Content uploaded by Polla Khanaqa
Author content
All content in this area was uploaded by Polla Khanaqa on Jan 02, 2019
Content may be subject to copyright.
Iraqi National Journal of Earth Sciences Vol. 18, No. 2, pp. 69 -98. 2018
69
Stratigraphy and Facies Analysis of the Govanda Formation from
Western Zagros, Kurdistan Region, Northeastern Iraq
Kamal H. Karim
Department of Geology
College of Science
University of Sulaimani
Irfan M. Yara
Department of Geology
College of Science
University of Sulaimani
Soran O. Kharajiany
Department of Geology
College of Science
University of Sulaimani
Polla A. Khanaqa
Kurdistan Institution
for Strategic Studies
and Scientific Research
Iraq
Khalid M. Sharbazheri
Kurdistan Institution for
Strategic Studies and
Scientific Research
Iraq
Mushir M. Baziany
Department of Geology
College of Science
University of Sulaimani
Yousif O. Mohammad
Department of Geology
College of Science
University of Sulaimani
Sherzad T. Mohammed
Department of Geology
College of Science
University of Sulaimani
(Received 18/2/2018 , Accepted 3/10/2018)
ABSTRACT
A part of the Govanda Formation is studied in five outcrops from northeastern
Iraq near the Iraqi-Iranian borders. It consists of polygenic conglomerates, detrital
limestones (conglomeratic limestone), and highly fossiliferous limestones of reef-
fore-reef facies with occasional interbedding of terrigenous sediments. Tectonically,
the formation is important for its location in the very active Sanandij-Sirjan (Suture)
Zone and for its deposition in Middle Miocene, which was assigned previously as an
age of continental-continental colliding of Zagros Fold-Thrust belt. Additionally, it is
overlaying different rocks units of pre-Miocene, especially resting on the Qulqula
Radiolarian Formation in an angular unconformity relationship. The high-energy and
tectonically active shallow and normal- marine environment is inferred from many
facies such as coral framestone, pelecypod floatstone facies, coral and lithoclast
rudstone, coral bufflestone, stromatolite bindstone, foraminifera and red algal
bioclastic packstone–wackstone, reworked foraminiferal-lithoclast grainstone-
Kamal H. Karim et al.,
70
packstone, lithoclast grainstone and terrigenous lime sandstone. The environment of
the formation was high energy, shallow and normal- marine sea, which consists of
fore-reef, reef and back-reef. The tectonic and paleogeographic relations of the
formation are discussed in terms of facies and boundary condition. It is confirmed that
the Sanandij-Sirjan Zone was subjected to an extension not compression (continental-
continental colliding), as cited in some studies. The richness of the basin and fauna
indicates that it was connected to Indian Ocean and Mediterranean Sea.
Keywords: Govanda Formation, Angular unconformity, Sanandij-Sirjan Zone,
Miocene facies analysis.
ــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــ
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
71
coral framestone, pelecypod floatstone, coral and lithoclast rudstone, coral
bufflestone, stromatolite bindstone, foraminifera and red algal bioclastic packstone–
wackstone, reworked foraminiferal-lithoclast grainstone-packstone, lithoclast
grainstone and terrigenous lime sandstone facies
ــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــــ
INTRUDUCTION
The Govanda Formation represents the deposits of early Middle Miocene and
has the thickness up to 150m (Jassim and Goff, 2006). It was first described,
according to Bellen et al. (1959) by Dunnington, Al-Naqib and Morton in 1957. In
Iran, it is equivalent to the Asmari Formation and its type localityin Iraq lies on the
northwestern slopes of the Govanda Plateau in the Imbricated Zone of northeastern
Iraq at latitude 37°07'58"N and longitude 44°12'53"E in Erbil Governorate.
According to Bellen et al., (1959), the lithology of the type section, from top to
bottom is as follows: the lowermost 6m is composed of a polygenic basal
conglomerate and passing upwards into conglomerates with pebbly sandstones and
siltstones. These terrigenous clastics are overlained by roughly 20m of silty and sandy
detrital limestones with abundant derived- Cretaceous fossils. The overlyjng 80-90m,
i.e. the bulk of the formation, is made up of limestones of reef-fore reef facies.
The previous studies of the Govanda Formation indicate to shallow marine reef-
fore-reef environment, strongly affected by the supply of the nearby rising land, as
Kamal H. Karim et al.,
72
testified by the presence of clastics not only at the bottom, as in the type locality, but
sometimes intercalating with the limestones too (Buday, 1980). He added that its
lower contact is unconformable and the formation had transgressed on the Red Bed
Series and its upper contact is not visible. In Shalair Valley, the thickness of the
formation is about 100m and it is composed of a basal conglomerate (containing chert
pebbles derived from the Qulqula Radiolarian Formation), which passed upwards and
laterally into fossil rich sandy limestone and capped by thick oyster-bearing limestone
(Jassim and Goff, 2006). They added that the formation is unconformably underlained
by the Swais Group, Tanjero Formation and locally by the Qulqula Formation.
LOCATION
The studied area belongs to Kurdistan Region, northeastern Iraq in the Sulaimani
Governorate near the Iraqi-Iranian borders (Fig.1). The sections of the formation are
distributed over six different areas. The first section is located at the southwestern
boundary of Shalair Valley at 25km to the northwest of Penjwin town (Figs.2 and 3).
The center of this section is located at latitude of 35o 45- 58.82= N and longitude 45o
49- 29.20= E. Its outcrop (Bahe outcrop) is the largest and has length 15km and 1km
width, and it elongates along Gole stream from Komari (southeast) to Bahe Village
(northwest) (Figs.4 and 5). The second section is located at the latitude of 35o 40-
32.75= N and longitude 45o 52- 14.01= E, and its outcrop (Qzlja outcrop) includes the
area at the north and northeast of the Qzlja Village at 10km southwest of Penjwin
town. These latter two outcrops are mapped by Buday and Jassim (1987).
