1300:
1758:
19:
907:(e.g., Alborz, East of Iran, Zagros). There is strong stratigraphic evidence that transition from Vendian to Lower Cambrian was a progressive one, without hiatuses; there is no evidence for any orogenic or epeirogenic movements in Iran at this time (e.g., south of Zanjan, Valiabad Chalus, Shahin Dezh). Early Cambrian started with an alternation of shale, phosphate-bearing limestone, and dolomite sitting conformably and transitionally over Vendian dolomites. Transition from Soltanieh Formation to
580:, is formed on the Hercynian metamorphosed basement at the southwestern margin of the Turan Platform. The belt is composed of about 10 kilometres of Mesozoic and Tertiary sediments (mostly carbonates) and, like the Zagros, was folded into long linear northwest–southeast trending folds during the last phase of the Alpine Orogeny, in the Miocene and Plio-Pleistocene time. No magmatic rocks are exposed in Kopet Dagh except for those in the basement in the Aghdarband and some
2672:
1074:. Transition from Middle to Upper Triassic coincides with Early Cimmerian orogenic episode, which led to the segmentation of the sedimentary basin into three sub-basins: Zagros in the south and southwest, Alborz in the north, and Central Iran. The Lower Jurassic rocks conformably overlie the Upper Triassic units; so are the Early Cretaceous deposits over the Upper Jurassic strata (e.g., Zagros). In North and Central Iran, the Upper Triassic and Lower–Middle
2682:
625:. Alborz is characterized by the dominance of platform-type sediments, including limestone, dolomite, and clastic rocks. Rock units from Precambrian to Quaternary have been identified, with some hiatuses and unconformities in Paleozoic and Mesozoic. Unlike its northern and southern boundaries, (Caspian Sea and Central Iran, respectively) there is not a consensus regarding the eastern and the western limits of Alborz. The
135:–bearing sutures. Other criteria such as structural style, crustal character and age of basement consolidation, age and intensity of deformation, age and nature of magmatism, are used to subdivide these major zones into smaller elements. The three major units and their main constituents could be defined as the southern, central and northern units. The southern unit has a crystalline basement consolidated in the
2279:
588:, it was covered with a vast continental shelf sea. In this period of time and due to transgression as well as rapid subsidence basin, the western part became deeper. In this basin, a thick sequence of continuous marine and continental sediments was deposited (about 10 km). No major sedimentary gap or volcanic activities during
1907:
and played a great role in the geological evolution of Iran. This event started under a compressional regime, followed by an extensional one. The compressional regime, that was associated with significant intrusive magmatic activities, led to the closure of the oceanic basins and
Neothetyan rifts. In
692:
situated in the southeast of the
Caspian Sea and in much smaller portions in the central and western parts of the Central Alborz Range. The central part of the Central Alborz Range is formed predominantly of the Triassic and Jurassic rocks, while the northwestern section of the range is made chiefly
604:
was closed and the
Arabian Plate collided with the Iranian Plate and was pushed against it, and with the clockwise rotation of the Eurasian Plate towards the Iranian Plate and their final collision, the Iranian Plate was pressed against the Turan Platform. This collision folded the entire rocks that
471:
or coloured melange of Zabol–Baluch Zone). Located to the west of Zabol–Baluch Zone, Lut Block is the main body of
Eastern Iran. Lut Block extends for about 900 kilometres (560 mi) in a north–south direction. It is bounded in the north by Dorooneh fault and in the south by Jazmurian depression.
1873:
The Late
Cimmerian orogeny occurred as a significant tectonic event in Iran in Late Jurassic–Early Cretaceous times. This event is represented by folding, facies changes in sedimentary environments, angular unconformity, magmatism, and metamorphism (e.g., Alborz, Sanandaj–Sirjan, and Central Iran).
1564:
have a widespread occurrence in Iran and can be grouped as follows: Ultramafic and mafic units of Late
Precambrian–Early Cambrian. Although comparable to modern ophiolites, these rocks do not display all typical features of an oceanic crust. The term “old ophiolite” might be a misnomer. These rocks
599:
This sedimentary complex provides suitable conditions for accumulation of hydrocarbons. Kopet Dagh sedimentary rocks were placed in their current position due to uplifting at the end of the
Miocene. The Kopet Dag Range, itself, is made chiefly of Cretaceous rocks with a smaller portion of Jurassic
1219:
with an age of 630–530 million years have been reported from many localities in Iran, particularly in
Central Iran and Azerbaijan. These magmatic rocks seem to be related to the Pan-African tectonic-magmatic episode. Most magmatic rocks of this time bear an alkaline nature. The following magmatic
809:
depression to the northern mountains of Tabriz (Mishu, Morou) and northwest of
Azerbaijan and the Caucasus. This event divided Azerbaijan into two blocks, one block in the northeast with subsidence and sedimentation in Early Devonian and the other in the southwest which remained high until Late
223:. The northern unit represents a marginal strip of the Hercynian realm of Central Asia- broadly overlapped by the Alpine realm. It was deformed and largely consolidated by the Early Cimmerian folding and the Late Alpine folding. The northern unit comprises the South Caspian Depression and the
360:
eras. As far as the trends, and particularly the folding style is concerned, some researchers consider the
Sanandaj–Sirjan Zone as being similar to Zagros; however, considerable differences exist in rock types, magmatism, metamorphism, and orogenic events. There are some similarities between
718:
as the Arabian Plate collided with the Iranian Plate and was pushed against it, and with the clockwise movement of the Eurasian Plate towards the Iranian Plate and their final collision, the Iranian Plate was pressed from both sides. The collisions finally caused the folding of the Upper
747:
began, therefore, with Eocene volcanism in southwestern and south-central parts of the Alborz and continued with the uplift and folding of the older sedimentary rocks in the northwestern, central and eastern parts of the range during the orogenic phases of importance that date from the
1099:
begins with the Cretaceous–Paleocene boundary that is characterized by striking changes in sedimentary environments (e.g., Alborz, Central Iran). An unconformity has been reported from many locations in Iran. Both continuous and discontinuous transitions have been discovered between
1716:
in Central Iran. This tectonic phase started with tension or extension leading to the formation of rifts and generation of oceanic crust (e.g., in Takab and Anarak) and ended with folding, closure, metamorphism, growth of the continental crust, and development of regional faults.
1078:
sediments have a detrital nature, consisting mainly of shale and sandstone with thicknesses varying from a few meters to more than 3,000 metres (9,800 ft). The presence of plant remains and coal beds suggest a continental or lagoon environment for the deposits. The
1007:
marine deposits has yet been discovered in Iran. Upper Carboniferous deposits are not significantly present in Iran and have only been identified in several localities from index goniatites. After a general regression and a distinct hiatus in Upper Carboniferous,
768:. According to some authors, the northeastern corner could be included in Alborz and the southeastern part in Sanandaj–Sirjan. Some believe that most of Azerbaijan lies in a zone called Azerbaijan–Alborz, and as they indicate, this zone is bounded in the north by
170:
The central unit, which comprises the central Iran and the Alborz, is interpreted as an assemblage of fragments that were in the vicinity of the Arabian Plate and formed a marginal section of Rodinia and Pannotia in the Neoproterozoic and of Gondwana in the
713:
volcano-sedimentary deposits with a strip of Paleozoic rocks and a band of Triassic and Jurassic rocks in the southern parts, both in a northwest–southeast direction. With the northward movement of Africa and the Arabian plate and with the closure of the
401:
volcanic belt is supposed to have resulted from the collision of the Arabian and Central Iranian continental plate margins. It is represented by sub-alkaline volcanics that vary in composition from basaltic through andesitic to rhyolitic composition.
