Study of Crustal variations in the part of Central Indus Basin with the help

of integrated geophysical data

SHAZIA ASIM

Submitted for the degree of Doctor of Philosophy

Department of Earth Sciences Quaid-I-Azam University, Islamabad

2009

Certificate Certified that Mrs. Shazia Asim carried out the work contained in this dissertation under my supervision. (Dr. Shahid Nadeem Qureshi) Department of Earth Sciences Quaid-I-Azam University Islamabad, Pakistan Submitted through Dr. Zulfiqar Ahmad Chairman, Department of Earth Sciences Quaid-I-Azam University Islamabad, Pakistan

Contents Dedication Page - 01 Acknowledgement Page - 02 Abstract Page - 03

Chapter one

Introduction to the Research area and data Page - 05

1.1 Introduction Page - 06 1.2 Previous work done Page - 07 1.3 objectives Page - 08 1.4 Available data Page - 09 1.5 Well information Page - 11 1.6 Basemap Page - 11 1.7 Well data correlation Page - 13 1.8 Synthetics Page - 13 1.9 Preparation of Time and Depth section Page - 13

Chapter Two

Geology & Tectonics of the Research area Page - 14 2.1. Central Indus Basin Page - 15 2.2. Punjab Platform Page - 15 2.3. Sulaiman Fore deep Page - 16 2.4. Sulaiman Fold Belt Page - 17

Chapter Three

Stratigraphy Page - 19 3.1 Stratigraphy of the area Page - 20 3.2 Pre-Cambrian Page - 20 3.3 Paleozoic Page - 22 3.4 Mesozoic Page - 24 3.5 Cainozoic Page - 28

Chapter Four

Interpretation Page-31 4.1 Interpretation of the Eastern Part of Sulaiman Fold Belt Page-32 4.2 Northern Zone Page-33 4.3 Central Zone Page-38 4.4 Southern Zone Page-42 4.5 Interpretation of the Sulaiman Foredeep & Punjab Platform Area Page-49 4.6 Interpretation of First E-W Profile Page-49 4.7 Interpretation of Second E-W Profile Page-58 4.8 Interpretation of Third E-W Profile Page-68 4.9 Interpretation of Fourth E-W Profile Page-77 4.10 Interpretation of Fifth E-W Profile Page-81 4.11 Interpretation of Sixth N-S Profile Page-94 4.12 Interpretation of Seventh N-S Profile Page-99 4.13 Interpretation of Eighth N-S Profile Page-104 4.14 Interpretation of Nineth N-S Profile Page-107 4.15 Depositional history of the area Page-108 4.16 An overview of the subsurface crustal variations Of area with the help of 3D Two way time models And Depth models Page-113 Conclusions & Recommendations Page-124 References Page-128 Appendix

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Dedicated to my family

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Acknowledgement

Up and above all glory to Almighty God, Creator of heavens and earth who

blessed me with the health and knowledge to enable me to complete this dissertation.

I pay a special gratitude to my dissertation supervisor Dr. Shahid Nadeem Qureshi for

giving an initiative to this study. His inspiring guidance, dynamic supervision and

constructive criticism, helped me to complete this work. He has been a continuous

source of encouragement the whole time.

Especially I acknowledge Professor, Dr. Zulfiqar Ahmed (Chairman, Department of

Earth Sciences, QAU) and my colleagues (teaching faculty of the department of Earth

Sciences) for a full support and cooperation during the research.

I greatly acknowledge Mr. S. Manshoor Ali (General Manager, Exploration activities,

HDIP), Dr. Muhammad Mujtaba (HDIP), Mr. Zahid A. Farani (OGDCL) and Mr.

Maas Saddiqui (Dewan Petroleum) who have never hesitated to discuss and to give

their valuable suggestions. I also acknowledge Dr. A.D. Khan, Director PCRWR for

enabling the use of GIS softwares.

Directorate General of Petroleum Concessions is greatly acknowledged for providing

the Research data.

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ABSTRACT

The Research Area comprises of Punjab Platform, Sulaiman Foredeep and Eastern

Part of Sulaiman Fold Belt (from east to west). Seismic lines are provided by the

Directorate General of Petroleum Concessions. The stratigraphic correlation of

approximately 3500 km seismic data is done with the help of the well data, formation

tops, Synthetics and general stratigraphy of the area. The Time and Depth sections

show the subsurface crustal variations. The Structural and Stratigraphical

interpretation is done in detail. The 3D subsurface Time and Depth models show the

structural highs and trough areas. A research area is divided into four Zones namely,

A, B , C & D on the basis of subsurface structural features. Zone A is an eastern most

part of the Research area in Punjab Platform where Paleozoic sediments (Permian &

Cambrian) are present. Mesozoic sediments (Cretaceous, Jurassic & Triassic) and

younger sediments (Paleocene & Eocene) are missing in this zone showing the uplift

of Sargodha High during Paleozoic time. An uneven distribution of Paleozoic rocks

shows some thickness in east. They show thinning and almost truncation in Sulaiman

Foredeep which indicate their depocenter lies in east. This also represents the time of

uplift of Sargodha High that shifted depocenter westward. Seismic data shows a thick

Mesozoic deposition in Sulaiman Foredeep. They give coastal onlaps on the Permo-

Triassic unconformity towards Sargodha High suggesting this as an area of non-

deposition. The gradual uplift of Sargodha high continues, tilting the Mesozoic strata.

Towards Pezu Uplift the time of major uplift is related to a collision of Indian Plate

with Eurasian Plate followed by the period of intense erosion. Below unconformity

sediments show an effect of folding and an angular termination against unconformity,

suggesting it as an angular unconformity in this region. Paleocene, Cretaceous,

Jurassic, Triassic, Permian, Cambrian and Pre-Cambrian sediments are uplifted and

eroded. Afterwards rapid and thick Eocene and post- Eocene sediments deposition

took place in Sulaiman Foredeep. Zone B is an area of thick deposition of Jurassic,

Triassic, Cretaceous, Paleocene & Eocene sediments, showing the westward shift of

depocenter after Paleozoic age. Paleozoic sediments are thinning in this zone.

Mesozoic sediments are thinning towards Punjab Platform. Zone C shows the

westward thinning and almost truncation of Cambrian & Permian sediments. An

ancient shelf margin of Paleocene age, is marked on various seismic sections of this

zone. An eastward truncation of the Vehowa and Chitarwata Formation in terms of

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stratigraphic pinchout shows the maximum extend of Early Miocene and Oligocene

strata respectively in Sulaiman Foredeep. Zone D is an eastern part of Sulaiman Fold

Belt. It comprises an area of Domanda Fault and Sulaiman Basement Fault. Zone D is

further divided into Northern, Central & Southern parts. Northern part comprises of a

trough area of Drazinda Synclinal structure which lies between the West Sulaiman

Transform Fault and Domanda Fault. The anticlinal structures of Domanda, Gulan &

Savi Ragha also lie in this part. Central part consists of a Safed koh trend. Southern

part consists of low relief Sakhi Sarwar, Drigri & Kotrum anticlinal structures. Flat-

Ramp geometry of the Basement Fault is observed, which separates the Sulaiman

Block from Punjab Platform. This could be a tear fault accommodating the

differential movements of Punjab platform Block and Sulaiman Block.

In Sulaiman Foredeep a prominent effect of flexuring is present in Eocene and older

sediments. This is marked on east-west oriented seismic sections. This effect is related

with the time of collision of Indian plate and westward resistance provided by a

Sulaiman Basement Fault. A normal fault is also marked in a seismic section which

cuts the over all strata. The sediments are detached and in west the anticlines are

formed as a fault propagation folds. Seismic data confirms the presence of Pre-

Cambrian rocks in the subsurface through out the area. The Salt Range Formation is

present in Punjab Platform. There is a transition zone in west where seismic data

shows presence of thick sediments of equivalent age. An ancient Paleohigh of

Paleozoic age is present in Bahawalpur area. It is extending in the south. It has a

deposition of Jurassic & Triassic sediments while Paleocene & Cretaceous sediments

onlap on Jurassic, then Eocene sediments are deposited over it.

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1.1. Introduction

Research area comprises of Dera Ismail Khan and Dera Ghazi Khan districts of

Pakistan (fig.1.1). It occupies an area of 75,000 sq.km approximately. Research area

is located between: 70° E - 72°15´ E & 29° N - 32° N

Fig.1.1 Map of Pakistan showing location of the Research Area. (www.msn.com)

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The Time and Depth Models of seismic lines, having a length of 3500 km

approximately, are prepared. In this research an extensive study of the subsurface

crustal variations is performed along with the 3D Time and Depth Models.

The study of subsurface crustal variations is done in detail in particular the sediments

of Paleozoic and Pre-Cambrian. The uplift and erosion of Paleozoic and Mesozoic

sediments followed by deposition of younger sediments related to collisional event of

Indian plate is shown in the Time & Depth Models. The different times of uplift of

Sargodha High and Pezu Uplift are studied in detail. Also their comparison with

Bahawalpur High is made in 3D models. A depth cross section of Safed Koh Trend is

prepared. The subsurface extend of Oligocene and Miocene sediments is studied

especially the effect of flexuring produced in the sediments due to collision of Indian

plate. Thinning and thickening of the Paleozoic and Mesozoic sediments with the

change in basin depocenter is shown in the Time and Depth Models. An ancient shelf

margin of Paleocene age is picked and marked that is present throughout the area.

This is a first attempt of its kind done in the research area. This study is beneficial in

the various relevant fields such as Petroleum geology, Sedimentology, Seismic

Stratigraphy, Structural geology, Tectonics, Geodynamics and Basin analysis for

researchers and industries.

1.2. Previous work done

A generalized view is obtained by the efforts of various authors :

Yeats and Lawrence (1984) explain the tectonic configuration of the Sargodha Ridge

as an outer “swell” due to loading of Indian Shield by the Himalayan thrusts.

Humayon et al. (1991) and Jadoon et al. (1994) interpret the structures of the eastern

& central Sulaiman Foldbelt on the basis of surface geology and seismic analysis.

According to them the sedimentary strata is detached from the basement with a floor

thrust in Paleozoic strata and roof-thrust in Cretaceous (Sembar Formation) except in

the frontal part of the Sulaiman Foldbelt where it occurs in Eocene sequences.

Bannert et al. (1989), Bannert and Raza (1992), Bannert et al. (1995), Bender and

Raza (1995), suggest that the oblique collision of the Eurasian and Indo-Pakistan

plates caused the development of large scale, N-S running, left-lateral strike-slip

faults in the basement which are responsible for the segmentation of the Indo-Pakistan

Plate. Kemal et al. (1991) consider East Sulaiman structural play of narrow straight

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anticlines as Flower Structure due to large scale distributive wrench faulting. An east-

west cross-section showing continuation of tertiary sediments of Drazinda syncline is

prepared by Hemphill and Kidwai, 1973. Waheed and Wells (1990) suggest an early

manifestation of the paleodrainage shift due to obduction and shelf reversal recorded

in the broadly distributed and marginal marine early Eocene Ghazij Formation in

western Pakistan. Iqbal and Helmcke (2004) suggest that the basement of Indo-

Pakistan is involved in structural deformation of Zindapir Anticlinorium and its

surroundings. Lillie et al. (1987), Humayun et al. (1991) and Jadoon et al. (1992)

believe the presence of a basal decollement in pelitic rocks or fine carbonates above

the crystalline basement at a depth of more than 11 km. On the basis of paleomagnetic

data Lindsay et al. (2005)have evaluated the age span of the Chitarwata Formation in

the Zinda Pir Dome as Oligocene at its base and earliest Miocene at the contact with

the Vihowa Formation. Ahmad et al. (2007) discuss the cross bedded Sandstone and

Coal in deltaic facies and fresh water facies having boulders of Tobra Formation. The

cross bedding suggests the activation of erosional phenomena. Hasany et al. (2007)

emphasize on exploration activity for Infracambrian sediments in Pakistan due to a

Heavy oil discovery in Baghewala-1 in 1991 in Bikaner-Nagur Basin, Rajasthan

India.

1.3. Objectives

Main objectives of research in this area are elaborated as follows:

1. To establish a Stratigraphic correlation in the subsurface with the help of well

data and seismic sections.

2. To mark the major unconformities in the research area.

3. To study the subsurface Structures.

4. To study the uplift of Sargodha High and the changes in basin depocenter with

the passage of time.

5. To Study the subsurface extent of Vehowa Formation (Miocene) and

Chitarwata Formation (Oligocene) in the area.

6. Preparation of depth cross section of Safed Koh Trend (eastern part of

Sulaiman Fold Belt).

7. To study the continuation of Permian and Cambrian (Paleozoic) and Pre-

Cambrian in the research area.

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1.4. Available Data

The available data is in the form of Seismic Reflection (filtered and migrated)

Sections and well data, sonic logs and the Formation tops. The data is provided by

Directorate General of Petroleum Concessions, Pakistan. Locations of Seismic

lines and well locations are marked on Basemap (fig 1.2). Five east-west and four

north-south profiles have been interpreted. Further information on the seismic line

number, shot point range and line length is given below:

First E-W Profile

Seismic Line Shot Point Range Length (km)

845-LEA-114 SP 100 – SP 2514 121 956-DIK-32 SP 590 – SP 948 18

956-DIK-32A SP 101 – SP 619 52

Second E-W Profile

Seismic Line Shot Point Range Length (km)

835-LEA-107 SP 100 – SP 2410 231 L36-91-20 SP 28 – SP 1996 98

Third E-W Profile

Seismic Line Shot Point Range Length (km)

PSPD-80-23 SP 1009 – SP 1404 39 836-LEA-06 SP 101 – SP 930 83 C95-LMT-17 SP 102 – SP 505 40

Fourth E-W Profile

Seismic Line Shot Point Range Length (km)

836-LEA-07 SP 101 – SP 683 58 C95-LMT-15 SP 102 – SP 812 71

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Fifth E-W Profile

Seismic Line Shot Point Range Length (km)

916-YZM-05 SP 101 – SP 822 54

914-RPR-03 SP 101 – SP 457 36

914-RPR-05 SP 101 – SP 360 26

954-FZP-05 SP 101 – SP 1661 156

954-FZP-09 SP 101 – SP 675 58

976-FZP-06 SP 104 – SP 665 28

C95-LMT-05 SP 102 – SP 122 112

PSPD-5340 SP 400 – SP 1704 195

PSPD-5085 SP 1064 – SP 1912 127

904-B-01 SP 101 – SP 403 450

904-B-05 SP 104 – SP 760 98

The N-S profiles

Four north-south profiles have been interpreted. The information about the seismic

line number, shot point range and line length is given below:

First N-S Profile

Seismic Line Shot Point Range Length (km)

804-DK-06 SP 101 – SP 580 48

804-DK-06A SP 101 – SP 853 75

Second N-S Profile

Seismic Line Shot Point Range Length (km)

804-DK-04 SP 101 – SP 960 86

Third N-S Profile

Seismic Line Shot Point Range Length (km)

956-DIK-11 SP 101 – SP 720 31

956-DIK-12 SP 102 – SP 488 19

956-DIK-38 SP 101 – SP 650 28

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Fourth N-S Profile

Seismic Line Shot Point Range Length (km)

854-KBR-72 SP 101– SP 201 10

854-KBR-65 SP 101– SP 229 13

845-KBR-28 SP 101– SP721 62

Additional data Some additional lines used are as follows :

C95-LMT-06, C95-LMT-07, C95-LMT-08, C95-LMT-09 and 904-B-01.

