Formation Of Red Beds Research Articles

Diagenetic processes and the mineralization in the triassic of Central England

Continental red beds are the host rocks of a characteristic style of mineralization which suggests a genetic link between red bed formation and ore formation. Samples of unmineralized and mineralized Triassic sediments from Central England have been studied sedimentologically, petrographically and geochemically with the aim of clarifying this link which may provide valuable guides for exploration. On the basis of sedimentological and petrographic observations it is suggested that these red beds were formed as a result of diagenetic alteration whereby detrital silicates and oxides are progressively dissolved and the iron released is deposited as hematite. A model for mineralization is proposed involving the release of trace metals from detrital minerals during diagenesis, their retention in saline interstitial solutions, migration to suitable sites of precipitation and deposition by reaction with trapped hydrocarbons or reduced sulphur.

Iron coating in recent terrace sequences under extremely arid conditions

Summary Precise documentation of ferric oxide coating on calcareous sands of 13–15 recent alluvial fan terraces in the Dead Sea area, Israel, indicates a gradual ferric enrichment over the last 12,00 years. Airborne dust is suggested as the main source. The staining on the low terraces indicates that coating during short increments of time than hitherto generally accepted, up to periods of a few tenths of years, is distinguishable in an extremely arid environment. The results suggest an initial stage of alluvial red bed formation.

Rate of dune reddening in a humid tropical climate

The formation of red beds has long interested geologists and pedologists1–3. It has been suggested that the nature and degree of reddening in dune sands can be a useful indicator of the relative age and environmental history of the sands; several authors have concluded that dune sands undergo progressive reddening with time4–7, and James and Stanley8 considered that coastal dunes might actually be mapped on the basis of colour. However, quantitative data regarding the rate of reddening in different environmental conditions are generally lacking. I present here radiocarbon evidence from north-east Australia which suggests that red weathering profiles have developed in stabilized dunes of Holocene age in humid tropical conditions within the past 7,500 yr.

Nearshore Marine and Continental Facies in Eocene of North-Central Pakistan: ABSTRACT

Stable-shelf carbonate sedimentation along the northwestern edge of the Indian subcontinent preceded the post-mid-Eocene Indian-Asian collision. The early Eocene section in Pakistan displays very rapid facies changes controlled by a cycle of regression and transgression. Beginning with the Paleocene Patala Formation in the Kohat area, quiet-water offshore dark shales grade up-section to include increasingly thick, extensive, and common marly limestones, becoming a foraminiferal limestone sequence. This section then becomes shalier with progressively thinner and more argillaceous micrites and grades upward into the unfossiliferous green Panoba Shale, which then passes into the nearshore, medium-energy, fossiliferous, and bioturbated limestones of the Shekhan Formation. The upper Shekhan beds are mud-cracked, festoon-bedded, channel-form dolostones, presumably tidal deposits. The topmost dolostones contain zones of small disruptive anhydrite nodules and pass rapidly into gypsum laminated with varicolored clays. To the west, the Panoba Shale and the Shekhan Formation grade into a massive salt deposit; to the northeast they grade into deeper water limestone. The evaporites are interpreted as sabkha deposits. All are covered by the mostly continental, mammal-bearing Kuldana Formation red beds. Drowning of the coastline then caused rapid development of (1) local lacustrine dolomite and chert units, (2) oyster-rich lagoonal or estuarine limestones, and finally (3) open-bay nummulitic limestones and shales of the mid-Eocene Kohat Formation. The succession is trun ated by a regional unconformity that records uplift, erosion, and dolomitization of the underlying carbonate rocks. The unconformity is then buried by continental Himalayan molasse. End_of_Article - Last_Page 802------------

Detrital magnetization in red beds of the Moenkopi Formation (Triassic), Gray Mountain, Arizona

Specularite, apparently formed and in part altered to red hematite before deposition, carries much of the stable magnetization in sandstone, siltstone, and claystone of the Moenkopi Formation (Lower Triassic) at Gray Mountain, northern Arizona. High‐temperature exsolution textures seen in polished section indicate that some, if not much, of the specularite is detrital. Progressive thermal and chemical demagnetization analyses indicate that the most stable magnetization resides in specularite. Last, a systematic depositional inclination ‘error’ is seen in both normally and reversely polarized sandstone. Part of its cause was the deposition along fine bedding laminations of subtabular grains of specularite carrying a strong direction of magnetization in the plane of tabularity. Magnetic inclinations are significantly shallower in sandstone than in siltstone, and the amount and sense of inclination error are controlled in detail by the dip of the horizontal and cross laminations. The foregoing leads to the conclusion that the stable magnetization is a detrital magnetization acquired during the course of deposition and that the Moenkopi Formation thus is suitable for magnetostratigraphy. Neither the formation of specularite nor the acquisition of the stable magnetization appears to be the consequence of prolonged and complicated postdepositional chemical alteration, a process invoked by some workers for formation and magnetization of ancient red beds. Because specularite is common in other ancient red bed sequences, their stable magnetizations also may be partly or largely detrital.

