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Статті в журналах з теми "Stratigraphic Proterozoic":

1
Halverson, Galen P., Susannah M. Porter, and Timothy M. Gibson. "Dating the late Proterozoic stratigraphic record." Emerging Topics in Life Sciences 2, no. 2 (July 2018): 137–47. http://dx.doi.org/10.1042/etls20170167.
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The Tonian and Cryogenian periods (ca. 1000–635.5 Ma) witnessed important biological and climatic events, including diversification of eukaryotes, the rise of algae as primary producers, the origin of Metazoa, and a pair of Snowball Earth glaciations. The Tonian and Cryogenian will also be the next periods in the geological time scale to be formally defined. Time-calibrating this interval is essential for properly ordering and interpreting these events and establishing and testing hypotheses for paleoenvironmental change. Here, we briefly review the methods by which the Proterozoic time scale is dated and provide an up-to-date compilation of age constraints on key fossil first and last appearances, geological events, and horizons during the Tonian and Cryogenian periods. We also develop a new age model for a ca. 819–740 Ma composite section in Svalbard, which is unusually complete and contains a rich Tonian fossil archive. This model provides useful preliminary age estimates for the Tonian succession in Svalbard and distinct carbon isotope anomalies that can be globally correlated and used as an indirect dating tool.
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Wu, He Yuan, and Bin Hao. "Third-Order Sequence Division of Yunmengshan and Baicaoping Formation of Proterozoic in Yuxi District of China: an Example from Xiatang Profile in Lushan." Advanced Materials Research 998-999 (July 2014): 1492–97. http://dx.doi.org/10.4028/www.scientific.net/amr.998-999.1492.
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There are controversies on the Proterozoic stratigraphic genesis, division, correlation and palaeogeographical evolution of western Henan in China. Based on the basic description of sedimentary facies, Yunmengshan and Baicaoping formation of Proterozoic typical section in western Henan is divided into 4 third-order sequences. Sequence stratigraphy framework which reflects sedimentary and overlap is established with basis of two kinds of facies-change surface and two kinds of diachrononism in stratigraphical records. Although chronostratigraphic belonging of Precambrian strata is controversial and Precambrian sequential stratigraphic study is tremendously challenging, the establishment of sequence stratigraphy framework of proterozoic Yunmengshan and Baicaoping formation in western Henan provides actual data to reshape palaeogeographic pattern of Palaeoproterozoic North China craton. What is more, it becomes a typical example of characteristics and exploration of stratigraphic accumulation under the background of tidal action.
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Martins-Neto, Marcelo A. "Sequence stratigraphic framework of Proterozoic successions in eastern Brazil." Marine and Petroleum Geology 26, no. 2 (February 2009): 163–76. http://dx.doi.org/10.1016/j.marpetgeo.2007.10.001.
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Ming, Yan, Liu Yingjun, and Ma Dongsheng. "Stratigraphic geochemistry of Upper-Middle Proterozoic Suberathem in northern Guangxi, China." Chinese Journal of Geochemistry 14, no. 3 (July 1995): 231–42. http://dx.doi.org/10.1007/bf02842046.
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Roscoe, S. M., and K. D. Card. "The reappearance of the Huronian in Wyoming: rifting and drifting of ancient continents." Canadian Journal of Earth Sciences 30, no. 12 (December 1993): 2475–80. http://dx.doi.org/10.1139/e93-214.
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Striking stratigraphic and sedimentological similarities between the Early Proterozoic Huronian Supergroup of the Canadian Shield and the Snowy Pass Supergroup of Wyoming suggest that they were deposited in a single, broad, epicratonic basin developed atop a large Archean continent that included the Superior and Wyoming geological provinces. Breakup of the continent after the 2.2 Ga intrusion of widespread gabbro sheets and dykes resulted in the separation of the Archean Superior and Wyoming cratons and their Early Proterozoic covers. These crustal fragments were subsequently reassembled during Early Proterozoic (~1.85 Ga) orogenesis, the end result being the present 2000 km separation of the Huronian and Snowy Pass supergroups and their Archean basements.
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Ansdell, Kevin M., T. Kurtis Kyser, Mel R. Stauffer, and Garth Edwards. "Age and source of detrital zircons from the Missi Formation: a Proterozoic molasse deposit, Trans-Hudson Orogen, Canada." Canadian Journal of Earth Sciences 29, no. 12 (December 1992): 2583–94. http://dx.doi.org/10.1139/e92-205.
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The Missi Formation in the Flin Flon Basin forms part of a discontinuous series of molasse-type sediments found throughout the Early Proterozoic Trans-Hudson Orogen in northern Saskatchewan and Manitoba. The Flin Flon Basin contains a sequence of proximal-fan to braided-stream fluvial conglomerates and sandstones, which unconformably overlie subaerially weathered Amisk Group volcanic rocks. Stratigraphic way-up indicators have been preserved, even though these rocks have undergone greenschist-facies metamorphism and polyphase deformation. The sedimentary rocks are crosscut by intrusive rocks, which provide a minimum age of sedimentation of 1840 ± 7 Ma.Detrital zircons from each of the six stratigraphic subdivisions of the Flin Flon Basin were analyzed using the single-zircon Pb-evaporation technique. Euhedral to slightly rounded zircons dominate each sample, and these zircons give ages of between about 1854 and 1950 Ma. The Missi sediments were thus deposited between 1840 and 1854 Ma. Possible sources for the detrital zircons are Amisk Group felsic volcanic rocks and post-Amisk granitoid rocks and orthogneisses in adjacent domains within the Trans-Hudson Orogen. However, the immature character of the sedimentary rocks, the composition of clasts, the euhedral character of many of the zircons, and the range in ages suggest that most were likely derived from Amisk Group and granitoid rocks in the western Flin Flon Domain. Rounded zircons are uncommon but provide evidence for the reworking of older Proterozoic sedimentary rocks, or a distant Archean or Early Proterozoic granitoid terrane.
