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Field Report Salt Range
1. FIELD REPORT OF SALT RANGE
BY
MUHAMMAD AFTAB SHABIR
ALI SHAN MALIK
TAYYAB IMRAN
ANAS AHMED
RANA MOHSIN
DEPARTMENT OF EARTH AND ENVIORNMENT SCEINCES
BAHRIA UNIVERSITY ISLAMABAD
2018
2. i
ACKNOWLEDGEMENT
Glory and thanks to Allah Almighty (SWT) Who guide us in darkness, and help us in our
difficulties, and due respect to Holy Prophet (PBUH) who recognize our creator. Without
Allah blessing it was impossible to complete our report.
Afterward we would like to thanks our parents who loved and helped us in our studies, and
without their prayers we wouldn’t be successful in our studies.
We would like to thanks Sir Raiees Amjad, Sir Tausif Ahmed, and Ma’am Urooj Shakir for
coming along with us to field trip to share their knowledge, and word of wisdom with us.
Special thanks to Dr Tahseenullah Khan and Department of Earth and Environmental
Sciences who arranged for us an educational trip that was delightful and knowledge able at
the same time.
3. ii
Abstract
A four days field trip was organized by Department of Earth, and Environmental Sciences,
Bahria University Islamabad Campus for BS Geophysics Sixth semester, from 25 October
2018 (Thursday) to 28 October 2018 (Sunday). The place chosen for field was Salt Range.
We set out for our field on 25 October 2018 at 9:00 AM from Bahria University Islamabad
Campus.
The Salt Range is considered as the most vital geologic and paleontological regions in
Pakistan. The major objective of our field was to study the geography, geology, structural
settings, Stratigraphy and paleontology of the area.
For obtaining our field objectives we visited various areas and different road sections to study
the outcrop in detail. We moved along various road sections and observe complex geological
settings and stratigraphic arrangements and recorded our information respectively. We were
provided with different instruments that were required during the field like chisel, Brunton
compass and many more to investigate the lithologies observed. We hike along different
strata for their close examination and study.
The four days field study let us know about the general tectonic setting of Salt Range. The
filed struggle brightens our knowledge and understanding about different stratigraphic
formations and their natural settings. We, after the field exposure become able to find out the
dip and strike of strata, the natural structural settings of different formations, the stratigraphic
sequences and mapping of observable outcrops.
We found out various sedimentary features and the importance of their presence on a rock
unit. The lecturers were highly cooperative and due to their cooperation, we ended our four-
day field with satisfaction that we have learned a lot from our field experience.
4. iii
CONTENTS
CHAPTER 1
INRODUCTION 1
1.1 Location: 1
1.2 Accessibility: 1
1.3 Climate: 2
1.4 Objective: 2
1.5 Equipment: 3
1.6 Methodology: 5
CHAPTER 2
GEOLOGY AND TECTONICS OF SALT RANGE 6
2.1 Geology and Tectonics: 6
2.1.1 Salt Range Thrust and Trans Indus Ranges: 7
2.1.2 Punjab Fore-Deep 7
2.1.3 Kalabagh Fault 7
2.1.4 Jhelum Fault 7
2.1.5 Structural Setting 7
2.1.6 Active Thrust System of Salt Range 8
2.1.7 Deformation in Salt Range 9
2.2 Stratigraphy of Salt Range: 9
CHAPTER 3
KARULI VILLAGE ROAD SECTION 11
3.1 Introduction: 11
3.2 Warcha Sandstone: 12
3.2.1 Observations: 13
3.2.2 Literature Work: 14
15. xiv
6.3.6 Fossils: 64
6.3.7 Age: 64
6.3.8 Contact: 64
6.4 Chorgali Formation 64
6.4.1 Observations: 64
6.4.2 Literature: 64
6.4.3 Type Section: 65
6.4.4 Lithology: 65
6.4.5 Fossils: 65
6.4.6 Age: 65
6.4.7 Contact: 65
Conclusion Day 4: 66
Conclusion 67
REFERENCES 68
LIST OF FIGURES
Figure 1.1: Route map of Bahria University to Kalar Kahar and Kalar Kahar to Mianwali 1
Figure 1.2: Graphs shows Annual Average temperature of Kallar Kahar 2
Figure 1.5.1: Brunton compass 3
Figure 1.5.2: Geological hammer 3
Figure 1.5.3: Hand lens 4
Figure 1.5.4: Acid bottle 4
Figure 1.5.5: Scale 4
Figure 2.1: Shows the map of Salt range 6
Figure 2.2: Active thrust system of the salt range 8
Figure 2.3: Active thrust system and plateau 8
Figure 2.4: Deformation in Salt Range 9
Figure 2.2.1: Shows stratigraphy of Salt Range 10
16. xv
Figure 3.1: Shows route map of BUIC to Karuli village 11
Figure 3.2.1.1: Shows outcrop of Sakesar Limestone 13
Figure 3.2.1.2: Shows outcrop of Warcha Sandstone 13
Figure 3.2.5.1: Shows laminated Warcha with clay 14
Figure 3.2.6.1: a) Shows red grey Warcha sandstone.b) Shows reddish clay of warcha formation of
oxidizing environment 14
Figure 3.2.8.1: Contact between Dandot formation and Warcha Sandstone 15
Figure3.2.10.1: Shows moderately fractured Warcha Sandstone 15
Figure 3.3.1: Shows faulted contact between Warcha and Dandot formation 16
Figure 3.3.5.1: Shows greenish grey sandstone with interbedded shales 17
Figure 3.3.6.1: Shows weathered colour of Dandot formation 17
Figure 3.3.10.1: Shows Phosphatic nodules 18
Figure 3.4.1.1: Shows flaggy sandstone with red shales of Baghanwala formation 19
Figure 3.4.8.1: Conformable lower contact of baghanwala with Jutana formation 20
Figure 3.5.4.1: Shows highly fractured outcrop of Jutana Dolomite 21
Figure 3.5.8.1: Shows contact between kussak and Jutana formation 22
Figure 3.5.10.1: Shows honeycomb weathering in Jutana Dolomite 22
Figure 3.6.4.1: Shows arkosic Sandstone of Kussak formation 23
Figure 3.6.4.2: Shows Gluconite mineral in Kussak Sandstone 24
Figure 3.6.5.1: a) Shows sandstone and interbedded shale b) shows shale lamina 24
Figure 3.6.6.1: Shows greenish grey sandstone and shales of Kussak Formation 24
Figure3.6.10.1: a) Shows bioturbation b) shows ripple marks 25
Figure 4.1.1: Location map of Pidh village; Kallar Kahar 27
Figure 4.2.4.1: Sandstone of Baghanwala formation 28
Figure 4.3.5: Shows massive bedding in Tobra formation 30
Figure 4.3.6.1: Shows sandstone with cobbels and pebbles 31
Figure 4.3.10.1: Shows transitional contact between Tobra and Dandot formation 31
Figure 4.4.8.1: Shows contact between Warcha and Dandot formation 33
Figure 4.4.10.1: Shows trough cross bedding and phosphatic nodules 33
17. xvi
Figure 4.5.10.1: Shows joints and linear cross bedding 35
Figure 4.6.1: Shows Normal fault 35
Figure 4.6.4.1:Shows Sakessar Limestone 36
Figure 4.7.4.1: Shows Khewra sandstone 38
Figure 4.8.9.1: Shows Salt Range Thrust. 40
Figure 5.1.1: Shows entrance ofNammal Gorge 41
Figure 5.2.1: Showing normal fault 42
Figure 5.3.4.1: Shows Amb formation 43
Figure 5.3.7.1: Shows contact between Amb and Wargal formation 43
Figure 5.3.4.6.1: Shows productus fossil in Wargal formation 44
Figure 5.4.8.1: Showing contact between Chhidru and Wargal formation 45
Figure 5.4.9.1: Shows Wargal formation 45
Figure 5.5.8.1 Shows contact b/w Chidru and mianwali which marks PT boundary 47
Figure 5.6.4.1: Shows members of Mianwali formation 48
Figure 5.6.6.1: Shows ammonides in Mianwali formation 48
Figure 5.7.4.1: Shows Tredian formation 50
Figure 5.7.6.1: Shows trough crossbedding in Tredian formation 50
Figure 5.7.9.1: Shows contact between Tredian and Kingriali 51
Figure 5.8.4.1: Showsdoya and Bingari member of Kingriali formation 52
Figure 5.9.4.1: Shows outcrop of Datta formation 53
Figure 5.9.4.2: Sows oil seepages in Data formation 53
Figure 5.9.6.1: Shows ripple marks in Datta formation 54
Figure 5.9.8.1: Shows contact between Datta and Samana-suk 54
Figure 5.10.4.1: Shows outcrop of Samanasuk formation 55
Figure 5.12.4.1: Shows outcrop of Lockart formation 57
Figure 5.12.7.1: Shows contact between Patala and Lockart formation 58
Figure 5.13.7.1: Shows contact between Patala and Nammal formation 59
Figure 5.15.1.1: Shows contact between Nammal and Sakesar formation 60
18. xvii
Figure 6.2.6.1: Showscontact with Murree and Kingriali formation 64
Figure 6.4.4.1: Shows anticlinal limb of Chorgali formation 65
LIST OF TABELS
Table 1.1 Climate of Kallar Kahar 2
Table No 4.3.1: Shows Value Of Dip and Strike 42
Table No 5.4.9.1: Shows Value Of True Dip and Strike 45
Table No 6.4.1: Values of True Dip and Strike 6
19. 1
CHAPTER 1
INTRODUCTION
1.1 Location
We departed from Bahria University, Islamabad at 10:00 a.m. on 25th
Oct 2018 towards
KalarKahar which 136 km SE of our university. We travelled Bahria University to KallarKahar via
Motorway M-2. Travelling time was almost 1 hour 40 minutes.
