DANDOT FORMATIONThis formation is the second member of the Neela Wahan group.

HISTORY:“Olive Series”, “Eurydesma beds”, and Conularia beds” by Wynne (1878),

“Speckled sandstone” by Waagen (1879) or “Dandot Group” by Noetling (1901).The name Dandot Formation has been since formalized by the Stratigraphic

Committee of Pakistan.LITHOLOGY:

In eastern Salt Range, the Dandot formation mainly consists of dark greenish-greysplintery shale and siltstone with intercalated sandstone, whereas in central Salt Rangegreenish-grey to balck, carbonaceous shlaes with sand flasers alternate with cross-beddedsandstones.

ENVIRONMENT OF DEPOSITIION:Environment of deposition of this formation is marine in eastern Salt Range and

becomes shallower towards the west.THICKNESS:


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Thickness of this formation is 45m- 50m in the east (Makrach Nala) and decreasestoward the central part of the Salt Range.CONTACTS: Upper contact of this formation is with Warchha formation which is

conformable. Lower contact of this formation is with Tobra Formation, which is a

gradational contact.FOSSILS:

The formation contains a rich fauna of brachiopods (Discina, Martiniopsis,Chonetes), bivalves (Eurydesma), gastropods, pteropods (Conularia), bryozoans andostrocods, as well as spores.

AGE:Age assigned to this formation is Early Pemian.

WARCHHA SANDSTONEThis formation is the third member of the Neela Wahan group. The second

member of this group i.e. Dandot formation is missing in the Zaluch Nala.HISTORY:

“Warchha Group” by Noetling (1901) is named as Warchha Sandstone by HusseinAhmed in 1967.

LITHOLOGY:This formation is mostly consisting of Sandstone of red to maroon color which

indicates oxidizing conditions. Sandstone is medium to coarse grained and mostly thickbedded and massive. Pebbles of granite and quartzite are also present. Carbonaceous shaleand coal are also present.

ENVIRONMENT OF DEPOSITION:Environment of deposition of this formation is non-marine, sub aerial to paludal.

THICKNESS:Thickness of this formation at its type locality is 26-80m.

CONTACTS: Upper contact of this formation is with overlying Sardhai formation which is

conformable. Lower contact of this formation is with underlying Dandot formation which is

also transitional and conformable.FOSSILS:

Some plants remains are found in this formation.AGE:

Age aasigned to this formation is Early Permian.

SARDHAI FORMATIONThis formation is the fourth and last member of the Neela Wahan group.

HISTORY:“Upper part of the Warcha group” by Noetling (1901) is named as “Lavender

Clays” or “Sardhai formation” by Gee and Pascoe in1959.LITHOLOGY:

This formation mainly consists of bluish to greenish colored clay, minor graysandstone and gypsum and calcareous beds in the upper part.


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ENVIRONMENT OF DEPOSITION:Environment of deposition of this formation is very shallow reducing marine to

estuarine environment.THICKNESS:

Thickness of this formation at its type locality is 42m and in western Salt range itsthickness is 65m.

CONTACTS: Upper contact of this formation is with overlying Amb formation which is

conformable contact. Lower contact of this formation is with Warcha Sandstone which is also


Brachiopods are commonly found in this formation.AGE:

Age assigned to this formation is Early Permian.

Sardhai Clays


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We observe the following formations on the way from Choa Saidan Shah to Mianwali atdifferent locations.

RAWALPINDI GROUP:This group contains two formations.

MURREE FORMATION:This is the first member of Rawalpindi group.