1.5. Well information

The data of following wells is used for the correlation:

Kamiab – 01, Saro – 01, Budhuana – 01, Drigri – 01, Ramak – 01, Domanda – 01,

Rhodho – 01, Dhodak – 01, Afiband – 01, Zindapir – 01, Saviragha – 01, Drigri – 01,

Kotrum – 01, Sakhi Sarwar – 01, Panjpir – 01, Nandpur – 01, Sarai Sidhu – 01,

Ahmedpur – 01 and Behawalpur East – 01.

1.6 Basemap

Base map (fig 1.2) is prepared and shows well locations and orientation of seismic

lines. Settlements and rivers are plotted on a base map.

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1.7 Well data correlation

Correlation of reflectors on seismic sections is done with the help of well logs and

well tops (appendix) along with the surface geology. Data of well Kamiab-01 is used

for correlation of seismic section 804-DK-04. The seismic section 804-DK-06A is

correlated with well Darbula-01, 804-DK-06 is correlated with Well Saro-01and 835-

LEA-107 is correlated with Kamiab-01, Saro-01 in south, Darbula-01 in north and

Ramak-01 in west with the help of crossing lines on which these wells are located. In

the same manner other profiles are correlated. Marking of the reflectors/formations is

done by using the well tops where the well logs are not available. The Stratigraphic

column of the area is thus established. But in the western part of the research area no

control for correlation is available below Cretaceous/Jurassic age. This problem was

overcome by correlating the wells from east in which the Permian, Cambrian and Pre-

Cambrian are drilled. In this regional study mostly the formations are referred by

ages, whereas in some cases the names are mentioned e.g. Chitarwata (Oligocene)

Formation to study its presence, its trend and maximum continuity in the area. It is

absent in eastern part of area. The research area is studied structurally, its depositional

trends and the unconformities are delineated.

1.8 Synthetics

Synthetics are prepared from well data of Drigri-01 & Ramak-01. The correlation of

the Seismic Sections is done with the Synthetic thus prepared and well tops (see

appendix).

1.9 Preparation of Time section and Depth section

The transformation of seismic signal into litho-structural domain needs information of

velocity and time. In the given seismic sections RMS velocities at selected shot points

(SP) are provided which in turn are used to calculate interval velocities and then

average velocities. The Time and Depth models are prepared using the time and

velocity thus calculated. Using the time and depth information 3D models are

generated with the help of GIS softwares.

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2.1. Central Indus Basin:

Research area lies in the Central Indus Basin of Pakistan. Central Indus Basin may be

divided into following broad tectonic divisions from east to west (Kadri, 1995)

(1) Punjab Platform (2) Sulaiman Depression (3) Sulaiman Fold Belt (fig 2.1 & 2.2).

The basin is separated from Upper Indus Basin by the Sargodha High & Pezu uplift in

north. It is bounded by Indian shield in the east, marginal zone of Indian Plate in the

west, and Sukkur rift in the south. It is the Sargodha High in fact which is considered

to be a divide between Upper Indus Basin & Lower Indus Basin (Kadri, 1995).

Another major feature of basement topography, as seen on the gravity data, is the

Khairpur-Jacobabad High & its associated structures which grew through Jurassic &

Cretaceous/Paleocene ages & divide the Lower Indus Basin further into two basins

namely Southern and Central Indus Basin. The Southern & Central Indus Basins are

separated by Jacobabad & Mari- Kandhkot highs together termed as the Sukkur Rift.

(Raza et al., 1989).

The oldest rocks exposed in this basin are of Triassic age (Wulgai Formation) while

the oldest rocks penetrated through drilling are of Precambrian Salt Range Formation.

The depth to the basement is about 15000 meters in the Trough areas. Precambrian

shield rocks are evident along the rim of the Indian Plate (Kadri, 1995).

2.2. Punjab Platform:

Kadri, (1995) describes this part as the eastern segment of Central Indus Basin where

no surface outcrops of sedimentary rocks are present. Tectonically it is a broad

monocline dipping gently towards the Sulaiman Depression. Punjab Platform is

tectonically the least affected area because of its greater distance from collision zone.

A number of wells have been drilled on this platform. The stratigraphic sequence

established on the basis of these wells revealed some of the most significant

stratigraphic pinch outs in Pakistan.

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Fig 2.1 Geological map showing the location of Research area (www.gsp.com).

2.3. Sulaiman Fore deep:

The Sulaiman Foredeep is also called Sulaiman Depression. This depression is

longitudinally oriented area of subsidence; it becomes arcuate and takes up a

transverse orientation along its southern rim. Like many other features, this

depression was also formed as a result of the collision between two plates. The

seismic evidence shows some buried anticlines (e.g. Ramak) which may have been

formed due to the flow of Eocene shales (Kadri, 1995).

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Fig 2.2 Area under study comprises of Eastern part of Sulaiman Fold Belt, Sulaiman

Foredeep and Punjab Platform (Raza, 1989).

2.4. Sulaiman Fold Belt:

This is a major tectonic feature in the proximity of collision zone & therefore contains

a large number of disturbed anticlinal features (Kadri, 1995). There are some large

anticlines within Kirthar and Sulaiman belts and especially along the eastern margins,

that are clearly detachments. The northward-striking east sulaiman structural play

domain has narrow, straight anticlines as long as tens of kilometers with limbs that are

broken locally by steeply dipping faults with reverse dip separation. These structures

are interpreted as flower structures that are products of large-scale distributive wrench

faulting having a prospective reservoirs like Ranikot Formation (Paleocene), Pab

Formation, Sember Formation and Lower Goru Formation of Cretaceous age (Kemal

et al, 1991). Bannert and Raza (1992) assumed that basement was segmented into

three different blocks during the collision of the Indo-Pakistan Plate with the Eurasian

Plate. Three basement faults separate these basement blocks from each other and from

the central part of the Indo-Pakistan Plate. The Khuzdar Block and the Sulaiman

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Block are separated by the Kirthar Basement Fault, the Sulaiman Block and the

Hazara Block by the Sulaiman Basement Fault and the Hazara Block and main body

of the Indo-Pakistan Plate to the east are separated by the Jhelum Basement Fault

(Bender and Raza, 1995).

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3.1 Stratigraphy of the area

The research area lies in Central Indus Basin of Pakistan (Table 2.1). A complete

stratigraphic correlation is done from the wells in east which are drilled in Paleozoic

rocks (Darbula-01, Sarai Sidhu-01 and Bahawalpur East-01). The wells in western

part of the area are drilled in Mesozoic rocks. They also indicate the presence of Late

Oligocene – Early Miocene sediments. The subsurface extend of these sediments is

further studied in Time and Depth sections.

3.2 Precambrian

Salt Range Formation with salt, marl, salt seams and dolomite forms the basement for

the fossiliferous Cambrian sequence of the Salt Range. It represents an evaporate

sequence similar to the Hormuz Salt Formation of Iran. Although its exposures are

restricted to the Salt Range, deep drill holes have confirmed its presence to the north

and south of the exposures. It has three members;

Sahwal, Marl Member

Bright, red marl beds with irregular gypsum, dolomite beds and Khewra Trap (3-100

m). Also it has dull red marl beds with some salt seems and 10 m thick gypsum bed

on top (more than 40 m).

Bhandar Kas Gypsum Member

Massive gypsum with minor beds of dolomite and clay (more than 80 m)

Billianwala Salt Member

Ferruginous red marl with thick seams of salt (more than 650 m)

Its exposure is along the southern flank of the Salt Range, from Kussak in the east to

Kalabagh in the west. In the subsurface, the rock unit is encountered as far south as

Karampur in the Punjab Plains. Its contact with the overlying Khewra Sandstone is

normal and conformable. Its age is assigned an Early Cambrian to Late Precambrian

age (Shah, 1977).

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Table 2.1: Stratigraphy of Central Indus Basin (after Kadri, 1995).

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3.3 Paleozoic

Rocks of Cambrian and Permian age are present in the Central Indus Basin. Cambrian

rocks were essentially deposited in the shallow water except for the lower most and

uppermost formation which represent transgressive and regressive facies respectively.

Cambrian

The Cambrian Formations are as follows:

Khewra Sandstone

The formation consists predominantly of purple to brown, yellowish brown, fine

grained sandstone. The lower most part of the formation is red, flaggy shale.

Sedimentary features like ripple marks and mud cracks are common in the formation.

The age is Early Cambrian.

Kussak Formation

The formation is composed of greenish grey, glauconitic, micaceous sandstone,

greenish grey siltstone, interbedded with light grey dolomite and some oolitic,

arenaceous dolomite. Numerous layers of intraformational conglomerate are present.

Pink gypsum lenses are present near the top. The age is Early Middle Cambrian.

Jutana Formation

The formation consists of light green, hard, massive, partly sandy dolomite and the

upper part is composed of light green to dirty white massive dolomite. Upper and

lower contact with Baghanwala Formation and Kussak Formation respectively is

conformable. The age is late Early Cambrian to early Middle Cambrian.

Baghanwala Formation

The formation is composed of red shale and clay, alternating with flaggy sandstone.

Ripple marks and mud cracks are common in the formation. Numerous

Pseudomorphic casts of salt crystals which are found along the bedding planes are

diagnostic feature of this formation. They indicate the lagoonal environment and arid

conditions for the deposition of the formation. The formation is encountered in the

subsurface at Karampur. Its contact with the overlying Tobra Formation is

unconformable. The age is early Middle Cambrian.

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Permian

Permian rocks of the Axial Belt are exposed as isolated outcops in the core of

anticlines. These exposures have been described from Wulgai, Ghazaband and Kalat

areas of Baluchistan. Permian rocks are sedimentary with lithologies of shale,

sandstone and limestone. These are divided into two groups:

Nilawahan Group

It consists of following formations:

Sardhai Formation

Warcha Formation

Dandot Formation

Tobra Formation

The Nilawahan Group represents a dominantly continental deposit consisting of

arenaceous and argillaceous sediments with marine intertonging in the upper part

which passes conformably into the overlying marine Zaluch Group. The lower most

beds of the Permian rocks rests disconformably on Cambrian rocks while the upper

part is separated from the Triassic rocks paraconformably.

Tobra Formation

This formation depicts a very mixed lithology in which the following three facies are

recognized:

1. Tillitic facies exposed in the eastern Salt Range. This rock unit grades into

marine sandstone containing Eurydesma and Conularia fauna.

2. Freshwater facies with few or no boulders. It is an alternating facies of

siltstone and shale containing spore flora.

3. A complex facies of diamictite, sandstone and boulder bed.

Lower contact with the Cambrian rocks is disconformable. The age is Early Permian.

Dandot Formation

The lithology consists of light grey to olive green yellowish sandstone with the

occasional thin pebbly beds and subordinate dark grey and greenish splintery shales.

It has agradational contact with the underlying Tobra Formation and it is terminated

in sharp but conformable contact with the overlying Warcha Sandstone. The age is

Early Permian.

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Warcha Sandstone

The formation consists of medium to coarse grained sandstone, conglomeratic in

places and interbeds of shale. The sandstone is cross bedded and arkosic. The pebbles

of the unit are mostly of granite of pink colour and of quartzite. It conformably

overlies the Dandot Formation. It is overlain by the Sardhai Formation with the

transitional contact. The age is Early Permian.

Zaluch Group

It consists of following formations:

Chhidru Formation

Wargal Formation

Amb Formation

Amb Formation

This formation consists of sandstone, limestone and shale. The sandstone beds occupy

the lower part of formation. Upwards the sequence limestone with some shale

appears. The upper contact with Wargal Limestone is conformable.

Wargal Formation

The lithology comprises dolomite of light to medium grey, brownish grey and olive

grey colors. The upper contact with the Chhidru Formation is transitional. The age is

Late Permian.

Chhidru Formation

The formation at the base has a shale unit. Overlying this unit are the beds of

calcareous sandstone with few sandy limestone. The top most part of this formation is

a white sandstone bed with oscillation ripple marks. The age is Late Permian (Shah,

1977).

3.4 Mesozoic

Rocks of the Mesozoic Era are widely distributed in Pakistan. They depict a great

variation in lithology and thickness in different parts of the country. Some important

mineral deposits (barite, fireclay, low grade iron ores, phosphatic showings and

others) and producing or potential oil and gas horizons are present within the rocks of

Cretaceous and Jurassic Systems.

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The Mesozoic rocks of the Lower Indus Basin are several thousand meters thick and

are widely exposed in the Lower Indus Basin (Sulaiman-Kirthat province) and in the

Axial Belt.

Triassic

Rocks of Triassic System are represented by Mianwali Formation, Tredian Formation,

Chak Jabbi Limestone and Kingriali Formation in the Kohat Potwar Province and by

the Wulgai formation in the Axial Belt. In the Axial Belt the Triassic System is

represented by shale with subordinate limestone and sandstone of the Wulgai

Formation. In the Upper Indus Basin the rocks of Triassic System maily consist of

limestone, dolomite, sandstone and shale and are divided into three formations

Permian-Triassic boundary

This boundary in Salt Range and Trans Indus ranges was placed at the top of the

dolomite unit of the Kathwai Member of Mianwali Formation. Some placed the

boundary in the middle of a white sandstone unit which is the highest bed of Chhidru

Formation. This boundary where exposed is marked by a paraconformity.

Mianwali Formation

It has following three members:

Narmia Member

Mittiwali Member

Kathwai Member

Kathwai Member

It consists of dolomite in the lower part and limestone in the upper part.

Mittiwali Member

It consists of grey, fine grained, non glauconitic limestone with abundant ammonites.

The rest of the unit consists of greyish shale, silty shale with some sandstone and

limestone beds.

Narmia Member

The basal bed is of limestone. The rest of the unit consists of grey to black shale with

interbeds of sandstone and lenticular limestone or dolomite. The top most bed is

limestone.

The age of the Mianwali Formation is Early Triassic.

26

Tredian Formation

This formation comprises of two members. The lower one is Landa Member which

consists of sandstone and shale. The upper one is Khat Kiara Member is a massive,

thick bedded, white sandstone that grades into the overlying Kingriali Formation. The

age is of Middle Triassic.

Kingriali Formation

It consists of thin to thick bedded, massive, fine to coarse textured light grey brown

dolomite and dolomitic limestone with interbeds of shale and marl in the upper part.

The lower contact with Tredian Formation is transitional which is marked by

interbedding of sandstone and dolomite. The upper contact with the Datta Formation

is disconformable. The age is Late Triassic.