KallarKahar Coordinates: (32°47′N 72°42′E) a town and subdivision (Tehsil) of Chakwal
District in Punjab, Pakistan. The world-famous Salt Range is in this region between latitude 32º-33º
North and longitude 70º-72º East. Our three-day field work was around the vicinity of Kallarkahar
including Karuli village, Pid village and various road sections.
Third day visit was made to Mianwali to study the western part of Salt Range. Mianwali
(Coordinates: 32°35′7″N 71°32′37″E) is the near the city of Mianwali District, Punjab province
Pakistan.
Figure 1.1 Route map of Bahria University to KallarKahar and KallarKahar to Mianwali
1.2 Accessibility:
For transport university provided two coasters. Coasters carried us to the karoli village on first
day and the area was easily accessible by them there was no route problems in that area. On our
second day 30 minutes’ drive to pidh village from our hotels were made, that area was also easily
accessible apart from some elevated areas where we have to go by hike as coasters cannot reach there.
Our third day trip was to mianwali, 2 hours 30 minutes drive from our hotel took us to the area.
Coasters droped us on the first station then rest of the area was covered on feet which is about 5 to 6
km in distance. Fourth day was along the road sections so no problem with the accessibility for
21. 3
different geological and geophysical field instruments. To know about different depositional
sequences. Compare ages and make out how and why a certain lithology is and where it is.
Also, the purpose was to make our practical knowledge sound and to identify the various
features that are exposed in the outcrop.
1.5 Equipment:
1. Brunton compass: Used to measure the Dip and Strike of different strata.
Figure 1.5.1 Shows Burnton compass
2. Geological Hammer: Used to collect the sample and to differentiate between
weathered color and fresh color.
Figure 1.5.2 Shows Hammer
3. Hand lens: Used to observe size of grains and sorting of grains.
22. 4
Figure 1.5.3 Shows Handlens
4. Acid ( Dillute Hydrochloric Acid – HCl): Used to confirm the presence of
Limestone or Dolomite.
Figure 1.5.4 Shows Acid bottle
5. Measuring Scale: Used to measuring bed Bedding Thickness.
Figure 1.5.5 Shows scale
6. Camera:Used tocapture pictures of the outcrops
23. 5
Figure 1.5.6 Shows camera
1.6 Methodology:
a) Locate yourself and marking our current position on map using Brunton compass.
b) Observe the formation, outcrop and lithology.
c) Measure the dip-strike, and the Bedding Thickness of the beds.
d) Collect samples.
e) Identifying lithology using previous literature.
f) Take pictures of formations; confirm contacts between different lithologies,
geological structure and specific features if present.
Criteria to define Bedding Thickness:
a) If Bedding Thickness of bed is less than 1 cm: Lamina.
b) If Bedding Thickness of bed is between 1 cm and 10 cm: Thin Bedded.
c) If Bedding Thickness of bed is between 10 cm and 30 cm: Thin Medium
Bedded.
d) If Bedding Thickness of bed is between 30 cm and 50 cm: Medium Bedded.
e) If Bedding Thickness of bed is above 50 cm: Thick bedded.
24. 6
CHAPTER 2
GEOLOGY AND TECTONICS OF SALT RANGE
2.1 Geology and Tectonics:
The Salt range strikes almost East-West and terminates at Kalabagh where the range is
intersected by river Indus. Beyond the river Indus the ranges beaks out into various
ranges collectively referred as Trans-Indus ranges. The rocks in the Salt ranges are
generally folded and are typically marked by large and small-scale faulting as well as
local over-thrusting with movements towards south. The sedimentary sequence ranges
from Pre-Cambrian to the Eocene and recent age. It is also marked by several
unconformities.
Potwar Plateau, the sedimentary rocks south of the Salt Range thrust lack structural
deformation (Yeats and others, 1984). The up thrown block of the thrust brings to the
surface the Salt Range Formation along the southward-facing edge of the over thrust
block, which contains evaporites of late Pre-Cambrian. Overlaying salt range formation
are Cambrian Khewra sandstone, Khussak Formation, Jutana dolomite, Baghanwala
sandstone, Permian Tobra and younger rocks till recent age are present Ordovician,
Silurian, Devonian and Carboniferous rocks are absent in salt range making a major
unconformity between Cambrian Baghanwala and Permian Tobra conglomerate (Yeats
and others, 1984).
Figure 2.1: Shows the map of salt range
25. 7
2.1.1 Salt Range Thrust and Trans Indus Ranges:
In the northern Pakistan most of the youngest thrusting has occurred along the frontal thrust
system in salt range along the salt range thrust (SRT) in the east and in Trans- Indus Ranges
thrust in the west. The frontal thrust system has accommodated about less than and equal to
20km of shortening in salt Range formation and + - 10km in the Trans Indus ranges along
this thrust front the eocambrian salt range formation ion the salt range. Permian rocks in the
surghar range and the Cambrian Jhelum group rocks in the Kishor range are thrust over the
Punjab fore deep in the south 2008.
2.1.2 Punjab Fore Deep
The Punjab plain lies south of the salt and Trans indus ranges and overlain Quaternary
sediments and is the present day depocenter for the eroded debris of the Himalayan chains in
the north. A prominent element in the Punjab plain is the Sargodha high a basement ridges
those trends obliquely to the salt range but parallel to the overall Himalayan trend. Its trend is
defined by both the exposed basement rocks of kirana hills and by a Pakistan India border. It
is an expression of recently activate intercontinental thrust.
2.1.3 Kalabagh Fault
This fault forms the western margin of the salt range and extends NNW from near Mianwali
for a distance of 120km. it has been described as an active dextral wrench fault associated
with several recorded earthquakes epicenters.
2.1.4 Jhelum Fault
This is left lateral fault which is at the eastern margin of the salt range.
2.1.5 Structural Setting
Structurally, the salt range is the result of the tectonic forces imposed during the later phase
of the Himalayan orogeny in the late Cenozoic time, the occurrence of the thick, competent
salt range formation at the base of the sedimentary sequence has strongly influenced the
structure.
26. 8
2.1.6 Active Thrust System Of The Salt Range
The salt range is separated from the Himalayan foothills by the potwar plateau nearly 150km
of slightly elevated(about 270m) land with very little topographic relied. The roughly ENE-
WSW trending Salt range is bounded by the right lateral Kalabagh fault in the west and the
Hazara-Kashmir syntax in the east. The Hazara – Kashmir syntaxes is formed by several fault
blocks bounded by forward and rearward verging thrust at the eastern margin of the potwar
plateau the salt range thrust, which is the leading edge of a decollement within eocambrian
evaporates, brings Phanerozoic strata over late quaternary fanglomerated and Jhelum river
alluvium. Some author argues that pre-existing basement faults played an important role in
the tectonics evolution of the salt range and potwar plateau. The extensive lateral extension of
salt as the remnant of large, ruptured and discharged salt dome. After the MBT zone under
the kala chitta range to the north was locked some 2 Ma age.
Fig 2.2 active thrust system of the saltrange
Fig 2.3 active thrust system and plateau
27. 9
2.1.7 Deformation in Salt Range
The deformational style of the salt range is typically marked by broad synclines and long,
Narrow anticlines similar to those in other shallow decollement fold and thrust belts,
underlain by salt, The roof sequence is very gently folded into the box folds and is moderate
lateral faulted by both forward and back thrust. Folding becomes more complex towards the
leading edge of the thrust system and faulting is more abundant in the west. The overall
structure at the leading edge of the salt range thrust front is increasing complex.
a) E-W imbricate thrust the lowest of which is the salt range thrust which brings the
entire sequence over the quaternary conglomerates.
b) N-S or oblique transverse normal faults relate to the extension, these bring up the
oldest Salt Range formation to the surface providing easy dissection and creation of
the well-known gorges.
c) The strike slips dextral high angle faults at the margins of salt range providing for the
southward transport of the range.
I. Salt diaper structures forming salt plugs along the strike slip fault in the west
and eastwards providing the upward push under the low pressure regions
created by the erosion of the Depp gorge. This later push has created tight N-S
salt cored anticlines separated by broad synclines.
2.2 Stratigraphy of Salt Range:
The Generalized stratigraphy of the area is of great importance and necessary to study before
carrying out the field work. In this section the formations which are present in salt range have
Fig 2.4 Deformation in Salt range
28. 10
been included along with their general stratigraphy and age. An overview of the salt range’s
stratigraphy is as under.
;
Figure 2.2.1: Shows stratigraphy of Salt Range
29. 11
CHAPTER 3
KARULI VILLAGE ROAD SECTION
3.1 Introduction:
On 25th
October, 2018; Thursday; we (BS Geophysics-6A) started our four days field
journey from Bahria University Islamabad Campus (BUIC) at 8:30-9:00 AM towards Karuli
Village. As we started our journey from Islamabad the climate was hot and dry with an
approximate temperature of 30◦C (Max)-14◦C (Min). We travelled through motorway and it
took us approximately 3 hours and 30 minutes to reach at our destination.
Karuli village was selected as the first day field station. We reached there in the noon about
12:30-1:00 PM. It is a village of KallarKahar Tehsil, Chakwal District, Pakistan. It is located
in a salt range near Motorway M-2. Geographical coordinates of Karuli are 32° 41' 0" North,
72° 47' 0" East. The climate over there was dry and the average temperature was about 29◦C
(Max)-13◦C (Min).There is not much rainfall in KallarKahar all year long. The average
annual rainfall is 485 mm.
Figure 3.1: Show route map of BUIC to Karuli village
30. 12
Karuli Village being part of Salt Range contain rich exposure of various lithological
units. It is deep, narrow steep sided valley which is located along the Western margin of
Eastern Salt Range and contain rock sequences from Late Permian to recent age deposits. As
the field was along Karuli road section, we observed two main Stratigaraphical groups i-e
Nilawahan Group (Early Permian Age) of which only Warcha Sandstone and Dandot
Formation was observed which was present above the Jhelum Group’s (Early to Middle
Cambrian Age) Baghanwala Formation, Jutana Formation and Kussak Formation. The two
groups are separated from each other by a major unconformity. Travelling along the Karuli
road section we took our observations from younger to older age rock sequences and the field
continued up till 5:00 PM in the evening.
