Salty Matters

The Blog is written by me, John Warren. Once every three or four weeks or so I will post an article or two on an evaporite topic that has piqued my interest. On the Saltwork Publications webpage (under "the Works") there is a growing library of pdfs and epubs based on these blogs. These articles on the website have much higher resolution extractable graphics in than in the blog. There is also a link to this set of pdfs and epubs on the home page (www.saltworkconsultants.com).

Non-solar thick salt masses: Part 1 - Mixing zone and cryogenic (freeze-dried) salts

John Warren - Saturday, May 18, 2019

Introduction

Conceptually, what defines evaporite sediment is broad, within the general theme that the rock was precipitated initially during solar heating of a brine. Heating drives the loss of water as vapour and concentrates of the residual brine to elevated salinities where a suite of evaporite salts precipitate (Babel and Schreiber, 2014; Warren 2016). In a modern marine-fed brine pan the precipitative sequence evolves from carbonate through gypsum, to halite and on into the various bittern salts (Figure 1).


But, evaporite salts are also highly reactive. Even in a simple single-pan evaporation scenario, crystallising salts tend to alter, backreact, replace, dissolve and reprecipitate. Then, as bedded sedimentary salts attain the subsurface and are exposed to increasing temperature and pressure, they continue to alter. Hydrated minerals, such as gypsum or carnallite transform into anhydrous phases such as anhydrite or sylvite. At the same time, thick halite beds tend to flow into halokinetic salt structures with a complete loss of depositional textures.

Some authors restrict the term "evaporite" to sediments forged by evaporation and use "saline deposit" or "salt deposit" for units formed not only by evaporation but also by ongoing alteration, cooling, heating or salting out in hydrothermal and diagenetic settings. Hence, the term salt structure rather than evaporite structure to describe many subsurface features encompassing the outcomes of halokinesis (salt flow). Some authors have suggested other names for the various bedded salt rocks precipitated by mechanisms other than solar heating of a brine; however, these names (burial salt, hydrothermal salt, reactionite, mixing precipitate, thermalite, replacementite, etc.) are not in general use in the sedimentological community.

In the subsurface sedimentary realm, most of the diagenetic processes described in preceding paragraphs have acted on a mass of salt first deposited by solar heating of brine and so are considered "true evaporites". This is so even though textures, total volumes of salts and mineralogies may have changed. Diagenetic processes acting on evaporite masses may also have transposed portions of the original salt mass into nearby saline cements within adjacent non-evaporite lithologies. These diagenetic or burial salt sediments lie outside the focus of this present series of articles, which will discuss mechanisms capable of precipitating large volumes of salts on or near the earth's surface without solar-driven heating of a brine (see Warren, 2016; Chapter 1 and 8 for a discussion of diagenetic or burial salts).

Cryogenesis, brine-mixing and mantle-driven thermal processes are the main surface and shallow-subsurface processes capable of precipitating significant volumes of non-evaporite salts. Many of the salt bodies precipitated in this way have similar mineralogies to those found in evaporite successions. So this, and the next Salty Matters article focus on mechanisms and products created by non-evaporite precipitation. I will attempt to define criteria that allow their separation from "true" evaporites. In this first article, we focus on mechanisms of brine mixing and cryogenesis, in the second we shall look at salt masses crystallising from fluids created and driven by mantle heating and cooling.

Some basic salt chemistry

Before that, we need to discuss a few basic chemical properties that define a crystal's response to heating and cooling of an enclosing brine. The questions we must ask are; in the ambient conditions are we dealing with influencing a prograde or retrograde salt phase and does the particular salt of interest undergo congruent or incongruent dissolution?

Prograde or retrograde salt?

A prograde salt crystallises as a brine cools and dissolve as brine is heated. With prograde salts, the average kinetic energy of the molecules in brine increases with temperature. The increase in kinetic energy allows solvent molecules to more effectively break apart the solute molecules; hence solubility increases with temperature and decreases with cooling. Halite and sylvite are both prograde salts (Figure 2a). When a shallow surface brine rich in either NaCl or KCl at say 45-50°C cools overnight, it will precipitate halite or sylvite-carnallite on the pan floor. If it sinks into an underlying porous salt bed and cools, it will precipitate as intercrystalline cement. This is happening beneath the salt flats of Dabuxum Lake in the Qaidam Basin of China where intercrystalline carnallite fill pores in a halite bed. In the deeper crust, with ongoing magmatic heating, the solubility of sodium chloride increases to where just below its critical point (≈400°C), salt content in a NaCl brine could be as high as 40 weight percent (see next article).

 

A retrograde (temperature-inverse) salt precipitates with increasing temperature and dissolves if it sits in a cooling saturated brine. Anhydrite is a retrograde salt and like all retrograde salts produces heat when dissolved in water (exothermic reaction). In an exothermic reaction the resulting additional heat shifts the equilibrium towards the reactants (Ca + SO4 --> CaSO4) (Figure 3b). In contrast, the hydrated form of CaSO4, gypsum, follows a prograde solubility curve, whereby in the temperature range where gypsum is the stable CaSO4 phase (<40-45°C) it is increasingly soluble with increasing temperature (Figure 3a). At higher temperatures (>45-50°C) both gypsum (where stable) and anhydrite possess retrograde solubility. Thus, when two anhydrite-saturated waters of different temperatures mix in the subsurface, the result is supersaturated brine with a propensity to precipitate anhydrite. A combination of retrograde solubility and brine mixing helps explain why anhydrite is a commonplace hydrothermal precipitate in mid-oceanic ridges and smoker chimneys (see next article).

On land, beneath the immediate surface of Abu Dhabi and Saudi sabkhas, the heating of desert playa and sabkha waters, rising through the capillary zone, to temperatures above 35°C drives the precipitation of CaSO4 (as nodular anhydrite) in a fashion that Wood et al. (2002, 2005) terms a sabkha thermalite (see Warren, 2016 for sabkha discussion). A reverse thermal gradient (upward cooling) in the winter sabkha permits dissolution of some of the previously precipitated retrograde minerals. Because the negative thermal gradient is less in the winter than the positive thermal gradient of the summer, but with nearly the same water flux, the cooling water cannot dissolve all of the mineral mass that precipitated in the previous summer. Thus, there is a net accumulation of retrograde (thermalitic) anhydrite nodules and layers in the capillary zone of an Abu Dhabi sabkha (Wood et al. 2005 ).