219:. Finally there is the northern unit which is separated from the central unit by the North Iran Suture. It is characterized by continental crust including remnants of more or less cratonized former Paleozoic oceanic crust that seems to reflect the
1645:. Ultramafic and mafic rocks also occur in association with large gabbroic intrusions. This type probably resulted from differentiation in a large mafic magma chamber, comparable to those of the layered mafic intrusions. Examples occur in Sero,
1908:
some areas, slices of the oceanic crust have obducted onto the continental margins producing what could be called ophiolite assemblages or coloured melanges (e.g., mostly seen suture zone between Sanandaj–Sirjan and Zagros, and alongside
426:
can be recognized. Central Iran in a broad sense, comprising the whole area between the North and South Iranian ranges. Within the Iranian plate the Central-East Iran microplate is bordered by the Great Kavir Fault in the north, by the
990:
rocks in Iran consist mainly of limestone, sandstone, shale and volcanic materials, known as Niur Formation in Central Iran. The Lower Devonian rocks have been reported from several localities in Central Iran (e.g., Tabas, Sourian,
307:. In the Elevated Zagros or the Higher Zagros, the Paleozoic rocks could be found mainly in the upper and higher sections of the peaks of the Zagros Mountains along the Zagros main fault. On the both sides of this fault, there are
2013:. The Pasadenian orogeny is the most important phase in forging the current shape of Iran. Some younger orogenic events might be the continuation of this orogenic phase (e.g., Alborz–Azerbaijan axis, Zagros, Central Iran).
1769:
in Iran is controversial; the Hercynian in Iran is largely represented by extensional rather than compressional tectonics (e.g., Sanandaj–Sirjan). Iranian microplates east and northeast of the Zagros were detached from
1811:
the Carboniferous magmatic activities in northwestern Iran and normal faulting and tilted blocks in the High Zagros Belt which, taken together, support extensional deformation related to the Variscan or Hercynian
1319:
are a typical example. There is strong evidence for significant magmatic activities in Late Paleozoic–Early Mesozoic (Early Permian to Early Jurassic) in Iran. Examples include: magmatic rocks in the Southern
351:
and faults like Shahr-e-Babak and Abadeh, and to the south-southwest by the main thrust fault of Zagros. A striking feature of this zone is the presence of immense volumes of magmatic and metamorphic rocks of
1368:
orogenic events that caused continental and oceanic rifting, followed by closures and collisions in vast areas of Iran (e.g., Sanandaj–Sirjan). The Mesozoic magmatic rocks can be divided into three groups:
629:
in the east, although the continuation of the Alborz, bear features comparable to those of Central Iran. The Alborz mountain range is only 60–130 km wide and consists of sedimentary series dating from
804:
was accompanied by faulting and fragmentation that led to a different sedimentary facies in Azerbaijan. This orogenic episode generated the Tabriz fault, extending in a northwest–southeast direction from
247:. Zagros is in fact the northeastern edge of the Arabian Plate. Some important features of Zagros include: Absence of magmatic and metamorphic events after Triassic, and low abundance of the outcrops of
831:
by various authors. Isotopic data of Iranian basement rocks give ages between 600 and 900 Ma. A similar range of isotopic data had been obtained for Arabian Shield rocks. An important post-Pan-African
1837:
in the northern Iran and tensional tectonics in the south. There is evidence that the compressional phase was preceded by tension and rift development. The compressional phase, happening in the
143:–type Paleozoic development and comprises the Zagros folded belt, southern and southwestern parts of the Zagros. This section made a part of the Arabian Plate that was located on the margin of
343:
This zone is located to the south-southwest of Central Iran and the northeastern edge of Zagros range. In the north and northeast, this zone is separated from Central Iran by depressions like
1765:
The effects of this orogenic episode in Iran can be traced from the Late Devonian. Due to the scarcity of magmatism, metamorphism, and folding related to this episode, the role of the
1735:
in Iran is characterized by facies change in sedimentary basins, hiatuses, and epeirogenic movements (e.g., parts of Alborz, Zagros, and Central Iran). This phase, starting from Late
970:
sediments are sitting on the Vendian sediments through an angular unconformity. In the Late Ordovician, most parts of Iran were affected by epeirogenic movements; this coincides with
381:, runs east and almost parallel to the Sanandaj–Sirjan Zone, and owes its existence to the widespread and intensive volcanic activity which developed on the Iranian plate from the
705:
are found mainly in the southwestern and south-central parts of the range. The far northwestern part of the Alborz that constitutes what is called the Western Alborz Range or the
299:
in front of the Iranian Plate. The process of collision continues to the present and as the Arabian Plate is being pushed against the Iranian Plate, the Zagros Mountains and the
131:
Considering geological and structural units of Iran, three main structural units or zones could be distinguished in Iran. These units or zones are separated from each other by
1153:
1938:
With regards to the geological evidence, this event was of compressional nature. This tectonic phase is represented by significant changes in the sedimentary environments,
439:
Fault in the east. It is surrounded by the Upper Cretaceous to Lower Eocene ophiolite and ophiolitic melange. The microplate consists of different structural components;
1193:
773:
70:
476:, whereas the western boundary with Central Iran is Nayband fault and Shotori Mountains. The oldest units include upper Precambrian Lower Cambrian schists overlain by
410:
Located in a triangle in the middle of Iran, Central Iran is one of the most important and complicated structural zones in Iran. In this zone, rocks of all ages, from
1397:. They are mainly alkaline in nature and are more abundant in Sanandaj–Sirjan. In Jurassic–Cretaceous, intrusive rocks exceed volcanic rocks; a significant number of
828:
903:. The influence of the orogenic episode is evident at the base of the Vendian sediments. Deposition of shallow marine sediments covered large areas in Iran during
552:
fault being the most important one. Along these faults lies large section of ophiolite series. The oldest rocks in this zone are the ophiolites of Late Cretaceous–
488:) to the east. In contrast to Lut Block, the Flysch Zone is highly deformed and tectonized and consists of thick deep-sea sediments like argillaceous and silicic
516:, and subordinate serpentinized ultramafic rocks. The basement is likely composed of an oceanic crust. Most rock units in this zone fall into three main groups:
848:
45:
952:
944:
852:
621:
mountain range forms a barrier between the south Caspian and the Iranian plateau. This range is located in northern Iran, parallel to the southern margin of
95:
35:
928:
1311:
Volcanic rocks of andesitic-basaltic composition accompany Upper Paleozoic sedimentary strata in many areas all over Iran. Basaltic rocks associated with
1157:
1124:). Oligocene sediments in most parts of Iran are of shallow marine character, turning into marine facies in Upper Oligocene through Lower Miocene (e.g.,
1087:
affects most parts of Iran, leading to uplift, folding, and faulting. This is a prelude to significant developments in the geological evolution of Iran.