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Mitchelmore, Marlene Dredge, and Frederick A. Cook. "Inversion of the Proterozoic Wernecke basin during tectonic development of the Racklan Orogen, northwest Canada." Canadian Journal of Earth Sciences 31, no. 3 (March 1994): 447–57. http://dx.doi.org/10.1139/e94-041.
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New deep seismic reflection data coupled with regional stratigraphic correlations, drill-hole information, and potential field data are interpreted to provide images of Middle Proterozoic Wernecke Supergroup (meta-)sedimentary layers that were uplifted during tectonic development of the ca. 0.9–1.3 Ga Racklan Orogen in Canada's western Northwest Territories. The reflection data are located at the eastern front of the Mackenzie Mountains portion of the Canadian Cordillera and on the western flank of the Fort Simpson structural trend that is a prominent Proterozoic structure in the subsurface throughout the region. Along three parallel profiles, layers that are correlated with thick Wernecke Supergroup sedimentary rocks produce prominent reflections between about 3.0 and 9.0 s (about 7.5 and 23 km) that were arched prior to deposition of younger Proterozoic (probably Mackenzie Mountains Supergroup) and Phanerozoic sedimentary rocks. The strata are considered to be Wernecke basin sedimentary rocks that were uplifted during deformation associated with the development of the Racklan Orogen.
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Sevigny, James H., Frederick A. Cook, and Elizabeth A. Clark. "Geochemical signature and seismic stratigraphic setting of Coppermine basalts drilled beneath the Anderson Plains in northwest Canada." Canadian Journal of Earth Sciences 28, no. 2 (February 1991): 184–94. http://dx.doi.org/10.1139/e91-018.
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Basalts drilled in the Petro-Canada – Canterra Tweed Lake M-47 well in the Anderson Plains of northwestern Canada have geochemical characteristics, including of major, trace, and rare earth elements, that are similar to those of the most enriched Coppermine lavas but significantly different from those of the younger Proterozoic volcanics, such as the Natkusiak basalts. This result provides a geological tie and timing constraint for structures observed on seismic reflection data in this area. Correlation of stratigraphic data from the well to seismic data shows that the lavas are within a sequence of layered reflections that onlap, and are thus younger than, easterly verging structures, and that were themselves probably uplifted prior to deposition of the Mackenzie Mountains Supergroup. These relationships thus show that at least two stages of Proterozoic compressional deformation, one that predated and one that postdated the basalts, produced structures beneath the Anderson Plains.
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Jinbiao, Chen. "An explanatory note on proterozoic stratigraphic nomenclature used in the People's Republic of China." Precambrian Research 29, no. 1-3 (June 1985): 3–4. http://dx.doi.org/10.1016/0301-9268(85)90054-3.
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Nagovitsin, K. E., A. M. Stanevich, and T. A. Kornilova. "Stratigraphic setting and age of the complex Tappania-bearing Proterozoic fossil biota of Siberia." Russian Geology and Geophysics 51, no. 11 (November 2010): 1192–98. http://dx.doi.org/10.1016/j.rgg.2010.10.004.
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Дисертації з теми "Stratigraphic Proterozoic":

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Strauss, Toby Anthony Lavery. "The geology of the Proterozoic Haveri Au-Cu deposit, Southern Finland." Thesis, Rhodes University, 2004. http://hdl.handle.net/10962/d1015978.
