The Stratigraphic and Petrographic Properties of the Rocks in Davut – Tazekent Vicinity, Diyadin-Ağrı-Turkey

The study is located in vicinity of Taşbasamak, Tazekent, Davut, Boyalan, Kuşburnu and Ulukent villages in the south of Diyadin district of Ağrı city. In the study area, Paleozoic aged Batıbeyli metamorphites which consist of crystallized limestones which contain calc-schist interlevels are observed at the bottom. The Upper Miocene aged Alibonca formation composed of conglomerate, trachyandesitic tuff-agglomerate, sandy limestone, marl, dolomite-dolomitic limestone and lacustrine limestone are located unconformably on these metamorphites. Upper Miocene aged Sekirdağ volcanites consisting of dacitic rhyodacitic tuffs, agglomerates and lavas are observed by lateral vertical transition over the Alibonca formation. Higher up, Lower Pliocene aged Solhan volcanites are composed of alkaline basaltic lavas are observed. The Solhan volcanites are covered by Upper Pliocene aged Hamur volcanites consisting of trachyandesitic lava and ignimbrite. Higher up, Upper Pliocene-Pleistocene aged Kale pyroclastics consisting of lapilli tuff, ash, volcanic bomb, slag and agglomerate with alkaline basalt composition are observed. These pyrolastics are covered by Upper Pliocene-Pleistocene aged Tutak volcanites which are composed of alkaline basalts. At the top, travertine and alluvium are found. Calcite + dolomite ± quartz ± muscovite mineral paragenesis is observed in metacarbonates belonging to Batıbeyli metamorphites. The tuffs belonging to the Kuşburnu pyroclastic member include quartz, plagioclase, sanidine, clinopyroxene (diopside/augite), biotite, amphibole (hornblende), sphene, opaque mineral, volcanic glass and litic fragment. These tuffs were named as lapillistone and ash tuff “according to grain size”, trachyandesite tuff “according to composition and grain size”, lapillistone, ash tuff and lapilli tuff “accoding to percentage distribution of grains” and vitric tuff “according to glass-crystals-lithic fragments composition”. The tuffs of Sekirdağ volcanites contain quartz, plagioclase, sanidine, biotite, amphibole (hornblende), opaque mineral, volcanic glass and litic fragment. The dacitic and rhyodacitic lavas belonging to these volcantecs include quartz, plagioclase, sanidine, biotite, amphibole (hornblende), opaque mineral, plagioclase microlites and volcanic glass. Tuffs belonging to Sekirdağ volcanites were named as lapillistone and ash tuff “according to grain size”, rhyodacitic tuff and dacitic tuff “according to composition and grain size”, lapillistone and ash tuff “according to percentage distribution of grains” and vitric tuff “according to glass-crystals-lithic fragments”. Alkaline basalts of Solhan volcanites include quartz, olivine, clinopyroxene (diopside/augite), apatite, opaque mineral and plagioclase microlites. Plagioclase, sanidine, amphibole (hornblende), clinopyroxene (diopside/augite), apatite, opaque mineral, plagioclase and sanidine microlites are observed in trachyandesites belonging to Tazekent trachyandesite member. Plagioclase, hornblende, clinopyroxene, sanidine, pumice fragments, litic fragments and volcanic glass are located in ignimbirites belonging to Dalören ignimbirite member. The tuffs of Kale pyroclastics include plagioclase, clinopyroxene (diopside/augite), olivine, opaque mineral, volcanic glass and litic fragment. Agglomerates of Kale pyroclastics include plagioclase, olivine, clinopyroxen (diopside/augite), orthopyroxen (enstatite), apatite, opaque mineral, volcanic glass and litic fragment. These tuffs were named as lapillistone “according to grain size”, basaltic tuff “according to composition and grain size”, lapilli tuff “according to percentage * This paper was presented at the International Conference on Access to Recent Advances in Engineering and Digitalization (ARACONF 2020). † Corresponding Author: Konya Technical University, Faculty of Engineering and Natural Sciences, Department of Geology Engineering, Konya, Turkey, ORCID: 0000-0002-4581-6076, gkansun@ktun.edu.tr European Journal of Science and Technology e-ISSN: 2148-2683 529 distribution of grains” and vitric tuff “according to glass-crystals-lithic fragments composition”. The agglomerate is in basaltic agglomerate composition “according to composition and grain size”. Alkali basalts belonging to Tutak volcanites include plagioclase, olivine, clinopyroxen (diopside/augite), orthoproxen (enstatite), apatite, opaque mineral and plagioclase microlites.