Zur geochemie der sedimentite des Permosiles im Südteil der D.D.R.

Since the beginning of this century the late Variscan red bed formations were said to be the source of the metals of the Upper Permian “Kupferschiefer”-mineralization. Up to the last years there was a lack of regional investigations of the geochemistry of these rocks. To prove the above mentioned theory, we determined the Fe-, Corg-, S-, Cu-, Pb-, Zn-, Ni-, Co-, Mn-, B-, Ba-, Sr-, Rb-, V-, Cr-, Ti-, Zr- and Sn- contents of more than 2000 samples of red, grey and bleached psephitic, psammitic and pelitic sedimentary rocks and of some coal samples. In all investigated rock types the average Fe-, Ni- and Cr-contents are higher in the red-coloured rocks than in the grey and bleached ones; the average B-, Rb- and Ba-contents are equal in the red, grey and bleached rocks; the average Corg-, S-, Cu-, Pb- and Zn-contents are higher in the grey rocks than in the red-coloured ones. Only in the last group of elements the average contents are higher than the planetary Clarke of each rock type. Special investigations were made about geochemical facies, distribution of base metals, diagenetic and epigenetic influences on the distribution of base metal mineralizations and the source of elements. The late Variscan volcanism was proved to be the main source of elements in the red bed formations. The sedimentary and magmatic rocks of the molasse stage are Pb-specialized, therefore the Central European Variscan belt forms a lead province.

A red-bed formation in the South Bohemian Basins, Czechoslovakia

Tectonic activity, climatic changes and associated weathering cooperated during the formation of Upper Cretaceous red beds of the South Bohemian Basins known as the Klikov Formation. The sediments are clastic and comprise: (1) light-grey or yellow conglomeratic, course-to-medium sandstone beds; (2) generally finer red beds; and (3) grey beds. They alternate in asymmetrical cycles, in succession fining upwards. Small- and large-scale cyclothems were recognized. The large-scale cyclothems are closely connected with paleogeographical changes and tectonic evolution of the South Bohemian Basins in Early Senonian time. In regard to rapid vertical and lateral lithological variations, the common presence of graded bedding, poor sorting and lack of fossils, the sediments are comparable to the fluviatile facies of molasse, known as “flysch in molasse”. They were deposited from highly fluctuating currents and periodically overloaded streams in an alluvial and/or lacustrine environment, suffering continuously from tectonic unrest emanating from the Alpine—Carpathian geosyncline. Differences between red and grey sediments are related mostly to the primary distribution and preservation of organic matter and to some extent to the redistribution of iron during early diagenetic changes (e.g. red stains). Ancient weathered gneiss and granite profiles preserved beneath the sediments show development of either two (on granite) or three (on gneiss) horizons differing in degree of weathering and distribution of red colour within the profiles. The trend of weathering documented by chemical analyses and presence of kaolinite as the end-product points to the red podzolic soil formation process.

Petrology and Origin of the Red Beds of the Perry Formation New Brunswick, Canada, and Maine, USA

ABSTRACT Fault trough deposition during the Late Devonian in the Perry Formation of Maine and Canada produced texturally and mineralogically immature red and green sandstones as well as conglomerates and mudstones containing angular clasts and hematite and calcite cement. Deposition occurred in two separate basins, each with different source areas. The origin of the red color of the Perry Formation is two fold. Some of the red pigment is primary, derived from underlying older lithologic units. Secondly, mafic minerals such as magnetite and hornblende, were altered and partially removed by intrastratal solutions providing in situ alteration to form additional hematite. Calcareous crusts associated with these sediments indicate they probably were formed in an arid setting. Once formed, th se crusts impeded upward migrating iron-laden groundwater, trapping some iron in cracks and fractures below the crusts. Migration and deposition of iron in solution by groundwaters is suggested as an agent which aided in the formation of the red beds. The iron in solution might have been derived from an external source in the groundwater recharge area to supplement iron formed by in situ alternation of mafic minerals.