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The Haveri Au-Cu deposit is located in southern Finland about 175 km north of Helsinki. It occurs on the northern edge of the continental island arc-type, volcano-sedimentary Tampere Schist Belt (TSB) within the Palaeoproterozoic Svecofennian Domain (2.0 – 1.75 Ga) of the Fennoscandian Shield. The 1.99 Ga Haveri Formation forms the base of the supracrustal stratigraphy consisting of metavolcanic pillow lavas and breccias passing upwards into intercalated metatuffs and metatuffites. There is a continuous gradation upwards from the predominantly volcaniclastic Haveri Formation into the overlying epiclastic meta-greywackes of the Osara Formation. The Haveri deposit is hosted in this contact zone. This supracrustal sequence has been intruded concordantly by quartz-feldspar porphyries. Approximately 1.89 Ga ago, high crustal heat flow led to the generation and emplacement of voluminous synkinematic, I-type, magnetite-series granitoids of the Central Finland Granitoid Complex (CFGC), resulting in coeval high-T/low-P metamorphism (hornfelsic textures), and D₁ deformation. During the crystallisation and cooling of the granitoids, a magmatic-dominated hydrothermal system caused extensive hydrothermal alteration and Cu-Au mineralisation through the late-D₁ to early-D₂ deformation. Initially, a pre-ore Na-Ca alteration phase caused albitisation of the host rock. This was closely followed by strong Ca-Fe alteration, responsible for widespread amphibolitisation and quartz veining and associated with abundant pyrrhotite, magnetite, chalcopyrite and gold mineralisation. More localised calcic-skarn alteration is also present as zoned garnetpyroxene- epidote skarn assemblages with associated pyrrhotite and minor sphalerite, centred on quartzcalcite± scapolite veinlets. Post-ore alteration includes an evolution to more K-rich alteration (biotitisation). Late D₂-retrograde chlorite began to replace the earlier high-T assemblage. Late emanations (post-D₂ and pre-D₃) from the cooling granitoids, under lower temperatures and oxidising conditions, are represented by carbonate-barite veins and epidote veinlets. Later, narrow dolerite dykes were emplaced followed by a weak D₃ deformation, resulting in shearing and structural reactivation along the carbonate-barite bands. This phase was accompanied by pyrite deposition. Both sulphides and oxides are common at Haveri, with ore types varying from massive sulphide and/or magnetite, to networks of veinlets and disseminations of oxides and/or sulphides. Cataclastites, consisting of deformed, brecciated bands of sulphide, with rounded and angular clasts of quartz vein material and altered host-rock are an economically important ore type. Ore minerals are principally pyrrhotite, magnetite and chalcopyrite with lesser amounts of pyrite, molybdenite and sphalerite. There is a general progression from early magnetite, through pyrrhotite to pyrite indicating increasing sulphidation with time. Gold is typically found as free gold within quartz veins and within intense zones of amphibolitisation. Considerable gold is also found in the cataclastite ore type either as invisible gold within the sulphides and/or as free gold within the breccia fragments. The unaltered amphibolites of the Haveri Formation can be classified as medium-K basalts of the tholeiitic trend. Trace and REE support an interpretation of formation in a back-arc basin setting. The unaltered porphyritic rocks are calc-alkaline dacites, and are interpreted, along with the granitoids as having an arc-type origin. This is consistent with the evolution from an initial back-arc basin, through a period of passive margin and/or fore-arc deposition represented by the Osara Formation greywackes and the basal stratigraphy of the TSB, prior to the onset of arc-related volcanic activity characteristic of the TSB and the Svecofennian proper. Using a combination of petrogenetic grids, mineral compositions (garnet-biotite and hornblendeplagioclase thermometers) and oxygen isotope thermometry, peak metamorphism can be constrained to a maximum of approximately 600 °C and 1.5 kbars pressure. Furthermore, the petrogenetic grids indicate that the REDOX conditions can be constrained at 600°C to log f(O₂) values of approximately - 21.0 to -26.0 and -14.5 to -17.5 for the metasedimentary rocks and mafic metavolcanic rocks respectively, thus indicating the presence of a significant REDOX boundary. Amphibole compositions from the Ca-Fe alteration phase (amphibolitisation) indicate iron enrichment with increasing alteration corresponding to higher temperatures of formation. Oxygen isotope studies combined with limited fluid inclusion studies indicate that the Ca-Fe alteration and associated quartz veins formed at high temperatures (530 – 610°C) from low CO₂, low- to moderately saline (<10 eq. wt% NaCl), magmatic-dominated fluids. Fluid inclusion decrepitation textures in the quartz veins suggest isobaric decompression. This is compatible with formation in high-T/low-P environments such as contact aureoles and island arcs. The calcic-skarn assemblage, combined with phase equilibria and sphalerite geothermometry, are indicative of formation at high temperatures (500 – 600 °C) from fluids with higher CO₂ contents and more saline compositions than those responsible for the Fe-Ca alteration. Limited fluid inclusion studies have identified hypersaline inclusions in secondary inclusion trails within quartz. The presence of calcite and scapolite also support formation from CO₂-rich saline fluids. It is suggested that the calcic-skarn alteration and the amphibolitisation evolved from the same fluids, and that P-T changes led to fluid unmixing resulting in two fluid types responsible for the observed alteration variations. Chlorite geothermometry on retrograde chlorite indicates temperatures of 309 – 368 °C. As chlorite represents the latest hydrothermal event, this can be taken as a lower temperature limit for hydrothermal alteration and mineralisation at Haveri.The gold mineralisation at Haveri is related primarily to the Ca-Fe alteration. Under such P-T-X conditions gold was transported as chloride complexes. Ore was localised by a combination of structural controls (shears and folds) and REDOX reactions along the boundary between the oxidised metavolcanics and the reduced metasediments. In addition, fluid unmixing caused an increase in pH, and thus further augmented the precipitation of Cu and Au. During the late D₂-event, temperatures fell below 400 °C, and fluids may have remobilised Au and Cu as bisulphide complexes into the shearcontrolled cataclastites and massive sulphides. The Haveri deposit has many similarities with ore deposit models that include orogenic lode-gold deposits, certain Au-skarn deposits and Fe-oxide Cu-Au deposits. However, many characteristics of the Haveri deposit, including tectonic setting, host lithologies, alteration types, proximity to I-type granitoids and P-T-X conditions of formation, compare favourably with other Early Proterozoic deposits within the TSB and Fennoscandia, as well as many of the deposits in the Cloncurry district of Australia. Consequently, the Haveri deposit can be seen to represent a high-T, Ca-rich member of the recently recognised Fe-oxide Cu-Au group of deposits.
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Swift, Peter Norton. "EARLY PROTEROZOIC TURBIDITE DEPOSITION AND MELANGE DEFORMATION, SOUTHEASTERN ARIZONA." Dissertation-Reproduction (electronic), The University of Arizona, 1987. http://hdl.handle.net/10150/187544.
