Surficial deposits on salt diapirs (Zagros Mountains and Persian Gulf Platform, Iran): Characterization, evolution, erosion and the influence on landscape morphology

Bruthans, Jiří; Filippi, Michal; Asadi, Naser; Zare, Mohammad; Šlechta, Stanislav; Churáčková, Zdenka

doi:10.1016/j.geomorph.2008.12.006

Cited by 43 publications

(40 citation statements)

References 11 publications

(15 reference statements)

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“…These minerals have a general mineralogical composition matching that of the sediments (Bruthans et al, 2009), and are present in the form of sand inside the halite crystals.…”

Section: X-ray Resultsmentioning

confidence: 97%

“…The rock salt is folded into tight to isoclinal folds, with alternating white to grayish and reddish salt with varicoloured carbonate, siliciclastic, Fe oxides and volcano-sedimentary rocks and rarely anhydrite. The surface of the visited salt diapirs is usually covered by a broad variety of weathering surficial deposits with thicknesses from several centimeters to several tens of meters (Bruthans et al, 2009). These surficial deposits form a caprock, which prevents many salt diapirs from fast erosion .…”

Section: Geographical and Geological Setting Of The Salt Karst Areasmentioning

confidence: 99%

“…1 and Table 1 in Bruthans et al (2009). A typical trip to the salt karst area was three weeks long and took place in the winter to spring seasons (in January to May) and under various weather conditions with predominating dry weather but also in periods during and after low and high intensity rainfall (a rain event causing flash-flood with ca 10 years recurrence interval occurred in April 2009).…”

Section: Documentation and Sampling In The Fieldmentioning

confidence: 99%

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Secondary halite deposits in the Iranian salt karst: general description and origin

Filippi¹,

Bruthans²,

Palatinus³

et al. 2011

IJS

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This paper summaries 12 years of documentation of secondary halite deposits in the Iranian salt karst. A variety of secondary halite deposits was distinguished and classified into several groups, on the basis of the site and mechanism of their origin. Deposits formed: i) via crystallization in/on streams and pools, ii) from dripping, splashing and aerosol water, iii) from evaporation of seepage and capillary water, and iv) other types of deposits. The following examples of halite forms were distinguished in each of the above mentioned group: i) euhedral crystals, floating rafts (raft cones), thin brine surface crusts and films; ii) straw stalactites, macrocrystalline skeletal and hyaline deposits, aerosol deposits; iii) microcrystalline forms (crusts, stalactites and stalagmites, helictites); iv) macrocrystalline helictites, halite bottom fibers and spiders, crystals in fluvial sediments, euhedral halite crystals in rock salt, combined or transient forms and biologically induced deposits. The occurrence of particular forms depends strongly on the environment, especially on the type of brine occurrence (pool, drip, splashing brine, microscopic capillary brine, etc.), flow rate and its variation, atmospheric humidity, evaporation rate and, in some cases, on the air flow direction. Combined or transitional secondary deposits can be observed if the conditions changed during the deposition. Euhedral halite crystals originate solely below the brine surface of supersaturated streams and lakes. Macrocrystalline skeletal deposits occur at places with rich irregular dripping and splashing (i.e., waterfalls, places with strong dripping from the cave ceilings, etc.). Microcrystalline (fine grained) deposits are generated by evaporation of capillary brine at places where brine is not present in a macroscopically visible form. Straw stalactites form at places where dripping is concentrated in small spots and is frequent sufficient to assure that the tip of the stalactite will not be overgrown by halite precipitates. If the tip is blocked by halite precipitates, the brine remaining in the straw will seep through the walls and helictites start to grow in some places. Macrocrystalline skeletal deposits and straw stalactites usually grow after a major rain event when dripping is strong, while microcrystalline speleothems are formed continuously during much longer periods and ultimately (usually) overgrow the other types of speleothems during dry periods. The rate of secondary halite deposition is much faster compared to the carbonate karst. Some forms increase more than 0.5 m during the first year after a strong rain event; however, the age of speleothems is difficult to estimate, as they are often combinations of segments of various ages and growth periods alternate with long intervals of inactivity. Described forms may be considered in many cases as the analogues of forms found in the carbonate karst. As they are created in a short time period the conditions of their origin are often still visible or can be reconstructed. The d...

