Salt range field report

FIELD REPORT – FIELD TRIP TO SALT RANGE
THRUST, PAKISTAN
BY
GROUP 6
DEPARTMENT OF EARTH AND ENVIRONMENTAL
SCIENCES, BAHRIA UNIVERSITY, ISLAMABAD

I
ACKNOWLEDGEMENT
All praise to Almighty Allah who granted us the determination and capability to work on
and bring together this field report. We are thankful to the Department of Earth and
Environmental Sciences, Bahria University Islamabad Campus for presenting us with this
opportunity of the four-day fieldwork during our coursework as it helped us gain extensive
practical knowledge. Finally, we are thankful to our field instructors; to whom we are
indebted to as they provided their constant support and guidance throughout the fieldwork.
Their instructions and oversights aided us in better understanding the geological features,
structures and formations in the fieldwork.

II
ABSTRACT
This report highlights our four-day fieldwork in the Salt Range from 07-11-17 to 11-11-
17. This report consists of the overview of the trip, the general stratigraphy and geology of
the areas visited, the observations made, and the conclusions drawn from these
observations.

III
Table of Contents
Table of Contents ...........................................................................................................................................................III
1. CHAPTER 1 INTRODUCTION ....................................................................1
1.2. LOCATION AND ACCESSIBILITY......................................................................................................2
1.4. MAIN THRUST FAULTS.........................................................................................................................3
1.5. THE AIMS AND OBJECTIVES ..............................................................................................................5
1.6. EQUIPMENT ...............................................................................................................................................5
1.7. METHODOLOGY ......................................................................................................................................5
2. CHAPTER 2 FIELD OBSERVATIONS................................................................................................8
2.1. DAY 1. EASTERN SALT RANGE (KAROLI ROAD SECTION) ………………………………………….8
2.1.1. STATION 1…………………………………………………………………………………………………………………….8
2.1.1.1. STOP 1………………………………………………………………………………………………………………………….9
2.1.1.2. STOP 2…………………………………………………………………………………………………………………………11
2.1.1.3. STOP 3……………………………………………………………………………………………………………………… 12
2.1.1.4. STOP 4(a) ………………………………………………………………………………………………………………….14
STOP 4(b) ………………………………………………………………………………………………………………….15
STOP 4(c) ……………………………………………………………………………………………………………….…17
2.1.1.5. STOP 5………………………………………………………………………………………………………………….…18
2.2. DAY 2. EASTERN SALT RANGE………………………………………………………………………………………21
2.2.1. STATION 1. PIDH ROAD SECTION……………………………………………………………………….21
2.2.1.1 STOP 1………………………………………………………………………………………………………………………21
2.2.1.2 STOP 2…………………………………………………………………………………………………………………….23
2.2.1.3 STOP 3…………………………………………………………………………………………………………………….25
2.2.1.4 STOP 4…………………………………………………………………………………………………………………….28
2.2.1.5 STOP 5……………………………………………………………………………………………………………………28
2.2.2. STATION 2………………………………………………………………………………………………………………30
2.2.2.1 STOP 1……………………………………………………………………………………………………………………30
2.2.2.2 STOP 2……………………………………………………………………………………………………………………33
2.2.2.3 STOP 3..………………………………………………………………………………………………………………….34
2.2.3. STATION 3 …………………………………………………………………………………………………………….34
2.2.4 STATION 4 …………………………………………………………………………………………………………….35
2.3. DAY 3. WESTERN SALT RANGE (NAMMAL GORGE) …………………………………………………37
2.3.1. STATION 1 ……………………………………………………………………..........................................37
2.3.1.1. STOP 1 ……………………………………………………………………………....................................37
2.3.1.2. STOP 2 ……………………………………………………………………………....................................38
2.3.1.3. STOP 3 ……………………………………………………………………………....................................40
2.3.1.4. STOP 4 ……………………………………………………………………………....................................40
2.3.1.5. STOP 5 …...………………………………………………………………………....................................43
2.3.1.6. STOP 6 ...................................................................................................................45
2.4. DAY 4. ……………………………………………………………………………………………………………………………….47
2.4.1. STATION 1 .……………………………………………………………………………………………………………47
2.4.2. STATION 2 ……………………………………………………………………………………………………………51
3. CHAPTER 3 CONCLUSION…………………………………………………….54
4. CHAPTER 4 REFERENCES…………………………………………….……..55