Brine mixing drives precipitation or dissolution of salts

Van’t Hoff’s work in physical chemistry, which won him the first Nobel Prize in Chemistry, showed that salts would precipitate at chemically-suitable brine interfaces. At that interface, all that is needed is a mixing of waters of two saturation states, with respect to the mineral of interest (Figure 3a). When two waters that are saturated with a particular salt phase are mixed, the resulting solution can be undersaturated or supersaturated with respect to that particular phase (Figure 3a). The saturation state during mixing depends on the convex or concave shape of the solubility curve for the mineral phase of interest and the parameter of interest (ion concentration, temperature, salinity, etc.). The only requirement is that the solubility curve for that particular component is nonlinear.

 

Raup (1970, 1982) in several experiments showed how halite and gypsum could be precipitated by the mixing of two seawater brines of differing salinity and densities. Figure 3b plots experimental results for the mixing of various low and high-density seawater brines and the resulting amount of gypsum precipitated (Raup, 1982). A similar plot can be drawn for the mixing of more saline NaCl (seawater) brines (Figure 4a, b; Raup, 1970).

Hence blending brines with different temperatures or salinities can be an important salting-out mechanism in the calcium sulphate (gypsum/anhydrite) salt system where gypsum follows a nonlinear solubility trend, as do saturated brines in a halite-MgCl2 bittern system (Raup, 1970, 1982). Figure 2b shows the solubility curves of both gypsum and anhydrite plotted with respect to increasing temperature in pure water. For gypsum, it clearly shows that when two gypsum-saturated waters with different temperatures mix in its stability range then the resulting solution is undersaturated and so gypsum tends to dissolve (Upper left curve in Figure 2b). In contrast, gypsum drops out of solution when two brines of differing density mix, with the amount of gypsum dependent on the density contrast between the two brines (Figure 3b).

Anhydritic solubility drives complex diagenetic effects when CaSO4-saturated brines mix via dispersion into adjacent less saline brines (Figure 2b). This happens in brine reflux systems where dense CaSO4-saturated brine plumes, derived at the surface at halite saturation, sink into and interact with less saline brines held in underlying or adjacent anhydritic carbonates. If the temperature remains near constant the tendency in this zone of dispersion or mixing is to dissolve gypsum, creating vugular porosity in the interval below or adjacent to a thick salt sequence. If temperature decreases and the brine plume cools, with little change in ionic proportions due to mixing, then the tendency is to precipitate anhydrite. It is not a simple system, with temperature and mixing processes pulling the brine chemistry in opposite directions.

A similar salting-out of halite occurs when halite-saturated brine mix with either MgCl2 or CaCl2 brine (Figure 4a, b, respectively). In potash basins, MgCl2-saturated brines are created by the incongruent dissolution of carnallite, while CaCl2 brines can typify the brine products of basinal hydrothermal waters. In both cases, the result is a sparry, relatively inclusion-free halite cement. Depending or the location where this mixing occurred, the cement can be part of a bedded carnallite unit that is converting to sylvite, or it can be localised in a fracture fill or form an intergranular cement in a non-evaporite host lithology.


Salt precipitation, driven by brine mixing, occurs in many stratified at-surface and shallow subsurface diagenetic interfaces in evaporitic settings. But, it is in the context of the mixing of deeply circulating mantle brines that it may be capable of precipitating significant volumes of salt and it in this context we shall discuss it further in the next article.


Cryogenic salts

Cryogenic brines and associated salts require temperatures at or below the freezing point of the liquid phase. These salts crystallise from a cold, near-freezing, residual brine as it concentrates via the loss of its liquid phase, which is converting/solidifying to ice (Figure 5a). As brine concentration increases, the freezing temperature decreases and minerals such as ikaite, hydrohalite, mirabilite, epsomite, potash bitterns and antarcticite can crystallise from the freezing brine (Figure 5a, b; Table 1; Warren, 2016; Chapter 12). Brine freezing ends when the phase cehemistry attains the eutectic point is reached. This is the point when all compounds (including H2O) pass to the solid state. Depending on the initial mineralization and compostion of the brine, the eutectic point is reached between -21 and -54 °C (Marion et al., 1999; Strakhov, 1970).


Cryogenic concentration of seawater precipitates mirabilite at four times seawater salinity and hydrohalite at eight times. In contrast, evaporating seawater precipitates gypsum at 4-5 times the original concentration and halite and 10-11 times (Figure 6). Evaporative gypsum precipitation decreases the relative proportions of both Ca and SO4 in the brine, while cryogenic precipitation of mirabilite decreases the sulphate proportion and drives the inflexion of the Na cryogenic curve slightly earlier than Na inflexion created by the precipitation of evaporative halite. In both the freezing and the evaporation situations, the brine remains chloride dominant prior to bittern crystallisation. Freezing seawater becomes increasingly sulphate enriched to where sulphate levels exceed sodium around 20 times the initial concentration. Evaporating seawater remains a Na-Cl dominant brine until the bittern stage is reached around 60 times the initial concentration (Warren, 2016, Chapter 2).


Mirabilite (NaSO4.10H2O) is one of several sodium sulphate salts and is stable in sulphate brines at temperatures lower than a few centigrade degrees (Figure 7a). Hence, it is a commonplace cold-climate lacustrine precipitate (Figure 8a-d; Table 1). Mirabilite beds are commercially exploited in colder climates; their latitudinal and altitudinal occurrences illustrate an interesting climatic dichotomy inherent to economic deposits of the various sodium sulphate salts. One sodium sulphate grouping of exploited deposits is characterised by mirabilite precipitated via brine freezing, as in the Great Salt Lake, Karabogazgol and Hedong (Yucheng) salt lake (Table 1 and illustrated in Figure 8a-d). The other sodium sulphate salt grouping is characterised by varying combinations of glauberite (CaSO4.Na2SO4)/bloedite-astrakanite (Na2SO4.MgSO4.4H2O) salts, which crystallised at higher temperatures via the evaporation of continental brines in saline groundwater sumps in warm to hot arid climates (as discussed in Warren, 2016, Chapter 12).


The climatic dichotomy reflects the fact that sodium sulphate solubility in water changes as a nonlinear function of temperature (Figure 7a). Below 1.2°C, ice and mirabilite tend to precipitate as seawater or a sodium sulphate brine freezes. As the temperature increases above 0°C, increasing amounts of hydrous sodium sulphate (as the decahydrate, mirabilite) become soluble, while the anhydrous form (thenardite- NaSO4) becomes the precipitative phase in brines saturated with respect to the sodium sulphate. At 32.4°C in pure water, a transition point on the solubility curve is reached, whereby mirabilite melts in its water of crystallisation and thenardite crystallises. Presence of other dissolved salts changes the transition temperature and solubility characteristics of sodium sulphate due to the double salt effect.