HISTORY:“Mari group” by Wynne (1874), “Murree beds” by Lydekee (1876), “Murree

Series” by Pilgrim (1910). Stratigrphic Committee of Pakistan has given the name MurreeFormation.TYPE LOCALITY:

North of Dhok Maiki (33 2̊5’N,72 3̊5’E)LITHOLGY:

The Formation is composed of a monotonous sequence of dark red and purpleclay and purple, grey and greenish grey sandstone with subordinate intraformationalconglomerate.DISTRIBUTION/THICKNESS:

The formation is widely distributed in Kohat-Potwar basin. It is 3,030m thick inthe northern Potwar but thins out to only 9m at Banda Shah in Western Kohat. Theformation ranges in thickness between 180-600m in the northern Salt Ranges.CONTACTS:

Lower unconformable contact with Chorgali Formation. Upper conformable and transitional contact with Kamlial Formation.

FOSSILS:The main body of the formation is poorly fossiliferous and only few plant remains,

silicified wood, fish remains, frog and mammalian bones have been recorded.AGE:

Early Miocene

KAMLIAL FORMATION:This is the second member of the Rawalpindi group.

HISTORY:“Kamlial beds” by Pinfold (1918), “Kamlial Satge” by Pascoe (1963). Stratigraphic

Committee of Pakistan has given the name Kamlial Formation.TYPE LOCALITY:

A section southwest of Kamlial (33 1̊5’N,72 5̊0’E), Cambellpur Ditrict has beendesignated as the type section.LITHOLGY:

The formation consists of purple-grey and dark brick-red sandstone which ismedium to coarse grained and contains interbeds of hard purple shale and yellow andpurple intraformational conglomerate. It is distinguished from the underlying Murreeformation by its usually spheroidal weathering and heavy mineral content in whichtourmaline dominates over epidote.DISTRIBUTION/THICKNESS:

The formation is widely distributed in Kohat and Potwar areas. It is 90m thick atKamlial, 580m at Khaur, 650m at Soan Gorge and 60m at Ling River near Rawalpindi.


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CONTACTS: Lower conformable and transitional contact with Murree Formation. Upper conformable contact with Chinji formation.

FOSSILS:A number of fossil mammals have been recorded from the formation.

AGE:Middle-Late Miocene

SIWALIK GROUP:This group contains four members.

CHINJI FORMATION:HISTORY:

Chinji zone by Pilgrim (1913), Lewis called it Chinji formation and the name isaccepted by Stratigraphic Committee of Pakistan.TYPE LOCALITY:

South of chinji village (32 4̊1’N, 72 2̊2’E)LITHOLOGY:

The formation consists of red clay with subordinate ash grey or brownish greysandstone. The sandstone is fine to medium grained, occasionally gritty, cross-bedded andsoft. Scattered pebbles of Quartzite and thin lenses of intraformational conglomerate arefound at different horizons throughout the formation.DISTRIBUTION/THICKNESS:

The formation is widely distributed in the Kohat-Potwar province. It is 750m thickin the type area and more than 1,800m in the shinghar range.CONTACTS:

Lower sharp conformable contact with Kamlial Formation Upper conformable contact with Nagri formation.

FOSSILS:The formation has yielded abundant vertebrate fossils e.g. crocodiles, lizards,

aquatic birds.AGE:

Late Miocene

NAGRI FORMATION:HISTORY:

Nagri zone by Pilgrim (1913), Lower Manchhar of Blanford. “Nagri formation” ofLewis (1937) has been accepted as such by the Stratigrphic Committee of Pakistan.TYPE LOCALITY:

The village of Nagri (32 4̊5’N, 72 1̊4’E) at Campbellpur DistrictLITHOLOGY:

The formation consists of sandstone with subordinate clay and conglomerate. Thesandstone is greenish grey, medium to coarse grained, cross-bedded and massive. The clayis sandy or silt, chocolate brown or reddish grey and pale orange.DSTRIBUTION/THICKNESS:

The formation is widely distributed in the Indus basin. Thickness ranges from300m to as much 2,000m.CONTACTS:


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Lower conformable with Chinji Formation. Upper transitional contact with Dhok Phattan.

FOSSILS:The formation has yielded fairly rich assemblage of vertebrate remains.

