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11
Chapter Two
Chapter Two Stratigraphy
2-1 Preface The Tertiary period in Kurdistan and Iraq is divided into five Sedimentary cycles, Buday (1980) but according to (Al – Kharsan and Al – Jawadi; 1995) they divided this period into five Megasequences. The division of Buday (1980) is suitable with the current researches. Some well exposed rock units are observed within the studied area, which represent the outcrops of different Formations from Paleocene to Quaternary age. This stratigraphic succession from the oldest to youngest rock unit involved:Kolosh Formation, Sinjar Formation, Gercus Formation, PilaSpi Formation, lower Fars Formation, Upper Fars Formation, Lower and Upper Bakhtiari Formations (Jassim et al ,1975 ).While according to (Lawa ,2004) the stratigraphic succession in the study area at NE limb of Darbandikhan anticline are Kolosh Formation, Sinjar Formation, Gercus Formation, PilaSpi Formatio and Fatha Formation . But at SW limb are Kolosh Formation, Sinjar Formation, Sargerma unit?, PilaSpi Formation and Fatha Formation .Fig(2-1). Detailed study and description of all the Formations at that area is not associated to this research, but only the study of the upper most part of the PilaSpi Formation and the lower most part of the Fatha Formation and the contact between these two Formations are the main subject that concerned the current research.
Chapter Two
12
Chapter Two
13
2-2 Detailed description and field observation of the upper parts of the PilaSpi Formation from the Selected Sections:-
2-2-1 Ahmad Brnau Section (AB): The upper part of the PilaSpi Formation of this section is composed of milky colored, massive bedded of dolostone and dolomitic limestone of more than 1m thick, these beds are intercalated with white to white gray, Semi – friable to consolidate well bedded chalky limestone of 1m thick. The marl and marly limestone beds are not well observed between the beds of chalky limestone and dolomitic limestone. More than two sets of joints Fractures occasionally vugy porosity were observed within the dolostones, dolomitic limestone and chalky limestone beds. Within the PilaSpi Formation an intraformational sedimentary breccia which characterized by angular grains was formed by syntectonic orogeny that leads to uplifting the PilaSpi Formation and redeposited these rocks within the same sedimentary basin (Numan,1998). Large horizontal Planolites trace fossil are observed and define within the chalky limestone beds.These burrows are different in dimensions and they have average lengths of (20 – 50cm) and their diameter range between (1.5 – 5cm) (Photo 2-1).These burrows were filled by some different materials. Some thin discontinuous horizon of iron oxides (limonite) also occurred within the upper part beds of PilaSpi formation (photo 2-2). The thickness of PilaSpi Formation in this section about (20m) figure (2-2)
2-2-2 Berki Section (BE): The PilaSpi Formation at this sections characterized by milky color, massive beds of dolostone, well bedded dolomitic limestone and chalky limestone of (11.10m) thick. White color, Friable beds of (15 – 40cm) thick of chalky marl are interbedded with the dolomitic limestone and dolostones beds (photo 2-3).Two sets of Joints and fractures occasionally vugy porosity were observed within the dolostones, dolomitic limestone and chalky limestone beds.
Chapter Two
14
Chapter Two
15
Chapter Two
16
The chert nodules are not well observed at the upper part of the PilaSpi Formation at this section, this may be due to the effect of rapid weathering and erosion processes which removed the chert nodules. 18m thick of the upper beds of PilaSpi Formation was taken from this section to completed the current work Figure (2-3).