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“…These minerals have a general mineralogical composition matching that of the sediments (Bruthans et al, 2009), and are present in the form of sand inside the halite crystals.…”

Section: X-ray Resultsmentioning

confidence: 97%

Section: Geographical and Geological Setting Of The Salt Karst Areasmentioning

confidence: 99%

Section: Documentation and Sampling In The Fieldmentioning

confidence: 99%

See 1 more Smart Citation

Secondary halite deposits in the Iranian salt karst: general description and origin

Filippi¹,

Bruthans²,

Palatinus³

et al. 2011

IJS

Self Cite

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“…Evaporite glaciers, more than 300 m high, are presently flowing in the eastern fold belt of the Zagros Mountains, Iran, and former evaporite glaciers are widespread in the copper belt of the Democratic Republic of the Congo (Jackson et al 2003). Evaporite glaciers have complex and variable composition and thickness depending on the location of the glacier, from various subaerial environments to marine settings, and the geological and tectonic settings (Fletcher 1995Hudec and Jackson 2006;Bruthans et al 2009). In subaerial settings, components of the glacier include gypsum and or anhydrite (halite has generally been dissolved even in arid climates), entrained clasts of rocks through which the diapir ascended, cap rock clasts and other diagenetic products (calcite, dolomite, and celestite), insoluble components from the surrounding residuum, and variable fluvial input of sediments.…”

Section: The Jinding Sandstone and Its Oresmentioning

confidence: 99%

The world-class Jinding Zn–Pb deposit: ore formation in an evaporite dome, Lanping Basin, Yunnan, China

2016

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The Jinding Zn-Pb sediment-hosted deposit in western Yunnan, China, is the fourth largest Zn deposit in Asia. Based on field observations of the ore textures, breccias, and the sandstone host rocks, the ores formed in a dome that was created by the diapiric migration of evaporites in the Lanping Basin during Paleogene deformation and thrust loading. Most of the ore occurs in sandstones that are interpreted to be a former evaporite glacier containing a mélange of extruded diapiric material, including breccias, fluidized sand, and evaporites that mixed with sediment from a fluvial sandstone system. A pre-ore hydrocarbon and reduced sulfur reservoir formed in the evaporite glacier that became the chemical sink for Zn and Pb in a crustal-derived metalliferous fluid. In stark contrast to previous models, the Jinding deposit does not define a unique class of ore deposits; rather, it should be classified as MVT sub-type hosted in a diapiric environment. Given that Jinding is a world-class ore body, this new interpretation elevates the exploration potential for Zn-Pb deposit in other diapir regions in the world.

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“…The chemical compositions vary and consist of three members: evaporite minerals (gypsum and anhydrite), carbonates (dolomite and calcite) and silicates-oxides (mostly quartz, phyllosilicates and hematite). Halite is mostly leached out from surficial deposits even in arid climates (Bruthans et al 2009). The rock salt consisted mainly of halite as well as secondary halite deposits in Hormuz Fm which are usually found in an evaporate rock salt environment.…”

Section: History Structure and Distribution Of Hormuz Saltmentioning

confidence: 99%

Stratigraphy of Oligocene–Miocene salt deposits in the SE Persian Gulf

Sajadi

Baghbani

Daneshian

et al. 2015

Carbonates Evaporites

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The purpose of this study is lithostratigraphic investigation of Oligocene-Miocene salt deposits in the SE Persian Gulf. This study is based on lithostratigraphy and biostratigraphy data, gamma ray and sonic logs of nine drilled wells along southeast Persian Gulf to Strait of Hormuz. As a result, the Oligocene-Miocene deposits of this region were subdivided into four formations (Fms) which include Pabdeh Fm (Rupelian-Chattian), Asmari Fm (Rupelian-Aquitanian), Gachsaran Fm (Aquitanian) and Mishan Fm (Burdigalian). The salt and evaporated deposits situated between the Pabdeh and Gachsaran Fms which are assigned to the Aquitanian age. Finally the stratigraphical setting and distribution of the salt deposits are cleared.

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Surficial deposits on salt diapirs (Zagros Mountains and Persian Gulf Platform, Iran): Characterization, evolution, erosion and the influence on landscape morphology

Cited by 43 publications

References 11 publications

Secondary halite deposits in the Iranian salt karst: general description and origin

Secondary halite deposits in the Iranian salt karst: general description and origin

The world-class Jinding Zn–Pb deposit: ore formation in an evaporite dome, Lanping Basin, Yunnan, China

Stratigraphy of Oligocene–Miocene salt deposits in the SE Persian Gulf

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