Jurassic

The Jurassic System is represented by limestone, shale and sandstone with

subordinate dolomitic and ferruginous beds. The lower part of the Lower Jurassic

consists of arenaceous and argillaceous sediments of dominantly continental origin

that grades up in the sequence into marine calcareous and argillaceous rocks. By

Middle Jurassic, marine conditions were well established in most of the areas and

mainly carbonate rocks were deposited. The close of the Middle Jurassic is marked by

regressive facies. The Jurassic in the Axial Belt and Lower Indus Basin is represented

by a great thickness (several thousand meters) of marine limestone and shale with

subordinates in the lower part. Marine sedimentation continued during the Early

Cretaceous and Jurassic-Cretaceous boundary is regarded as transitional.

Jurassic rocks are widely distributed in the Axial Belt and Sulaiman and Kirthar

provinces of the Lower Indus Basin. Triassic rocks transitionally underlie Jurassic

strata. The change in lithology is from a dominant shale of Triassic System to thin

bedded limestone and intercalated shale of the early part of the Jurassic System. The

Jurassic formations of the Lower Indus Basin comprises of:

Mazar Drik Formation

Chiltan Limestone

Shirinab Formation

27

Shirinab Formation

It consists of thin bedded limestone and shale, transitional to the underlying Triassic

Wulgai Formation. The age is Early Jurassic.

Chiltan Limestone

It consists of massive thick bedded limestone. Its upper contact with Mazar Drik

Formation is transitional.

Mazar Drik Formation

It consists of thin bedded limestone and shale. Its upper contact with the Sember

Formation is disconformable. It is not developed in the Sulaiman range.

The Jurassic System of the Upper Indus Basin is represented by Datta Formation

(Early Jurassic), Shinwari Formation (Early to middle Jurassic) having three members

Anjira Member, Loralai Limestone Menber and Spingwar Member, Samana Suk

Formation (Middle Jurassic) and the lower part of the Chichali Formation.

Cretaceous

In the adjoining regions of Sulaiman and Kirthar provinces of the Lower Indus Basin

the Cretaceous rocks are mostly of sedimentary origin and except for local

disconformities constitute a continuous sequence from Early to Late Cretaceous. The

overlying Tertiary sediments are transitional in parts of this area while local

disconformities between the Cretaceous and Tertiary have been recognized.

The following formations have been recognized in the Sulaiman and Kirthar

provinces:

Sember Formation

Goru Formation

Parh Limestone

Mughal Kot Limestone

Fort Munro Formation

Pab Sandstone

Moro Formation

In the Upper Indus Basin Kawagarh Formation, Lumshiwal Formation and Chichali

Formation are recognized (Shah, 1977).

28

3.5 Cainozoic

The close of the Mesozoic Era is marked by the period of emergence in parts of

Pakistan. There is an angular unconformity between Paleocene and the older units in

parts of the Sulaiman province and Axial Belt. These rocks were deposited in a broad

sea which gradually narrowed and retreated southward with the passage of time till it

came to occupy its present position as Arabian Sea.

Tertiary

Paleocene

Limestone is the dominant lithology in most parts of the Lower Indus Basin, shale

dominates in the Axial Belt and Eastern Sualiman Province.

Ranikot Group has Khadro Formation, Bara Formation (Lower Ranikot sandstone)

and Lakhra Formation (Upper Ranikot limestone). It overlies Pab Sandstone

unconformably. It is correlated with Dungan Formation.

Eocene

The shale and marl are the major lithology in the Early Eocene times in the Lower

Indus Basin and adjoining areas of Axial Belt. Ghazij Formation, Laki Formation and

Kirthar Formation are recognized in this area. Kirthar Formation is divisible into four

members in parts of the eastern Sulaiman Province as Habib Rahi Limestone

Member, Sirki Member, Pir koh Member and Drazinda Member.

Oligocene

Rocks of Oligocene age are developed in the Lower Indus Basin, Axial Belt and the

Baluchistan Basin. Nari Formation of the Momani Group is recognized in the Kirthar

Province, parts of Sulaiman Province and the Axial Belt. Nari Formation consists of

sandstone, shale and subordinate limestone. It is conformably overlain by the Gaj

Formation in the Sulaiman and Kirthar provinces. In the eastern part of Sulaiman

range the contact is unconformable with Siwaliks as Gaj Formation is absent. Its age

is Oligocene with some upper strata is of Early Miocene age (Shah, 1977). In the

Sulaiman Range the Oligocene sequence which was previously referred to as Nari

Formation has now been renamed as the Chitarwata Formation (Kazmi and Jan,

1997).

29

Miocene-Pliocene

The rock units recognized in the region of Indus Basin and Calcareous Zone of Axial

Belt are as follows:

Gaj Formation

It consists of shale with subordinate sandstone and limestone. Its lower contact with

Nari Formatoin is transitional and conformable. The upper contact with Siwalik group

is also transitional. The age is Early Miocene.

Rawalpindi Group

It consists of Murree Formation and Kamlial Formation

Siwalik group

It consists of following formations:

Chinji Formation

It consists of red clay with subordinate ash grey or brownish grey sandstone. It is only

confined to the southern half of the eastern Sulaiman Range and is not developed in

the rest of the Lower Indus Basin. In the Sulaiman Range it disconformably overlies

the Nari Formation. It is conformably overlain by Nagri Formation. The age is Late

Miocene.

Nagri Formation

It consists of sandstone with subordinate clay and conglomerate. The upper contact

with Dhok Pathan Formation is transitional. The age is Late Miocene.

Dhok Pathan Formation

It consists of cyclic alternations of sandstone and clay beds. Its upper contact with

Soan Formation is gradational in the Lower Indus Basin. The age is Early to Middle

Pliocene.

Soan Formation

It consists of compact, massive conglomerate with subordinate interbeds of

varicoloured sandstone, siltstone and/or clay. The upper contact with the Lei

Conglomerate is marked by an angular unconformity. However, in parts of the Lower

Indus Basin and Quetta region, the contact has been transitional. The age is Late

Pliocene to Early Pliestocene.

Quaternary

Lei Conglomerate is recognized in the Indus Basin and Quetta region of Axial Belt.

It is regarded as a valley fill, laid down as fluviatile, lacustrine and piedmont outwash

deposits in the lower parts of the structural depressions. The formation is composed of

30

coarser boulder and pebble conglomerates with minor coarse and cross bedded

sandstone. The age is Early Pliestocene (Shah, 1977).

31

32

4.1 Interpretation of the Eastern Part of Sulaiman Fold Belt.

An eastern part of Sulaiman Fold Belt which includes Safed Koh Trend, Zindapir

Anticlinorium, Domanda Fault and West Sulaiman Transform Fault area is studied in

detail (fig4.1).

Fig 4.1 Map showing the location of Domanda Fault, Sulaiman Basement Fault and

Zindapir Anticlinorium (Bannert et al., 1992).

It comprises of structures of Domanda, Dhodak, Rodho, Afiband, Zindapir, Sakhi

Sarwar, Drigri & Kotrum anticlines. This area is divided into Northern, Central &

Southern parts.

33

4.2 Northern Part:

Seismic lines 812-DA-08 & L36-91-01, oriented in a north-south direction are

interpreted. The prominent structures present in the area are Drazinda Syncline and

Domanda Fault. A well Domanda-01 is located in Domanda area on seismic line 812-

DA-08 at Shot Point 660. Seismic line L36-91-01 has a well Ramak-01 at Shot Point

1100 whereas Seismic line L36-91-01 lies in the east of Domanda Fault (fig 1.2).

Formations are correlated with the help of these wells and a north-south cross-section

of Drazinda syncline is prepared.

Interpretation of the Seismic lines

812-DA-08

Interpretation of time & depth sections of 812-DA-08 (fig 4.2 & 4.3) suggests that

Tertiary Formations are present in the core of Drazinda Syncline. Litra (Pliocene),

Vehowa ( Miocene) and Chitarwata (Oligocene) are exposed at the surface. Drazinda

and Pirkoh Formations (Eocene), underlay the Chitarwata formation. The flow of

Drazinda Shales can be observed in the northern part. Domanda and Habib Rahi

Formations are present below Pirkoh Limestone. Baska Shales underlying the Pirkoh

Limestone have thickened in the northern limb of syncline due to the flowage. Most

peculiar behavior is the flowage of Ghazij Shales along the Domanda Fault. This

syncline has a steeper southern limb and thickened northern limb, which indicates the

northwards flowage of shales. The core of Drazinda syncline is present under the SP

457 - SP 475 (fig 4.2). Litra, Vehowa & Chitarwata Formations are exposed at the

surface between SP 285 – SP 585. They have a depth of 1399 m in the core (fig 4.3).

The Average velocity ranges from 2256 m/sec to 2366 m/sec. Drazinda Formation

and underlying Pirkoh Formation are exposed at the surface between SP 105 to SP

285 on the northern limb and SP 585 – SP 595 on the southern limb, which shows the

thinning of limbs towards south. The Average velocity ranges from 2329 m/sec to

2407 m/sec. Drazinda Formation & Pirkoh Formation have a depth of 1769 m in the

core of syncline.

In Domanda Formation & Habib Rahi Formation velocity ranges from 2407 m/sec to

2488 m/sec. They are exposed at the surface between SP 595 to SP 615 on the

southern limb whereas northern limb is not exposed at the surface. Habib Rahi

Limestone attains a depth of 2249m in the core of syncline.

34

Baska Shale is exposed between SP 615 to SP 635 at the southern limb of

Drazinda syncline. In the core it has a depth of 3255 m. Underlying Baska Shale is

Ghazij Formation. Domanda well is drilled in the SE part of the seismic line which

has encountered only Ghazij Formation up to the depth of 3409m.

Fig 4.2 Time Section of Seismic line 812-DA-08

Fig 4.3 Depth Section of Seismic line 812-DA-08

35

L36-91-01

The Quaternary-Eocene (Cenozoic) sediments are correlated with the well data of

Ramak-01, Mesozoic sediments are correlated from well Saro-01 and Paleozoic

sediments are correlated from well Darbula-01. This line has a NW-SE orientation.

Well Ramak-01 is located near SP 1100. The depth section shows Overall 10 Km

(approx.) thick sedimentary cover in the area (fig 4.4 & 4.5). A buried anticline

(Ramak structure) is present between SP 1014 – SP 1214 and a syncline is present

between SP 310 – SP 913.

Vehowa Formation is overlain by Litra Formation (Pliocene), Chaudhwan Formation

(Pliocene) and Alluvium (Pliestocene). Vehowa Formation (Miocene) is thinning in

North. Chitarwata Formation (Oligocene) underlies the Vehowa Formation. It is

thinning in North and pinching under SP 2014 which shows maximum northern

extend of the Chitarwata Formation (fig 4.6). Drazinda Formation of Eocene age

underlies the Chitarwata Formation. It attains a maximum depth of 3918m under SP -

913. It is also observed that Eocene shale has provided a decollement for an overlying

sandstone of the Chitarwata Formation, which has shown an intense fracturing (fig

4.6). Eocene, Paleocene & Cretaceous sediments underlay Oligocene sediments.

Jurassic & Triassic sediments have a maximum depth of 8000 m under SP -813. The

thickenning and thinning at some places is observed by the Mesozoic shales. A

synclinal structure is shown by cretaceous, Jurassic & Triassic formations in south.

Top of Salt Range Formation is at 8449 m under SP -913 (core of the syncline).

Basement is present at a depth of 9000 m (approx.).

36

Fig 4.4 Time section showing the subsurface structures of L36-91-01

Fig 4.5 Depth section showing the subsurface structures of L36-91-01

38

4.3 Central Zone

Safed Koh Block is situated in the tribal areas of district Dera Ghazi khan of Punjab

province and located west of sulaiman foredeep in the Middle Indus Basin of

Pakistan. It is a 100 km north-south trend located in a Fault Propagation Folded

Zone, in the east of Sulaiman fold belt. Safed Koh is exposed as a first line of folding

on the folded flank of Sulaiman Foredeep. To the north it is separated by Pezu

Transverse uplift whereas in the South by Mari Bugti. In the East the Punjab

Monocline is a stable area and the Sulaiman Fold and Thrust belt makes the western

boundary of the area. Dhodak, Rodho, Afiband and Zindapir (fig 4.7) anticlines are

the four culminations of the Safed-Koh Trend.

During 1947- 1957 Pakistan Shell Oil carried the regional studies here. In 1958, POL

& PPL had the concession of the area, but due to the negative results of Domanda and

Giandari wells it was not supposed to be a potential area for Hydrocarbons. Untill

OGDC explored and obtained a commercial gas flow from Cretaceous Pab Formation

and Paleocene (Lower Ranikot & Dunghan Formation) in Rodho well.

Fig 4.7 Satellite imagery showing Zindapir Structure (http://disc.sci.gsfc.nasa.gov)

Dewan Petroleum (Pvt) Ltd., a Pakistani Exploration and Petroleum company and

operator of Safed Koh Block has drilled well at Salsabil (Rodho) structure up to the

depth of 3305 metres and made first discovery of Gas in Chiltan Limestone and in the

Cretaceous Sembar Sands. This discovery is believed to have material impact on the

39

exploration potential of the Safed Koh Block itself in both Rodho and unexplored

structure namely Afiband.

A north-south cross-section of Safed-Koh Trend is prepared fig (4.8). Seismic lines

used are 795-SK-06, 795-SK-06A, 805-SK-17, 805-SK-23, 805-SK-22, 805-SK-26,

855-SK-33, and 785-SK-04.

The results combined with a surface geology are as follows:

Dhodak is the northern lower most culmination. The sediments of Kirthar Formation,

Nari-Gaj Formation and Siwaliks are exposed. It is an asymmetrical anticlinal fold.

The axis is north-south trending. The crest is shifted towards southward in a cross-

section of Safed-Koh Trend. A cross-section shows amplitude of Dhodak structure is

above 500 m and it is separated from a Rodho anticline in south by a narrow syncline.

A Thrust fault cuts the southern limb of Dhodak anticline dips in north. By comparing

the data of Dhodak-01 and Rodho-01 wells, the increase in thickness in Ghazij

Formation is observed northwards.

Fig 4.8 Depth model of Safed Koh Trend

Rodho is the second culmination from north and lower than Afiband anticline. The

crest shifs towards north in the subsurface. The Thrust fault cuts the northern limb of

this culmination dipping in south. The region bounded by these two faults show a

synclinal structure. The northern flank of this syncline is steeper and the southern

40

flank is broader. When the data of Dhodak-01 and Rodho-01 wells is compared the

increase in thickness in Upper Ranikot Formation and Lower Ranikot Formation is

observed southwards (Rodho-01). Dunghan is thinning in Rodho-01.

Afiband is a third culmination of the Safed-Koh Trend. The subsurface picture shows

the broad folded anticline as compare to Rodho and Dhodak (fig 4.8). Crest shifts

towards north in the subsurface cross-section. The northern limb on Afiband anticline

is steeper and the southern limb is gentler. Syncline bounded by the faults is

separating Afiband anticline with Zinda Pir Anticline.