Before continuing the field our teacher SirTouseef delivered a brief lecture on the
geology and tectonics of the area.
3.2 Warcha Sandstone:
Travelling through the Karuli road section we stopped at the first spot to observe the
outcrop. At this point we marked ourselves on the Karuli road section satellite map by
observing the nearby visible features (like the school building). By the help of Brunton
compass we found true north at the particular area and then mark it on the map as well. We
first calculated the true dip and strike of the strata which was found out to be:
Table 3.2: Shows values of dip and strike
Dip Strike
22⁰ NW N40⁰E
We observe different colour of sandstones in one formation. As we were moving across the
dip so probably older formations should be encountered. Change in colour of warcha
sandstone shows change in environment. Grey colour shows reducing environment and
reddish colour of sandstone shows oxidizing environment.
3.2.1 Observations:
The outcrop was observed thoroughly. Its weathered colour was dark grey, dark
green, blackish grey. By the help of hammer we collected a sample to see the fresh color of
the lithology which was found out to be pale yellow to light brown. The grains were poorly
sorted as there was a major volume of courser grains with a minor volume of finer and
shinnygrains present as well. The lithology was friable and weakly cemented. We found
Systematic Joints as a sedimentary feature out there. Standing on the same spot in NW
direction we observe the presence of Eocene Age Sakesar Limestone. Below which Patala
Formation’s coal seam was also present on the surface but we did not go to the outcrop.
31. 13
Figure 3.2.1.1: Shows outcrops of Sakesar Limestone at Stop 1
Figure 3.2.1.2: Shows outcrop of Warcha Sandstone
32. 14
3.2.2 Literature Work:
The term Warcha Sandstone was coined by Hussain (1967), which has been approved by
the Stratigraphic Committee of Pakistan. Prior to the formalization of this name other terms
were used such as the “Warcha George” of Noetling (1901). The name such as “Speckled
Sandstone” of Gee (1945) and “Middle Speckled Sandstone” of Waagen (1879).
3.2.3 Type Section:
Its type section is in the Warcha Village in the Salt Range.
3.2.4 Lithology:
The formation consists of medium to coarse grained cross bedded sandstone. The grains
are poorly sorted and less cemented.
3.2.5 Bedding Thickness:
We have seen thick to massive bedding but as we go down along the road we see laminated
sandstone with interbedded red clays which shows oxidizing environment.
Figure 3.2.5.1: Shows laminated warcha sandstone with clays
3.2.6 Colour:
The sandstone is greenish grey in start then changes to red, or shows lighter shades of
pink. As per our observation the weathered colour of rock was found to be brownish to
reddish grey while its fresh colour was pinkish grey. This sand stone shows oxidizing
environment. Red colour clays were also present which shows oxidizing environment.
33. 15
Figure 3.2.6.1: (A) Shows reddish grey warcha sandstone and (B) shows reddish clay of warcha formation of
oxidizing environment
3.2.7 Environment of Deposition:
The formation is continental to fluvial deposits.Grey colour shows reducing environment and
red colour shows oxidizing environment.
3.2.8 Contact:
The upper contact of the formation is with Sardhai Formation which is conformable.
The lower contact of the formation is with Dandot Formation which is transitional and
conformable.
Figure 3.2.8.1: Shows Transitional contact between Dandot and Warcha formations
3.2.9 Fossils:
We did not observe any fossils during our study.
3.2.10 Sedimentary Features:
The formation shows is moderately fractured, contain large joint sets.
Figure 3.2.10.1: Shows moderately fractured warcha sandstone
3.2.11 Age:
Its age is Early Permian.
34. 16
3.3 Dandot Formation:
Travelling a little further along the road section, change in the lithology was observed.
3.3.1 Observations:
A normal fault was observed while moving along the road section. The foot wall was Warcha
Sandstone while the hanging wall was made up of two different lithologies. At the top;
Warcha Sandstone and at the bottom; a lithological unit different from Warcha Sandstone.
That thin to medium bed was olive green in color composed up of Sandstone (Grey) and
Shales (olive green). The olive green color was due to the presence of micaceous mineral. We
also observed Trough-Cross bedding and Phosphatic nodules in the formation.
Figure 3.3.1.1: Shows faulted contact between Warcha and Dondot formation
3.3.2 Literature Work:
The name Dandot Formation is formalized after the “Dandot Group” of Noetling (1901),
and includes the “Olive Series” of Wynne (1878) and the “Speckled Sandstone” of Waagen
(1879).
3.3.3 Type Section:
The type locality is near Dandot Village, eastern Salt Range.
3.3.4 Lithology:
The lithology consists of sandstone with occasional thin pebbly beds and subordinate
splintery shales.
35. 17
Figure 3.3.5.1: Shows greenish grey sandstone with interbedded shales
3.3.5 Bedding Thickness:
Its bedding Bedding Thickness medium to thick.
3.3.6 Colour:
It has light grey to olive green yellowish sandstone and dark grey and greenish shales.
Figure 3.3.6.1: Shows weathered colour of Dandot Formation
3.3.7 Environment of Deposition:
It is deposited in marine environment.
3.3.8 Contact:
The upper contact of the formation with Warcha Sandstone is sharp and conformable
as in Figure 3.2.8.1.
The lower contact of the formation with Tobra Formation is gradational.
36. 18
3.3.9 Fossils
We did not observe any fossils at the study area.
3.3.10 Sedimentary Features
It is characterized by the presence of Trough Cross Bedding and Phosphatic nodules.
Figure 3.3.10.1: Shows phosphatic nodules in Dandot formation
3.3.11 Age:
Early Permian.
3.4Baghanwala Formation:
Travelling along the same road section another contrast in the lithology was observed.
3.4.1 Observations:
We observed a change in lithology as we moved a little further across the dip direction. The
clear indication of lithology change was due to the presence of shales and flaggy sandstone
.However the bed was thin and most of the characteristic features of that particular lithology
was not exposed in the area of interest. At the top of that formation we observed the beds of
Warcha Sandstone and at the bottom a carbonate rock was encountered which was Jutana
Dolomite.
37. 19
Figure 3.4.1.1: Shows Flaggy sandstone with red shales of Baghanwala Formation
3.4.2 Literature Work:
The name Baghanwala Formation is now given to the rocks of the “Pseudomorph Salt Crystal
Zone” of Wynne (1878) and the “Baghanwala Group” of Noetling (1849).
3.4.3 Type Section:
The type section is located near Baghanwala Village in the eastern Salt Range
3.4.4 Lithology:
The formation is composed of red shales and clays with alternate beds of flaggy Sandstone.
3.4.5 Bedding Thickness:
In the study area we observed thin to medium beds of flaggy sandstone of slaty appearance.
3.4.6 Colour:
It contains blood red shales with several colors of sandstone including pink grey and blue
green.
3.4.7 Environment of Deposition:
Lagoonal environment and arid climate conditions are the requirements for the deposition of
Baghanwala formation.
3.4.8 Contact:
The upper contact of the formation with Tobra formation is unconformable.
The lower contact of the formation with Jutana Dolomite is conformable.
38. 20
Figure 3.4.8.1: Shows conformable lower contact of Banghanwala with Jutana Formation
3.4.9 Fossils
The formation only contains trace fossils but they were not recognized at the study area.
3.4.10 Sedimentary Features
Numerous pseudomorphic casts of salt crystals are usually present along the bedding
planes but in the study area due to its less exposure we did not see these Salt Pseudomorphs.
3.4.11 Age
Early to Middle Cambrian.
3.5Jutana Dolomite:
At the same station on which we observe Banghanwala Formation there was little exposure of
Non-clastic reddish in colour rock.
3.5.1 Observations:
At station where we observe Baghanwala Formation there was a reddish colour Thick to
massive bedded carbonate rock was seen(Fig 3.4.8.1). On hammering it produces some
different sound than we hammer a sandstone. It was highly compacted rock and difficult to
break and sample was bit heavier shows high specific gravity of rock. Now question was that
whether it is a Limestone or a Dolomite. Then we pour acid on the rock surface which did not
produce effervesce then we powder it with the help of hammer then put few drops of acid, we
seen effervesce then. Then we were moving across the dip direction so it will be Jutana
Dolomite. Here due to less exposure of the rock unit, we did not conclude it properly then we
move little further along the road and seen such type of rock with same features but little
different in colour. It was also Jutana Dolomite. As we move further sandiness in dolomite
increases.
39. 21
3.5.2 Literature Work
Fleming (1853) named this unit “Magnesian Sandstone”. Noetling (1894) described it
as “Jutana Stage”. The Stratigraphy Committee of Pakistan formalized the name as “Jutana
Formation”
3.5.3 Type Section
The type locality is near Jutana Village in the eastern Salt Range.
3.5.4 Lithology
The lower Part of the formation consists of sandy dolomite(greenish tone), while the upper
part is composed of massive dolomite(Reddish tone).
Figure 3.5.4.1: Shows highly fractured outcrop ofJutana Dolomite
3.5.5 Bedding Thickness
Bedding Bedding Thickness Thick to massive.
3.5.6 Colour
Dolomite is light green to dirty white in color. Along the study area we found its
weathered color brownish grey and its fresh color pinkish-white.
3.5.7 Environment Of Deposition
It is deposited on the shelves (marine environment).
3.5.8 Contact
The upper contact of the formation with Baghanwala Formation is conformable (Fig
3.4.8.1).
The lower contact of the formation with Kussak Formation is conformable but not
clear due to rubble in field.
