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Journal articles on the topic 'Oolitic ironstone'

Author: Grafiati

Published: 4 June 2021

Last updated: 7 February 2022

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1

Taylor, Kevin G. "Non-marine oolitic ironstones in the Lower Cretaceous Wealden sediments of southeast England." Geological Magazine 129, no. 3 (May 1992): 349–58. http://dx.doi.org/10.1017/s0016756800019282.

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AbstractOolitic ironstones are described from the early Cretaceous non-marine Wealden sediments of southeast England. The recognition of non-marine oolitic ironstones in the geological record is rare and, therefore, warrants further study. The oolitic ironstones described take two forms, named here type-I and type-2 ironstones.Type-1 ironstones contain pisoids and ooids of berthierine together with sandstone fragments and detrital quartz grains. The pisoids (up to 0.5 cm in size) vary from subspherical to highly irregular. The smaller ooids (up to 1 mm in size) are generally ellipsoidal but strongly asymmetrical forms are also present. The form of these pisoids and ooids suggest that mechanical accretion was not the dominant mechanism controlling their formation. It is proposed that this ironstone type formed from the reworking and redeposition of local soil material.Type-2 ironstones, of which only one unequivocal example has been studied, is composed of iron oxide ooids set in a detrital matrix. The ooids are most commonly regularly ellipsoidal and exhibit a decrease in iron at their centres. It is proposed here that the ooids suffered post-depositional iron depletion at their centres, in a similar fashion to that proposed for the recent Lake Chad oolites. There is no unequivocal evidence as to the origin of the ooids.This study is important in that it shows that different ironstones can be formed by different processes essentially within the same environment. Comparison of non-marine oolitic ironstones with the better-developed marine examples should prove a valuable exercise.

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2

Poudel, Lalu, and Sujan Devkota. "Petrology and Genesis of the Bhainskati Iron Ore Deposit of Palpa District, Western Nepal." Tribhuvan University Journal 28, no. 1-2 (December 2, 2013): 153–60. http://dx.doi.org/10.3126/tuj.v28i1-2.26237.

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The Bhainskati Formation of the Tansen Group in Palpa area is known for hematite iron ore deposit for long time. A prominent band of hematite of about 1-2 km thickness extending >5 km was identified in the upper part of the Bhainskati Formation in the present study and the band is repeated three times in the area by folding and faulting. Petrographic study shows that it is oolitic ironstone of sedimentary shallow marine origin. Main minerals in the band are hematite, goethite, quartz, calcite, siderite and albite. Hematite content varies considerably among samples and occurs mainly as oolite and cement. The Bhainskati ironstone with its ferrous mineral assemblage and well-rounded texture of the ooids suggests prodeltaicto estuarine with shallow marine environment reduced clastic input.

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3

Devkota, Sujan, and Lalu Prasad Paudel. "Petrology and genesis of the Bhainskati iron ore deposit of Palpa District, western Nepal." Bulletin of the Department of Geology 15 (January 21, 2013): 63–68. http://dx.doi.org/10.3126/bdg.v15i0.7418.

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The Bhainskati Formation of the Tansen Group in the Palpa area is known for hematite iron ore deposit for long time. A prominent band of hematite of about 1-2 m thickness and extending >5 km was identified in the upper part of the Bhainskati Formation in the present study. The band is repeated three times in the area by folding and faulting. Petrographic study shows that it is oolitic ironstone of sedimentary origin. Main minerals in the band are hematite, goethite, quartz, calcite, siderite and albite. Hematite content varies considerably among samples and occurs mainly as oolite and cement. The Bhainskati ironstone with its ferrous mineral assemblage and well-rounded texture of the ooids suggests shallow marine environment (prodeltaic to estuarine) with reduced clastic input. DOI: http://dx.doi.org/10.3126/bdg.v15i0.7418 Bulletin of the Department of Geology, Vol. 15, 2012, pp. 63-68

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4

Ozulu, George Uchebike, Anthony Uwaoma Okoro, and Evangeline Njideka Onuigbo. "Sedimentary facies and environments of the sedimentary fill of Southern Bida Basin, Nigeria." Global Journal of Geological Sciences 19, no. 1 (July 13, 2021): 53–74. http://dx.doi.org/10.4314/gjgs.v19i1.5.