Zindapir is the southern and the most uplifted culmination of the Safed-Koh Trend

(fig 4.7 & 4.8). It’s a broader structure comparatively showing the decrease in

intensity of folding southward.

Petroleum Aspect

Dunghan and Ranikot in this area have already proved to be a good quality reservoirs.

Pab Fm of Cretaceous and Chilton Fm of Jurassic could also be the important

reservoirs in Dhodak & Rodho anticlines. The anticlines are converging with depth

and also the syncline separating them becomes steeper with depth, and the faults near

the crests of Dhodak and Rodho might have provided the migration path for oil/gas,

which has accumulated along their crests and thick Ghazij shales have built up the

high pressure above them. Chilton is not encountered in Rodho and Dhodak wells.

The synclinal structure/ down thrown block buried the source at greater depth for

generation of hydrocarbon. The southward advancing nappes were met with

increasing friction along the Sulaiman Basement Fault. This caused the synclines to

be squeezed out between the anticlines in the Sulaiman Anticlinorium and resulted in

uplift of the Sulaiman Range (Raza and Ahmad, 1990). The erosion of Himalayas

provided the rapid thick deposition of Eocene sediments which resulted in an increase

in the over burden pressure and subsidence of the source rock. Potential source rocks

are the Jurassic shales, Sember shale and Mughalkot Formation of the Cretaceous age

and Dunghan & Ranikot Formations of Paleocene age.

There are close relations between compressive features and strike-slip faults in this

area. Also, based on occurrence of earthquakes between 1966-1994 reveals

concentration of high magnitude earthquakes at a depth of more than 30 kilometers

(fig 4.9). It suggests that the basement of the Indo-Pakistan is involved in structural

41

deformation of Zindapir Anticlinorium and its surroundings (Iqbal and Helmcke,

2004).

Earthquake studies (Quittmeyer et al., 1984) demonstrate that two recent earthquakes

originated in the superficial structures, whereas two other recorded earthquakes

resulted from thrusting in the basement. Such a differentiation between earthquakes is

only possible when the upper layer of the crust has detached itself from the basement.

The regional structure also indicates that the Kingri fault and associated folds are the

result of detachment; the structure is indeed similar to that of other thrust and fold

belts characterized by detachment.

Fig 4.9 Plot of the recent earthquakes of Zindapir area.

Thick Infracambrian evaporates, probably correlative to the Hormuz salts of Iran,

these salt units provided the detachment surface for the apparent décollement

movements.

The successive breaching of the multicolored Tertiary formations of the Zinda Pir

anticline reveals in its core the same Paleocene rocks that host the gas in the Sui

anticline These rocks were the prime target in two wells drilled in the northern end of

the anticline where the Paleocene formations had plunged beneath a cover of younger

Tertiary rocks. Evolution of foreland structures: an example from the Sulaiman thrust

lobe of Pakistan, southwest of the Himalayas (http://disc.sci.gsfc.nasa.gov). A 10 km

thick stratigraphic section outcrops at the deformation front. Available evidence

42

suggests detachment of nearly all the stratigraphic sections from the crystalline

basement (Jadoon et al., 1993).

4.4 Southern Zone

This zone is located in the south of Zindapir culmination of Safed-Koh Trend. Sakhi

Sarwar, Drigri & Kotrum anticlines lie in this zone. The intensity of folding seems to

be decreased in this region. Kotrum is the southern most structure. Seismic lines are

located in Sakhi Sarwar, and NW of Rajanpur of district D.G.Khan, Punjab, Central

Indus Basin of Pakistan. Seismic line 976-FZP-06 lies near a well Sakhi Sarwar-01.

Time and Depth sections show the Sakhi Sarwar Anticline (4.10, 4.11 & 4.12).

Fig 4.10 Time section of 976-FZP-06 (Sakhi Sarwar Anticline).

Fig 4.11 Depth section of 976-FZP-06 (Sakhi Sarwar Anticline).

44

The Time & Depth sections of 914-RPR-03 & 914-RPR-05 show the cross-sections of

Drigri & Kotrum structures respectively (fig 4.13, 4.14, 4.15 & 4.16).

Fig 4.13 Time section of 914-RPR-03

Fig 4.14 Depth section of 914-RPR-03

These structures lie in the SE of Sakhi Sarwar anticline. Folding is prominent in the

cross sections. Cross section of Drigri anticline shows that it is extended E-W over 17

Km approx. and the Thrust Faults are present on both flanks of a fold. Kotrum is

situated between a Sulaiman Range in west and Indus River in east. At surface

Pliocene-Pleistocene strata is exposed. The amplitude of Kotrum is low. When these

45

cross sections are compared with the surface structure it seems that the gentle

anticlinal fold is in the eastern side of 914-RPR-05 and an adjacent broad syncline in

north-west. These anticlines are separated by a Syncline in the NW from Sakhi

Sarwar, as it is located between SP 110-220 of 914-RPR-03 (fig 4.17) and SP 100-270

of 914-RPR-05 (fig 4.18). If these folds are considered to be a part of a same

anticlinal fold then the trend of the fold is in NE-SW direction, with Drigri as a more

uplifted one, showing a plunge in SW. Drigri is a fault propagation fold. These folds

may develop as a result of thrusting to accommodate the deformation above the tip

line of the thrust. This anticlinal fold lies in the south of Zindapir anticline which is a

part of a Safed Koh trend. Also Choti, Karar & Sakhi Sarwar anticlines lie in the N-

NE. Depth sections show that a sedimentary cover of 8 Km approx. is present in the

area. Pliocene-Pleistocene strata is 2000-2200 approx. thick. Nagri & Chinji

Formations 1700 m approx. thick have been deposited (Kotrum-01). Nari Formation

(Oligocene) is overlain by Gaj Formation in the area. Gaj Formation & Nari

Formation are 326m thick in Drigri structure and thickened to 707m in Kotrum

anticline. Their trend is throughout fractured in the section. It could be due to the

flowage of intraformational clay or the underlying Drazinda shales have provided the

decollement. A very strong reflector of Habib Rahi Limestone is present with a

fracture visible under SP 200 in 914-RPR-03 (fig 4.13) and SP 260 in 914-RPR-05

(fig 4.14). Thickness of Habib Rahi Limestone is increasing in south (38 m in Drigi-

01 and 76 m in Kotrum-01). The interesting feature is of flowage of shales of Ghazij

Formation (500 m approx.), Upper Ranikot Formation and Lower Ranikot Formation

from 2.3 – 3.0 seconds in west of the seismic section 914-RPR-03 (fig 4.17). They are

thickening in west which is a very prominent feature in the seismic section. Another

very prominent feature is a fracture in Pab Formation under SP 280 in 914-RPR-03.

Either the depression is a subsidence due to overburden of Ghazij Formation &

Ranikot Formation as they have thickened in west or it could be an unconformity.

There is a transition zone as the Lower Ranikot Formation thins in east (fig 4.17).

Eocene & Paleocene sediments are 1300 m & 800 m approx. respectively

thick.Cretaceous, Jurassic and Triassic sediments are correlated from the east with a

Well Bahawalpur East-01. Basement is uplifted in the east.

46

Fig 4.15 Time section of 914-RPR-05

Fig 4.16 Depth section of 914-RPR-05

49

4.5 Interpretation of the Sulaiman Foredeep & Punjab Platform Area

The seismic lines present in the Sulaiman Foredeep and Punjab Platform area are

interpreted in this section.

4.6 Interpretation of First E-W Profile

845-LEA-114 is at a most uplifted northern edge of research area. It shows a

sedimentary wedge which is 0-4 sec thick in Sulaiman Foredeep (fig 4.19, 4.20 &

4.21).

Fig 4.19 Time section of 845-LEA-114 showing a sedimentary wedge of Paleocene-

Pre-Cambrian strata uplifted and then eroded.

Fig 4.20 Depth section of 845-LEA-114 showing a sedimentary wedge of Paleocene-

Pre-Cambrian strata uplifted and then eroded.

51

The major Angular (erosional) unconformity in the area is present between the

Eocene – Siwaliks sediments and underlying sediments of Paleocene, Mesozoic,

Paleozoic and Pre-Cambrian age. This is marked at 0.65 sec at SP 170 (fig 4.19). At

SP 1970 Cretaceous strata is truncating. Top Jurassic is terminating at SP 1820. The

rest of the strata continue till the Permian truncation. Under SP 1580 the Top Permian

also terminates against the unconformity. Below SP 1430 the Top Cambrian truncates

against the unconformity and also it is thinning in west. There is an incised valley

between these two truncations (fig 4.21 & 4.22).

Fig 4.22 Incised Valley in the Permian Strata (zoomed image of 845-LEA-114).

Under Sp2090 – Sp2450 Paleocene rocks underlie the unconformity. This event

marks the Shelf Margin of Paleocene time (fig 4.20 & 4.23).

Fig 4.23 Paleocene age Shelf Margin which is uplifted at the time of collision of

Indian Plate (zoomed image of 845-LEA-114).

52

In the eastern end (Punjab Platform) Siwaliks overlie the Salt Range Formation

unconformably. The decollement and faulting is observed in the salt (fig 4.24).

Fig 4.24 Siwaliks Unconformably overlie Salt Range Formation in the Punjab

Platform (zoomed image of 845-LEA-114).

The uplift is also visible below the basement (fig 4.21). Strata present in west is thick

for Pre-Cambrian which abruptly thins in east which is visible on the seismic section.

The basement is marked within these sediments in order to follow the general trend,

suggesting the presence of Pre-Cambrian sediments (apart from Salt Range

Formation) equivalent to those of Oman & India. In west the deep burial of sediments

is favorable for the source rock maturation and hydrocarbon generation. The presence

of thick strata of Pre-Cambrian age suggests their presence under Sulaiman Fold &

Thrust Belt and Sulaiman Foredeep. There is a possibility of detachment surface at

this level under the Sulaiman Range and Kirthar Range. This inference is based on the

unique structural style and arrangement of lobes and orocline in aforesaid ranges (low

surface slope, large width of the fold and thrust belt and the gentle folding of the

Sulaiman Lobe and Karachi Arc) (Kadri, 1995). Heavy oil discovery in Baghewala-1

in 1991 in Bikaner-Nagur Basin, Rajasthan India, from Infracambrian sandstone and

carbonates has renewed exploration activity for Infracambrian play (Hasany et al.,

2007). Basement is uplifted from 8000 m in west to 600 m in east (fig 4.20).

53

956-DIK-32 & 956-DIK-32A show Eocene has an unconformable contact with the

overlying Litra Formation (Pliocene). In eastern end Litra Formation thins and

pinches out (fig 4.25). Paleocene, Mesozoic and Paleozoic sediments are uplifted in

East. Cambrian formations are thinning in west. Decollement is observed in Pre-

Cambrian sediments, as it’s a peculiar feature of Salt (fig 4.26).

fig 4.25 Depth Section of 956-DIK-32

In seismic line 956-DIK-32A Chitarwata Formation (Oligocene) and Vehowa

Formation (Early Miocene) are pinching in east, marking the eastern boundary of

Oligocene sediments, as they are absent in east (fig 4.27 & 4.28). Chitarwata &

Vehowa are termed as Nari & Gaj respectively.

55

Fig 4.27 Time section of 956-DIK-32A

Fig 4.28 Depth section of 956-DIK-32A

The deposition of Vehowa Formation has been recognized as a river-dominated delta

system. The Chitarwata and overlying Vehowa Formations span an important interval

of tectonic history recording the character of Himalayan foreland basin sedimentation

during the obduction of the Indian and Asian plates in western Pakistan, with regional

transition from marginal marine to fluvial environments, and the rise of the high

56

Himalayas. Previous investigation of the lithostratigraphy in the foothills of the

Sulaiman Range at Dalana in Zinda Pir Dome (Downing et al., 1993) indicates the

Chitarwata Formation is dominated by coastal paleo-environments. In ascending

order, the three units are associated with estuary, strandplain and tidal flat

environments. The Vehowa Formation represents the prominent development of

fluvio-deltaic sedimentation related to the southward progradation of the Indus River

system.

On the basis of paleomagnetic data, the age span of the Chitarwata Formation in the

Zinda Pir Dome has been evaluated as early Miocene from 22.3 –18.6 Ma (Friedman

et al., 1992) and currently Oligocene at its base and earliest Miocene at the contact

with the Vehowa Formation (Lindsay et al., 2005).

Chitarwata/Nari Formation tends to end under SP 520 and Vehowa Formation pinches

out under SP 610 (fig 4.28). The overlying Litra Formation (Pliocene) & Chaudhwan

Formation are fairly thick almost 1300 m &1500 m respectively. Alluvium is 600 m

thick. There is an angular unconformity between Litra Formation (Pliocene) &

Vehowa Formation (Miocene). Between SP 610 to SP 648 at time 2.3 sec the Eocene

sediments directly lie below the Litra Formation (fig 4.27). Paleocene, Mesozoics and

Paleozoics continue to uplift in East (fig 4.29). Another interesting feature is the

Detachment level at 4.6 sec in the Pre-Cambrian rocks. Also the Permian & Cambrian

strata is being cut by this detachment. This confirms the presence of Pre-Cambrian

rocks under the Sulaiman Ranges.

58

4.7 Interpretation of Second E-W Profile

835-LEA-107 represents a very interesting subsurface picture. Uplift of Sargodha

High, Unconformities, Salt dome, carbonate buildup /mound and a Shelf margin

structures are interpreted. Time section shows a major uplift of strata after Paleocene

age. Triassic sediments onlap on Permian sediments (fig 4.30).

Fig 4.30 Time section of 835-LEA-107

60

Sediments along with the basement are uplifted in the east towards Sargodha High.

Basement uplift is visible at 1.5 sec under SP 2440 and in west at 4.8 sec under SP100

(fig 4.30 & 4.31). Sargodha Ridge is seismically active and belongs to Punjab seismic

zone of Seeber & Armbruster (1979) that includes the Hissar Ridge and extends to

Dehli, India (Menke & Jacobs, 1976, Talent & Mawson 1982, Dolan et al. 1987)

indicate that a Geosyncline extended to the north and northwest far beyond the MBT.

Sources of pelitic and clastic deposits in the Geosyncline since the Late proterozoic

were the Indian Shield and its structurally elevated Pre-Cambrian elements. Yeats and

Lawrence (1984) explained the tectonic configuration of the Sargodha Ridge as an

outer “swell” that had risen as a result of bending-moment stresses generated by

loading of the Indian Shield by the Himalayan thrusts. Earlier Lefort (1975) had

suggested that tectonic activity along the Sargodha Ridge represents a new thrust fault

forming an incipent subduction zone after the buoyancy constraints did not allow

further subduction within the Himalayas.

The Time section of 835-LEA-107 illustrates a continuous deposition of Pre-

Cambrian in the area (fig 4.30). The Salt Range Formation is correlatable

chronologically and lithologically to the Hormuz series and Huqf Group of Iran.

(Kadri, 1995). A large number of oil and gas fields, including the giant ones, have

been discovered in the Infracambrian rocks of the Siberian Platform and Oman.