40. 22
Figure 3.5.8.1: Shows contact between Kussak and Jutana Formation
3.5.9 Fossils
Non-fossiliferous with very high specific gravity.
3.5.10 Sedimentary Features
It is characterized by Honey Comb Weathering (Secondary Porosity).
Figure 3.5.10.1: Shows Honey comb weathering in Jutana Dolomite
3.5.11 Age
Early to Early-Middle Cambrian.
3.6 Kussak Formation:
Travelling along the same road section we finally arrived at our last spot of the day.
41. 23
3.6.1 Observations:
We observed an outcrop composed of grey and purple color shales and Sandstone
(Argillaceous). The outcrops of shales were showing perfect laminae. And sandstone had
interbeds of shale (Arkosic); that was not very compacted. Large amount of micaceous
minerals were present. The beds of sandstone were less porous and the grains were medium
to fine grained. We also observed Bioturbations and Ripple Marks in the outcrop.
3.6.2 Literature Work
Waagen and Wynne (1895) used the name “Neobolus Beds”. Noetling (1849) proposed
the name “Kussak Group” and finally the Stratigraphic Committee of Pakistan formalized the
name of the unit as Kussak Formation (Fatmi, 1973).
3.6.3 Type Section
The type locality lies near the Kussak Fort in the eastern part of the salt range.
3.6.4 Lithology
The formation is composed of glauconitic, micaceous, and argillaceous sandstone and
siltstone with interbeds of dolomite (present occasionally) and laminated shales.
Figure 3.6.4.1: Shows Arkosic Sandstone of Kussak Formation
42. 24
Figure 3.6.4.2: Shows Gluconite Mineral in Kussak Sandstone
3.6.5 BeddingBedding Thickness
It has Thin bedding Bedding Thickness and shale laminae.
Figure 3.6.5.1: (A)Shows Sandstone and interbedded shales (B) shows shale lamina
3.6.6 Color
The sandstone and siltstone in the formation exhibit greenish-grey color and the interbeds of
dolomite exhibit light grey color.
43. 25
Figure 3.6.6.1: Shows greenish grey sandstone and shales of Kussak Formation
3.6.7 Environment of Deposition
Environment of deposition of Kussak formation is typical continental shelf environment.
Glaconite is a Digenetic mineral which formed at the time of diagenesis of rock and complex
structure of Na, K, Mg form glaconite.
3.6.8 Contact
The upper contact of the formation with Jutana formation is conformable as inFigure
3.5.8.1.
The lower contact of the formation with Khewra Sandstone is gradational.
3.6.9 Fossils
The formation is fossiliferous but at the study area we did not examined any fossils.
However the presence of bioturbations in the formation was a strong indication of presence of
fossils and organic matter was eaten by burros.
3.6.10 Sedimentary Features
Bioturbations and ripple marks are observed clearly in the formation. And the presence of
Bioturbations indicates the presence of ancient organism over here but they are not preserved
over here (due to Bioturbations). That’s why Kussak Formation can’t act as a potential source
rock.
Figure 3.6.10.1: (A) shows Bioturbation and (B) shows Ripple Marks in Kussak Formation
3.6.11 Age
Cambrian age.
3.7 Conclusion (Day 1):
First day field study along Karuli Road Section started in the noon about 1:00 PM and
ended in the evening about 5:00 PM. The field was carried along the road section observing
various outcrop at various stations. At station no 1 we found the second member of Early
Permian Nilawahan Group i-e Warcha Sandstone. At the same station we calculated the Dip
and Strike and locate ourselves on map. At the second station the third member of
Nilawahan Group i-e Dandot Formation was encountered. Moving a little further at Station
44. 26
no 3 the first member of Jhelum Group i-e Baghanwala Formation was observed however it
was not well outcropped in the particular area. At station no 4the second member of Jhelum
Group i-e Jutana Formation was observed. At last we arrived at our last station marked on the
map as station no 5 where we observed the third member of Jhelum Group i-e Kussak
Formation and ended our first day field exposure.
45. 27
CHAPTER 4
PIDH VILLAGE ROAD SECTION
4.1 Introduction:
On 26th
Oct, 2018; the second day of our four days field started as we departed from our hotel
in KallarKahar towards Pidh Village (the second day field destination). The busses pick us up
at 10:00 AM in the morning from our hotels and it took us approximately one hour in
reaching Pidh Village. We arrived at Pidh Village around 11:00AM. The day was hot and dry
as the journey started and the average temperature was approximately 29◦C- 14◦C.
Pidh is a village, union council, and administrative subdivision of Chakwal District in
the Punjab Province of Pakistan. It is part of ChoaSaidan Shah Tehsil. Its geographical
coordinates are 32.6812° N, 72.9712° E. It is located about 170 km at the south of Islamabad,
the capital city Pakistan and about 36.4 km SE of KallarKahar.
Figure no 4.1.1: Location Map of Pidh Village; KallarKahar
We started our second day field and our teacher give us briefing about the area and we
concluded that we were standing on a dome. Dome is formed due to salt tectonics. All strata
was dipping away snd the central portion of the dome was collapsed.
46. 28
4.2 Baghanwala Formation
4.2.1 Observations:
We observed sandstone, shales of thin bedding of grey to light green in colour. Rock was not friable
and hardness was greater than 5 because it scratches hammer. We find salt pseudomorph crystals on
thr bedding plane but they were of small size. Due to vegetation contact with tobra was not clear.
4.2.2 Literature Work:
The name Baghanwala Formation is now given to the rocks of the “Pseudomorph Salt Crystal
Zone” of Wynne (1878) and the “Baghanwala Group” of Noetling (1849).
4.2.3 Type Section:
The type section is located near Baghanwala Village in the eastern Salt Range
4.2.4 Lithology:
The formation is composed ofshales and clays with alternate beds of flaggy Sandstone.
Figure 4.2.4.1 Shows sandstone of Baghanwala formation
4.2.5 Bedding Bedding Thickness:
In the study area we observed thin to medium beds of flaggy sandstone of slaty appearance.
4.2.6 Color:
It contains blood red shales with several colors of sandstone including greenish grey, olive
green and reddish white.
4.2.7 Environment of Deposition:
Lagoonaland restricted environment and arid climate conditions are the requirements for the
deposition of Baghanwala formation.
4.2.8 Contact:
The upper contact of the formation with Tobra formation is unconformable.
47. 29
The lower contact of the formation with Jutana Dolomite is conformable.
4.2.9 Fossils
The formation only contains cast and moldfossils but they were not recognized at the study
area.
4.2.10 Sedimentary Features
Numerous pseudomorphic casts of salt crystals are usually present along the bedding
planes and symmetrical ripple marks are also present.
4.2.11 Age
Early to Middle Cambrian.
4.3 Tobra Formation
Above the baghanwala formation there was massive beds of sand and conglomerates
4.3.1 Observations
We have observed Tobra Formation at 2 stops. One at contact of Baghanwala and Tobra at
station 1 and 2nd
at station 2 where it has contact with Dandot Formation. At station 1 it was
overlyn by splintery shales which was compacted and cement was sand in Tobra and having
variation in size of conglomerates. Roundness of conglomerates shows that this Tobra is of
Fluvial Environment rather than glacial environment.
4.3.2 Literature Work
The name Tobra Formation refers to the lowest formation of Nilawahan Group previously
known as “Talchir Boulder Beds “or “Talchir Stage” of Gee (1959) and “Salt Range Boulder
Beds” of Tichert (1967).
4.3.3 Type Section:
The type locality is located near Tobra Village in the eastern Salt range.
4.3.4 Colour
We observed variation in colour. In some beds fresh colour was golden brownish with
cobbles and pebbles and in some beds colour was light brown.
4.3.5 Bedding Thickness:
We observe Massive bedding Bedding Thickness.
48. 30
Figure 4.3.5 Shows massive bedding in Tobra Formation
4.3.6 Lithology
In lithology cement was sand and cobbles and pebbles are present. Sand of greenish grey,
golden brown in colour. Lithology was friable. Pink colour granite was also present.
49. 31
Figure4.3.6.1 Shows sandstone with cobbles and pebbles of Tobra Formation
4.3.7 Environment of Deposition:
It shows Fluvial environment of deposition.
4.3.8 Fossils
We did not recognize any fossil in field area.
4.3.9 Age
Early Permian.
4.3.10 Contact
The upper contact of the formation with Dandot Formation is transitional and
conformable.
The lower contact of the formation with Baghanwala Formation is disconformable.
Figure 4.3.10.1 Shows Transitional contact between Tobra and Dandot Formations
50. 32
4.4Dandot Formation:
After crossing Tobra Formation; at the top of last bed of Tobra formation we recorded
dip and strike which was found out to be:
Table 4.3.1 Shows Dip and Strike values
Dip Strike
6⁰NE N20⁰W
4.4.1 Observations:
Starting from the top of Dandot formation a change in visible lithology was observed. The
last conglomeratic bed of Tobra Formation was overlain transitionally by alternating beds of
shales and sandstone. The color of the outcrop was greenish grey or olive grey Which shown
oxygen deficient environment. The olive green color was due to the presence of micaceous
mineral. We also observed Trough-Cross bedding and Phosphatic nodules in the formation.
4.4.2 Literature Work:
The name Dandot Formation is formalized after the “Dandot Group” of Noetling
(1901), and includes the “Olive Series” of Wynne (1878) and the “Speckled Sandstone” of
Waagen (1879).
4.4.3 Type Section:
The type locality is near Dandot Village, eastern Salt Range
4.4.4 Lithology:
The lithology consists of sandstone with subordinate splintery shales.
4.4.5 Bedding Bedding Thickness:
Thin to medium beds of sandstone with shales.
4.4.6 Color:
It has light grey to olive green yellowish sandstone and dark grey and greenish shales
4.4.7 Environment of Deposition:
It is deposited in marine environment.
