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).

Evaporites and climate: Part 2 of 2 - Ancient evaporites

John Warren - Saturday, February 25, 2017

Introduction

Evaporites, along with coal and bauxites, are sediments considered to be climate sensitive. Ancient evaporite distribution and associated paleolatitudes are used to reconstruct the distribution of the world's arid belts across time. As we saw in Part 1 (Salty Matters, Tuesday, January 31, 2017), thick, widespread evaporite deposit are essentially a result of the atmospheric circulation of the Hadley cells. That is, locations of subtropical dry zones and tropical/subtropical deserts of the globe are mostly determined by the positions of subsiding branches of cool, dry descending air in a Hadley cells (aka Trade Wind Belt; Lu et al., 2007; Crowley and North, 1991) within low-lying regions tied a sufficient supply of mother brine. Thus, climate plus ongoing brine supply are the underlying factors controlling locales of significant evaporite deposition (Ziegler et al., 1981). The previous article focused on regional and local climatic controls across the Quaternary (Salty Matters, Tuesday, January 31, 2017). This article extends the time frame for the evaporite/climate association across the Phanerozoic and into the Precambrian.


As we move back in time, we move out of an icehouse-dominated world climate, with permanent ice caps waxing and waning at the world's poles, into greenhouse-dominant world climates. In greenhouse times there are no permanent polar ice sheet and glaciers occurred only in some high-altitude mountainous belts (Figure 1a, b). The transition into greenhouse climate changes the dominant 4th-order eustatic style from 100m amplitude changes every 100,000 years or so into 4th-order responses with much lower 3-5 m amplitude oscillations every 100,000 years (Figure 2a, b). Lack of polar caps raises world sealevel on the order of 40-50 metres. Thus, even without tectonic considerations, there is less continental freeboard in greenhouse times and increased the potential for significant cratonic coverage by epicontinental and pericontinental seaways (Warren, 2016; Chapter 5).


Looking back in time, beyond the last few million years of the Quaternary, means our conceptual models must encompass a broader range of tectonic settings as well as changes in the rates of seafloor spreading, supercontinents, and times of significant igneous outpourings (superplumes). All these additional world-scale variables across a longer set of available time explain the greater range of climate potentials on the earth, compared to anything that has occurred in the time-limited base seen in icehouse-dominant Quaternary climate spreads. The last few million years of the current icehouse mode is inhabited by the human species or its primate ancestors. The previous Icehouse dominant mode was in the Carboniferous-Mid Permian when the dominant land animals were amphibians and primitive reptiles.
One the first questions this broader ancient climate spectrum, tied to evaporites over deep time, offers up is; "How do the positions of Hadley cells vary across geological time frames?" In part 1, we saw how the rise of the Himalayas deflected a belt of cool, dry descending air much further south toward the Equator. Moving back in time creates a broader scaffolding for documenting climate variation, in part driven by the rise and fall of mountain ranges, but also influenced by increases in the rate of seafloor spreading driving ocean basin shallowing and by changes in atmospheric/seawater compositions and temperatures.


Hadley cells and latitudinal variability over time
According to Chen Xu et al., 2013 and Boucot et al., 2013, much of the world-scale Phanerozoic distribution of significant bedded evaporite accumulations indicates the ongoing presence of two mid-latitude arid belts, presumably situated beneath Hadley Cells. There are exceptions in locales generated in local rain shadows with orographic control provided by neighbouring mountain ranges. However, in the later Permian, through the Triassic, and much of the Jurassic the two formerly mid-latitude Hadley Cells merged over the more central Pangaeanic regions of Africa, Europe and the adjacent Americas, to form an arid belt that also encompassed low-latitude, equatorial arid regions (Figure 3). Across the continental interior of the Pangean supercontinent, this arid to hyperarid equatorial belt in the supercontinent interior prevented the formation of climate-sensitive sediments that are more typical of humid equatorial conditions that deposit coals, kaolinites, lateritic materials and bauxites. However, in this same time interval, these more humid sediment products are typically present at low latitudes of these time slices adjacent to the Panthalassic ocean.
That is, in the absence of an equator-spanning supercontinent, low latitudes, typically imply humid and non-seasonal tropical conditions throughout much of the Phanerozoic, as we see today. But the assembly of the Pangaean supercontinent disrupted this latitudinally-zoned atmospheric circulation, replacing it with a progressively more monsoonal (seasonal) circulation and more arid, at times hyperarid, conditions in the equatorial continental interior of Pangaea (Parrish, 1993). The Pangean supercontinent reached its maximum areal extent in the Triassic and was associated with what is known as the Pangaean Megamonsoon. There were immense arid regions across the interior regions of the supercontinent that were nearly uninhabitable, with scorching days and frigid nights. However, Panthalassian coasts still experienced seasonality, transitioning from rainy weather in the summer to dry conditions during the winter and the associated accumulation of humid sediments (Figure 3b' Boucot et al., 2013). Megamonsoon aridity is evidenced not just in the accumulation of low-latitude bedded evaporite deposits. Low latitude continental aridity also drove the accumulation of thick, widespread low-latitude desert redbeds, sourced by eolian, not fluvial, detrital transport (Sweet at al., 2013) and the precipitation of bedded salt crusts in ephemeral saline lakes under exceptionally-high surface temperatures of up to 73°C (Zambito and Benison, 2013).
Paleolatitude reconstructions Chen-Xu et al. (2013) show these continental interior arid belts in low latitude tropical-subtropical regions persisted from the Permian to the Early Cretaceous. Reunion of the humid regions from both sides of Pangaea by the early Late Cretaceous formed a through-going low latitude humid tropical-subtropical belt. This coincides with the disaggregation of Pangaean supercontinent, as the initial stages of a modern latitudinal climate belt distribution pattern emerged, tied to latitudinally-restricted evaporites that continue to the present (Figure 4).