Infracambrian oil from Oman has strong resemblance and considered to be

comparable source type as found in the heavy oil of Karampur-1 and oil seepage of

Salgi Nala, Salt Range, Punjab (Hasany et al., 2007). Pre-Cambrian sediments in fig

4.31 and fig 4.32 are prominent which is not a Salt Range Formation but the

sediments of equivalent age.

Cambrian formations are deposited over Pre-Cambian with basin orientation as north-

south at that time and the westward thinning in the section marks the western edge of

basin. During Permian the deposition was not uniform and at that time the uplift of

Sargodha High must have began as the onlaps of Triassic sediments on Permian

explains the fact. This event at time 0.5 sec under SP 2410 is a Permo-Triassic

boundary and Triassic onlaps are marked (fig 4.32).

61

Fig 4.32 Permo-Triassic Unconformity in the east towards Punjab Platform (zoomed

image of 835-LEA-107)

This shows that towards the Sargodha High the sediments of Jurassic & Triassic age

were not deposited and it was already uplifted at that time because these sediments are

thinning and then onlaps on Permian sediments. Cretaceous & Paleocene sediments

almost ends up under SP 2020 (fig 4.30 & 4.31). Well Saro-01 lies in south and it also

confirms 62 m thick Early Cretaceous (Lumshiwal & Chichali Formations) and 11 m

thick Paleocene sediments. There is another unconformable surface between Middle

Jurassic (Samana Suk Formation) and Early Cretaceous (Chichali Formation) (fig

4.33). In the south of SP 1400 well Kamiab-01 was drilled. When the data is

correlated under SP 1400 Ghazij Formation is very thin and this also ends under SP

1960. This is also confirmed as Ghazij Formation is not encounterd in Saro-01.

Chorgali & Sakesar Formations overlying Ghazij Formation have already pinched out

in east and south of SP 1400 (fig 4.30 & 4.31).

62

Fig 4.33 Jurassic & Cretaceous onlaps are visible (zoomed image of 835-LEA-107).

In eastern part of seismic line (fig 4.31) an intrusion underlying the basement is

visible. The bulge in the base of Pre-Cambrian rocks is obvious at 1.5 sec in east. In

the southeast, uplift and erosion were accompanied by the Deccan trap volcanism

(Bender & Raza, 1995).

Pre-Cambrian sediments show a change in lithology against the Salt Range

Formation. This tremendous amount of strata must have deposited in west against Salt

Range Formation and it appears at 5 sec in the seismic sections of 845-LEA-114, 835-

LEA-107, 836-LEA-06 and 836-LEA-07 (fig 4.21 & 4.31).

Towards Punjab Monocline the sedimentary cover is less than 2 km thin and it is

more than 9 km thick in a Sulaiman Foredeep area (fig 4.34). Between SP 1310 - SP

1340 a set of normal faults appears. There is a presence of a Salt dome (fig 4.35).

Normal faults of local extent are generally associated with other structures whose

geometry requires extension of crustal layers, e.g. domes etc. structural domes cut by

a system of normal faults commonly result from the intrusion of bodies of salt or

magma. The faults radiate from the center of the dome and may include a single major

fault, one or two grabens or a Y shaped set of grabens. At depth the faults terminate at

or near the margin of the dome (Twiss & Moores, 1992).

63

Fig 4.34 Depth section of 835-LEA-107.

Fig 4.35 Salt dome and an associated Graben structure (zoomed image of 835-LEA-107).

64

Cambrian and Pre-Cambrian strata show a carbonate buildup (fig 4.36). Carbonate

buildups, including reefs and banks, are ideally suited for stratigraphic interpretation

from reflection seismic data because of pronounced differences in depositional or

bedding characteristics between the buildups and enveloping strata. Bank denotes a

bathymetrically positive sediment accumulation formed by the gregarious growth of

organisms which cause and contribute to sediment deposition but do not form a rigid

structure. Reef is a term used for bathymetrically positive rigid structures formed by

sedentary, intergrowing organisms. The direct geophysical criteria that allow

recognition of buildups are those seismic parameters that directly outline buildups

such as reflections from the boundaries of the buildups, onlap of overlying cycles, or

seismic facies changes between the buildups and enveloping beds.

Fig 4.36 Shelf Margin Carbonate buildup of Pre-Cambrian age (zoomed image of 835-LEA-107).

Carbonate buildups, including reefs and banks, form important and prolific

hydrocarbon reservoirs in many operating areas of the world, particularly in the US,

Canada, North Africa, Mexico, Southeastern Asia and the Middle East.

Carbonate buildups are grouped into four major types,

Barrier buildups: They are linear, with relatively deep water on both sides during

deposition.

65

Pinnacle buildups: They are equidimensional and were surrounded by deep water

during deposition.

Shelf-margin buildups: They are linear, with relatively deep water on one side and

shallow water on the other side during deposition.

Patchup buildups form in shallow water, either in a close proximity to shelf-margins,

or over broad, shallow seas (Bubb and Hatlelid, 1977).

It seems this is a shelf margin buildup as the onlaps are marked.

Another interesting structure present is the shelf margin of Paleocene age and a very

strong reflection is generated from here (fig 4.37).

Fig 4.37 Shelf Margin of Paleocene age (zoomed image of 835-LEA-107).

This is an important structure for the Hydrocarbons prospect. This lies in the

Hydrocarbon generation Zone. The depth of burial shows Source rock maturation

zone. The strong reflector can act as a Reservoir. Also overlying seal is present.

66

L36-91-20 The subsurface cross-section shows an uplift of 9 km thick sediments in

west. Basal detachment is provided by the Pre-Cambrian sediments (fig 4.38).

Fig 4.38 Time section of L36-91-20

Another interesting feature is the fractured/fragmented reflector of Chitarwata

Formation (fig 4.39) and flowage of underlying Drazinda Shale (Eocene), which is

also visible in L-36-01 (fig 4.6). It is marked and correlated by well Ramak-01. It

shows the flowage of shales due to intense deformation. Also other flowages among

Ranikot shales (Paleocene) & Mesozoic shales are present (fig 4.39).

68

Fig 4.40 Depth section of L36-91-20

The Paleozoic sediments terminate against the Pre-Cambrian detachment level under

SP 900 and again restore at SP 550 in west (fig 4.40). This shows a ramp-flat

geometry of Sulaiman Basement Fault. This is Normal Fault with ramp-flat geometry

and the Fault bend anticline is produced. If a flat connects two more steeply dipping

segments of the fault, slip produces a fault-bend anticline which is compatable in part

to a rollover anticline. (Twiss & Moores, 1992).The ramp is visible in the section (fig

4.40).

On the western end of line there is a thrust fault which belongs to a Domanda Fault

System. A resistance is provided by the Sulaiman Basement Fault and the Ghazij

shales have flowed along the Domanda Fault plane. They are exposed at the surface

and continue at a depth of more than 3500m approx in well Domanda-01 (north).

4.8 Interpretation of Third E-W Profile

This is a deeper part of the basin showing thick Siwaliks (Late Miocene - Quaternary)

& Eocene, thin Paleocene & Cretaceous sediments. The overall trend is an increase in

thickness of Mesozoic & Cenozoic sediments towards Sulaiman Foredeep. Presence

of a Sulaiman Basement Fault in the west is also indicated.

70

Interpretation of PSPD-80-23, 836-LEA-06 & LMT-17

Seismic line PSPD-80-23 (fig 4.41) is correlated with wells Nandpur-01, Panjpir-01

and Sarai Sidhu-01 in south. The major unconformity marked is at Base Miocene.

Eocene & Paleocene are very thin in this area (fig 4.42).

Fig 4.42 Time section of PSPD-80-23

Mesozoic sediments show a syncline under SP-1290 to SP-1330 (fig 4.42 & 4.43).

Sediments contained within this structure give good reflections.

71

Fig 4.43 Cretaceous age synclinal structure on zoomed image of PSPD-80-23

Another important feature is a presence of very sharp reflection from the Cambrian

Khewra Sandstone Formation, which gradually dies out (down lap) under SP-1290

(fig 4.42 & 4.44).

Fig 4.44 Cambrian downlap on Pre-Cambrian on zoomed image of PSPD-80-23

72

Fig 4.45 Depth cross section of PSPD-80-23

Cambrian pinchout is not marked here. Generally the sediments are uplifted in east

(fig 4.45). Sedimentary cover is 6 km thick in west.

836-LEA-06 lies in west of PSPD-80-23. This shows the fragmented reflectors of

Cretaceous, Jurassic & Triassic in east (fig 4.46). Eocene & Paleocene strata is very

thin in the area. Permian & Cambrian thins towards west considerably (fig 4.47).

Whereas Pre-Cambrian does not seem to vary in thickness.

74

Fig 4.47 Time section of 836-LEA-06

Fig 4.48 Depth section of 836-LEA-06

Nagri Formation overlies Chinji Formation. Nagri & Chinji Formations are quite thick

i.e. 2600 m in west and 1100 m in east (fig 4.48). 1700 m thick Chinji is deposited in

west and it remains almost 200 m in east. Cretaceous is approx. 800m thick. Jurassic

& Triassic is having a thickness of 1000 m approx. in the area. Basement is uplifted in

75

east from 4.5 sec to 3.0 sec and from 8 km in west to 4.5 km in east. It seems that

Permian & Cambrian strata ends against Pre-Cambrian strata at 4 sec in west under

SP 720 (fig 4.48), similar to the northern lines 956-DIK-32A & L36-91-20.

C95-LMT-17 Time section shows there is a fault along the western margin (fig 4.49).

This indicates the presence of Sulaiman Basement Fault as the sediments terminates

against it. The Eocene shales have flowed along the fault (fig 4.50 & 4.51). Sediments

are not visible on left hand side of the fault. Safed Koh Trend is located in the

immediate west of this seismic line. Culminations of this trend are the detached

sediments.

Fig 4.49 Time section of C95-LMT-17

77

Fig 4.51 Depth section of LMT-17

4.9 Interpretation of Forth E-W Profile

Interpretation of 836-LEA-07 & LMT-15

836-LEA-07 lies in the southern part. Thick Cretaceous, Jurassic & Triassic are

deposited (fig 4.52). Permian & Cambrian are thinning and they merge into Pre-

Cambrian rocks at the western end of line. LMT-15 (fig 4.53) lies in west of 836-

LEA-07. Top Eocene is unconformable with overlying Chinji Formation (Miocene).

An event between 3.0 – 3.2 sec under SP 111 SP 271 is a shelf margin of Paleocene

time which has been deformed due to folding and subsidence (fig 4.53, 4.54 & 4.55).

Data shows folding throughout in Mesozoic and Pre-Cambrian sediments (fig 4.56)

due to a collision of Indian Plate and a resistance provided by a Sulaiman Basement

fault present at the western end.

80

Fig 4.54 Shelf margin of Paleocene age on zoomed image of LMT-15

Fig 4.55 Shelf margin of Paleocene age on zoomed image of LMT-15

81

Fig 4.56 Westward flexure and folding of Paleozoic & Mesozoic sediments on

zoomed image of LMT-15.

4.10 Interpretation of Fifth E-W Profile

This is a 205 km profile correlating the sediments between wells Bahawalpur East-01

(east) and Drigri-01 & Kotrum-01 (west). This part of the Central Indus Basin

displays a very different situation as compare to First & Second E-W profiles. The

Eocene & Post Eocene sediments are thick (fig 4.57). Paleocene & Cretaceous are

thin, even pinch out over Jurassic strata in east (fig 4.58). Jurassic & Triassic

sediments show the deposition with no relation with the Permian/Cambrian Paleo-

high (fig 4.58).

82

Fig 4.57 Depth model of the subsurface from Bahawalpur East-01 to Drigri-01

916-YZM-05 is correlated with well Bahawalpur East-01. Here the Paleocene &

Cretaceous thins in east and onlaps on Jurassic strata (fig 4.58). Bahawalpur East-01

is drilled over an asymmetrical anticlinal structure present in Base Permian/Top

Cambrian (fig 4.58). Cambrian is over 400 m thick & Pre-Cambrian is more than 800

m. Paleozoic shows a high from SP 152- SP 602 (fig 4.58).

84

Fig 4.59 Zoomed image from Seismic section of 916-YZM-05 showing a presence of

a Paleohigh.

Eocene & Mesozoic sediments deposited after the deformation and shows no signs of

Paleo-high (fig 4.60).

Fig 4.60 Zoomed image from Seismic section of 916-YZM-05 showing onlaps of

Cretaceous & Paleocene over Paleohigh.

85

This indicates that Jurassic sediments deposited (fig 4.60) over the Paleo-high unlike

the Sargodha high over which the Jurassic & Triassic sediments onlap. Also

Cretaceous and Paleocene sediments are thinning suggesting again uplift after

deposition of Jurassic and Triassic sediments. Lower Permian sequences are reported

as source and reservoir in Oman, Saudi Arabia, Australia, and India. (Ahmad et al.,

2007).

PSPD-5085

The most prominent feature is in Permian strata. It could be a feature of outbuilding of

delta. The eroded segments deposited down slope and they are visible in the seismic

section PSPD-5085 (fig 4.61, 4.62 & 4.63). This shows the erosion and the reworking

of sediments during the deposition of Permian sediments.

Fig 4.61 Out building of Delta in Permian age on zoomed image from Seismic section

of PSPD-5085.

86

Fig 4.62 Reworking of sediments is prominent on zoomed image from Seismic

section of PSPD-5085

Marine environment prevailed gradually during the deposition of Sardhai Formation.

Then Clastics of Nilawahan Group give way to the carbonates of Zaluch Group with

the development of Permian basin.

Jurassic & Triassic sediments overlay the Permian. The photographs published in the

Proceedings of Annual Technical Conference, 2007 by Ahmad et al., (2007) show the

cross bedded sandstone and coal in delta facies of Tobra Formation and fresh water

facies of Tobra Formation, showing boulder. It suggests the deltaic environment

during their deposition. While the cross bedding suggests the activation of erosional

phenomena.

89

PSPD-5340 shows under SP-445 a very prominent feature of flexure (fig 4.64 &

4.65). The Jurassic & Triassic along with the Permian shows same reflection pattern

as in PSPD-5085 and 916-YZM-05.

Fig 4.65 Effect of flexuring in west on zoomed image of Seismic section of PSPD-

5340.

90

C95-LMT-05 shows a Listric normal fault. Listric fault is the one with curved fault

surface and the dip decreases with depth. Also the drag folds occur in the hanging

wall as the foot wall bends down and hanging wall bends up in order to maintain the

contact. With the increasing depth it turns into rollover anticline (Twiss & Moores,

1992). This fault cuts upsection from Basement to Eocene strata (fig 4.66 & 4.67).

Fig 4.66 Zoomed image of Eocene and older sediments (C95-LMT-05).

92

Resistance provided by Sulaiman Basement Fault in west produces flexures in

subsurface sediments and these flexures are prominent in various seismic sections

(4.56, 4.66 and 4.67).

954-FZP-09 lies in Fazilpur area. The data quality is not so good (fig 4.68). The

general stratigraphic successions are marked.

