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GEOLOGY FIELD REPORT
Presented for
Dr. Muhib ur Rehman
Comsats Islamabad Abbottabad University
By
Abubakkar Saddique
Student of Geology, Reg No FA20-GEO-006
Comsats Islamabad Abbottabad University
January 30, 2023

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INTRODUCTION ..............................................Error! Bookmark not defined.
Hazara slates .......................................................Error! Bookmark not defined.
Mansehra granite ................................................Error! Bookmark not defined.
Gneiss in batagram................................................................................................5
Besham site ...........................................................................................................6
Dubair....................................................................................................................7
Jijal complex .........................................................................................................8
Near pattan kohistan............................................................................................10
Gilgit to chillas....................................................................................................12
Raikot..................................................................................................................13
Thilichi................................................................................................................14
Junction point......................................................................................................16
Collision point.....................................................................................................19
Karakoram belt....................................................................................................20
Attabad landslide.................................................................................................24
Gukmit landslide.................................................................................................25
leecher landslide..................................................................................................26
Hotspring.............................................................................................................27
References...........................................................................................................29

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Introduction
Field geology means Field work, geology as practiced by direct observation of outcrops,
exposures, and landscapes. Those who practice geology in the field examine rocks and rock
materials in their natural environment. Field geologists, therefore, attempt to describe and explain
the surface features, subterranean structures, and their interrelationships. However, it emphasizes
that although field geology is based on observation, many conclusions are predicated on
inferences. He states that “the ability to infer and infer correctly is the goal of training in field
geology”. A geologist is largely measured by one's ability to draw reasonable conclusions from
the observed phenomena and to predict the occurrence of the features, conditions, or processes
using field experience.
Figure Digital-Geologic-Map-of-northern-Pakistan-showing-the-Upper-Indus-River-watershed (ahmad, 1993)

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Abbottabad Area
At the first stop, we observed Hazara slates and Tanawal quartzite. Hazara slates are divided into
two sections.
Hazara slates
Hazara formation is the metamorphosed rock of shale which formed Hazara slates lithology
consists of slates, phyllite sandstones, and quartzite with a horizon of gypsum and two limestone
beds. Hazara slates have will cleavage Hazara slate is tilted by tectonic activity on Tanakki
boulders. Hazara formation is in the middle of two formations Hazara formation overlies the super
positionally of the Abbottabad formation and is overlain by Jurassic Tanakki boulders. The
Tanakki boulders are the eroded form of the Hazara formation which makes Tanakki
boulders/conglomerates in between the Hazara slates and Tanakki boulders there is an angular
unconformity. The age of the Hazara formation is Precambrian.
Abbottabad Formation
Abbottabad’s formation is lithological and consists mainly of dolomite with sandstones, shale in
the lower part, boulder beds at the base, and many lithological changes inter-fingeringring facies
from place to place. The Abbottabad formation contains also contains Marble beds. The
Abbottabad formation has an unconformable contact with the Tanawal formation but in the eastern
part of southern Hazara the Tanawal formation is missing and the Abbottabad formation is
unconformable with the Hazara formation. Oolites are found in the Abbottabad formation. The age
of Abbottabad formation is Cambrian.
Mansehra Granite
Igneous rock double Mica black is biotite and white is muscovite, Acidic rock with high silica
content, we also call it Mansehra batholiths, and xenolith is also documented. The rocks observed
at this stop were granite. There is also some amount of mafic minerals in it. This is part of the
Mansehra batholith. Schistocity and gniesstocity are also present due to shearing. The age of these
rocks is 516my (Cambrian). Swat granite and Ahal granite form at the same time. A dyke was
intruding into the Manshera Granite. These are dolerite dykes and dolerite is composed of
plagioclase, pyroxene, and biotite along with other accessory minerals. Spheroidal weathering,
Phenocryst of feldspar pure white grain feldspar the economic perspective we see tourmaline, and
rare earth Elements.

