Tectono-sedimentary framework of the Gachsaran Formation in the Zagros foreland basin

Bahroudi, Abbas; Koyi, Hemin

doi:10.1016/j.marpetgeo.2004.09.001

Cited by 147 publications

(67 citation statements)

References 37 publications

(88 reference statements)

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“…The stratigraphic column of the Zagros basin contains evaporites. The Hormuz salt (Precambrian) is located at the base of the sedimentary column, and the Gachsaran Formation (GF, Miocene) is composed of widespread evaporate units (Bahroudi and Koyi, 2004). The GF was deposited under the following conditions: evaporation exceeding the supply of seawater, arid climates, and nearly isolated salt basins.…”

Section: Geology and Stratigraphy Of Gypsum Formations In Iranmentioning

confidence: 99%

“…The GF outcrops in southwest and south-central Iran with a total exposure of 20,400 km 2 , making up 25.3% of the total gypsum outcrop in the country. The Zagros foreland basin is divided into sub-basins where Gachsaran salt and its non-salt equivalents were deposited (Bahroudi and Koyi, 2004). The Salt Gachsaran Formation (SGF) outcrops in a region from the Kazerun-Qatar faults to Dehloran City.…”

Section: Geology and Stratigraphy Of Gypsum Formations In Iranmentioning

confidence: 99%

“…2). The thickness of the GF usually varies over short distances (Dunnington, 1968;O'Brien, 1957;Stö cklin, 1968), typically from several hundred up to 2000 meters (Edgell, 1996;James and Wynd, 1965;Murris, 1980;Stö cklin, 1968;Bahroudi and Koyi, 2004). Although the GF is generally considered as lower Miocene in age (James and Wynd, 1965), stratigraphic correlations between wells on Qeshm Island in the extreme southeast of the basin reveals that its base is Oligocene or even older (Eocene).…”

Section: Geology and Stratigraphy Of Gypsum Formations In Iranmentioning

confidence: 99%

“…The base of the Fars group is diachoronous along the foreland basin and becomes younger with evaporite increases northwestward ( Fig. 2) (Gill and Ala, 1972;Motiei, 1993;Bahroudi and Koyi, 2004).…”

Section: Geology and Stratigraphy Of Gypsum Formations In Iranmentioning

confidence: 99%

“…Stocklin and Setudehnia (1977) divided the GF of the salt basin into seven members based on a type section from a well in the Gachsaran Oilfield. James and Wynd (1965) Although exposures of Gachsaran rock salt are rare, it is known from wells and quarries in the south of Masjed Suleyman in the Dezful embayment (Dunnington, 1968;Gill and Ala, 1972;Kashfi, 1980;Motiei, 1993;Bahroudi and Koyi, 2004).…”

Section: Geology and Stratigraphy Of Gypsum Formations In Iranmentioning

confidence: 99%

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Hydrogeology of Gypsum Formations in Iran

Raeisi¹,

Zare²,

Aghdam³

2013

JCKS

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Section: Geology and Stratigraphy Of Gypsum Formations In Iranmentioning

confidence: 99%

Section: Geology and Stratigraphy Of Gypsum Formations In Iranmentioning

confidence: 99%

Section: Geology and Stratigraphy Of Gypsum Formations In Iranmentioning

confidence: 99%

Section: Geology and Stratigraphy Of Gypsum Formations In Iranmentioning

confidence: 99%

Section: Geology and Stratigraphy Of Gypsum Formations In Iranmentioning

confidence: 99%

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Hydrogeology of Gypsum Formations in Iran

Raeisi¹,

Zare²,

Aghdam³

2013

JCKS

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Drainage Responses to Oblique and Lateral Thrust Ramps: A Review

Vergés

2007

Sedimentary Processes, Environments and Basins

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The relationships between oblique or lateral ramps in fold-and-thrust belts and their impact on syntectonic fluvial drainage are analysed in this review. Both ancient and recent cases from Cenozoic belts are examined. The southern flank of the Pyrenees provides good examples to decipher the long-term effects of oblique ramps on fluvial arrangement. Recent examples from the Indus River across the front of the Himalayas in northwest Pakistan, the frontal domains of the Andes in Bolivia and the northwest Zagros Mountain Belt provide examples of the short-term interaction between oblique or lateral thrust ramps and foreland drainage systems. The interpretation of these case studies, some of them developed on top of blind thrust ramps, can facilitate the analysis of drainage distortions in active complex tectonic regions.Oblique ramps are present either permanently or episodically at different scales in all fold-andthrust belts. The simplest scenario is related to piggyback basins, which display an oblique ramp linked to each frontal thrust termination. This oblique ramp forms the natural outlet for confined longitudinal systems along the piggyback basin. The change in topography across the ramp constrains the position of deltaic deposits between a subaerial fluvial system deposited in its hangingwall and an open marine system deposited in its footwall. Fluvial systems can also develop either in the hangingwall or in the footwall of larger oblique ramps that grow by the tectonic inversion of earlier structures. The growth of a large oblique ramp beneath a fluvial system operates in the same way as oblique ramps related to piggyback basins. However, its larger scale causes a larger differential topographic elevation across it, accommodating fluvial deposits in its hangingwall and deep marine turbidites in its footwall. In opposition, large oblique ramps growing in front of river systems create a topographic barrier that deflects the drainage.A complication of the interaction of oblique ramps and drainage occurs where two opposed oblique ramps form a tectonic reentrant. These tectonic reentrants form at different scales and are characterized by lower topography. The confined domains concentrate rivers flowing out from surrounding higher topographic deformed regions. Further development of deeper thrusts can uplift these reentrants, modifying the previous concentrated drainage and diverting the river courses towards regions with lower topography.As an example, the late Miocene longitudinal fluvial system flowing along the foreland basin of the Zagros during the deposition of the lower Agha Jari Formation was shifted to the southwest in the earliest Pliocene by the uplift of the Pusht-e Kuh Arc. The present river configuration is incising through the Pusht-e Kuh Arc anticlines and flows towards the lowlands of the Dezful Embayment (tectonic reentrant), limited by two major oblique ramps along the Mountain Front Flexure. The large-scale Mountain Front Flexure confines the Tigris River towards the southwest of the front of ...

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