Introduction
The study area covers the area of 135 km 2 including Günbuldu, Dibekli, Taşbasamak, Tazekent, Davut, Boyalan, Taşkesen, Kuşburnu, Yukarı Dalören and Ulukent villages in the south of Diyadin district of Ağrı province (Figure 1). The aim of this study is to determine the stratigraphic and petrographic properties of the units which are commonly made of volcanic -pyroclastic rocks and outcrops in the region including Diyadin geothermal field.
The study area is an area where dense volcanic activity is observed in Neogene -Quaternary young volcanics (Figure 1). Turkey is located along the Alpine-Himalayan orogenic belt which form a part of Tethys Ocean.
The grabens, faults, volcanoes and hydrothermal alteration zones and related geothermal activities with these are observed throughout this belt (Şimşek, 1997). Turkey's continental crust was shifted northward from Oligo-Miocene with the movement of the Arabian plate and was fractured as Anatolia sub-plate in Pliocene (Irrlitz, 1972;Şengör and Kidd, 1979;Şengör and Yılmaz, 1981;Koçyiğit et al., 2001). This fragmentation provided magma penetration into Eastern Anatolia and was concluded with formation of various stratovolcanoes including Ağrı, Nemrut, Süphan and Tendürek volcanoes as a result of wide volcanic activity (Şaroğlu et al., 1980). Güleç et al. (2002) and Pasvanoğlu and Chandrasekharam (2011)), b) The location map of the study area Bilgin (1984 and1987) stated that Miocene aged volcanites in the vicinity of Serçeme (Erzurum) have the composition ranging from basalt to rhyolite and that they occur as a result of Himalayan type orogenic events developed during the East Anatolian compressional zone in Middle-Upper Miocene. Güner and Şaroğlu (1987) said that Ağrı Mountain completed its formation in 11 different volcanic phases and that the last phase developed towards the end of Upper Quaternary and that hornblende basalts, hyalo andesites and volcanic clays emerged in this last phase. Yılmaz et al. (1987a and1987b), in petrochemical investigations which they made in volcanic rocks in Bingöl and Muş regions, suggested that the neotectonic period that started in Middle Miocene was formed as a result of the compression regime that started with the continental-continental collision in Eastern Anatolia. These researchers stated that Solhan volcanites were the first products of this phase in the region and that the magma in alkaline character originated from the upper mantle. Buket (1989) said that the Upper Miocene-Lower Pliocene aged Hamurpet volcanites around Varto (Muş) are composed of basaltic andesite, trachybasalt, trachyandesite, andesite, latite and dacite and these are in alkali, calc-alkaline and partly tholeiitic composition. Pearce et al (1990) suggested that volcanic rocks in Kars and Ağrı vicinity have the ages of 7 -0.5 Million years and that these volcanites occur as a result of subalkaline basalt-andesite-dacite-rhyolite fractionation. Ercan et al. (1990) said that the volcanites in Eastern Anatolia were generally upper continental crust, partly lower crust and rarely mantle origin. These researchers stated that the crust fragments belonging to the Arabian plate which had plunged to the bottom before the collision of the Anatolian and Arabian plates mixed with the magma forming these volcanites. silicic volcanites were composed of lava, obsidian and ignimbrite and that peralkaline ignimbrite had the very widespread outcrop. Ercan and Asutay (1993) said that Bingöl volcanites consisted of basaltic lava flows, tuffs, agglomerates and trachytes and they are formed by partial melting in the mantle. Ercan et al. (1994) stated that basic rocks consisting of schist, marble, ophiolite and the young units consisting of claystone, tuff and marls surfaced in Diyadin, Zilan and Çaldıran regions. Erişen et al. (1996) said that Paleozoic aged marble, Neogene aged limestone, lava, tuff and volcanic sandstone surfaced in Diyadin region and that the dominant tectonic regime in the region was NE-SW, N-G, NW-SE trending. Sümengen (2009a), in the study which he made in Karayazı (Erzurum), Aras (Iğdır) and Tahir (Ağrı) regions, stated that Paleozoic aged Akdağ metamorphites consisting of gneiss, amphibolite, schist and marble and Kağızman complex consisting of ophiolite and rock types of sedimentary origin form the bottom in the region. The researcher said that the Çullu formation, which is composed of Late Miocene aged tuff, tuffite, sandstone and marl interlevels, was conformably observed on the Late Miocene aged Yastıktepe formation consisting of alternation of conglomerate, sandstone and marl. This researcher stated that the Late Miocene aged volcanites in the region are represented by Kaletepe volcanites consisting of pyroclastics and andesitic lavas and Sekirdağ volcanites consisting of dacite, rhyodacite, pyroclastic and andesite. He claimed that the Plio-Quaternary aged Karayazı volcanites are composed of basalt and andesite and same aged Tutak volcanites are composed of basalt, hawaiite and mugearite. Sümengen (2009b) states that the Kağızman complex is located on the Paleozoic aged Akdağ metamorphic rocks which form the bottom in Patnos (Ağrı) and Malazgirt (Muş) vicinities. This researcher said that Middle-Late Miocene aged Cemalverdi volcanites, which consist of andesites and dacites, are unconformably overlain by Pliocene aged sediments and volcanites. This researcher stated that Upper Miocene aged units is represented by Karaali formation consisting of alternation of sandstone, claystone, shale and gypsum, Alibonca formation consisting of conglomerate, mudstone, siltstone and gypsum and Sekirdağ volcanites at calc-alkaline feature consisting of andesite-dacite type lavas in the region. This researcher said that the Solhan volcanites, which consist of Early Pliocene aged basalt, mugearite, hawaiite and benmorite type lava flows, were lateralvertical transition with Pliocene aged Zırnak formation consisting of conglomerate, sandstone, claystone and limestone. This researcher indicated that the Plio-Quaternary aged Bulanık formation and Tutak volcanites are unconformably observed on Pliocene aged Hamur volcanites consisting of dacite, trachyte and ignimbrite in the region. This researcher suggested that the volcanism in the region started in the alkaline character and then ended with Süphan volcanites, which showed calc-alkaline character. Açlan and Turgut (2017) stated that plutonic and volcanic units are observed around Şekerbulak (Ağrı). They said that the plutonic units were represented by Taşlıçay Granitoid consisting of tonalite, granodiorite, monzogranite and granite. They indicated that Yeltepe trachyandesite and Yuva rhyolite are formed the volcanic units. These researchers suggested that volcanic units showed subalkalic, calcalkalic, high K series and shoshonitic features.

Material and Method
In the field studies, detailed geological map of the study area was prepared on Doğubayazıt -I 51-d3, Doğubayazıt -I 51-d4, Doğubayazıt -J 51-a1 and Doğubayazıt -J 51-a2 numbered the topographic maps at the 1/25000 scale by using the geological map which was made by Burçak et al. (1997) (Figure 2). The stratigraphic cross section of the study area was made by taking into consideration ages, stratigraphic positions and boundary relations of the units which outcrops in the study area ( Figure 3). During the field studies, 85 rock samples were taken from different units. Thin sections were made from 52 of these samples in Konya Technical University, Faculty of Engineering and Natural Sciences, Department of Geological Engineering.
Volcanic rocks were classified in "double triangular diagrams of Streckeisen (1967)" according to their mineralogical composition. In addition, these rock classications were supported with the geochemical analysis results which were made from these rocks. The pyroclastic rocks were denominated by taking into consideration the grain size, the mineralogical composition and the volcanic glass-lithic fragments composition in the naming diagrams for pyroclastic rocks of Schmid (1981), Pettijohn et al. (1987) andLe Maitre (2005). The mineralogical composition and texture-structure characteristics of the metamorphic rocks are taken into consideration at the nomenclature of metamorphic rocks. The classification diagrams of metamorphic rocks at low and high temperature of Winkler (1979) and percent mineral contents of metamorphic rocks were used in these naming. Also, the structural features of the metamorphic rocks were also taken into consideration in these names. The classification diagrams of Folk (1962) and Dunham (1962) were used in the nomenclature of clastic and carbonate sedimentary rocks.