914-RPR-03 shows Drigri is a broad anticline where all the formations are folded.

Very thick Siwaliks including Dhok Pathan (Pliocene), Nagri (Pliocene) and Chinji

(Miocene) Formations are deposited in this area of Rajanpur. Gaj & Nari Formations

are lying below Siwaliks. Under lying Eocene shales are very prominent. Lower

Ranikot shales thinning and pinching into Pab Formations are also noticeable. Pab

Formations is fractured and the faults are marked making a pop up structure (fig

4.17). This area is a Fault propagation folded zone of Sulaiman fold and thrust belt.

914-RPR-05 line shows the cross-section of Kotrum anticline which is low

amplitude fold (fig 4.18) with an adjacent syncline. Pab Formation is fractured. Lower

Ranikot is thinning in east and merges into Pab Formation.

954-FZP-05 is a north-south oriented line crossing FZP-09 & FZP-06. It is used for

correlation purposes (fig 4.68).

976-FZP-06 shows a cross-section of Sakhi Sarwar anticline. A flower structure is

present in the core (fig 4.12).

94

4.11 Interpretation of Sixth N-S Profile

804-DK-06 & 06A 804-DK-06 shows an unconformity (Base Miocene) between

Siwaliks and Eocene. Jurassic & Triassic are terminated against angular unconformity

(fig 4.69 & 4.70). Basement lies at 4500 m under SP 110 and at 500 m at the northern

end of profile.

Fig 4.69 Time section of 804-DK-06 & 06A

Fig 4.70 Depth section of 804-DK-06 & 06A

96

A seismic section of 804-DK-06 shows uplift in north towards Pezu Uplift (fig 4.71)

Permian Strata shows a bulge against an unconformity along eastern wedge and an

effect of folding below an unconformity is present (fig 4.72).

Fig 4.72 Folding in Paleozoic and Pre-Cambrian sediments and a bulge in Permian

sediments shown on zoomed image of seismic section of 804-DK-06

Decollement in Salt Range Formation (Pre-Cambrian) is a prominent feature (fig

4.73).

Fig 4.73 Zoomed image of seismic section of 804-DK-06 showing decollement in

Pre-Cambrian sediments

98

804-DK-06A is an extension of 804-DK-06. Seismic section of 804-DK-06A (fig

4.74) shows a sedimentary wedge in north towards Pezu Uplift. Paleozoic and Pre-

Cambrian sediments are uplifted and Siwaliks rest unconformably over them. From

SP 430 – SP 580 Cambrian strata has an unconformable contact with Siwaliks. From

SP 580 – SP 830 Salt Range Formation under lies the unconformity (fig 4.69 & 4.70).

A syncline in Permian strata is present between SP130 – SP 280 against an

unconformity (fig 4.75).

Fig 4.75 Zoomed image of seismic section of 804-DK-06A shows Permian syncline.

From SP 630 – SP 830 Salt Range Formation underlies the unconformity (fig 4.70 &

4.76).

Fig 4.76 Zoomed image of seismic section of 804-DK-06A shows Salt Range

Formation (Pre-Cambrian) lies unconformably below Siwaliks in northern end.

99

Permian, Cambrian and Pre-Cambrian sediments show a synclinal structure. Pre-

Cambrian sediments equivalent to Salt Range Formation are visible at the southern

end of 804-DK-06A (fig 4.77).

Fig 4.77 Zoomed image of seismic section of 804-DK-06A shows Pre-Cambrian

sediments in south which is not Salt Range Formation but the sediments of equivalent

age.

4.12 Interpretation of Seventh N-S Profile

804-DK-04 Time & Depth sections of 804-DK-04 show a sedimentary wedge uplifted

in north (fig 4.78 & 4.79). Pre-Cambrian sediments underlay Siwaliks unconformably

(fig 4.80)

Fig 4.78 Time section of 804-DK-04

100

Fig 4.79 Depth section of 804-DK-04

Sedimentary wedge is present in the subsurface (fig 4.80) and sediments are uplifted

in north towards Pezu Uplift. Pre-Cambrian sediments underlay Siwaliks

unconformably in Punjab Platform (fig 4.81). Decollement due to Salt is also visible

at the northern end of seismic section and thick Pre-Cambrian sediments equivalent to

Salt Range Formation are present towards the southern end (fig 4.82).

102

Fig 4.81 Salt Range Formation lies below Siwaliks showing decollement in zoomed

image of seismic section of 804-DK-04.

Effect of folding is present in sediments of Mesozoic, Paleozoic and Pre-Cambrian

age (fig 4.82 & 4.83). This folding is not present in the younger sediments that lies

above an unconformity. The cause of folding is a pre-uplift event (fig 4.82).

Transition from Salt Range Formation in northern end (fig 4.81) to sediments of

equivalent age towards southern end (fig 4.82) is very clear (fig 4.80). Pre-Cambrian

sediments are getting thicker in south.

103

Fig 4.82 Mesozoic and Paleozoic sediments are uplifted in north and terminating

against an angular unconformity in zoomed image of seismic section of 804-DK-04

(Thick Pre-Cambrian sediments are also visible)

Fig 4.83 Mesozoic, Paleozoic and Pre-Cambrian sediments show folding below an

angular unconformity in zoomed image of seismic section of 804-DK-04

104

4.13 Interpretation of Eighth N-S Profile

956-DIK-11 shows a 7 km thick sedimentary wedge uplifted in north. It lies in a more

deeper region than the Sixth and Seventh N-S profile (fig 4.84 & 4.85).

Fig 4.84 Time section of 956-DIK-11

Fig 4.85 Depth section of 956-DIK-11

105

956-DIK-12 is an E-W seismic line with the crossings of 956-DIK-11 & 956-DIK-38

on it. Time & Depth cross-sections (fig 4.86 & 4.87) of 956-DIK-12 are also

correlating with the First & Second E-W profiles. The strata is uplifted in east from

7500m to 6500m in east. 956-DIK-38 is a north south seismic line with its southern

end against 835-LEA-107 and northern end crossing 956-DIK-12. Thin Paleocene

sediments are present. Also thin Paleozoic sediments are present. Strata is uplifted in

north (fig 4.88 & 4.89).

Fig 4.86 Time section of 956-DIK-12

Fig 4.87 Depth section of 956-DIK-12

106

Fig 4.88 Time section of 956-DIK-38

Fig 4.89 Depth section of 956-DIK-38

107

4.14 Interpretation of Nineth N-S Profile

Wells Piranwal-01, Panjpir-01, Nandpur-01 and Sarai Sidhu-01 lie close to these

lines.

845-KBR-28 shows a sunclinal depression in the Jurassic & Triassic sediments

between SP 256 – SP 385 (fig 4.90). Generally the strata is uplifted in north towards

SP 114.

Fig 4.90 Time section of 845-KBR-28 (SP 114-SP 427)

SP 478 - SP 653 of 845-KBR-28 (fig 4.91) show a thick Chinji Formation (Miocene)

has deposited in the area whereas Eocene, Paleocene and Cretaceous strata is thin.

Mesozoic and Permian strata is forming a large synclinal depression. Basement is

gently dipping in south (fig 4.92).

Fig 4.91 Time section of 845-KBR-28 (SP 478-SP 653)

108

Fig 4.92 Depth section of 845-KBR-28

5.15 Depositional history of the area

Thick Pre-Cambrian sediments are deposited in the area (835-LEA-107, 845-LEA-

114, 836-LEA-06, 836-LEA-07, 804-DK-04, 804-DK-06 & 804-DK-06A). During

the Pre-Cambrian age there was a subsidence (Dolan et al. 1987). Pre-Cambrian

sediments are present in subsurface throughout the research area (956-DIK-32 & 956-

DIK-32A, L36-91-20, L36-91-01, C95-LMT-17, C95-LMT-05, 914-RPR-03 & 914-

RPR-05, 916-YZM-05, PSPD-5340 & 5085, 954-FZP-05 & 976-FZP-06 & 954-FZP-

09). The presence of normal Faults in the Pre-Cambrian strata (804-DK-06 &804-DK-

06A) suggests the extension and subsidence after the deposition. At the end of

Cambrian time there is an uplift followed by erosion as Base Permian and Top

Cambrian level is not very clear in the research area (835-LEA-107 & 916-YZM-05).

Base Permian shows an eroded boundary with Cambrian. During Sargodha High

uplift Permian sediments of continental origin (Nilawahan Group) were deposited

with fluviatile depositional environments. Then the subsidence introduces the shallow

marine shelf region and the deposition of Zaluch Group. The change in the

depositional environment is very obvious in the PSPD-5085. The signs of outbuilding

109

of delta are very much obvious in this seismic section. This eroded the pre-deposited

sediments and then down slope deposited them. A syncline is present under the SP-

100 to SP-220 in Seismic profile 804-DK-06A (It is eroded and Siwaliks

unconformably overlie the syncline). Thickness of Permian sediments is not uniform

in the area showing some tectonic activity in the area (835-LEA-107). The thick

Cambrian & Permian deposition in east and its thinning and pinching in west (956-

DIK-32A, 835-LEA-107, 836-LEA-06, PSPS-5340) suggests a presence of

depocenter in east. In the south-eastern part of research area (916-YZM-05) a

Paleohigh in Paleozoic sediments is present. The sediments of Jurassic and Triassic

were deposited over the Permian sediments and have no relation with Paleohigh.

Paleocene and Cretaceous sediments show the onlap on the Jurrasic sediments (916-

YZM-05 & PSPD-5340) suggesting uplift of Behawalpur High after Jurassic age.

The Sargodha High uplifted during Permian time (Permo-Triassic angular

unconformity of 835-LEA-107) and no deposition of Mesozoics on Sargodha high.

The sea was shifted westward and the onlaps on Permian sediments (835-LEA-107)

strongly suggest the depocenter shifted farther west where the subsidence and rifting

caused the thick Jurassic & Triassic deposition (956-DIK-32A, L36-91-20, C95-

LMT-17, C95-LMT-15, C95-LMT-05). In western part of research area Mesozoic

sediments overlie the Pre-Cambrian sediments. Uplift of Sargodha High continued

which caused farther westward deposition of Cretaceous sediments (835-LEA-107).

During Paleocene - Early Eocene time there is a major uplift in north eastern part of

research area (845-LEA-114 & 835-LEA-107) towards Pezu Uplift. A subsurface

Sedimentary wedge is formed towards Pezu Uplift which is overlain by Siwaliks

unconformably. The sediments of Paleozoic, Mesozoic, Paleocene & Eocene were

greatly uplifted due to an Indian Plate collision with Eurasian Plate. Simultaneously

the intense erosion of these sediments began making major angular erosional

unconformity below which Paleocene – Pre-Cambrian sediments underlies (804-DK-

04, 804-DK-06 & 804-DK-06A, 956-DIK-11 & 956-DIK-12 & 956-DIK-38, 956-

DIK-32 & 956-DIK-32A, 835-LEA-107 & 845-LEA-114). The sediments of Eocene

are thick in west, thin in east and uniform over the central and southern part of

research area (836-LEA-06, 916-YZM-05, PSPD-5340). But the northern part

suggests the stages of uplift and deposition simultaneously during the Eocene

sediments deposition.

110

Fig 4.93 Map showing the north-eastern truncations of the uplifted sediments against

an angular unconformity towards Pezu Uplift.

111

The Indo-Pak Plate collided obliquely with the southern part of the Eurasian Plate

during the Paleocene (Sarwar & De Jong, 1984). It was dissected into three basement

blocks (Bannert and Raza, 1992). The collision resulted in the detachment of the

sediments from the basement at the Pre-cambrian level and formation of Safed Koh

Trend. East Sulaiman Basement Fault and Domanda Fault (C95-LMT-17 and L36-91-

01) mark the boundary between the Sulaiman Range and Sulaiman Foredeep area.

Domanda Fault has a surface lineation of left lateral strike slip fault. It is marking the

eastern boundary of the Sulaiman Fold & Thrust Belt. The flowage of Eocene,

Paleocene and Mesozoic shales is very prominent in 914-RPR-03, 914-RPR-05, 812-

DA-08, L36-91-01. Ghazij shales have flowed along the Domanda Fault. Domanda

Fault System plays a very important part in the structures of the area. Drazinda

Syncline has been formed as a result of the flowage of Ghazij shales (more than 3400

m in well Domanda-01) along the Domanda Fault. The decollement in Chitarwata

Formation (sandstone) due to underlying Drazinda Shale is visible (L36-91-01, L36-

91-20 and 914-RPR-03). While part of research area that lies in east of Sulaiman

Basement Fault shows folding of the Paleocene – Pre-Cambrian sediments due to

compressional forces acting during collision (845-LEA-114 & C95-LMT-15). An

effect of flexuring is present in Mesozoic and Paleozoic sediments in C95-LMT-05 &

PSPD-5340. Time & Depth sections of Drigri and Kotrum anticlines show these are

the low amplitude fault propagation folds.

Safed-Koh Trend and Sakhi Sarwar anticlines are the detached structures having

faulted cores. A flower structure is present in the core shown in the cross-section of

Sakhi Sarwar anticline (976-FZP-06) which suggests wrench tectonics in the area.

The Pre-Cambrian Formation is acting as a basal detachment level in the area.

Sulaiman Foredeep and Punjab monocline act as a separate block from the Sulaiman

Block. Base Siwaliks has an unconformable contact with underlying Salt Range

Formation in Punjab Platform.

An ancient Shelf Margin of Paleocene is marked on fig 5.94. The Paleocene

sediments show a shelf margin (835-LEA-107 & C95-LMT-15).

112

Fig 5.94 An ancient Shelf Margin of Paleocene age is marked on Basemap.

113

Late Oligocene – Early Miocene sediments deposited in the north-western margin of

research area , foothills of Sulaiman Range (DIK-32A, L36-91-01, L36-91-20, C95-

LMT-05, 914-RPR-03, 914-RPR-05). Vehowa Formation & Chitarwata Formation

(Oligocene – Early Miocene) show a shallow marine conditions related to the closing

of Tethys sea. The marine environment began to retreat to the south and the fluvial

environments prevailed in the area bringing the large amount of eroded material from

the north, resulting in the thick deposition of Nagri Formation and Chinji Formation

(835-LEA-107, 836-LEA-06, C95-LMT-05 & C95-LMT-17).

4.16 An overview of the subsurface crustal variations of area with the help of 3D

Two way time models and Depth models

Three dimensional models of the area are constructed using two way time and depth

data of time and depth sections respectively with the help of GIS softwares showing

the sub-surface crustal variations from different directions (fig 4.95 – fig 4.107).

These models represent sub-surface views of different layers with different angles.