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Gneiss in Batagram
Gneiss is a metamorphic rock that has a distinct banding, which is apparent in hand specimens or
on a microscopic scale. Gneiss usually is distinguished from schist by its foliation and schistosity;
gneiss displays a well-developed foliation and a poorly developed schistosity and cleavage. Most
of the mineral grains of gneissose rocks are visible to the naked eye. Banding in this rock is a result
of mineral segregation into separate, typically light- and dark-colored layers; light-colored layers
are usually composed of feldspars and quartz and dark-colored layers are usually composed of
hornblende and biotite. Individual bands are usually 1-10 mm in thickness. Layers larger than that
imply that partial melting or the introduction of new material has probably taken place. Such rocks
are called migmatite. In some areas, gneiss grades laterally into granitic rocks. This feature is one
of the important factors that have led some to call upon a metamorphic process (granitization) for
the development of granitic plutons.
The rocks observed at this stop were gneiss have Augen structures. These are part of Mansehra
granite that metamorphosed means the protolith of this gneiss was granite or granodiorite. When
pressure is exerted on mega crystals of Mansehra granite Augen structures are formed.
Gniesstocity is more and Tanawal quartzite is intruded by this granite.
Figure 2 Augen (from German "eyes") are large, lenticular eye-shaped mineral grains or mineral aggregates visible in some
foliated metamorphic rocks.

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Besham route
The rocks which were observed on the field are below
 Garnet-mica schist
 Igneous rocks
 Gneiss(Para) Quartzite
 Graphite schist
Besham site
At this stop, we observed Schist, Granodiorite, Quartzite, Gneiss, Amphibolite, and Chromite. This
section is part of the Besham Complex. The granodiorite observed here is also called Shange
Granodiorite whose age is 1836my. Amphibolite is also observed. Gniesstocity is present in the
rocks. Schistocity is also present but not too much. The mafic intrusion was also present below the
iron bridge.
Besham city
The rocks observed at this stop were Meta sedimentary rocks that contain Feldspar, Quartz, and
Biotite. Quartz vein was also present in the rocks. Some researchers named it paragneiss and some
researchers named it Kishar formation. This section`s rocks are also part of the Besham complex.
The age of the rocks is Precambrian.
Figure 3 metasedimentary rock is a type of metamorphic rock. Such a rock was first formed through the deposition and solidification
of sediment. Then, the rock was buried underneath the subsequent rock and was subjected to high pressures and temperatures,
causing the rock to recrystallize.

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Dubair
This granodiorite (biotite – hornblende) belongs to the Precambrian “Besham Group”. This Meta
diorite is deformed heterogeneously and displays unfoliated facies with angular xenoliths. The
foliation intensity varies from almost none to pronounce into mylonitic bands. Granites are coarse-
grained intrusive igneous rocks made of two different kinds of feldspar (potassium- and sodium-
rich), together with quartz and a small proportion of dark minerals. Granodiorite is very similar to
granite. It has less of the potassium variety of feldspar, and more of the sodium feldspar
(plagioclase). The dark minerals in this rock include green hornblende and brown mica (biotite).
This Granodiorite is equal to Shange granodiorite.
Jijal complex
At this stop, we observed dunite which mostly consists of Olivne. Olivine has a green color that
shows some transparency. Dunite contains more than 90 percent olivine. Peridotite was also
observed at this stop which consists of dark color minerals like pyroxene, and amphibole. This
section is part of the Kohistan island arc. MMT (Main mantle thrust) lies at the back side of this
section. Mostly MMT is marked by Blueschist but In the Kohistan Island arc.
Figure 4 Dunite also known as olivine is an intrusive igneous rock of ultramafic composition with phaneritic (coarse-grained)

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Near Pattan koshitan
At this stop we observed garnet granulite; the texture of the rock is granular. The age of the rocks
is cretaceous. This section is part of the Jijal complex. Granulite is a fine- to medium-grained
metamorphic rock with a granular texture of polygonal crystals (granoblastic texture). Granulites
typically contain amphibole, quartz, feldspar, and pyroxene with very little or no mica. Granulites
frequently contain garnet, kyanite, sillimanite, and/or sapphirine. Granulites form by regional
metamorphism of a wide range of protoliths including argillaceous and arenaceous sediments,
mixed siliciclastic and carbonate sediments, and igneous rocks.
Figure 5 Granulites are a class of high-grade metamorphic rocks of the granulite facies that have experienced high-temperature
and moderate-pressure metamorphism.