IV
List of figures:
1. FIGURE NO. 1. ……………………………………………………………….. 4
1.1. FIGURE NO. 1 ………………………………………………………………….8
1.2. FIGURE NO. 2 ………………………………………………………………….12
1.3. FIGURE NO. 3 ………………………………………………………………….13
1.4. FIGURE NO. 4 ………………………………………………………………….13
1.5. FIGURE NO. 5 …………………………………………………………….……14
1.6. FIGURE NO. 6 ………………………………………………………………….15
1.7. FIGURE NO. 7 ………………………………………………………………….16
1.8. FIGURE NO. 8 ………………………………………………………………….16
1.9. FIGURE NO. 9 ………………………………………………………………….17
1.10. FIGURE NO. 10 …………………………………………………………….18
1.11. FIGURE NO. 11 …………………………………………………………….19
1.12. FIGURE NO. 12 …………………………………………………………….20
2.1. FIGURE NO. 1 ………………………………………………………………….22
2.2. FIGURE NO. 2 ………………………………………………………………….23

1
3. CHAPTER 1 INTRODUCTION
3.1. INTRODUCTION TO SALT RANGE THRUST:
Salt range is one of the most important localities in the sub-continent in terms of its
stratigraphy, structure and interesting paleontological record. The Salt Range forms the
southern border of the hydrocarbon-bearing Potwar Basin in northern Pakistan, along the
north-western margin of the Indo-Pakistan plate.
Extensive anticlinal folds, synclines and various types of fault are present in the Salt Range.
It is the home of important minerals i.e. Halite, Gypsum, Coal, Fire clay etc. The
occurrence of these minerals is important from both Stratigraphic and Paleontological point
of view. Various type of fossils, their traces and tracks formed by bioturbations are also
well preserved. Salt range sequence of Pakistan has fascinated geologists from all over the
world due its well preserved formal assemblages.
The Indus Basin of Pakistan is mainly divided in two parts, Upper Indus basin and Lower
Indus Basin. The Upper Indus Basin is further divided into two parts by Sargodha Highs.
Towards the east of the Sargodha highs, Potwar Plateau is present while towards the west
is Kohat Plateau. The region of North Punjab is known as Potwar Plateau and it is bounded
by Salt range from South and in North by (Main Boundary Thrust) MBT.
The Salt Range is mainly divided into two parts, i.e. ‘Main Salt Range’ or ‘Cis-Indus Salt
Range’ which is to the East of Indus River, and ‘Trans-Indus Salt Range’, which is present
to the West of the Indus River. Further sub-divisions of ‘The Main Salt Range’ are:
• Eastern salt range: Jhelum to Kallar Kahar (32°30’-33°N & 71°45’-72E)
• Central salt range: Kallar Kahar to Jogi Tilla (72°45’-73°30’E & 32°30’-33°N)
• Western salt range: Jogi Tilla to Indus River (72°_72°45’E & 32°30°-33°N)
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 has, therefore, been rightly called a field museum of geology and paleontology.

2
3.2. LOCATION AND ACCESSIBILITY
Salt Range is located between latitude 32°-33° North and longitude 70°-72° East. Our area
of study was in the vicinity of Kallar Kahar extending from Eastern Salt Range to Central
Salt Range. It is located at a distance of about 190 km from Bahria University Islamabad
shown in figure 2. The area can be easily accessed from motorway (M-2) in 2 hours from
Islamabad, depending on the local conditions.