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Greenschist-facies, Lower Proterozoic metasedimentary rocks of the Johnny Lyon Rills and Little Dragoon Mountains of southeastern Arizona were deposited prior to the intrusion of an approximately 1690 Ma rhyodacite pluton. Well-preserved primary structures indicate deposition by turbidity currents in an intermediate to neardistal setting. Sandstone compositions suggest derivation from either a complex, heterogeneous source or multiple source terranes that provided mature, quartzose sediment as well as lesser quantities of volcaniclastic detritus. Earliest deformation, predating both intrusion of the rhyodacite and metamorphism, produced sections of melange composed primarily of dismembered turbidite beds, but also incorporating large (up to several km long) blocks of deformed basalt. Subsequent deformation, in part post-dating intrusion of the rhyodacite and in part coinciding with metamorphism, affected both melange and coherent strata, and involved isoclinal folding and layerparallel faulting and shearing. It is proposed that turbidite deposition occurred in a trench associated with a north-dipping subduction zone or on ocean floor outboard of such a trench. Melange formed primarily by ductile disruption of unlithified sediments within the subduction zone. Basalt blocks incorporated within the melange represent fragments of oceanic crust or seamounts detached from the lower plate during subduction. Later deformation and intrusion of the rhyodacite occurred within an accretionary prism above the subduction zone. Deformation within the prism ended prior to intrusion of the 1625 ± 10 Ma posttectonic Johnny Lyon Granodiorite.
3
Li, Longming, and 李龙明. "The crustal evolutionary history of the Cathaysia Block from the paleoproterozoic to mesozoic." PG_Thesis, The University of Hong Kong (Pokfulam, Hong Kong), 2010. http://hub.hku.hk/bib/B45693596.
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Wang, Wei, and 王伟. "Sedimentology, geochronology and geochemistry of the proterozoic sedimentary rocks in the Yangtze Block, South China." PG_Thesis, The University of Hong Kong (Pokfulam, Hong Kong), 2003. http://hdl.handle.net/10722/196033.
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The South China Craton comprises the Yangtze Block in the northwest and Cathaysia Block in the southeast. Located in the southeastern Yangtze Block, the Jiangnan Orogen formed through the amalgamation between the Yangtze and Cathaysia Blocks. The Yangtze Block has sporadically exposed Archean rocks in the north, Paleoproterozoic to Mesoproterozoic volcano-sedimentary sequences in the southwest and widespread Neoproterozoic sedimentary sequences accompanied by syn-sedimentary igneous rocks on the western and southeastern margins. The late Paleoproterozoic to early Mesoproterozoic Dongchuan, Dahongshan and Hekou groups in the southwestern Yangtze Block formed in a series of fault-controlled, rift-related basins associated with the fragmentation of the supercontinent Columbia. These sedimentary sequences were deposited between 1742 and 1503 Ma, and recorded continuous deposition from alluvial fan and fluvial sedimentation during the initial rifting to deep marine sedimentation in a passive margin setting. Sedimentation during initial rifting received felsic detritus mainly from adjacent continents, whereas sedimentation in a passive margin basin received detritus from felsic to intermediate rocks of the Yangtze Block. Paleoproterozoic to Mesoproterozoic rift basins in the southwestern Yangtze Block are remarkably similar to those of north Australia and northwestern Laurentia in their lower part (1742-1600 Ma), but significantly different after ca. 1600 Ma. The southwestern Yangtze Block was likely connected with the north Australia and northwestern Laurentia in Columbia but drifted away from these continents after ca. 1600 Ma. Traditionally thought Mesoproterozoic sedimentary sequences in the southeastern Yangtze Block are now confirmed to be Neoproterozoic in age and include the 835-830 Ma Sibao, Fanjingshan and Lengjiaxi groups, and 831-815 Ma Shuangqiaoshan and Xikou groups. These sequences are unconformably overlain by the ~810-730 Ma Danzhou, Xiajiang, Banxi, Heshangzheng, Luokedong and Likou groups. The regional unconformity likely marked the amalgamation between the Yangtze and Cathaysia Blocks and thus occurred at ~815-810 Ma. The lower sequences (835-815 Ma) received dominant Neoproterozoic (~980-820) felsic to intermediate materials in an active tectonic setting related to continental arc and orogenic collision, whereas the upper sequences represent sedimentation in an extensional setting with input of dominant Neoproterozoic granitic to dioritic materials (~740-900 Ma). The upper parts of the Shuangqiaoshan and Xikou groups, uncomfortably underlain by lower units, are molasse-type assemblages with additional input of pre-Neoproterozoic detritus, representing accumulation of sediments in a retro-arc foreland basin associated with the formation of the Jiangnan Orogen. Stratigraphic correlation, similarly low-δ18O and tectonic affinity of igneous rocks from different continents suggest that the Yangtze Block should be placed in the periphery of Rodinia probably adjacent to northern India. Paleoproterozoic (~2480 Ma and ~2000 Ma) and Early Neoproterozoic (711-997 Ma) were the most important periods of crustal and magmatic events of the southeastern Yangtze Block, but there is a lack of significant Grenvillian magmatism. Early Neoproterozoic magmatism highlights the contribution from both juvenile materials and pre-existing old crust, whereas ~2480 Ma and ~2000 Ma events are marked by reworking of pre-existing continental crust. Magmatism at 1600-1900 Ma was dominated by reworking of pre-existing crust, whereas the 1400-1600 Ma magmatic event recorded some addition of juvenile materials.
published_or_final_version
Earth Sciences
Doctoral
Doctor of Philosophy
5
Zhao, Junhong, and 趙軍紅. "Geochemistry of neoproterozoic arc-related plutons in the Western margin of the Yangtze Block, South China." PG_Thesis, The University of Hong Kong (Pokfulam, Hong Kong), 2008. http://hub.hku.hk/bib/B40203748.