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Six lithofacies were identified in the Lokoja Formation, Southern Bida Basin: fanglomerate/ conglomerate lithofacies (Gmc), fine to coarse-grained ferruginized weakly cross-bedded, pebbly sandstone lithofacies (Scx), fine to coarsegrained sandstone lithofacies (Sfc), silty claystone lithofacies (Csm), siltstone lithofacies (Slt) and lateritic ironstone lithofacies (Ilt). These were grouped into three lithofacies associations viz: alluvial fan, braided river channel, floodplain lithofacies association. Nine lithofacies were identified in the Ahoko Formation. These are: black-dark grey carbonaceous shale lithofacies (Shc), bioturbated ripple-laminated siltstone lithofacies (Sbr), poorly cross-laminated claystone lithofacies (Cxl), concretionary/nodular ironstone lithofacies (Icn), medium to coarse-grained sandstone lithofacies (Smc) fine grained, well-sorted, friable bioturbated herringbone cross-bedded sandstone lithofacies (Sxf), massive brownish claystone lithofacies (Clm), massive claystone with lateritic ironstone lithofacies (Cli) and lateritic ironstones lithofacies (Ilt). These have been grouped into three lithofacies associations viz: shallow marine lithofaciesassociation, tidal-intertidal flat lithofacies association and floodplain lithofacies association. Similarly, three lithofacies were identified in the Agbaja Formation and have been grouped into two lithofacies association. These are: fine to medium-grained sandstone ironstone interbedded lithofacies (Sti), oolitic–pisolitic ironstone lithofacies (Iop) and concretionary ironstone lithofacies (Icr). The lithofacies associations are: tidal-intertidal flat lithofacies association and shallow marine lithofacies association. Result of lithofacies analysis helped in interpreting the depositional environments. The Lokoja Formation is a product of a fluvial dominated alluvial system from debris/gravity flow in alluvial fan. This developed further into braided river channels and later meandering river during the closing stages. Sediments of the Ahoko Formation were deposited in tidal/intertidal flats and shallow marine environments while sediments of the Agbaja Formation were produced by a shallow marine system with a high tidal influence.

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5

Guerrak, S. "Paleozoic patterns of oolitic ironstone sedimentation in the Sahara." Journal of African Earth Sciences (and the Middle East) 12, no. 1-2 (January 1991): 31–39. http://dx.doi.org/10.1016/0899-5362(91)90055-4.

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6

Villas, E. "New Caradoc brachiopods from the Iberian Chains (northeastern Spain) and their stratigraphic significance." Journal of Paleontology 66, no. 5 (September 1992): 772–93. http://dx.doi.org/10.1017/s0022336000020795.

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New collections of Caradoc brachiopods from the lower half of the Fombuena Formation in the Iberian Chains (northeastern Spain) have yielded rich fossil associations that, in spite of the endemism of most of their species, permit detailed correlations with other sequences in southwestern Europe, Bohemia, and the British Isles. The oldest association studied occurs at the top of the basal oolitic ironstone of the Fombuena Formation, where 10 brachiopod species have been recorded; the youngest association occurs in sandstones in the middle part of the unit, having yielded seven brachiopod species. Herein, 11 forms are described including four new species (Gelidorthis carlsi, Saukrodictya tormoensis, Reuschella herreraensis, and Rostricellula marciali) and one new subspecies (Aegiromena aquila intermedia). The stratigraphic setting of the oolitic ironstone and its brachiopods suggest a correlation with similar beds that crop out at various localities in the Iberian Peninsula and northwestern France, as well as with the Zdice-Nucice Iron Ore, placed at the base of the Vinice Formation in Bohemia. The regressive–transgressive cycle, whose point of maximum shoaling coincides with the deposition of the apparently widespread ferruginous bed, is restricted to the Mediterranean Province and may have been caused by regional epeirogenic movements. The stratigraphic gap marked by the ironstone had been assessed at several localities in Iberia and Armorica; it ranges from late Costonian to Soudleyan, an age not in disagreement with the occurrence of a new species of Reuschella immediately above the ironstone of the Iberian Chains, since Reuschella is not known before the Soudleyan. Dalmanella unguis unguis, which has been recorded in the youngest assemblage and which in Wales is restricted to the Marshbrookian, is another important guide form in the problematic correlation between the Mediterranean Caradoc and the British type sequence.

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7

Abazar, M. A. Daoud, M. A. Rashed, A. M. Elsharief, N. Sediek Kadry, and A. M. Elamein. "The geotechnical properties of the oolitic ironstone formation, Wadi Halfa, North Sudan." Journal of Geology and Mining Research 12, no. 1 (February 29, 2020): 25–34. http://dx.doi.org/10.5897/jgmr2019.0326.

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8

Gehring, A. U., and R. Karthein. "An ESR and calorimetric study of iron oolitic samples from the Northampton ironstone." Clay Minerals 25, no. 3 (September 1990): 303–11. http://dx.doi.org/10.1180/claymin.1990.025.3.06.