4.4.8 Contact:
The upper contact of the formation with Warcha Sandstone is sharp and conformable.
The lower contact of the formation with Tobra Formation is gradational.
51. 33
Figure 4.4.8.1 Shows contact between Warcha and Dandot Formation
4.4.9 Fossils:
Dandot Formation is fossiliferous but we did not observe any fossils at the study area.
4.4.10 Sedimentary Features:
It is characterized by the presence of Trough Cross Bedding and Phosphatic nodules.
Figure 4.4.10.1: Shows trough cross bedding and phosphatic nodules in Dandot formation
4.4.11 Age:
Early Permian.
52. 34
4.5 Warcha Sandstone:
4.5.1 Observations:
Travelling laterally along the same point after Dandot Formation a visible change in
lithology was observed. We saw the massive beds of sandstone whose weathered color was
greyish brown that was showing reducing environment. The grains when observed carefully;
were fine to medium. The fresh colour was greyish white. The sample extracted showing
medium grade sorting, and the grains were friable, less cemented and less compacted. The
outcrop was showing and Linear or Planner-cross bedding formed due to Bidirectional flow
of water. The characteristic features prove the outcrop to be Warcha Sandstone.
4.5.2 Literature:
The term Warcha Sandstone was coined by Hussain (1967), which has been approved by the
Stratigraphic Committee of Pakistan. Prior to the formalization of this name other terms were
used such as the “Warcha George” of Noetling (1901). The name such as “Speckled
Sandstone” of Gee (1945) and “Middle Speckled Sandstone” of Waagen (1879).
4.5.3 Type Section:
Its type section is in the Warcha George in the Salt Range.
4.5.4 Lithology:
The formation consists of medium to coarse grained cross bedded sandstone,
conglomeratic in places and has interbeds of shale. The grains are poorly sorted and less
cemented.
4.5.5 Bedding Bedding Thickness:
Bedding Bedding Thickness was thick to massive.
4.5.6 Color:
The sandstone is red, purple or shows lighter shades of pink. As per our observation the
weathered color of rock was found to be brownish grey while its fresh color was whitish
grey.
4.5.7 Environment of Deposition:
The formation is fluvial deposit.
4.5.8 Contact:
The upper contact of the formation is with Sardhai Formation which is conformable.
The lower contact of the formation is with Dandot Formation which is transitional and
conformable as in Figure 4.4.8.1.
4.5.9 Fossils:
We did not observe any fossils during our study.
53. 35
4.5.10 Sedimentary Features:
The formation shows Linear Cross-bedding and is moderately jointed, contain Systematic
joints.
Figure 4.5.10.1 Shows systematic joints and Linear cross bedding in Warcha Sandstone
4.5.11 Age:
Its age is Early Permian.
4.6Sakesar Limestone:
As we were moving uphill to examnineDandot and Warcha after this we move
downhill and move to the next spot where another formation was observed. Before it we
observe a normal fault which was not recognized on uphill.
Figure 4.6.1 Shows a normal fault
54. 36
4.6.1 Observations:
We observe the outcrop that appear to be highly fractured. The weathered color of the
outcrop was greyish white. After collecting the sample we observe the fresh color; that
appears creamy white in color. The beds were thick to massive and heavily fractured. The
grains were not visible even by the help of hand lens. Which proved it to be a chemical
sedimentary rock. The next step was to differentiate between; weather the rock is limestone
or dolomite.
With the help of acid we confirm presence of calcite in the rock which produced effervence
further some fossils was also observed.
4.6.2: Literature Work:
The name “Sakesar Limestone” was introduced by Gee (1935) for the most prominent
Eocene Limestone unit in the Salt and Trans-Indus Ranges.
4.6.3 Type Section:
Sakesar Peak in the Salt Range has been designed the type locality.
4.6.4 Lithology:
The unit consists dominantly of limestone. It was massive Limestone with nodular chert in it.
Figure 4.6.4.1 Shows Sakesar Limestone
4.6.5 Bedding Bedding Thickness:
Beds are of massive Bedding Thickness.
4.6.6 Colour:
The limestone is cream coloured to light grey.
4.6.7 Environment of Deposition:
The formation was deposited in shallow shelf environment.
4.6.8 Contact:
Lower contact of the formation is conformable with Nammal Formation
Upper contact of the formation is conformable with Chorgali Formation.
55. 37
4.6.9 Sedimentary Features:
The Sakesar limestone is heavily fractured and it is generally recognized by Chert nodules
(Cryptocrystalline Silica).
4.6.10 Fossils:
The formation consists of Assilina (eye shape) and Nummulities (rounded shape). The
outcrop is fossiliferous and contain other species of fossils as well.
4.6.11 Age:
Early Eocene age.
After observing Sakesar Limestone, we moved to our next formation. It was near Khewara
Salt Mine so busses took us there.
4.7 Khewra Sandstone:
4.7.1 Observations:
There were massive beds of reddish brown colored sandstone and there were joints and
fractures in it. After collecting the sample we observed it carefully and it was very well sorted
and compacted. The grains were medium to coarser. The fresh color of the sample was
appeared to be reddish brown. Economically Khewra Sandstone can act as a potential
reservoir rock. The sandstone beds were thick.
4.7.2: Literature Work:
The name “Khewra Group” was originally proposed by Noetling (1894). Prior to that, Wynne
(1878) called the formation “Purple Sandstone Series”. The latter name continued until
recently, when the name of the formation was formalized as “Khewra Sandstone’ by the
Stratigraphic Committee of Pakistan, Fatmi (1973).
4.7.4 Lithology:
The formation is predominantly composed of fine grained sandstone.
Figure 4.7.4.1 Shows khewra sandstone
56. 38
4.7.5 BeddingBedding Thickness:
Beds were thick to medium.
4.7.6 Colour:
The sandstone is reddish brown.
4.7.7 Environment of Deposition:
Lagoonal environment of deposition.
4.7.8 Contact:
The upper contact of the formation with Kussak Formation is gradational.
The lower contact of the formation with Salt Range Formation is normal and
conformable.
4.7.9 Fossils:
We do not observe any fossil there.
4.7.10 Age:
Early Cambrian.
4.8 Salt Range Formation
4.8.1 Observations:
We reached at the last stop of day 2 field. Here we observe Salt Range Formation. It has three
members Sahwal Marl Member, BandrkasGpysumMember ,Billian Walla Salt Member. We
observe Sahwal Marl Member practically due to shortage of time we did not able to observe
Bandar kas Gpysum Member. Billiawala Salt Member is not exposed.
4.8.2: Literature Work:
Wynne named and described the formation as “Saline Series” (1878). Gee called the same
unit as “Punjab Saline Series” (1945). Asrarullah has given the present name “Salt Range
Formation” (1956) after the Salt Range.
4.8.3 Type Section:
Khewra George in the eastern Salt Range is designed as the type section.
4.8.4 Lithology:
Billianwala Salt Member:
It is largely composed of hematitic, dull red, gypsiferousmarly beds with thick seams of salt.
Its base is not exposed.
Bandar Khas Gypsum:
It is composed of massive gypsum, dolomite and marl it overlies the Billianwala and marl.
57. 39
Sahwal Marl Member:
The member overlies the Bandar Khas Member and is comprised of an upper bright marly
unit containing dull red marl.
4.8.5 Environment of Deposition
Environment of deposition for Marl is deep marine with Arid climate conditions.Gpysum and
Salt formed in Restricted and lacustrine environment. If evaporation is 80% then gypsum is
formed is 90% then salt will formed.
4.8.6 Contact:
The upper contact of the formation with Khewra Sandstone is normal and
conformable.
The lower contact of the formation is with metamorphic rock complexes of
Precambrian age.
4.8.7 Fossils:
No fossilswas observed.
4.8.8 Age:
Its age is Precambrian.
4.8.9 Tectonics:
Standing on the Sahwal Marl Member of Salt Range Formation; we studied the general
tectonics of that area. That is:
From MBT to SRT part of Himalayas are called sub Himalayas (lowest most
Himalayas).
From MBT to MCT is lesser Himalayas.
From MCT to MMT there are higher Himalayas. And;
Between MMT and MKT is KIA and North of MKT is Eurasian plate. SRT is the
youngest thrust fault and trending East to West and dipping toward North-northeast.
Eastern boundary and surrounding zone between MBT and SRT is called Potwar Sub-
Basin and also there is Jhelum strike slip fault along Jhelum river whereas, western boundary
is with Kalabagh strike slip fault along Indus river. Portion between Jhelum fault and
Kalabagh fault is called Potwar Sub-Basin and west of Kalabagh fault between SRT and
MBT portion is called Kohat Sub-Basin. West of Kalabagh fault range making curve is called
Surghar range and below this is Khisor range. Ranges between two rivers (Jhelum and Indus)
is called Sis-Indus ranges and Surghar andKhisor ranges are called trans-Indus ranges
Potwar sub basin is divided in two parts:
I. Southern Potwar deformed zone: area between SRT and SOAN SYNCLINE
58. 40
II. Northern Potwar deformed zone: area between SOAN SYNCLINE and MBT
Both have different structure style deformation due to presence of salt and Bedding
Thickness of salt at Southern Potwar deformed zone salt cover is thicker and all the
deformation is controlled by salt. Salt shows ductile behavior and above it the hard material
shows brittle behavior and when Collison takes place basement doesn’t disturbs and salt and
gypsum act as lubricant but upper hard strata is deformed that’s why SRT is called
Decollement fault and effect doesn’t goes to the basement rock so this tectonic is called thin
skin tectonic or salt tectonics whereas, at Northern Potwar deformed zone salt cover is thin
but more imbrications. For salt to take part practically in deformation its Bedding Thickness
must be more than hundred meters.
Figure 4.8.9.1 Shows Salt Range Thrust
59. 41
CHAPTER 5
NAMMAL GORGE
5.1 Introduction:
On 27th
Oct, 2018 we departed from hotel at 09:30am. We reached Nammal Gorge at 12:00pm. It is
located in western salt range.