Cryogenesis in saline lacustrine sumps

Every year, once the water temperatures drop below 5.5-6°C in late November in Karabogazgol, mirabilite precipitates as transparent crystals on the embayment bottom. The crystals are then transported by wind and wave action, especially during winter storms, into low dunes lining shore-zone (Figure 8b). By mid-March when the bay waters are heated to over 6°C, the mirabilite on the bay floor begins to redissolve. By July–August the entire precipitated mirabilite crop in the bay has redissolved. Historically, the period from November through March was a period of ‘‘harvesting’’ mirabilite on the bay shores. In summer with its arid climate, any remaining strandzone salt converts to thenardite (Na2SO4), and this too was gathered at the end of each summer.


Below the floor of Karabogazgol are four NaSO4 beds that are likely cryogenic remnants from colder climatic periods over the last 10,000 years (Figure 9; Karpychev, 2007). Back then, large amounts of mirabilite formed each winter, much like today but, unlike today, the colder more humid glacial climate meant the bay was not as subject to summer desiccation and warming. Dense residual bottom brines were perennially ponded and so preserved a summer-halite sealing bed. This allowed the underlying mirabilite/epsomite winter precipitates to be preserved across the lake floor. During the following winter, the process was repeated as mirabilite/epsomite/halite couplets stacked one atop the other to create a future ore horizon. In time, the combination of groundwater and exposure, especially nearer the Gulf’s strandzone, converted most of the mirabilite, along with epsomite, to astrakanite, and then both phases to glauberite in the upper three beds. This explains the association of the richer glauberite zones with the lake edges (Figure 9a; Strakhov, 1970). Water of crystallisation released by the subsequent mirabilite to thenardite conversion, slightly diluted any strong residual brines, facilitating a dominant sodium-sulphate mineral and brine composition across the bay (Kurilenko et al., 1988).

Winter mirabilite also crystallises cryogenically from Kuchuk Lake brines on the Kulunda Steppe, southwest of Novosibirsk, western Siberia (Kurilenko, 1997; Garrett, 2001. The lake area is 170 km2, and brine depth is around 3.2 metres. In 1938 that lake was estimated to contain some 540 million mt of equivalent sodium sulfate. Thick, glassy mirabilite occurs as two crystalline layers, the upper one is around 3 m thick, and both layers are pure containing <1% other soluble salts. In total, the crystalline mirabilite interval ranges up to 7 m thick, covers around 133 km2 and is overlain by a 0.05- to 2-m thick unconsolidated interval of mud and salt oozes. The ooze typically contains some 40.5% salts, 20.6% water, and 38.9% insolubles (including considerable gypsum). Much of the mirabilite in the upper ooze layer has been transformed into thenardite, with the previous water of crystallisation supply much of the dense brine held in the ooze, which also contains halite, glauberite, hydrohalite and epsomite.

Mirabilite crystallises from the lake brine during the winter and cool summer evenings (volume estimated to be ≈ 340-580 thousand mt/yr of mirabilite). Then, during the warm summer months, some of it converts to thenardite. A limited amount of insoluble accumulates with the crystals, forming thin layers of mud with the thenardite. Brine in the lake has a 10-31% soluble salt content, depending upon the season and lake level. Every every three years, at the end of summer this brine is pumped to solar ponds to allow cryogenic mirabilite to crystallise during the autumn (a process similar to the production of mirabilite in the Canadian Salt Lake (Warren 2016, Chapter 12). Residual brine in the ponds is returned to the lake before winter sets in, and the ponds are harvested as needed for the production of sodium sulfate (Charykova et al., 1996). For most of a year, the lake's surface brine is a magnesium chloride water, but during the summer it changes to a sodium sulfate base, because of the dissolving of the underlying mirabilite, thenardite, and glauberite held in the lake floor oozes.

Ebeity (Ebeyty) Lake, located 110 km west of Omsk, is another cryogenic salt lake with a cyclic pattern of mirabilite crystallising in the winter and having it dissolve in the summer (Garrett, 2001; Kolpakova et al., 2018). Brine concentration can reach 30-31% total salts by the end of summer and can begin to crystallise halite (which usually dissolves in the spring). Mirabilite deposition starts when the brine temperature in the lake is less than 18-19°C (which can be as early as August or September). At 0°C, 70% of the sodium sulfate has crystallised from the lake brine. At -10°C, 85% has been deposited, and at -15°C 98%. At -7°C some ice crystallizes with the mirabilite, and at -21.8°C hydrohalite forms. The lake does not freeze solid because of the insulating effect of surface layers of snow on top of floating mirabilite rafts, but brine temperatures of -23.5°C have been recorded (Strakhov, 1970). The winter deposit of mirabilite, with some hydrohalite, covers the entire lake bottom is 25-30 cm thick and is quite pure. Laboratory tests have shown the soluble salts in this mirabilite, including hydrohalite, can be almost completely removed (i.e., reduced to 0.08%) by a single stage of washing.

Hydrohalite is a stable precipitate in a freezing brine only when the water temperature is below 0°C. In a NaCl–H2O system in the laboratory, hydrohalite is a stable phase that begins to precipitate cryogenically at temperatures below 0.12 °C, forming hydrohalite and a brine solution until it reaches the eutectic point for a solution saturated with NaCl at −21.1°C, where the remaining solution freezes (Figure 7b). Above 0.12 °C hydrohalite melts incongruently and decomposes to NaCl and a NaCl-saturated solution, losing 54.3% of its volume (Craig et al., 1974, 1975; Light et al., 2009). Hydrohalite (NaCl.2H2O) crystals have pseudo-hexagonal cross sections and are found in a number of modern cold saline lakes and springs (Table 1, Figure 8e-f).

Cryogenesis in salty springs

The mutual occurrence and downdip evolution of mirabilite/thenardite and hydrohalite/halite in brine spring encrustations (barrage structures) downdip of Stolz diapir on Axel Heiberg Island in the Canadian Archipelago illustrate the ephemeral nature of cryogenic salts on the Earths surface, even in extremely cold settings (Fox-Powell et al., 2018; Ward and Pollard, 2018). The halite-exposed core of the Stolz dome rises some 250 m above the adjacent flood plain, while the salt/hydrohalite deposit occurs autochthonously within a narrow, steep-sided tributary valley carved by a small stream fed mainly by perennial groundwater discharge emanating from the base of the diapir. The host valley begins abruptly at the spring outlet and is incised through surficial colluvial and glacial sediments into steeply dipping bedrock (shale). The Stolz diapir is the only diapir within the archipelago where the halite core is exposed, and the surface is extensively karstified with a suffusion cover, along with several large sinkholes and collapse structures.