Development of Chemical Remanent Magnetization during Early Stages of Red-Bed Formation in Late Cenozoic Sediments, Baja California

Petrographic, rock magnetic, and paleomagnetic studies of fine-grained red sediments of late Cenozoic age in Baja California show that the sediments have variably acquired chemical remanent magnetization (CRM) overprints that have obscured the original magnetization of the deposits. The chemical remanence in the sediments is carried predominantly by three authigenic minerals — hematite, goethite, and a Mn · Ba compound, herein called “hydropsilomelane” — that occur as pigments and as concretions. Remanence directions generally associated with each mineral are goethite, reverse; hydropsilomelane, normal; and hematite, normal or reverse. Some samples possess a remanence that is strong and normal or strong and reverse; these generally contain only one of the authigenic minerals in abundance. Many samples, however, are weak in intensity and random in direction. When such samples are split into parts and measured, it is generally found that each part is strongly magnetized but that some parts are normal and others are reverse in direction. In such cases, the magnetization of the whole sample is resultant of the multiple components that are generally carried by two or more of the authigenic minerals. The following conclusions can be drawn concerning the acquisition of CRM in the Baja California deposits: (1) The sediments contain chemically unstable iron- and manganese-bearing minerals, such as hornblende and biotite, that are susceptible to postdepositional alteration, and they have provided the parent material for the authigenic magnetic minerals. (2) Authigenic magnetic minerals, growing from crystallites, generally acquired a remanence that was parallel to the Earth9s field when they surpassed the critical grain size. (3) The rate of CRM acquisition has not been uniform in these sediments, probably because the processes of alteration and formation of authigenic magnetic minerals depend on an interplay of highly variable factors such as the chemistry of the interstitial water, hydraulic gradients, and mineralogy of the sediments. (4) Complex variability in acquisition of CRM has led to a remanence stratigraphy that bears little discernible correlation with the geomagnetic field at the time of deposition.

Formation of Red Beds in Moist Tropical Climates: A Hypothesis

Studies of alluvial deposits of Holocene and Pleistocene age in Puerto Rico and in The Orinoco basin suggest that red beds can form diagenetically in moist tropical climates by intrastratal alteration processes that are similar to those producing red beds diagenetically in deserts. The studies show that modern sediments from these tropical regions contain ample iron, in the form of both detrital oxides and unstable iron-bearing silicates, to produce bright red sediments if the interstitial chemical environment is favorable for the formation and preservation of iron oxide. That such favorable environments exist in some tropical regions is indicated by the fact that yellow and brown iron oxides commonly occur in Quaternary alluvial deposits in Puerto Rico many tens of feet below the water table. In addition, chemical analyses of ground-water samples from Puerto Rico show that the interstitial environment in the alluvium commonly lies in the stability field of hematite. These data indicate that sediments which may be precursors of red beds are accumulating in Puerto Rico today. Where favorable interstitial chemical conditions persist long enough for the yellow and brown oxides (both detrital and authigenic) to be converted to red oxides, these deposits should produce red beds. Such deposits may be modern analogues of ancient red beds associated with fauna, flora, or other evidence of warm, moist conditions at the time of deposition. Chemical and mineralogic analyses of samples from Puerto Rico and the Orinoco basin, when compared with analogous data from the Sonoran Desert, do not reveal any criterion that can be confidently extrapolated to ancient sediments to differentiate red beds formed in moist climates from those formed in deserts. Other characteristics of ancient red beds, such as fauna, flora, and association with evaporite minerals or with aeolian sandstone, provide the most reliable evidence of the climate at the time of deposition.

Structures in the Iranides of South-eastern Turkey

The effects of two phases of deformation in Cretaceous rocks of the Alpine Orogenic Zone of south-eastern Turkey are described. These can be correlated with the late Cretaceous and Tertiary phases of deformation already known from the zone of foreland folding to the south. Some details of the stratigraphical succession are given and a previously unrecorded development of Oligocene rocks is described. The upper Cretaceous sediments are dominantly marine carbonates but include a red bed formation. Basic volcanics are intercalated with the lower carbonate beds. A profound unconformity separates the Eocene from the Upper Cretaceous. This unconformity results from uplift consequent upon the first phase of deformation which produced north-westward plunging folds and related thrusts. Some of these north-westerly folds have been considerably modified by the superposition of younger east-north-easterly trending Alpine folds and thrusts.