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Harris, Charles William. "A sedimentological and structural analysis of the Proterozoic Uncompahgre Group, Needle Mountains, Colorado." Dissertation, Virginia Polytechnic Institute and State University, 1987. http://hdl.handle.net/10919/79644.
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Siliciclastic sediments of the Proterozoic Uncompahgre Group can be subdivided into stratigraphic units of quartzite (Q) and pelite (P); these units include a basal, fining- and thinning-upward retrogradational sequence (Q1-P1) that records the transition from an alluvial to a shallow-marine setting. Overlying the basal sequence are three thickening- and coarsening-upward progradational sequences (P2-Q2, P3-Q3 and P4-Q4) that were influenced by tide-, storm- and wave-processes. The progradational units are subdivided into the following facies associations in a vertical sequence. Outer-to inner-shelf mudstones, Bouma sequence beds and storm beds of association A are succeeded by inner-shelf to shoreface cross-stratified sandstones of association B. Conglomerates and cross-bedded sandstones of upper association B represent alluvial braid-delta deposits. Tidal cross-bedded facies of the inner shelf/shoreface (association C) gradationally overlie association B. Interbedded within the tidal facies in upper association C are single pebble layers or <1 m-thick conglomerate beds and trough cross-bedded pebbly sandstones. Single pebble layers could be due to storm winnowing whereas conglomerates and pebbly sandstones may record shoaling to an alluvial/ shoreface setting. A temporally separated storm/alluvial and tidal shelf model best explains the origin and lateral distribution of facies in the progradational sequences. The presence of smaller progradational increments in the mudstone dominated units (P3) and the recurrence of facies associations in the thick quartzite/conglomerate units (Q2, Q3, Q4) suggests that external cyclic factors controlled sedimentation. A composite relative sea level curve integrating glacio-eustatic oscillations and long-term subsidence may account for the evolution of the thick progradational sequences of the Uncompahgre Group. Sedimentary rocks of the Uncompahgre Group have been subjected to polyphase deformation and greenschist facies metamorphism. Phase 1 structures (localized to the West Needle Mountains) include bedding-parallel deformation zones, F₁ folds and an S₁ cleavage. Phase 2 coaxial deformation resulted in the development of upright, macroscopic F₂ folds and an axial-planar crenulation cleavage, S₂. In addition basement-cover contacts were folded. Phase 3 conjugate shearing generated strike-parallel offset in stratigraphic units, a macroscopic F₃ fold, and an S₃ crenulation cleavage. In addition, oblique-slip, reverse faults were activated along basement-cover contacts. The Uncompahgre Group unconformably overlies and is inferred to be parautochthonous upon ca. 1750 Ma gneissic basement that was subjected to polyphase deformation (DB) and amphibolite facies metamorphism. Basement was intruded by ca. 1690 Ma granitoids. Deformation of gneissic and plutonic basement together with cover (DBC) postdates deposition of the Uncompahgre Group. The structural evolution of the Uncompahgre Group records the transition from a ductile, north-directed, fold-thrust belt to the formation of a basement involved “megamullion" structure which was subjected to conjugate strike-slip faulting to accommodate further shortening. DBC deformation may be analogous to the deep foreland suprastructure of an orogenic belt that developed from ca. 1690 to 1600 Ma in the southwestern U.S.A ..
Ph. D.
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Saylor, Beverly Z. (Beverly Zella). "Sequence stratigraphic and chemostratigraphic constraints on the evolution of the terminal Proterozoic to Cambrian Nama Basin, Namibia." Thesis, Massachusetts Institute of Technology, 1996. http://hdl.handle.net/1721.1/10668.
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Thesis (Ph. D.)--Massachusetts Institute of Technology, Dept. of Earth, Atmospheric, and Planetary Sciences, 1996.
Includes bibliographical references (p. 117-124).
by Beverly Z. Saylor.
Ph.D.
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Gibson, R. G. "Structural studies in a Proterozoic gneiss complex and adjacent cover rocks, west Needle Mountains, Colorado." Dissertation, Virginia Polytechnic Institute and State University, 1987. http://hdl.handle.net/10919/76096.
