The Zagros orogenic belt is a result of the Neogene collision between the Arabian and Cimmerian plates [26] - [28] . Tectonic column of the Zagros can be divided into at least, five tectonic stages [29] that existed between orogenic event at late Proterozoic (Pan-African), early rifting (intense chasmic in continental condition) event at Infra-Cambrian, late rifting event (quiet chasmic in marine condition) at Triassic and orogenic event at Neogene, that is related to continental collision.

The sedimentary succession in the Zagros is 6 - 18 km thick and ranges in age from Infra-Cambrian to Recent. There is a break up unconformity (the absence of Silurian and Carboniferous sediments) that is appropriate with [30] model for Passive margins evolution. Break up unconformity is coinciding with ocean floor spreading and sea transgression.

The northeastern part of Afro-Arabian plate margin began to undergo regional extension in the Infra-Cambrian to Carboniferous, finally caused to appear of a narrow oceanic basin between the Afro-Arabian plate and Cimmerian miniplate (Neo-Tethys) from the Carboniferous.

Then, post-rifting facies of passive margin from early Permian to the late Cretaceous were deposited on the Zagros basin. Since the late Jurassic, the Neo-Tethys ocean began subduction under the Cimmerian miniplate. A proforeland basin [31] formed at the NE margin of the Afro-Arabian plate from the Late Cretaceous, which it was accompanied to emplacement of Ophiolite rocks [32] [33] . The folding and regional uplifting of Zagros proforeland basin occurred at the end of Early Miocene. Therefore, Zagros is an active fold and thrust belt [34] same to Central Iran [35] - [38] and Alborz [39] - [43] .

Salt diapirs of Zagros present a large variety of shapes and elevation from high relief to entirely eroded structures. In addition, they have different sizes at outcrop scale, ranging from craters a few km wide to diapirs and glaciers more than 5 km wide. These different morphologies are controlled by various factors, for example, position related to other structures, the time of emergence, the rate of salt dissolution, which is controlled by the rate of erosion, the bulk rate of salt emission from the source layer, and eventually by the tectonic activity [16] .

The Salt plugs of the southern Iran can be divided into four areas, based on geographic distribution and geological setting of salt plugs (Figure 1):

1) The first area is central Zagros, with 23 emergent salt plugs.

2) The second area is southeastern part of Zagros, with 84 emergent salt plugs.

3) The third area is north margin of Persian Gulf, with 10 emergent salt plugs such as Hormuz, Larak and Abu Musa Islands.

4) The fourth area is an area between the first and second region in Zagros, with many subsurface salt plugs.

The diapiric province of Hormuz, in the east end of Zagros, with eighty four exposed salt diapirs is the widespread salt depotrough in Zagros. Because, based on previous studies, such as [16] , there are six type salt diapirs by investigation of the present-day surface morphology of them. They believe that nearly all the diapirs of the study area were already active prior to Zagros folding either as emergent diapirs forming islands in the Paleo- gene to Neogene Sea or as buried domes initiated at least by the Permian. They have been reactivated by subsequent tectonic events [44] .

Therefore, only some of salt diapirs have been exposed in post-orogenic phase, and their shape and location have controlled by folds and faults interactions during orogeny (Figure 2). So, the most of salt domes on this province are pre-orogenic diapirs. Also, big salt glacier such as Mazijan salt dome with a very clear salt Fountain (Figure 3) is a general phenomenon in Hormuz diapiric province [44] .

The diapiric province of Nyriz-Jahrum, in the centrral Zagros is a small salt minibasin. It has got a few exposed salt diapirs, many blind domes such as Sim, Meymand, Bavush, Kharman (Figure 4), Kuh-e Gavbast anticline (Figure 5) and diapiric fold such as Kuh-e Bavush (Figure 5) that located on the west part of Hormuz diapiric province.

The Gavbandi High [33] has been formed the south termination of Nyriz-Jahrum province. The Gavbandi High has been formed by regional uplifting of northward continuation of the Qatar Arc towards Iran, during the Late Pre Cambrian - Early Cambrian. Therefore, there are not thick evaporate layer.

The diapiric province of Shiraz-Kazerun is located in the west part of Nyriz-Jahrum diapiric province .It has got twenty three exposed salt diapirs and its area is smaller than Hormuz diapiric province.

The main north-south striking right-lateral faults in Zagros have been controlled location of this salt diapirs such as Kazerun fault with six, Kareh Bas fault [45] [46] with six (Figure 6) and Sarvestan fault with three salt diapirs [47] . It means that they are pre-orogenic salt diapirs, and their positions have been determinate current condition of folds [48] [49] . In addition, salt glacier such as Kuh-e Jahani dome (Figure 7), some blind salt dome such as Gardan anticline and diapiric fold such as Khaftar anticline (Figure 8) are general phenomenon in the Shiraz-Kazerun province.

However, based on previous study [50] - [52] and our investigations on the position, shape and orientation of salt domes in Zagros, three diapiric provinces have been introduced. Salt diapirism of these provinces has been

affected by rift development during Paleozoic that it has accompanied with sedimentation of Banded Iron Formation (BIF) in Hormuz Group (Figure 9) on Zagros basin.

Finally, based on previous work on the neotectonic regime in Iran, Zagros in south Iran is the most active zone [53] - [73] . Then, North Iran nd Central Iran [73] - [83] have been situated in the next orders.