1055:
960:
912:
323:
rocks on the both sides. The Folded Zagros (the mountains south of the Elevated Zagros and almost parallel to the main Zagros fault) is formed mainly of
75:
50:
295:. This collision primarily happened during the Miocene and folded the entire rocks that had been deposited from the Carboniferous to the Miocene in the
2242:"Foraminiferal-based paleobiogeographic reconstructions in the Carboniferous of Iran and its implications for the Neo-Tethys opening time: a synthesis"
1312:
1037:
1013:
956:
916:
80:
1825:
is one of the most important tectonic events in the geological history of the earth. Many diverse features are associated with this phase, including
1340:
Series in Northern Sanandaj–Sirjan. Ultramafic and mafic rocks and their metamorphosed equivalents could be observed in Eastern Iran (Fariman area),
1241:
1165:
1048:
1041:
1021:
1017:
908:
876:
872:
844:
473:
60:
887:, and Anarak metamorphic units. The sedimentary facies of Precambrian–Lower Cambrian rocks in Northern Iran is different from that of Central Iran.
1288:
1284:
1173:
1169:
924:
880:
868:
864:
55:
1341:
1161:
1149:
227:
Range. These three main structural units are divided into some smaller geological and structural subdivisions which include the following zones:
827:, partial granitization and partly by intense folding took place in the Late Precambrian. This event has been attributed to the 'Baikalian' or
777:
769:
2637:
1794:
1373:: These rocks occurred mainly as a result of extension or tension related to the continental rifting, or subduction of the developed oceanic
537:
65:
30:
1083:
deposits, characterized by diverse sedimentary facies, are widespread all over Iran. In Late Cretaceous, tectonic movements related to the
884:
40:
1739:, caused the marine facies of Barut and Zaigoon Formations to change into the continental facies of Lalun Formation, and continued on to
1240:
composition, in Ghareh Dash, Azerbaijan. Volcanic rocks associated with Kushk Series in the Bafq area. Volcanic rocks of Rizu, Dezu, and
25:
859:
age. The oldest rocks in Iran belong to the Kushk Series consisting of clastic sediments, acidic volcanic, tuff, and carbonates (mainly
2063:
1116:
stages are characterized by rapid subsidence, deposition, and facies changes in both marine and continental sedimentary basins (e.g.,
1012:
marine transgression deposits cover most parts of Iran (e.g., Alborz, Zagros, Central Iran); The Permian sediments are represented by
1220:
series can be attributed to this phase: Doran-type intrusions in Azerbaijan. Narigan and Zarigan-type intrusive bodies extend from
1781:
The Neo-Tethys opening and rifting of Iran from the northern margin of Gondwana has probably occurred sometime between the latest
2586:
2647:
2045:
about 1.78 million years ago and after several known eruptions around 600,000 and 280,000 years ago, it finally erupted in the
2199:
Map showing geology, oil and gas field, and geologic provinces of Iran pubs.usgs.gov/of/1997/ofr-97-470/OF97-470G/Iranmap.pdf
2163:
Map showing geology, oil and gas field, and geologic provinces of Iran pubs.usgs.gov/of/1997/ofr-97-470/OF97-470G/Iranmap.pdf
303:
are getting higher and higher. The Zagros mountain range, itself, has a totally sedimentary origin and is made primarily of
2311:
2058:
999:
is characterized by marine transgression, particularly in Alborz, that extends into Lower Carboniferous. With exception of
1058:
dolomites in Central Iran. A continuous Permian–Triassic sequence has been reported from several areas in Iran, including
191:. They were submerged, moved northwards, and were finally attached to the Eurasian section of the northern supercontinent
2561:
480:
limestone and other Paleozoic sedimentary rocks. Flysch Zone (Zabol–Baluch) is located between Lut Block to the west and
939:
of Middle and Late Cambrian age. In some areas, the Late Cambrian carbonate facies turns transitionally into Ordovician
2606:
600:
rocks in the southeastern parts. The mountains were mainly formed in the Miocene during the Alpine orogeny. As the
2241:
923:
is characterized by uplift and regression; however, a renewed progression at this time led to the deposition of
1581:, Shanderman, and Asalem. These rocks display many typical features of modern ophiolites. Ophiolite series of
835:
is documented by the widespread Doran Granite, which cuts the Upper Precambrian rocks and is covered by Lower
2118:
GEOLOGICAL SURVEY OF IRAN - Manuel berberian, www.manuelberberian.com/Berberian%201976%20-%20Report%2039.pdf.
2109:
GEOLOGICAL SURVEY OF IRAN - Manuel berberian, www.manuelberberian.com/Berberian%201976%20-%20Report%2039.pdf.
1833:, folding, faulting, creation of new basins, and facies change. This event was associated with compressional
2396:
1589:
age show typical features of ophiolitic sequences and are thought to be associated with the closure of the
1279:
Magmatic rocks of this time have been reported from many areas in Iran. Examples include basaltic rocks of
1965:. The northern movement and the final collision of Afro-Arabia (significantly the Arabian Plate) with the
2642:
284:
2601:
2506:
1445:. Data from various structural zones indicate that the volcanic and plutonic activities started in the
2706:
2611:
2328:
2304:
1465:(or Urumiyeh-Dokhtar) volcanic-plutonic belt with a series of famous mountain ranges including the
1385:: Many intrusive bodies of mafic to granitic composition, with ages varying from early Triassic to
843:, rhyolite tuff and basic dikes are known in the Eocambrian formations. In North and Central Iran,
2556:
2521:
2476:
1577:
of Upper Paleozoic occur as metamorphosed as well as non-metamorphosed bodies in some areas like
796:
and the Southern Azerbaijan is comparable with Central Iran and Western Iran and extends to the
2446:
2441:
2336:
1793:
the northern Paleo-Tethyan affinity of the foraminiferal associations in the late Viséan-late
1593:. These ophiolite series are widespread in Iran. Some of the more important locations include
2566:
2541:
2456:
2436:
2386:
2356:
2346:
378:
2652:
2531:
2526:
2406:
1457:. Some of the more important regions in terms of the Tertiary magmatic activities include:
8:
2626:
2596:
2546:
2501:
2481:
2471:
2371:
2297:
1689:
1683:
1662:
896:
1973:
towards the Iranian Plate caused the Alpine orogeny with the Pyrenean phase in the Late
931:, consisting of limestone, dolomite, and shale, over older units. These formations bear
2571:
2486:
2466:
2351:
2341:
1732:
1726:
1700:, folding, and faulting during Late Precambrian–Early Cambrian in Iran (e.g., south of
1666:
1622:
1518:
1200:
1059:
971:
781:
533:
275:
rocks about 8-10 kilometres in thickness has undergone folding from the Miocene to the
140:
1692:
is equivalent to Asynitic in other parts of the earth. This event was associated with
2681:
2616:
2551:
2516:
2451:
2431:
2421:
2381:
2366:
2361:
2263:
2259:
1822:
1766:
1752:
1429:
is of great concern in Iran because of the great volumes and highly diverse types of
1361:
1299:
765:
680:) rocks, while the western part of the Eastern Alborz Range is made primarily of the
626:
520:
sediments; volcanic, volcanosedimentary, and intrusive rocks; and ophiolitic series.
1757:
1176:). A correlation exists between distribution of magmatic rocks and certain types of
2657:
2576:
2536:
2511:
2491:
2426:
2401:
2391:
2376:
2255:
1913:
1896:
1890:
1582:
1466:
1410:
1268:
1248:
1084:
797:
789:
710:
706:
382:
280:
85:
1036:
sediments in Iran are mainly of shallow marine or continental shelf nature (e.g.,
780:. According to the some authors, the northern part of Azerbaijan continues to the
18:
2496:
2461:
2416:
2320:
1900:
1731:
There was no considerable folding or faulting related to this event in Iran. The
1654:
1561:
1474:
1446:
1386:
1377:
under the continental lithosphere (e.g., Central Alborz for continental rifting;
1044:
995:, Zagros); however, they seem to be missing in Alborz and parts of Zagros. Upper
860:
585:
300:
204:
1761:
Late Carboniferous paleogeography (about 320 Ma) with the Paleo-Tethys indicated
548:. The northern part is characterized by dominance of east–west trending faults,
2283:
2246:
2038:
2030:
1982:
1970:
1962:
1933:
1542:
1482:
1382:
1128:). The Middle to Upper Miocene sediments are mostly of continental nature. The
744:
631:
152:
609:
or basin from the Jurassic to the Miocene and formed the Kopet Dag Mountains.
