Formation and evolution of the tertiary carbonate reefs in the Madura Strait Basin of Indonesia
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Carbonate platform
Paleogene
Neogene
Middle Miocene disruption
Association Round Table 555 high/low or shallow/deep.Special facies types include stromatoporoid and evaporite, both supratidal and deep.Facies and fabrics vary considerably throughout the sequence, both interformationally and intraformationally.Mudstones, wackestones, and packstones are most common although grainstones and boundstones also occur.Within textural constraints, each fabric contains their respective amounts of skeletal and nonskeletal allochems.Because of frequent and sharp facies changes, it is important to discriminate among different facies that superficially have similar fabrics.Examples are deep/shallow evaporites, or supratidal/subtidal oolites and pisolites.Peloidal wackestones/grainstones, skeletal wackestones/packstones, and mottled mudstones are the prevalent fabric types.Significant sedimentary structures include burrows, flat pebble interclasts, desiccation cracks, bird's-eye structures, and collapse breccias.Porosity types common to all, except for the Ashern and Bakken, are intercrystal, interparticle, moldic, vuggy, and breccia.Significant porosity in the Ashern and Bakken formations is from fractures.
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Abstract Sequence stratigraphic studies of the Triassic through Paleogene carbonate successions of platform, slope and basin in western Sicily (Palermo and Termini Imerese Mountains) have identified a sedimentary cyclicity mostly caused by relative oscillations of sea level. The stratigraphic successions of the Imerese and Panormide palaeogeographic domains of the southern Tethyan continental margin were studied with physical-stratigraphy and facies analysis to reconstruct the sedimentary evolution of this platform-to-basin system. The Imerese Basin is characterized by a carbonate and siliceous-calcareous succession, 1200–1400m thick, Late Triassic to Eocene in age. The strata display a typical example of a carbonate platform margin, characterized by resedimented facies with progradational stacking patterns. The Panormide Carbonate Platform is characterized by a carbonate succession, 1000–1200 m thick, Late Triassic to Late Eocene, mostly consisting of shallow-water facies with periodic subaerial exposure. The cyclic arrangement has been obtained by the study of the stratigraphic signatures (unconformities, facies sequences, erosional surfaces and stratal geometries) found in the slope successions. The recognized pattern has been compared with coeval facies of the shelf. This correlation provided evidence of sedimentary evolution, influenced by progradation and backstepping of the shelf deposits. The stratigraphic architecture of the platform-to-basin system is characterized by four major transgressive/regressive cycles during the late Triassic to late Eocene. These cycles, framed in a chronostratigraphic chart, allows the correlation of the investigated shelf-to-basin system with the geological evolution of the African continental margin during the Mesozoic, showing tectono-eustatic cycles. The first cycle, encompassing the late Triassic to early Jurassic, appears to be related to the late syn-rift stage of the continental margin evolution. The following three cycles, spanning from the Jurassic to Eocene, can be related to the post-rift evolution and to thermal subsidence changes.
Carbonate platform
Sequence Stratigraphy
Paleogene
Progradation
Passive margin
Subaerial
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Carbonate platform
Paleogene
Neogene
Middle Miocene disruption
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Large allochthonous blocks up to several tens of meters across are adjacent to reef-fringed isolated carbonate buildups and platforms in the Canning basin of Western Australia and in western Canada. Distinctive criteria such as geopetal fabrics, stratification, lack of facies changes within the blocks, enclosure within basin sediments, and occurrence several kilometers from the nearest buildups indicate the blocks and breccias are allochthonous, although often misinterpreted as in-place bioherms. Framebuilding reef-core facies is the predominant block type, hence most were derived from the margins of carbonate buildups. In Australia they occur as isolated blocks and contain abundant stromatoporoids and Renalcis, interpreted as reef-core facies, increasing in number toward the carbonate platforms. Some of the blocks have disrupted the underlying basin sediments. A few debris beds of finer breccia beds (fragments floating in carbonate mud matrix) wedge out laterally and presumably formed shallow channels perpendicular to the carbonate platforms. In Canada isolated blocks are unknown. Locally megabreccia beds flank some of the buildups and extend several kilometers into the basin. More common are finer breccias in beds and channels. Both types consist of disoriented, angular fragments of reef-margin stromatoporoid and coral facies, external lagoon facies, and basin mud in a pervasive dark, interstitial dolomitized micrite of basin origin. The isolated blocks represent material tumbled into the adjacent basin, apparently during times of active slumping of the platform margins. The Canadian deposits apparently were transported by submarine debris flows analogous to subaerial mudflows from buildup margin environments when relief and slope at the margins were greatest. End_of_Article - Last_Page 641------------
Devonian
Debris flow
Submarine landslide