Tectonism and eustacy in arid climates drive the formation of mega-evaporite basins
Within this Phanerozoic climatic framework, there are times when significant volumes of evaporites form what are know as saline giants, or megahalite/megasulphates deposits. These massive accumulations of salts formed beneath arid climates that can span both greenhouse and icehouse climates (Figure 1; Warren, 2010, 2016). Ancient marine saline giants (megahalites and megasulphates) accrued in either of two plate-scale settings, which at times merged into one another, namely; 1) Platform evaporites (Figure 5) and, 2) Basinwide evaporites (Figure 6).

The first major contrast with nonmarine continental dominance in Quaternary evaporite settings is the fact that platform evaporites require greenhouse eustasy a and a marine feed, the second is that basinwide evaporites require tectonically- and hydrographically-isolated widespread subsealevel depressions, typically found along plate edges with continent-continent proximity in regions with a marine seepage feed and/or periodic marine overflows (Figure 6). Neither platform or basinwide conditions are present on the current earth surface. For basinwides, suitable hydrologic conditions were last present during the Messinian Salinity Crisis in the Mediterranean region, and platform evaporite settings were last present on earth across large parts of the Middle East carbonate platform during the Eocene (Tables 1, 2). There is a third group of ancient evaporite deposits; it encompasses all nonmarine lacustrine beds past and present (Table 3). This group has same-scale modern-ancient counterparts, unlike ancient marine platform and basinwide evaporites (Warren, 2010, 2016). Interestingly, the lacustrine depositional style for bedded salt accumulation dominates in the icehouse climate that is the Quaternary, and so biases a strictly uniformitarian view of the past with respect to the relative proportions of nonmarine versus marine evaporite volumes (see Part 1; Salty Matters, Tuesday, January 31, 2017).


Platform evaporites
Are made up of stratiform beds, usually <50 m thick and composed of stacked <1 to 5 m thick parasequences or evaporite cycles, with a variably-present restricted-marine carbonate unit at a cycle base (Table 1). Salts were deposited as mixed evaporitic mudflat and saltern evaporites, sometimes with local accumulations of bittern salts. Typically, platform salts were deposited in laterally extensive (>50-100 km wide), hydrographically-isolated, subsealevel marine-seepage lagoons (salterns) and evaporitic mudflats (sabkhas and salinas). These regions have no same-scale modern counterparts and extended as widespread depositional sheets across large portions of hydrographically isolated marine platform areas that passed seaward across a subaerial seepage barrier into open marine sediments (Figure 5). In marine margin epeiric settings, such as the Jurassic Arab/Hith and Permian Khuff cycles of the Middle East or the Cretaceous Ferry Lake Anhydrite in the Gulf of Mexico, these platform evaporites are intercalated with shoalwater marine-influenced carbonate shelf/ramp sediments, which in turn pass basinward across a subaerial sill into open marine carbonates. Landward they pass into arid zone continental siliciclastics or carbonate mudflats.

 

Platform evaporite deposition occurred in both pericontinental and epicontinental settings, at times of low-amplitude 4th and 5th order sealevel changes, which typify greenhouse eustasy (Figure 5; Warren, 2010). Platform evaporites also typify the saline stages of some intracratonic basins. Platform evaporites cannot form in the high-amplitude, high-frequency sealevel changes of Icehouse eustasy. The 100m+ amplitude oscillations of Icehouse times mean sealevel falls off the shelf edge every 100,000 years, so any evaporite that had formed on the platform is subaerially exposed and leached. Fourth order high-amplitude icehouse eustatic cycles also tend to prevent laterally-continuous carbonate sediment barriers forming at the top of the shelf to slope break, and so icehouse evaporite systems tend not to be hydro-graphically isolated (drawdown) at the platform scale. Rather icehouse eustasy favours nonmarine evaporites as the dominant style, along with small ephemeral marine-margin salt bodies, as seen today in the bedded Holocene halites and gypsums of Lake Macleod in coastal West Australia (Part 1; Salty Matters, Tuesday, January 31, 2017).
Ancient platform evaporite successions may contain halite beds, especially in intracratonic basinwide settings, but periplatform settings, outside of intracratonic basins, are typically dominated by 5–40 m thick Ca-sulphate beds intercalated with normal-marine platform carbonates (Table 1). The lateral extent of these epeiric platform sulphate bodies, like the Middle Anhydrite Member of the Permian Khuff Fm. of Saudi Arabia and the UAE, with a current area of more than 1,206,700 sq. km., constitute some of the most aerially-extensive evaporite beds ever deposited.


Basinwide evaporites
Are made up of thick evaporite units >50–100 m thick made up of varying combinations of deepwater and shallow water evaporites (Figure 1; Table 2). They retain textural evidence of different but synchronous local depositional settings, including mudflat, saltern, slope and basin (Figure 6). When basinwide evaporite deposition occurs, the whole basin hydrology is evaporitic, holomictic, and typically saturated with the same mineral phase across vast areas of the basin floor, as seen on a much smaller scale today in the Dead Sea basin. The Dead Sea currently has halite forming simultaneously as; 1) decimeter-thick chevron-dominated beds on the saline-pan floor of the shallow parts around the basin edge in waters typically less than 1-10 metres deep, and 2) as coarse inclusion-poor crystal meshworks of halite on the deep basin floor that sits below a halite-saturated brine column up to hundreds of metres deep. Ancient basinwide successions are usually dominated by thick massive salt beds, generally more than 100-500 m thick. Deposits are made up of stacked thick halite beds, but can also contain substantial volumes of thick-bedded Ca-sulphate and evaporitic carbonate, as in the intracratonic basinwide accumulations of the Delaware and Otto Fiord Ba-sins (Table 2).
Owing to inherent purity and thickness of the deposited halite, many halite-dominant basinwide beds are also remobilized, via loading or tectonics, into various halokinetic geometries (Hudec and Jackson, 2007). Some basinwide systems (mostly marine-fed intracratonic settings) entrain significant accumulations of marine-fed potash salts, as in the Devonian Prairie Evaporite of western Canada. In contrast, all Quaternary examples of commercial potash deposits are accumulating in continental lacustrine systems (Warren 2016; Chapter 11).