2700:
2675:
2267:
2006:
1966:
1854:
1838:
1775:
1740:
1661:
in age. The most remarkable occurrence of ophiolite could be observed in the
1634:
1434:
1394:
1370:
1233:
1216:
1004:
899:
and following this orogenic episode, shallow marine sediments formed in Late
654:
456:
292:
288:
260:
212:
200:
196:
188:
2037:
of this orogenic phase. With an elevation of 5,610 metres (18,410 ft),
1881:
of Kolah Ghazi, Shir Kuh, and Shah Kuh was made during this orogenic phase.
642:
core. Continental conditions regarding sedimentation are reflected by thick
1943:
1921:
1826:
1701:
1693:
1618:
1506:
1430:
1406:
1304:
1121:
1070:(the continuation of the Taurus in Turkey), north of Kandovan and Southern
824:
806:
564:. The whole sequence is deformed prior to Early Miocene. Thick sequence of
541:
419:
236:
112:
2226:
Geological Map of Iran, National Geoscience Database of Iran, www.ngdir.ir
2217:
Geological Map of Iran, National Geoscience Database of Iran, www.ngdir.ir
2208:
Geological Map of Iran, National Geoscience Database of Iran, www.ngdir.ir
2172:
Geological Map of Iran, National Geoscience Database of Iran, www.ngdir.ir
2154:
Geological Map of Iran, National Geoscience Database of Iran, www.ngdir.ir
1263:
and Anarak areas, seem to have originally been volcanic materials, either
2685:
2042:
2010:
1846:
1842:
1610:
1478:
1470:
1374:
1256:
1252:
1245:
1197:
1141:
856:
685:
622:
606:
493:
485:
411:
296:
268:
220:
136:
1997:
mountains were mainly formed in the Miocene during this orogenic phase.
1808:
fusulinid assemblages of Iran to the northern margin of the Paleo-Tethys
1393:–Shamsabad axis). In Triassic–Jurassic, volcanic rocks predominated the
1994:
1801:
1786:
1709:
1642:
1609:(south of Jazmurian), ultramafic–mafic rocks related to Flysch Zone in
1594:
1574:
1522:
1486:
1454:
1442:
1145:
1129:
1080:
979:
975:
967:
940:
936:
715:
601:
577:
467:
Eastern Iran can be divided into two parts: Lut Block and Flysch Zone (
428:
415:
344:
320:
240:
224:
176:
1865:
section of the northern supercontinent Laurasia in the Late Triassic.
668:
In the Eastern Alborz Range, the far eastern section is formed by the
2034:
1978:
1958:
1939:
1917:
1909:
1904:
1834:
1830:
1697:
1658:
1590:
1586:
1557:
1526:
1514:
1414:
1398:
1204:
1117:
1109:
1101:
932:
904:
832:
740:
728:
720:
681:
662:
646:
635:
557:
553:
549:
517:
423:
353:
348:
328:
304:
252:
248:
160:
132:
120:
116:
90:
1782:
1207:
have been identified in Iran. These episodes could be described as:
863:). Other formations of Late Precambrian–Early Cambrian ages include
2046:
2022:
1875:
1858:
1850:
1805:
1771:
1736:
1650:
1646:
1626:
1538:
1498:
1494:
1426:
1402:
1390:
1365:
1357:
1321:
1316:
1237:
1229:
1203:
deposit related to Sarcheshmeh porphyry body). Several episodes of
1096:
1075:
1067:
1033:
996:
987:
983:
920:
840:
836:
801:
785:
753:
732:
724:
677:
673:
669:
643:
589:
584:
basic dikes. This basin was located in the northeastern Iran. From
581:
545:
513:
505:
386:
362:
357:
324:
316:
312:
308:
276:
272:
256:
192:
184:
180:
172:
164:
156:
148:
111:
include the study of the geological and structural units or zones;
2289:
839:
sediments. Late Precambrian postorogenic volcanics, mainly alkali
693:
of Jurassic rocks. Very thick beds of the Tertiary (mostly of the
199:. These fragments or microplates were fused together and made the
2282:
Material was copied from this source, which is available under a
2018:
1878:
1862:
1705:
1630:
1614:
1578:
1534:
1502:
1329:
1280:
1113:
1009:
900:
749:
658:
639:
593:
565:
501:
481:
477:
436:
332:
264:
216:
208:
144:
104:
1946:(e.g., west of Central Iran, south of Central Alborz, Lut). The
1573:
Regions. They might be representing a protorift. Ultramafic and
1287:
in Central Iran, and tuffaceous materials in the upper parts of
2041:
is the highest peak in Iran. This volcano first erupted in the
2026:
2014:
1990:
1986:
1974:
1955:
1951:
1947:
1606:
1598:
1570:
1546:
1530:
1510:
1462:
1458:
1450:
1438:
1378:
1345:
1337:
1333:
1325:
1221:
1189:
1105:
1063:
992:
948:
800:
in Turkey. The significant structural event occurring in Early
793:
736:
694:
689:
618:
529:
509:
497:
468:
452:
440:
398:
394:
390:
366:
2278:
1566:
1490:
1348:
schists, and Shanderman mafic/ultramafic metamorphic series.
1260:
1051:
1000:
489:
444:
1857:
and that had been submerged and had moved northwards toward
1713:
1638:
1602:
1303:
Early Carboniferous paleogeography (about 350 Ma) with the
1264:
1225:
1185:
1181:
1071:
702:
698:
650:
568:
rock units, in excess of 5,000 m, covers the older series.
561:
448:
432:
244:
108:
1617:
Belt, ultramafic and mafic rocks north of Dorooneh fault,
764:
There is no agreement regarding the geological setting of
126:
123:
series and ultramafic rocks; and orogenic events in Iran.
2145:
A Summary of Geology of Iran - Springer, www.springer.com
2136:
A Summary of Geology of Iran - Springer, www.springer.com
2127:
A Summary of Geology of Iran - Springer, www.springer.com
1177:
1125:
287:
was formed by the collision of two tectonic plates — the
1552:
1437:
of this age are widespread all over Iran, except in the
743:
to form the Alborz Mountains mainly in the Miocene. The
2284:
Creative Commons Attribution 4.0 International License
2100:
Geology of Iran, Geological Survey of Iran, www.gsi.ir
2082:
Geology of Iran, Geological Survey of Iran, www.gsi.ir
472:
In the east, it is separated from Flysch Zone by the
187:. These fragments were detached from Gondwana in the
1405:, and Shah Kuh were formed by Jurassic granite; and
919:
is very difficult to recognize in the field. Middle
1849:). Iranian microplates that had been detached from
1485:. The Tertiary magmatism could also be observed in
1210:
496:, and pelagic limestone and volcanic rocks such as
203:which was rejoined by Gondwanic Afro-Arabia in the
2175:
1954:volcanic arc or belt was mainly formed during the
1188:related to Zarigan–Narigan-type granites, Mazraeh
215:ultimately collided with the Iranian Plate in the
1497:, Central Alborz and its southern margins, Kavir–
974:in Europe and some other parts of the earth. The
389:time. The peak of this volcanism happened in the
331:rocks south of the Cretaceous rocks and then the
2698:
1927:
1132:is the prominent feature of the plains of Iran.