Economically Nammal gorge is very important. Large quantities of limestone, sandstone and
silica sand are being extracted from the gorge. The quarries of limestone present here are
fulfilling the needs of cement factories as well as construction purposes.
Nammal gorge is a domal structure cut by the water body, on both sides we found the
same formation along the strike. We started moving towards dip so the next formation was
younger and the sequence of formations were from older to younger.
Figure 5.1.1 Shows entrance of Nammal Gorge
5.2 Observations at Starting Point:
At starting point first we locate our self on the map and find the north. We observed the
faulted surface. These faults were normal faults, horst and graben structures were observed,
formed due to salt tectonics. Overall colour of the outcrop was light brown.
60. 42
Figure 5.2.1 Shows normalfault
5.3 Amb Formation
It is the first member of Zaluch Group.
5.3.1 Observations:
Travelling little further small upper bed of Amb Formation was only exposed at this
point. We observed the contact between the two formations. We locate our self on map and
mark the contact. With help of chisel collected the sample of the formation and observe them.
Fresh sample smells like rotten egg.
5.3.2 Literature:
Teichert (1966) suggested the name Amb Formation which was formalized by the
Stratigraphic Committee of Pakistan.
5.3.3 Type Section:
Amb village in the central Salt Range is designated as the type section for the formation.
5.3.4 Lithology:
Amb Formation consist of shale, sandstone and limestone.The sandstone is brownish grey,
medium-grained, calcareous and medium to thick bedded. These sandstone beds occupy the
lower part of the formation.
61. 43
Figure 5.3.4.1 Shows Amb formation
5.3.5 Fossils:
The formation is highly fossiliferous,has reported abundant pollen and spores. Pascoe
(1959) described the presence of rich fauna rom the formation, which consists of fusilinids,
bryozoans, brachiopods, bivalves and gastropods. (SHAH,2009)
5.3.6 Age:
Age of the formation is late Permian.
5.3.7 Contact:
Amb formation have sharp contact with overlying Wargal formation
Figure 5.3.7.1 Shows contact between Amb formation and Wargal Limestone
62. 44
5.4 WargalFormation
It is the second member of ZaluchGroup. It is not purely composed of limestone that’s why it
is not called wargal limestone.
5.4.1 Observations:
We collected the outcrop of the formation that have contact with Amb formation with
the help of chisel. We identify the lithology as the outcrop was compacted and have crystals.
The formation have very thick massive beds. Weathered color of outcrop was creamy white
while fresh color of outcrop was light greyish too white.
5.4.2 Literature:
The name Wargal Limestone, as approved by the Stratigraphic Committee of Pakistan
was introduced by Teichert (1966) to the unit formerly known as “Middle Products
limestone” of Waagen (1879) and “Wargal group of Noetling (1901).
(SHAH,2009)
5.4.3 Type Section
Type section is Wargal village in the central salt range.
5.4.4 Lithology:
The lithology comprises of compacted massive beds of limestone and dolomite of light
to medium grey, Shale and sandy limestone.
5.4.5 Environment of Deposition:
Its environment of deposition is shallow marine.
5.4.6 Fossils:
The fauna consists of abundant bryozoans, brachiopods, bivalves, gastropods,
nautiloids, ammonoids, trilobites and crinoids.
We observed the productus during the field.
Figure 3.4.6.1 Shows productus brachiopods fossil in Wargal Formation
63. 45
5.4.7 Age:
Age of formation is late Permian.
5.4.8 Contact:
Lower contact with Amb Formation is Sharp.
Transitional contact with overlying Chhidru Formation.
Figure 5.4.8.1 Shows contact between Wargal and Chhidru formation
5.4.9 Dip and Strike of Wargal
Dip Strike
65⁰NW N50⁰E
Table 5.4.9.1 Shows values of dip and strike
Figure 5.4.9.1 Shows Wargal Formation
64. 46
5.5 Chhidru Formation:
It is the last member of ZaluchGroup.
5.5.1 Observations:
Travelling little further we observed the change in lithology. We collected the outcrops
with the help of chisel at different points and observe them to identify the formation. The
lithology at the base was fine grained,friable and have phosphatic nodules. Its weathered
color was pale yellow. Above this lithology we observe the outcrop that have crystals whose
weathered color is greyish white. On the top we observe compacted fine grained white
sandstone whose weathered color was brownish white but its fresh color was white. The beds
of the formation were medium to thick.
5.5.2 Literature:
The name, "Chhidru beds" was given by Waagen (1891) and " Chhidru Group" by
Noctling (1901) to the topmost beds of commonly known "Productus Limestone". The name
Chhidru Formation was introduced by Dunbar (1933), which is now formalized by
stratigraphic committee of Pakistan.
5.5.3 Type Section:
Type locality is Chhidrunala.
5.5.4 Lithology:
The formation at the base is composed of shale unit have thin to medium beds of
brownish grey color with yellow spots of phosphatic nodules. Overlying this unit have beds
of calcareous sandtone and few sandy limestone of greyish white color. On the top have
white sandstone which is medium to fine grained.
5.5.5 Environment of Deposition:
Environment of deposition is shallow marine, littoral to paludal
5.5.6 Sedimentary Structure
Wavy bedding was observed in the formation as shown in Figure 5.4.8.1.
5.5.6 Fossils:
Various fossils reported from Chhidru Formation are Brachiopods and Ammonites.
5.5.7 Age:
Age of the formation is late Permian.
5.5.8 Contact:
Lower contact with Wargal Limestone is transitional
Upper contact with Mianwali formation have Paraconfirmity making the permio-
triassic boundary between the chhidru and mianwali formation
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Figure 5.5.8.1 Shows contact between Chhidru and Mianwali formation which marks the PT boundary
5.6 Mianwali Formation
It is the first member of Musakhel Group.
5.6.1 Observations:
White sandstone of Chhidru Formation ends and new formation starts comparatively
less resistant. At this point we observed the 3 different formations up hill, their members and
mark their contacts. We also observed the fossils impressions in the outcrops.
5.6.2 Literature:
Lower part of Mianwali series” by Gee (1959), “Top most limestone and dolomite
beds” by Waagen (1879) was named as “Mianwali formation” by Kummel in (1969).
5.6.3 Type Section:
Formation is best exposed in Zaluchnala and Khisor ranges.
5.6.4 Lithology:
It consists of three members.
Kathwai member:
It is the lower most part of the Mianwali formation and mainly consist of crystalline
dolomite in the lower part have fossil fragments ammonoids and limestone in the upper part.
Mittiwali member:
The lithology consists of grey, fine-grained, non-glauconitic limestone with abundant
ammonides. The basal beds consist of limestone. The rest of the unit consists of greenish to
greyish shale, silty shale with some sandstone and limestone interbeds. The unit is richly
fossiliferous
Narmia member:
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The basal bed of Narmia member consists of dark grey to brown fragmental limestone,
sandy in part and containing fossils. The rest of the unit consists of grey to black shale with
interbeds of sandstone and lenticular limestone or dolomite. The topmost bed is a grey to
brown massive dolomite.
Figure 5.6.4.1 Shows Members of Mianwali Formation
5.6.5 Environment of Deposition:
Environment of deposition is marine to deltaic environment.
5.6.6 Fossils:
Ammonoids are reported in the formation.
Figure 5.6.6.1 Shows Ammonites in Mianwali Formation
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5.6.7 Age:
Age of the formation is early Triassic.
5.6.8 Contact:
Lower contact with Chhidru Formation have paraconfirmity
Upper contact with Tredian formation is well defined/sharp and confirmable.
5.7 Tredian Formation:
It is the second member of MusakhelGroup.
5.7.1 Observations:
Contact of Mianwali formations was marked with overlying Tredian formation. Two
members of Tredian formation were distinguished. Weathered color of lower member was
reddish to mehroonish while uppermember was greyish brown.
5.7.2 Literature:
The name Tredian Formation was introduced by Gee (in Kummel 1966) to replace, in
part, his earlier name "Kingriali sandstones" (Gee, 1945). (SHAH,2009)
5.7.3 Type Section:
Its Bedding Thickness is 76 m in the Zaluch section of the Salt Range
5.7.4 Lithology:
The formation comprises of two members; the lower is Landa Member (Kummel,
1966) and the upper is the Khatkiara Member (Shah 1967).
Landa Member:
It consists of sandstone and shale. The sandstone is micaceous and varies in colour
from reddish to mehroonish. It is thin to thick-bedded, with ripple marks and slump structure.
Khatkiara Member:
It is massive, thick-bedded white sandstone whose weathered color is greyish brown
that grades into the overlying Kingrali Formation.
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Figure 5.7.4.1 Shows Member of Tredian Formation
5.7.5 Environment of Deposition:
Environment of deposition is shallow marine to deltaic.
5.7.6 Sedimentary Structure:
Trough cross bedding was observed in Khatkiara member of Tredian Formation.
Figure 5.7.6.1 Shows Trough cross bedding in Tredian Formation
5.7.7 Fossils:
Various fossils found in formation are plant fossils
5.7.8 Age:
Age of the formation is middle Triassic
5.7.9 Contact:
Lower contact with mianwali formation and well defined and confirmable
Upper contact with Kingriali formation is confirmable.
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Figure 5.7.9.1 Shows contact between Tredian and Kingriali Formation
5.8 Kingriali Formation:
It is the last member of MusakhelGroup.
5.8.1 Observations:
We marked the contact of the formation with underlying Tredian formation and
distinguished two members of Kingriali Formation. Doya member consist of orange
(weathered color) beds of sandstone and dolomite. Outcrop of Vingari member was observed
which was compacted and its weathered color was light brown.
5.8.2 Literature:
The name "Kingriali Dolomite" was used by Gee (1945) and later amended as Kingriali
Formation, because several lithological facies are represented.