Batıbeyli Metamorphites
It is composed of crystallized limestones with calcschist interlevels. The unit was named as Batıbeyli metamorphics by Çakır (1994). In this study, these metacarbonates were defined as Batıbeyli metamorphites. Batıbeyli metamorphites are observed in Ulukent Village, Ortadüz Ridge and the southwest of Kuş Ridge in the southwest of the study area ( Figure 2).  Burçak et al. (1997)) and horizontal geology section of the study area  In the unit, dolomitic limestone and calcschist interlevels are observed. Crystallized limestones are gray, dark gray, whitish gray in color, generally layered and sometimes blocky in appearance ( Figure 4). Layer thicknesses vary between 10-30 cm. They are mostly coarse and sometimes fine grained. Secondary calcite veins are sometimes observed in crystallized limestones. Dolomitic limestones, which are observed as interlevels in crystallized limestones, are gray-dark gray colored and thin-medium bedded. Layer thicknesses vary between 10-25 cm. Dolomitic limestones are very hard and medium-coarse grained. These metacarbonates are operated as marble and crushed stone. Metacarbonates belonging to Batıbeyli metamorphites contain yellowish greenish gray colored calcschist interlevels. The calcschists have schistosity structure due to the phyllosilicate minerals such as muscovite and chlorite. Especially in metacarbonate levels, overturned and oblique isoclinal folds are observed in some places due to deformation effect. In addition, abundant small scale faults were found in the unit. As a result of these tectonic movements, metacarbonates gained dense fractured structures at vertical and oblique position to bedding.
The calcite crystals are more than 90% in the crystallized limestones ( Figure 5-a). 73-82% calcite and 16-24% dolomite crystals is observed in dolomitic limestones. Calcites, commonly observed in these metacarbonates, are generally xenoblastic, and have highvery high birefringence and distinct duplex cleavage in some crystals. Dolomite crystals observed in dolomitic limestones are generally xenoblastic and sometimes typical with romboeder appearance. Quartz and muscovite crystals in metacarbonates are observed in minor ratios (1% quartz, 1% muscovite).
Calcites, which constitutes the main component of the calcschists, are 52 -65% in these rocks. The muscovites (15-24%) observed in the calc-schists are platy-shaped and show flat extinct. Chlorites, which are observed as 12-18%, are leafy-platy-shaped, green colored and probably in "ripidolite-picnochlorite" composition. Muscovite and chlorite elongated in one direction within the calcschists gave these rocks a granolepidoblastic texture ( Figure 5-b). Batıbeyli metamorphites, which form the basis of the study area, show dense folds due to their intense deformation effects. That the unit form the basis and it shows folded structure complicate to give real thickness to the formation. On the other hand, when the outcrops in the study area of the unit and tectonic structures (folds) of the metacarbonates take into account, the formation presents a visible thickness of approximately 400 m. Batıbeyli metamorphites, whose bottom surface cannot be observed in the study area, are unconformably overlain stratigraphically by Alibonca formation (Figures 2 and 3). The unit is unconformably overlain by Sekirdağ volcanites and Dalören ignimbrites belonging to the Hamur volcanites in the southwest of the study area ( Figure 2). Batıbeyli metamorphites are Paleozoic aged according to Çakır (1994). Batıbeyli metamorphites show comparable properties with the metacarbonate levels of the Akdağ metamorphites outcropping in Patnos (Ağrı) and Malazgirt (Muş) vicinities.

Alibonca Formation
Conglomerates (Boyalan conglomerate member) are observed at the lower levels of this formation. Higher up trachandesitic tuffs and agglomerates (Kuşburnu pyroclastic member) take place in lateral-vertical transition. At the top, crystallized limestones and dolomitic limestones (Taşbasamak limestone member) are observed by lateral-vertical transition ( Figure 3). Alibonca formation was first named by İlker (1966). This researcher states that the Alibonca formation consists of conglomerate, mudstone, sandstone, siltstone, marl, clayey limestone, gypsum and pyroclastic rocks.

Boyalan Conglomerate Member
The unit is made up of conglomerates. It was named as Boyalan conglomerate member within Alibonca formation in relation to Boyalan Village in the northeast of the study area where typical outcrops are observed. The unit is observed particularly in the vicinities of Boyalan Village, the nort of Davut Village, Geleref Hill and Taşkesen Village in the east the examination area (Figures 2  and 6).
Boyalan conglomerate member consists of reddish-yellowish burgundy colored conglomerates. The sandstone and mudstone interlevels are observed sometimes within the unit. Marble, schist, chert and tuff pebbles are seen in the conglomerates. The pebbles are generally semi-angular and semi-round, and the grain sizes of pebbles are quite variable. Conglomerates show medium-thick bedding and medium-good grading ( Figure 6). They contain material ranging from mud size to large block size. The matrix of the conglomerates generally consist of carbonates. The sandstone levels in the unit are medium bedded, and the layer thicknesses of these levels vary between 5-10 cm. The lamination and cross stratification are prominent in sandstones.

Figure 6. Conglomerates belonging to the Boyalan conglomerate member observed around Boyalan Village
In the conglomerate sample taken from Boyalan conglomerate member, the grains are formed from chert fragments, crystallized limestone pebbles and magmatic rock pebbles (Figure 7-a). In this rock containing carbonate matrix, the ratio of matrix is more than 1%. The grains are round and close to the round. Since the pebbles in this conglomerate come from outside the deposition basin, they are named as "epiclastic conglomerate". The naming according to textures of conglomerates is "paraconglomerate". That the grains which form conglomerate are very different indicate to "polymictic conglomerate". They was named as "extraformational conglomerate" according to the origin of the grains.
Boyalan conglomerate member shows similar features with Yastıktepe formation which defined in Karayazı (Erzurum) region by Sümengen (2009a) and with conglomerate-mudstone levels of Alibonca formation which defined in Bulanık (Muş) region by Sümengen (2009a). Upper Miocen age was given to Yastıktepe formation according to stratigraphic position of this formation and Ostragod fossils, such as Cordona angulata, Ilyocypris bradyi and Cyprinotus salinus, by Sümengen (2009a).

Kuşburnu Pyroclastic Member
The unit is composed of tuffs and agglomerates in trachyandesitic composition. It was named as Kuşburnu pyroclastic member in Alibonca formation since it was observed typically in Kuşburnu village vicinity. It is also observed in the western and eastern parts of Davut Village, in the Davut Thermal Spring, Tazekent Thermal Spring and Yılanlı Thermal Spring vicinities and on the eastern and western slopes of Harabe Ridge ( Figure 2).
The tuffs, tuffites and agglomerates which are light grayyellowish colored and in trachyandesitic composition are observed in Kuşburnu pyroclastic member ( Figure 8). The tuffs are easy dispersible feature. The tuffites show good bedding and bed thickness vary. Disseminated pyritic zones are observed within the unit. It is seen that these pyrite turn sometimes into limonite at alteration result.