The Permian-Triassic Boundary in New Zealand and New Caledonia and Its Relationship to World Climatic Changes and Extinction of Permian Life [Abstract

Abstract In New Zealand the stratigraphic contact between Triassic and Permian is generally unconformable, and there is no faunal intergradation. Griesbachian and Dienerian (basal Triassic) faunas are not known. The Permian segment is unusually thick, almost entirely marine, and moderately fossiliferous. The penultimate faunas, characteristic of the Waiitian Stage, are normal Permian faunas, approximately equivalent to the middle Dzhulfian zones of Armenia and Iran, Japan (Gujo), upper Ferntree Group of Tasmania, and upper Bellerophonkalk of Italy and Austria. Younger faunas, equivalent to the so-called Eotriassic of Armenia and Iran, are not present, though marine rocks are found. The topmost Permian fauna, characteristic of the Makarewan Stage of New Zealand, unlike the preceding faunas, lacks any of the major brachiopod groups, such as Stropho-menida or Productida which virtually disappeared at the end of the Paleozoic era. The brachiopod genera are members of orders and families which survived into the Triassic, such as Rhynchonellida, Spiriferacea and Dielasmatidae, but the genera are characteristic of the Permian Period. It is thus possible that the Makarewan Stage represents the very latest Permian, and the most convincing transition yet known into Triassic. The earliest Triassic in New Zealand contains poorly-dated bivalves. The earliest ammonoids are of middle Scythian, or Smithian age. The contact between Permian and Triassic in New Caledonia is less well exposed, and falls somewhere between brachiopods and bivalves of Capitanian (= basal Tatarian) age, equivalent to the Puruhauan Stage of New Zealand and Ladinian brachiopods. Ammonoids, including Xenodiscids, have been described by Avias and Guerin (1958) as either Late Permian or Early Triassic. Some are ascribed to Xenaspis of Middle Permian (Wargal-Chhidru age) but are accompanied by the Scythian genus Meekoceras. Mid-Permian Cyclolobus has also been identified. The sequence of Permian faunas in New Zealand provide a key to the nature of the Permian-Triassic contact. Three faunas in the sequence of eight are relatively impoverished generically, with strong affinities to faunas of eastern Australia, and coincide in age with the main glacial phases of the east Australian Permian. Overlying faunas are more diversified, and therefore, indicate relatively warmer water. Following faunas are very diverse and include Fusulinacea and reef-building corals, absent from the other faunal suites. Each warm-water fauna is followed by an abrupt faunal change to a cold-water fauna. This pattern of three cold episodes followed by warmer faunas is also reflected widely by faunas in the Northern Hemisphere through Canada and Siberia, and the cold episodes even affected paleotropical regions such as Texas, when cold-water genera such as Yakovlevia and Spiriferella were introduced for brief times. The pattern of glaciation and amelioration is also reflected in an intricate way by the nature of sedimentation over the entire globe, particularly in the formation of coral reefs, coal measures, tillites, salt deposits and red beds. Climatic changes provide a simple explanation of the great destruction of life at the end of the Permian Period. This is considered to have been real, affecting over 50 per cent of all life. Faunal analyses show that the genera and families which perished were essentially tropical in habitat, and that a prime cause lay in unusually high temperatures for a brief interval.

The Distribution and Formation of Permian-Triassic Red Beds [Abstract

The Distribution and Formation of Permian-Triassic Red Beds [Abstract

Formation of Red Beds in Modern and Ancient Deserts: Reply

Research Article| February 01, 1968 Formation of Red Beds in Modern and Ancient Deserts: Reply THEODORE R WALKER THEODORE R WALKER DEPT. GEOLOGICAL SCIENCES, UNIVERSITY OF COLORADO, BOULDER, COLORADO Search for other works by this author on: GSW Google Scholar GSA Bulletin (1968) 79 (2): 281–282. https://doi.org/10.1130/0016-7606(1968)79[281:FORBIM]2.0.CO;2 Article history received: 10 Jul 1967 first online: 02 Mar 2017 Cite View This Citation Add to Citation Manager Share Icon Share Twitter LinkedIn Tools Icon Tools Get Permissions Search Site Citation THEODORE R WALKER; Formation of Red Beds in Modern and Ancient Deserts: Reply. GSA Bulletin 1968;; 79 (2): 281–282. doi: https://doi.org/10.1130/0016-7606(1968)79[281:FORBIM]2.0.CO;2 Download citation file: Ris (Zotero) Refmanager EasyBib Bookends Mendeley Papers EndNote RefWorks BibTex toolbar search Search Dropdown Menu toolbar search search input Search input auto suggest filter your search All ContentBy SocietyGSA Bulletin Search Advanced Search Abstract No Abstract available This content is PDF only. Please click on the PDF icon to access. First Page Preview Close Modal You do not have access to this content, please speak to your institutional administrator if you feel you should have access.