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AbstractElectron spin resonance (ESR) spectroscopy and calorimetric methods were used to characterize conversion processes in multimineral samples from the Northampton ironstone (NIS) at temperatures between 25°C and 800°C. The beginning of the thermal conversion processes can be determined by the formation of asymmetric ESR spectra with g ≈ 2 at 250°C. The breakdown of the berthierine structure between 250°C and 520°C is indicated by the disappearance of the hyperfine splitting in the Mn2+ spectrum and the formation of magnetite. The decomposition of siderite and calcite was found by calorimetric methods at 580°C and 700°C, respectively. The hematite formation between 550°C and 800°C is explained by the decomposition of siderite but also by the oxidation of previously formed magnetite. The occurrence of hematite as the dominant ferric oxide at 800°C signifies the end of the conversion process of the major mineral phases in the NIS samples.

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9

Berendsen, Pieter, John H. Doveton, and Stanislaw Speczik. "Distribution and characteristics of a Middle Ordovician oolitic ironstone in northeastern Kansas based on petrographic and petrophysical properties: a Laurasian ironstone case study." Sedimentary Geology 76, no. 3-4 (March 1992): 207–19. http://dx.doi.org/10.1016/0037-0738(92)90084-5.

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10

Opeloye, Saka Adelayo, John Olurotimi Amigun, Sherif Olumide Sanusi, and Olujide Alabi. "Palaeoenvironmental reconstruction and oolitic ironstone mapping of the Agbaja Ironstone Formation in the Nupe Basin, North-central Nigeria: Insights from sedimentological and aeromagnetic analyses." Results in Geophysical Sciences 5 (March 2021): 100010. http://dx.doi.org/10.1016/j.ringps.2021.100010.

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11

Duan, Chao, Yanhe Li, Yun Yang, Yongsheng Liang, Minghui Wei, and Kejun Hou. "U-Pb Ages and Hf Isotopes of Detrital Zircon Grains from the Mesoproterozoic Chuanlinggou Formation in North China Craton: Implications for the Geochronology of Sedimentary Iron Deposits and Crustal Evolution." Minerals 8, no. 12 (November 26, 2018): 547. http://dx.doi.org/10.3390/min8120547.

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The Chuanlinggou Formation is the lower formation of the Changchengian System, and hosts sedimentary iron deposits (marine oolitic ironstones) of the North China Craton (NCC). To determine the age of the iron deposits, and provide insight into the crustal growth of the craton, laser ablation multiple collector inductively coupled plasma mass spectrometry (LA-MC-ICP-MS)U-Pb and in situ Hf isotope analysis were performed on detrital zircon grains. Samples were taken from the roof sand-shale of the sedimentary iron deposits at Jiangjiazhai and Pangjiapbu. Overall, 186 detrital zircon grain U-Pb ages yield three major age populations, with weighted average ages of 2450 Ma, 1848 Ma, and 1765 Ma, respectively. Four younger ages from magmatic zircon grains were obtained, ranging from 1694 to 1657 Ma. Combined with observations from published studies, the results define the lower limit for the age of the Chuanlinggou Formation, and constrain the age of the sedimentary iron deposits (marine oolitic ironstone) close to 1650 Ma. The peak ages of 1848 Ma and 2450 Ma define the major collisional events of the NCC. The age of 1765 Ma can be linked to the age range of the widespread mafic dyke swarms that represent the rifting of the NCC within the Columbia supercontinent. Detrital zircon grains from the Chuanlinggou Formation form two obvious groups, with different εHf (t) values ranging from −1 to −8 and from +1 to +8, which correspond to the U-Pb age ranges of 1.7–1.9 Ga and 2.3–2.6 Ga, respectively. They have a similar two-stage Hf model age peak at 2.65–2.85 Ga, suggesting that the source rocks for each of these events were derived from the recycling of ancient crust. The source rocks of the older group of zircon grains might be derived from juvenile crust with a short reworking period. The critical crust–mantle differentiation event might happen during the period of 2.65–2.85 Ga, marking the most significant stage of the crustal growth in the NCC.

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12

Moëlo, Yves, Olivier Rouer, and Martine Bouhnik-Le Coz. "From diagenesis to hydrothermal recrystallization: polygenic Sr-rich fluorapatite from the oolitic ironstone of Saint-Aubin-des-Chateaux (Armorican Massif, France)." European Journal of Mineralogy 20, no. 2 (April 30, 2008): 205–16. http://dx.doi.org/10.1127/0935-1221/2008/0020-1792.