 

Basinwide evaporite deposits are the result of a combination of tectonic and hydrological circumstances that are not currently active on the world’s surface (Figure 1). They were last active in the Late Miocene (Messinian), in association with soft-suture collision basins tied to the Alpine-Himalaya orogenic belt, and in Middle Miocene (Badenian) basins developed in the early rift stages of the Red Sea. Basinwide systems will be active again in the future at sites and times of appropriate plate-plate interaction, when two continental plate edges are nearby, and the intervening seafloor is in or near a plate-edge rift or suture and is both subsealevel and hydrographically isolated (Figure 6). Unlike most platform evaporites, basinwides do not require greenhouse eustacy, only the appropriate association of arid climate and tectonics. The latter sets up a deep hydrographically-isolated subsealevel tectonic depression with a geohydrology that can draw on a huge reserve of marine mother brine in the nearby ocean. For this reason, saline giants tend to form at times of plate-scale continent-continent proximity and so occur mostly in craton-margin settings.

 

Lacustrine (nonmarine) evaporites
Quaternary continental playa/lacustrine are constructed of stratiform salt units, with the greater volume of saline sediment accumulating in lower, more-saline portions of the lacustrine landscape. Beds are usually dominated by nodular gypsum and displacive halite, deposited in extensive evaporitic mudflats and saltpans with textures heavily overprinted by capillary wicking, rather than as bedded bottom-nucleated layers on the subaqueous floors of perennial brine lakes (Ruch et al., 2012). In ancient counterparts, the total saline lacustrine thickness ranged from meters to hundreds of meters, with lateral extents measured in tens to hundreds of kilometres (Table 3). Lacustrine salt beds are separated vertically, and usually surrounded by, deposits of lacustrine muds, alluvial fans, ephemeral streams, sheet floods, eolian sands, and redbeds. As today, ancient lacustrine salts accumulated in endorheic or highly restricted discharge basins, with perennial saline water masses tending to occur in the drainage sumps of steep-sided drainage basins (Warren, 2010, 2016). Saline lake basins accumulating gypsum, or more saline salts like halite or glauberite, typically have a shallow water table in peripheral saline mudflat areas and so are dominated by continental sabkha textures. Nearby is the lowermost part of the lacustrine depression or sump where deposition is typified by ephemeral ponded brine pan deposits, rather than permanent saline waters.
Saline lacustrine mineralogies depend on compositions of inflowing waters, so depositional sumps in regions with non-marine ionic proportions in the feeder inflow, accumulate thick sequences of nonmarine bedded salts dominated by trona, glauberite, and thenardite. In contrast, nonmarine areas with thalassic (seawater-like) inflows tend to accumulate more typical sequences of halite, gypsum, and anhydrite.
Across the Pliocene-Quaternary icehouse, less-saline perennial saline-lake beds tend to occur during more humid climate periods in the same continental-lacustrine depressions where saline-pan beds form (e.g., Lake Magadi, Great Salt Lake, Lake Urmia). On a smaller scale, in some modern saline lake basins, parts of the lake floor can be permanently located below the water surface (Northern Basin in the Dead Sea or Lake Asal). In some modern saline sumps dominated by mudflats, a perennial saline lake water mass is located toward the edge of a more central salt-flat zone, forming a perennial water filled “moat” facies surrounding a seasonally desiccated saline pan (as in Salar, de Atacama, Salar de Uyuni, Lake Magadi, Lake Natron). These permanent to near-permanent saline water “moat” regions are typically created where fresher inflows encounter saltier beds of the lake centre, dissolve them, and so form water-filled peripheral depressions. Bottom sediment in the moats tends to be mesohaline carbonate laminites, which can contain TOC levels as high as 12%.
High-water stage perennial saline lacustrine sediments tend to be carbonate-rich or silica-rich (diatomaceous) laminites. Ancient examples of large saline lacustrine deposits made up of alternating humid and desiccated lacustrine units include the Eocene Green River Formation of Wyoming and the Permian Pingdiquan Formation of the Junggar Basin, China (Table 4). Evaporites deposited in a suprasealevel lacustrine basin (especially Neogene deposits) have numerous same-scale Quaternary analogues, unlike the more voluminous ancient marine platform and basinwide evaporites (Figure 7). Clearly, across the Quaternary, saline continent lacustrine settings possess areas of bedded salt accumulation that are far greater than those of any contemporaneous marine-fed salt sumps (Part 1; Salty Matters, Tuesday, January 31, 2017). But in ancient climes, especially during in the continental interior of the Pangean supercontinent (mid Permian to Triassic), regions of continental interior sabkhas and saline pans had areas far greater than any seen in Quaternary continental saline sumps (Zambia and Benison, 2013).


