Evaporites: Sediments, Resources and Hydrocarbons

Warren, John K.

doi:10.1007/3-540-32344-9

Cited by 657 publications

(733 citation statements)

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“…Most authors found only a few basic chemical types (4-5) of saline waters (brine type) with certain combinations of Na, Mg, Cl, SO 4 , HCO 3 and CO 3 (e.g., Eugster and Hardie, 1978;Williams, 1998;Warren, 2006). Hammer (1986) divided them into six types (Na-HCO 3 , NaCl, Ca-HCO 3 , Mg-HCO 3 , Na-SO 4 , Mg-SO 4 ) based on the 25 equivalence per cent (e%) dominance of the cations and anions, while according to multiple ion dominances, many subtypes of saline waters (at least 20-25) were described all over the world.…”

Section: Introductionmentioning

confidence: 99%

“…If groundwater chemistry is dominated by bicarbonate (HCO 3 > > Ca + Mg), there is an evidence that soda lake formation is dependent on low levels of dissolved calcium and magnesium among the cations as alkaline carbonates fall out of solution, which determines soda lake genesis (Grant, 2006;Warren, 2006).…”

Section: Introductionmentioning

confidence: 99%

“…Recently, Warren (2006) provided a detailed hydrological classification of nonmarine (athalassohaline) brines and associated evaporite minerals all over the world. He described the hydrogeological genesis of alkaline waters and the phase chemistry of sodium carbonate.…”

Section: Introductionmentioning

confidence: 99%

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Salinity and ionic composition of the shallow astatic soda pans in the Carpathian Basin

Boros

Horváth

Wolfram³

et al. 2014

Ann. Limnol. - Int. J. Lim.

103

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-We investigated the chemical characteristics of the astatic soda pans in the Carpathian Basin based on comprehensive new and archive data. Analysed parameters were salinity and ionic composition. The most frequent type of soda waters was the basic alkaline type (Na-HCO 3 ) that represented more than half of the natural soda pans. Besides 11 subtypes occurred. The second and third most frequent types were the chloride (13%) and sulphate subtypes (11%), with the secondary dominance of these anions. The other subtypes meant < 4% of the pans. Magnesium sometimes occurred as a secondary dominant cation beside sodium. Until now, this subtype of soda waters has not been published in any part of the world, because of the general rule of soda lake formation (depending on low levels of magnesium and calcium). We found a regionally constant correction factor [Salinity (mg.L x1 ) = 0.8 r El.Cond. (mS.cm x1 )] for confidentially estimating salinity from electrical conductivity in these habitats. Salinity varied between sub-(0.5-3 g.L x1 ) and hypersaline (> 50 g.L x1 ) ranges, with its mean value (y 4 g.L x1 ) in the hyposaline range (3-20 g.L x1 ). The basic alkaline type had random geographical distribution, while the other subtypes were restricted to certain regions of the Basin. The high number of subtypes reflects the high chemical diversity of alkaline soda pans in the relatively small territory of the Carpathian Basin.

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Section: Introductionmentioning

confidence: 99%

Section: Introductionmentioning

confidence: 99%

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Salinity and ionic composition of the shallow astatic soda pans in the Carpathian Basin

Boros

Horváth

Wolfram³

et al. 2014

Ann. Limnol. - Int. J. Lim.

103

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“…One of these rare occurrences of thick bischofite layers occurs on the southern edge of the Groningen High in the NE Netherlands, where it is solution mined by the squeeze mining technique (Fokker, 1995). Bischofite is the last mineral precipitating during a full evaporation cycle (Lotze, 1957;Warren, 2006). For its precipitation out of bittern brines, extremely arid conditions are required.…”

Section: A F Raith Et Al: Evolution Of Rheologically Heterogeneousmentioning

confidence: 99%

“…Our understanding of large-scale salt tectonics has grown tremendously over the last century (e.g. Jackson et al, 1996;Warren, 2006), but the internal deformation of evaporites, as can be observed in outcrops, mines and surface exposures (Jackson et al, 1990), is less well known. Our knowledge of this domain is making some progress, because the internal layering of salt bodies can now be studied at high resolution using modern industrial 3-D seismic reflection data (Van Gent et al, 2011;Cartwright et al, 2012;Fiduk and Rowan, 2012;Jackson et al, 2014Jackson et al, , 2015.…”