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13

Moëlo, Yves, Emmanuel Fritsch, Eric Gloaguen, and Olivier Rouer. "Polygenic chamosite from a hydrothermalized oolitic ironstone (Saint-Aubin-des-Châteaux, Armorican Massif, France): crystal chemistry, visible–near-infrared spectroscopy (red variety) and geochemical significance." Clay Minerals 55, no. 1 (March 2020): 83–95. http://dx.doi.org/10.1180/clm.2020.13.

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AbstractSeveral generations of chamosite, including a red variety, occur in the Ordovician hydrothermalized oolitic ironstone from Saint-Aubin-des-Châteaux (Armorican Massif, France). Their chemical re-examination indicates a low Mg content (0.925 < Fe/(Fe + Mg) < 0.954), but a significant variation in IVAl. Minor vanadium is present at up to 1.1 wt.% oxide. Variations in IVAl, the vanadium content and the colour of chamosite are related to the hydrothermal reworking of the ironstone. Taking into account other published data, the ideal composition of chamosite is (Fe5–xAl1+x)(Si3–xAl1+x)O10(OH)8, with 0.2 < x < 0.8 (0.2: equilibrium with quartz; 0.8: SiO2 deficit). The red chamosite (IIb polytype) has a mean composition of (Fe3.87Mg0.23Mn0.01□0.07Al1.74V0.07)(Si2.33Al1.67)O10(OH)8. This chamosite is strongly pleochroic, from pale yellow (E || (001)) to deep orange red (E ⊥ (001)). Visible–near-infrared absorbance spectra show a specific absorption band centred at ~550 nm for E ⊥ (001), due to a proposed new variety of Fe/V intervalence charge-transfer mechanism in the octahedral sheet, possibly Fe2+ – V4+ → Fe3+ – V3+. While the formation of green chamosite varieties is controlled by reducing conditions due to the presence of organic matter as a buffer, that of red chamosite would indicate locally a weak increase of fO2 related to oxidizing hydrothermal solutions.

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14

Hofer, John W., and John P. Szabo. "Port Bruce ice-flow directions based on heavy-mineral assemblages in tills from the south shore of Lake Erie in Ohio." Canadian Journal of Earth Sciences 30, no. 6 (June 1, 1993): 1236–41. http://dx.doi.org/10.1139/e93-105.

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The flow directions of ice lobes within the Erie basin may be deduced from heavy-mineral assemblages of the Hayesville, Hiram, and Ashtabula tills deposited during the Port Bruce Stade after the Erie Interstade. These tills have heavy-mineral assemblages dominated by purple garnet, green hornblende, and clinopyroxene. Oolitic hematite occurs in all tills, but is dominant in the Ashtabula Till. The probable source of hematite is the Furnaceville Ironstone Member of the Clinton Group which crops out south of Lake Ontario. Trilinear plots of purple garnet – red garnet – epidote suggest that the eastern Grenville Subprovince is the provenance of all three tills. Southwestward-flowing ice of an Ontario–Erie lobe deposited these tills in the Erie basin. The Huron–Erie lobe did not deposit tills along the south shore of Lake Erie after the Erie Interstade.

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15

VANHOUTEN, F. "Green marine clays. Oolitic ironstone facies, verdine facies, glaucony facies and celadonite-bearing facies—A comparative study." Earth-Science Reviews 27, no. 4 (June 1990): 396–97. http://dx.doi.org/10.1016/0012-8252(90)90077-9.

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16

Chamley, Hervé. "Green marine Clays. Oolitic ironstone facies, verdine facies, glaucony facies and celedonite-bearing rock facies — a comparative study." Marine Geology 91, no. 1-2 (January 1990): 156–57. http://dx.doi.org/10.1016/0025-3227(90)90140-f.

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17

Yoshida, Mitsuo, Ibrar H. Khan, and Mirza Naseer Ahmad. "Remanent magnetization of oolitic ironstone beds, Hazara area, Lesser Himalayan thrust zone, Northern Pakistan: Its acquisition, timing, and paleoenvironmental implications." Earth, Planets and Space 50, no. 9 (September 1998): 733–44. http://dx.doi.org/10.1186/bf03352166.

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18

Guerrak, Salah. "Metallogenesis of cratonic oolitic ironstone deposits in the Bled el Mass, Azzel Matti, Ahnet and Mouydir basins, Central Sahara, Algeria." Geologische Rundschau 76, no. 3 (October 1987): 903–22. http://dx.doi.org/10.1007/bf01821072.