3
3.3. TECTONICS OF SALT RANGE:
Range is the continuous sequence of mountains which developed due to thrust faulting.
Salt range has been formed in the Cenozoic time, as a result of different tectonic forces that
have acted during the later phases of the Himalayan orogeny. SRT is the youngest thrust
fault. To the South, the connection between the Salt Range and the formations underlying
the alluvial plains is due to thrust faulting. Salt Range Thrust contains the older formations
of the salt range upon the less distressed Cenozoic sequence that underlies the alluvium.
Due to collision of Indian and Eurasian plate different ranges develop. The ranges that
developed on Indian plate are categorized in to three types of Himalayas:
 Higher Himalayas
 Lesser Himalayas
 Sub Himalayas
3.4. MAIN THRUST FAULTS
Thrust fault is the type of reverse fault, movement of hanging wall relative to footwall will
move upward of an angle less than 450, then it is called thrust fault. These are the thrust
faults due to collision of Indian and Eurasian plate.
 MKT (Main Karakoram Thrust)
 MMT (Main Mantle Thrust)
 MCT (Main Central Thrust)
 MBT (Main Boundary Thrust)
 SRT (Salt Range Thrust)
Ranges between MCT and MBT, they are called Lesser Himalayas, and towards north of
MCT we have Higher Himalayas and MBT to SRT ranges are called Sub Himalayas. All
Faults are dipping towards North.

4
Figure 1 Cross-sectional view of major faults

5
3.5. THE AIMS AND OBJECTIVES
The aims and objectives of the field trip were to:
 To identify the geology and stratigraphy of Salt Range.
 To identify the lithology of particular formations and rocks.
 Measurement of orientations of planes i.e. strike and dip.
 Observation of different geological structures (folds, faults and unconformities etc)
 Measure bearing of fractures utilizing Brunton compass.
3.6. EQUIPMENT
The equipment and instruments used in the field were:
 Geological hammer: It is used to collect samples.
 Hand lens: Used to observe size and shape of grains.
 Brunton compass: Used to measure Dip and Strike of different strata.
 Measuring tape: Used to measure the thickness of the beds.
3.7. METHODOLOGY
The methodology by which we studied the Stratigraphy was:
 Oriented our direction using Brunton Compass.
 Use GPS for identifying location co-ordinates.
 Observe the formation members, outcrop and the lithology.
 Observe physical characteristics of rocks such as grain size and shape by hand lens.
 Measure the dip-strike using Brunton Compass and the thickness of the beds with
the help of measuring tape.
 Collect samples.
 Take pictures of formations; confirm contact between the different lithologies,
geological structures and features present in them.

6
3.8. STRATIGRAPHY:
The generalized stratigraphy of the area is shown in the table below. It is of great important
and is necessary to know before carrying out the field. Formations which are present in
Salt Range are mentioned along with their general stratigraphy, environment of deposition,
ages and fossils content.

8
4. CHAPTER 2 FIELD OBSERVATIONS
4.1. DAY 1: EASTERN SALT RANGE (KAROLI ROAD SECTION)
On our first day, formations of Jhelum group were observed which are of Cambrian age.
These formations were Khewra Sandstone, Kussak Formation and Jutana Dolomite.
The Khewra formation consists predominantly of purple to brown and yellowish brown
fine grained sandstone.
Kussak formation is not pure sandstone and contains flaky minerals clay. The thickness of
Kussak Formation varies significantly at different places. The formation is widely
distributed throughout the salt range, with the best exposures in eastern part.
Jutana Formation is mainly consistent of yellowish white or cream colored partly sandy
dolomites. Dolomite thickness varies from thin to think and then to massive in the upper
part. Fractures, honeycomb weathering and butcher-chop weathering are recognizable
sedimentary structures.
4.1.1. Station 1:
Figure 2 Karoli road section (satellite image)

9
4.1.1.1. STOP 1:
At stop 1, we oriented ourselves using the Brunton compass, and then took photograph of
the exposed formations which were in southeast direction. A cross-sectional diagram of the
photograph was also drawn which can be seen in figure below.

11
4.1.1.2. STOP 2:
Here we stopped and took a sample and took dip and strike. We also saw crescent shaped
ripple marks. This was Khewra formation of Jhelum group and age is Cambrian.
Type of Sedimentary rock Clastic
Lithology Sandstone, some clay bands(shale)
Weathered color Reddish, grayish beds
Fresh color Grey
Grains Fine sand
Sorting Well sorted
Beds Medium to Thin
Structures/Features Crescent Shaped (asymmetrical) Ripple Marks
Age Cambrian
Environment of deposition Shallow marine
Dip 52°NW
Strike N27°E