Section: Introductionmentioning

confidence: 99%

Evolution of rheologically heterogeneous salt structures: a case study from the NE Netherlands

Raith

Strozyk

Visser³

et al. 2016

Solid Earth

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Abstract. The growth of salt structures is controlled by the low flow strength of evaporites and by the tectonic boundary conditions. The potassium-magnesium salts (K-Mg salts) carnallite and bischofite are prime examples of layers with much lower effective viscosity than halite: their low viscosity presents serious drilling hazards but also allows squeeze solution mining. In contrast, intrasalt anhydrite and carbonate layers (stringers) are much stronger than halite. These rheological contrasts within an evaporite body have an important control on the evolution of the internal structure of salt, but how this mechanical layering affects salt deformation at different scales is not well known. In this study, we use high-resolution 3-D seismic and well data to study the evolution of the Veendam and Slochteren salt pillows at the southern boundary of the Groningen High, northern Netherlands. Here the rock salt layers contain both the mechanically stronger Zechstein III Anhydrite-Carbonate stringer and the weaker K-Mg salts, thus we are able to assess the role of extreme rheological heterogeneities on salt structure growth. The internal structure of the two salt pillows shows areas in which the K-Mg salt-rich ZIII 1b layer is much thicker than elsewhere, in combination with a complexly ruptured and folded ZIII Anhydrite-Carbonate stringer. Thickness maps of supra-salt sediments and well data are used to infer the initial depositional architecture of the K-Mg salts and their deformation history. Results suggest that faulting and the generation of depressions on the top Zechstein surface above a Rotliegend graben caused the local accumulation of bittern brines and precipitation of thick K-Mg salts. During the first phase of salt flow and withdrawal from the Veendam area, under the influence of differential loading by Buntsandstein sediments, the ZIII stringer was boudinaged while the lens of Mg salts remained relatively undeformed. This was followed by a convergence stage, when the K-Mg salt-rich layers were deformed within the inflating salt pillows. This deformation was strongly disharmonic and strongly influenced by folding of the underlying, ruptured ZIII stringer, leading to thickening and internal deformation of the K-Mg salt layers.

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The honeycomb terrain on the Hellas basin floor, Mars: A case for salt or ice diapirism

et al. 2016

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We present quantitative plausibility studies of potential formation mechanisms for the “honeycomb” terrain on the northwestern Hellas basin floor. The honeycomb terrain is a unique landscape of ~10.5 × 5 km wide, mostly cell‐shaped depressions that are arranged in a regular, dense pattern covering ~36,000 km2. We argue against the honeycombs being (peri)glacial landforms (till rings, iceberg imprints, and thermokarst) or the result of igneous diapirism, as terrestrial analogs do not reproduce their key characteristics. Fossilized impact melt convection cells also appear to be an unsuitable interpretation, as melt solidification should not permit such structures to be retained. We present arguments in favor of salt or ice diapirism as honeycomb formation models. Honeycomb‐sized diapirs could be formed by a ~2 km thick salt layer (~72,000 km3 for the entire honeycomb terrain), which might have been derived from the highlands north of Hellas Planitia—an area of abundant chloride signatures and intense snowfall according to ancient Mars climate models. Nearby volcanic activity ~3.8 Ga ago potentially enabled recurring phases of (probably salty) meltwater runoff (as indicated by meandering channels) and might therefore have enabled evaporite deposition in the Hellas basin. Being twice as buoyant as salt, water ice would require an only ~1 km thick layer (i.e., ~36,000 km3) to form honeycomb‐sized diapirs, which would be in agreement with a likely ~2 km thick ice stability zone beneath the Hellas basin floor. However, it would remain an open question as to why we find only one such ice diapir landscape on Mars.

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Evaporites: Sediments, Resources and Hydrocarbons

Cited by 657 publications

References 0 publications

Salinity and ionic composition of the shallow astatic soda pans in the Carpathian Basin

Salinity and ionic composition of the shallow astatic soda pans in the Carpathian Basin

Evolution of rheologically heterogeneous salt structures: a case study from the NE Netherlands

The honeycomb terrain on the Hellas basin floor, Mars: A case for salt or ice diapirism

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