Is the present-day climate the key to evaporite understanding?
This short answer is yes, Hadley Cells across the Phanerozoic are mostly tied to climate belts that maintain sub-tropical positions, but to this notion, we must add a geological context. Today we are living in an icehouse climate mode and have been for the last 12 Ma. It is tied to the presence of polar ice-sheets that wax and wane over 100,000-year time frames, so moving the position of the Hadley cells and changing the intensity of atmospheric circulation. In this icehouse climate, large eustatically-controlled marine-fed evaporite deposits are not preserved, as sea level falls off the continental shelf every 100,000 years or so. The world's largest bedded salt deposits formed sometime in the last 2 million years, are found in continental interiors, typically in endorheic tectonic sumps in either hot arid or steppe climate settings, often with salt diapirs outcropping or subcropping in the drainage basin and the basin floor can be located at elevations well above sealevel (Part 1; Salty Matters, Tuesday, January 31, 2017).
As we move back into much of Phanerozoic time, we see world climates dominated by greenhouse modes, with shorter episodes of polar ice-sheets and icehouse climates in the Carboniferous-Early Permian ≈ 50 million years long, and the Ordovician, some 15 million years long (Figure 1). Greenhouse climate lacks permanent polar ice sheets, so sea-levels are higher, and 4th-order eustatic amplitudes in sea level are much less (a few meters versus hundred meters plus changes). Greenhouse sets up epeiric and intercontinental seaways that when hydrographically isolated, but still marine-fed, can deposit huge areas of platform evaporites centred in isolated seepage-fed sub-sealevel sumps. These platform deposits can also form outside of Greenhouse times in marine-fed tectonically-induced intracratonic sumps.
Basinwide evaporite deposits span icehouse and greenhouse mode arid belts, whenever a marine-fed subsealevel tectonic sump forms at positions of continent-continental proximity in an arid belt. Across much of the Phanerozoic, basinwide deposits typically accumulated beneath subtropical belts of cool, dry descending air set up in a Hadley cell, and so are located north and south of a tropical equatorial belt. But the accretion of the Pangaean supercontinent (Carboniferous to Jurassic) set up conditions of continentality and orographic shadowing that allowed an arid saline belt to span the hyperarid interior of the supercontinent.
 
References

Boucot, A., Chen-Xu, and C. Scotese, 2013, Phanerozoic Paleoclimate: An Atlas of Lithologic Indicators of Climate: Concepts in Sedimentology and Paleontology, v. 11: Tulsa, OK, SEPM, 32 p.

Chen-Xu, A. J. Boucot, C. R. Scotese, F. Junxuan, W. Yuan, and Z. Xiujuan, 2012, Pangaean aggregation and disaggregation with evidence from global climate belts: Journal of Palaeogeography, v. 1, p. 5-13.

Crowley, T. J., and G. R. North, 1991, Paleoclimatology: New York, Oxford University Press, 339 p.

Hudec, M. R., and M. P. A. Jackson, 2007, Terra infirma: Understanding salt tectonics: Earth-Science Reviews, v. 82, p. 1-28.

Lu, J., G. A. Vecchi, and T. Reichler, 2007, Expansion of the Hadley cell under global warming: Geophysical Research Letters, v. 34.

Parrish, J. T., 1993, Climate of the Supercontinent Pangea: Journal of Geology, v. 10.

Ruch, J., J. K. Warren, F. Risacher, T. R. Walter, and R. Lanari, 2012, Salt lake deformation detected from space: Earth and Planetary Science Letters, v. 331-332, p. 120-127.

Sweet, A. C., G. S. Soreghan, D. E. Sweet, M. J. Soreghan, and A. S. Madden, 2013, Permian dust in Oklahoma: Source and origin for Middle Permian (Flowerpot-Blaine) redbeds in Western Tropical Pangaea: Sedimentary Geology, v. 284–285, p. 181-196.

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.

Zambito, J. J., and K. C. Benison, 2013, Extremely high temperatures and paleoclimate trends recorded in Permian ephemeral lake halite: Geology, v. 41, p. 587-590.

Ziegler, A. M., S. F. Barrett, C. R. Scotese, and B. W. Sellwood, 1981, Palaeoclimate, Sedimentation and Continental Accretion [and Discussion]: Philosophical Transactions of the Royal Society of London. Series A, Mathematical and Physical Sciences, v. 301, p. 253-264.


 

 

Silica recycling and replaced evaporites - 4. Proterozoic atmospheric transitions and saline microporous chert reservoirs

John Warren - Friday, October 07, 2016

Sulphate and oxygenation levels across the Proterozoic

Proterozoic (2.5 – 0.542 Ga) saline sediments encompass significant transitions in evaporite style and chemistry within an evolving atmospheric and oceanic framework. Lithospheric changes tie to a cooling and biologically-evolving earth as earth-scale plate tectonics move to a system set comparable with that operating today. The Proterozoic eon is divided into three eras: the Paleoproterozoic, Mesoproterozoic and Neoproterozoic. Thick sequences of halite are only found as the actual bedded salts in sediments of the Neoproterozoic (and the Phanerozoic), while calcium sulphate residues and beds occur in all three Proterozoic eras, especially in parts of the Paleoproterozoic and the Neoproterozoic.

Paleoproterozoic era sediments (2.5-1.6 Ga) contain isotopic evidence the first significant oxygenation event in the world's atmosphere, largely driven by the increasing dominance of cyanobacterial photosynthesis. Neoproterozoic sediments (1.0 – 0.542Ga) contain evidence of the second oxygenation event, which is associated with the evolution of widespread multicellular life and CaCO3/siliceous carapaces. By the end of the Neoproterozoic, the world oceans had chemistries, temperatures and salinities similar to those of the Phanerozoic (Blamey et al., 2016). The intervening Mesoproterozoic (1.6- 1.0 Ga) retains evaporitic residues with aspects of both the late Archean and the Phanerozoic.