Figure 8. A view from the tuffs belonging to Kuşburnu pyroclastic member observed in the vicinity of Kuşburnu Village
The tuffs and tuffites were formed by fusion of ash and lapilli grains. Gray colored quartz, whitish colored plagioclase, whitish gray colored and shiny looking sanidine and black -brown colored -platy-shaped biotite are observed in these rocks. In addition, these rocks have a fine-grained phase (matrix) which can not be seen by eye in macro samples. These rocks are composed of different grain sizes and show porphyritic texture.
Agglomerates were formed by attaching with a matrix composed of a volcanic material of volcanic rock fragments which are pebble-block size. The volcanic matrix consists of ash-sized materials. Within the agglomerates, the volcanic material which is observed in block size consists of trachyandesites. These trachyandesites are graydark gray in color and consist of plagioclase, sanidine, biotite, hornblende, pyroxene phenocrystals and matrix. These rocks show porphyritic texture.
The tuffs belonging to Kuşburnu pyroclastic member contain quartz, plagioclase, sanidine, clinopyroxene (diopside/augite), biotite, amphibole (hornblende), sphene, opaque mineral in the phenocrystalline phase and volcanic glass in matrix phase and also lithic fragments. The components, grain sizes and classifications of tuffs belonging to Kuşburnu pyroclastic member are shown in Table 1.

According to Glass-Crystals-Litic Fragments Composition
The grain size of two tuff samples is mostly between 2-64 mm and the grain size of one tuff sample is mostly < 2 mm belonging to Kuşburnu pyroclastic member (Table 1). Therefore, these rocks are defined as "lapillistone" and "ash tuff " when they are evaluated in grain size classification diagram of pyroclasts of Schmid (1981). These rocks are in "trachyandesite" composition according to chemical analysis results (Kansun and Üçgün, 2019) and mineralogical compositions of these. When these tuffs are evaluated in the triangular diagram of Le Maitre (2005) according to percentage distribution of grains in pyroclastic rocks, they are named as "lapillistone", "ash tuff " and "lapilli tuff" (Figure 9-a). The tuffs are seen in "vitric tuff" area in glass-crystals-lithic fragments diagram (Pettijohn et al., 1987) (Figure 9-b). Figure 9. Classification diagrams according to percentage distribution of grains (a) and according to glass-crystals-lithic fragments composition (b) for the tuffs belonging to Kuşburnu pyroclastic member. Diagram a was gotten from Le Maitre (2005), and Diagram b was gotten from Pettijohn et al. (1987) Plagioclases observed in tuffs are generally long prismatic and sub-idiomorphic. Plagioclases show polysynthetic and albitekarlsbad twins. Sanidins typically have karlsbad twins and low angle oblique extinction. Sericitization is observed in places in these feldspar. Biotites which are mafic mineral observed in tuffs are brown colored and platy-shaped (Figures 10-a and b). Clinopyroxenes are very pale green colored and prismatic shaped and show oblique extinction at 45 o -48 o angle. With these properties, it is thought to have diopside / augite composition of these clinopyroxenes. Amphiboles, which are another mafic mineral in tuffs, are brown colored and show oblique extinction 24 o -27 o angle and generally long prismatic shape. Amphiboles are probably in hornblende composition. Oxidation in biotites and hornblendes and opacitization in clinopyroxenes and hornblendes are observed. Volcanic rock fragments form to rock fragments in the tuffs (Figures 10-c and d). Tuffs consisting of phenocrystals, volcanic glass and rock fragments show porphyritic texture (Figure 10). Since the matrix in the tuffs consists entirely of volcanic glass, the tuffs have also of vitrophyric porphyritic texture. Kuşburnu pyroclastic member shows an apparent thickness of 200-250 m in the study area. The member shows lateral-vertical transition with Boyalan conglomerate member belonging to Alibonca formation from below. It is overlain stratigraphically with a lateral-vertical transition by Taşbasamak limestone member belonging to Alibonca formation ( Figure 3). The unit is cut by alkali basalts belonging to Tutak volcanites in Harabe Ridge vicinity in the northeast of the study area. The unit is unconformably covered by Kale pyroclastics in Kale Hill vicinity in the east of the study area ( Figure 2).

Taşbasamak Limestone Member
The unit consists of lacustrine limestone, dolomite and dolomitic limestone. It is named as Taşbasamak limestone member within the Alibonca formation, since it is observed typically in Taşbasamak Village vicinity in north of the study area.
The unit deposited in lacustrine environment starts with sandy limestone, marl, dolomite and dolomitic limestone which contain white, gray, bluish gray chert interlevels at the lower levels. Higher up, It passes to white, light gray colored limestone and gray, yellowish gray, pinkish colored and thin-middle bedded limestone and dolomitic limestones ( In the dolomitic limestone sample taken from the Taşbasamak limestone member; micrite (76%), sparite (10%) and fossil shells (14%) are observed (Figure 11-a). The rock was formed by attaching allokems (fragments of the fossil shells) with a micritic matrix. A small amount of sparite greater than 10 microns is also present in the rock. It was found that 65% of micrites and sparites was calcite and 35% of these was dolomite crystals. Neomorphism is observed in the rock. As a result of the neomorphism, the fossil shells were dissolved and they filled with sparite again (Figure 11-a). The grain sizes of the shell fragments in the rock vary from thin to large (Figure 11-a). Sparite crystals in the rock are anhedral and show very high birefringence. In some sparite crystals, bi-directional oblique cleavages are evident. The rock show cracked stucture. These cracks developed in several directions. The cracks were subsequently filled by the secondary sparite. This rock, which is named as "dolomitic limestone" in the macro observations, is named as "biomicrite" according to the limestone classification of Folk (1962) considering the above mentioned components in micro (thin section) observations. Since fossils more than 10% are observed in the rock, it can be named as "wackestone" according to the classification of Dunham (1962).
As a result of the thin section study made from another limestone sample taken from Taşbasamak limestone member; sparite (50%), skeletal grain (17%), micrite (25%) and pellet (8%) were observed in the rock. This rock was named as "wackstone" according to Dunham (1962), and as "pel-biosparite" according to Folk (1962) (Figure 11-b). Taşbasamak limestone member presents comparable features to clayey limestone and marl levels of Upper Miocene aged Alibonca formation in the vicinities of Patnos (Ağrı) and Malazgirt (Muş) (Sümengen, 2009b). In the study area, Taşbasamak limestone member belonging to Alibonca formation shows lateralvertical transition with Upper Miocene aged Kuşburnu pyroclastic member belonging to the same formation ( Figure 3). Therefore, the age of Taşbasamak limestone member is Upper Miocene.