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Proterozoic rocks in the Needle Mountains include ca. 1750 Ma amphibolite-grade, metavolcanic and metaplutonic gneisses and ca. 1690 Ma granitoids that comprise the basement to the siliciclastic Uncompahgre Group. The mafic and felsic gneisses underwent synkinematic metamorphism and two phases of isoclinal folding and foliation development during DB, prior to emplacement of the ca. 1690 Ma plutons. DBC deformation caused folding of DB fabrics in the gneisses, development of a subvertical, east-striking foliation in the granitoids, and generation of a macroscopic sigmoidal foliation pattern throughout the area prior to 1430 Ma. DBC structures in the basement are correlated with macroscopic structures in the Uncompahgre Group, which was deformed into an east-trending cuspate synclinorium during this event. Gently plunging mineral lineations and asymmetric kinematic indicators in the basement record a component of dextral strike-slip shearing in domains of east-striking foliation and sinistral shearing in areas of northeast-striking foliation. A model for DBC involving the development of conjugate strike-slip shear zones in response to north-northwest shortening is most consistent with the kinematic and fabric orientation data. A zone of phyllite, derived largely from basement, occurs everywhere along the basement-cover contact. Kinematic indicators along and near the contact record upward movement of the cover relative to the basement on each side of the synclinorium and imply that the cover rocks are parautochthonous. Stratigraphic facing of the cover rocks away from the basement supports the interpretation of this contact as an unconformity at the base of the Uncompahgre Group. Alteration of the basement rocks along this contact involved hydration and the loss of CaO, MgO, SiO₂, and Na₂O. The phyllite zone is interpreted as a metamorphosed and deformed regolith that localized out-of-synform movement while the basement and its parautochthonous cover were folded together during DBC. Rocks in the Needle Mountains comprise part of the Colorado Province, one of several terranes that were possibly accreted to the Archean Wyoming Craton during the Proterozoic. Age constraints on the timing of deformation indicate that DB and DBC are representative of two regionally extensive deformational episodes. Pre-1700 Ma deformation is attributed to the assembly of volcanogenic terranes and their accretion to the Wyoming Craton along the Cheyenne Belt. Post-1700 Ma deformation resulted from regional north-northwest crustal shortening induced by tectonic interactions along the southern margin of the Colorado Province. These results support the hypothesis that terrane accretion was important in the Proterozoic crustal evolution of southwestern North America.
Ph. D.
9
Hill, Robert E. (Robert Einar). "Stratigraphy and sedimentology of the Middle Proterozoic Waterton and Altyn Formations, Belt-Purcell Supergroup, southwest Alberta." Electronic Thesis or Dissertation, McGill University, 1985. http://digitool.Library.McGill.CA:80/R/?func=dbin-jump-full&object_id=63330.
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10
Lane, Robert Andrew. "Geologic setting and petrology of the Proterozoic Ogilvie Mountains breccia of the Coal Creek inlier, southern Ogilvie Mountains, Yukon Territory." Thesis/Dissertation, University of British Columbia, 1990. http://hdl.handle.net/2429/29196.
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Анотація:
Ogilvie Mountains breccia (OMB) is in Early (?) to Late Proterozoic rocks of the Coal Creek Inlier, southern Ogilvie Mountains, Yukon Territory. Host rocks are the Wernecke Supergroup (Fairchild Lake, Quartet and Gillespie Lake groups) and lower Fifteenmile group. Distribution and cross-cutting relationships of the breccia were delineated by regional mapping. OMB was classified by clast type and matrix composition. Ogilvie Mountains breccia crops out discontinuously along two east-trending belts called the Northern Breccia Belt (NBB) and the Southern Breccia Belt (SBB). The NBB extends across approximately 40 km of the map area, and the SBB is about 15 km long. Individual bodies of OMB vary from dyke- and sill-like to pod-like. The breccia belts each coincide with a regional structure. The NBB coincides with a north side down reverse fault—an inferred ruptured anticline—called the Monster fault. The SBB coincides with a north side down fault called the Fifteenmile fault. These faults, at least in part, guided ascending breccia. The age of OMB is constrained by field relationships and galena lead isotope data. It is younger than the Gillespie Lake Group, and is at least as old as the lower Fifteenmile group because it intrudes both of these units. A galena lead isotope model age for the Hart River stratiform massive sulphide deposit that is in Gillespie Lake Group rocks is 1.45 Ga. Galena from veinlets cutting a dyke that cuts OMB in lower Fifteenmile group rocks is 0.90 Ga in age. Therefore the age of OMB formation is between 1.45 and 0.90 Ga. Ogilvie Mountains breccia (OMB) has been classified into monolithic (oligomictic) and heterolithic (polymictic) lithologies. These have been further divided by major matrix components—end members are carbonate-rich, hematite-rich and chlorite-rich. Monolithic breccias with carbonate matrices dominate the NBB. Heterolithic breccias are abundant locally in the NBB, but are prevalent in the SBB. Fragments were derived mainly from the Wernecke Supergroup. In the SBB fragments from the lower Fifteenmile group are present. Uncommon mafic igneous fragments were from local dykes. OMB are generally fragment dominated. Recognized fragments are up to several 10s of metres across and grade into matrix sized grains. Hydrothermal alteration has locally overprinted OMB and introduced silica, hematite and sulphide minerals. This mineralization has received limited attention from the mineral exploration industry. Rare earth element chemistry reflects a lack of mantle or deep-seated igneous process in the formation of OMB. However, this may be only an apparent lack because flooding by a large volume of sedimentary material could obscure a REE pattern indicative of another source. The genesis of OMB is significantly similar to modern mud diapirs. It is proposed that OMB originated from pressurized, underconsolidated fine grained limey sediments (Fairchild Lake Group). These were trapped below and loaded by turbidites (Quartet Group) and younger units. Tectonics and the initiation of major faults apparently triggered movement of the pressurized fluid-rich medium. The resulting bodies of breccia are sill-like and diapir-like sedimentary intrusions. Fluid-rich phases may have caused hydrofracturing (brittle failure) of the surrounding rocks (especially in the hanging wall). Breccia intrusion would have increased the width of the passage way while encorporating more fragments. Iron- and oxygen-rich hydrothermal fluids apparently were associated with the diapirism. Presumably these fluids are responsible for the high contents of hematite and iron carbonate in fragments, and especially, in the matrix of the breccias. Exhalation of these fluids may have formed the sedimentary iron formations that are spatially associated with the breccias.