The oxygenation of Earth’s atmosphere-ocean system occurred in two steps: 1) the Paleoproterozoic “Great Oxygenation Event” (GOE ≈ 2.3 Ga), which refers to the transition from a pervasively reducing Earth-surface system to one with an oxygenated atmosphere and oxygenated shallow seas, and 2) the “Neoproterozoic Oxygenation Event” (NOE), when the Earth’s atmosphere and ocean are understood to have become persistently oxygenated down to the deep ocean bottom (Turner and Bekker, 2016; Scott et al., 2014). The GOE is indicated by a Proterozoic carbon isotope anomaly known as the “Lomagundi event,” a positive carbon isotope excursion between ca. 2.22 and 2.06 Ga, interpreted to be the result of high organic carbon burial and attendant accumulation of atmospheric oxygen (Figure 1; Bekker and Holland, 2012)). A long interval spanning the remainder of the Paleoproterozoic and much of the Mesoproterozoic followed the Lomagundi event, typified by lower levels of atmospheric oxygen and little variation in carbon isotope values. This ended in the late Neoproterozoic with dramatic fluctuations, of escalating magnitude, in the biogeochemical carbon cycle and attendant fluctuations within an overall increasing oxygen content (Figure 2). By the end of the Neoproterozoic, not just shallow shelf waters but much of the deep-ocean water column was consistently oxygenated (see article 1 in this series)


 

Chert evolution

 We have already seen how low levels of oxygen and high levels of CO2 in the Archean favoured the precipitation of nahcolite, and its hydrothermal silica association, atop subsealevel isolated saline sumps in microcontinents and island arcs in a saline waterworld (article, 28 August 2016). The hydrothermally-dominated silica of the silica-rich Archean oceans is reflected in more negative 30Si isotope values in widespread marine cherts of that time, compared with most Proterozoic cherts (Chakrabarti et al., 2012; see also Figure 3b). However, shorter-term fluctuating levels of atmospheric oxygen in the Proterozoic also influenced drop-out salinities for gypsum in Mesoproterozoic marine brines. In brines derived from the modern, well-oxygenated world oceans, as in evaporite successions deposited throughout the Phanerozoic, the sulphate minerals gypsum and anhydrite precipitated from evaporating seawater after aragonite or calcite, but before halite (see 26 August, 2015, blog for more detail). At lower seawater sulphate levels across the Archean and much of the Proterozoic, gypsum and anhydrite precipitated after halite, even at Na and Cl concentrations similar to those of the modern ocean.

This is why some post-Lomagundi, Paleoproterozoic marine evaporite successions show clear evidence of halite precipitation before gypsum or anhydrite or even an absence of gypsum or anhydrite with halite (e.g., ≈ 1.88 Ga Stark Formation; Pope and Grotzinger, 2003). The post-halite precipitation of calcium sulphate is construed as evidence for a limited marine sulphate reservoir and little atmospheric oxygen (Scott et al., 2014). In contrast, Lomagundi- age sedimentary successions contain evidence for sulphate precipitation before halite (Melezhik et al., 2005; Bekker et al., 2006; Schröder et al., 2008). Sulphur isotope values of marine sulphates (in CaSO4, barite) and sulphides in marine pyrite also record expansion and contraction of anoxic oceanic settings. That is, a higher burial rate of pyrite in anoxic settings is indicated by a positive shift in the sulphur isotope values of sulphates, whereas ocean oxygenation creates a negative shift in values (e.g., Claypool et al., 1980; Strauss, 1997). Furthermore, expansion of the area of anoxic oceanic settings decreases the size of the seawater sulphate reservoir, resulting in more variable sulphur isotope values of sulphate evaporites, barites, and other carbonate-associated sulphates (Figure 2; Kah et al., 2004). This applies in particular in the Mesoproterozoic when only tshallow oceanic waters were consistently oxygenated.

When we look at silica mobility and chert styles across a Proterozoic milieu of evolving oxygen and sulphate levels we see some aspects similar to the Phanerozoic and others more akin to the high-silica oceans of the Archean. Maliva et al. (2005) and Perry and 2014 show that the latter part of the Paleoproterozoic era (post-Lomagundi) is marked by the end of widespread primary and early diagenetic silica precipitation in normal marine subtidal environments. However, silica precipitation continued apace in the deeper marine in waters that were still anoxic. The Paleoproterozoic is defined by the “rusting” of the shallower parts (shelves and upper slopes) of the world’s ocea,n as dissolved oxygen levels increased and the accumulation of widespread Banded Iron Formations (BIFs) occurred, including the huge deposits of NW Australia.

So where and when do we see nodular cauliflower chert after sulphate in the Proterozoic?

Some of the oldest silicified nodular sulphates with cauliflower chert textures and actual relict anhydrite are found in the Huronian Gordon Lake Formation (≈2.4 Ga; Chandler, 1988). The nodules are commonest in mud chip breccia at the base of sandstone, siltstone and mudstone upward-fining storm cycles. Anhydrite nodule relicts are composed of a mosaic and meshworks of blocky crystal laths. Earlier laths are preserved in silicified outer rims of many cauliflower chert nodules, with texture alignments similar to that of Recent displacive sabkha anhydrite nodules. Completely silicified nodules are composed of megaquartz, some calcite-cored, or of jasper, with replacement textures identical those documented the Phanerozoic by Milliken (1979). Similarly-textured cauliflower cherts are found in the Mallapunyah Formation (1650 Ma) in the Paleoproertozoic sediments of the McArthur Basin in the Northern Territory of Australia (Warren, 1999). Thin sections through 5-30cm diameter Mallapunyah nodules (in a redbed host) can still retain small relict highly-birefringent laths of anhydrite, but most of the former felted cores to the nodules are now composed of mimetic silica. There are also older sedimentary chert nodules in the McArthur Basin succession located in units below the level of the Mallapunyah, but they are smooth walled not rugose-surfaced features.