Sekirdağ Volcanites
The unit is composed of dacitic and rhyodacitic tuff, agromera and sometimes lava levels. The unit was first named as Sekirdağ volcanites by Türkecan et al. (1992a) according to typical outcrops in Sekirdağ vicinity observed in south of Eleşkirt (Ağrı). Sekirdağ volcanites is observed in vicinities of Günbuldu Village, Altınkilit Village, Dibekli Village, Ulukent Village, Yukarı Dalören Village, Dim Hill, Mağara Hill, Kır Hill and Hari Hill in the sudy area ( Figure 2). Sekirdağ volcanites are composed of whitish light gray colored dacitic-rhyodacitic pyroclastics and dark gray-gray colored dacitic-rhyodacitic lavas (Figure 12). Lava levels are observed in the upper levels of Sekirdağ volcanites. Pyroclastic precipitated from time to time in a water-containing environment. The majority of pyroclastic are agglomerates. Tuffs were formed by fusing ash and lapilli sized grains. The rock fragments of dacites and trachyandesites are common in tuffs. Plagioclase, quartz, sanidine and biotite phenocrysts are prominent in some tuff samples. Volcanic glass forms the fine grained section of the tuffs. The agglomerates were formed by attaching with a volcanic matrix which had ash size of the dacite and trachyandesite rock fragments in the size of gravel and block. The dacitic-rhyodacitic lavas observed in the upper levels of Sekirdağ volcanites are dark gray-gray colored and the flow structures are particularly prominent in the dacitic levels. These rocks, which are characterized by porphyritic textures, are generally thin and rarely medium grained. Quartz, plagioclase, sanidine, hornblende and biotite phenocrysts can be distinguished in these rocks. The tuffs belonging to Sekirdağ volcanites contain quartz, plagioclase, sanidine, biotite, amphibole (hornblende), opaque mineral in phenocrystal phase and volcanic glass in matrix phase and also litic fragments. The dacitic and rhyodacitic lavas belonging to Sekirdağ volcanites contain quartz, plagioclase, sanidine, biotite, amphibole (hornblende), opaque mineral in the phenocrystal phase and plagioclase microliths and volcanic glass in matrix phase. Tuffs show vitrophyric porphyritic texture, and lavas show hypocrystalline porphyritic texture. The components, grain sizes and classifications of tuffs and lavas belonging to Sekirdağ volcanites are shown in Table 2.

According to Glass-Crystals-Litic Fragments Composition
The grain size of one tuff sample which is examined belonging to Sekirdağ volcanites is mostly between 2-64 mm and the grain size of the other tuff sample which is examined is mostly < 2 mm (Table 2). Therefore, these rocks are defined as "lapillistone" and "ash tuff" when they are classified in the grain size classification diagram of the pyroclasts of Schmid (1981). When the chemical analysis results (Kansun and Üçgün, 2019) and the mineralogical compositions (Table 2) in Q-A-P-F diagram (Streckeisen, 1967) of these tuffs are considered, these are "rhyodacite" and "dacite". When these tuffs are examined in the classification diagram according to percentage distribution of grains in pyroclastic rocks of Le Maitre (2005), they are named as "lapillistone" and "ash tuff" (Figure  13-a). Tuffs are seen as "vitric tuff" in glass-crystals-lithic fragments diagram (Pettijohn et al., 1987) (Figure 13-b). When the analysis results (Kansun and Üçgün, 2019) and the mineralogical compositions in Q-A-P-F diagram (Streckeisen, 1967) of the lavas are considered, these lavas are "dacite" and "rhyodacite" (Table 2).

Figure 13. The classification diagrams according to percentage distribution of grains (a) and according to composition of glasscrystals-lithic fragments (b) for the tuffs belonging to Sekirdağ volcanites. Diagram a was gotten from Le Maitre (2005), and Diagram b was gotten from Pettijohn et al. (1987)
The quartzs observed in tuffs and lavas are xenomorphic (Figure 14-a). Plagioclases, which are generally sub-idiomorphic, show typically polysynthetic twins and zoned structures (Figures 14-c and d). The plagioclases in dacitic-rhyodacitic lavas are in oligoclase (Ab75An25, Ab78An22) and andesine (Ab66An34, Ab52An48) compositions. Sanidines which are other felsic mineral show typical prismatic form, karlsbad twin and low angle oblique extinction. The biotites in these rocks are brown colored and platy-shaped. The amphiboles are brown colored and show oblique extinction at low angle and prismatic shape (Figures 14-c and d). These amphiboles are in hornblende composition. Amphiboles and biotites which are observed in especially tuffs and in rarely lavas are commonly opacited and oxidized (Figure 14-b). Volcanic rock fragments rock fragments form in tuffs (Figure 14-c). The age of the unit was found as 11.2 ± 1.5 Ma according to the age determinations made from the agglomerates belonging to Sekirdağ volcanites in Eleşkirt-Horasan vicinity (Ercan et al., 1990). Therefore, the age of Sekirdağ volcanites is Upper Miocene.

