Step-like growth of the continental crust in South China: evidence from detrital zircons in Yangtze River sediments
Zheng-Wei LiangShan GaoChris HawkesworthYuan-Bao WuCraig StoreyLian ZhouMing LiZhao-Chu HuYongsheng LiuXiaoming Liu
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Supercontinent
Rodinia
The break-up of Rodinia, the supercontinent assembled in the Middle Proterozoic chelogenic cycle (1.65--1.0 Ga), and the simultaneous assembly of the Gondwana Supercontinent were the major tectonic events of the Neoproterozoic. Laurentia occupied a central keystone position in the configuration of Rodinia. Its break-up resulted in rearrangement of Rodinia fragments: some were incorporated in the accreting Gondwana, while Laurentia, Baltica and Siberia drifted independently. Reconstructions of the position of Laurentia in the Rodinia Supercontinent are based on two criteria. The first is the continuity of Middle Proterozoic mobile belts suturing the older cratons and the match of piercing points of the mobile belts at the post- Middle Proterozoic margins of the older cratons. The second is the similarity of sedimentary sequences along Late Proterozoic passive margins formed during break-up of Rodinia. The first criterion allows for several interpretations. The second may be invalid, as conjugate margins developing over an oblique detachment will accumulate dissimilar sedimentary sequences. In reconstructions of the Gondwana Supercontinent the recently redefined Salvador-Congo craton occupied the central keystone position, between the East Gondwana continent and a number of smaller cratons of West Gondwana. It is entirely surrounded by collisional mobile belts, all containing important transcurrent shear zone more » systems. The margins of the Salvador-Congo craton were facing three major Late Proterozoic oceans. « less
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An interpretation of available paleomagnetic data from the Laurentia, Congo-Sao Francisco, Kalahari, and Amazonia cratons favors the hypothesis that these units were juxtaposed in a supercontinent by 1000 Ma. This supercontinent is similar to Hoffman's (1991) Rodinia, except for the Kalahari craton, whose 1300 to 1000 Ma Namaqua-Natal mobile belt is now juxtaposed against the correlated 1300 to 1000 Ma Grenville belt in eastern Laurentia, Our model suggests that a continuous 1300 to 1000 Ma orogenic belt, formed by the Grenville, Sunsas, Kibaride-Irumide-Lurio, Namaqua-Natal, and Dronning Maud Land-Coats Land belts, represents the suture zone between the Amazonia, Congo-Sao Francisco, Kalahari-Grunehogna, and Laurentia blocks. The formation of western Gondwana (from our Rodinia supercontinent) may be accomplished by the closure of the large Mozambique Ocean and the more restricted Adamastor Ocean, combined with some counterclockwise rotation of the Congo-Sao Francisco craton. Rotation of the Congo-Sao Francisco craton can explain the observed oblique convergence and wrench tectonics of Pan African-Brasiliano mobile belts that encircle this craton. The model is also consistent with the synchroneity between the Rodinia break-up and the assembly of Gondwana, as suggested by several authors (Laurentia began to separate from Rodinia at ∼625 Ma or later).
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Available geochronological data substantiate the existence of an apparent ca. one billion year gap in geological activity in the southern part of the Siberian craton. The duration of the gap is about 0.8 to 1.1 Ga in the Sayan Uplift and at least 0.9 Ga in the Baikal Uplift. We suggest that the absence of major geological activity in this interval might be due to the southern margin of Siberia occupying an internal position within a Transproterozoic supercontinent, that is, a fragment of Nuna that did not disperse until the late Neoproterozoic breakup of Rodinia. The absence of Mesoproterozoic--early Neoproterozoic sedimentary successions in southern Siberia could possibly be explained by their removal by erosion. Ediacaran subsidence following the breakup of Rodinia may reflect the solidification of magma chambers that fed Neoproterozoic mafic dike swarms. We suggest that a combination of these factors (dike emplacement and erosion) has a significant influence on global tectonics, controlling the uplift and subsidence of ancient cratons.
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The Amazonian craton major accretionary and collisional processes may be correlated to supercontinent assemblies developed at several times in the Earth history. Based on geologic, structural and paleomagnetic evidence paleocontinent reconstructions have been proposed for Archean to younger times. The oldest continent (Ur) was formed probably by five Achaean cratonic areas (Kaapvaal, Western Dhawar, Bhandara, Singhhum and Pilbara cratons). Geologic evidences suggest the participation of the Archaean rocks of the Carajás region in the Ur landmass. Supercontinental 2.45 Ga Kenorland amalgamation is indicated by paleomagnetic data including Laurentia, Baltica, Australia, and Kalahari and Kaapvaal cratons. There is no evidence indicating that Amazonian craton was part of the Kenorland supercontinent. From 1.83 Ga to 1.25 Ga Columbia and Hudsonland supercontinents including Amazonian craton were proposed based on NE portion of the Amazonian craton (Maroni/Itacaiunas province) connection with West Africa and Kalahari cratons. Rodinia supercontinent reconstructions show Amazonia joined to Laurentia-Baltica as result of 1.1 Ga to 1.0 Ga fusion based on the Sunsas-Aguapei belts and Greenville and Sveconorwegian belts, respectivelly. The large Late Mesoproterozoic landmass included also Siberia, East Antartica, West Nile, Kalahari, Congo/Sao Francisco and Greenland. The 750 - 520 Ma Gondwana assembly includes most of the continental fragments rifted apart during the break-up of Rodinia followed by diachronic collisions (Araguaia, Paraguay and Tucavaca belts). The supercontinent Pangea is comprised of Gondwana and Laurentia formed at about 300 - 180 Ma ago. The Amazonian craton margins probably were not envolved in the collisional processes during Pangea because it was embebed in Neoproterozoic materials. As consequence, Amazonian craton borders have no record of the orogenic processes responsible for the Pangea amalgamation.