2-2-3 Baranan Mountain Section (BM): The PilaSpi Formation in this location represents very ridge rocks and it is composed of massive milky colored dolostones, which are characterized by highly Jointed and well fractured beds. Thin to thick beds of gray to dark gray dolomitic limestone were intercalated in the dolostone beds. Thin to very thin white colored, marl and chalky marl are intercalated with the dolostone and white colored chalky limestone at Berki section but at this section and Barkal section, marl and marly limestone were not well developed and observed, this may be due to the same reason that was discussed at the Ahmad Brnau section which leads to miss these beds. Irregular shapes of dark brown and reddish brown colored chert nodules occurred and distributed randomly at the upper surface of the PilaSpi Formation beds (photo 2-4). The thickness of the total beds of PilaSpi Formation at this section under study is (9m) thick. Figure(2-4)
2-2-4 Barkal Section (BA): The Upper part of PilaSpi Formation at this section is characterized by pink ,purple color,massive bedded highly jointed and well fractured beds of dolostone and dolomitic Limestone of (1-1.25m) thick. Some excavation features and vugy porosity were observed within these beds which cause by dissolution. The beds of dolostone and dolomitic limestone laterally change in their thickness. This may be due to the effect of a great fault which was observed in the field. One of the characteristic features of this section that can not be
Chapter Two
17
Chapter Two
18
Chapter Two
19
Chapter Two
20
Chapter Two
21
Chapter Two
22
observed in the other sections is the presence of white, milky colored, massive beds of gastropodic limestone layer of (30-50cm) thick, which are recorded at the upper part of this section (photo 2-5).Also dark brown colored chert nodules are found at the top surface of dolomitic limestone beds which have an irregular distribution and shape (photo 2-6). The total thickness of the upper beds of PilaSpi Formation of this section was (15m) thick Fig (2-5). In the current research the term Boundary zone has been suggested for describing and studying the upper most parts of the PilaSpi Formation , the lower most parts of Fatha Formation and the contact between these two Formations. The three units in this Boundary zone are well developed and well recognizable in the field within the studied areas. The detailed description of these zone, based on their diagnostic sedimentological features and field observation .
2-3 Descriptions of the Boundary Zone are given from the bottom to the top of the studied sections:
2-3-1Unit A: This unit represent the basal part of the Boundary zone. It is white – gray colored massive beds, which have brecciated characters.Some local chalky limestone and dolomitic limestone beds, which belong to the upper part rock units of the PilaSpi Formation , intercalated with this unit. It has a variable thickness, and ranged between (0.5 – 4 m). At Ahmad Brnau section it is (0.5m),thick; at Berki section (0.7m), while at Baranan mountain Section it is (4m)thick and at Barkal section it is (3m) thick. This unit is mostly composed of angular to subangular clasts of limestone and chalky limestone , mostly it represents residual fragments of the weathered rock units of PilaSpi Formation mixture with red soil.
Chapter Two
23
Chapter Two
24
25
Chapter Two
This character is very common in the Ahmad Brnau and Berki sections photo (2-7, 2-8) but it is different at the two other sections (Baranan mountain and Barkal sections).At Baranan mountain section this unit is mostly composed of angular to subangular clasts of limestone and dolomitic limestone. Toward the upper part, angular to sub angular clasts change to rounded to well rounded clasts. Due to the effect of dissolving of the paleosols unit which located over the unit A, this causes the dissolution of the carbonate clasts which is later formed dark gray color and rounded shape (photo 2-9), . This unit at Barkal section is dark gray colored beds, which is mostly composed
of
angular
to
sub
angular
clasts
of
limestone
and
dolomitic ,limestone. (Photo 2-10).These reworked limestone and dolomitic limestone are belonging to the upper part of the PilaSpi Formation. Unit A of the Boundary zone at all exposed section is represented by sedimentary breccia.
2-3-2 Unit B :This unit was located on the top of the (unit A) directly it is composed of a mixture of red sand, silt and red clay sediments. Shape and configuration of this unit are different and it has a variable thickness from place to place, and it is thickness ranged between (20 – 50 cm). At Ahmad Brnau section this unit is not well observed due to the effect of compaction processes caused by strong orogenic movement or by the effect of rapid weathering and erosion processes removed this unit at this section.While at Baranan mountain and Berki sections this unit is well developed and it has a lensoidal shape with a variable thickness of (20-50cm) which is rested irregularly on the top of unit A. This unit is composed of reddish colored,fine grain sand with reddish clay sediment. The thickness of this unit laterally changes and sometimes it may disappear after a few tens of meters and it is reexposured again (pho2-9),(2-14) Figure (2-3),(2-4).
Chapter Two
26
Chapter Two
27
Chapter Two
28
At Barkal section is composed of medium to fine grain of red sand, silt and red clay sediment mixed with coarse carbonate rock fragments which are derived from the limestone beds of PilaSpi Formation. Pelecypod shells and their fragments are irregularly distributed at the upper part of this unit (pho 2-11).This unit may be represented an oxidational zone and it is a good indication of subaerial exposure (Selley, 1975; Shanmugam , 1988). Unit(B) seem to be developed as a paleosols horizon which will be proven later on by sedimentological analysis.