Unfortunately, the term cauliflower chert is loosely defined and is used to describe cemented features in Meosproterozoic and earlier sediments and metasediments, which are not true calcium sulphate evaporite replacements.Although termed cauliflower features, they do not have surface textures resembling the florets of a cauliflower (see article 2 in this series - July 31, 2016). For example, aggregates and clusters of growth-aligned barite crystals in the Archean of South Africa are described as cauliflowers when they should be described as bladed, palmate crystal aggregates (Reimers and Heinrich, 1997). Interstingly, Chowns and Elkins (1974) in a study of cauliflower cherts occurrences across the USA list no examples older than Cambrian. Using a tighter definition of cauliflower chert and recognising that this term should not be interchangeable with crocodile-skin chert it seems that Proterozoic occurrences of cauliflower chert nodules largely mirror times when oxygen levels were sufficiently high in the world's ocean to allow sulphate in solution. In the Paleoproterozoic and Mesoproterozoic only the upper parts of the ocean column, including waters covering the world's continental shelves (and derived evaporite basins) were sufficiently oxygenated to allow the formation of cauliflower chert after nodular anhydrite. However in some Neoproterozoic basins, especially if located in sumps in a highly-restricted brine layered seafloor, the levels of anoxia in the ponded bottom brines facilitated the accumulation of laminar microporous chert in association with evaporites or their early replacements


Primary laminated hypersaline silica chert in an evaporite basin at the Precambrian-Cambrian boundary

An organic-rich laminated porous chert known as the Athel or Al Shamou silicilyte consists of up to 90% microcrystalline quartz along with dolomite, magnesite, anhydrite and halite (Rajaibi et al., 2015). It occurs at the Precambrian-Cambrian boundary in the subsurface of the South Oman Salt Basin, Sultanate of Oman, where it acts as a light-oil reservoir  (Ramseyer et al., 2013; Amthor et al., 2005). Fully encased in variably halokinetic salt masses, it was first discovered during the 1990's hydrocarbon exploration activities of Petroleum Development Oman. This laminated microporous and variably fractured chert, has its source of silica and its mode of precipitation tied to an anoxic, sulphur-rich, stagnant and highly saline basin. Its homogeneous silica distribution and high Si isotope values (avg. d30Si = +0.83 ± 0.28), coupled with a low molar Ge/Si ratio (<0.25 x 10-6) in its microcrystalline quartz matrix imply dissolved silica in concentrated seawater as the Si source, and hydrothermal or biogenic (e.g. sponge-derived) silica are excluded.

Silica precipitation from a seawater-sourced brine was likely the result of a dramatic increase in salinity in response to halokinetic salt dissolution atop and adjacent to the edges of transtensional depressions on a deep basin floor in the South Oman Salt basin, thus markedly reducing the solubility of amorphous silica in these brine-filled seawater depressions. This saturation triggered the formation of silica gel. The gel accumulated at the base of a brine-layer covered basin floor, forming a soft silica-rich layer bound into bacterial mats, giving rise to its fine-scale lamination. The mean number of laminae in this laminated chert is ca. 32 per year suggesting that layering is non-annual and controlled by processes such as fluctuations in nutrient supply, lunar driven re-mixing or diagenetic segregation. The transformation of the silica-gel to microcrystalline quartz occurred below 45°C indicating a less than -4.5‰ d18O composition of the pore-water during microcrystalline quartz formation. The  microporous hydrocarbon filled nature of this ancient chert and the fact the hydrocarbon-filled micropores are still distinct after more than 500 million years after they filled (Figure 4d, e) is  why when artificially fractured the silicilyte can act as a hydrocarbon reservoir (See Rajaibi et al. 2015 and Warren, 2016; Chapter 10 for a summary of relevant literature).
 

 

What does this mean for other evaporite-associated laminar cherts in the Phanerozoic?
Beds of laminated chert (not replaced, but precipitated, primary silica accumulations) are unusual across the Phanerozoic, but cauliflower cherts as replacement of calcium sulphate evaporites are not (Chowns and Elkins, 1974). Spanning the Precambrian boundary, the Athel Silicilyte is the first Phanerozoic example of a laminar chert-hypersaline association. Then, there is the somewhat younger but world-famous Devonian to early Carboniferous Caballos Novaculite. This chert location was the site of a world-famous set of arguments as its origin, between two world-renown professors, Dr Earle McBribe and Dr Robert Folk, both on the faculty of the University of Texas at that time. Folk argued for a shallow-water peritidal hypersaline depositional setting, McBride for a deep a marine setting but still with possible hypersaline indicator textures (Folk, 1973; Folk and Mcbride, 1976; McBride and Folk 1977).

The Caballos Novaculite outcrops in the Marathon Uplift of Texas, while its lithologic and time equivalent, the Arkansas Novaculite, outcrops in the Ouachita Mountains of Arkansas and Oklahoma (Figure 5). Novaculite chert) in outcrop is very resistant to erosion so that layers of novaculite stand out as characteristic ridges and dip slopes in the Ouachita and Marathon mountains (Figure 5). This outcrop forms and its hard abrasive nature gives it the name novaculite, which in its Latin root novacula, means razor-stone. When some novaculite is fractured in the subsurface, there is sufficient connected porosity to form a fractured reservoir play, as in Arkansas and Texas. There, some 30 years ago, oil and gas fields such as Isom Springs in Oklahoma and McKay Creek, Pinion and Thistle fields in West Texas were discovered in the Caballos and Arkansas novaculite-chert. The chert reservoir is most productive when it is highly fractured, occurs within complex thrust faults and has had any enclosed carbonate material leached from its chert matrix, so creating microporosity (Figure 6; Godo et al., 2011).