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19

Yapp, Crayton J. "Oxygen isotopes in an oolitic ironstone and the determination of goethite δ18O values by selective dissolution of impurities: The 5M NaOH method." Geochimica et Cosmochimica Acta 55, no. 9 (September 1991): 2627–34. http://dx.doi.org/10.1016/0016-7037(91)90378-i.

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20

Moelo, Y., Y. Lulzac, O. Rouer, P. Palvadeau, E. Gloaguen, and P. Leone. "SCANDIUM MINERALOGY: PRETULITE WITH SCANDIAN ZIRCON AND XENOTIME-(Y) WITHIN AN APATITE-RICH OOLITIC IRONSTONE FROM SAINT-AUBIN-DES-CHATEAUX, ARMORICAN MASSIF, FRANCE." Canadian Mineralogist 40, no. 6 (December 1, 2002): 1657–73. http://dx.doi.org/10.2113/gscanmin.40.6.1657.

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21

BOULVAIN, Frédéric, Isabelle BELANGER, Dominique DELSATE, Danièle DOSQUET, Pierre GHYSEL, Pascal GODEFROIT, Martin LALOUX, Marc ROCHE, Hervé TEERLYNCK, and Jacques THOREZ. "New lithostratigraphical, sedimentological, mineralogical and palaeontological data on the Mesozoic of Belgian Lorraine: a progress report." Geologica Belgica 3, no. 1-2 (April 1, 2001): 3–33. http://dx.doi.org/10.20341/gb.2014.021.

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A multidisciplinary study of some extensively cored boreholes together with the new 1/25,000 geological mapping of Wallonia led us to propose a new lithostratigraphic canvas for Belgian Lorraine. This area is located on the N-E border of the Paris Basin, south of the Ardennes; the studied stratigraphic interval covers the Keuper to the Toarcian. Each of the new lithostratigraphic units is interpreted by macroscopic and microscopic sedimentological observations. Detailed palynological and claystratigraphical analyses were also performed, providing additional stratigraphical, palaeoecological and sedimentological data. The Habay Formation (conglomerates and red mudstones) is a fluvial unit, with immature channel conglomerates and paleosoils. The Attert Formation (dolomitic marls with gypsum and pseudomorphs) exhibits an evaporitic trend. The Mortinsart Formation (sands and marls) corresponds to a restricted marine unit, evolving towards an alluvial plain (Levallois Member). The second cycle begins with the Jamoigne Formation (bioturbated marls and limestones), a marine subtidal restricted unit, evolving towards a more sandy series (Metzert Member). The base of the third cycle corresponds to the rest of the Luxembourg Formation, composed by a superposition of sand waves. The Ethe Formation (laminar mudstones and marls) marks a deepening of the basin and the outset of marine dysaerobic conditions. The Aubange Formation (bioturbated marls with sandstones and limestones) is characterized by the reappearance of a normal benthic fauna. The Grandcourt Formation (laminar mudstones and marls) marks a return to open marine dysaerobic conditions. The Mont-Saint-Martin Formation (marls, sandy marls and oolitic ironstone) is a highly regressive unit, while the Longwy Formation (limestones) marks the initiation of a carbonate platform.

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22

Gloaguen, Eric, Yannick Branquet, Philippe Boulvais, Yves Moëlo, Jean-Jacques Chauvel, Pierre-Jacques Chiappero, and Eric Marcoux. "Palaeozoic oolitic ironstone of the French Armorican Massif: a chemical and structural trap for orogenic base metal–As–Sb–Au mineralisation during Hercynian strike-slip deformation." Mineralium Deposita 42, no. 4 (January 30, 2007): 399–422. http://dx.doi.org/10.1007/s00126-006-0120-4.

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23

Schieber, J. "Anomalous iron distribution in shales as a manifestation of ?non-clastic iron? supply to sedimentary basins: relevance for pyritic shales, base-metal mineralization, and oolitic ironstone deposits." Mineralium Deposita 30, no. 3-4 (June 1995): 294–302. http://dx.doi.org/10.1007/bf00196365.

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24

Van Houten, Franklyn Bosworth. "Interpreting Silurian Clinton Oolitic Ironstones – 1850–1975." Journal of Geological Education 39, no. 1 (January 1991): 19–22. http://dx.doi.org/10.5408/0022-1368-39.1.19.

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25

Van Houten, F. B. "Search for Milankovitch patterns among oolitic ironstones." Paleoceanography 1, no. 4 (December 1986): 459–66. http://dx.doi.org/10.1029/pa001i004p00459.

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26

Van Houten, Franklyn B. "Oolitic ironstones and contrasting Ordovician and Jurassic paleogeography." Geology 13, no. 10 (1985): 722. http://dx.doi.org/10.1130/0091-7613(1985)13<722:oiacoa>2.0.co;2.