The third section is located between Rashan and Qzlja outcrops on the Mila
Kawa peak, exactly on the western side of the paved road to Penjwin Town. On the
peak there is small outcrop (Mila Kawa outcrop) of the formation having about 10 m
thickness and lateral continuity for only about 100m. The forth section is located in
the middle of the bottom of the Rashan (Taza De) Valley especially along the
southern side of the stream that flows in the valley. The center of the section is
located at the intersection of latitude and longitude 35o 31- 14.91= N and 45o 59-
54.84= E respectively. Its outcrop has thickness, length and width 10, 10000 and 200
meters respectively. The fifth section (Rashan outcrop) is located at the head of Dola
Chawt near Barda Balaka Village and its outcrop (Barda Balaka outcrop) is small,
which is less than one quarter of square kilometer. The outcrops are distributed over
both sides of the unpaved road that pass through the village (Figs.2 and 3) and rested
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
73
on the Qulqula Radiolarian Formation. The center of this section is located at the
intersection of latitude and longitude 35o 33- 07.82= N and 45o 49- 35.02= E
respectively.
There is another section (sixth section) at 3km to the west of Chwarta town. It is
found by Al-Barzinjy (2005). This outcrop is very small and has a surface area of 50
square meters and it consists of coral colony limestone; and this author attributed this
to the Unit Six of the Red Bed Series, but it possibly belongs to the Govanda
Formation. The center of its exposure is located at latitude and longitude of
35o 43- 26.94= N and 45o 51- 32.76= respectively (Figs.2 and 3).
Tectonic setting of the studied area:
According to Buday (1980), the studied section is tectonically located within the
Thrust Zone regarding the tectonic divisions of Jassim and Goff (2006). It is located
in the Qulqula-Khwakurk and Penjwin-Walash Zones as two neighboring zones of the
Suture Zone. The area has the most complex geological setting in Iraq, which
manifested by brecciation, thrusting, transpress deformation, igneous intrusion and
metamorphism.
In the studied area, four main thrust sheets can be identified in the field. The
largest is outer (lower) one, which consists of the Qulqula Radiolarian Formation
sheets thrusted up on different units in different formation, such as the Tanjero, the
Shiranish, the Kometan and the Balambo in addition to Jurassic rocks units.
The Qulqula Radiolarian Formation is about 1000 meters thick and consists of
bedded chert, siliceous shale, marl and limestones, which are studied by Karim and
Baziany (2007), Karim et al. (2009), Karim et al. (2011) and Baziany (2013). The
second sheet consists of the Avroman Formation, which is thrusted on the Qulqula
Radiolarian Formation. The Avroman Formation is composed of detrital and biogenic
limestone of reefal facies (Karim, 2007). The third sheet consists of many smaller
sheets, but the main one is Penjwin Ophiolite Complex, which is thrusted on the
Merga Red Bed and the Qulqula Radiolarian Formation. The Penjwin Ophiolite
Complex consists of gabbro, peridotite, dunite and small bodies of acidic rocks. The
fourth sheet is composed of metamorphic phyllite, hornfels and calcsilicate marble
(Karim et al. 2016). Structurally, the main folds are so deformed that cannot be
identified, and only the small folds are observable.
The studied area is located within the Sanandij-Sirjan Zone, it is located between
Main Zagros Thrust at southwest and Urmia-Dokhtar Magmatic Zone at the northwest
Kamal H. Karim et al.,
74
(Moghadam and Stern, 2015; Jamshidi Badr et al., 2010). However, the definition of
Stocklin (1968; in Yousefirad, 2011) and tectonic map of Ghazi and Moazzen (2015)
are considered in this study.
Geomorphologically, the area is a part of high- Mountain series of Zagros belt
and due to aforementioned sheets. The main (large) valleys have northwest-southeast
trends, which are subsequent valleys such as Taza De, Nalparez, Ahmad Klwan,
Qzlja, Shalair and Gole valleys. These valleys are surrounded by high mountains from
northeast and southwest, their heights are more than 2000m above mean sea level.
The mountains are Suren, Spidara, Kani Shawkat, Shawkat, Taryar Qaya, Harzala,
Nizara, and Bahe. Many small subsequent and consequent valleys are of descending
heights from the high mountains. These valleys have emepheral streams and joining
the large ones.
Fig. 1 a): Tectonic Subdivisions of Northern Iraq (Jassim and Goff, 2006)
Showing the Studied Area,
b): Location of the Studied area in the Zagros Fold-Thrust Belt
(Modified from Ghazi and Moazzen, 2015).
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
75
Fig. 2: Location of the Studied Outcrops on Google.
Kamal H. Karim et al.,
76
Fig. 3: Geological Map of the Studied Area (Modified from Buday and
Jassim, 1987) on which the Studied Sections (outcrops) are Indicated.
Fig. 4: An outcrop of the Govanda Formation at South and Southwest Sides
of Bahe and Kani Mirani Komari, Southwestern Boundary of Shalair
Valley, Penjwin Area.
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
77
Fig. 5: An outcrop of the Govanda Formation (Section No.1) at 200m West of
Bahe Village, Southwestern Boundary of Shalair Valley, Penjwin Area.