Chert beds in the Caballos Novaculite are composed of equant grains of microcrystalline quartz, minor amounts of illite and radiolaria, and trace amounts of pyrite, carbonate and other minerals and organic matter. The chert beds are generally interpreted as having formed by the silicification and alteration of precursor sediment, sometimes massive, other times finely laminated. Some beds retain occasional evidence biogenic silica derived from radiolaria, while underlying levels retain can contain abundant siliceous sponge spicules. Fractures and crackle breccias developed in a grey chert following lithification; green siliceous sediment, whose lithification was impeded by clay, filled these pre-orogenic fractures.
Beds of red shale, chert pebble and cobble conglomerate, sandstone, limestone, dolomite, and lumpy manganiferous and jasperitic chert make up no more than 3% of the chert and shale members of the Caballos, but still are of controversial origin and environmental significance. The chert conglomerate beds, for example, are interpreted as tidal-channel deposits by Folk and as mass-flow deposits by McBride. Jasper beds texture are considered bizarre by many geologists who have worked on them: they are lumpy, uneven beds 0.2 to 2 m thick composed of cherry-red chert with local geopetal cavities, contorted laminae. manganiferous zones, cauliflowerlike quartz-filled nodular cavities sometimes with hollow centres and variably filled or partially filled with zebraic chalcedony, lutecite, quartzine, pseudocubic quartz crystals, and filamentous structures resembling algae. These beds are interpreted by Folk as the product of diagenetic alteration of sabkha evaporite nodules and siliceous ooze, during and following subaerial exposure with soil development, and by McBride as the product of diagenetic alteration of evaporite beds deposited in deep water and sandwiched between radiolarian ooze. Synthesis of evidence on the origin of both the novaculite and chert and shale members leads to contrasting interpretations of water depth during deposition. However, if the evaporite solution breccias, recognised as such by both authors and the cauliflower cherts as replaced diagenetic anhydrite clusters then the depositional setting is akin to that of the Athel Silicilyte (namely a deepwater holokinetic hypersaline evaporite setting not unlike a siliceous DHAL association (see Warren, 2016; Chapter 9, for discussion of the DHAL literature).
Economic implications of understanding what defines a silicilyte versus novaculite versus tripolite versus diatomaceous ooze
We have already seen that microporous cherts when fractured are possible reservoir rocks as illustrated by the saline-associated Athel Silicilyte and the Caballos Novaculite. The former retains its microporosity because of an early hydrocarbon charge into existing microporosity (Rajaibi et al. 2013; Amthor et al., 2005), while the reservoir quality of the latter was enhanced by diagenetic leaching of finely dispersed carbonate material, likely when it was caught up in the Ouachita Orogeny (Figure 6; Godo et al., 2011). Like the Athel, the Arkansas (Caballos) Novaculite is thought to be self-sourcing in terms of reservoir hydrocarbons (Zemmels et al., 1985).
The term silicilyte is defined by Rajaibi et al. (2013) as a "locally-used" term to describe porous organic-rich laminated chert, it is a succession of microcrystalline quartz that is preserved within salt-encased slabs, 300 to 400 m thick, at a depth of 4 to 5 km in the South Oman Salt Basin. As mentioned earlier, the term novaculite comes from its outcrop expression and its "razorstone" properties and does not necessarily have a direct connection to microporosity in the reservoir portions of the unit (Figure 5). Outcrops of weathered microporous chert zones in the upper part of the Arkansas (Caballos) Novaculite are called tripoli or rottenstone (Figure 6). When present in this finely powdered microporous form, it is quarried and crushed for use as a polishing abrasive in metalsmithing and woodworking. When present as a very hard dense rock, it can be cut and shaped for use as a whetstone or razorstone. Before European settlement, novaculite was a source for numerous arrow-tips, spear tips and knives. 
Etymological variations of the terms tripoli, novaculite and silicilyte as forms of chert, as currently used in the geological literature are interesting and geologically confused. This is particularly true if the writer did not 1) understand there are various origins to laminar sometimes microporous cherts, and  2) that there various possible silica sources and precipitation/replacement mechanisms can be halotolerant bacteria, or other silica sources that can be tied to marine sponges and yet others to radiolaria and diatomaceous oozes. Hence, there is the time-related aspect of biogenic chert evolution tying back to the source of the silica in some cherts and the presence or lack of salinity indicators in a laminar chert and chert nodules (e.g., cauliflower versus crocodile-skin cherts).
A diatomaceous ooze is a form of opaline silica made up of accumulations of siliceous frustules of diatoms in normal marine pelagic sediments and when it retains microporosity is sometimes called tripolite or tripolitic earth. Diatomaceous oozes, the precursor to this type of tripolitic earth is often laminated, but is harsh to the feel and scratches glass. To add to the confusion there are microporous mesohaline diatomaceous oozes called the Tripoli unit in many Messinian subbasins.
Tripoli or tripolite powder is also the term used to describe the form of microporous laminar chert used as an abrasive and collected from weathered zones of the Caballos and Arkansas Novaculites. The Palaeozoic age of the Caballos and Arkansas Novaculite means it cannot contain diatoms. Diatoms evolved in the Cretaceous and have been the dominant source of remobilised silica in marine chert nodules ever since. Palaeozoic silica remobilized into chert is often related to nearby sponge spicule horizons, or less often to radiolarian beds. The further back in time, and perhaps the more saline the marine bottom water, the greater the likelihood of a microbial association with chert precipitation and remobilisation.
Even in Tertiary strata some microporous diatomaceous earths can have a normal-marine, organic-enriched depositional association and can constitute a fractured microporous hydrocarbon reservoir. This is the case with the Miocene-age fractured microporous chert reservoirs that produce today in the Santa Barbara Basin of offshore California (Reid and McIntyre, 2001). Cores and coastal outcrops of the Monterey Formation show this type of marine-deepwater diatomaceous ooze is interlayered with microbial (bacterial-archeal) methanogenic organic-rich dolomites. Then, there are the deepwater diatomaceous saline oozes in the Miocene units that immediately underly Messinian evaporites in the Lorca and other sub-basins across the Mediterranean (Rouchy et al., 1998). These diatomaceous organic-rich oozes were deposited as pelagic sediments in saline waters on stratified bottoms that herald the creation of saline bottom water layers related to the onset of hypersaline conditions. Their depositional setting is in restricted basins with increasingly saline bottoms, driven by tectonic isolation and drawdown that soon after precipitated the salts of the Messinian Salinity Crisis. Finally, there are the lacustrine diatomaceous oozes accumulating at the base of density-stratified water columns in lakes of African Rift Valley. This type of laminar ooze occurred in the deeper parts of the lake floor and in Lake Magadi and Lake Natron define units that immediately predate significant lake drawdown episodes that are defined by the type 1 (sodium bicarbonate) evaporite layers. These laminar diatomaceous chert beds contain nodules with the characteristic surface shrinkage textures of crocodile-skin chert (see article 1 in this series of four).
So, in terms of silica with an evaporite association, "one size does not fit all.' There are multiple saline settings, both depositional and diagenetic, with silica sources evolving with life across the Proterozoic into the Phanerozoic. Interactions between biology and brine chemistry control the accumulation of silica in various forms in a range of evaporite settings, ranging across the marine to deep halokinetic seafloors to lacustrine basins. Once we understand how to recognise cauliflower chert and its possible association with laminar saline cherts of the Proterozoic and the Phanerozoic, then particular chert styles can help to define the evolution of atmospheric oxygen and the saline versus non-saline origins of some organic-rich laminar biogenic microporous cherts.