688:rocks can be found chiefly south of the city of
556:overlain by a thick sequence (about 5,000 m) of
377:This volcanic belt, which is usually called the
1283:and Khosh Yeilagh, andesitic-basaltic units of
576:The northeastern active fold belt of Iran, the
1135:
523:
372:
2305:
1800:the unique similarity between the Bashkirian-
823:The consolidation of the Iranian basement by
259:and continuous marine sedimentation from the
1453:, and continued, with short stops, into the
1401:in Iran occurred at this time. Kolah Ghazi,
435:Fault in the west and southwest and by the
2312:
2298:
2064:National Geographical Organization of Iran
1672:
1517:, Bazman, Taftan, East Iran, and Southern
653:seams. Marine conditions are reflected by
251:rocks. Structurally, it consists of large
243:in the northwest and continues through to
207:. As Afro-Arabia moved northwards towards
103:The main points that are discussed in the
2239:
1924:was formed during the Laramide orogeny.
1756:
1298:
1112:(e.g., Central Iran). The Oligocene and
638:, prevalently Jurassic limestone over a
540:; to the south, it is restricted by the
17:
1108:strata; as is the case with Eocene and
813:
127:Geological and structural units of Iran
22:Structural geological features of Iran.
2699:
1389:, have been identified in Iran (e.g.,
1336:of Sirjan area) and volcanic rocks of
1066:(Southern Central Iran), and Southern
2293:
2190:Paleogeographic Maps, www.scotese.com
2091:Paleogeographic Maps, www.scotese.com
1789:). Evidence for this conclusion are:
1553:Ophiolite series and ultramafic rocks
1140:Magmatic rocks of all ages, from the
2059:National Geoscience Database of Iran
1841:, finally led to the closure of the
1633:regions, and Central Iran–Nain–Baft–
1473:and important peaks such as Karkas,
536:depression. Its western boundary is
335:rocks south of the Paleogene rocks.
2319:
1360:magmatic rocks are associated with
661:strata that are composed mainly of
544:, and to the east, it extends into
418:, and several episodes of orogeny,
13:
1969:and the clockwise rotation of the
1816:
1294:
1274:
649:and by Jurassic shales containing
338:
14:
2718:
2005:This orogenic phase began in the
1868:
1845:(e.g., southeast to southwest of
1529:produced very high peaks such as
1433:and associated mineral deposits.
2680:
2671:
2670:
2277:
2260:10.1344/GeologicaActa2017.15.2.5
1912:fault in the east of Iran). The
1381:-Sanandaj axis for subduction).
1211:Upper Precambrian–Lower Cambrian
1148:, are widespread in Iran (e.g.,
978:caused a distinct hiatus at the
867:volcanic-sedimentary formation,
532:zone is located to the south of
2233:
2220:
2211:
2202:
2193:
2184:
2166:
2157:
1509:, Lut and Kavir, Central Iran,
462:
405:
2638:British Indian Ocean Territory
2148:
2139:
2130:
2121:
2112:
2103:
2094:
2085:
2076:
2033:were mainly formed during the
1677:
818:
267:. On the whole, a sequence of
1:
2069:
2000:
1981:and the Styrian phase in the
1928:Alpine (Pyrenean and Styrian)
1785:to early Late Carboniferous (
1720:
1420:
1351:
986:boundary. Where present, the
759:
571:
319:rocks that are surrounded by
1778:during this orogenic phase.
1746:
890:
7:
2052:
1884:
1136:Magmatism and igneous rocks
1090:
1027:
605:had been deposited in this
524:Southeastern Iran or Makran
373:Sahand–Bazman Volcanic Belt
285:Zagros fold and thrust belt
10:
2723:
1931:
1888:
1861:finally collided with the
1750:
1724:
1681:
1669:in the northeast of Iran.
1003:area, no record of Middle
851:and the lower half of the
2666:
2625:
2585:
2327:
1665:in the southeast and the
612:
596:have ever been reported.
230:
71:Makran Accretionary Prism
2387:East Timor (Timor-Leste)
311:rocks, a combination of
99:• HZB - High Zagros
2648:Cocos (Keeling) Islands
2049:almost 7300 years ago.
1673:Orogenic events in Iran
1154:Zarigan–Narigan Granite
235:This zone extends from
2181:Arefifard, 2017, p.143
1762:
1308:
1244:in Central Iran. Most
776:, and in the south by
709:is made mainly of the
100:
2240:Arefifard, S (2017),
2009:and continued in the
1760:
1302:
1194:Sheyvar–Daghi Granite
1062:(northwest of Iran),
943:shales, known as the
849:Gharehdash Formations
774:Tabriz–Urumiyeh Fault
528:Southeastern Iran or
379:Central Iranian Range
21:
2562:United Arab Emirates
1192:deposits related to
955:in Central Iran and
814:Stratigraphy of Iran
46:Sanandaj-Sirjan Zone
2589:limited recognition
1690:Pan-African orogeny
1684:Pan-African orogeny
1663:Bashagard Mountains
1259:facies, such as in
1120:and Halab south of
953:Shirgasht Formation
945:Lashkarak Formation
929:Kuhbonan Formations
897:Pan-African orogeny
853:Soltanieh Formation
829:Pan–African orogeny
500:, spilitic basalt,
119:and igneous rocks;
96:Paleo Tethys Suture
36:Posht-e-Badam Block
1985:respectively. The
1763:
1733:Caledonian orogeny
1727:Caledonian orogeny
1667:Jaghatai Mountains
1623:Torbat-e Heydarieh
1565:are widespread in
1309:
972:Caledonian orogeny
961:Zardkuh Formations
782:Caucasus Mountains
369:and Central Iran.
101:
2694:
2693:
2631:other territories
1823:Cimmerian orogeny
1767:Hercynian orogeny
1753:Hercynian orogeny
1549:and many others.
1525:. The Quaternary
1291:in Eastern Iran.