12
Figure 3 Khewra Sandstone with clay bands
4.1.1.3. Stop 3:
Here we observed Khewra formation mostly composed of sandstone, having features like
ripple marks and cross bedding, which shows it had shallow environment of deposition.
Lithology Sandstone
Weathered color Light reddish
Fresh color Light Red to pink
Grains Fine
Sorting Well Sorted
Beds Medium
Structures/Features Highly weathered and fractured
Age Cambrian
Environment of deposition Shallow fluvial to Lagoonal environment

13
Dip 40°NW
Strike N2°E
Structures/features Crescent Shaped (asymmetrical) Ripple Marks, cross
bedding
Figure 4 Khewra formation
Figure 5 ripple marks

14
Figure 6 cross bedding
4.1.1.4. Stop 4(a):
After Khewra formation ends there is erosion and then Kussak formation starts. We
observed this stop at three points and noted interbeds of shale burrows tracks
(Bioturbations), change in thickness of beds, ripple marks, load casts. Kussak formation
is not pure sandstone; it contains flaky minerals of biotite mica (Arkosic Sandstone).
Lithology Sandstone and interbeds of shale
Color Grey
Grain Size Fine
Sorting Well Sorted
Beds Medium
Structures/Features Burrows tracks (bioturbations)
Age Cambrian
Dip 34°NW
Strike N20°W

15
Figure 7 Kussak formation shale and sandstone
Stop 4(b):
Material carried away by rivers gets stuck in mud and forms load cast.
Lithology Arkosic Sand
Color Grey
Grain Size Fine
Sorting Well Sorted
Bedding Massive bed at bottom
Structures/Features Burrows Tracks
Age Cambrian
Dip 65°NW
Strike N45°E

16
Figure 8 Kussak massive sandstone bed at bottom
Figure 9 Burrows Tracks (bioturbations)

17
Figure 10 Load cast
Stop 4(c):
Not a reservoir due to clay content and not a source rock due to bioturbations. Flaky
minerals present shows that it is Arkosic sandstone showing that origins or area from
which eroded material was coming, consisted of Feldspar. Burrowed sandstone in cross-
sectional view looks easily breakable but is strong and not easily hammered.
Lithology Sandstone with clay content (flaky minerals)
Grains Fine grained
Sorting Well sorted
Beds Massive
Structures/Features Burrows, Zigzag formation (Showing bioturbations)

18
Figure 11 Burrowed cross-sectional view of sandstone
4.1.1.5. Stop 5:
This formation is Jutana which is of Jhelum group of Cambrian age. Magnesium coating
on grains which shows little to no effervescence when acid directly put on sample. When
sample is crushed, Magnesium coating is removed and high effervescence shown.
Dolomite shows deepening of basin. It also had honeycomb weathering and Butcher-chop
weathering due to water movement.
Type of Sedimentary rock Non-Clastic
Lithology Dolomite and minor sandstone
Weathered color Dark Brown
Fresh color Light brown to pinkish
Grains N/A
Sorting N/A
Beddings Thick to massive

19
Structures/Features Butcher-Chop and Honeycomb Weathering, highly
fractured
Acid Test High effervescence when crushed.
Age Cambrian
Environment of deposition Deep Marine
Dip 11°NW
Strike N23°E
Hardness < 5
Figure 12 Jutana Dolomite

20
Figure 13 honeycomb weathering

21
4.2. DAY 2: EASTERN SALT RANGE
On 2nd day we visited 4 different stations. Our first station was along Pidh road section
where we observed Tobra, Dandot, Warcha formations of early Permian age and Sakesar
Limestone of Eocene age. We then went to 2nd station where we observed Baghanwala
formation, Tobra, Dandot and Warcha formations. On 3rd station we observed Khewra
sandstone and then at 4th station we received lecture about how Salt Range Thrust has
uplifted the area. We saw how suddenly area is uplifted right next to the Punjab plain.
4.2.1. STATION 1: PIDH ROAD SECTION
We stopped at the Pidh road section and were standing inside core of a dome. We were
facing south and uplifted parts on all four sides were dipping away from the valley, which
showed that it was dome, but then after faults developed, river flowed in and widen the
dome into valley.
4.2.1.1. STOP 1:
Our first stop is at Tobra formation of early Permian age of Nilawahan group. It mostly
consists of conglomerate in friable sand. Sand has low cementing material and easily
breakable by hand. It had massive beds containing conglomerate and breccia and some
beds did not have conglomerate or breccia. We could not take dip and strike at lower part
because no bedding plane was visible so we took dip and strike at upper part.
Lithology Sand (poorly cemented) in upper part, Sand (poorly
cemented) with rounded and angular pebbles in lower
part.
Weathered color Dark grey – Brownish
Fresh color Rusty Brown- light brown
Grains Fine Grained, has pebbles both angular and rounded
Sorting Upper well sorted, lower poorly sorted.
Beds Massive beds