Formation of Red Beds in Modern and Ancient Deserts: Discussion

Research Article| February 01, 1968 Formation of Red Beds in Modern and Ancient Deserts: Discussion ROBERT F SCHMALZ ROBERT F SCHMALZ THE PENNSYLVANIA STATE UNIVERSITY, UNIVERSITY PARK, PENNSYLVANIA Search for other works by this author on: GSW Google Scholar GSA Bulletin (1968) 79 (2): 277–280. https://doi.org/10.1130/0016-7606(1968)79[277:FORBIM]2.0.CO;2 Article history received: 05 May 1967 first online: 02 Mar 2017 Cite View This Citation Add to Citation Manager Share Icon Share Facebook Twitter LinkedIn MailTo Tools Icon Tools Get Permissions Search Site Citation ROBERT F SCHMALZ; Formation of Red Beds in Modern and Ancient Deserts: Discussion. GSA Bulletin 1968;; 79 (2): 277–280. doi: https://doi.org/10.1130/0016-7606(1968)79[277:FORBIM]2.0.CO;2 Download citation file: Ris (Zotero) Refmanager EasyBib Bookends Mendeley Papers EndNote RefWorks BibTex toolbar search Search Dropdown Menu toolbar search search input Search input auto suggest filter your search All ContentBy SocietyGSA Bulletin Search Advanced Search Abstract No Abstract available This content is PDF only. Please click on the PDF icon to access. First Page Preview Close Modal You do not have access to this content, please speak to your institutional administrator if you feel you should have access.

Formation of Red Beds in Modern and Ancient Deserts

Research Article| March 01, 1967 Formation of Red Beds in Modern and Ancient Deserts THEODORE R WALKER THEODORE R WALKER University of Colorado, Boulder, Colorado Search for other works by this author on: GSW Google Scholar GSA Bulletin (1967) 78 (3): 353–368. https://doi.org/10.1130/0016-7606(1967)78[353:FORBIM]2.0.CO;2 Article history received: 28 May 1965 first online: 02 Mar 2017 Cite View This Citation Add to Citation Manager Share Icon Share Facebook Twitter LinkedIn MailTo Tools Icon Tools Get Permissions Search Site Citation THEODORE R WALKER; Formation of Red Beds in Modern and Ancient Deserts. GSA Bulletin 1967;; 78 (3): 353–368. doi: https://doi.org/10.1130/0016-7606(1967)78[353:FORBIM]2.0.CO;2 Download citation file: Ris (Zotero) Refmanager EasyBib Bookends Mendeley Papers EndNote RefWorks BibTex toolbar search Search Dropdown Menu toolbar search search input Search input auto suggest filter your search All ContentBy SocietyGSA Bulletin Search Advanced Search Abstract New evidence supports the theory that the hematite pigment in many red beds, particularly those associated with evaporites and aeolian sandstones, formed after deposition in hot arid or semiarid climates. The evidence includes field, petro-graphic, and chemical data collected from studies of two stratigraphic sequences that contain red beds: (1) Recent, Pleistocene, and Pliocene deposits in the Sonoran desert of northeastern Baja California, Mexico, and (2) late Paleozoic deposits in Colorado.The sequence in the Sonoran desert contains examples of red beds forming today in a hot dry climate. They are associated with bedded evaporites and occur where regional faunal, floral, and pedological evidence indicates rainfall has been low throughout the postdepositional history of the sediments. The facies associations reflect deposition in fluvial and fluvial-marine transitional environments. Red arkose fanglomerates occur on the flanks of the highland source areas, and red muds, probably of intertidal and shallow subtidal origin, occur in the transition sediments. Both of these red-stained facies show progressive stages of in situ alteration of nonred sediments to hematite-stained red beds, and in each, the iron in the stain is derived from intra-stratal alteration of iron-bearing detrital grains, particularly iron silicates such as hornblende and bio-tite.The late Paleozoic red beds of Colorado contain rock types and facies associations similar to those of the Sonoran desert; they are interpreted as ancient counterparts of those red beds. Numerous lines of field and petrographic evidence indicate that the hematite pigment in the late Paleozoic red beds formed in place after the sediments were deposited in desert basins. This content is PDF only. Please click on the PDF icon to access. First Page Preview Close Modal You do not have access to this content, please speak to your institutional administrator if you feel you should have access.