1269:pyroclastic rocks
1249:metamorphic rocks
1205:magmatic activity
1158:Torghabeh Granite
1014:Dorood Sandstones
966:In Kalmard area,
917:Laloon Formations
772:, in the west by
697:) green volcanic
627:Binalud Mountains
76:Main Zagros Fault
51:High Zagros Fault
2714:
2684:
2674:
2673:
2643:Christmas Island
2329:Sovereign states
2321:Geology of Asia
2314:
2307:
2300:
2291:
2290:
2281:
2276:
2275:
2274:
2227:
2224:
2218:
2215:
2209:
2206:
2200:
2197:
2191:
2188:
2182:
2179:
2173:
2170:
2164:
2161:
2155:
2152:
2146:
2143:
2137:
2134:
2128:
2125:
2119:
2116:
2110:
2107:
2101:
2098:
2092:
2089:
2083:
2080:
1914:Upper Cretaceous
1899:happened in the
1897:Laramide orogeny
1891:Laramide orogeny
1583:Early Cretaceous
1562:ultramafic rocks
1467:Karkas Mountains
1449:, peaked in the
1411:Upper Cretaceous
1313:Jeyrud Formation
1242:Kushk Formations
1180:deposits (e.g.,
1085:Laramide orogeny
1022:Nesen Limestones
873:Tashk Formations
798:Taurus Mountains
790:Pontus Mountains
711:Upper Cretaceous
707:Talish Mountains
383:Upper Cretaceous
327:rocks, with the
281:Zagros Mountains
239:in the south to
81:Tabriz-Qom Block
2722:
2721:
2717:
2716:
2715:
2713:
2712:
2711:
2707:Geology of Iran
2697:
2696:
2695:
2690:
2662:
2630:
2621:
2602:Northern Cyprus
2588:
2581:
2323:
2318:
2272:
2270:
2236:
2231:
2230:
2225:
2221:
2216:
2212:
2207:
2203:
2198:
2194:
2189:
2185:
2180:
2176:
2171:
2167:
2162:
2158:
2153:
2149:
2144:
2140:
2135:
2131:
2126:
2122:
2117:
2113:
2108:
2104:
2099:
2095:
2090:
2086:
2081:
2077:
2072:
2055:
2003:
1936:
1930:
1901:Late Cretaceous
1893:
1887:
1871:
1819:
1817:Early Cimmerian
1755:
1749:
1729:
1723:
1686:
1680:
1675:
1655:Late Cretaceous
1555:
1447:Late Cretaceous
1423:
1387:Late Cretaceous
1383:Intrusive rocks
1354:
1297:
1295:Upper Paleozoic
1277:
1275:Lower Paleozoic
1213:
1166:Chaghand Gabbro
1138:
1093:
1040:sandstones and
1030:
893:
877:Aghda Limestone
821:
816:
810:Carboniferous.
762:
731:rocks, and the
615:
586:Middle Jurassic
574:
526:
474:Nehbandan Fault
465:
408:
375:
341:
339:Sanandaj–Sirjan
301:Iranian Plateau
233:
205:Late Cretaceous
129:
98:
93:
88:
83:
78:
73:
68:
63:
61:East Iran Block
58:
53:
48:
43:
38:
33:
28:
23:
12:
11:
5:
2720:
2710:
2709:
2692:
2691:
2689:
2688:
2678:
2667:
2664:
2663:
2661:
2660:
2655:
2650:
2645:
2640:
2634:
2632:
2623:
2622:
2620:
2619:
2614:
2609:
2604:
2599:
2593:
2591:
2583:
2582:
2580:
2579:
2574:
2569:
2564:
2559:
2554:
2549:
2544:
2539:
2534:
2529:
2524:
2519:
2514:
2509:
2504:
2499:
2494:
2489:
2484:
2479:
2474:
2469:
2464:
2459:
2454:
2449:
2444:
2439:
2434:
2429:
2424:
2419:
2414:
2409:
2404:
2399:
2394:
2389:
2384:
2379:
2374:
2369:
2364:
2359:
2354:
2349:
2344:
2339:
2333:
2331:
2325:
2324:
2317:
2316:
2309:
2302:
2294:
2288:
2287:
2247:Geologica Acta
2235:
2232:
2229:
2228:
2219:
2210:
2201:
2192:
2183:
2174:
2165:
2156:
2147:
2138:
2129:
2120:
2111:
2102:
2093:
2084:
2074:
2073:
2071:
2068:
2067:
2066:
2061:
2054:
2051:
2039:Mount Damavand
2002:
1999:
1983:Middle Miocene
1971:Eurasian Plate
1963:Alpine orogeny
1934:Alpine orogeny
1932:Main article:
1929:
1926:
1889:Main article:
1886:
1883:
1870:
1869:Late Cimmerian
1867:
1818:
1815:
1814:
1813:
1809:
1798:
1751:Main article:
1748:
1745:
1725:Main article:
1722:
1719:
1682:Main article:
1679:
1676:
1674:
1671:
1554:
1551:
1435:Magmatic rocks
1422:
1419:
1395:plutonic rocks
1371:Volcanic rocks
1353:
1350:
1296:
1293:
1289:Mila Formation
1285:Niur Formation
1276:
1273:
1234:Volcanic rocks
1217:plutonic rocks
1212:
1209:
1174:Natanz Granite
1170:Alvand Granite
1137:
1134:
1092:
1089:
1029:
1026:
892:
889:
881:Kalmard Series
820:
817:
815:
812:
761:
758:
745:Alpine orogeny
632:Upper Devonian
614:
611:
573:
570:
525:
522:
464:
461:
407:
404:
374:
371:
340:
337:
232:
229:
153:Neoproterozoic
128:
125:
56:Sabzevar Block
9:
6:
4:
3:
2:
2719:
2708:
2705:
2704:
2702:
2687:
2683:
2679:
2677:
2669:
2668:
2665:
2659:
2656:
2654:
2651:
2649:
2646:
2644:
2641:
2639:
2636:
2635:
2633:
2628:
2624:
2618:
2615:
2613:
2612:South Ossetia
2610:
2608:
2605:
2603:
2600:
2598:
2595:
2594:
2592:
2590:
2584:
2578:
2575:
2573:
2570:
2568:
2565:
2563:
2560:
2558:
2555:
2553:
2550:
2548:
2545:
2543:
2540:
2538:
2535:
2533:
2530:
2528:
2525:
2523:
2520:
2518:
2515:
2513:
2510:
2508:
2505:
2503:
2500:
2498:
2495:
2493:
2490:
2488:
2485:
2483:
2480:
2478:
2475:
2473:
2470:
2468:
2465:
2463:
2460:
2458:
2455:
2453:
2450:
2448:
2445:
2443:
2440:
2438:
2435:
2433:
2430:
2428:
2425:
2423:
2420:
2418:
2415:
2413:
2410:
2408:
2405:
2403:
2400:
2398:
2395:
2393:
2390:
2388:
2385:
2383:
2380:
2378:
2375:
2373:
2370:
2368:
2365:
2363:
2360:
2358:
2355:
2353:
2350:
2348:
2345:
2343:
2340:
2338:
2335:
2334:
2332:
2330:
2326:
2322:
2315:
2310:
2308:
2303:
2301:
2296:
2295:
2292:
2285:
2280:
2269:
2265:
2261:
2257:
2253:
2249:
2248:
2243:
2238:
2237:
2223:
2214:
2205:
2196:
2187:
2178:
2169:
2160:
2151:
2142:
2133:
2124:
2115:
2106:
2097:
2088:
2079:
2075:
2065:
2062:
2060:
2057:
2056:
2050:
2048:
2044:
2040:
2036:
2032:
2028:
2024:
2020:
2016:
2012:
2008:
2007:Late Pliocene
1998:
1996:
1992:
1988:
1984:
1980:
1976:
1972:
1968:
1967:Iranian Plate
1964:
1960:
1957:
1953:
1949:
1945:
1941:
1935:
1925:
1923:
1919:
1915:
1911:
1906:
1902:
1898:
1892:
1882:
1880:
1877:
1866:
1864:
1860:
1856:
1855:Carboniferous
1852:
1848:
1844:
1840:
1839:Late Triassic
1836:
1832:
1828:
1824:
1810:
1807:
1803:
1799:
1796:
1792:
1791:
1790:
1788:
1784:
1779:
1777:
1776:Carboniferous
1773:
1768:
1759:
1754:
1744:
1742:
1741:Late Devonian
1738:
1734:
1728:
1718:
1715:
1711:
1707:
1703:
1699:
1695:
1691:
1685:
1670:
1668:
1664:
1660:
1656:
1652:
1648:
1644:
1640:
1636:
1635:Shahr-e Babak
1632:
1628:
1624:
1620:
1616:
1613:–Nosrat Abad–
1612:
1608:
1604:
1600:
1596:
1592:
1588:
1584:
1580:
1576:
1572:
1568:
1563:
1559:
1550:
1548:
1544:
1540:
1536:
1532:
1528:
1524:
1520:
1516:
1512:
1508:
1504:
1500:
1496:
1492:
1488:
1484:
1480:
1476:
1472:
1468:
1464:
1460:
1456:
1452:
1448:
1444:
1440:
1436:
1432:
1431:igneous rocks
1428:
1418:
1416:
1412:
1408:
1404:
1400:
1396:
1392:
1388:
1384:
1380:
1376:
1372:
1367:
1363:
1359:
1349:
1347:
1343:
1342:Taknar Series
1339:
1335:
1331:
1327:
1323:
1318:
1314:
1306:
1301:
1292:
1290:
1286:
1282:
1272:
1270:
1266:
1262:
1258:
1254:
1250:
1247:
1243:
1239:
1235:
1231:
1227:
1223:
1218:
1215:Volcanic and
1208:
1206:
1202:
1199:
1195:
1191:
1187:
1183:
1179:
1175:
1171:
1167:
1163:
1162:Ghaen Granite
1159:
1155:
1151:
1150:Doran Granite
1147:
1143:
1133:
1131:
1127:
1123:
1119:
1115:
1111:
1107:
1103:
1098:
1088:
1086:
1082:
1077:
1073:
1069:
1065:
1061:
1057:
1053:
1050:
1046:
1043:
1039:
1035:
1025:
1023:
1019:
1015:
1011:
1006:
1005:Carboniferous
1002:
998:
994:
989:
985:
981:
977:
973:
969:
964:
962:
958:
954:
950:
946:
942:
938:
934:
930:
926:
922:
918:
914:
910:
906:
902:
898:
888:
886:
882:
878:
874:
870:
866:
862:
858:
854:
850:
846:
842:
838:
834:
830:
826:
811:
808:
803:
799:
795:
791:
787:
783:
779:
775:
771:
767:
757:
755:
751:
746:
742:
738:
735:(chiefly the
734:
730:
726:
722:
717:
712:
708:
704:
700:
696:
691:
687:
683:
679:
675:
671:
666:
664:
660:
656:
655:Carboniferous
652:
648:
645:
641:
637:
633:
628:
624:
620:
610:
608:
603:
597:
595:
591:
587:
583:
579:
569:
567:
563:
560:, shale, and
559:
555:
551:
547:
543:
539:
535:
531:
521:
519:
515:
511:
507:
503:
499:
495:
491:
487:
483:
479:
475:
470:
460:
458:
454:
450:
446:
442:
438:
434:
430:
425:
421:
417:
413:
403:
400:
396:
392:
388:
384:
380:
370:
368:
364:
359:
355:
350:
346:
336:
334:
330:
326:
322:
318:
314:
310:
306:
302:
298:
294:
293:Arabian Plate
290:
289:Iranian Plate
286:
282:
278:
274:
270:
266:
262:
261:Carboniferous
258:
254:
250:
246:
242:
238:
228:
226:
222:
218:
214:
213:Arabian Plate
210:
206:
202:
201:Iranian Plate
198:
197:Late Triassic
194:
190:
189:Carboniferous
186:
182:
178:
174:
168:
166:
162:
158:
154:
150:
146:
142:
138:
134:
124:
122:
118:
114:
110:
106:
97:
92:
87:
86:Zagros Orogen
82:
79:• TQB -
77:
74:• MZF -
72:
69:• MAP -
67:
62:
57:
52:
49:• HZF -
47:
44:• SSZ -
42:
37:
34:• PBB -
32:
27:
20:
16:
2627:Dependencies
2557:Turkmenistan
2522:Saudi Arabia
2411:
2271:, retrieved
2251:
2245:
2234:Bibliography
2222:
2213:
2204:
2195:
2186:
2177:
2168:
2159:
2150:
2141:
2132:
2123:
2114:
2105:
2096:
2087:
2078:
2004:
1944:metamorphism
1937:
1922:Mount Alvand
1894:
1872:
1827:metamorphism
1820:
1780:
1764:
1730:
1694:metamorphism
1687:
1619:Torbat-e Jam
1556:
1507:Torbat-e Jam
1424:
1409:was made by
1407:Mount Alvand
1355:
1310:
1305:Paleo-Tethys
1278:
1236:, mostly of
1214:
1184:deposits in
1139:
1095:In Iran the
1094:
1031:
965:
894:
825:metamorphism
822:
778:Semnan Fault
770:Alborz Fault
763:
667:
616:
598:
575:
542:Gulf of Oman
527:
466:
463:Eastern Iran
420:metamorphism
409:
406:Central Iran
376:
342:
279:time in the
237:Bandar Abbas
234:
169:
130:
113:stratigraphy
102:
94:• PS -
89:• KD -
84:• ZO -
64:• AB -
54:• SB -
39:• YB -
29:• TB -
24:• LB -
15:
2686:Asia portal
2587:States with
2507:Philippines
2447:South Korea
2442:North Korea
2337:Afghanistan
2254:: 135–151,
2043:Pleistocene
2011:Pleistocene
1920:granite of
1847:Caspian Sea
1843:Paleotethys
1795:Sepukhovian
1678:Pan-African
1575:mafic rocks
1560:series and
1471:Jebal Barez
1375:lithosphere
1257:amphibolite
1253:greenschist
1246:Precambrian
1198:Sarcheshmeh
1142:Precambrian
1047:in Alborz,
1024:in Alborz.
963:in Zagros.
937:brachiopods
857:Precambrian
819:Precambrian
686:Precambrian
684:rocks. The
623:Caspian Sea
607:geosyncline
538:Minab Fault
494:radiolarite
486:Afghanistan
412:Precambrian
297:geosyncline
269:Precambrian
221:Paleotethys
139:time and a
137:Precambrian
66:Alborz Belt
59:• EIB
31:Tabas Block
2567:Uzbekistan
2542:Tajikistan
2457:Kyrgyzstan
2437:Kazakhstan
2357:Bangladesh
2347:Azerbaijan
2273:2020-01-02
2070:References
2001:Pasadenian
1995:Kopet-Dagh
1821:The Early
1802:Kasimovian
1787:Bashkirian
1721:Caledonian
1710:Azerbaijan
1595:Kermanshah
1523:Sabzevaran
1487:Azerbaijan
1455:Quaternary
1443:Kopet Dagh
1399:batholiths
1146:Quaternary
1130:Quaternary
1081:Cretaceous
1032:The Lower
980:Ordovician
976:epeirogeny
968:Ordovician
941:graptolite
933:trilobites
885:Shorm Beds
766:Azerbaijan
760:Azerbaijan
716:Tethys Sea
663:limestones
647:sandstones
602:Tethys Sea
578:Kopet Dagh
572:Kopet Dagh
451:Block and
416:Quaternary
345:Lake Urmia
321:Cretaceous
255:and small
253:anticlines
241:Kermanshah
225:Kopet Dagh
177:Ordovician
91:Kopeh Dagh
41:Yazd Block
2653:Hong Kong
2607:Palestine
2532:Sri Lanka
2527:Singapore
2407:Indonesia
2268:1695-6133
2035:volcanism
1979:Oligocene
1959:volcanism
1940:plutonism
1918:Paleocene
1910:Nehbandan
1905:Paleocene
1835:tectonics
1831:magmatism
1804:and late
1797:in Alborz
1747:Hercynian
1698:magmatism
1659:Oligocene
1657:to Lower
1653:that are
1649:, and in
1591:Neotethys
1587:Paleogene
1558:Ophiolite
1527:volcanism
1519:Jazmurian
1475:Marshenan
1417:granite.