Method of the study:
This study depends on the field observations during which the upper and lower
boundaries of the Govanda Formation are examined. The geographical extends are
plotted on the map, and 23 samples are collected for lab study and stereoscopic
microscopy for indication of allochems and orthochems. The selected samples are cut
for thin section preparation to study petrography under polarizer microscope. In the
thin sections and hand specimens, the facies are identified after differentiation of the
rocks constituents that include faunas, lithoclasts, intraclasts, extraclsts and boiclasts.
For this identification, the Dunham (1962) classification and its modification by
Embry and Klovan (1971) are followed.
RESULT
Geological boundaries of the formations
1- The lower boundary
The lower contact of the Govanda Formation is exposed in many areas that are
rested on different lithologic units. The type area, in Erbil Governorate, it is
unconformably rested on the Kirkuk Group Formation and Tanjero Formation
(Bellen et al., 1959 and Buday, 1980); and according to Al-Hietee (2012), it
represents transgressive facies that is rested on the previous units. In the northwestern
part of the studied area in Bahe and Qzlja outcrops (Figs.2, 3, 4 and 5), it
Kamal H. Karim et al.,
78
unconformably overlies the Qulqula Radiolarian Formation in an angular relationship
near Gole, Bahe and Qzlja Villages. The angular unconformity can be seen clearly
from intensive folding of the beds of the Qulqula Radiolarian Formation below the
Govanda Formation (Fig.6a). In this area, there is about 1.5m of polygenetic basal
conglomerates between the two formations and it consists of gravel conglomerates
with red- clayey sandstone matrix or cemented by calcite (Fig.6b). In some locations,
it shows intensive brecciation especially on the northern bank of the Gole stream. The
same angular relationship is true for Barda Balka outcrop near Razla Village, which is
rested on the Qulqula Radiolarian Formation with highly shearing, and brecciation
that are possibly tectonic. The lower boundary in southeastern part of the studied area
(Rashan outcrops) is rested on the sandstone of the Merga Red Bed that may be
tectonic; the Merga Red Bed is possibly of late Miocene age (Buda, 1980).
2- The Upper Boundary
According to Bellen et al. (1959) and Buday (1980), the upper boundary is
erosional in most places while the formation is overlained by the Merga Red Bed in
some places. In the studied area, it seems that the so-called “Merga Red Bed” in
Penjwin area is located below the Govanda Formation. There is a small outcrop of the
formation between Rashan and Qzlja outcrops, exactly on the Milakawa peak and on
the western side of the paved road. This outcrop is intensively brecciated and it
consists of a mixture of detrital and nummulitic limestones with sandstone and
calcareous shale (Fig.7). It is located between ophiolite (Penjwin ophiolite by Jassim
and Goff, 2006) at the top, and the Merga Red Bed at the base. In this locality, both
boundaries are tectonics. This outcrop contains nummulite of the Eocene age that is
probably reworked. A small part of Bahe outcrop, at 800m to the southwest of Gole
Village, is overlain by lithified oncoidal massive limestone and travertine (Fig.8). The
age of this limestone is unknown, but it may belong to Pleistocene or Sub-Recent as
the dips of its strata are nearly coinciding with the local slope of the area.
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
79
Fig. 6 A): The Govanda Formation (Middle Miocene) rested on the Qulqula
Radiolarian Formation in an angular relationship (angular unconformity) at
5km south of Siaguez Village in Shalair Valley directly to the north of Bahe
Village. B): Basal conglomerate between the Govanda and the Qulqula
Radiolarian formations near Bahe Village.
Fig. 7: Possible Govanda Formation (brecciaed) between Penjwin Ophiolite and the
Merga Red Bed on the Mila Kawa peak near Kani Manga Village.
Kamal H. Karim et al.,
80
Fig. 8: Stromatolitic (oncoidal) limestone within the Govanda Formation, 200m north of
Bahe Village.
FACIES ANALYSIS
Lithofacies and biofacies analyses of the Govanda Formation are difficult for
interpretation due to many issues, the first issue is the presence of reworked fossils
from the Cretaceous (Bellen et al, 1959) and from possible Eocene ages (Inferred
from present study). The second is the complexity of its boundaries condition, which
is greatly variable (geographically and chronologically), which constrained the
accurate definition of the facies. The third is the intensive deformation and distortion
of the allochem constituents of the facies due to its location in the Suture Zone or
Sanandij-Serjan Zone; therefore, the deformation limits the accuracy of the
identification. The fourth is the degree of recrystallization that diminishes the
accuracy of documentation and the photos of the facies might not be clear. The fifth is
that the most facies contain more or less terrigenous clasts, which restrict accurate
terminology. However, many facies were found in the Govanda Formation of
environmental and paleogeographic importance. These facies can be recognized in
both polished slabs and thin sections. In rare cases, this facies contains whole
echinoderms skeletons.
1- Pelecypod floatstone Facies (F1)
This facies is supported by a carbonate matrix that contains more than 10%
grains larger than 2mm. The matrix of floatstone does not necessarily correspond to
be only micrite, but often consists of fine-grained textures that must be described
separately (Flugel, 2004). This facies is very common in the lower part Bahe section
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
81
and it occurs rarely in the Qzlja and Barda Balaka sections (Fig.9). This facies consist
of skeletons or bioclasts of pelecypods (Fig.10) with or without coral and red algae
fragments (that are larger than sand size) and floated or embedded in fine matrix of
sand or silt sized bioclast or lithoclasts. The thicknesses of this facies are 10–80 cm
and have sharp base with sandy marlstone. This facies show crude lamination and
alternated with sandy marlstone. In one case and in the Barda Balaka section, there is
a sample contain clasts of large gastropod and other unknown fossils (Fig.11).
Generally, in this outcrop and its section, the clasts are very angular and the delicate
sculptures are clear, which are denoting very short distance of transportation and
relatively rapid deposition. This facies may be deposited in back-reef setting.