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Pattan Kohistan
At this stop we observe Gabbro. But we also observe gniesstocity which may be mafic gneiss that may be
formed by forceful injection of the magma that elongates the minerals. In this section, magnetization may
occur. The grain size of the rock is fine. The rocks observed at this stop are a part of the Kohistan Island
Arc.
Figure 6 Gabbro is a mafic intrusive coarse-grained rock with allotriomorphic texture.

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Amphibolite is a metamorphic rock whereas gabbro is an igneous rock. The grain size is fine.
Intrusion produces shearing and bending. The rocks of this section are included in the Kamila
amphibolite formulation was present in the rocks. The color of the rock was dark.
Figure 7 Amphibolite is a rock of convergent plate boundaries where heat and pressure cause regional metamorphism.
Gigit to chillas
The first rock that was observed at this stop is gabbro. The gabbro is mafic rock and has some
amount of olivine and plagioclase. The greenish color represented that that rock was gabbro. In
gabbro the amount of blackish minerals is high. The amount of plagioclase is also high in it. These
rocks are not gabbro may be they were tonality rocks. In gabbro the pyroxene amount is high.
Gabbro is a coarse-grained and usually dark-colored igneous rock. Gabbro is an intrusive rock. It
means that it formed as magma cooled slowly in the crust.
The second rock that was observed was the Dunites rocks. This rock has a vitreous luster. In this
rock, pyroxene is much less. If Dunites has 90% of pyroxene this may be peridotites.
Some veins of pegmatite intruded into it. Peridotite is a generic name used for coarse-grained,
dark-colored, ultramafic igneous rocks. Peridotites usually contain olivine as their primary
mineral, frequently with other mafic minerals such as pyroxenes and amphiboles. Their silica
content is low compared to other igneous rocks, and they contain very little quartz and feldspar.
There was also a peridotitic rock which has pyroxene minerals. In this rock there are black, shining,
vitreous, elongated minerals called hornblendites also present.
The rock which has hornblende is called hornblendities. These all rock parts of the Kohistan
batholith. Unites and peridotites are light greenish grey to dark grey with a greasy appearance.
These rocks are partially serpentinized. This phenomenon is more prominent in the rocks along
southern contact. Shearing of the rocks has taken place and serpentinization is intense along joints,

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weak and sheared zones. Serpentinites are light grey and brown to dark grey in color. Dark grey
and thin veins of serpentinite are also seen in these rocks. Chrornitite has been found with these
rocks on the basal side as massive lenses and layered bodies. Magnetite dissemination is common
in peridotites and dunites and is up to a maximum of 20% in the rocks so far observed. These rocks
are magnetic in character.
Figure 8 biotite in quartz
Raikot
We observed Diorites of medium grain size. These rocks are also part of Kohistan batholiths.
Pegmatite veins were also present in the rocks. On the way, many springs were observed that
represent Raikot Fault. Raikot fault is a strike-slip fault. Many Pleistocene deposits were observed.
On the right side of the road, the Himalayas were present and MMT pass through this zone.

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Thilichi
These are fined-grained sedimentary rocks that undergo metamorphism. In this the amounts of
mica or clay minerals are high. All these sediments are a part of the Jaglot Group. In this, there
were different Meta sediments, phyllites, and schist. In these sediments, the turbid tic sequences
developed. Many volcanic rocks were also observed that were metamorphosed. Tuffaceous
materials and pyroclastic materials were also observed that were metamorphosed. Pegmatite’s
veins were also observed at this stop. These rocks are called Gashu volcanic rocks.