22
Structures/Features Lower part has conglomerate and breccia with Pink
Granite fragments of Nagar Parkar.
Acid Test No effervescence
Age Early Permian
Environment of deposition Glacial (lower), Glacio-fluvial (upper)
Fossils None found
Dip 15°NE
Strike N30°W
Vertical variation Lower part has conglomerate and breccia but upper part
doesn’t have
Figure 14 Tobra formation, friable sand beds with and without pebbles

23
Figure 15 Conglomerate (rounded) and Breccia (angular)
4.2.1.2. STOP 2:
Here we observed Dandot formation, which mostly consists of compacted fine grained
sand with shale interbeds. It has features like phosphetic nodules and through cross
bedding.
Lithology Sand with shale interbeds
Weathered color Rusty brown (sand), light grayish (shale)
Fresh color Light rusty brown (sand), light grey
Grains Fine grain sand
Sorting Well sorted
Beds Thin beds
Structures/Features Through cross bedding, phosphetic nodules
Age Early Permian

24
Fossils None
Dip 15°NE
Strike N30°W
Figure 16 Dandot formation (sandstone and shale), phospheticnodule

25
Figure 17 through cross bedding
4.2.1.3. STOP 3:
Here we observed Warcha sandstone of Nilawahan group. Lower part consisted of friable
sand and was fractured, it also had calcite veins. But as we moved more shallow
environment and sand became less friable. Upper part also had cross bedding.
Lithology Sandstone
Weathered color Rusty brown
Fresh color Reddish white
Grains Coarse grain sand
Sorting Well sorted
Beds Massive (lower), Thin (upper)
Structures/Features Heavily fractured, calcite veins, friable, cross bedding
(upper part)

26
Age Early Permian
Environment of deposition Deltaic environment
Fossils None found
Vertical variation Friability less as we move up, beds become thin, cross
bedding in upper part
Figure 18 Friable sand (Warcha)

27
Figure 19 Calcite vein
Figure 20 Cross bedding in upper Warcha

28
4.2.1.4. STOP 4:
At stop 4 we saw thrust fault, due to that fault there was displacement of about one and a
half feet i.e. Dandot moved up. The picture below shows the fault displacement.
Figure 21 Reverse fault
4.2.1.5. STOP 5:
Here we observed Sakesar limestone of Chhart Group of Eocene age. Here we also saw
two types of fossils Asilina (eye shaped) and Neumilites (rounded shape), which are
index fossils of Eocene age which helps us to determine the age of the formation. Other
features include chert nodules () and castification (due to rain water forms weakly acid
dissolving limestone).
Type of Sedimentary rock Non Clastic (crystalline)
Lithology Limestone
Weathered color Light grayish
Fresh color White grayish
Grains None

29
Structures/Features Chert nodules (cryptocrystalline silica, shows no
effervescence), Castification, vertical fractures (highly)
Acid Test High effervescence
Age Eocene
Environment of deposition Shallow to deep (on continental shelf)
Fossils Asilina (eye shaped) and Neumilites (rounded shape)
Hardness 3 (calcite)
Figure 22 Neumilities (rounded)
Figure 23 Asilina (eye shaped)

30
Figure 24 SakesarLimestone showing Castification
4.2.2. STATION 2:
Here we stopped along a road section and observed formations from Baghanwala, Tobra,
Dandot and Warcha. Here Tobra formation was different from the Pidh road section but
the Dandot and Warcha were same.
4.2.2.1. STOP 1:
Here we saw Baghanwala formation which mainly consists of red color shale with some
sandstone interbeds. It contains a special diagnostic feature called Salt Pseudomorph.
After Baghanwala there was abrupt change in lithology and Tobra formation started. This
abrupt contact is an unconformity due to missing of deposition from Ordovician to
Carboniferous, this unconformity is called disconformities. Baghanwala formation was