References

 

Al Rajaibi, I. M., C. Hollis, and J. H. Macquaker, 2015, Origin and variability of a terminal Proterozoic primary silica precipitate, Athel Silicilyte, South Oman Salt Basin, Sultanate of Oman: Sedimentology, v. 62, p. 793-825.

Amthor, J. E., K. Ramseyer, T. Faulkner, and P. Lucas, 2005, Stratigraphy and sedimentology of a chert reservoir at the Precambrian-Cambrian boundary: the Al Shomou Silicilyte, South Oman Salt Basin: Geoarabia, v. 10, p. 89-122.

Bekker, A., and H. D. Holland, 2012, Oxygen overshoot and recovery during the early Paleoproterozoic: Earth and Planetary Science Letters, v. 317-318, p. 295-304.

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Chowns, T. M., and J. E. Elkins, 1974, The origin of quartz geodes and cauliflower cherts through the silicification of anhydrite nodules: Journal Sedimentary Petrology, v. 44, p. 885-903.

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Godo, T. J., P. Li, and M. E. Ratchford, 2011, Exploration for the Arkansas Novaculite Reservoir, in the Southern Ouachita Mountains, Arkansas: AAPG Search and Discovery Article #90124 © 2011 AAPG Annual Convention and Exhibition, April 10-13, 2011, Houston, Texas.

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Melezhik, V. A., A. E. Fallick, D. V. Rychanchik, and A. B. Kuznetsov, 2005, Palaeoproterozoic evaporites in Fennoscandia: implications for seawater sulphate, the rise of atmospheric oxygen and local amplification of the delta C-13 excursion: Terra Nova, v. 17, p. 141-148.

Milliken, K. L., 1979, The silicified evaporite syndrome; two aspects of silicification history of former evaporite nodules from southern Kentucky and northern Tennessee: Journal Sedimentary Petrology, v. 49, p. 245-256.

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Ramseyer, K., J. E. Amthor, A. Matter, T. Pettke, M. Wille, and A. E. Fallick, 2013, Primary silica precipitate at the Precambrian/Cambrian boundary in the South Oman Salt Basin, Sultanate of Oman: Marine and Petroleum Geology, v. 39, p. 187-197.

Reid, S. A., and J. L. McIntyre, 2001, Monterey Formation porcellanite reservoirs of the Elk Hills field, Kern County, California: Bulletin American Association Petroleum Geologists, v. 85, p. 169-189.

Rouchy, J. M., C. Taberner, M. M. Blanc-Valleron, R. Sprovieri, M. Russell, C. Pierre, E. Di Stefano, J. J. Pueyo, A. Caruso, J. Dinares-Turell, E. Gomis-Coll, G. A. Wolff, G. Cespuglio, P. Ditchfield, S. Pestrea, N. Combourieu-Nebout, C. Santisteban, and J. O. Grimalt, 1998, Sedimentary and diagenetic markers of the restriction in a marine basin: the Lorca Basin (SE Spain) during the Messinian: Sedimentary Geology, v. 121, p. 23-55.

Schroder, S., A. Bekker, N. J. Beukes, H. Strauss, and H. S. van Niekerk, 2008, Rise in seawater sulphate concentration associated with the Paleoproterozoic positive carbon isotope excursion: evidence from sulphate evaporites in the 2.2-2.1 Gyr shallow-marine Lucknow Formation, South Africa: Terra Nova, v. 20, p. 108-117.

Scott, C., B. A. Wing, A. Bekker, N. J. Planavsky, P. Medvedev, S. M. Bates, M. Yun, and T. W. Lyons, 2014, Pyrite multiple-sulfur isotope evidence for rapid expansion and contraction of the early Paleoproterozoic seawater sulfate reservoir: Earth and Planetary Science Letters, v. 389, p. 95-104.

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Warren, J. K., 1999, Evaporites: their evolution and economics: Oxford, UK, Blackwell Scientific, 438 p.

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

Zemmels, I., P. L. Grizzle, C. C. Walters, and F. R. Haney, 1985, Devonian Novaculites as Source of Oil in Marathon-Ouachita Thrust System (Abstract): Bulletin American Association Petroleum Geologists, v. 69, p. 318-319.


 


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