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Figure 9 fined-grained sedimentary rocks that undergo metamorphism

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Junction point
The fined-grained granitic rock is sometimes also known as Athelites. It is also intruded by the Kohistan
batholith part, so different types of veins and dikes are formed. The rocks were veins or dikes. This is a
massive body of rock.
It is very important to point geographically because two rivers, Gilgit, and river Indus meet because of the
river three different types of ranges are observed.
Figure 10 the junction of the three mightiest mountain ranges, the Himalayas, Karakorum, and Hindukush.

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Gilgit
The rocks observed were granite, composed of biotite, quartz, and feldspar. The grain size was
fine to medium. This section is also part of the Kohistan batholith.
Normal
At this stop, we observed mafic rocks that may be basaltic. The grain size was fine and foliation
was present in the rocks. Green color patches were also observed that may be chlorine that forms
by metamorphism. Gniesstocity was also present in the rocks. Pillow structures were also observed
that formed when extrusion occur in the ocean. It is also called the Chalt volcano. color of the
basalt was darkish grey to black.
Collision point
This is a point where Indian plates collide with Eurasian Plates. As a result of the collision the Himalayan
devolved. Hunza quartzite. Hunza quartzite is a part of Korakarram block. A tight fold was observed at this
point. Some people mark MKT in this zone.
Figure 11 Indian and Eurasian collision point

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Figure 12 according to some geologist especially Peshawar University recognize that this is the point where content collide a little
away from the main documented point
Karakoram belt
Karakorum plates represent the northernmost of Pakistan and it is located on the northern side of
NSZ or MKT. The rock body exposed here are highly deformed sedimentary, Meta sedimentary,
and igneous assemblages and they are ranges in age from Jurassic to late Cretaceous and formed
as a result of a collision between KIA with Eurasian plate along NSZ or MKT.
The Karakorum plate is divided into;
 Northern Sedimentary Belt
 Karakorum Axial Batholith
 Southern Metamorphic Belt

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Northern Sedimentary Belt
The northern sedimentary belt is the northernmost unit of the Karakorum block and is mainly
consisting of up to a 7km thick belt which is transgressive on a pre-Ordovician crystalline
basement rock. The sedimentary belt is further divided into thrust sheets in Chitral and Hunza
Valley along the western and eastern margins of the Karakorum block. The rock body present in
this block ranges in age from Permian to Paleozoic and most of the succession with the eastern
Karakorum along Hunza valley are of Permian age. The Hunza includes calc-alkaline granodiorite
which has both biotite and hornblende minerals.
Karakorum Axial Batholith
It is a large body of igneous rocks that intrudes at different times and the earliest magmatic episode
is recorded earlier than 100 Ma and can be correlated with the initial stages of intra-oceanic
subduction. The extension of this batholith is up to Ladakh in the east and across into Afghanistan
in the west. The northern sedimentary belt in the northern Karakorum plates is separated from the
marginal mass present in the southern part of the Karakorum plate by this axial batholith in the
Hindukush and Karakorum ranges. The dominant rock phases of this batholith are granodiorites,
granites, and pegmatite which are readily intruded by the sills and dykes mostly basic in nature.
At least three major tectonic episodes of magmatic intrusion were identified in the magma axial
batholith. The earliest episode was in the mid –Cretaceous and mainly consisted of sub-alkaline
and calc-alkaline intrusion. The second phase of intrusion consists of sub-alkaline granites of
Eocene age having mainly biotite, amphiboles, and andalusite. The last episode occurred in
Miocene and is represented by leucogranite sheets and the intrusion of batholithic dimensions.
A linear batholithic body, about 20 km wide and 150 km long, occupies higher peaks of the Eastern
Karakoram and Pangong Mountain in Ladakh. This batholith extends into the western Karakoram
across the Baura range. Hispar, Biafo to the west of Baltoro and is known as Karakoram axial
batholith. In general, the Karakoram batholith is porphyritic in texture and pink in color but in
western Karakoram homogeneous and fine-grained with occasional coarse-grained varieties also
reported. The belt occurs as an elongated arcuate composite body comprising different sub-alkaline
and calc-alkaline units.