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Rodinia
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<p>Currently three supercontinent cycles have been identified and existed supercontinents named from youngest to oldest: Pangea, Rodinia and Nuna/Columbia. Recently Wang et al. (2020) suggested that supercontinent amalgamation were each preceded by ~200 Myr by the assembly of long-lasting <em>megacontinent</em> aking to Gondwana.</p><p>The Congo-S&#227;o Francisco (C/SF) craton is a main building block in Gondwana due to its central location, but its participation to Rodinia is controversial. Salminen et al. (2018) presented 1.11 Ga paleomagnetic and geochronological data from a prominent Epembe-Huila swarm of gabbronoritic dykes in the southern part of the Congo craton in Namibia and in Angola. This paleomagnetic pole yields a relatively low paleolatitude for the C/SF craton at ca. 1.11 Ga and permits a direct connection between Congo and Kalahari cratons. This connection supports an earlier qualitative comparison (Ernst et al., 2013), that the mafic Epembe-Huila swarm was an integral component of the Umkondo Large Igneous Province (LIP). The 1.11 Ga Umkondo LIP is widespread across Kalahari craton, and coeval mafic magmatism has been identified in several of the world&#8217;s other late Mesoproterozoic cratons: Laurentia, India, Amazonia, and Antarctica (Grunehogna). Were these coeval provinces spatially linked at the time of emplacement during the amalgamation of Rodinia? Robust paleomagnetic and geochronological data from Laurentia and Kalahari have demonstrated substantial separation between those two blocks at 1.11 Ga (Swanson-Hysell et al., 2015). However, based on similar tholeiitic magmatism Choudhary et al. (2019) proposed that Kalahari and C/SF together with Amazonia and northern India constituted &#8220;Umkondia&#8221; at 1.11 Ga. It has been proposed that Umkondia occupied an intermediary &#8220;megacontinental&#8221; role in the Nuna-Rodinia transition analogous to Gondwana in Rodinia-Pangea evolution (Wang et al., 2020). Contradicting Gondwana the proposed Umkondia was not long-lasting, since it has been proposed that Kalahari and Congo separated after 1.10 Ga to form a vast ocean (ca. 6000 km) during the formation of Rodinia and widespread juvenile intra-oceanic magmatism along the present-day central Brazil indicates a large ca. 0.94 Ga ocean between C/SF and Amazonia (Cordani et al., 2003).</p><p>&#160;</p><p>Choudhary et al. 2019. Precambrian Research 332, 105382.</p><p>Cordani et al. 2003. Gondwana Research 6, 275-283.</p><p>Ernst et al. 2003. Lithos 174 1-14.</p><p>Salminen et al. 2018. Geology 46, 1011-1014.</p><p>Swanson-Hysell et al. 2015. Geophysical Journal International 203, 2237-2247.</p><p>Wang et al. 2020. Geology 49, https://doi.org/10.1130/G47988.1</p><p>&#160;</p>
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Abstract The location of the Tarim craton during the assembly and breakup of the Rodinia supercontinent remains enigmatic, with some models advocating a Tarim-Australia connection and others a location at the heart of the unified Rodinia supercontinent between Australia and Laurentia. In this study, our new zircon U-Pb dating results suggest that middle Neoproterozoic sedimentary rocks in the Altyn Tagh orogen of the southeastern Tarim craton were deposited between ca. 880 and 760 Ma in a rifting-related setting slightly prior to the breakup of Rodinia at ca. 750 Ma. A compilation of existing Neoproterozoic geological records also indicates that the Altyn Tagh orogen of the southeastern Tarim craton underwent collision at ca. 1.0-0.9 Ga and rifting at ca. 850-600 Ma related to the assembly and breakup of Rodinia. Furthermore, in order to establish the paleoposition of the Tarim craton with respect to Rodinia, available detrital zircon U-Pb ages and Hf isotopes from Meso- to Neoproterozoic sedimentary rocks were compiled. Comparable detrital zircon ages (at ca. 0.9, 1.3-1.1, and 1.7 Ga) and Hf isotopes indicate a close linkage among rocks of the southeastern Tarim craton, Cathaysia, and North India but exclude a northern or western Australian affinity. In addition, detrital zircons from the northern Tarim craton exhibit a prominent age peak at ca. 830 Ma with minor spectra at ca. 1.9 and 2.5 Ga but lack Mesoproterozoic ages, comparable to the northern and western Yangtze block. Together with comparable geological responses to the assembly and breakup of the Rodinia supercontinent, we offer a new perspective of the location of the Tarim craton between South China and North India in the periphery of Rodinia.
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The North China Craton (NCC) was clearly different from the Yangtze and Tarim cratons during the late Mesoproterozoic to early Neoproterozoic period because no distinct geological records have been found about the thermotectonic events related to assembly and breakup of the Rodinia Supercontinent. Therefore, various assumptions occur regarding relation between the NCC and the Rodinia. In recent years, some typical Grenville ages were successively yielded using the detrital zircons from the Yushulaiz Group in Liaoning, Penglai and Tumen groups in Yantai of Shandong, all of them belonging to the Neoproterozoic clastic strata distributing on both sides of the Tanlu fault. The data are similar to those from the Upper Riphean at the southeastern margin of Siberia Craton. The ages of these zircons are not characteristic of the NCC and Siberian craton, indicating that there is a close relation between the eastern margin of the NCC, the southeastern margin of Siberian craton, and the Grenville Orogen. On the basis of the assumption, we propose a hypothesis (GOSEN joining hypothesis) that the Grenville Orogen, the southeastern margin of Siberia and eastern NCC was linked.
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