Mantle peridotites are one of the most important rock units of Jandaq ophiolite that are affected by numerous phases of dynamic and static serpentinization, and metamorphism. The main part of mantle peridotites is lherzolite. This ophiolitic association is covered by Paleozoic metamorphic rocks that are schist and marble. All olivines are changed to serpentine. Most of orthopyroxenes are bastitized and some of clinopyroxenes are changed to tremolite by metamorphism. Clinopyroxenes are the most resistant mineral against the metamorphism and alteration. Most of spinels are magnetitized, but in some cases the inner parts are fresh. Composition of chromian-spinels are the same in all mantle peridotites with Cr# = 0.46. Gabbros that intruded the peridotites are rodingitized. Peridotites of Jandaq ophiolite are abyssal peridotites that belong to spinellherzolite facies. Crystallization temperature of pyroxenes in lherzolites ranges from 1041 to 1178°C. One of the most characteristics of these peridotites is absence of chromitite that relates to lherzolitic system of mantle, low degree of partial melting, low activity of mantle in continual ascending melt production, and low Cr content of pyroxenes.

In north of Chah Zard farm, Jandaq metamorphic complex contains schising and marble underlay the amphibolites. Amphibolites are metamorphosed basalts of Jandaq ophiolite. and Jandaq metamorphic rocks are metasedimentary cover of Jandaq metaophiolite. Ampbibolites contain hornblende, plagioclase, garnet, alkali feldspar (orthoclase), magnetite. biotite. muscovite, sphene and quartz. These rocks present very good lineation and foliation. By metamorphic differentiation. mafic and felsic minerals are seperated in some locations. Mineralogical studies. Hornblende barometry, and hornblende - plagioclase thermometry, conclude the metamorphism of these rocks under upper part of amphibolite facies (7.10 to 9.91 Kbars and 619 to 650°C). Presence of actinolite, epidote and calcite in amphibolites demonstrates a retrograde metamorphism under green schist facies.

Amphibolites are one of the metamorphic rock units of Jandaq ophiolite and exposed in a considerable volume. These rocks are metamorphism products of basalts, pillow lavas and diabasic dikes of Jandaq ophiolite. Amphibolites contain amphibole, plagioclase, garnet, alkali feldspar (orthoclase), magnetite, biotite, muscovite, sphene, quartz, epidote and calcite minerals. These rocks contain very good lineation and foliation. By metamorphic differentiation, mafic and felsic minerals are separated in some locations. Metasediments that are present in Jandaq area were originaly sedimentary cover of Jandaq ophiolite, before the metamorphism has taken place. Mineralogical studies, hornblende barometry, and amphibole – plagioclase thermometry, conclude that the metamorphism of Jandaq ophiolite amphibolites occured in upper part of amphibolite facies condition (7.98 to 9.01 Kbars and 714 to 737oC). Temperature of metamorphism in Jandaq ophiolite amphibolites is higher than amphibolites that are in Jandaq metamorphic rocks (8.58 to 10.87 Kbars and 619 to 668oC).

Jandaq ophiolite suites are covered by metamorphic rocks that are marbles and schists. This old ophiolitic association has passed different phases of serpentinization and metamorphism. In this rock association, gabbroic dikes cross cut the serpentinized mantle peridotites. Joints and cracks of brittle gabbroic dikes are filled by veins that are light in color. These veins are formed after metamorphism and serpentinization. These coarse grain rocks are free from deformation and foliation, and are formed by calcite, prehnite, epidote, clinopyroxene and chlorite. The most important mineralogical characteristic of these veins is existence and considerable amount of calcite, that is the evidence of high f CO2 in minerals bearing fluid. Vein enclosing gabbros, are metamorphosed in amphibolite facies (2.7 to 9 kbar pressure and 630 to 750 of C temperature), and then pass through a retrograde metamorphism in green schist facies.

The Eocene volcanic rocks from the southwest of the Jandaq (Kuh-e-Godar-e-Siah, Central-East Iran microcontinent) are andesitic basalt and andesite in composition. These rocks contain xenoliths with granulitic mineralogy. Mineral assemblage of these xenoliths is plagioclase+phlogopite+corundum+sillimanite+ chlorite+phengite with granublastic, poiklioblastic and foliated textures in the pick metamorphic condition. Thermometry of phlogopite in these xenoliths suggests the average temperature 782oC. The characteristics of the xenoliths are consistent with the granolitic facies metamorphism of the Al-saturated Si-undersaturated crustal sediments at the lower crust condition. Melting of these granulites forms the magma which crystallized the S-type granitoids. Differentiation and crystallization of this magma causes the S-type granite formation. Therefore, the S-type granites in the study area are probably generated from melting of the granulites parts of which brought to the surface as xenoliths by Eocene magmatism in south of the Jandaq (Kuh-e-Godar-e-Siah). S-type granites in the study area are located along the Doruneh, Chupanan and Aeirakan faults in the Aeirakan area and Jandaq ophiolite. These granites are the source of uranium, thorium and uranium ore in southwest of the Aeirakan mountain.