The cryogenically influenced part of the at-surface salt deposit is approximately 800 m long and is thickest at the spring outlet (≈4.0 m) and gradually thins down-valley until it fans out, creating a salt pan that extends 300 m into the Whitsunday River floodplain. The morphology of the deposit is characterised by a series of salty barrage structures that staircase down the valley until the dispersing and dissolving at the valley opening. The barrages are constructed of salts but morphologically resemble typical fluvial travertines and tufas and are predominantly curvilinear with a downstream convexity, particularly the larger dams in the upper valley.

Sub-zero air temperatures persist at the site for at least ten months of the year, and the spring’s outlet temperature is relatively constant at −1.9°C ±0.1°C, confirming the presence of permafrost and so facilitating the precipitation of mirabilite and hydrohalite via freezing of spring waters (Figure 8f). In July air temperatures reach 5° - 6°C.

Although initial precipitates in the permafrost zone of the spring outflow are cryogenic (mirabilite and hydrohalite) the presence of these cryogenic salts in the spring precipitates is ephemeral (Figure 10).

The main body of a deposit is layered (Figure 4a, b) with alternating light and dark bands interpreted by Ward and Pollard (2018) as alternating periods of winter hydrohalite deposition and periods of summer pool drainage, when hydrohalite decomposes, and halite/thenardite sediment is deposited (Figure 11). As layers likely reflect an annual couplet cycle, then single winter accumulations can be as thin as a few millimetres in some parts of the deposit and as much as half a meter in others. It appears the accumulation phase ends as pools drain in early May corresponding with mean daily temperatures rising above 0°C. The darker layers are generated during summer as the hydrohalite decomposes leaving a granular halite crust with a veneer of fine clastic sediment transported into the deposit by wind, rain and runoff from adjacent slopes (during the spring snowmelt). The contact between the primary sediment and halite is abrupt and unconformable. The excavation of the deposit revealed numerous thin frozen layers (Figure 4c). These layers first appear ≈47cm below the surface, and overlying unfrozen material is considered analogous to an active layer in permafrost (Ward and Pollard, 2018). Samples of frozen salt collected from this layer and exposed to ambient air temperatures in summer reverted to a mixture of brine and halite grains (Figure 4d-e). It is not clear if these are residual hydrohalite layers preserved by thicker precipitate accumulations or if they represent secondary hydrohalite formation.


The lack of mirabilite or thernadite within the upper portion of the stream/spring deposit is thought to be due to the low kinetic rates of precipitation for sulfate salts (Ward and Pollard, 2018). Below the halfway point, thernadite is present (Figure 8f). This is also reflected in the SO4 concentrations along the spring in winter, as the precipitation of mirabilite removes sulfate ions from solution beyond the halfway point. Based on the morphology of the crystals observed in the deposit, the low concentration of sulfate ions compared to chloride ions, as well as the extensive identification of halite in the XRD samples, the deposit is dominated by hydrohalite (not mirabilite), which decomposes to halite in the summer and at the same time the mirabilite that is present dehydrates to thenardite (Figure 11).

Glacial and sea-ice cryogenesis

Whenever polar seawater freezes, salts precipitate in the increasingly dense residual brines held in inclusions or fissures in the ice (Butler et al., 2016). Salts that are known to precipitate within the freezing brine include CaCO3.6H2O (ikaite), Na2SO4.10H2O (mirabilite), NaCl.2H2O (hydrohalite), KCl (sylvite), and MgCl2.12H2O (magnesium dichloride dodecahydrate), while hydrohalite is the most abundant salt to precipitate in sea ice (Light et al., 2009). In the seawater system, hydrohalite begins to precipitate at -22.9C, and further cooling results in additional precipitation until the source of Na is exhausted at the eutectic (Figure 7b).

Salts do not only accumulate in sea ice. As dense brines and inclusion waters in flowing glacial ice sink into underlying rocks they can accumulate in ice sheet fissures at the base of the ice, or in load-induced fractures in the ice understory (Herut et al., 1990). Residual dense interstitial saline brines are found in pore waters extracted from deep cores sampling submarine sediments in McMurdo Sound, Antarctica (Frank et al., 2010). It seems that when ice sheets retreat, the at-surface cryogenic salts dissolve into a freshening at-surface hydrology, but dense hypersaline brines remain behind in deep fissures, held and preserved in the rock fractures (Starinsky and Katz, 2003).

In the extreme setting of at-surface brine freezing in small saline depressions in the Dry Valleys of Antarctica, a solid form of calcium chloride, antarcticite, grows cryogenically in what is probably the most saline perennial natural water mass in the world (47% salinity in Don Juan Pond, Antarctica; Figure 8g-h; Horita et al., 2009).


Mirabilite beds are known to be exposed atop ice floes of the Ross Ice Shelf near immediately down dip of the Hobbs glacier, on Cape Barne on Ross Island and in the vicinity of Cape Spirit, Black Island (Figure 12a; Brady and Batts, 1981). The bed is made up of relatively pure mirabilite that in places is more than a metre thick (Figure 12b). It is exposed in three coast-parallel ice pressure ridge systems and may not be continuous between the three sampling sites. According to Brady and Batts (1981), the mirabilite formed in response to a recent retreat of the Ross Ice Shelf that began some 840 years ago.

The upper contact of the ice beneath the McMurdo mirabilite bed is not conformable as there are often small irregularities and undulations in its surface ranging from 2 to 6 cm high (Figure 12b). These undulations control the thickness of a silty sand interval (0-8cm thick) separating the ice from the mirabilite. The upper surface of the basal sediment layer defines a sharp conformable contact with the overlying mirabilite bed. This basal sediment layer is devoid of internal bedding and consists of 80% glacial flour mixed with sand and small pebbles. The sediment also contains many ice-crushed fragments of marine diatoms and sponge spicules (< 10 µm long).

The overlying mirabilite bed is massive up to 1/2m thick and primarily made up of transparent cm-scale crystal clusters. Locally crystals can aggregate into large granules up to 95 mm across, that when exposed to air are coated by an anhydrous sodium sulphate powder rind Although there is no apparent bedding in the mirabilite bed, small pods and layered stringers of pebbly sand do occur. These are usually parallel or sub-parallel to the salt bed layer itself and vary in thickness from 0 to 12 cm. Broken shell fragments occur as rare isolated individual fragments in the salt. When the mirabilite is dissolved in distilled water, some fine mud and rare sand grains are recovered, as well as a perfectly preserved flora of non-marine diatoms.