31
eroded and at some points Tobra was entering the Baghanwala which shows time gap and
erosion.
Lithology Shale with some fine grained sandstone interbeds
Weathered color Reddish brown
Fresh color Reddish maroon
Sorting Well sorted
Beds Thin to medium
Structures/Features Salt Pseudomorph, Ripple marks, some greenish grey
color clay laminas, abrupt contact showing
Disconformities, Tobra entering Baghanwala which
shows time gap and erosion
Age Middle Cambrian
Environment of deposition Estuaries
Fossils None
Dip 19°NE
Strike N74°W
Figure 25 Tobra entering Baghanwala

32
Figure 26 Baghanwala and Tobra Contact
Figure 27 Salt Pseudomorph

33
Figure 28 Ripple Marks
4.2.2.2. STOP 2:
After Baghanwala and disconformity Tobra formation stared. The difference between this
Tobra and Pidh road Tobra was of size of boulder size conglomerate and sand was in
very less amount. It shows pure glacial deposits as boulders are well rounded and had
polished surface. It also had pink color granite of Nagar Parkar. The rest of the
observations are same as Pidh road section Tobra which have been mentioned before.
Figure 29 Tobra (large boulder and NagarParkar Pink Granite)

34
4.2.2.3. STOP 3:
After Tobra again Dandot and Warcha were present which were same as observed in Pidh
Road section. We found very excellent through cross bedding in Dandot formation. All
Permian age rocks ended at the road bend and Sakesar Limestone was present. It was
faulted contact of Sakesar limestone with Permian age rocks.
Figure 30 through cross bedding in Dandot
4.2.3. STATION 3:
Here we saw Khewra sandstone of Cambrian explosion. Although we did not see any
trilobites tracks but Doctor G. has reported trilobite’s tracks in Khewra sandstone.
Opposite to the Khewra sandstone behind us was salt range marl which had reddish color
and it was soft material.
AGE Cambrian
TYPE Clastic
LITHOLOGY / COMPOSITION Sandstone
WEATHERED COLOUR Dark reddish
FRESH COLOUR Reddish maroon and some grey
EFFERVESCENCE Negative

35
ENVIRONMENT OF DEPOSITION Shallow fluvial to Lagoonal
environment
GRAIN SIZE Coarse sand
GRAIN SHAPE Rounded
SORTING Well Sorted
BEDDING Thick to massive bedded
OTHER FEATURES Ripple marks, Intra-formational Faults,
Cross bedding, compacted, Trilobites
tracks are reported
Figure 31 Khewra Sandstone
4.2.4. STATION 4:
This was our last station and here we were given lecture upon general tectonics and
uplifting caused by the Salt range thrust. Tectonics has been discussed earlier in the
introduction part of the report.

36
Figure 32 Cross section of Thrusts in Pakistan

37
4.3. DAY 3: WESTERN SALT RANGE (NAMMAL GORGE)
On third we went to Nammal Gorge, part of Western Salt Range, which is present in
Mianwali city. Nammal Gorge contains formations from late Permian (Wargal) up to
Miocene age, some are missing but mostly are observable. Although we only observed
formation of late Permian to late Triassic, which are Wargal, Chiddru, Mianwali, Tredian
and Kingriali. Here we saw mostly limestone and some shale, sandstone and dolomite. We
also saw a lot of fossils and found traces of fossils too. This area was highly weathered and
difficult to walk and climb. We walked along the stream in valley and observed lithologies
and their contacts. Limestone was being excavated by machines for making cement.
Geographical coordinates of Nammal Gorge are Latitude 32°39'35"N and longitude
71°47'40"E.
4.3.1. Station 1:
4.3.1.1. Stop 1:
At first stop we observed normal faults caused by salt tectonics (halokinesis) because salt
under pressure does not fracture or bend rather it starts to flow and forms domes due to
which strata above it undergoes local extension causing local normal faults. The picture
below shows the faults and direction is in the South. The diagram of the faults is also shown
here.
Figure 33 Normal faults caused by halokenesis