AGE:Early Pliocene

DHOK PHATTAN FORMATION:HISTORY:

The name “Dhok Phattan” was introduced by Pilgrim (1913) in a biostratigaphicsense for the upper subdivision of the “Middle Siwalik”. Cotter (1913) redefined the unitas “Dhok Phattan Formation” which was adopted as such by the Startigraphic Committeeof Pakistan.TYPE LOCALITY:

Village Dhok Phattan (33 0̊7’N, 72 1̊4’E), Campbellpur DistrictLITHOLOGY:

The formation is typically represented by monotonous cyclic alternations ofsandstone and clay beds. The sandstone is commonly grey, light grey, greenish grey or buffcoloured, thick bedded, calcareous, moderately cemented, soft and cross-bedded. The clayis orange, brown, dull red or chocolate coloured, calcareous and sandy. Minorintercalations of yellowish brown siltstone are common.DISTRIBUTION/THICKNESS:

The formation is widely distributed in the Indus basin. It has maximum thicknessof 1,820m at Southeast of the Khair-e-Murat Range in the Potwar Area.CONTACTS:

Lower transitional contact with Nagri Formation. Upper disconformable contact with Soan Formation.

FOSSILS:A very rich vertebrate fauna has been recorded from the Dhok Phattan formation.

The fauna is remarkable for its rich Hipparion assemblage and numerous artiodactyls.AGE:

Middle PlioceneSOAN FORMATION:

HISTORY:In the northwest Punjab the Upper Siwalik of Meddlicott (1864), which was later

divided biostratigraphically into the Tatrot and Pinjor zones or stages by Pilgrim (1913) hasbeen formally named “Soan formation” by the Stratigraphic Committee of Pakistan.TYPE LOCALITY:

The section along the road from Gali Jagir to Sihal near Mujahad village north ofthe Soan River (32 2̊2’N, 72 4̊7’E), Campbellpur District, has been designated as typelocality.LITHOLOGY:

The formation consists essentially of compact, massive conglomerate withsubordinate interbeds of varicoloured sandstone, siltstone and clay. Commonly, sandstoneand claystone are intercalated. The claystone is orange, brown or pale pinkish and soft.The sandstone is grey, greenish grey, coarse grained and soft.DISTRIBUTION/THICKNESS:


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The formation has widespread distribution in the Indus Basin. Its thickness variesfrom 120m to 450m in the Kohat-Potwar province.CONTACTS:

Lower disconformable contact with Dhok Phattan formation. Upper unconformable (angular) contact with Lei-conglomerate.

FOSSILS:The formation is poorly fossiliferous.

AGE:Late Pliocene to Early Pliestocene

CALCAREOUS TUFA:Tufa is a soft, friable and porous calcite rock. It is a calcium carbonate (CaCO3)

deposit that forms by chemical/biological precipitation from bodies of water with ahigh dissolved calcium content.

Tufa deposition occurs in seven known ways:

Mechanical precipitation by wave action against the shore. This form of tufacan be useful for identifying the shoreline of extinct lakes.

Precipitation from supersaturated hot spring water entering cooler lake water.

Precipitation in lake bottom sediments which are fed by hot springs from below.

Precipitation from calcium-bearing spring water flowing into an alkaline lake.

Precipitation throughout a lake as the lake water evaporates, leaving the lakesupersaturated in calcium.

Through the agency of algae. Microbial influence is often vital to tufa precipitationand may be involved in the other methods listed.

Precipitation from cold water springs.

Choa Saidan Shah tufa deposits are precipitated from cold spring water.

FOSSILS:It contains leaves, root casts etc.

AGE:Pliestocene

Choa Saidan Shah contains this type of spring deposits (calcareous tufa).


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Calcareous tufa (Choa Saidan Shah)


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REFRENCES:

Kazmi and Abbasi, 2008. Stratigraphy and Historical Geology of Pakistan

Ibrahim Shah, 1977. Stratigraphy of Pakistan

salt range

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