Fig. 9: Stratigraphic Column of the Studied Sections.
Kamal H. Karim et al.,
82
Fig. 10: Pelecypod (including oysters) Floatstone in the Lower Part of
the Govanda Formation, Bahe Outcrop.
Fig. 11 a): Gastropod and lithoclast floatstone in Barda Balaka Outcrop,
b): Gastropod Lithoclast Floatstone with Patches of Stromatolite at
the Left.
2- Coral and lithoclast rudstone (F2)
This facies consists of pebble-sized limestone lithoclasts and bioclasts or
skeletons of coral, and it is very common in all sections. Coral bioclast rudstone is
common in Rashan and Bahe sections, which consists of elongated, 2 - 3cm long and
0.3-1cm in diameter (Fig.12). The lithoclast rudstone is very common in Qzlja and
Barda Balaka sections and it makes up more than 50% of the thickness of
the section (Fig.13). The lithoclast rudstones are composed of angular to sub-angular
pebbles of limestone clasts of different constituents includjng coral or algae or
bioclasts or lithoclasts pebbles. The lithoclasts can be called limestone conglomerates
(extraformational or intraformational conglomerates) or breccia. The thickness of this
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
83
facies is about 30m around Qzlja Village and this huge thickness cannot be formed by
faulting, but it is depositional product that formed by erosion of tectonically fractured
limestones in the basin or on surrounding terrestrial lands; or it may be a reef talus
deposit.
This facies might be derived from reef tops and deposited in a high energy
setting (forereef) due to rock-fall and various mass-flow processes.
According to Flugel (2004), rudstone is, an equivalent to packstone and
grainstone, but its grains are self-supported carbonate rocks containing more
than 50% grains larger than 2mm. This facies can be further characterized by
compositional and textural criteria. Deposition of rudstone needs erosion and
transportation. Flugel farther added that erosion could be triggered by shallow water
settings allowing destruction by storms.
The allochems are bound by fine-grained matrix such as: sand and silt sized-
carbonate grains in addition to lime mud (matrix-supported fabric). This facies is
introduced into Dunham (1962) classification by Emery and Klovan (1971), it
consists of self-supporting allochems (more than 2mm in diameter) that bounded by
micrite (mudstone). According to Wilson (1975), rudstones is deposited in fore-reef
environment; where strong waves are prevalent. Praptisih and Kamton (2014) have
found this facies in the Klapanunggal Formation (Late Miocene), western Java,
Indonesia, which is deposited in fore-reef environment. Melim and Scholle (1995)
have found this facies in fore-reef of Capitan Reef, which is associated with packstone
and wackstone.
Fig. 12 a): Coral Rudstone Consisting of Broken Fragment of
Scleractina Coral Colony Near Taza De Village in the Rashan Outcrop.
b): Detail of the Coral under Stereoscope Microscopy.
Kamal H. Karim et al.,
84
Fig. 13: Limestone Rudstone (limestone Conglomerate) in the
Middle Part of the Govanda Formation at 100m North
of Qzlja Village.
3- Coral bafflestone (F3)
This facies is well-expressed in the sections of Barda Balaka and Qzlja outcrops.
It resembles a loose bundle of thin wood sticks of about 0.2–4cm thick and more than
10cm long (Fig.14). It occurs in thick and massive beds of the middle part of the
section of Qzlja outcrops. The broken and re-deposited fragments of this facies have
generated the coral floatstone or rudstone (Fig.12a).
In hand specimen, the red algae coated corals and other grains look like
elongated oncoids (Fig.15b) but they are not oncoids due to the fact that red algae
excluded from algae that formed stromatolies and oncoids (Scholle and Ulmer-
Scholle, 2006). In many cases, the corals steam and polyps are surrounded and
covered by crustose red algae (Figs.15b and c), which might be resulted from the
competition between algae and corals on coral reefs as discussed by McCook et al.
(2001).
The spaces between the coral branches are filled with white lime mud and sand-
sized bioclasts. In literature, this facies is called bafflestone (Emery and Klovan,
1971), because it has dendritic shape and performs as sediment accumulator from the
nutrient- bearing currents and waves by filtering and trapping sediments. Walker and
James (1992) have included this facies in the colonization stage of the reef structure.
The presence of corals indicates normal marine salinity (Riding and Tomas, 2006).
According to Flugel (2004), the criterion for identifying the bafflestone is the
presence of large number of in situ stick-shaped fossils. Pomar et al., (2005)
mentioned this facies in the rocks of the Upper Cretaceous platform in the Pyrenees,
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
85
Spain. The present study indicates that this facies is most possibly deposited in back-
reef environment.
Fig. 14 a): Photo of the Coral Bafflestone of Barda Balaka Outcrop, Between the
stems, Fine Lime Mud and Sand-sized Allochems are Deposited.
b): Same facies of the Rashan outcrop showing vertical finger like corals
streams, some are branching.
4- Coral framestone (F4)
This facies is common in Barda Balaka and Chwarta sections while it is rare in
Qzlja and Bahe sections; under hand lens and binocular microscope, it consists mainly
of irregular or global bodies (colonies) or patches of pentagonal coral and brain-like
corals. The sizes of the colonies or patches are different, but the common one is
5- 30cm in diameter (Fig.15a, b). The spaces between patches are filled with fine-
grained carbonate (lime mud and fine-grained allochems). Many specimens are found
to contain single large corals (mushroom corals) with a diameter of 3 - 7 cm,
consisting of framestone and associated with red algae (Fig.15a). The present study
indicates that this facies is most possibly deposited in backreef environment.
According to Flugel (2004) and Wu. et al., (2012). This facies is deposited on reef
core (reef body) environment.