5.8.3 Type Section:
Good sections of the formation occur in ZaluchNala in the Western Salt Range,
LandaNala In the Surghar Range and in the TapanWahan Gori Tang Nala in the Khisor
Range.
5.8.4 Lithology:
The formation comprises of two members
Doya member:
The name Doya Member is derived ater the Doya Village in the SurgharRange.It
consists of sandstone and dolomite interbeds with fossiliferous limestone and minor shale.
The sandstone is light grey to greyish white, pinkish, weathering brownish grey, fine to
medium grained, thick bedded, soft, micaceous, dolomitic, friable and cross-bedded. The
dolomite is brownish grey to brown, coarse grained, hard, sandy, jointed and fractured. The
limestone is grey to brownish grey, medium bedded, dolomitic, sandy crinoidal and hard.
Vingari member:
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The name Vanjari Member is derived after Vanjari Village in the Surghar Range. It
mainly consists of dolomite. The dolomite in the lower part is brown, purple to purplish grey,
weatheing dark brown to brownish grey, coarse grained, massive, hard, highly brecciated,
jointed, fractured and forms cliffs. The dolomite in the upper part is whitish to light grey,
micritic, thin bedded to flaggy and medium hard.
Figure 5.8.4.1 Shows Doya and Vingari Member of Kingriali Formation
5.8.5 Environment of Deposition:
Environment of deposition is shallow marine.
5.8.6 Sedimentary Structure:
Honey comb weathering was observed.
5.8.7 Fossils:
Poorly preserved fossils of brachiopods, bivalves and crinoids are present.
5.8.8 Age:
Age of the formation is late Triassic.
5.8.9 Contact:
Lower contact with Tredian Formation isconfirmable.
Upper contact with data formation is disconfirmable.
5.9 Datta Formation:
Data formation is member of Surgar Group.
5.9.1 Observations:
After the Kingriali Formation the lithology changes, contact between the Kingriali and
overlying formation was marked. The outcrop of the formation was collected whose
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weathered color was reddish to brownish grey. Red color was due to hematite. Sulphur was
also present and oil seepages were also seen at this point.
5.9.2 Literature:
The name Datta Formation was introduced by Danilchik (1961) and Danilchik and
Shah, (1967) to replace the name "Variegated stage of Gee.
5.9.3 Type Section:
Type section is located in Data nala in Surgar ranges.
5.9.4 Lithology:
It consists of variegated red, maroon, grey, green and white sandstone, shale, siltstone
and mudstone with irregularly distributed calcareous, dolomitic, carbonaceous, ferruginous
glass sand and fireclay horizons. The fireclay is normally present in the lower part while the
upper part includes a thick bed of maroon shale.
Figure 5.9.4.1 Shows outcrop of Datta Formation
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Figure 5.9.4.2 Shows oil seepage in Datta Formation
5.9.5 Environment of Deposition:
Environment of deposition is very shallow marine to deltaic and alluvial plains.
5.9.6 Sedimentary Structure:
Ripple marks ionand cross bediing was observed in formation
Figure 5.9.6.1 Shows Ripple marks in Datta Formation
5.9.7 Age:
Age of the formation is Early Jurassic.
5.9.8 Contact:
Lower contact with Kingriali Formation is disconfirmable.
Laterite bed of Datta formation marks the KT Boundary
Formation has confirmable contact with upper Samanasuk Formation.
Figure 5.9.8.1 Shows Contact between Datta and Samanasuk Formation
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5.9.9 Economic Importance:
fire clays used in pottery,
abundant sulphur.
china clay
coal mines
organic shale source
5.10 SamanaSuk Formation:
It is the member of SurgarGroup.
5.10.1 Observations:
As we move forward lithology changes, small bed of the formation was exposed at this
point. Outcrop of the formation was observed that have patches and ooids. Weathered color
of the outcrop is brownish white.
5.10.2 Literature:
“Bared limestone” by Gee, “Upper part of Kyoto limestone” by Cutler (1933) is named as
Samana Suk formation by Davies in 1930(SHAH,2009)
5.10.3 Type Section:
Fatmi (1968) designated a section northeast of Shinawari in the western part of the Samana
Range as the type locality.
5.10.4 Lithology:
The formation consists of grey to dark grey limestone with subordinate marl and calcareous
shale intercalations. The limestone is oolitic and has some shelly beds. The limestone is
lighter in colour, medium to thin- bedded and is marly and shaly in the lower part.
Figure 5.10.4.1 Shows outcrop of samanasuk limestone
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5.10.5 Environment of Deposition:
Environment of deposition this formation is shallow marine shelfful to super tidal
environment
5.10.6 Fossils:
From the uppermost beds a middle Callovian fauna has been recorded in the Surghar
Range. It consists of brachiopods, bivalves, gastropods, ammonoids and crinoids. In field we
had not observed any fossil. (SHAH, 2009)
5.10.7 Age:
Age of the formation is Middle Jurassic.
5.10.8 Contact:
Lower contact with Datta Formation is confirmable.
Contact with overlying Chichali formation is disconfirmable.
5.11Hangu Formation:
It is the member of MakarwalGroup.
5.11.1 Observations:
Change in lithology was observed after the Lumshiwal. Weathered color of the outcrop
is greyish black.
5.11.1 Literature:
The "Hangu Shale" and "Hangu Sandstone" of Davies (1930) from the Kohat area have
been formalized by the Stratigraphic Committee of Pakistan (1973) as Hangu Formation.
5.11.2 Type Section:
Type section of the formation has been designated at Fort Lockhart
5.11.3 Lithology
In the Salt Range and Trans-Indus ranges, the formation consists of dark grey, rarely
variegated sandstone, shale, carbonaceous shale and some nodular, argillaceous limestone.
The carbonaceous content increased locally and constitutes coal seems in parts of the Surghar
Range.
5.11.4 Fossils:
Formation contains beleminites.
5.11.5 Age
Age of the formation is Early Paleocene.
5.11.6 Contact
Lower contact with Lumshiwal Formation is disconfirmable.
Upper contact is confirmable with overlying Lockhart Limestone
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5.12 Lockhart Limestone
It is the member of MakarwalGroup.
5.12.1 Observations:
Above Hangu shale lithology changes and nodularity is observed in the outcrop.
Weathered color of the outcrop is light brown and have massive beds.
5.12.2 Literature
Davies introduced the term “Lockhart Limestone” for a Paleocene limestone unit in the
Kohat area and this usage has been extended by the Stratigraphic Committee of Pakistan to
similar units in other parts of the Kohat-Potwar and Hazara areas.
5.12.3 Type Section
Fort Lockhart in the Samana Range has been designated as the type locality of the uni
5.12.4 Lithology
In the Salt Range and Trans-Indus ranges, the limestone is grey to light-grey, medium
bedded, nodular, with minor amounts of grey marl and dark bluish grey calcareous shale in
the lower part. The weathered color of the outcrop is light brown. Fresh surface give pungent
smell due to carbonaceous material and act as source rock in Dhakni oil field. Formation also
have sulphur content.
Figure 5.12.4.1 Shows outcrop of Lockhart Formation
5.12.5 Fossils:
Micro fossils are found,umbrella shape called Lokhartia ,no mega fossils are found but we
have not seen them on field.
5.12.6 Age
Age of the formation is Paleocene
5.12.7 Contact:
Lower contact is conformable with Hangu Formation.
Upper contact is conformable and transitional with Patala.
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Figure 5.12.7.1 Shows contact between patala and lokhart limestone
5.13Patala Formation
5.13.1 Observations:
After the top bed of Lockhart limestone change in lithlogy was observed. Thin beds of
nodular limestones were present. It was mainly composed of splintery shale with interbedded
limestone having weathered colour yellow to rusty brown. The formation was Patala
Formation. It is proven source rock in upper indus basin.
5.13.2 Literature:
Patala Shales” by Davies (1937), “TarkhobiShales” by Eames (1952), “Hill Limestone” by
Wynne (1873). The present name was given by Stratigraphic Committee of Pakistan.
(SHAH,2009)
5.13.3 Type Section:
The section exposed in Patalanala is designated as type section in Salt range.
(SHAH,2009)
5.13.4 Lithology:
In the Salt Range the formation consists of shale and marl with subordinate limestone
and sandstone. The shale is dark greenish grey selenite-bearing, in places carbonaceous and
calcareous and also contains marcasite nodules. The limestone is white to light grey and
nodular. It occurs as interbeds. Subordinate interbeds of yellowish brown and calcareous
sandstone are present in the upper part.
5.13.5 Fossils:
The formation is richly fossiliferous and contains abundant foraminifcrs, molluscs and
Ostracodes. From the Salt Range, Smout and Haque (1956) recorded larger foraminifcra
including Assilina.
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5.13.6 Age:
Age of the formation is Late Paleocene
5.13.7 Contact:
Lower contact with Lockhart Limestone is transitional and confirmable.
Upper contact with overlying Nammal Formation is transitional and conformable.
Figure 5.13.7.1 Shows contact between Nammal and patala formation
5.14Nammal Formation
It is member of ChharatGroup.
5.14.1 Observations:
After Patala Formation first proper beds of white limestone appears that marks the
change in formation. Beds of whitish or greyish loose shale was also present so alternating
beds of shale and Limestones were present. The Bedding Thickness of limestone beds
increases. Thin to medium and some thick bed of limestones were observed.
5.14.2 Literature:
The term Nammal Formation has been formally accepted by the Stratigraphic
Committee of Pakistan for the “Nammal Limestone and Shale” of Gee (in Fermor, 1935) and
“Nammal Marl” of Danilehik and Shah (1967) occurring in the Salt and Trans Indus Ranges
5.14.2 Type Section:
The section is exposed in the Nammal Gorge
5.14.3 Lithology:
The formation, throughout its extent, comprises of shale, marl and limestone. In the
Salt Range, these rocks occur as alternations. The shale is grey to olive green, while the
limestone and marl are light grey to bluish grey. The limestone is argillaceous in places.
