Coastal current

According to the autochthonous, in situ theory of coal formation, peat beds and subsequently coal were formed from the accumulation of plants and plant debris in place. According to the allochthonous theory, the coal-producing peat bogs or swamps were formed from plant debris that had been transported, usually by streams or coastal currents, to the observed burial sites. 

The top right of Figure 1.22 shows the tidal turbine that can be used in many tidal areas. They are basically wind turbines that can be located anywhere there is strong tidal flow. They are arrayed underwater in rows, as in some wind farms. The turbines function best where coastal currents run between 3.6 and 4.9 knots (4 and 5.5 mph). In currents of that speed, a 15-meter (49.2-feet) diameter tidal turbine can generate as much energy as a 60-meter (197-feet) diameter wind turbine. Ideal locations for tidal turbine farms are close to shore in water depths of 20-30 meters (65.5-98.5 feet). 

Figure 6.1 The major routes of sediment transport from land to the open ocean can simply be illustrated through the following sequence streams, rivers, estuaries, shallow coastal waters, canyons, and finally the abyssal ocean. Arrows indicate the effects of coastal currents and resuspension events on the transport and distribution of particles delivered to the coastal zone. There can be substantial storage in each of these environments. (From Degens, 1989, with permission.)...

The sediments of the Caucasian region are formed under the influence of the solid runoff of mountain rivers and due to the intensive development of the processes of abrasion and denudation. Waves and coastal currents significantly affect the distribution of the terrigenous-detrital matter over the underwater slope, concentrating largest particles of the matter of boulders, pebbles, and sands close to the coastline and on the beach. Beyond the zone of the wave action, fine-grained sands and silty oozes are accumulated. Often, bedrocks are exposed at abrasive surfaces of the underwater slope at depths down to 60 m. 

Titov VB (1989) Characterization of coastal current regime off northern Caucasus coast. SB IO RAS, Gelendjic (in Russian)... 

Figure 17. 2 Schematic representation of the seasonal variations in physical forces, discharges, and suspended sediment inventory on the Amazon shelf (from Nittrouer and DeMaster 1996, and Kineke et. al. 1996). The suspended sediment inventories include the fluid mud layers, which can comprise more the 90% of the suspended material on the shelf. The timing of the 4 AmasSeds cruises are shown at the bottom of the figure. In the upper figure NBC refers to the North Brazilian Coastal Current,...

Coastal Current is essential to unraveling complex chemical cycles in this dynamic coastal environment. 

At the same time, this strong wind causes the development and the impact of high waves onto the beach. This generates a strong coastal current, which repeatedly and rapidly deforms the local shoreline. Therefore, high water levels up to the storm surge can occur... 

Methane August, 1980. The surface distribution of dissolved methane (nL/L, STP) in August 1980 is shown in Figure 3a. The highest surface concentrations were found near the entrance to Port Moller and near Unimak Pass (see Figure 1). At the entrance to Port Moller, concentrations of dissolved methane were greater than 2500 nL/L (about 35 times the equilibrium value) and decreased along the coast toward the northeast. The direction of the methane plume marks the mean drift of the coastal current. 

The lower concentrations of methane correlate with lower sea surface temperatures (SST) and near-bottom temperatures over the middle shelf. Bottom temperatures over the middle shelf were < -1 C in October 1975 and July 1976, compared to temperatures of 3.5-4.5 C observed in May 1981 (39). Water temperatures this low indicate local ice formation the previous winter. On the other hand, bottom temperatures in St. George Basin in May 1981 were about the same as those observed in October 1975 and July 1976 (17) indicating that these waters were less influenced by the abnormally cold winters than the middle shelf region. This is expected because the north-setting coastal current brings relatively warm Gulf of Alaska water across the outer shelf (19). 

Shetye, S.R., Gouveia, A., Shenoi, S.S.C., Michael, G.S., Sundar, D., Almeida, A.M. and Santanam K. (1991) The coastal current off western India during northeast monsoon. Deep-Sea Research, 38, 1517-1529. 

Hill, A.E. and Simpson, J.H. (1988) Low-frequency variability of die Scottish Coastal Current induced by along-shore pressure gradients. Estuarine, Coastal and Shelf Science, 27, 163—180. 

Unit C encompasses the basal sediments of a marine transgression. As the sea level continued rising the eroded material coming from the tidal flats, the intertidal zones, the lagoons and the volcanic expanses of the Lower Series was deposited on the coastal sea floors under a shallow water cover. Most of these materials were derived from the reworking of the Cambro-Ordovician sediments and transported along the coast by coastal currents. 

The Yellow Sea is affected by warm and saline oceanic currents and less saline coastal currents in a basin-wide scheme of a cyclonic gyre. In general, the former flow northward whilst the latter flow southward. On the east side of the Yellow Sea, the Kuroshio and Tsushima Warm Currents and the Yellow Sea... 

Fig. 1.23. Schematic map of the regional circulation patterns in the YeUow Sea. BCC Bohai coastal current LDCC Liaodong coastal current KCC Korea coastal current YSCC Yellow Sea coastal current YSWC Yellow Sea Warm Current CDFW Changjiang diluted freshwater TC Tushima current YSCW YeUow Sea Cold Water (Yang et al., 2003) (With permission from Elsevier s Copyright Clearance Center)...

The East China Sea circulation is dominated by the northward flow of two loops of the Kuroshio Current (KC) the Taiwan Warm Water (TWW) in the west and the Yellow Sea Warm Water (YSWW) in the east. Both water masses are characterized by high salinity and warm water temperatures. In contrast, a southward flow in close to sea bottom water occurs from the flow of the Changjiang (CJCW) and Jiangsu Coastal Waters (JCW) along the Chinese coast, the Korean Coastal Waters (KCW) in the east, and the Yellow Sea Cold Waters (YSCW) in the north (Fig. 1.30, Lee and Chao, 2003). The coastal currents in particular appear as seasonally cold and brackish water masses. 

Fig. 1.40. Diagrams of the surface current patterns on the climatological map in the SCS for (a) winter and (b) summer. K, Kuroshio KC, Karimata current SCSWC, South China Sea Warm Current GC, Guangdong coastal current LCE, Luzon cold eddy VCE, Vietnam cold eddy (Liu QY et al., 2008) (With permission from Springer)...

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