A lag of sediment, pebbles, cobbles, and boulders covers the mirabilite bed. The majority of the class are erratics, some of which are striated and come from the McMurdo alkaline volcanic province. There are also some erratics of gneiss, granite, and sandstone from continental suites. This lag is mostly overlain by a non-marine microbial mat (0-26 cm thick) but, in some places, the mat underlies or is mixed with the boulder lag. One mat sample collected 4 m above the level of the pool-and-channel systems on a pressure ridge at site 1, yielded a radiocarbon age of 870±70 years n.p. This single date cannot be used to date the whole mat since algae are still growing in pools in small depressions atop the salt deposit. The algal mat contains non-marine diatoms, but these are not as numerous as in nearby pools on the present-day ice shelf.

Debenham (1920) suggested that the mirabilite he had observed on the Ross Ice Shelf was formed under the ice shelf by precipitation from brines. But it is unlikely that extensive linear pods and beds of friable salt could be brought directly to the surface by anchor ice; furthermore, the salt beds contain non-marine diatoms that indicate surface precipitation (Brady and Batts, 1981). Since non-marine diatoms have only settled in the salt itself, it would seem that the basal sediment layer was formed immediately after the injection of a sub-ice-shelf brine and before non-marine algal production in the brine pools.

Hence, Brady and Batts (1981) conclude that mother brines first formed underneath an ice shelf from freezing sea-water. These brines were displaced to the ice-shelf surface by the weight of a large area of thick ice shelf as it grounded. Fine marine sediment carried in suspension by these brines settled to form an irregular thin discontinuous basal sediment layer containing marine diatoms. Mirabilite then crystallised cryogenically from this brine. During precipitation of the massive mirabilite beds, some non-marine diatoms, which can tolerate the high salt content of Antarctic saline lakes, were deposited with the salt. After the deposition of the mirabilite, massive non-marine algal production occurred, forming a thick irregular mat up to 26 cm thick on the mirabilite surface.

Mirabilite beds lying on the Ross Island coast near Cape Barne and on the mainland near Hobbs Glacier likely formed in the same manner as those at Cape Spirit. That is, they were stranded on the coast as the ice shelf retreated to its present position in the south of McMurdo Sound during the last interglacial period.


Extraterrestial cryogenic salts

Cryogenic gypsum is released via ice ablation and is spread widely by katabatic winds across the circumpolar Martian dunefields (Table 2). Hydrated and calcium perchlorate cryogenic salts grow seasonally in soils of Mars and typify slope lineae on parts of the Marian surface Lineae activity is possibly tied to periodic release of liquid water in paces on the Martian surface. More than 3 billion years ago, evaporitic halite once precipitated in impact sumps on the surface of Mars.

Cryogenesis explains the presence of hydrated magnesium sulphate salts in megapolygonal ice-crack fissures that crisscross the icy surfaces of Europa and Ganymede (moons of Jupiter) (Table 2; (Figure 13). The presence of hydrated magnesium sulphate and sodium carbonate salts indicates the presence of liquid salty oceans up to 100 km deep below an icy crust that is tens of kilometres thick (McCord et al., 1998; Craft et al., 2016. The fissures indicate an icy type of plate tectonics driven by strong tides in response to the varying gravitational pull of nearby Jupiter. Similar plumes of icy saline water escape from cracks and cryovolcanoes on the surface of Enceladus, an icy moon that circle Saturn. Spectral analysis shows the escaping plumes of Enceladus contain a variety of sodium and potassium salts (Postberg et al., 2011.


Recognition of ancient terrestrial cryogenic salts

Outside of relatively unaltered cool-temperature Quaternary lacustrine, permafrost and ice examples, as listed in Table 1, dehydration linked to the heating inherent to burial diagenesis will create mineralogical and textural difficulties in reliably interpreting the remains of ancient cryogenic salt beds. This is because all ionic salts forming in ambient surface conditions become metastable in the subsurface as they experience increased temperatures, pressures and evolving pore-fluid chemistries inherent to the diagenetic realm (Warren, 2016).

Across all subsurface and re-exhumed ancient examples, the original low-temperature cryogenic salts (mirabilite, hydrohalite) will be long gone. Anhydrous salty remnants (thenardite, halite) may be preserved but are typically altered, replaced and dissolved. This makes it more challenging to assign a depositional setting to a cryogenic salt than it is to a typical evaporite.

In their study of Miocene lacustrine thenardite in the Tajo Basin, Spain, Herrero et al. (2015) used three main criteria to suggest the conversion from a cold climate mirabilite precursor They were; 1) inclusion chemistry in the thenardite, 2) cooler climate mammal fauna synchronous with deposition of sodium sulphate salts and, 3) widespread dewatering structures tied to a burial transition from mirabilite to thenardite. A perusal of the depositional settings in the Quaternary examples listed in Table 1, underlines the conclusion that a glaciogenic association should be added as a fourth recognition criterion. Almost every case is either underlain or overlain by varying combinations of glacial till, glacial flour or glacial laminites with dropstones (Table 3).


In terms of pre-Quaternary deposits of sodium sulphate salts, it was noted by Warren (2010, 2016), that the greater majority of economic deposits are Neogene sediments. Pre-Neogene cryogenic deposits are typically so diagenetically altered that no significant volumes of the original metastable NaSO4 cryogenic salts remain. Across all pre-Neogene greenhouse climate settings, that is across times that lack permanent polar ice sheets, there is little documentation of preserved volumes of cryogenic salts. Worldwide warmer temperatures mean it is unlikely there were extensive cryogenic salt beds. This leaves past periods in Earth history when the planet was in ice-house mode as possible times of cryogenic salt deposits were possible. As yet, no pre-Neogene cryogenic salt beds are known. Mirabilite/hydrohalite deposits have been inferred to be reasonable at tropical latitudes during the Neoproterozoic snowball period (Light et al. 2009; Carns et al., 2015)). Their presence has bee inferred to have increased albedo in tropical ice sublimation regions and so modify climate models, but as yet no evidence of their existence is known either then or in younger Ordovician or Permo-Carboniferous ice-age sediments. Likewise, the presence of glauberite in Permian lithologies is not diagnostic; glauberite forms from evaporating marine waters at times of MgSO4 -enriched oceans (Hardie 1985; Warren, 2016).