38
4.3.1.2. STOP 2:
At stop 2 we observed Wargal limestone. Limestone was widely spread and had fossils in
lower part. Upper part was more light color and less hard. As we moved across the dip we
found a very good exposed surface where we took dip and strike.
Observations:
Type of Sedimentary
rock
Non-clastic
Lithology Limestone
Weathered color Light brown to yellowish and grey
Fresh color Greyish white
Grains no grains observed
Effervescence Yes highly
Beds medium to thick
Features Highly Fossiliferous
Structure Highly fractured, large fractures
Fossils Brachiopods (Productus)
Age Late Permian
Environment of
deposition
Shallow marine
Dip 80 NW
Strike N 29 E
Vertical variation Hardness decrease upwards, Grey color beds have fossils
only, bed thickness increases upwards, lighter color upwards

39
Figure 34 Wargal Limestone
Figure 35 Brachiopods (Productus)

40
4.3.1.3. Stop 3:
Here we observed the end of the Wargal limestone, marked by the shale bed and after the
Chiddru formation starts. The limestone near the end was lighter and did not have any dark
beds like in the start.
Type of Sedimentary
rock
Non Clastic
Lithology Limestone
Weathered color Rusty yellow
Fresh color Whitish gray
Effervescence Positive
Beds Massive
Features Fractured, end marked by shale
Age Late Permian
Environment of
deposition
Shallow marine
Figure 36 Ending of Wargal Limestone
4.3.1.4. STOP 4:

41
Next formation to the Wargal limestone is Chiddru formation. Chiddru formation consists
of sandy limestone, shale and friable sand. Friable sand was at the top of the Chiddru
formation. Occurrence of sand shows that sea level was retreating towards basin. After
friable white sandstone there was paraconformity due to Permian mass extinction. After
that Mianwali formation started.
Type of Sedimentary
rock
Non-Clastic and Clastic
Lithology Sandy Limestone, friable sand and shale
Weathered color Grayish and white
Fresh color Grayish and white
Grains Coarse grains sand
Effervescence Showed effervescence
Beds medium to thick
Features Concoidal fracture, phosphetic nodules in shale
Age Late Permian
Environment of
deposition
Deltaic to Shallow marine
Vertical variation Lower part has limestone and shale then comes sandy sandy
limestone and then friable white sandstone

42
Figure 37 Interbeds of Limestone and Shale

43
Figure 38 White friable Sandstone
4.3.1.5. STOP 5:
From here we observed Mianwali formation which had three members. The lowest member
is Kithwai, then Mittiwali and at top Narmia. Mianwali formation is of early Triassic age
and has dolomite, limestone, sandstone and shale lithologies. Abundant fossil found in
Mianwali was Ammonites which was present in Mittiwali limestone.
Kithwai:
Kithwai member starts right after Chiddru formation, after the white friable sandstone of
Chiddru formation ends, the Kithwai member dolomite overlays it. Kithwai member
mostly consists of dolomite and it has some limestone beds in it.
Mittiwali:
After the Kithwai member is Mittiwali member, lower part consists of limestone which has
Ammonites fossils present in abundance; the upper part has sandstone and shale. The
limestone was not that visible and mostly covered with weathered rubble and was very to
climb. It had greenish grayish beds of sand and shale.
Narmia:

44
This is the last member of Mianwali formation. Lower part consists of sandstone and shale
and upper most part is red color dolomite which also marks the end of Mianwali formation.
Figure 39 Upper part of Mittiwali
Figure 40 Ammonites Traces

45
Figure 41 End of Mianwali, lower dolomite and sandstone are of Doya Member of Kingriali
formation, the upper dolomite is of Wanjari member also called Kingriali Dolomite
4.3.1.6. STOP 6:
This was our last stop and here we observed the upper member of the Kingriali formation
called Wanjari member.
Type of Sedimentary
rock
Non-clastic
Lithology Dolomite
Weathered color Light brown to yellowish
Fresh color Light brown
Grains no grains observed
Effervescence Only when crushed
Beds Massive
Features Honeycomb weathering
Age Late Triassic