Solhan Volcanites
The unit is mainly composed of alkali basalts. These basalts are called as Solhan volcanites by Yılmaz et al. (1987a) according to the their typical outcrops in Solhan (Bingöl) region. The unit is seen in the vicinity of Korkuluk Hill and in the northern part of the Ulukent Village in the central and southwestern parts of the study area ( Figure 2).
The unit consists of alkali basalts, which are dark gray-black colored and brown alteration colored and show columnar blocks and occasional gas voids. These basaltic lavas were generally formed by cleft eruption and flowed as plateau lavas. They usually show a massive structure in macro samples. These basalts shows a porous structure at the levels where pores which are formed due to gas outlets are more. They are generally fine grained. Plagioclase phenocrysts are sometimes observed as slats in these basalts. Therefore, the basalts show aphanitic porphyritic texture. In some outcrops of alkaline basalts in the study area, columnar block structures are quite characteristic.
Alkali basalts belonging to Solhan volcanites contain quartz, olivine, clinopyroxene (diopside/augite), apatite, opaque mineral in phenocrystal phase and plagioclase microliths in matrix phase. The components, percentage values of the components and rock names of these components of the alkali basalts are shown in Table 3. The basalts belonging to Solhan volcanites are fine grained. The matrix which is formed from plagioclase microlites is commonly observed in basalts ( Figure 15). Phenocrystalline phase of these rocks is less than 20%. Plagioclase, olivine and clinoproxen form phenocrystal phase. Plagioclases show generally long prismatic shape, polysynthetickarlsbad twin and distinct zoned structure. These plagioclases are in andesine (Ab55An45, Ab52An48) and labrador (Ab37An63, Ab40An60) compositions. Olivines show characteristically prismatic -sub-idiomorpic shapes, colorless-very pale green colors, cracked structures and flat extinctions ( Figure  15-a). Clinopyroxenes generally have long-short prismatic shape and oblique extinction at 42 o -44 o angle. It are thought that these pyroxenes, which are very pale green colored, are in diopside/augite composition. The olivines and pyroxenes are observed both in phenocrystalline phase and in matrix phase in basalts (Figure 15-b). These basalts whose matrix are composed of only microliths show holocrystalline porphyritic texture. In some basalts, the microlites extend in one direction and give these rocks a trachytic texture. The porous structure was also found in basalts. Some pores are filled with secondary carbonate minerals. In the study area, the rocks belonging to Solhan volcanites were named as olivine basalt "and pyroxene basalt" according to their mineralogical composition (Table 3). According to chemical analysis values (Kansun and Üçgün, 2019), these rocks are in "alkaline basalt" composition.  Figure  2). In the study area, Solhan volcanites cover Upper Miocene clastic, carbonated and pyrolastic-volcanic rocks. Akay and Türkecan (1990) and Türkecan et al. (1992b) sayed that the age of the unit was 4.3 ± 0.8 Ma, 4.4 ± 1.3 Ma and 6.0 ± 0.6 Ma according to the radiometric age analysis which are made from Solhan volcanites in Solhan (Muş) vicinity. Therefore, the age of Solhan volcanites is Lower Pliocene.

Hamur Volcanites
Hamur volcanites were named by Türkecan et al. (1992a) and Türkecan et al. (1992b). Hamur volcanites were investigated by dividing into two members as Tazekent trachyandesite member and Dalören ignimbirite member from bottom to top in the study area (Figure 3).

Tazekent Trachyandesite Member
The unit is composed of trachyandesites. These trachyandesites are named as Tazekent trachyandesite members due to their outcrops in south of Tazekent Village where they are typically observed. The unit is observed in Keçikıran Hill vicinity in south of Tazekent Village (Figure 2).
Trachyandesites are gray-dark gray-brownish colored (Figure 16). They are observed as lava flows and domes in the study area. The sizes sanidine and plagioclase phenocrysts in the rocks reach up to 1 cm. These rocks are characterized by their hard structures, fine grains and massive appearances. The gas gaps are rarely seen in trachyandesites observed at the upper levels of the member.  Table 4. The trachyandesites are fine grained and contain small amounts of phenocrysts. The matrix phase in these rocks is around 80%. The matrix phase of these rocks consists of plagioclase and sanidine microliths (Figure 17). Plagioclases in phenocrystalline phase are mostly zoned, twinning and long prismatic (Figure 17-a). Plagioclases are in composition of oligoclase (Ab73An27) and andezine (Ab58An42, Ab62An38). Sanidines show a very pronounced karlsbad twin and a prismatic shape (Figure 17-b). The mafic minerals in the rocks are generally small amounts in matrix phase. Amphiboles from these mafic minerals show brown color and long prismatic shape. Amphiboles are probably in hornblende composition. Clinopyroxenes, which are colorless-very pale green colored, show prismatic shape and oblique extinction between 43 o -47 o . Clinopyroxenes are probably in diopside/augite composition according to these properties. Oxidation and carbonation are observed in trachyandesites. Carbonation is observed in plagioclases and amphiboles in matrix and phenocrystalline phase. Oxidation is observed in mafic minerals. The trachyandesites show holocrystalline porphyritic texture ( Figure 17). Some trachyandesite samples also show trachytic texture. The rocks belonging to tazekent trachyandesite member are in "trachyandesite" composition both according to their chemical analysis values (Kansun and Üçgün, 2019) and according to their mineralogical compositions (Table 4). Tazekent trachyandesite member has an apparent thickness of approximately 30 m in the study area. This unit, which is observed stratigraphically on Sekirdağ volcanites (Figure 3), cuts out Sekirdağ volcanites in the study area (Figure 2). The unit is covered by Dalören ignimbirite member belonging to Hamur volcanites. Innocenti et al. (1980) sayed that the age of lavas belonging to Hamur volcanites was 5.6 ± 0.3 Ma and 5.1 ± 0.2 Ma. Therefore, the age of Tazekent trachyandesite member is Lower Pliocene.

Dalören Ignimbrite Member
The unit contains ignimbrites. These ignimbrites are observed in Yukarı Dalören Village and Mağara Hill vicinities, north of Günbuldu Village, west of Dibekli Village and northwest of Taşbasamak Village in the sudy area (Figures 2 and 18).

Figure 18. The view from the ignimbrites belonging to Dalören ignimbirite member (Nhd) and the tuffs belonging to Sekirdağ volcanites (Nse) observed southwest of Dibekli Village
The ignimbrites are brown-black colored, and show fiamme structure. These ignimbrites show lateral-vertical transition with trachyandesitic lavas which are gray-brown colored and contain rarely gas gaps. The ignimbrites consist of grains of ash and lapilli size. Fiamme structures in the ignimbrites are dark brown-black colored and lenticular. Pumice fragments form fiamme structures. In the study area, ignimbrites flowed over a large area. The upper surfaces of the ignimbrites are plateau-shaped and the lower surfaces of these conform to the morphology. Plagioclase, sanidine, hornblende and proxene phenocrysts are observed in some ignimbrite samples. They have porphyritic texture.
When we look at the thin section samples of ignimbirites, plagioclase (5%), hornblende (4%), clinopyroxen (4%), sanidine (2%), pumice fragments (8%), litic fragments (7%) and matrix which contain volcanic glass (70%) are observed (Figure 19). The rock fragments are composed of volcanic, pyroclastic and metamorphic rock fragments. Very prominent flowing texture is observed in these rocks. The ignimbrites have vitrophyric porphyritic texture. Plagioclases in the ignimbrites show zoned structure, albite twinning and long prismatic shape. Sanidines are characterized by karlsbad twin and oblique extinction at low angle. The hornblendes show prismatic shape and brown color. Clinopyroxenes show prismatic shape and colorless-very pale green color. Pumice parts are observed as generally ellipsoidal grains extending in one direction (Figure 19). The ignimbrites have the andesite/trachyandesite composition according to their mineralogical compositions.