Cryogenic salts are an extreme end-member of the concept of "the salt that was." Across past geological time, beyond Neogene remnants, even with isotopic and inclusion techniques, it is next to impossible to identify a cryogenic evaporite reliably.

As W. Edwards Deming (Engineer and statistician, 1900-1993) once said "...Without data, you're just another person with an opinion."

References

Alderman, S. S. J., 1985, Geology of the Owens Lake evaporite deposit, in B. C. Schreiber, and H. L. Harner, eds., Sixth international symposium on salt, v. 1, Salt Institute, VA, p. 75-83.

Bąbel, M., and B. C. Schreiber, 2014, 9.17 - Geochemistry of Evaporites and Evolution of Seawater, in H. D. Holland, and K. K. Turekian, eds., Treatise on Geochemistry (Second Edition): Oxford, Elsevier, p. 483-560.

Bowser, C. J., T. A. Rafter, and R. F. Black, 1970, Geochemical evidence for the origin of mirabilite deposits near Hobbs Glacier, Victoria Land, Antarctica: Mineralogical Society America Special Paper, v. 3, p. 261-272.

Brady, H. T., and B. Batts, 1981, Large salt beds on the surface of the Ross ice shelf near Black Island, Antarctica: Journal of Glaciology, v. 27, p. 11-18.

Braitsch, O., 1964, The temperature of evaporite formation, in A. E. M. Nairn, ed., Problems in palaeoclimatology: New York, Wiley, p. 479-490.

Butler, B. M., S. Papadimitriou, A. Santoro, and H. Kennedy, 2016, Mirabilite solubility in equilibrium sea ice brines: Geochimica et Cosmochimica Acta, v. 182, p. 40-54.

Charykova, M. V., 1996, The Hydrochemical Regime of Lake Kachuk: Water Resources, v. 23, p. 650-655.

Craft, K. L., G. W. Patterson, R. P. Lowell, and L. Germanovich, 2016, Fracturing and flow: Investigations on the formation of shallow water sills on Europa: Icarus, v. 274, p. 297-313.

Craig, J. R., J. F. Light, B. C. Parker, and M. G. Mudrey, 1975, Identification of hydrohalite: Antarctic Journal, v. 10, p. 178-179.

Craig, J. R., B. L. Weand, and R. D. Fortner, 1974, Halite and Hydrohalite from Lake Bonney, Taylor Valley, Antarctica: Geology, v. 2, p. 389-390.

Crétaux, J.-F., R. Létolle, and S. Calmant, 2009, Investigations on Aral Sea Regressions from Mirabilite Deposits and Remote Sensing: Aquatic Geochemistry, v. 15, p. 277-291.

De Sanctis, M. C., A. Raponi, E. Ammannito, M. Ciarniello, M. J. Toplis, H. Y. McSween, J. C. Castillo-Rogez, B. L. Ehlmann, F. G. Carrozzo, S. Marchi, F. Tosi, F. Zambon, F. Capaccioni, M. T. Capria, S. Fonte, M. Formisano, A. Frigeri, M. Giardino, A. Longobardo, G. Magni, E. Palomba, L. A. McFadden, C. M. Pieters, R. Jaumann, P. Schenk, R. Mugnuolo, C. A. Raymond, and C. T. Russell, 2016, Bright carbonate deposits as evidence of aqueous alteration on (1) Ceres: Nature, v. 536, p. 54.

Debenham, F., 1920, A new mode of transportation by ice: the raised marine muds of south Victoria Land (Antarctica): Quarterly Journal of the Geological Society of London, v. 75, p. 51-78.

Fox-Powell, M. G., G. R. Osinski, M. Gunn, D. Applin, E. Cloutis, and C. R. Cousins, 2018, Low-Temperature Hydrated Salts on Axel Heiberg Island, Arctic Canada, as an Analogue for Europa. . Available from http://www.lpi.usra.edu/meetings/lpsc2018/pdf/2564.pdf.: In 49th Lunar and Planetary Science Conference. Lunar and Planetary Institute, Houston. Abstract #2564.

Frank, T. D., Z. Gui, and t. A. S. M. S. S. Team, 2010, Cryogenic origin for brine in the subsurface of southern McMurdo Sound, Antarctica: Geology, v. 38, p. 587-590.

Garrett, D. E., 1998, Borates: Deposits, processing, properties and use: Amsterdam, Elsevier, 483 p.

Garrett, D. E., 2001, Sodium sulfate: Handbook of deposits, processing, properties and uses: Amsterdam, Elsevier, 384 p.

Grasby, S. E., I. Rod Smith, T. Bell, and D. L. Forbes, 2013, Cryogenic formation of brine and sedimentary mirabilite in submergent coastal lake basins, Canadian Arctic: Geochimica et Cosmochimica Acta, v. 110, p. 13-28.

Hardie, L. A., 1984, Evaporites: Marine or non-marine?: American Journal of Science, v. 284, p. 193-240.

Herrero, M. J., J. I. Escavy, and B. C. Schreiber, 2015, Thenardite after mirabilite deposits as a cool climate indicator in the geological record: lower Miocene of central Spain: Clim. Past, v. 11, p. 1-13.

Herut, B., A. Starinsky, A. Katz, and A. Bein, 1990, The role of seawater freezing in the formation of subsurface brines: Geochimica et Cosmochimica Acta, v. 54, p. 13-21.

Horita, J., 2009, Isotopic Evolution of Saline Lakes in the Low-Latitude and Polar Regions: Aquatic Geochemistry, v. 15, p. 43-69.

Hu, Y.-B., D. A. Wolf-Gladrow, G. S. Dieckmann, C. Völker, and G. Nehrke, 2014, A laboratory study of ikaite (CaCO36H2O) precipitation as a function of pH, salinity, temperature and phosphate concentration: Marine Chemistry, v. 162, p. 10-18.

Hussmann, H., F. Sohl, and T. Spohn, 2006, Subsurface oceans and deep interiors of medium-sized outer planet satellites and large trans-neptunian objects: Icarus, v. 185, p. 258-273.

Hynek, B. M., M. K. Osterloo, and K. S. Kierein-Young, 2015, Late-stage formation of Martian chloride salts through ponding and evaporation: Geology, v. 43, p. 787-790.

Iess, L., D. J. Stevenson, M. Parisi, D. Hemingway, R. A. Jacobson, J. I. Lunine, F. Nimmo, J. W. Armstrong, S. W. Asmar, M. Ducci, and P. Tortora, 2014, The Gravity Field and Interior Structure of Enceladus: Science, v. 344, p. 78.