Fig 4.95 shows Bahawalpur High is an uplifted area and the sediments are dipping in

west towards Sulaiman Foredeep area where they are thickening and deepening. Fig

4.96 shows a comparison between Sargodha High and Bahawalpur High. Fig 4.97

shows a generalized view of High and Trough areas. Fig 4.98 shows the Basement

uplift towards Sargodha High. Fig 4.99 shows the uplift of Pre-Cambrian sediments

towards Sargodha High and Bahawalpur High from a deep burial in Sulaiman

Foredeep. Uplift and erosion of Permian sediments towards Pezu Uplift is shown in

fig 4.100. Cretaceous, Jurassic and Triassic sediments show non deposition over

Sargodha High. They are uplifted and eroded towards Pezu Uplift, then deeply buried

in Sulaiman Foredeep and again uplifted in Safed Koh Trend and Domanda Anticline

(fig 4.101, 4.102 & 4.103). Eocene and Paleocene sediments lie at two time of 0.51 -

1.67 (sec) in Punjab platform and 1.67 – 2.58 (sec) in Sulaiman Foredeep (fig 4.104 &

4.105). They are uplifted towards Eastern Sulaiman Fold Belt. Paleocene (Dunghan

Limestone) is exposed at the surface in Zinda pir Anticline. Fig 4.106 & 4.107 shows

crustal variations in the region.

114

Fig 4.95 A 3D two way time model of sub-surface between Bahawalpur and Sulaiman

Foredeep showing towards Sulaiman Foredeep the sediments are thickening and

deepening.

Fig 4.96 A 3D model of sub-surface between Sargodha High and Bahawalpur High

showing sediments are uplifted more towards Sargodha High.

Fig 4.97 A 3D model of sub-surface showing the uplifted Safed-Koh trend, Drazinda

Syncline, the depression in Sulaiman Foredeep, uplifted Sargodha and Bahawalpur

Highs.

115

Fig 4.98 A 3D view of Basement showing more uplift in Sargodha High.

Fig 4.99 A 3D view of sub-surface showing uplift of Pre-Cambrian sediments in

Bahawalpur and Sargodha area also a depression in Sulaiman Foredeep area.

Fig 4.100 A 3D view of sub-surface showing Permian strata dipping towards

Sulaiman Foredeep and uplifted in Bahawalpur High and towards Pezu Uplift.

116

Fig 4.101 A 3D sub-surface view showing Triassic sediments dipping in west and

uplifted in Safed-Koh Trend. Towards Pezu Uplift they are uplifted, eroded and

terminated against an unconformity related to an event of collision of Indian plate.

Fig 4.102 A 3D sub-surface view of Jurassic sediments.

117

Fig 4.103 A 3D sub-surface view of Cretaceous sediments.

Fig 4.104 A 3D sub-surface view of Paleocene sediments.

118

Fig 4.105 A 3D sub-surface view of Eocene sediments.

Fig 4.106 A 3D sub-surface view from different directions and orientations.

119

Fig 4.107 A 3D sub-surface view showing crustal variation between Bahawalpur High

and towards Sargodha High.

3D Depth models of the subsurface layers show Sargodha High, Pezu uplift,

Behawalpur High, Sulaiman Foredeep and an eastern part of the Sulaiman Fold Belt

(fig 4.108 – fig4.115). Basement is present at 4742 m in the area middle of

Bahawalpur and Sargodha and at 632 meters towards Sargodha High (fig 4.108).

Cambrian & Permian sediments are uplifting towards Pezu Uplift and Sargodha High

(fig 4.109 & 4.110) and deepening in the region between Bahawalpur High and

Sargodha High (fig 4.111). Jurassic, Paleocene and Eocene are deepening in Sulaiman

Foredeep and again uplifting towards Sulaiman Fold and Thrust Belt. Also they are

uplifting towards Pezu Uplift (fig 4.112, 4.113 & 4.114). Base Miocene Unconformity

is a major unconformity in the area. Fig 4.115 shows its subsurface trend whereas it is

deepening to a depth of 3421 m in the Sulaiman Foredeep area. It is present at a

depth of 632 m in north east of the research area where Salt Range Formation

underlies Siwaliks. and towards west gradually Cambrian, Permian, Triassic, Jurassic,

Cretaceous, Paleocene and Eocene underlies this unconformity (fig 4.115). The

depression in the Sulaiman Foredeep area show the sediments are buried deeply and

again uplifted along the fault plane in a sulaiman Fold Belt.

120

Fig 4.108 A 3D sub-surface view of Basement.

Fig 4.109 A 3D sub-surface view of Cambrian strata.

121

Fig 4.110 A 3D sub-surface view of Permian strata.

Fig 4.111 A 3D sub-surface view of Permian strata between Sargodha High &

Bahawalpur.

122

Fig 4.112 A 3D sub-surface view of Jurassic sediments

Fig 4.113 A 3D sub-surface view of Paleocene sediments.

123

Fig 4.114 A 3D sub-surface view of Eocene sediments showing a trough area towards

Drazinda depression and uplift in the Eastern Sulaiman Fold Belt.

Fig 4.115 A 3D sub-surface view of Base Miocene unconformity.

124

125

Conclusions

Research area is divided into (east-west) Zone A, B, C and D (fig 4.116).

In Zone A thick Cambrian & Permian are deposited. These sediments are thickening

in east. The basin depocenter lies in east in this age. The Jurassic & Triassic are not

deposited in north towards Sargodha high and very thin in the middle on Zone A.

They get thick in southern part of Zone A towards Bahawalpur High.

Zone B is the zone showing thinning of Paleozoic sediments and thickening of

Mesozoic sediments in west. Thick Cretaceous, Jurassic & Triassic are deposited.

They are thinning in east and thickening in west showing the shifting of depocenter in

west.

Zone C is a most interesting one. Vehowa (Miocene) and Chitarwata (Oligocene)

Formations are thinning and pinching in east. They are absent in Zone A & Zone B.

This Zone marks their maximum subsurface extend. Zone C shows presence of an

ancient shelf margin of Paleocene age. The depocenter of Mesozoic sediments lies

here. The Cretaceous, Jurassic and Triassic attain the maximum thicknesses in this

zone. Another interesting feature of this zone is the termination of Paleozoics

(Permian & Cambrian) after thinning in west in the subsurface. The Mesozoics

overlie the Pre-Cambrian rocks in this zone.

Zone D is the zone which marks the eastern edge of Sulaiman Block. Here the

detached sediments are forming the structures due to Sulaiman Basement Fault and

Domanda Fault. In northern part of this zone due to the activity of Ghazij shales along

the Domanda Fault a large asymmetrical syncline is present called Drazinda syncline

which converges in south-east. In central part, Safed Koh Trend shows the four

culminations (Dhodak, Rodho, Afiband and Zindapir) of the detached north south

plunging fold. Zindapir is the most uplifted one.

126

Fig 4.116 Research area is divided into various zones with respect to the depositional

trends.

127

In the southern part of this zone the intensity of folding is decreasing. Sakhi Sarwar is

an anticlinal structure with a flower structure at its core. Drigri and Kotrum are the

Fault propagation folds. Drazinda and Ghazij shales of Eocene, Lower Ranikot of

Plaeocene and Cretaceous shales show the flowage in the core.

Pre-Cambrian is present throughout the area and these sediments could be compared

with the Pre-Cambrian sediments of Oman, Iran etc.

Recommendations

Permian and Cambrian and Pre-Cambrian sediments show a good hydrocarbon

potentials for heavy oil in the eastern part of area (Zone A & Zone B). Cambrian

Pinchout is a very prominent feature on PSPD-80-23. The location of this seismic line

is adjacent to wells Panjpir-01 and Nandpur-01.

A Synclinal structures of Cretaceous (PSPD-80-23 and KBR-28) and Permian (804-

DK-06A and PSPD-5085) age should be explored whereas Salt dome structure and a

Carbonate Buildup (835-LEA-107) are remarkable structures for hydrocarbon

accumulation (heavy oil).

Sandstone and Limestone of Eocene, Paleocene and Mesozoic age can act as good

reservoir in Zone B & Zone C. Northern and eastern Pinchouts of Eocene sediments,

Vehowa Formation and Chitarwata Formation should be explored on L36-91-01 and

DIK-32A respectively.

A Shelf Margin on 845-LEA-114, 835-LEA-107, C95-LMT-15 and 914-RPR-03

shows a strong reflector (acting as a reservoir) and poor reflectors (shales acting as

seal and cap) are lying above and below it. This structure has never been located and

explored before.

Dunghan and Ranikot Formations of Paleocene, Pab, Chiltan & Alozai Formations of

Mesozoic act as a good reservoir rocks in Zone D whereas the overlying shales

provide the good seals. The sources are also buried deep in order to attain the maturity

levels in the Sulaiman Foredeep area.

128

129

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135

Correlation of 914-RPR-03 with the Synthetic prepared from well data of Drigri-01.

136

Correlation of L36-91-01 with the Synthetic prepared from well data of

Ramak-01.

137

WELL TOPS

well Name DRIGRI-01 Type EX Status ABD

Operator OGDC Spud date 02/09/1992 Compl.date 28/11/1992

Depth(m) 3250.0 Latitude 29 22 04.92 Longitude 70 10 54.28

K.B.E 149.02 Province PUNJAB Formation GHAZIJ

Sr.no Formation Age Formation Top(m) Thickness(m)1 PLIOCENE DHOK PATHAN 0.0 847.0 2 PLIOCENE NAGRI 847.0 1011.0 3 MIOCENE CHINJI 1858.0 406.0

4 OLIGOCENE-

MIOCENE GAJ-NARI 2264.0 326.0

5 EOCENE DRAZINDA 2590.0 302.0 6 EOCENE PIRKOH 2892.0 22.0 7 EOCENE SIRKI 2914.0 225.0 8 EOCENE HABIB RAHI 3139.0 38.0 9 EOCENE GHAZIJ 3177.0 73.0

WELL TOPS

well Name RODHO-01 Type EX Status ABD

Operator OGDC Spud date 26/09/1972 Compl.date 04/12/1973

Depth(m) 189.6 Latitude 30 44 27.00 Longitude 70 26 32.00

K.B.E 582.00 Province PUNJAB Formation GHAZIJ

Sr.no Formation Age Formation Top(m) Thickness(m)

1 EOCENE KIRTHAR 0.0 25.0 2 EOCENE GAZIJ 25.0 164.6

138

WELL TOPS

well Name SAKHI SARWAR-01 Type EX Status ABD

Operator AMOCO Spud date 10/01/1976 Compl.date 13/10/1976 Depth(m) 4580.9 Latitude 29 55 23.00 Longitude 70 20 03.00 K.B.E 238.43 Province PUNJAB Formation PAB SAND STONE

Sr.no Formation Age Formation Top(m) Thickness(m)

1 MIOCENE-PLIOCENE

NAGRI EQUIVALENT

0.0 878.7

2 MIOCENE-PLIOCENE

CHINJI EQUIVALENT

878.7 1188.7

3 OLIGOCENE CHITARWATA 2067.4 508.7 4 EOCENE DRAZINDA 2576.0 156.0 5 EOCENE PIRKOH 2732.1 150.6 6 EOCENE SIRKI 2882.7 224.3 7 EOCENE HABIB RAHI 3107.0 76.1

8 EOCENE GAZIJ 3183.1 895.9 9 PALEOCENE DUNGHAN 4078.9 96.0 10 PALEOCENE RANIKOT 4174.9 193.1 11 LATE

CRE/EARLY CRE PAB 4368.0 212.9

WELL TOPS

well Name DARBULA-01 Type EX Status ABD

Operator OGDC Spud date 20/12/1989 Compl.date 12/01/1990 Depth(m) 1550.0 Latitude 31 28 09.68 Longitude 71 57 02.67

K.B.E 184.05 Province PUNJAB Formation SALT RANGE

Sr.no Formation Age Formation Top(m) Thickness(m)

1 PLIOCENE SIWALIK 0.0 742.0 2 MIDDLE

CAMBRIAN BAGHANWALA 742.0 41.0

3 MIDDLE CAMBRIAN

JUTANA 783.0 46.0

4 MIDDLE CAMBRIAN

KUSSAK 829.0 105.0

5 EARLY CAMBRIAN

KHEWRA SANDSTONE

934.0 211.0

6 PRE CAMBRIAN

SALT RANGE 1145.0 405.0

139

WELL TOPS

well Name RAMAK-01 Type EX Status ABD

Operator LASMO Spud date 10/02/1993 Compl.date 23/04/1993 Depth(m) 4455.0 Latitude 31 22 40.20 Longitude 70 30 26.50 K.B.E 218.00 Province N.W.F.P Formation DRAZINDA

Sr.no Formation Age Formation Top(m) Thickness(m)

1 RECENT ALLUVIUM 7.9 592.1 2 LOWER

PLIOCENE-EARLY

PLEISTOCENE

CHAUDWAN 600.0 1278.0

3 EARLY –MIDDLE PLIOCENE

LITRA 1878.0 1555.0

4 OLIGOCENE-EARLY

PLIOCENE

VEHOWA 3433.0 630.0

5 OLIGOCENE CHITARWATA 4063.0 286.0 6 EOCENE DRAZINDA 4349.0 106.0

WELL TOPS

well Name DHODAK-01 Type EX Status CON

Operator OGDC Spud date 12/06/1975 Compl.date 17/12/1977 Depth(m) 2133.0 Latitude 30 55 20.45 Longitude 70 22 39.00 K.B.E 514.00 Province PUNJAB Formation PAB SANDSTONE

Sr.no Formation Age Formation Top(m) Thickness(m)

1 EOCENE DRAZINDA-PIRKOH-DOMAND

0.0 480.0

2 EOCENE HABIB RAHI 480.0 30.0 3 EOCENE ALABASTER

SHALE 510.0 138.0

4 EOCENE RUBBLY LIMESTONE

648.0 296.0

5 EOCENE GHAZIJ SHALE

944.0 864.0

6 PALEOCENE DUNGAN 1808.0 26.0 7 EARLY

PALEOCENE UPPER

RANIKOT 1834.0 95.0

8 EARLY PALEOCENE

LOWER RANIKOT

1929.0 150.0

9 UPPER CRETACEOUS

PAB SANDSTONE

2079.0 54.0

140

WELL TOPS

well Name PANJPIR-01 Type EX Status GAS

Operator OGDC Spud date 02/10/1984 Compl.date 03/04/1985

Depth(m) 2120.0 Latitude 30 41 02.81 Longitude 71 57 29.40 K.B.E 142.37 Province PUNJAB Formation TREDIAN

Sr.no Formation Age Formation Top(m) Thickness(m)

1 PLIOCENE NAGRI 0.0 620.0 2 MIOCENE CHINJI 620.0 706.0 3 EOCENE SAKESAR 1326.0 0.0

4 EOCENE NAMMAL 1326.0 34.0 5 OLIGOCENE GHAZIJ SUI

MEMBER 1360.0 161.0

6 PALEOCENE DUNGHAN 1521.0 21.0

7 PALEOCENE RANIKOT 1542.0 60.0 8 EARLY

CRETACEOUSLUMSHIWAL 1602.0 70.0

9 EARLY

CRETACEOUSCHICHALI 1672.0 55.0

10 MIDDLE

JURASSIC SAMANA

SUK 1727.0 127.0

11 MIDDLE JURASSIC

SHINWARI 1854.0 77.0

12 EARLY JURASSIC

DATTA 1931.0 18.0

13 EARLY JURASSIC

KINGRIAL 1949.0 128.0

14 MIDDLE TRIASSIC

TREDIAN 2077.0 43.1

141

WELL TOPS

well Name ZINDA PIR-01 Type EX Status ABD

Operator OGDC Spud date 25/03/1986 Compl.date 06/04/1987

Depth(m) 4406.0 Latitude 30 24 07 .29 Longitude 70 27 52.72 K.B.E 400.18 Province PUNJAB Formation ALOZIA