46
Environment of
deposition
Shallow marine
Figure 42 Honeycomb weathering

47
4.4. DAY 4:
4.4.1. STATION 1:
Here we draw road section walking from north to south covering both side of the road and
matched the lithologies present at both sides of road. Formations present here were
Chorgali of Eocene age and Murree formation of Rawalpindi group of Miocene.
CHORGALI FORMATION:
Chorgali formation had highly fractured limestone with thin beds of shale.
AGE Eocene
LITHOLGY Limestone + Shale
WEATHERED COLOUR yellowish white (limestone), light grayish (shale)
FRESH COLOUR Limestone had whitish grey color
Shale had brownish grey color
EFFERVESCENCE Positive
ENVIRONMENT OF DEPOSITION Shallow marine
BEDDING Medium to thick beds of limestone, thin beds of
shale
FEATURES Fractures in limestone, anticline and syncline
structure,faults, presence of Marl
FOSSILS Neumilites and Asilina are present in limestone
but small

48
Figure 43 Chorgali formation
MURREE FORMATION:
After the Chorgali formation there is unconformity and then Murree formation starts. There
is no deposition of Oligocene age and after uplifted of Himalayas, Rawalpindi group and
Siwaliks group started to deposits.
AGE Miocene
LITHOLOGY Sandstone
WEATHERED COLOUR Brownish Reddish
FRESH COLOUR Brownish Grey
EFFERVESCENCE Negative
ENVIRONMENT OF DEPOSITION Fluvial
GRAIN SIZE Coarse Grained
SORTING Medium to poor sorting
GRAIN SHAPE Angular

49
BEDDING Massive beds of sandstone
Figure 44 Faulted contact between Chorgali and Murree
The road section drawn is shows the 2D map view of the area. Different lithologies and
structures like anticline, syncline and faults are shown. If dips are towards each other it
shows syncline and if dips are opposite then it shows anticline structure. Stations are
pointed according to change in lithology of structure across the road. The actual distance
on the ground is converted into centimeters and scale is shown in map.

51
4.4.2. STATION 2:
Here we observed Rawalpindi group of Miocene age, consisting of two members Kamlial
and Murree. We found reworked fossils of Belemnites. Murree and Kamlial formations
had transitional contact between them. At their contact there were conglomerate present
which showed high energy of river. Both members are fluvial deposits.
MURREE FORMATION:
This formation consists of Red clay and Shale, siltstone and coarse grain sandstone. These
are fluvial deposits so there was no visible bedding plane. Coarse grain sandstone was
showing effervescence because cementing material is calcite. The red color clay shows
highly oxidizing environment. Clay due to water has flowed due to which there is
deformation.
Figure 45 Abrupt contact between Murree (red) and Kamlial (gray)
KAMLIAL FORMATION:
Kamlial formation consists of dark grey color friable sandstone, well sorted, medium to
thick beds and loose material. It was highly fractured and had intraformational faults
caused by unloading of upper material; we will consider them fractures as faults are on
large scale.

52
Figure 46 Intraformational faults in Kamlial formation

54
5. CHAPTER 3 CONCLUSION
Our four-day field trip was one of the most informative trips we have been to. Observing
many different types of lithologies and identifying them on the basis of their features and
environments of deposition was an interesting task. Learning to use different equipment
like Brunton compass and hand lens was something we learned during our field.
The geophysical survey conducted was a new and informative learning experience.
Overall, we have learnt quite a lot from our field trip and got great knowledge about the
geology of salt range.
Salt range is the result of tectonic collision. The salt range is composed of rocks of different
ages starting from the precambrian to the recent one it has many structure features present.
The salt range has wide variety of different rocks indicating the geology of all types of
rocks. It is in fact museum of geology with large amount of exposures.

55
6. CHAPTER 4 REFERENCES
Shahid Jamil Sameeni , The Salt Range: Pakistan's unique field museum of geology
and paleontology
Shahid Ghazi, Syed Haroon Ali, Mohammad Sahraeyan & Tanzila Hanif, An overview
of tectonosedimentary framework of the Salt Range, northwestern Himalayan fold and
thrust belt, Pakistan
Mohammad Attaullah Khan and Mohammad Javed Khan, Stratigraphy Of The
Baghanwala Formation, Khewra Gorge, Khewra, Jhelum District; Punjab
https://www.scribd.com/doc/61469018/Field-Report-of-Salt-Range

Salt range field report

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