Kamal H. Karim et al.,
86
Fig. 15 a): Coral and rudstone consisting of broken fragment of scleractinian coral
colony near Taza De village on the Rashan outcrop,
b): detail of the coral under stereoscope microscope.
5- Stromatolitic bindstone (F5)
Flugel (2004) cited that this facies, as a type of limestone, consists of rigid
framework (skeleton) built by framework of the organisms. Embry and Klovan (1971)
introduced bindstone as a part of the boundstone of Dunham (1962) to the
classification of carbonate. The distribution and morphology of the skeletons should
fit into an imaginary three-dimensional organic framework. Many organisms
contribute to deposition of framestones as corals, coralline sponges, stromatoporoids,
rudist bivalves and calcareous red algae.
In the studied sections and outcrops, this facies is not common, but it exists in
all sections especially in Qzlja and Barda Balaka sections. In hand specimen, it can be
seen as dense undulated and corrugated laminations that probably represent
stromatolites (Fig.16a). In Qzlja section, there is a highly wavy limestone and under
stereoscope microscope it shows dense reticulate texture that is made of layers
of tiny pillars, which forms brick- like wall structures and are distinctive features of
stromatolites (Figs.16b and 17). These limestones are stromatoporoids
bindstone according to the comparison of the present sample with those
published in web site (see http://www.earthsurfaceprocesses.com/3f-E-Stromatojlites
Stromatoporoids.html). In the Bahe section, the stromatolitic limestone occurs too,
which consists of oncoids formed by microbes (microbalite), but the age of this bed is
unknown. In this context, McConnell (1975) considered this type of stromatolite as
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
87
stratiform type and attributed its deposition to intertidal and possibly supratidal
environment.
Fig. 16 a): Algal Stromatolitic Bindstone in the Barda Balaka Outcrops,
b):Stromatoporoid Bindstone in the Qzlja Outcrop, See Figure 17 for
Enlarged Views.
Fig. 17: Stromatoporoid (Sponge) Bindstone (or Framestone) Under Normal Light
stereoscope microscope in the Qzlja outcrop, it was taken from the top of figure
16b. a Cross Section and b) Vertical (longitudinal) Section, the Scale: is the Tip
of Paper Pin (Needle).
6- Foraminifera and red algae bioclasts packstone–wackstone (F6)
This facies is located in the middle of the formation; it alternates with coral
bafflestone facies, and consists, in outcrop, of dark - grey massive to crudely
laminated limestone. This limestone is characterized by the occurrence of various
Kamal H. Karim et al.,
88
foraminiferas skeletons of in-situ species and in most cases; it is associated with
bioclasts of red algae and pelecypods in addition to lithoclasts, but without planktonic
forams. There are many species of forams in the Bahe outcrop such as Borelis melo
melo and Borelis melo Curdica and unknown miliolids (Figs.18a and b). While those
of Mila Kawa outcrop, include different reworked nummulites, lepidocyclina and
rotalids species (Fig. 19).
The age of the in situ forams of the former section is Late Middle Miocene due
to presence of Borelis melo curdica-Borelis melo melo with other miliolids forams,
while the age of latter outcrop is not known because the fossils are reworked.
Fig. 18 a): Borelis melo curdica in the Qzlja-Bahe Outcrops, S. No.3., Under
Stereoscopic Microscopy b): Foraminifera-Lithoclast Packstone with Borelis
melo melo with other Miliolids foram S.No.10. Both Photos are Taken Under
Normal Light by Stereoscope Microscope, S.No.4.
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
89
Fig. 19 a): Red algae (grey and black grains) and Foramioneral (Borelis melo curdica)
Wackstone of the Bahe Outcrop.
b): Crustose red algae Covering Coral and Forming Massive Rocks in Lower
Part of Qzlja Section, S.No.9.
7- Reworked Foraminiferal-lithoclast grainstone-packstone (F7)
The reworked forams are accompanied by terrigenous clasts of sedimentary,
igneous and metamorphic rocks that are derived from nearby uplifted land.
Additionally, they have intensively deformed both in brittle and ductile manners,
which can be seen as suture contact between the forams and relatively deep
penetration of one foram into others (Fig.20a and b). This deformation is tectonic and
not lithostatics due to their location under the ophiolite sheets (Penjwin Ophiolite) and
bounded below by the Merga Red Beds.
8- Lithoclast grainstone (F8)
The major components of this facies are lithoclasts, which consist of oval
or spherical sand- sized grains of limestone. They consist of limestone clasts that are
well sorted and well-rounded allochems bound together by spary calcite cement.
They appear transparent under binocular microscope and in some intervals; this
facies contains bioclasts (Fig.21a). The facies was deposited in high energy agitating
environment in which all the fine grain sediments (lime mud) are washed out.
Due to this washing, the space between the grains is remained empty and later
during diagenesis filled with spary calcite cement. This facies is recorded in the
Barda Balaka section only and alternates with lithoclast rudstone
Kamal H. Karim et al.,
90
(limestone conglomerate) ,(Fig.21b) and coral bindstone. The age of this facies is not
known and the present authors are not sure if it belongs to Govanda Formation
because the rocks of this outcrop are mixed and brecciated, and the layer boundaries
are not distinguishable between facies (beds).
Fig. 20a and b: Reworked Foraminiferal Packstone from Mila Kawa Outcrop. The
Forams are Intensively Deformed Both in Brittle and Ductile Situation so that
Appear as Suture Contact Between the Forams and Relatively Deep Penetration
of One Foram into Others. S.No.14, ppl., X40.