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27

Van Houten, F. B., and Hong-Fei Hou. "Stratigraphic and palaeogeographic distribution of Palaeozoic oolitic ironstones." Geological Society, London, Memoirs 12, no. 1 (1990): 87–93. http://dx.doi.org/10.1144/gsl.mem.1990.012.01.07.

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28

Van Houten, Franklyn B. "Palaeozoic oolitic ironstones on the North American Craton." Palaeogeography, Palaeoclimatology, Palaeoecology 80, no. 3-4 (November 1990): 245–54. http://dx.doi.org/10.1016/0031-0182(90)90135-t.

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29

Yapp, Crayton J. "Paleoenvironmental interpretations of oxygen isotope ratios in oolitic ironstones." Geochimica et Cosmochimica Acta 62, no. 14 (July 1998): 2409–20. http://dx.doi.org/10.1016/s0016-7037(98)00164-1.

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30

Van Houten, F. B., and M. A. Arthur. "Temporal patterns among Phanerozoic oolitic ironstones and oceanic anoxia." Geological Society, London, Special Publications 46, no. 1 (1989): 33–49. http://dx.doi.org/10.1144/gsl.sp.1989.046.01.06.

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31

Guerrak, Salah. "Paleozoic oolitic ironstones of the Algerian Sahara: a review." Journal of African Earth Sciences (1983) 6, no. 1 (January 1987): 1–8. http://dx.doi.org/10.1016/0899-5362(87)90102-3.

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32

Trythall, R. J. B. "The mid-Ordovician oolitic ironstones of North Wales: a field guide." Geological Society, London, Special Publications 46, no. 1 (1989): 213–20. http://dx.doi.org/10.1144/gsl.sp.1989.046.01.18.

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33

Schwarz, T., and K. Germann. "Ferricretes as a source of continental oolitic ironstones in northern Sudan." Chemical Geology 107, no. 3-4 (July 1993): 259–65. http://dx.doi.org/10.1016/0009-2541(93)90187-n.

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34

Teyssen, T. "A depositional model for the Liassic Minette ironstones (Luxemburg and France), in comparison with other Phanerozoic oolitic ironstones." Geological Society, London, Special Publications 46, no. 1 (1989): 79–92. http://dx.doi.org/10.1144/gsl.sp.1989.046.01.09.

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35

Boucot, A. J., and Jane Gray. "Comment and Reply on “Oolitic ironstones and contrasting Ordovician and Jurassic paleogeography”." Geology 14, no. 7 (1986): 634. http://dx.doi.org/10.1130/0091-7613(1986)14<634b:carooi>2.0.co;2.

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36

Van Houten, F. B. "Comment and Reply on “Oolitic ironstones and contrasting Ordovician and Jurassic paleogeography”." Geology 14, no. 7 (1986): 635. http://dx.doi.org/10.1130/0091-7613(1986)14<635:carooi>2.0.co;2.

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37

Curtis, C. D. "G.S. Odin (Editor) Green Marine Clays. Oolitic Ironstone Facies, Verdine Facies, Glaucony Facies and Celadonite-Bearing Facies — A Comparative Study. (Developments in Sedimentology, 45). Elsevier Science Publishers, Amsterdam, 1988. 445 pp. Price US $110.50/Dfl.210.00. QE389.625.055 1988 552'.5 88-31042. ISBN: 0444-87120-9." Clay Minerals 24, no. 3 (September 1989): 565–66. http://dx.doi.org/10.1180/claymin.1989.024.3.11.

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38

Bhattacharyya, D. P. "Concentrated and lean oolites: examples from the Nubia Formation at Aswan, Egypt, and significance of the oolite types in ironstone genesis." Geological Society, London, Special Publications 46, no. 1 (1989): 93–103. http://dx.doi.org/10.1144/gsl.sp.1989.046.01.10.

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Franceschelli, M., M. Puxeddu, and M. Carta. "Mineralogy and geochemistry of Late Ordovician phosphate-bearing oolitic ironstones from NW Sardinia, Italy." Mineralogy and Petrology 69, no. 3-4 (June 26, 2000): 267–93. http://dx.doi.org/10.1007/s007100070024.

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Guerrak, S. "Time and space distribution of Palaeozoic oolitic ironstones in the Tindouf Basin, Algerian Sahara." Geological Society, London, Special Publications 46, no. 1 (1989): 197–212. http://dx.doi.org/10.1144/gsl.sp.1989.046.01.17.