James, N. P., G. M. Narbonne, R. W. Dalrymple, and T. K. Kyser, 2005, Glendonites in Neoproterozoic low-latitude, interglacial, sedimentary rocks, northwest Canada: Insights into the Cryogenian ocean and Precambrian cold-water carbonates Geology, v. 33, p. 9-12.

Karpychev, Y., 2007, Variations in the sedimentation in Kara Bogaz Gol Bay related to sea level fluctuations during the Novocaspian time: Oceanology, v. 47, p. 857-864.

Kolpakova, M., O. L. Gaskova, O. Naymushina, and S. K. Krivonogov, 2018, Ebeity lake, Russia: Chemical-organic and mineral composition of water and bottom sediments: v13BeCTv1H T0MCK0,O nonv1TeXHW-leCK0,O YHv1BeprnTeTa. v1H)Kv1Hv1pv1H, ,eopecypcoB., v. 329, p. 111-123.

Kosarev, A., A. Kostianoy, and I. Zonn, 2009, Kara-Bogaz-Gol Bay: Physical and Chemical Evolution: Aquatic Geochemistry, v. 15, p. 223-236.

Kurilenko, V. V., I. G. Ruday, and A. A. Shvarts, 1988, The origin and commercial exploitation of subsurface brines in the northern half of Kara-Bogaz-Gol: International Geology Reviews, v. 30, p. 1238-1245.

Last, W. M., 2002, Geolimnology of salt lakes: Geosciences Journal, v. 6, p. 347-369.

Lebedeva, M., O. Lopukhina, and N. Kalinina, 2008, Specificity of the chemical and mineralogical composition of salts in solonchak playas and lakes of the Kulunda steppe: Eurasian Soil Science, v. 41, p. 416-428.

Light, B., R. E. Brandt, and S. G. Warren, 2009, Hydrohalite in cold sea ice: Laboratory observations of single crystals, surface accumulations, and migration rates under a temperature gradient, with application to “Snowball Earth”: Journal of Geophysical Research: Oceans, v. 114.

Makhnach, A. A., 2008, Diagenetic gypsum, anhydrite and halite in non-evaporite deposits of Belarus: Baltica,, v. 21, p. 25-39.

Marion, G. M., R. E. Farren, and A. J. Komrowski, 1999, Alternative pathways for seawater freezing: Cold Regions Science and Technology, v. 29, p. 259-266.

McCaffrey, M. A., B. Lazar, and H. D. Holland, 1987, The evaporation path of seawater and the coprecipitation of Br(-) and K(+) with halite: Journal of Sedimentary Petrology, v. 57, p. 928-937.

McCord, T. B., G. B. Hansen, F. P. Fanale, R. Carlson, W. , D. L. Matson, T. V. Johnson, W. D. Smythe, J. K. Crowley, P. D. Martin, A. Ocampo, C. A. Hibbitts, and J. C. Granahan, 1998, Salts on Europa's surface detected by Galileo's near infrared mapping Spectrometer: Science, v. 280, p. 1242-1245.

Muessig, S., 1958, First known occurrence of inyoite in a playa at Laguna Salinas: Am. Mineral., v. 43, p. 1144–1147.

Nelson, K. H., and T. G. Thompson, 1954, Deposition of salts from seawater by frigid concentration: Journal Marine Reseearch, v. 13, p. 166-182.

Nikolaevsky, A. P., 1938, The winter minerals of the Baskunchak salt lake: Priroda, v. 1, p. 86-93.

Ojha, L., M. B. Wilhelm, S. L. Murchie, A. S. McEwen, J. J. Wray, J. Hanley, M. Masse, and M. Chojnacki, 2015, Spectral evidence for hydrated salts in recurring slope lineae on Mars: Nature Geosci, v. 8, p. 829-832.

Peterson, R. C., and R. Y. Wang, 2006, Crystal molds on Mars: Melting of a possible new mineral species to create Martian chaotic terrain: Geology, v. 34, p. 957-960.

Postberg, F., J. Schmidt, J. Hillier, S. Kempf, and R. Srama, 2011, A salt-water reservoir as the source of a compositionally stratified plume on Enceladus: Nature, v. 474, p. 620.

Raup, O. B., 1970, Brine mixing - an additional mechanism for formation of basin evaporites: Bulletin American Association of Petroleum Geologists, v. 54, p. 2246-2259.

Raup, O. B., 1982, Gypsum precipitation by mixing seawater brines: Bulletin American Association of Petroleum Geologists, v. 66, p. 363-367.

Roberts, S. M., R. J. Spencer, W. B. Yang, and H. R. Krouse, 1997, Deciphering some unique paleotemperature indicators in halite-bearing saline lake deposits from Death Valley, California, USA: Journal of Paleolimnology, v. 17, p. 101-130.

Ruesch, O., T. Platz, P. Schenk, L. A. McFadden, J. C. Castillo-Rogez, L. C. Quick, S. Byrne, F. Preusker, D. P. O’Brien, N. Schmedemann, D. A. Williams, J. Y. Li, M. T. Bland, H. Hiesinger, T. Kneissl, A. Neesemann, M. Schaefer, J. H. Pasckert, B. E. Schmidt, D. L. Buczkowski, M. V. Sykes, A. Nathues, T. Roatsch, M. Hoffmann, C. A. Raymond, and C. T. Russell, 2016, Cryovolcanism on Ceres: Science, v. 353, p. aaf4286.

Smith, G. I., 1979, Subsurface stratigraphy and geochemistry of Late Quaternary evaporites, Searles Lake, California: US Geological Survey, Professional Paper, v. 1043, p. 130 pp.

Starinsky, A., and A. Katz, 2003, The formation of natural cryogenic brines: Geochimica et Cosmochimica Acta, v. 67, p. 1475-1484.

Strakhov, N. M., 1970, Principles of Lithogenesis (Reviews of USSR Sodium Sulfate Deposits): New York, Plenum Publishing.

Vance, S., M. Bouffard, M. Choukroun, and C. Sotin, 2014, Ganymede's internal structure including thermodynamics of magnesium sulfate oceans in contact with ice: Planetary and Space Science, v. 96, p. 62-70.

Ward, M. K., and W. H. Pollard, 2018, A hydrohalite spring deposit in the Canadian high Arctic: A potential Mars analogue: Earth and Planetary Science Letters, v. 504, p. 126-138.