Fig. 21 a): lithoclast Grainstone in the Barda Balaka Outcrop, S.No.19a, Normal
Light, X20.
b): Rudstone Consisting of Lithoclast (Black Grains Indicated by Arows)
and Coral Bioclast (Light Grey), S.No.19b.
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
91
9- Terrigenous lime sandstone (F9)
The name of this facies refers to its derivation from terrestrial (terrigenous) land
by rivers and to its limestone clasts content. The major components of this facies are
lithoclasts, which have angular, elongate and badly sorted coarse sand-sized grains of
different rocks (Figs.23a and b). They consist of deformed fossils Nummulite whole
skeletons and fragments (nu), fossil fragment, black limestone, chert, jasper
metamorphic, volcanic and igneous (Figs.22 and 23) and clasts that were derived
from terrestrial lands and they were surrounded basin of deposition.
Fig. 22: The Terrigenous Sandstone Containing Lithoclasts and Deformed Fossils
(df), Nummulite (nu), Fossil Fragment (ff), Black Limestone (bl), Chert (ch),
Jasper (ja), Limestone (l) Metamorphic (m), Shale (sh) Volcanic (v) and
Igneous (ir), Both Photos are Under Plane Polarized Light, S. No. 14. ppl,
X40.
Kamal H. Karim et al.,
92
Fig. 23 a.): Association of Deformed Nummulite (df) and lepidocyclina (le) with
Volcanic (v) and Chert Fragments (ch). b): Clear Flexure Slip and Flexure Flow
Folding (1 and 2) and Faulting (3), Both Photos Belong to the Mila Kawa
Section (or outcrop), S. No.15, ppl, X40.
This facies is directly located below the reworked- foraminiferal packstone in
Mila Kawa outcrop. In few beds, sedimentary, igneous and metamorphic rocks clasts
can be seen together. These clasts show clear syntectonics flexure-slip and flexure-
flow folding (1 and 2) and faulting (3) (Fig. 23b). The different types of clasts are
indicative of diversity of sources from which the sediments derived, which included
different type of sedimentary, igneous and metamorphic rocks. There are gradational
facies that changes between this facies and the previous one (foraminifera and
lithoclast packstone-wackstone). Figures (20a and b) show this gradation, which
contains both nummulite (nu) and lepidocyclina (le) forams with clasts of different
rocks (Fig. 23a).
INTERPRETION AND DISCUSSION
In the discussion of the Govanda Formation, one does not know when and where
to start writing because of many factors and properties. Among these factors, the
boundary condition of the formation, lithology, facies diversity, and its tectonic
location in the area, which is highly variable. The most important issue of the
boundary condition is its resting on the tilted and folded Qulqula Radiolarian
Formation in a stratigraphic relation of angular unconformity (Fig. 6). In literature,
this unconformity is not the only angular one in the Zagros Fold - Thrust Belt
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
93
(Karim et al., 2011). Karim and Baziany (2007, p.58) concluded an angular
unconformity between the Qulqula Radiolarian Formation and the Red bed Series in
foothill of the Qandil and Gimo Mountain Ranges in Qaladiza and Mawat areas
nearly on the southern boundary of the Sanandij-Sirjan Zone. They discussed that the
age of tilting is pre-Paleocene age. The angularity of the present unconformity is
better expressed in lateral continuity and the tilting angle between the two units that
was represented by basal conglomerates (Fig.7).
Another issue is its location in the Suture (Sanandij-Sirjan) Zone and according
to Ghazi and Moazzen (2015), it is the most active tectonic zone of Zagros since
Jurassic. Moreover, Sadeghi and Yassaghi (2016) mentioned that this zone was an
area of collision of Zagros. The original location of the Govanda Formation was more
northeastward in the Zone but it had been moved (with all other rocks) southwestward
by thrusting of the Iranian (Eurasian) plate over the Arabian one.
From description of the facies types, it is obvious that normal- marine and
shallow carbonate rich fossils were deposited during the late Middle Miocene. The
richness of the formation with fossils is most possibly attributed to rich nutrients that
were arrived the basin from the surrounding sources areas. It is possible that each
source was represented by a thrust sheet and the basin may be piggy back basin. The
age, zone and angularity of deposition are very important for tectonic and
paleogeographic evolution of the Zagros. Although, the carbonate deposition
(with associated clastics) shows active tectonic, but not to a degree to justify a
continental-continental colliding of the Arabian–Iranian plates as cited by Mouthereau
et al. (2007), Allen and Armstrong (2008); Aral et al. (2010), McQuarrie and van
Hinsbergen (2013); they concluded that it happened during the Miocene. This
colliding does not match with the subsidence of the area and deposition of normal-
marine carbonate during the Miocene as mentioned by Buday (1980); Jassim and
Goff (2006) and it is inferred in this present study. Conversely, the studied area must
be subsided to a basin not uplifted to a terrestrial area.
Therefore, the colliding must had occurred before the Miocene due to intense
deformations in the pre-Miocene age as testified by angular unconformity with the
Qulqula Radiolarian Formation (Figs.6 and 9). It seems that the studied area was an
intercontinental shallow basin. It is more or less similar to the present day eastern
Mediterranean Sea or Arabian Gulf in which shallow water carbonates and clastics
deposit. The Paleogeographic map of Scotese (2001) during the Middle Miocene
shows that this basin was connected to open marine via Mediterranean, Arabian Seas
and Arabian Gulf (Fig. 24). Other evidence for connection is the map published by
Kamal H. Karim et al.,
94
Rögl and Steininger, 1983 in Çağatay et al. (2006), it shows the latter sea that extend
to the near studied area during Middle Miocene. Additionally, when the map of the
Bosworth et al. (2005) is considered, there is a connection to the Arabian Gulf and
Indian Ocean. The richness of the Govanda Formation with normal marine fauna
strongly aids the connection of the studied area to the above-mentioned seas and
ocean.