Figure 19. Pumice parts (Pm) and litic fragment (Lf) observed in ignimbirite belonging to Dalören ignimbirite member, / Nicol
Dalören ignimbirit member shows the visible thickness of approximately 20 m in the study area. Dalören ignimbirit member stratigraphically covers Tazekent trachyandesite member belonging to Hamur volcanites from the bottom and is overlain unconformably by Kale pyroclastics at the top (Figure 3). Dalören ignimbirite member is observed on Boyalan conglomerate member belonging to Alibonca formation, Sekirdağ volcanites and Solhan volcanites in the study area (Figures 2 and 18). Innocenti et al. (1980) determined that the age of ignimbrites belonging to Hamur volcanites was 5.2±0.2 Ma. Accordingly, the age of Dalören ignimbirit member is Lower Pliocene.

Kale Pyroclastics
The pyroclatics consist of lapilli tuff, ash, volcanic bomb, basaltic slag and agglomerate in alkaline basalt composition. These lithologies were named as Kale pyroclastics, referring to Kale Hill where typically was observed in the east of the study area. This unit was named as "pyroclastics" by Aydoğan (2000) which studied in the investigation area and as "Tutak volcanites" by Sümengen (2009b) which studied in Patnos (Ağrı) -Malazgirt (Muş) and Bulanık (Muş) vicinities. Sümengen (2009b) specified that Upper Pliocene -Pleistocene aged Tutak volcanites are composed of basalt, hawaiite and benmorite lavas which contained sometimes slag. In this study, seperation of the pyroklastics and basalts, which were lithologies which Sümengen (2009a) was named as "Tutak volcanites" was done. The pyroklastics were named as "Kale pyroclastics", and basaltic lavas were named as "Tutak volcanites". Kale pyroclastics are observed in Kale Hill and its vicinity in the east of the study area ( Figure 2).
The unit is composed of dark graybrownish colored lapilli tuff, ash, volcanic bomb, slag and agglomerate in alkaline basalt composition ( Figure 20). Lapilli tuffs are easily dispersed and have porphyritic texture. Plagioclase and pyroxene phenocrysts in the these tuffs are sometimes prominent. The fine grained section of lapilli tuffs forms from the matrix. Volcanic bombs are in basaltic composition. They are very hard structured and have a diameter of up to 20 cm. The slags are black colored and very light and have plenty pore and a irregular surface. The slags are composed of pyrolastic grains at lapilli and block sizes. The tuffs belonging to Kale pyroclastics include plagioclase, clinopyroxene (diopside/augite), olivine, opaque mineral in phenocrystalline phase, volcanic glass in matrix phase and also litic fragments. The agglomerates belonging to Kale pyroclastics include plagioclase, olivine, clinopyroxene (diopside/augite), orthopyroxene (enstatite), apatite, opaque mineral in phenocrystalline phase, volcanic glass in matrix phase and also litic fragments. Tuffs and agglomerates show vitrophyric porphyritic texture. The components, grain sizes and classifications of tuffs and agglomerates belonging to Kale pyroclastics are shown in Table 5.  Türkecan et al. (1992a) determined that the age of the Tutak volcanites, which consisted of pyroclastic and lavas and which were observed in Tutak (Van) vicinity, was Upper Pliocene -Pleistocene. In addition, Sanver (1968), which studied Hamur (Ağrı) vicinity, and Innocenti et al. (1980), which studied Patnos (Ağrı), specified that the age of the basaltic lavas observed together with these pyroclastics was Upper Pliocene -Pleistocene according to the radiometric age determinations. Therefore, the age of the Kale pyroclastics is Upper Pliocene -Pleistocene.

Tutak Volcanites
They consist of alkaline basalts which show columnar structure and flow structure. Türkecan et al. (1992a), which studied in Tutak (Van) vicinity, were named as "Tutak volcanites" to the lithologies which consisted of basalt, hawaiite and mugearite. Later, Sümengen (2009a and2009b) , which studied in Patnos (Ağrı) -Malazgirt (Muş) and Bulanık (Muş) vicinities, were defined as "Tutak volcanites" to the rocks which consisted of basalt, hawaiite and benmorite lavas which contained slag. The seperation of pyroclastics and basalts, which were named as "Tutak volcanites" by Sümengen (2009aSümengen ( ve 2009b, was done in this study. In the study, the pyroclastics were named as "Kale pyroclastics", and the basaltic lavas were named as "Tutak volcanites" adhering to the first nomenclature of Türkecan et al. (1992a). Tutak volcanites are located in the vicinities of Değirmen Ridge and Harabe Ridge in the northeast of the study area ( Figure 2).
Tutak volcanites are composed of gray-black-reddish colored alkaline basalts, and these basalts show column structure ( Figure  22). Also, they is observed as lava flows in the study area. The basalts is generally fine grained and porous. Plagioclase, olivine and pyroxene phenocrysts rarely distinguish in macro samples. The fine grained sections of these rocks are formed from matrix. The basalts show aphanitic porphyritic texture.  Table 6. Basalts are fine grained and phenocrystals in these are small amount. The matrix formed by plagioclase microlites is commonly observed in the basalts (Figure 23). The phenocrystals rarely observed in basalts are plagioclase, olivine and proxen. Plagioclases, characterized by their prismatic form, show polysynthetickarlsbad twins and mostly zoned structure. Plagioclases are in andesine (Ab59An41, Ab62An38) and labrador (Ab48An52, Ab43An57) compositions according to the extinction angle determination of these. Olivines observed in the basalts are mostly observed as small size crystals (Figure 23-a). Olivines are prismatic shaped, sometimes cracked and colorless-very pale green colored. Clinopyroxenes are observed as prismatic and sub-idiomorphic crystals. They show angled extinction between 45 o -47 o . It is thought that the colorlessvery pale green colored clinopyroxenes are in "diopside/augite" composition. Orthopyroxenes are typical with flat extinction, whitish pale green colors and prismatic shapes (Figure 23-b). Orthopyroxenes are probably in "enstatite" composition according to these properties. The pyroxenes observed in the basalts are mostly observed as small size crystals (Figure 23-d). The basalts have holocrystalline porphyritic and trachytic textures.
The rocks belonging to Tutak volcanites according to chemical analysis values (Kansun and Üçgün, 2019) are in "alkaline basalt" composition. In the Q-A-P-F diagram (Streckeisen, 1967), these rocks were named as "olivine basalt" according to their mineralogical compositions (Table 6).  (Figure 3). Tutak volcanites are unconformably observed on Boyalan and Kuşburnu pyroclastic members belonging to Alibonca formation to northeast of the study area ( Figure 2). Sanver (1968) determined that the age of basaltic lavas, which were located in Hamur (Ağrı) vicinity, were 1.07 ± 0.12 Ma. Innocenti et al. (1980) sayed that the age of basaltic lavas belonging to Tutak volcanites, which are observed in northeast of Karabulak Village (Patnos-Ağrı), was 2.0 ± 0.1 Ma and that the age of basaltic lavas belonging to Tutak volcanites, which are observed in Gülkoru (Malazgirt-Muş) vicinity, was 3.9 ± 0.4 Ma. Therefore, the age of Tutak volcanites is Upper Pliocene -Pleistocene.