5.14.4 Fossils:
Abundant fossils, mainly foraminifers and molluscs, have been reported from the formation.
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Assilina and Numilities are the index fossils of Eocene age.
5.14.5 Age:
Age of the formation is Early Eocene
5.14.6 Contact:
Lower contact with Patala Formation is transitional and confirmable.
Upper contact is transitional with Sakeser limestone.
(SHAH,2009)
5.15Sakesar Limestone:
It is a member of chharat group.
5.15.1 Observations:
Four massive beds of limestones were observed
Figure 5.15.1.1 Shows Nammal and Sakesar limestone
5.15.2 Literature:
The term "Sakesar Limestone" has been introduced by Gee after the peak Sakesar in the
Central Salt Range.
(SHAH, 2009)
5.15.3 Type Section:
The formation is widely distributed in the Salt Range and the Surghar Range. In the Salt
Range its Bedding Thickness varies between 70 m and 150 m.
5.15.4 Lithology
The Formation consists predominantly of limestone with subordinate marl. The
limestone throughout its extent is cream colored to light grey, nodular, usually massive with
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considerable development of chert in the upper part.In the mapped area, the Sakesar
limestone is composed of dense homogeneous limestonewhich varies from light grey to dark
grey in color. It is massive too thick bedded and is highly fossiliferous at places.
5.15.5 Fossils:
The formation has yielded a ich assemblage of foraminifers, molluscs and
echinoids.Some of the important foraminifers are Assilina. Assilina and Numilites are index
fossils of Eocene age.
(SHAH,2009)
5.15.6 Age:
Age of the formation is Early Eocene
5.15.7 Contact:
Lower contact with Nammal formation is transitional.
Upper contact with Chorgali formation is confimable.
5.16 Physiographic Profile:
Conclusion Day 3
On day 3 we started our field trip at 11:30 am in Nammal gorge and ended in the evening at
about 5 pm. At first we locate ourselves on map and identify the north. Throughout our field
we observed different formations, contact between the formations and identify the formations
by observing their outcrops.
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CHAPTER 6
KALLAR KAHAR ROAD SECTION
6.1 Introduction
KallarKahar is a town and subdivision (Tehsil) of Chakwal District in Punjab, Pakistan.
It is the capital of KallarKahar Tehsil. It is Located .at a distance of 25 km north to Chakwal
city and 124.2 km from Islamabad via Islamabad-Lahore motorway M2. Geographic co-
ordinates of KalarKahar are latitude 32°46.9998′ N and longitude: 72°42′ E.
The climate of the area is sub-humid, sub-tropical continental type with hot to moderate
summer and severe winter. The thirty-year average precipitation was 853 mm for the Salt
Range region but is estimated 500 mm for KallarKahar. The mean monthly temperature
varies between, 29◦C (Max)-13◦C (Min).
On 28 2018 field was take place in KalarKahar along road section. We move along the
road section and observed three formations, Kamliyal Formation, Murree Formation and
Chorgali Formation. The sequence of formations was from younger to older. Travelling
through the KallarKahar road we stopped at our first station and started the field.
6.2 Kamliyal Formation
It is a member of Rawalpindi group.
6.2.1 Observations:
The outcrop was observed thoroughly. Between two massive beds thin bed of
conglomerate was present. Weathered color of outcrop from massive bed was greenish grey
while its fresh color was olive green. It was semi compacted, comparatively fraiable and have
medium to coarse grains, some grains were dull white angular or semi rounded and some
grains give blackish and greenish appearance.
6.2.2 Literature:
The "Kamlial beds" of Pinfold (1918) have been formally established as Kamlial
Formation by the Stratigraphic Committee ofPakistan. The formation is equivalentto the "
Kamlial Stage" of Pascoe (1963). (SHAH,2009)
6.2.3 Type Section:
A section southwest of Kamlial, Attock District has been designated as the type section.
6.2.4 Lithology
The formaion consists of greenish-grey sandstone which is medium to coarse grained
and contains interbeds of shale, and intra fonnational conglomerate. It is distinguished from
the underlying Murree Formation by its usually spheroidal weathering and heavy minerals
content mainly epidote.
6.2.5 Age:
Age of the formation is Late Miocene age.
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6.2.6 Contact
The formation underlies the Murree Formation conformably with a broadly sharp
contact.
Figure 6.2.6.1 Shows contact of murree with kamlial formation
6.3 Murree Formation
It is a member of Rawalpindi group. First originated from Himalayas, on foot hill have
molasse deposits.
6.3.1 Observations:
Lithology changes, massive bed of sandstone disappear and maroonish to purplish
massive bed of clays appear at the base. Beds of sandstone and conglomerates are also
present over the clays. Outcrop from these beds have coarse grains. The weathered color of
the outcrop was brownish grey while its fresh color is grey. Through hand lens we observe
white shiny grains and blackish grains which are of flaky nature while angular white grains
are also present. Blackish flaggy grains are due to presence of Biotite and whitie shiny grains
are due to presence of Muscovite. White angular grains are slica.
6.3.2 Literature:
The "Mat Group" of Wynne (1874), "Murree Beds" of Lydekker (1876) and "Murree
Series" of Pilgrim (1910) have been formally named Murree Formation by the Stratigraphic
Committee of Pakistan.
6.3.3 Type Section:
A section exposed to the north of the DhokMaiki in the AttockDistricthas been designated the
type section.
6.3.4 Lithology:
The formation is composed of a monotonous sequence of darkred and purple clay and
purple grey and greenish grey sandstone with subordinate intra-formational and conglomerate
with abundant derived larger foraminifers of Eocene age.
6.3.5 Fossils:
Bullet shape fossils were observed called belliminites which are reworked fossils.
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6.3.6 Age:
Age of the formation is Early Miocene
6.3.7 Contact:
The formation unconformably overlies various formations of Eocene age.
6.4 Chorgali Formation
6.4.1 Observations:
After observing the Murree formation we travel along the road section and after five
minutes’ drive we reach at our last station which was Best way cement road section where we
observe new formation.. It was an anticline, we started our observation from one limb
towards the second limb. At the base massive beds were present whose weathered color was
pale yellow and fresh color was greyish white. Fossils was present in these beds and also
show effervescence which confirm that these are beds of limestone. Between beds of
limestone friable greenish grey shale was present. As we move towards the second limb we
also found massive beds of clays and highly compacted poorly sorted lithology whose
weathered color was reddish brown but fresh color was greyish brown. We found the values
of Dip and Strike at this point.
Dip Strike
7NW N70E
On reaching the second limb we again find the dip and strike values.
Dip Strike
9SW N67E
We observed that the Dip angle changes from one limb to the another limb.
6.4.2 Literature:
The term "Chorgali beds" of Pascoe (1920) has been formalized as Chorgali Formation by the
Stratigraphic Committee of Pakistan.
6.4.3 Type Section:
The section exposed in the Chorgali Pass in the Khair-e-Murat Range, has been chosen
as the type section.
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6.4.4 Lithology:
In the Salt Range, the formation is also divisible into two parts. The lower part consists
of shale and limestone, while the upper part is mainly limestone. The shale of the lower part
is greenish grey or buff and calcareous, and the limestone is light grey and argillaceous. the
formation have massive beds.
Figure 6.4.4.1 Shows Anticlinal limb of chorgali formation
6.4.5 Fossils:
Rich fossil assemblage including foraminifers, molluscs and ostracodes has been reported.
Assilina and Numilites are index fossils of Eocene age.
6.4.6 Age:
Age of the formation is Early Eocene.
6.4.7 Contact:
Hazara. In the Salt Range, the formation conformably overlies the Sakesar Limestone
and at other places Margala Hill Limestone. In the Salt Range, it is unconformably overlain
by the Murree Formation, while conformably in other areas by the Kuldana Formation.
84. 66
Conclusion Day 4:
During our last day field we observed three formation that was Kamliyal, Murree and
Chorgali Formation. We observed the outcrops of the formation, their grain sizes and the
fossils that are present in them. We also found the contact between the Kamliyal, and Murree
formations. These formations show erosion of Himalayas, and deposition after uplifting of
Himalayas. In Chorgali formation that form an anticline we find out dip, and strike values
which shows that dip angle changes from one limb to another. Thin beds of shale are present
between the massive beds of limestones in Chorgali Formation.
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CONCLUSION
The Salt Range is one of the most important geological regions in Pakistan. It is easily
accessible and displays a wide variety of geological features and paleontological remains. It
is characterized by extensive Anticlines folds, Synclines folds and various types of Faults. It
is also considered as a source of minerals e.g. Halite, gypsum, Coal, fire clay etc. Numerous
coal mines are present in the area, being extracted from Patala Formation of Eocene age. The
occurrence of these minerals is important in stratigraphic as well as paleontological point of
view. It represents an open book of geology with richly fossiliferous. All the strata are
excellently exposed due to lack of vegetation. The quality of the exposure also provides
excellent opportunities to appreciate tectonic features in the field. The Salt Range is,
therefore, of international scientific and educational value, and is highly worthy of
conservation and preservation.
Main purpose of the field trip was to give students practical hands on experience about the
field work, back bone of geology. Study the distribution of the various time units in the Salt
Range area, so as to investigate the lateral changes in these units and how to correlate them in
different parts of the Salt range. After this field, we got a clear idea how to mark litho-logical
units, sedimentary and structural features.
We observed certain sedimentary features like joints; ripple marks, cross bedding fault,
Honeycomb weathering and Trough cross bedding etc. We also learnt how to measure dip
and strike. We observed rocks of different ages like from Pre-Cambrian to Miocene along
with the structural and sedimentary features in the areas of Karoli village, Pidh village,
Nammal gorge, KalarKahar Road section.