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Evans, Graham. "Some comments upon: Palaeozoic oolitic ironstones on the North American Craton (Van Houten, 1990)." Palaeogeography, Palaeoclimatology, Palaeoecology 96, no. 3-4 (October 1992): 319–20. http://dx.doi.org/10.1016/0031-0182(92)90108-h.

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Novoselov, K. A., E. V. Belogub, V. A. Kotlyarov, K. A. Filippova, and S. A. Sadykov. "Mineralogical and Geochemical Features of Oolitic Ironstones from the Sinara–Techa Deposit, Kurgan District, Russia." Geology of Ore Deposits 60, no. 3 (May 2018): 265–76. http://dx.doi.org/10.1134/s1075701518030066.

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Hodych, J. P., R. R. Pätzold, and K. L. Buchan. "Chemical remanent magnetization due to deep-burial diagenesis in oolitic hematite-bearing ironstones of Alabama." Physics of the Earth and Planetary Interiors 37, no. 4 (March 1985): 261–84. http://dx.doi.org/10.1016/0031-9201(85)90013-5.

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Galmed, Mahmoud A., Bassam A. Amarah, Habes A. Ghrefat, and Abdullah A. Al-Zahrani. "Petrology of oolitic ironstones of Ashumaysi Formation of Wadi Fatima, western Arabian Shield, Saudi Arabia." Journal of King Saud University - Science 33, no. 1 (January 2021): 101266. http://dx.doi.org/10.1016/j.jksus.2020.101266.

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Dreesen, Roland. "Oolitic ironstones as event-stratigraphical marker beds within the Upper Devonian of the Ardenno-Rhenish Massif." Geological Society, London, Special Publications 46, no. 1 (1989): 65–78. http://dx.doi.org/10.1144/gsl.sp.1989.046.01.08.

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Hughes, C. R. "The application of analytical transmission electron microscopy to the study of oolitic ironstones: a preliminary study." Geological Society, London, Special Publications 46, no. 1 (1989): 121–31. http://dx.doi.org/10.1144/gsl.sp.1989.046.01.12.

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Garnit, Hechmi, and Salah Bouhlel. "Petrography, mineralogy and geochemistry of the Late Eocene oolitic ironstones of the Jebel Ank, Southern Tunisian Atlas." Ore Geology Reviews 84 (April 2017): 134–53. http://dx.doi.org/10.1016/j.oregeorev.2016.12.026.

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Oggiano, Giacomo, and Paola Mameli. "Diamictite and oolitic ironstones, a sedimentary association at Ordovician–Silurian transition in the north Gondwana margin: New evidence from the inner nappe of Sardinia Variscides (Italy)." Gondwana Research 9, no. 4 (June 2006): 500–511. http://dx.doi.org/10.1016/j.gr.2005.11.009.

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Hillier, S. "Pore-lining chlorites in siliciclastic reservoir sandstones: electron microprobe, SEM and XRD data, and implications for their origin." Clay Minerals 29, no. 4 (October 1994): 665–79. http://dx.doi.org/10.1180/claymin.1994.029.4.20.

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Abstract:

AbstractPore-lining chlorites are often responsible for the preservation of porosity in deeply buried sandstones because they inhibit the formation of quartz overgrowths, but little is understood about when and how they form. Chemical analyses and XRD data indicate that there are at least two common types: Fe-rich, and Mg-rich. The Fe-rich examples occur as individual euhedral crystals, are invariably interstratified with 7 Å layers (probably berthierine) and form as the Ib β = 90° polytype at low temperatures. With increasing temperature, their chemistry changes, 7 Å layers are lost, crystal size increases, and eventually they transform to the high temperature IIb β = 97° polytype. The Mg-rich examples occur as boxwork arrangements of crystals, are not interstratified with 7 Å layers and are exclusively the IIb β = 97° polytype. The Fe-rich examples occur most frequently in sandstones that were deposited at the transition between marine and non-marine environments and the presence of Fe-rich oolites in many samples suggests a link to the ironstone facies. They probably formed originally at surface or near-surface conditions as a 7 Å mineral, such as berthierine or even odinite, in a fresh water/marine water mixing zone in tropical regions. The Mg-rich varieties tend to be found in aeolian or sabkha sandstones in close association with evaporites. They are probably replacements of Mg-rich smectites via the intermediate mineral corrensite. Precursor Mg-rich smectites formed originally from evaporite brines at near-surface conditions; chlorite itself was not formed until temperatures were high enough to crystallize the IIb β = 97° polytype.

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Jeans, C. V. "Clay mineralogy of the Jurassic strata of the British Isles." Clay Minerals 41, no. 1 (March 2006): 187–307. http://dx.doi.org/10.1180/0009855064110198.