Travertine
Travertines is carbonated rocks, which are deposited by carbonated spring waters and show sometimes bedding. Travertines are observed the vicinities of Köprü Thermal Spring, Yılanlı Thermal Spring, Davut Thermal Spring, Tazekent Thermal Spring, Hocayurdu Hill, Ali Hill and Ulukent Village in the study area (Figures 2 and 24). They have a visible thickness of about 30 m. The age of the travertines is Holocene (Quaternary).

Discussion
The aim of this study is to determine the stratigraphic and petrographic properties of the units which are commonly made of volcanicpyroclastic rocks and outcrops in the region including Diyadin geothermal field. Keskin (1998) and Pasvanoğlu (2013) stated that the Upper Miocene aged lithologies consisted of pyroclastics, lavas, ignimbrites and lacustrine sediments in the region. On the other hand, carbonated-clastic rocks and trachyandesitic tuffs-agglomerates (Alibonca formation) and dacitic-rhyodacitic tuffsagglomerates-lavas (Sekirdağ volcanites) are Upper Miocene aged in the study area. The ignimbrites belonging to Hamur volcanites are Lower Pliocene aged and cover unconformably to Upper Miocene lithologies. Pasvanoğlu (2013) stated that glassy textured basalts and andesitic-dacitic tuffs were deposited on Upper Miocene aged lacustrine limestones. In this study, it was found that dacitic-rhyodacitic tuffs and agglomerates were deposited by lateral-vertical transitions on the lacustrine limestones forming the Taşbasamak limestone member and that these units were cut by the Lower Pliocene aged alkaline basaltic lavas (Solhan volcanites). Pasvanoğlu (2013) stated that the lavas, which are stratigraphically related to pper Miocene aged ignimbrites, are in andesite composition. This researcher also sayed that the basalts overlying these are covered by pyroclastics which consisted of volcanic bombs, lapilli and volcanic ash. In contrast, these lavas that Pasvanoğlu (2013) specified are in trachyandesite composition and are Lower Pliocene aged. The Pyroclastics (Kale proklastics), which are composed of, lapilli tuff, ash, volcanic bomb, slag and agglomerate in alkaline basalt composition, are covered by alkaline basaltic lavas (Tutak volcanites) in the region.

Conclusions
Paleozoic and Cenozoic aged lithologies take part in the study area. Paleozoic aged Batıbeyli metamorphites are observed at the base of the study area. Batıbeyli metamorphites are composed of crystallized limestones containing calcschist interlevels. The Upper Miocene aged Alibonca formation is unconformably observed on these metamorphites. Alibonca formation consists of conglomerates (Boyalan conglomerate member) at the base, on these, of tuffs and agglomerates in trachyandesitic composition (Kuşburnu pyroclastic member). The sandy limestone-marl-dolomite-dolomitic limestone-lacustrine limestone-limestone which contain chert interlevels are observed at upper levels of Alibonca formation. Upper Miocene aged Sekirdağ volcanites are observed with lateral-vertical transition on Alibonca formation. These volcanites consist of daciticrhyodacitic tuffs, agglomerates and lavas. Towards up, Lower Pliocene aged Solhan volcanites, which are composed of alkaline basaltic lavas, are observed. Solhan volcanites are covered by Upper Pliocene aged Hamur volcanites. Hamur volcanites are composed of trachyandesites (Tazekent trachyandesite member) at the base and ignimbrites (Dalören ignimbrite member) covering these trachyandesites. Towards up, Upper Pliocene-Pleistocene aged Kale pyroclastics consisting of lapilli tuff, ash, volcanic bomb, slag and agglomerate and being in alkaline basalt composition are observed. Kale pyroclastics are covered by Upper Pliocene-Pleistocene aged Tutak volcanites, which show columnar block structure and flow structure and are in alkaline basalt composition. At the top, travertine and alluvium are found.
The tuffs belonging to Sekirdağ volcanites contain quartz, plagioclase, sanidine, biotite, amphibole (hornblende), opaque mineral in phenocrystalline phase, volcanic glass in matrix phase and also litic fragments. The dacitic and rhyodacitic lavas belonging to these volcanites contain quartz, plagioclase, sanidine, biotite, amphibole (hornblende), opaque mineral in phenocrystalline phase and plagioclase microliths and volcanic glass in matrix phase. The tuffs of Sekirdağ volcanites have been named as lapillistone and ash tuf "according to grain size", as rhyodacitic tuff and dacitic tuff "according to composition and grain size", as lapillistone and ash tuff "according to percentage distribution of grains" and as vitric tuff "according to glass-crystals-lithic fragments components".
The tuffs belonging to Kale pyroclastics contain plagioclase, clinopyroxene (diopside/augite), olivine, opaque mineral in phenocrystalline phase, volcanic glass in matrix phase and also litic fragments. The agglomerates belonging to Kale pyroclastics include plagioclase, olivine, clinopyroxene (diopside/augite), orthopyroxene (enstatite), apatite, opaque mineral in phenocrystalline phase, volcanic glass in matrix phase and also lithic fragments. These tuffs have been named as lapillistone "according to grain size", as basaltic tuff "according to composition and grain size", as lapilli tuff "according to percentage distribution of grains" and as vitric tuff "according to glass-crystals-lithic fragments compositions". The agglomerate in basaltic agglomerate composition "according to composition and grain size". The alkaline basalts belonging to Tutak volcanites contain plagioclase, olivine, clinopyroxene (diopside/augite), orthopyroxene (enstatite), apatite, opaque mineral in phenocrystalline phase and plagioclase microliths in matrix phase.

Acknowledge
This study was prepared by using the project numbered 10201138 supported by Selçuk University Scientific Research Projects Coordination Unit.