Anomalous current recorded at lower low water off the Changjiang River mouth, China
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1 Geo-Mar Lett (2004) 24: DOI /s ORIGINAL Zhanghua Wang Æ Zhongyuan Chen Kazumaro Okamura Æ Jianhua Gao Æ Kaiqin Xu Hiroshi Koshikawa Æ Masataka Watanabe Anomalous current recorded at lower low water off the Changjiang River mouth, China Received: 19 November 2003 / Accepted: 5 May 2004 / Published online: 8 July 2004 Ó Springer-Verlag 2004 Abstract A hydrographic-sedimentological investigation was conducted in May 2001, aimed at assessing dynamic sedimentation patterns near and off the Changjiang River mouth, East China Sea. Current speed/direction, suspended sediment concentration (SSC), and turbidity were measured at eight nearshore and offshore sites, spanning a distance of ca. 150 km. The results identified a high-speed current ranging from 0.9 to 1.6 m/s at lower low water in the front of the turbidity maximum zone. This anomalous current, lasting about 4 h, was the fastest recorded over two semi-diurnal tidal cycles. Simultaneous measurements showed a high SSC (0.5 g/l) and high turbidity (>230 ppm) near the seafloor. This phenomenon would help explain periodic enhancement of sediment resuspension in the area, and an associated southward transport route from the Changjiang River mouth. Introduction The Changjiang Estuary, East China Sea, ranks as a major depositional sink. It receives large quantities of fluvial material which, at a runoff of m 3 /year, amount to t/year (Chen et al. 1988). Z. Wang (&) Æ Z. Chen State Key Laboratory for Estuarine and Coastal Research, East China Normal University, Shanghai, China zhwang@geo.ecnu.edu.cn Tel.: Fax: K. Okamura Seikai National Fisheries Research Institute, 49 Kokubu-Chou, Nagasaki, Japan J. Gao Key Laboratory of Coast & Island Development, Ministry of Education, Nanjing University, Nanjing, China K. Xu Æ H. Koshikawa Æ M. Watanabe National Institute for Environmental Studies, Tsukuba, Japan Semi-diurnal tides dominate the flow in the estuary, which is characterized by a mean tidal range of 2.70 m and a maximum range of 4.62 m. Regular tides occur off the estuary and irregular tides appear at the inner river mouth. Tidal currents move back and forth in the distributaries of the inner estuary, but rotate clockwise off the river mouth (Chen et al. 1988). In the distributaries the ebb tidal current (1.13 m/s) is stronger than the flood tidal current (0.96 m/s). In addition, the ebbing phase lasts longer than the flooding phase (Chen et al. 1988). At a regional scale, littoral and oceanic currents are the other major hydrodynamic forces in the study area. In response to the Coriolis force, littoral currents constantly flow southwards along the Changjiang coast, thereby promoting sediment transport towards the southern East China Sea (Milliman et al. 1985; Chen et al. 1988). The warm Taiwan Current, by contrast, varies seasonally in distance from the Changjiang River mouth, moving northwards all year round and blocking the dispersal of suspended sediment further offshore (Chen et al. 1988). The large amount of suspended sediment contained in freshwater plumes over the salt wedge is largely dispersed offshore south-eastwards of the river mouth (Milliman et al. 1985). The plumes seldom extend beyond the estuarine front, which usually lies at about E (Chen et al. 1999; Shen and Pan 2001). This is also the seaward margin of the modern Changjiang subaqueous delta (Chen et al. 2000, 2003). Over the last two decades, numerous studies have investigated tidal processes and associated sediment transport in this large river mouth (cf. Milliman and Jin 1985; Chen et al. 1988; Yang and Sun 1988; Shen et al. 1993; Shi et al. 1997; Li and Zhang 1998; Chen et al. 1999; Shi et al. 1999; He et al. 1999, 2001; Shen and Pan 2001; Wu et al. 2001; Chen et al. 2003). These have shown periodic variations of tidal current speed in the area, i.e. high speed around mid-tide (maximum flood and ebb) and low speed at high and low tide (slack flood and slack ebb tide; Chen et al. 1988; Shen and Pan 2001). Earlier work also revealed factor 2 to 4 increases in sediment resuspension, caused by various mechanisms including