Science, Faculty of
Earth, Ocean and Atmospheric Sciences, Department of
Graduate

Книги з теми "Stratigraphic Proterozoic":

1
Wisconsin--Madison), International Proterozoic Symposium (1981 University of. Proterozoic geology: Selected papers from an International Proterozoic Symposium. Boulder, Colo: Geological Society of America, 1986.
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2
Dawes, Peter R. The Proterozoic Thule Supergroup, Greenland and Canada: History, lithostratigraphy, and development. Copenhagen, Denmark: Geological Survey of Denmark and Greenland, Ministry of Environment and Energy, 1997.
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3
Truswell, J. F. Early Proterozoic red beds on the Kaapvaal craton. Johannesburg: University of the Witwatersrand, 1990.
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4
Greene, Robert C. Stratigraphy of the Late Proterozoic Murdama Group, Saudi Arabia. [Menlo Park, CA: U.S. Geological Survey], 1993.
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5
Aitken, James D. Uppermost Proterozoic formations in central Mackenzie Mountains, Northwest Territories. Ottawa, Ont., Canada: Energy, Mines and Resources Canada, 1989.
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6
Frarey, M. J. Proterozoic geology of the Lake Panache-Collins Inlet area, Ontario. Ottawa, Canada: Geological Survey of Canada, 1985.
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7
Blacet, Philip M. Proterozoic geology of the Brady Butte area, Yavapai County, Arizona. [Reston, Va.?]: Dept. of the Interior, U.S. Geological Survey, 1985.
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8
NATO, Advanced Study Institute on the Deep Proterozoic Crust in the North Atlantic Provinces (1984 Moi Norway). The Deep Proterozoic crust in the North Atlantic provinces. Dordrecht: D. Reidel Pub. Co., 1985.
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9
Whipple, James W. Stratigraphy and lithocorrelation of the Snowslip Formation (Middle Proterozoic Belt Supergroup), Glacier National Park, Montana. [Washington, D.C.]: U.S. G.P.O., 1988.
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10
Sims, P. K. Geology and geochemistry of Early Proterozoic rocks in the Dunbar area, northeastern Wisconsin. Washington: U.S. G.P.O., 1992.
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Частини книг з теми "Stratigraphic Proterozoic":

1
Young, Grant M. "Earth's Earliest Extensive Glaciations: Tectonic Setting and Stratigraphic Context of Paleoproterozoic Glaciogenic Deposits." In The Extreme Proterozoic: Geology, Geochemistry, and Climate, 161–81. Washington, D. C.: American Geophysical Union, 2013. http://dx.doi.org/10.1029/146gm13.
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2
Gradstein, Felix M. "Proterozoic Eon." In Encyclopedia of Astrobiology, 2038. Berlin, Heidelberg: Springer Berlin Heidelberg, 2015. http://dx.doi.org/10.1007/978-3-662-44185-5_1291.
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3
Gradstein, Felix M. "Proterozoic (Aeon)." In Encyclopedia of Astrobiology, 1351. Berlin, Heidelberg: Springer Berlin Heidelberg, 2011. http://dx.doi.org/10.1007/978-3-642-11274-4_1291.
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4
Frazier, William J., and David R. Schwimmer. "The Proterozoic." In Regional Stratigraphy of North America, 39–97. Boston, MA: Springer US, 1987. http://dx.doi.org/10.1007/978-1-4613-1795-1_3.
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Gradstein, Felix M. "Proterozoic Aeon." In Encyclopedia of Astrobiology, 1–2. Berlin, Heidelberg: Springer Berlin Heidelberg, 2014. http://dx.doi.org/10.1007/978-3-642-27833-4_1291-3.
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6
Gradstein, Felix M. "Proterozoic Eon." In Encyclopedia of Astrobiology, 1–2. Berlin, Heidelberg: Springer Berlin Heidelberg, 2020. http://dx.doi.org/10.1007/978-3-642-27833-4_1291-4.
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Miall, Andrew D. "Stratigraphic Correlation." In Principles of Sedimentary Basin Analysis, 79–140. Berlin, Heidelberg: Springer Berlin Heidelberg, 2000. http://dx.doi.org/10.1007/978-3-662-03999-1_3.
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Miall, Andrew D. "Stratigraphic correlation." In Principles of Sedimentary Basin Analysis, 83–148. New York, NY: Springer New York, 1990. http://dx.doi.org/10.1007/978-1-4757-4235-0_3.
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9
Emslie, R. F. "Proterozoic Anorthosite Massifs." In The Deep Proterozoic Crust in the North Atlantic Provinces, 39–60. Dordrecht: Springer Netherlands, 1985. http://dx.doi.org/10.1007/978-94-009-5450-2_4.
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10
Jin, Bai, and Dai Fengyan. "Early Proterozoic Crust." In Precambrian Crustal Evolution of China, 87–159. Berlin, Heidelberg: Springer Berlin Heidelberg, 1998. http://dx.doi.org/10.1007/978-3-662-03697-6_3.
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Тези доповідей конференцій з теми "Stratigraphic Proterozoic":

1
Crombez, Vincent, Marcus Kunzmann, Claudio Delle Piane, Mohinudeen Faiz, Stuart Munday, and Anne Forbes. "STRATIGRAPHIC ARCHITECTURE OF A PROTEROZOIC SHALE PLAY: INSIGHTS FROM WELL CORRELATION IN THE VELKERRI FORMATION (BEETALOO SUB-BASIN, NORTHERN TERRITORY, AUSTRALIA)." In GSA 2020 Connects Online. Geological Society of America, 2020. http://dx.doi.org/10.1130/abs/2020am-357071.