Warren, J. K., 2010, Evaporites through time: Tectonic, climatic and eustatic controls in marine and nonmarine deposits: Earth-Science Reviews, v. 98, p. 217-268.

Warren, J. K., 2016, Evaporites: A compendium (ISBN 978-3-319-13511-3): Berlin, Springer, 1854 p.

Wood, W. W., W. E. Sanford, and A. R. S. Al Habshi, 2002, Source of solutes to the coastal sabkha of Abu Dhabi: Geological Society of America Bulletin, v. 114, p. 259-268.

Wood, W. W., W. E. Sanford, and S. K. Frape, 2005, Chemical openness and potential for misinterpretation of the solute environment of coastal sabkhat: Chemical Geology, v. 215, p. 361-372.

Xiyu, Z., 1984, Distribution characteristics of boron and lithium in brine of Zhacang Caka salt lake, Xizang (Tibet), China: Chinese Journal of Oceanology and Limnology, v. 2, p. 218-227.

Zavialov, P., A. Ni, T. Kudyshkin, D. Ishniyazov, I. Tomashevskaya, and D. Mukhamedzhanova, 2009, Ongoing Changes of Ionic Composition and Dissolved Gases in the Aral Sea: Aquatic Geochemistry, v. 15, p. 263-275.

Zheng, M., 1997, An introduction to saline lakes on the Qinghai-Tibet, Plateau: Monographiae Biologicae, v. 76, Springer, 328 p.

Zheng, M., T. Jiayou, L. Junying, and Z. Fasheng, 1993, Chinese saline lakes: Hydrobiologia, v. 267, p. 23-36.

Zheng, M., and X. Liu, 2009, Hydrochemistry of Salt Lakes of the Qinghai-Tibet Plateau, China: Aquatic Geochemistry, v. 15, p. 293-320.

 


Recent Posts


Tags

magadiite seawater evolution epsomite Lamellibrachia luymesi CO2: albedo potash ore stevensite solikamsk 2 nitrogen LIP salt suture Large Igneous Magmatic Province Gamma log Neoproterozoic Oxygenation Event lapis lazuli phreatomagmatic explosion bedded potash allo-suture supercritical halite authigenic silica Weeks Island salt mine sodium silicate Ripon namakier sinjarite astrakanite 18O enrichment Sulphate of potash supercritical phase brine pan antarcticite deep seafloor hypersaline anoxic basin evaporite karst Pangaea Beebe hydrothermal field base metal Lake Peigneur freefight lake Koeppen Climate methanotrophic symbionts salt trade Kara bogaz gol causes of glaciation dark salt End-Cretaceous geohazard Warrawoona Group tachyhydrite brine lake edge lithium brine Hadley cell: vadose zone York (Whitehall) Mine Seepiophila jonesi brine evolution anomalous salt zones Lake Magadi lazurite salt ablation breccia snake-skin chert dissolution collapse doline Dallol saltpan sulfate cryogenic spring salts source rock phreatic explosion climate control on salt NPHI log Clayton Valley playa: evaporite Karabogazgol mummifiction carbon oxygen isotope cross plots methanogenesis chert Atlantis II Deep Boulby Mine auto-suture lithium battery marine brine doline recurring slope lines (RSL) ozone depletion 13C non solar heating salts saline clay Stebnyk potash basinwide evaporite salt leakage, dihedral angle, halite, halokinesis, salt flow, bischofite Noril'sk Nickel Archean Hell Kettle Neutron Log Realmonte potash Ethiopia gypsum dune wireline log interpretation cryogenic salt Quaternary climate SO2 salt mine H2S Red Sea McMurdo Sound Thiotrphic symbionts mine stability Lomagundi Event mirabilite intersalt Precambrian evaporites extraterrestrial salt anthropogenically enhanced salt dissolution capillary zone Crescent potash lot's wife lithium carbonate CaCl2 brine alkaline lake Paleoproterozoic Oxygenation Event GR log water in modern-day Mars hydrogen SOP Zabuye Lake Mega-monsoon Great Salt Lake Lop Nor retrograde salt Neoproterozoic Catalayud Dead Sea karst collapse gas outburst trona well log interpretation methane circum-Atlantic Salt Basins meta-evaporite Hyperarid venice Belle Plain Member African rift valley lakes Dead Sea saltworks SedEx End-Triassic MgSO4 depleted Turkmenistan Calyptogena ponderosa Corocoro copper salt seal white smokers Bathymodiolus childressi black salt Zaragoza rockburst knistersalz subsidence basin salting-out blowout Magdalen's Road K2O from Gamma Log MOP halogenated hydrocarbon organic matter Dead Sea caves dihedral angle gem causes of major extinction events halotolerant natural geohazard Platform evaporite silicified anhydrite nodules well logs in evaporites Ingebright Lake salt tectonics 13C enrichment evaporite-metal association Phaneozoic climate hydrothermal potash Evaporite-source rock association Density log Jefferson Island salt mine Ganymede stable isotope sulfur Messinian Mixing zone water on Mars eolian transport Hadley Cell Five Island salt dome trend Musley potash Ceres perchlorate collapse doline Sumo RHOB potash Lop Nur Mars halocarbon carnallitite mass die-back Pilbara gassy salt evaporite dissolution sinkhole Danakhil Depression, Afar Stolz diapir cauliflower chert silica solubility vanished evaporite DHAB saline giant Koppen climate Enceladus HYC Pb-Zn Schoenite solar concentrator pans evaporite-hydrocarbon association End-Permian crocodile skin chert 18O well blowout Ure Terrace anthropogenic potash North Pole intrasalt sulphate hydrothermal anhydrite ancient climate Deep seafloor hypersaline anoxic lake Belle Isle salt mine potash ore price Deep halite-hosted cave hydrothermal halite seal capacity halophile waste storage in salt cavity oil gusher nacholite palygorskite Stebnik Potash CO2 Patience Lake member hydrothermal karst Prairie Evaporite carbon cycle halite extrasalt McArthur River Pb-Zn supercontinent endosymbiosis halokinetic MVT deposit Muriate of potash NaSO4 salts Mesoproterozoic kainitite jadarite sedimentary copper hectorite sulphur flowing salt lunette Proterozoic hydrological indicator gas in salt Badenian vestimentiferan siboglinids Mulhouse Basin nuclear waste storage Kalush Potash salt periphery Prograde salt zeolite phreatic evaporite DHAL sepiolite Salar de Atacama hydrohalite MgSO4 enriched deep meteoric potash Europe High Magadi beds salt karst

Archive