Occurrence of Detrital Magnetite and Ilmenite in Red Sediments: New Approach to Significance of Redbeds: GEOLOGICAL NOTES

In mottled red and green sedimentary rocks, detrital magnetite and ilmenite are abundant in the red zones and have been removed by solution from the reduced zones. Study of available specimens has shown that all redbeds contain detrital magnetite or ilmenite, commonly in abundance; gray, green, or white sedimentary rocks contain little or none. It is suggested, therefore, that the formation of redbeds depends primarily on the presence of an igneous or metamorphic source which supplies detrital magnetite or ilmenite, and is only indirectly dependent on climate or environment of deposition. This hypothesis explains why most redbeds are related to the arkose or graywacke clans. Magnetite is abundant as an accessory mineral in igneous rocks; its general paucity in all except he red sediments is caused by its solution under the reducing conditions in which most sediments form.

Geological Exploration Between Upper Jurua River, Brazil, and Middle Ucayali River, Peru

The northern Territory of Acre, in the Alto Jurua River area, Brazil, and the middle valley of the Ucayali River, Peru, have not been studied geologically heretofore. It is a sparsely inhabited region. Flat plains, swamps, and tropical jungle make precise geological work in a short time rather precarious. However, as this contribution emphasizes, stratigraphical and structural conditions in the northwestern Territory of Acre, particularly the Serra do Moa region, show possibilities of important petroleum accumulations and the area deserves detailed surveying. The sediments range in age from Lower Cretaceous to Pleistocene and are of continental and marine intermittent deposition, although poorly fossiliferous. No rocks of igneous origin were observed. Tertiary and Cretaceous formations of the Pachitea, Pongo de Manseriche, and Contamana areas, Peru, can be stratigraphically correlated with those of the Serra do Moa and upper Jurua areas in the northwestern Territory of Acre. The structural characteristics correspond with the physiographical features. The Serra do Moa Range, of Andean folding and apparently the last eastern spur of the Cordillera Oriental, is an anticline in partly Cretaceous beds, traversed by several tributaries of the upper Jurua. Although oil seeps were not observed in the Serra do Moa region, they have been found in the headwaters of the Ahuaya River, a tributary of the upper Cashiboya River. The seeps occurred in faults in hard, red clay sandstones of the red-bed formation; the exact horizon from which the petroleum generated is not known since many seeps occur in Tertiary or Cretaceous outcrops. In the Pachitea River district, seeps have been observed and drilling is planned for the near future by a private concern. The region of the upper Jurua geologically is a part of the potentially oil-bearing structural belt extending along the eastern foothills of the Andes, south through Bolivia into Argentina and north through eastern Peru into Colombia and Venezuela.

The Origin of Red Beds: A Study of the Conditions of Origin of the Permo-Carboniferous and Triassic Red Beds of the Western United States

Previous articleNext article FreeThe Origin of Red Beds: A Study of the Conditions of Origin of the Permo-Carboniferous and Triassic Red Beds of the Western United StatesC. W. TomlinsonC. W. Tomlinson Search for more articles by this author PDFPDF PLUS Add to favoritesDownload CitationTrack CitationsPermissionsReprints Share onFacebookTwitterLinkedInRedditEmail SectionsMoreDetailsFiguresReferencesCited by The Journal of Geology Volume 24, Number 3Apr. - May, 1916 Article DOIhttps://doi.org/10.1086/622326 Views: 34Total views on this site Citations: 3Citations are reported from Crossref PDF download Crossref reports the following articles citing this article:X. R. Ming, L. Liu, M. Yu, H. G. Bai, L. Yu, X. L. Peng, T. H. Yang Bleached mudstone, iron concretions, and calcite veins: a natural analogue for the effects of reducing CO 2 -bearing fluids on migration and mineralization of iron, sealing properties, and composition of mudstone cap rocks, Geofluids 16, no.55 (Nov 2016): 1017–1042.https://doi.org/10.1111/gfl.12203Jarmila Slánská A red-bed formation in the South Bohemian Basins, Czechoslovakia, Sedimentary Geology 15, no.22 (Feb 1976): 135–164.https://doi.org/10.1016/0037-0738(76)90041-5E. Bölau Rote Tone im Rhät-Lias Schonens, Geologiska Föreningen i Stockholm Förhandlingar 76, no.22 (Jan 2010): 215–233.https://doi.org/10.1080/11035895409453538