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2
Planavsky, Noah J., Mingyu Zhao, and Christopher T. Reinhard. "MID-PROTEROZOIC OXYGEN AND METHANE." In GSA Annual Meeting in Seattle, Washington, USA - 2017. Geological Society of America, 2017. http://dx.doi.org/10.1130/abs/2017am-308114.
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3
Dayal, A. "Discovery of Hydrocarbon in Proterozoic Basin." In 71st EAGE Conference and Exhibition incorporating SPE EUROPEC 2009. European Association of Geoscientists & Engineers, 2009. http://dx.doi.org/10.3997/2214-4609.201400471.
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4
Nowak, Ethan J., and Matthias G. Imhof. "Stratigraphic filtering." In SEG Technical Program Expanded Abstracts 2003. Society of Exploration Geophysicists, 2003. http://dx.doi.org/10.1190/1.1817814.
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5
Bykova, Natalia, Qin Ye, Dmitriy Grazhdankin, and Shuhai Xiao. "MACROALGAE THROUGH PROTEROZOIC: MORPHOLOGICAL AND PALEOECOLOGICAL ANALYSES." In GSA Annual Meeting in Indianapolis, Indiana, USA - 2018. Geological Society of America, 2018. http://dx.doi.org/10.1130/abs/2018am-316654.
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6
Karlstrom, Karl E., Michael L. Williams, Mark Edward Holland, Jacob Mulder, George E. Gehrels, and Mark Pecha. "PROTEROZOIC ACCRETIONARY OROGENS OF SOUTHERN LAURENTIA REVISITED." In GSA Annual Meeting in Denver, Colorado, USA - 2016. Geological Society of America, 2016. http://dx.doi.org/10.1130/abs/2016am-282369.
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7
Karimi, Parvaneh, and Sergey Fomel. "Stratigraphic coordinate system." In SEG Technical Program Expanded Abstracts 2011. Society of Exploration Geophysicists, 2011. http://dx.doi.org/10.1190/1.3628232.
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8
Hamilton, Trinity L. "MODEL PHOTOAUTOTROPHS ISOLATED FROM A PROTEROZOIC OCEAN ANALOG." In Joint 52nd Northeastern Annual Section and 51st North-Central Annual GSA Section Meeting - 2017. Geological Society of America, 2017. http://dx.doi.org/10.1130/abs/2017ne-289804.
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9
Boerner, D. E., R. D. Kurtz, J. A. Craven, and F. W. Jones. "Electromagnetic imaging of the Alberta Paleo‐Proterozoic basement." In SEG Technical Program Expanded Abstracts 1996. Society of Exploration Geophysicists, 1996. http://dx.doi.org/10.1190/1.1826620.
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10
Dunham, Jeremy I., Ashley R. Manning-Berg, Linda C. Kah, and Julie K. Bartley. "VARIATION IN MICROFABRIC WITHIN PROTEROZOIC EARLY DIAGENETIC CHERT." In GSA Annual Meeting in Denver, Colorado, USA - 2016. Geological Society of America, 2016. http://dx.doi.org/10.1130/abs/2016am-283245.
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Звіти організацій з теми "Stratigraphic Proterozoic":

1
Lane, L. S., and R. B. MacNaughton. Central Foreland NATMAP Project: Proterozoic to Devonian stratigraphic sections in British Columbia and Yukon. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 2017. http://dx.doi.org/10.4095/299863.
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2
Lane, L. S., and R. B. MacNaughton. Introduction to stratigraphic sections from the Central Foreland NATMAP Project area: Proterozoic to Devonian successions. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 2017. http://dx.doi.org/10.4095/306301.
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3
Norris, D. K., and L. D. Dyke. Proterozoic. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 1997. http://dx.doi.org/10.4095/208890.
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4
Sevigny, J. H. Field and Stratigraphic Relations of Amphibolites in the Late Proterozoic Horsethief Creek Group, northern Adams River area, British Columbia. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 1987. http://dx.doi.org/10.4095/122536.
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5
Williams, G. K. Proterozoic, Mackenzie Corridor. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 1986. http://dx.doi.org/10.4095/130056.
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6
Wilton, D. H. C., C. S. MacDougall, L. M. Mackenzie, and C. Pumphrey. Stratigraphic and metallogenic relationships along the unconformity between Archean granite basement and the early Proterozoic Moran Lake Group, central Labrador. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 1988. http://dx.doi.org/10.4095/122642.
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7
Cook, F. A. Lower Paleozoic and Proterozoic stratigraphy in the Colville Hills-Tweed Lake area, Northwest Territories: implications for regional seismic stratigraphic correlations. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 1992. http://dx.doi.org/10.4095/132860.
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8
Aitken, J. D., and M. E. McMechan. Chapter 5: Middle Proterozoic Assemblages. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 1991. http://dx.doi.org/10.4095/134083.
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9
Gabrielse, H., and R. B. Campbell. Chapter 6: Upper Proterozoic Assemblages. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 1991. http://dx.doi.org/10.4095/134085.
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10
Bednarski, J. Surficial stratigraphic framework. Natural Resources Canada/ESS/Scientific and Technical Publishing Services, 2016. http://dx.doi.org/10.4095/298877.
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