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Albania
Published in Enzo Pranzini, Allan Williams, Coastal Erosion and Protection in Europe, 2013
this coastal lowland was created by river deposition from the sixteenth century to the present, with the growth mechanism being delta progression (Mathers et al., 1999). Geological profiles based on heavy mineral analysis (rutile, zircon, chromium, etc.) show the coastline's progress and successive levels up to the present. The presence of these minerals in Quaternary lowland deposits indicates five successive steady growth stages, ranging from the Flandrian transgression to the present. In general, coastal morphological features and coastline extension are similar for the river mouths of Vjosa, Seman and Shkumbin, all functions of the riverine solid load volume reflected in the number of deltas (7-8) and the size of the impact sectors through river mouth displacement. The maximum displacement distance of the Seman river mouth reaches about 33 km; at the Vjosa River it is 20 km while at all other rivers this value is 9-15 km. The evidence is the presence of old riverbeds in the form of abandoned meanders, the river Drin being the most characteristic. Typical also are the old riverbeds of the Seman, Vjosa and Shkumbin, which formed the major part of this lowland, especially after the fifteenth and sixteenth centuries. During this period the coastline constantly advanced westward to its present position, evidenced by the presence of lagoons, swamps and abandoned meanders in the form of a wide belt along its eastern side. Obviously, in this evolution, along with accumulation, there has also been erosion activity in the opposite sectors of the river mouth displacement, e.g. along the Capes of Rodon, Bishti Palles, Cape of Turra and Treporte (Berreti, 1998).
Paleo-environment and provenance in a lacustrine shallow-water delta-meandering river sedimentary system: insights from the Middle–Upper Jurassic formations of the Fukang Sag of Junggar Basin, NW China
Published in Australian Journal of Earth Sciences, 2019
L. Luo, X. Gao, X. Tan, J. Gluyas, J. Wang, X. Kong, J. Huang, H. Shao, F. Qu
Generally heavy minerals are derived from specific source rocks and heavy mineral analysis is the most common technique for provenance determination (Aubrecht et al., 2017; Bassis, Hinderer, & Meinhold, 2016; Do Nascimento et al., 2015; Garzanti, Andò, & Vezzoli, 2008; Morton & Hallsworth, 1999; Nie et al., 2012; Sevastjanova, Hall, & Alderton, 2012; Svendsen & Hartley, 2002). The heavy mineral composition of a source rock can be altered and modified by many processes such as chemical weathering, hydraulic sorting during transport, sorting by grainsize, diagenetic alteration during deposition and burial processes (Garzanti et al., 2008; Morton & Hallsworth, 1999). Therefore, some heavy mineral (HM) assemblages, which are sensitive to their environment, can also be used to evaluate the approximate paleogeographic conditions, including paleoclimate, paleo-environment and paleotopography (Dinis & Soares, 2007; Jin, Lin, Yang, & Ji, 2002; Lin, Chen, & Liu, 2008; Liu, 2012). Heavy mineral analysis was performed on 30 samples, which were collected from the Toutunhe and Qigu formations, to identify the species and characteristics. Moreover, the heavy mineral data of 56 samples from the East Fukang slope were collected from the Xinjiang oilfield and previous published results (Ji et al., 2014).