The Khoy ophiolite with Precambrian basement rock is located in north western of Iran.The tectonite peridotites are most formed by clinopyroxene harzburgites. These harzburgites characterized by protogranular, porphyroclastic and transformation textures, and composed of olivine (with kink band), orthopyroxene (with wavy extinction and exsolution clinopyroxene), spinel (like Holly – Leaf and shaped) and less than 10% of clinopyroxene. Two stages of alteration occur in these rocks, including static and dynamic. These peridotites are partial melting residual of spinel lherzolites.The Khoy taconite periodontitis show the U-form pattern in the REEs. These patterns are probably related to the partial melting procedures and the process following the partial melting such as influence of felsic magmas after emplacement of ophiolites.

The Siah-Cheshmeh ophiolites at the north-northwest part of the Khoy ophiolites show a dismembered pile of metamorphic units, mantle sequence, and basaltic-andesitic lavas associated with Late Cretaceous pelagic limestones and cherts. The basaltic-andesitic lavas can be divided into alkaline and calc-alkaline varieties. The presence of Ti-rich amphibole prisms and Ti-bearing clinopyroxenes is characteristic of these lavas. The calc-alkaline lavas are characterized by enrichment in LREE and depletion in HFSE while the alkaline lavas display positive LREE and HFSE anomalies. The interaction between mantle plumes with a spreading center can be considered for generation of alkaline basalts while a subduction zone is responsible for the genesis of calc-alkaline basalts.

Dorouneh Fault is located in the north of Central Iran Microplate with left-lateral strike-slip mechanism and plays an important role in the formation of Iran plateau’s morphology. Dorouneh fault, with bend geometry and 900 km length, extends from Hyrmand River in the Afghanistan border to Anarak area in the Central Iran. Dorouneh Fault terminates in the Jandaq area as sub-parallel branches. Towards west, general trend of Dorouneh Fault System changes from northeast-southwest to north-south in the north of Talmessi Mine. Fault branches are observed as left-lateral strike-slip faults with normal dip-slip component in the Jandaq-Talmessi area that is introduced as a trailing extensional imbricate fan. But, considering slip sense inversion along Dorouneh Fault, the main mechanism for formation of western termination before slip sense inversion is a trailing compressional imbricate fan.

Located on the southern margin of the Dasht-e Kavir desert, the historical city of Jandaq has long served as a significant settlement. During the Qajar period, Jandaq Fortress encompassed approximately one hundred houses of varying sizes, housing the entire population within its walls. The historical fabric of the fortress is characterized by a dense and interconnected ensemble of affluent residences, the Jāmeh Mosque, a public bathhouse, covered passageways (Sābāts), and a labyrinthine network of alleys. The architecture of the fortress and its houses vividly reflects efforts to ensure comfort, security, and resilience against the harsh desert climate and potential external threats. Jandagh Fortress remains inhabited today, with 23 local households residing. Several of the historic houses have been repurposed as ecolodges, while others stand abandoned or partially ruined. This article presents architectural documentation, describes the components and their functions, and analyzes the spatial relationships among prominent houses within the Jandagh Fortress, including the residences of the Yaghmā, Safāyi, Heshmat, Kāfi, Bitaraf, and Mirzā Abdolkarim. Additionally, the article provides an analysis of key architectural elements, including entranceways and bahārband, eywāns, bādgirs, winter quarters, and kitchens (matbax). Through a critical examination of historical records and written sources, and a comparative analysis with similar structures in Yazd and Meybod—regions sharing geographic and socio-political characteristics with Jandaq—this research offers more profound insights into the architectural legacy of the fortress. Based on the surviving architectural evidence and comparative studies, the tradition of settlement within Jandaq Fortress can be traced back to the 8th century AH (14th century CE), during the Muzaffarid dynasty. However, various additions, alterations, functional changes, and periods of abandonment have shaped its present form.

Sabzevar Ophiolite Zone (SOZ) is located in northern Central Iran (north of Great Kavir fault and south of Miamey fault) and separates Kopp e Dagh sedimentary basin (in the north) from the Central Iran plateau (in the South). The evolution and replacement time of this ophiolite complex has been in the Upper Cretaceous) Santonian – Campanian) and the Middle Campanian to Upper Maastrichtian respectively. This ophiolite belt contains a high amount of ultramafic rocks, small masses of gabbros and a thick sequence of submarine basaltic lavas with Upper Cretaceous pelagic limestone and radiolarite, which are angular unconformable and have a base of conglomerates of volcanic and sedimentary rocks. This study examines the brittle structures of SOZ and carries out a geometrical analysis. The purpose of this study is to obtain a suitable structural model consistent with the area structures. In this paper, the geometrical condition is compared with all the area structures and a logical relationship between fractures has been identified. Also the relationship between the regional macro-structures and area fractures has been identified. For this purpose during the field visits and study of the satellite imagery, structures and exposure which make the base of a structural map of the area have been provided.. Then with the surveyed data and provided rose and contour diagrams the main direction of fractures and the pattern of orientation were obtained. This direction is N59W, the same trend as the Miamey fault. The structures in the region are affected by this fault. If this direction is considered the main right-lateral shear trend, other trends are consistent with pattern of fractures orientations Related to fault cutting. Generally the fractures with N14E, N68E, N86E, N77W, N59W and N41W trend, respectively are consistent with type X, R', T, R, D and P fractures.