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Southern Metamorphic Belt
The southern metamorphic belt of the Karakorum plates is developed as a hanging wall along the
NSZ or MKT. the different groups included in this belt are variously named as we move from the
western to the eastern margins (i.e. Chitral slate in the Hindu Kush, Darkot group in the Yasin
valley, Baltit group, and Damurdu Formation in the Hunza valley, and Shigar group in the Baltistan
group). The low-grade metamorphic rock in this belt is the biotite schist, chlorites schist, and quartz
schist, while the high-grade metamorphism is demarcated by kyanites and illuminates schists.
Northern Suture Zones or Main Karakorum Thrust (MKT)
Main Karakorum Thrust is a fault contact that separates the rocks of Eurasian plates from that of
KIA. This suture zona is formed as a result of the collision of KIA with Eurasian plates. NSZ is a
compromise of ophiolites mélange containing rocks like’s serpentines, volcanic, and marine.
Sediments in a slate. The different types of sedimentary volcanic present on the northern sides of
KIA are separated from the slates and quartzite of the Eurasian plates by this mélange. The rock
body present along this thick mélange is limestone, quartz, volcanic greenstones, and altered rocks
like serpentine in a slate matrix.
Kohistan Island Arc
A Kohistan island arc is formed as a result of intra-oceanic subduction of neo-Tethys beneath the
Eurasian plate in late Jurassic to Early Cretaceous times and covering an area of about 3600 km2.
KIA is separated from the Indian plates by MMT or ISZ in the south while its northern boundary
is marked by MKT or NSZ which separates it from the Eurasian volcanic rocks. KIA consists of
associated volcanic rocks. KIA consists of the following geological bodies of rocks as we move
from north to south.
Attabad Landslide
On January 4, 2010, in the remote Hunza Valley of Northern Pakistan, a massive landslide buried
the village of Attabad, destroyed 26 houses, and killed 20 people. The landslide dammed the Hunza
River and formed an extensive lake of 100m in depth. Until the end of July 2010, 381 houses were
ruined; out of which 141 were directly affected by the Attabad landslide, and others were
submerged due to the expansion of the lake. By the end of May 2010, local authorities excavated
a spillway to guide the flow of impounding lake over the natural dam. Until August 2010, the
spillway is performing well but the internal response of the loosely deposited debris is unknown.
(al, january 2010)

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Figure 13 attabad landslide (Ahmed, 2013)

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Gulmit landslide
Figure 14 it’s an unstable zone and this has the potential to block the river.

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Leecher landslide
This is a historical landslide it occurs in 1984 and block the river when the river burst hundreds of
British soldiers were killed in the Attock area. It was documented and observed by a tourist.
Figure 15 leecher landslide

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Hotspring
Hotspring indicates that there is an active fault because of which the groundwater is heated

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Shangla top
Two different kinds of rock were observed in the shingle area greenschist and blueschist.
Greenschist facies
The greenschist facies is at medium pressure and temperature. The facies is named for the typical
schistose texture of the rocks and the green color of the minerals chlorite, epidote, and actinolite.
Figure 16 dendritic texture within Greenschist

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Blueschist facies
The blueschist is relatively low temperature but high pressure, such as occurs in rocks in a
subduction zone. The blue minerals glaucophane and lawsonite.
Figure 17 blueschist rock

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ACKNOWLEDGMENT
We would like to acknowledge the University of Comsats University Islamabad Abbottabad
campus, Pakistan which arranged the field trip for geology 5th
-semester students. We would also
acknowledge the HOD of the institute of geology for providing transport facilities during
geological fieldwork.