2-3-3 Unit C : This unit is reseted directly on the top of unit B, and it is representing the conglomeratic unit. It is composed of subrounded to rounded clast of pebble to cobble grain size, poorly to moderate sorted sediments. The thickness of this unite is variable and ranges between (30 cm – 4m).At Ahmad brnau section this unit is (4m) thick, at Berki section (30cm) thick, while at Baranan mountain section it is (2.5m) thick and at Barkal section it is (1m) thick. This unit stratigraphcally belongs to the lower part rocks of the Fatha Formation.Ii is composed of subrounded to rounded ,grain supported,poorly sorted carbonate fragments ranging from granules to pebble grain size and this character is very commonat the Ahmad Brnau section. Generally this unit is belonging to the lower part of Fatha Formation at all the studied sections:At Berki section, this unit represents a grain-supported conglomerate, which is composed of rounded to well rounded and good sorted carbonate fragments ranging from pebble to cobbles grain size (photo 2-12). While At Baranan Mountain section it was composed of angular to sub angular clasts limestone of PilaSpi Formation mixture with red colored sandstone. The angular clasts were forming a fining upward structure (photo 213). But at Barkal section this unit represent a grain-supported conglomerate which is composed of different size (1/2-2mm) subrounded to rounded pebble; poorly sorted grains (photo 2-14). The ground mass of this unit is composed of
Chapter Two
29
Chapter Two
30
Chapter Two
31
green colored sandy limestone matrix . Some benthonic foraminifer is distributed within this groundmass. Stylolite seams are the most diagnostic features of this unit that observed in the field. (Photo 2-15).
2-4 Detailed description and field observation of the lower parts of the Fatha Formation from the selected sections:-
2-4-1 Ahmad Brnau Section (AB): The lower part of Fatha Formation at this section is composed of mottled sandstone. The mottled sandstone is a mixture of reddish and green fine to medium grains friable sandstone, with siltstone.The pebble of carbonate rock fragment of PilaSpi Formation is well observed within the sandstone beds of Fatha Formation. The distributions of these pebbles are forming irregular horizon(Photo 2-16) .Mottled sandstone are highly biotubated (Photo 2-17). This part of Fatha Formation (lower most part) is about 12m Fig(2-2).
2-4-2 Berki section (BE): This section composed of rhythmic alternating of Friable red brown claystone; red brown silty sandstone and green marlstone. The green marlstone is Friable, contains fossils, the whole skeletal grains of Oysters and other bioclasts are well observed within this bed (pho2-18). According to (Mustafa, 1983 – 1984, Karim; 1988), the alternating cycles completed are composed of green marls, carbonate rock, evaporate, clastic rocks at Sinjar basin and Hammam Ali area. The most lower beds of Fatha Formation which represent (21m) were taken from this section for the current work. Fig (23).
2-4-3 Baranan Mountain section (BM): This section is too different from other sections in lithology, thickness and type of sedimentary cycles.
Chapter Two
32
Chapter Two
33
Chapter Two
34
It is composed of rhythmic alternation between greenish and reddish gray fine sandstone with reddish brown claystone and greenish gray siltstone.Some trace fossil such as (Scoyian trace fossil) are well developed within the claystone bed (Lawa, 1995).( photo 2-21). Flaser bedding is another sedimentary structure that observed within this section (Photo 2-19).This structure implies that during the periods of current activity both the sand and mud are available and alternate with periods of quiescence,Reineck and Singh.,(1988).Within the green sandstone beds ,a symmetrical ripple mark is also developed and well observed (photo 2-20). The total thickness of lower part beds of Fatha Formation which was studied in this section reaches (16.1m), Figure (2-4).
2-4-4 Barkal section (BA): The Fatha Formation at this section is composed of cyclicity of rhythmic alternation between light green friable marlstone, reddish brown claybeds and thin limestone beds (photo 2-22). The thickness of the total beds of Fatha Formation in this section which is under study is (10m) thick. Figure (2-5).
Chapter Two
35
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