Sr.no Formation Age Formation Top(m) Thickness(m)

1 PLIOCENE DUNGAN LIMESTONE

0.0 100.0

2 PLIOCENE RANIKOT 100.0 88.0 3 LATE

CRETACEOUSPAB

SANDSTONE 188.0 428.0

4 LATE CRETACEOUS

MUGHAL KOT

616.0 407.0

5 LATE CRETACEOUS

RARH LIMESTONE

1023.0 91.0

6 CRETACEOUS GORU 1114.0 296.0 7 EARLY

CRETACEOUSSEMBAR 1410.0 757.0

8 MIDDLE JURASSIC

CHILTAN LIMESTONE

2167.0 844.0

9 JURASSIC LORALAI 3011.0 479.0 10 JURASSIC TO

TRIASSIC ALOZAI 3490.0 916.0

142

WELL TOPS

well Name SARAI SIDHU-01 Type EX Status ABD

Operator AMOCO Spud date 02/12/1973 Compl.date 16/02/1974

Depth(m) 3279.5 Latitude 30 32 21.40 Longitude 71 55 39.60

K.B.E 145.26 Province PUNJAB Formation SALT RANGE

Sr.no Formation Age Formation Top(m) Thickness(m)

1 MIOCENE-PLEISTOCENE

NAGRI 0.0 629.1

2 MIOCENE CHINJI 629.1 63.7 3 MIDDLE-

LOWER EOCENE

SAKESAR 1333.1 63.7

4 MIDDLE-LOWER EOCENE

NAMMAL 1396.8 30.2

5 OLIGOCENE GHAZIJ SUI MEMBER

1427.0 151.5

6 MIDDLE-LOWER EOCENE

DUNGAN 1578.5 34.5

7 PALEOCENE RANIKOT 1613.0 24.3 8 PALEOCENE LOWER

RANIKOT 1637.3 18.7

9 LOWER CRETACEOUS

LUMSHIWAL 1656.0 111.0

10 LOWER CRETACEOUS-

UPPER JURASSIC

CHICHALI 1767.0 57.4

11 MIDDLE JURASSIC

SAMANA SUK 1824.4 136.9

12 MIDDLE JURASSIC

SHINWARI 1961.3 95.1

13 MIDDLE JURASSIC

DATTA 2056.4 18.6

14 TRIASSIC KINGIALI 2075.0 115.5 15 MIDDLE

TRIASSIC TREDIAN 2190.5 51.5

16 LATE PERMIAN

AMB 2242.0 94.2

17 PERMIAN SARDHAI 2336.2 163.8

143

Sr.no Formation Age Formation Top(m) Thickness(m)

18 EARLY PERMIAN

WARCHA 2500.0 158.0

19

EARLY PERMIAN

DANDOT 2658.0 24.7

20 CAMBRIAN BAGHANWALA 2682.7 50.3 21 EARLY

PERMIAN TOBRA 2733.0 18.0

22 CAMBRIAN KHERA SANDSTONE

2751.0 306.1

23 INFRA CAMBRIAN

SALT RANGE 3057.1 222.5

WELL TOPS

well Name RODHO-02 Type EX Status GAS/SUS

Operator OGDC Spud date 15/01/1973 Compl.date 22/12/1974 Depth(m) 2468.8 Latitude 30 44 36.83 Longitude 70 26 34.25 K.B.E 581.00 Province PUNJAB Formation SEMBAR

Sr.no Formation Age Formation Top(m) Thickness(m)

1 EOCENE HABIB RAHI 0.0 20.0 2 EOCENE GHAZIJ 20.0 1127.0 3 PALEOCENE DUNGHAN 1147.0 177.0 4 PALEOCENE RANIKOT 1324.0 111.0 5 LATE

CRET/EARLT CRET

PAB 1435.0 277.0

6 LATE CRET/EARLT

CRET

FORT MUNRO

1712.0 418.0

7 LATE CRET/EARLT

CRET

PARH 2130.0 95.0

8 CRETACOUS GORU 2225.0 184.0 9 EARLY

CRETACOUS SEMBAR 2409.0 59.8

144

WELL TOPS

well Name DOMANDA-01 Type EX Status ABD

Operator PPL Spud date 26/11/1959 Compl.date 21/04/1960 Depth(m) 3408.4 Latitude 31 29 43.00 Longitude 70 11 58.00

K.B.E 723.00 Province N.W.F.P Formation GHAZIJ

Sr.no Formation Age Formation Top(m) Thickness(m)

1 EOCENE GHAZIJ 0.0 3408.4 WELL TOPS

well Name SAVI RAGHA-01 Type EX Status GAS/CON

Operator BG Spud date 2701/1994 Compl.date 15/06/1994 Depth(m) 2977.0 Latitude 31 11 27.38 Longitude 70 12 04 .53

K.B.E 689.0 Province BALOUCHISTAN Formation MUGHAL KOT

Sr.no Formation Age Formation Top(m) Thickness(m)

1 QUATERNARY QUATERNARY 0.0 14.3 2 EOCENE KIRTHER 14.3 95.7 3 MIDDLE

EOCENE HABIB RAHI LIMESTONE

110.0 24.5

4 MIDDLE EOCENE

BASKA SHALE MEMBER

134.5 149.5

5 MIDDLE EOCENE

RUBLY LIMESTONE

284.0 630.0

6 EARLY EOCENE

GHAZIJ SHALE

914.0 1467.0

7 PALEOCENE UPPER RANIKOT

2381.0 117.0

8 PALEOCENE LOWER RANIKOT

2498.0 163.0

9 UPPER CRETACEOUS

PAB SANDSTONE

2883.0 94.0

145

WELL TOPS well Name KAMIAB -01 Type EX Status ABD

Operator AMOCO Spud date 15/01/1974 Compl.date 21/11/1974 Depth(m) 2298.4 Latitude 31 11 37.00 Longitude 71 31 13.00 K.B.E 163.18 Province PUNJAB Formation SAMANA SUK

Sr.no Formation Age Formation Top(m) Thickness(m)

1 PLIOCENE NAGRI 0.0 768.1 2 MIOCENE CHINJI 768.1 846.7 3 EOCENE CHORGALI 1614.8 8.8 4 EOCENE SAKESAR 1623.6 36.8 5 OLIGOCENE GHAZIJ SUI

MEMBER 1660.4 121.4

6 PALEOCENE PATALA EQUIVALENT

1781.8 53.3

7 PALEOCENE DUNGHAN 1835.1 81.3 8 PALEOCENE RANIKOT 1916.4 39.0 9 CRETACEOUS GORU 1955.5 180.2 10 EARLY

CRETACEOUSLUMSHIWAL 2135.7 125.4

11 EARLY CRETACEOUS

CHOCHALI 2261.1 24.8

12 MIDDLE JURASSIC

SAMAN SUK 2285.9 12.5

146

WELL TOPS

well Name AFIBAND-01 Type EX Status ABD

Operator OGDC Spud date 25/01/1986 Compl.date 27/07/1986 Depth(m) 2020.0 Latitude 30 38 18.37 Longitude 70 27 31.78

K.B.E 861.32 Province PUNJAB Formation MUGHAL KOT

Sr.no Formation Age Formation Top(m) Thickness(m)

1 EOCENE GHAZIJ 0.0 1073.0 2 PALEOCENE DUNGHAN 1073.0 42.0 3 PALEOCENE UPPER

RANIKOT 1115.0 65.0

4 PALEOCENE LOWER RANIKOT

1180.0 205.0

5 LATE CRET/EARLY

CRET

PAB SANDSTONE

1385.0 303.0

6 LATE CRET/EARLY

CRET

MUGHAL KOT

1688.0 332.0

147

WELL TOPS

well Name PIRANWAL-01 Type EX Status ABD

Operator OGDC Spud date 24/11//1986 Compl.date 02/01/1987 Depth(m) 2581.0 Latitude 30 20 41.18 Longitude 72 01 02.14

K.B.E 143.71 Province PUNJAB Formation BAGHANWALA

Sr.no Formation Age Formation Top(m) Thickness(m)

1 PLIOCENE NAGRI 0.0 295.0

2 MIOCENE CHINJI 295.0 877.0

3 EOCENE SAKESAR 1172.0 74.0

4 EOCENE NAMMAL 1246.0 244.0

5 PALEOCENE DUNGHAN 1490.00 33.0

6 PALEOCENE UPPER RANIKOT

1523.0 23.0

7 PALEOCENE LOWER RANIKOT

1565.0 8.0

8 EARLY CRETACEOUS

LUMSHIWAL 1573.0 89.0

9 EARLY CRETACEOUS

CHICHALI 1662.0 48.0

10 MIDDLE JURASSIC

SAMANA SUK 1710.0 127.0

11 EARLY JURASSIC

SHINWARI 1837.0 103.0

12 EARLY JURASSIC

DATTA 1940.0 49.0

13 LATE TRIASSIC KINGRIALI 1989.0 43.0

14 MIDDLE TRIASSIC

TREDIAN 2032.0 77.0

15 LATE PERMIAN AMB 2109.0 74.0

16 EARLY PERMIAN

SARDHAI 2183.0 108.0

17 EARLY PERMIAN

WARCHA 2291.0 181.0

18 EARLY PERMIAN

DANDOT 2472.0 57.0

19 EARLY PERMIAN

TOBRA 2529.0 26.0

20 MIDDLE CAMBRIAN

BAGHANWALA 2555.0 26.0

148

WELL TOPS

well Name KOTRUM-01 Type EX Status ABD

Operator OGDC Spud date 16/12//1997 Compl.date 18/08/1979 Depth(m) 4797.9 Latitude 29 16 52.40 Longitude 70 09 28.20 K.B.E 138.54 Province PUNJAB Formation PAB SANDSTONE

Sr.no Formation Age Formation Top(m) Thickness(m)

1 MIOCENE-PLEISTOCENE

PLIOCENEN

SIAWALIK 0.0 2073.0

2 MIOCENE GAJ 2073.0 172.0 3 OLIGOCENE NARI 2245.0 535.0 4 EOCENE DRAZINDA 2780.0 220.0 5 EOCENE PIKOH 3000.0 15.0 6 EOCENE SIRKI-

DOMANDA 3015.0 215.0

7 EOCENE HABIB RAHI 3230.0 76.0 8 EOCENE GHAZIJ 3306.0 502.0 9 PALEOCENE DUNGHAN 3808.0 18.0 10 PALEOCENE UPPER

RANIKOT 3826.0 419.0

11 PALEOCENE LOWER RANIKOT

4245.0 180.0

12 LATE CRET/EARLY CRET

PAB 4425.0 372.9

149

WELL TOPS

well Name SARO-01 Type EX Status ABD

Operator OGDC Spud date 18/01/1992 Compl. date 21/02/1992

Depth(m) 1040.0 Latitude 31 13 55.49 Longitude 71 49 33.07

K.B.E 166.74 Province PUNJAB Formation Samana suk

Sr.no Formation Age Formation Top(m) Thickness(m)

1 PLIOCENE NAGRI 0.0 517. 0 2 MIOCENE CHINJI 517.0 425.0 3 PALEOCENE DUNGHAN 942.5 8.5 4 PALEOCENE RANIKOT 951.0 2.5 5 EARLY

CRETACEOUSLUMSHIWAL 953.5 50.5

6 EARLY CRETACEOUS

CHICHALI 1004.0 12.0

7 MIDDLE JURASSIC

SAMANA SUK

1016.0 24.0

150

WELL TOPS

well Name NANDPUR-01 Type EX Status GAS

Operator OGDC Spud date 20/04//1984 Compl.date 12 /08/1984 Depth(m) 2110.0 Latitude 30 31 45.20 Longitude 71 55 38.00

K.B.E 141.50 Province PUNJAB Formation KINGGIALI

Sr.no Formation Age Formation Top(m) Thickness(m)

1 PLIOCENE NAGRI 0.0 655.0 2 MIOCENE CHINJI 655.0 670.0 3 EOCENE SAKESAR 1325.0 25.0 4 EOCENE NAMMAL 1350.0 70.0 5 EOCENE GHZIJ SUI

MEMBER 1420.0 150.0

6 PALEOCENE DUNGHAN 1570.0 34.0 7 PALEOCENE RANIKOT 1604.0 37.0 8 EARLY

CRETACEOUSLUMISHWAL 1641.0 117.0

9 EARLY CRETACEOUS

CHICHALI 1758.0 74.0

10 MIDDLE JURASSIC

SAMANA SUK

1832.0 140.0

11 MIDDLE JURASSIC

SHINWARI 1972.0 100.0

12 EARLY JURASSIC

DATTA 2072.0 31.0

13 LATE TRIASSIC

KINGRIALI 2103.0 7.0

151

WELL TOPS

Sr.no Formation Age Formation Top(m) Thickness(m)

1 MIOCENE-QUATENARY

SIWALIK RAWALPINDI

0.0 800.00

2 EOCENE CHORGALI 800.00 121.0

3 EOCENE SAKESAR 921.0 72.0

4 PALEOCENEEOCENE NAMMAL 993.0 64.0

5 EOCENE GHAZIJ SUI MEMBER

1057.0 17.0

6 PALEOCENE DUNGHAN 1074.0 5.0

7 EARLY CRETACEOUS

CHICHALI 1079.0 15.0

8 MIDDLE JURASSIC SAMANA SUK 1094.0 98.0

9 MIDDLE JURASSIC SHINWARI 1192.0 95.0

10 EARLY JURASSIC DATTA 1287.0 13.0

11 MIDDLE TRIASSIC TREDIAN 1300.0 94.0

12 EARLY PERMIAN AMB 1394.0 71.0

13 EARLY PERMIAN SARDHAI 1465.0 98.0

14 EARLY PERMIAN WARCHA 1563.0 122.0

15 EARLY PERMIAN DANDOT 1185.00 45.0

16 EARLY PERMIAN TOBRA 1730.0 10.0

17 MIDDLE CAMBRIAN KUSSAK 1740.0 129.0

18 EARLY CAMBRIAN KHEWRA SANDSTONE

1869.0 285.0

19 PRE-CAMBRIAN SALT RANGE 2154.00 817.0

20 PRE CAMBRIAN BASEMENT 2971.0 53.0

well Name BAHAWALPUR EAST-01

Type EX Status ABD

Operator SHELL Spud date 19/12/1980 Compl.date 17/02/1981 Depth(m) 3024.0 Latitud 29 22 07.00 Longitude 72 09 07.40 K.B.E 134.90 Province PUNJAB Formation BASEMENT