1415:Paleocene
1362:Cimmerian
1315:of Upper
1307:indicated
1118:Mahneshan
1110:Oligocene
1102:Paleocene
1045:dolomites
905:Paleozoic
895:With the
891:Paleozoic
833:magmatism
741:volcanism
729:Paleogene
721:Paleozoic
682:Paleozoic
672:(chiefly
636:Oligocene
558:sandstone
554:Paleocene
550:Bashagard
534:Jazmurian
518:flyschoid
424:magmatism
354:Paleozoic
349:Gavkhouni
329:Paleogene
305:limestone
257:synclines
249:Paleozoic
161:Paleozoic
155:, and of
133:ophiolite
121:ophiolite
117:magmatism
26:Lut Block
2701:Category
2676:Category
2597:Abkhazia
2547:Thailand
2502:Pakistan
2482:Mongolia
2477:Maldives
2472:Malaysia
2372:Cambodia
2053:See also
2047:Holocene
2023:Damavand
1977:- Early
1885:Laramide
1876:Jurassic
1863:Eurasian
1859:Laurasia
1851:Gondwana
1812:orogeny.
1806:Gzhelian
1772:Gondwana
1737:Cambrian
1651:Masooleh
1647:Urumiyeh
1627:Sabzevar
1539:Damavand
1499:Sabzevar
1495:Taleghan
1483:Lalehzar
1427:Tertiary
1421:Cenozoic
1403:Shir Kuh
1391:Borujerd
1366:Laramide
1358:Mesozoic
1352:Mesozoic
1330:granites
1322:Sanandaj
1317:Devonian
1255:or even
1238:rhyolite
1230:Kuhbonan
1201:porphyry
1097:Cenozoic
1091:Cenozoic
1076:Jurassic
1068:Urumiyeh
1034:Triassic
1028:Mesozoic
997:Devonian
988:Silurian
984:Silurian
921:Cambrian
861:dolomite
841:rhyolite
837:Cambrian
802:Devonian
788:and the
786:Caucasia
756:epochs.
754:Pliocene
752:and the
733:Cenozoic
725:Mesozoic
678:Jurassic
674:Triassic
670:Mesozoic
644:Devonian
590:Jurassic
582:Triassic
546:Pakistan
514:rhyolite
506:andesite
363:Sanandaj
358:Mesozoic
325:Tertiary
317:Jurassic
313:Triassic
309:Mesozoic
291:and the
273:Pliocene
193:Laurasia
185:Devonian
181:Silurian
173:Cambrian
165:Mesozoic
157:Gondwana
149:Pannotia
141:platform
2572:Vietnam
2487:Myanmar
2467:Lebanon
2397:Georgia
2352:Bahrain
2342:Armenia
2019:Sabalan
1961:of the
1879:granite
1853:in the
1774:in the
1706:Mahabad
1631:Fariman
1615:Birjand
1579:Fariman
1535:Sabalan
1503:Kashmar
1338:Songhor
1334:gabbros
1281:Shahrud
1144:to the
1114:Miocene
1056:Shotori
1010:Permian
913:Zaigoon
901:Vendian
855:are of
750:Miocene
659:Permian
640:granite
594:Miocene
566:Neogene
502:diabase
482:Helmand
478:Permian
459:Block.
447:Block,
437:Harirud
333:Neogene
265:Miocene
263:to the
217:Miocene
209:Eurasia
195:in the
159:in the
151:in the
145:Rodinia
105:geology
2617:Taiwan
2552:Turkey
2517:Russia
2452:Kuwait
2432:Jordan
2422:Israel
2382:Cyprus
2367:Brunei
2362:Bhutan
2266:
2031:Taftan
2027:Bazman
2015:Sahand
1993:, and
1991:Alborz
1987:Zagros
1975:Eocene
1956:Eocene
1952:Bazman
1948:Sahand
1942:, and
1783:Viséan
1702:Zanjan
1607:Makran
1605:Belt,
1599:Neyriz
1571:Anarak
1547:Bazman
1543:Taftan
1531:Sahand
1511:Sistan
1463:Bazman
1459:Sahand
1451:Eocene
1439:Zagros
1379:Saghez
1346:Gorgan
1326:Sirjan
1222:Anarak
1190:copper
1122:Zanjan
1106:Eocene
1064:Abadeh
1052:shales
1038:Doroud
993:Kerman
957:Ilbeyk
949:Alborz
915:, and
807:Zanjan
794:Turkey
737:Eocene
727:, and
695:Eocene
690:Gorgan
619:Alborz
613:Alborz
530:Makran
510:dacite
498:basalt
490:shales
469:flysch
453:Anarak
441:Kerman
422:, and
399:Bazman
395:Sahand
393:. The
391:Eocene
387:Recent
367:Sirjan
283:. The
277:Recent
231:Zagros
211:, the
2658:Macau
2577:Yemen
2537:Syria
2512:Qatar
2492:Nepal
2427:Japan
2402:India
2392:Egypt
2377:China
1611:Khash
1567:Takab
1491:Tarom
1479:Hezar
1261:Takab
1060:Jolfa
1049:Sorkh
1042:Elika
1018:Ruteh
1001:Tabas
909:Barut
845:Kahar
703:lavas
699:tuffs
445:Tabas
2497:Oman
2462:Laos
2417:Iraq
2412:Iran
2264:ISSN
2029:and
1895:The
1874:The
1714:Bafq
1688:The
1643:Maku
1639:Khoy
1603:Oman
1569:and
1481:and
1469:and
1441:and
1425:The
1364:and
1356:The
1332:and
1265:lava
1228:and
1226:Bafq
1186:Bafq
1182:iron
1172:and
1104:and
1072:Amol
1054:and
1020:and
959:and
935:and
927:and
925:Mila
871:and
869:Dezu
865:Rizu
847:and
701:and
676:and
657:and
651:coal
617:The
562:marl
484:(in
457:Khur
449:Yazd
433:Baft
429:Nain
356:and
315:and
245:Iraq
183:and
163:and
147:and
109:Iran
2629:and
2256:doi
1708:in
1515:Bam
1267:or
1251:of
1224:to
1178:ore
1126:Qom
947:in
792:in
784:in
634:to
592:to
414:to
385:to
271:to
107:of
2703::
2262:,
2252:15
2250:,
2244:,
2025:,
2021:,
2017:,
1989:,
1829:,
1743:.
1712:,
1696:,
1637:,
1545:,
1541:,
1537:,
1533:,
1513:,
1501:,
1489:,
1477:,
1344:,
1271:.
1232:.
1196:,
1168:,
1164:,
1160:,
1156:,
1152:,
1016:,
951:,
911:,
883:,
879:,
875:,
739:)
723:,
665:.
512:,
508:,
504:,
492:,
347:,
179:,
175:,
167:.
115:;
2313:e
2306:t
2299:v
2286:.
2258::
1950:-
1916:-
1903:–
1704:–
1641:–
1629:–
1625:–
1621:–
1601:–
1597:–
1585:–
1521:–
1505:–
1493:–
1461:-
1413:-
1328:(
1324:–
982:–
455:-
443:-
431:–
397:-
365:–
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