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Kaybob is one of a group of geologic reefs which underlie west-central Alberta and which comprise the Upper Devonian Swan Hills Formation of the Beaverhill Lake Group. Kaybob is a flat north-south elongate lens, 250 ft thick, 11 mi long, and 3 mi wide, built on the Slave Point Formation, a widespread platform carbonate. Detailed core study of sedimentary structure, texture, and constituents reveals that the carbonate sediments composing the can be grouped into 3 environmentally controlled facies groups: reef-slope, reef-margin, and shelf-lagoon facies. The reef-slope facies is a stromatoporoid-crinoid-brachiopod grainstone. The marginal deposits consist of a groundmass of massive stromatoporoid grainstone containing varied concentrations of different stromatoporoid growth forms (ranging from slender branching to large massive heads). The interior facies includes several rock types arranged in repeated vertical sequences. A basal unit of massive wackestone is overlain by combinations of massive, thin-bedded, and laminated mudstones, mudclast grainstones, and amphiporid carbonate conglomerate. Submarine and subaerial scoured surfaces are present within the upper units. The outer slope sediments intertongue with contemporaneous open-marine deposits seaward and with the reef-marginal facies on the inner side of the reef. This pattern changes laterally in vertical section, as the thickness of the changes from place to place. The upper half of the shows a marked westward displacement. Position of the various facies within the geologic mass, and comparison with Holocene carbonate sediments from several Caribbean localities, together provide a paleoenvironmental interpretation. The interior facies includes most of the sediment types which have been described from recent shallow shelf-lagoon environments. Sequential arrangements are the same and result from similar processes. The marginal realm includes many facies comparable with those observed in Holocene reef tracts, ranging from scattered coral growth on a sand bottom to coral constructed buttresses of ecologic reefs. Circumferential variations in geologic development, the westward displacement of the upper part, and a thick pile of open-marine deposits on the southwest are attributed to prevailing nor h winds during the Devonian. Tectonic control is exhibited at 4 levels. 1. The interior shelf-lagoon sequences are initiated by small-scale pulses of subsidence, perhaps complicated by eustatic sea-level changes. 2. Larger scale subsidence variations account for the thickening and thinning of the geologic body as a whole. 3. An orthogonal pattern of sharp elongate folds trending NE-SW and NW-SE is expressed clearly at the base of the reef. The folds are confined to the area of reefing, where they controlled initiation by forming mud mounds during upper Slave Point deposition. The pattern may reflect Slave Point block faulting. 4. This and others in the region, together with their associated carbonate-shelf deposits, fit into a well-expressed orthogonal tectonic pattern controlled by larger scale ba ement features. The basement features include a family of NE-SW-trending, relatively stable arches revolving about a NW-SE-trending major arch, the West Alberta ridge. They form part of the system of stable arches that provides the tectonic framework of the continent. End_of_Article - Last_Page 854------------
Devonian
Sedimentation
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Calcimicrobialites, which could be correlated to the layer 27 in Meishan section according to the Hindeodus parvus, occur abruptly on the end-Permian mass extinction boundary in South China. Microbialites mainly distribute on the top of reef facies or shallow carbonate platforms, thinning into deep facies. All the microbialites discovered are composed of micrite and coarse crystal digitate carbonate or patch carbonate. Microfossils usually dominate in the microbialites, and small gastropods, bivalves and ostracodes can also be found. This fossil assemblage represents a simple but particular remanent biota after the end-Permian mass extinction on the top of reefs or shallow carbonate platforms.Abrupt occurrence of microbialites above the mass extinction boundary is the ecological response to the end-Permian global event in reef or shallow carbonate facies. Many studies have been done on the Permian-Triassic boundary and event in deep water facies sections or middle to lower shelf facies sections. However, the calcimicrobialites in South China are mainly located above reef facies or shallow carbonate platform facies. It will surely be helpful for people to know more about the different responses in different depths of ancient marine environment during the transition between Permian and Triassic by the study of petrology,palaeontology and palaeoecology of the calcimicrobialites.
Carbonate platform
Micrite
Permian–Triassic extinction event
Extinction (optical mineralogy)
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Map 1. Late Eocene (Priabonian-Beloglinian) -- Map 2. Early Oligocene (Early Rupelian, Early Kiscellian - Pschekhian) -- Map 3. Late Oligocene (Chattian - Egerian - Kalmykian) -- Map 4. Early Miocene (Burdigalian, Eggenburgian, Sakaraulian) -- Map 5. Early Middle Miocene (Langhian, Early Badenian, Chokrakian) -- Map 6. Mid Middle Miocene (Middle Serrvallian, Late Badenian, Konkian) -- Map 7. Late Middle Miocene (Late Serrvallian, Sarmatian s.s., Middle Sarmatian s.l.) -- Map 8. Mid Late Miocene (Late Tortonian - Early Messinian - Early Maeotian - Late Pannonian) -- Map 9. Latest Miocene (Late Messinian, Early Pontian - Late Pannonian) -- Map. 10. Middle Late Pliocene (Piacentian - Gelasian, Late Romanian - Akchagilian) -- [chart] Stratigraphic scheme of the Late Paleogene - Neogene Paratethys and mapped intervals.