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AbstractThe nature and origin of the clay mineralogy of the Jurassic strata of the British Isles are described and discussed within their lithological and biostratigraphical framework using published and unpublished sources as well as 1800 new clay mineral analyses. Regional clay mineral variation is described systematically for the following formations or groups:England and Wales(i)Hettangian-Toarcian strata (Lias Group): Redcar Mudstone Fm.; Staithes Sandstone Fm.; Cleveland Ironstone Fm.; Whitby Mudstone Fm.; Scunthorpe Mudstone Fm.; Blue Lias Fm.; Charmouth Mudstone Fm.; Marlstone Rock Fm.; Dyrham Fm.; Beacon Limestone Fm.; Bridport Sand Fm.(ii)Aalenian-Bajocian (Inferior Oolite Group): Dogger Fm.; Saltwick Fm.; Eller Beck Fm.; Cloughton Fm.; Scarborough Fm.; Scalby Fm. (in part); Northampton Sand Fm.; Grantham Fm.; Lincolnshire Limestone Fm.; Rutland Fm. (in part); Inferior Oolite of southern England.(iii)Bathonian (Great Oolite Group): Scalby Fm. (in part); Rutland Fm. (in part); Blisworth Limestone Fm.; Great Oolite Group of southern England; Forest Marble Fm.; Cornbrash Fm. (in part).(iv)Callovian-Oxfordian: Cornbrash Fm. (in part); Kellaways Fm.; Oxford Clay Fm.; Corallian Beds and West Walton Beds; Ampthill Clay Fm.(v)Kimmeridgian-Tithonian: Kimmeridge Clay Fm.; Portland Sandstone Fm.; Portland Limestone Fm.; Lulworth Fm.; Spilsby Sandstone Fm. (in part). Scotland(vi)Hettangian-Toarcian: Broadfoot Beds, Dunrobin Bay Fm. Aalenian-Portlandian: Great Estuarine Group (Dunkulm, Kilmaluag and Studiburgh Fm.s); Staffin Shale Fm.; Brora Coal Fm.; Brora Argillaceous Fm.; Balintore Fm.; Helmsdale Boulder Beds (Kimmeridge Clay Fm.).Dominating the Jurassic successions are the great marine mudstone formations — the Lias Group, Oxford Clay, Ampthill Clay and Kimmeridge Clay. These are typically characterized by a detrital clay mineral assemblage of mica, kaolin and poorly defined mixed-layer smectite-mica-vermiculite minerals with traces of chlorite. Detailed evidence suggests that this assemblage is derived ultimately from weathered Palaeozoic sediments and metasediments either directly or by being recycled from earlier Mesozoic sediments. A potassium-bearing clay is a persistent component and formed at approximately the same time as the deposition of the host sediment, either in coeval soils or during very early diagenesis.At three periods during the deposition of the Jurassic (Bajocian-Bathonian, Oxfordian and late Kimmeridgian-Tithonian), the detrital clay assemblage was completely or partially replaced by authigenic clay mineral assemblages rich in kaolin, berthierine, glauconite or smectite minerals. Associated with these changes are major changes in the lithofacies, with the incoming of non-marine and proximal marine strata. The authigenic clay assemblages rich in kaolin and berthierine are generally restricted to the non-marine and very proximal marine beds, those rich in glauconite or smectite are typical of the marine lithofacies. Clay mineral assemblages containing vermiculite and mixed-layer vermiculite-chlorite sometimes occur in the non-marine and proximal marine facies. The causes of these major changes in lithofacies and clay mineralogy are discussed, and present evidence favours an important volcanogenic influence and not climatic control. It is suggested that the Bajocian-Bathonian, Oxfordian and Late Kimmeridgian-Tithonian were periods of enhanced volcanic activity, with centres probably located in the North Sea and linked to regional tectonic changes which caused major modifications of the palaeogeography of the British Isles. The most important of these changes was the development of the central North Sea Rift Dome during the Bajocian and Bathonian. Volcanic ash was widespread in both the non-marine and marine environments and its argillization under different conditions provided the wide range of authigenic clay mineral assemblages.Metre-scale clay mineral cyclicity is widespread in most of the Jurassic mudstone formations that have been examined in sufficient detail. The cyclicity is defined by systematic variations in the mica/ collapsible minerals (mixed-layer smectite-mica-vermiculite) ratio. This variation is unrelated to changes in lithology and its possible origins are discussed in detail using data from the Kimmeridge Clay provided by Reading University's contribution to the Rapid Global Geological Events (RGGE) Project.

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