Last issue of the Formation is its environment, which was normal- marine-
shallow water sea as indicated by its richness in fossil content. This environment can
be subdivided into several ones according to the specific depositional facies. The
content of echinoderm and coral floatstone and rudstone are indicative of fore-reef.
While the coral framestone and bufflestone with different algae represent reefal core
environment. The foraminiferas and red algae bioclasts, packstone–wackstone with
miliolid forams and stromatolies are best evidence for back-reef environment.
The existed lagoon environment was of semi-restricted lagoons, which is called
“leaky lagoon” by Kjerfve (1994), who defined it as a lagoon connected through wide
channels to sea by which the water interchange is fast and unlimited. Lower, middle
and upper parts of the formation were deposited in the fore-reef, reef and back-reef
respectively.
Fig. 24 Paleogeographic Mmap of Middle East During Middle Miocene Showing the
Connection of the Studied Area to Arabian Gulf, Mediterranean and Arabian
Sea (Scotese, 2001).
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
95
CONCLUSION
1- The upper boundary of the Govanda Formation is erosional (not exist) while the
lower contact is tectonic, it rested on the Qulqula Radiolarian Formation in an
angular unconformity relationship and rested on the Red Bed Series in Rashan
Section.
2- The main facies of the formation are pelecypod floatstone Facies, coral and
lithoclast rudstone, coral bufflestone, stromatolitic bindstone, foraminifera and red
algal bioclasts, packstone–wackstone, reworked foramioneral-lithoclast
grainstone-packstone, lithoclast grainstone and terrigenous lime sandstone.
3- Detailed Facies analysis indicates that the formation was deposited in a high-
energy shallow, normal marine of fore-reef, reef and back-reef environments.
4- The Sanandij-Sirjan Zone was subjected to extension not compression (continental-
continental collision) as cited in some studies.
5- The richness of the basin with fauna indicates that the formation was connected to
normal marine of both Indian Ocean and Mediterranean Sea.
REFERENCES
Al-Barzinjy, S.T.M., 2005. Stratigraphy and Basin Analysis of Red Bed Series from
Northeastern Iraq, Kurdistan Region. Unpublished Ph.D. Thesis, University of
Sulaimani, 159 p.
Al-Hietee, S.A.A., 2012. Facies Architecture and Sequence Stratigraphy of the Lower
and Middle Miocene, Kirkuk area, North Iraq. MSc Thesis, College of Science,
University of Baghdad, 97 p.
Allen, M. B., and Armstrong, H. A., 2008. Arabia–Eurasia Collision band the Forcing
of Mid-Cenozoic Global Cooling. Palaeogeogr. Palaeocl., Vol. 265, pp. 52 - 58.
Aral I. O., Zattin M., and Cavazza W., 2010. Apatite fission-track data for the
Miocene Arabia-Eurasia collision Geology, Vol. 38, No. 1, pp. 35 - 38.
Baziany M. M., 2013. Depositional Systems and Sedimentary Basin Analysis of the
Qulqula Radiolarian Formation of the Zagros Suture Zone, Sulaimani Area,
Iraqi Kurdistan Region. PhD Thesis, College of Science, University of
Sulaimani, 200 p.
Bellen R. C., Dunnington H. V., Wetzel R. and Morton D. 1959. Lexique
Stratigraphique, International. Asia, Iraq, Vol. 3c. 10a, 333 p.
Bosworth W., Huchon P., and McClay, K., 2005.The Red Sea and Gulf of Aden
Basins, Journal of African Earth Sciences 43: 334 - 378.
Buday T., 1980. Regional Geology of Iraq, vol. 1, Stratigraphy, Edited by Kassab IM,
Jassim SZ, GEOSURV. Baghdad, 432 p.
Kamal H. Karim et al.,
96
Buday T., Jassim S.Z.,(1987). The regional geology of Iraq, Vol. 2: Tectonism,
Magmatism, and Metamorphism, edited by Abbas M. J., Jassim S. Z.,
GEOSURV, Baghdad, 352 p.
Çağatay M. N., Görür N., Flecker R., Sakınç M., Tünoğlu C., Ellam R., Krijgsman
W., Vincent S., Dikbaş A., 2006. Paratethyan–Mediterranean Connectivity in the
Sea of Marmara region (NW Turkey) during the Messinian, Sedimentary
Geology 188: 171 - 187.
Dunham R. J., 1962. Classification of Carbonate Rocks According to Depositional
Texture: in Northern Iraq. Arabian Gulf, Geology and Productivity. AAPG,
Foreign Reprint Series, No.2.
Embry A. F., and Klovan J. E., 1971. A late Devonian Reef Tract on North-Eastern
Banks Island, N.W.T.: Bulletin of Canadian Petroleum Geology, Vol. 19,
pp. 730 - 781.
Flugel E., 2004. Microfacies Aanalysis of Limestones, Springer Verlag, Berline,
976 p.
Ghazi J. M., and Moazzen M., 2015. Geodynamic Evolution of the Sanandij-Sirjan
Zone, Zagros Orogen, Iran, Turkish J Earth Sci., Vol. 24, pp. 513 - 528.
Jamshidi B. M., Masoudi F., Collins A.S., and Cox G. , 2010. Dating of Precambrian
Metasedimentary Rocks and Timing of their Metamorphism in the Soursat
Metamorphic Using - LA-ICP-MS_U Pb_Dating_of_Zircon_and_Monazite
Complex, NW-Iran, Journal of Sciences, University of Tehran, Islamic Republic
of Iran, No. 21, Vol. 4, pp. 311 - 319.