Neogene
Paleogene
Middle Miocene disruption
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Abstract The Hagen-Balve Reef is one of the largest Devonian carbonate complexes in the Rhenish Massif exposed in many former or active, economically significant quarries, especially in the Hönne Valley region at its eastern end. The timing and patterns of reef drowning, final extinction, and the middle Frasnian to middle Famennian post-reefal facies history, including details of the global Kellwasser Crisis, were studied based on two boreholes (HON_1101 and B102) and one outcrop at the Beul near Eisborn. More than 100 conodont samples provided a fine biostratigraphic framework and included new forms left in open nomenclature. The ca. upper 80 m of the new Asbeck Member of the Hagen-Balve Formation consists of relatively monotonous lagoonal successions assigned to four microfacies types. The local diversity of reef builders, mostly stromatoporoids, is low. Fenestral microbialites indicate very shallow and rather hostile back-reef settings. Near the Middle/Upper Devonian boundary, the eustatic pulses of the global Frasnes Events led to a significant backstepping of the reef margin, with reef core/outer slope facies overlying lagoonal facies. This flooding drastically reduced the carbonate accumulation rate and enabled the invasion of drowned back-reef areas by open-water organisms, such as polygnathid conodonts. Within this Eisborn Member, five microfacies types and numerous subtypes are distinguished including low-diversity “coral gardens” and a final, top lower Frasnian parabiostrome dominated by tabulate and colonial rugose corals. There was no cap stage (“Iberg Facies”). Two phases of the Basal Frasnes Event are marked by dark, organic rich limestones with subordinate reef builders. Based on conodont fauna from overlying nodular limestones of the new, (hemi-)pelagic Beul Formation, the final Hönne Valley reef extinction was caused by the eustatic Middlesex Event at the lower/middle Frasnian boundary. Within the Beul Formation, eight subphotic submarine rise microfacies types are distinguished. After a lower middle Frasnian phase of extreme condensation, rich conodont faunas enable the recognition of most upper Frasnian to middle Famennian zones. The global semichatovae Event led to a regionally unique intercalation by four phases of organic-rich, laminated black shales and intervening thin limestones in core HON_1101. The Lower Kellwasser Event is represented in HON_1101 by atypical, moderately C org -rich, recrystallized, peloidal ostracod-mollusk pack-grainstones. The Upper Kellwasser level begins with an ostracod bloom, followed either by recrystallized mollusk wacke-packstones (HON_1101) or laminated, argillaceous mudstones (B102). The first indicates a rarely documented shallow subphotic, better oxygenated setting than typical Upper Kellwasser facies. As elsewhere, the top-Frasnian conodont extinction was severe. The lower/middle Famennian carbonate microfacies of the Beul Formation is relatively monotonous and typical for an oxic, pelagic submarine rise. The youngest recorded nodular limestones fall in the Palmatolepis marginifera utahensis Zone. Regionally uniform lydites of the Hardt Formation show that the local palaeotopography was levelled before the base of the Viséan. The Hönne Valley case study and comparisons with western parts of the Hagen-Balve Reef and other Rhenish reefs underline the significance of Givetian to middle Frasnian eustatic and anoxic events as causes for reef extinctions.
Devonian
Massif
Late Devonian extinction
Conodont
Carbonate platform
Outcrop
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Palaeogeography
Siliciclastic
Marine transgression
Marl
Sequence (biology)
Shoal
Sequence Stratigraphy
Transgressive
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The Paleogene rocks of the Magdalena Valley and the Cordillera Oriental of Colombia represent the synorogenic sedimentary fill of the ancestral Andean foreland basin. Although detailed correlation of the Paleogene is hampered by poor biostratigraphic control, recent field studies document variations between the Upper and Middle Magdalena Valleys in vertical facies succession and paleocurrent direction, suggesting independent depositional systems separated by the Girardot fold belt. In the northern Upper Magdalena Valley, the Paleogene Gualanday Group lies unconformably to paraconformably on marine Upper Cretaceous and Paleocene rocks. Lower and upperconglomeratic units in the Gualanday Group grade eastward into finer grained fluvial sandstones in the western Cordillera Oriental. North of the Girardot belt, conglomerates occur only in the lower part of the Paleogene and grade northeastward into fluvial sandstones. These unconformably overlie rocks as old as Neocomian in a series of en echelon structures on the west flank of the Cordillera Oriental. The structural trends and thickness of the Cretaceous here suggest inversion of the marine depocenter prior to Paleogene deposition. Previous reports of early Paleogene uplift of the Quetame Massif south of Bogota indicate that similar processes acted elsewhere in the Cordillera Oriental. These studies show that the Cordillera Oriental underwentmore » at least one phase of uplift prior to the main inversion in the Neogene.« less
Paleogene
Massif
Paleocurrent
Neogene
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