Jassim S. Z., and Goff J. C., 2006. Geology of Iraq. Published by Dolin, Prague and
Moravian.
Karim K. H., Koyi, H., Baziany M. M., and Hessami, K., 2011. Significance of
Angular Unconformities Between Cretaceous and Tertiary Strata in the
North Western Segment of the Zagros Fold–Thrust Belt, Kurdistan Region, NE-
Iraq. Geological Magazine, Cambridge University Press, No. 148, Vol. 5 - 6,
pp. 925 - 939.
Karim K.H., Hama N. R., and A-Bidary M., 2016. Paragenesis of Asnawa Iron Ore in
Penjween Area, Zagros Suture Zone Kurdistan Region, North-eastern Iraq”
accepted for publication by Iranian Journal of Earth Science Azadi University,
Mashhad, Iran.
Karim K. H., 2007. Lithology of Avroman Formation (Triassic) Northeast Iraq. Iraqi
journal of earth Science, No. 7, Vol. 1, pp. 1 - 12.
Stratigraphy and Facies Analysis of the Govanda Formation from…………….
97
Karim K. H., and Baziany M. M., 2007. Relationship between Qulqula Conglomerate
Formation and Red Bed Series at Qulqula area, NE-Iraq, Iraqi journal of Earth
science, Mosul university, No. 7, Vol. 1, pp.1 - 12.
Karim K. H., Habid H. R., and Raza S. M., 2009. Lithology of the Lower Part of
Qulqula Radiolarian Formation Kurdistan Region, NE-Iraq. Iraqi Bulletin of
Geology and Mining, No, 5, Vol. 1, pp. 9 - 23.
Kjerfve B., 1994. Coastal Lagoons, in Coastal Lagoon Processes. B. Kjerfve (ed.).
Elsevier Oceanography Series, Vol. 60, pp. 1 - 8.
McCook L. J., Jompa J., and Diaz-Pulido G., 2001. Competition Between Corals and
Algae on Coral Reefs: a Review of Evidence and Mechanisms. Coral Reefs.
No. 19, Vol. 4, pp. 400 - 417.
McConnell R. L., 1975. Biostratigraphy and Depositional Environment of Algal
Stromatolites from the Mescal Limestone (Proterozoic) of Central Arizona
Precambrian Research, No. 2, Vol. 3, pp. 317 - 328.
McQuarrie N., and van Hinsbergen D. J. J., 2013. Retro-Deforming the Arabia-
Eurasia Collision Zone: Age of Collision Versus Magnitude of Continental
Subduction, Geology, Vol. 41, pp. 315 – 318.
Melim L. A., and Scholle P.A., 1995. The Forereef Facies of the Permian Capitan
Formation: The role of Sediment Supply Versus Sea Level Changes. J. Sed. Res.
Vol. 65, No. 1, pp. 107 - 118.
Moghadam H. S., and Stern R. J., 2015. Ophiolites of Iran: Keys to Understanding the
Tectonic Evolution of SW Asia: (II) Mesozoic Ophiolites, Journal of Asian Earth
Sciences 100: pp. 31 - 59.
Mouthereau F., Tensi J., Bellahsen N., Lacombe O., De Boisgrollier T., and Kargar
S., 2007. Tertiary Sequence of Deformation in a Thin-Skinned/Thick-Skinned
Collision Belt: the Zagros Folded Belt (Fars, Iran), Tectonics, 26, TC5006.
Pomar L., Gili E., Obrador A. and Ward W.C., 2005. Facies Architecture and High-
Rresolution Sequence Stratigraphy of an Upper Cretaceous Platform Margin
Succession, Southern Central Pyrenees, Spin. In Sedimentary Geology175, 2005,
Sedimentology In: The 21st Century, pp. 338 - 365.
Praptisih S., and Kamton M. S., 2014. Carbonate Facies and Sedimentation of the
Klapanunggal Formation in Cibinong, West Java Indonesian Journal of
Geoscience, Vol. 3, pp. 175 - 183.
Kamal H. Karim et al.,
98
Riding R., and Tomas S., 2006. Stromatolite Reef Crusts, Early Cretaceous, Spain:
Bacterial Origin of in Situ-Precipitated Peloid Microspar. Sedimentology,
Vol. 53, pp. 23 - 34.
Sadeghi S., and Yassaghi A., 2016. Spatial Evolution of Zagros Collision Zone in
Kurdistan, NW Iran: Constraints on Arabia–Eurasia Oblique Convergence, Solid
Earth, Vol. 7, pp. 659 - 672.
Scholle P. A., and Ulmer-Scholle D. S., 2006. Color Guide to Petrography of
Carbonate Rocks AAPG Memoir 77, Publisher: AAPG, 474p.
Scote C. R., 2001. Atlas of Earth History, Volume 1, Paleogegraphy, PALEO MAP,
Arlington, Texas, 52p.
Yousefirad M. 2011.Genetic Relation of the Zagros Thrust and Sanandaj-Sirjan Zone.
Journal of American Science, Vol. 7, No. 7, pp. 835 - 841.
Walker R. G., and James N. P. 1992. Facies Models Response to Sea Level Change.
Geo Text, Geological Association of Canada, 454 p.
Wilson J. L., 1975. Carbonate Facies in Geologic History. Spriger -Verlag, Berlin
Heidelbreg,, 471 p.
Wu L., Jiao Y., and Rong H., 2012 .Reef Types and Sedimentation Characteristics of
Changing Formation in Manyue - Honghua Section of Kaixian, Northeastern
Sichuan Basin Journal of Earth Science, Vol. 23, No. 4, pp. 490 - 505.