2 253 tidal current and estuarine front processes over a tidal cycle in and off the turbidity maximum (TM) zone of the Changjiang Estuary (Shen and Pan 2001). Thus, resuspension plays a critical role in eroding the estuarine seafloor, enhancing the TM zone and re-circulating nutrients (Li and Zhang 1998; Chen et al. 2000; Shen and Pan 2001). The present study focuses on an anomalous current occurring at lower low water, with highest current speeds at the estuarine front off the Changjiang River mouth. Indeed, a literature search has revealed that this phenomenon and the associated sediment transport pattern have not been adequately investigated in the study area to date. Materials and methods On May 2001, a hydrographic and sedimentological investigation was conducted near and off the Changjiang River mouth ( E, N; Fig. 1). Eight sites, spanning >150 km in total at water depths of ca m, were chosen to examine tidal current characteristics and sediment dispersal patterns (sites A2, B1, B2, B3, C1, C3, C4 and C5; Fig. 1). Water depths are approximately 10 m at sites A2 and B1, 14 m at site B2, 24 m at site B3, 40 m at site C1, 36 m at site C3, and m at sites C4 and C5 (Fig. 1). Note that these are mean water depth values, because water depths vary as a result of tidal influences, particularly at shallow sites. Tidal current speed/direction, suspended sediment concentration (SSC) and turbidity were measured simultaneously at maximum ebb at sites B1, B3, C1, C3 and C5, at lower low water at sites A2 and C4, and over two tidal cycles for 26 h at site B2. Current speed and direction were measured with a direct-reading current meter (SLC-9) at depth intervals of 0.5 m at all sites. Current speed/direction were measured every hour from 06:00 on 25 May to 06:00 on 26 May at site B2, and only once throughout the whole water column at the other sites. Current speed/direction were also measured continuously over 26 h on May at site B2, with a COMPACT-EM current meter at a water depth of 7 m. A Chlorotech nephelometer (ACL208-RS) was used to measure turbidity at site B2, at water depth intervals of 0.1 m every 3 h from 06:00 to 21:00 on 25 May In all, 93 water samples (500 ml/sample) were collected for SSC measurements at all sites. The water samples were taken every hour for 25 h (on May) in surface (0.5 m below sea surface), mid-depth (6 8 m depth), and bottom (1 m above seafloor) waters at site B2 (water depth ranging from 12 to 16 m due to tidal influence). Water samples were taken at water depths of 0.5, 5, 15 m and at the bottom at sites C1 (depth 40 m, 23 May) and C3 (depth 35.5 m, 22 May), and at an additional water depth of 20 m at sites C4 (depth 35 m, 21 May) and C5 (depth 40 m, 21 May). The water samples were filtered through pre-weighed 0.45-lm Nucleopore filters, which were then oven-dried at 40 C in the laboratory. The dried filters were weighed individually for calculation of SSC (g/l). Results Anomalous current at lower low water Measurements of the irregular semi-diurnal tides at site B2 indicate that the tidal range at night was larger than that during the daytime between 25 and 26 May Fig. 1 Geographic locality map of the study area and the locations of the measuring sites off the Changjiang River mouth (depth contours in metres). TM Turbidity maximum
3 (Fig. 2a). Lower low water occurred at about 18:00 on 25 May, and higher high water at about midnight (Fig. 2a). Maximum flood appeared at 10:00 and 21:00 on 25 May, and maximum ebb at 15:00 on 25 May and 04:00 on 26 May. At site B2, maximum flood current speed ranged from 0.9 to 1.3 m/s, and maximum ebb current speed from 1.2 to 1.5 m/s (Fig. 2a). An anomalous high-speed current ( m/s) occurred at lower low water and lasted almost 4 h at a water depth of 7 m. The directreading current meter showed that current speed generally exceeded 0.9 m/s throughout the whole water column at lower low water, the maximum value reaching >1.3 m/s in the mid-depth water layer (3 10 m; Fig. 2b). These high values at lower low water at site B2 are even greater than that recorded at maximum ebb at site B1 (ca m/s), and close to that observed at lower low water at site A2 (Fig. 2c). A high-speed current at lower low water occurred also at site C4, where the values exceeded 0.6 m/s throughout the whole water column, the maximum value being >1.0 m/s at 8 13 m (Fig. 2d). These current speeds are even faster than those recorded at maximum ebb at the other sites (B3, C1, C3 and C5; Fig. 2d). The current speed profile recorded over 26 h at site B2 was subdivided into W E and N S profiles (Fig. 3a, b). Tidal current speed and direction agreed well with a full tidal fluctuation over 12 h. Maximum flood headed west, whereas maximum ebb headed east (Fig. 3a, b). For each profile, high and low water showed mainly north and south directions respectively. The high-speed current at lower low water at site B2 was mainly directed southwards at a depth of 7 m, and also throughout the vertical current speed profile (Fig. 3b d). A similar pattern was recorded at site C4, where the high-speed current at lower low water flowed southwards below a water depth of 5 m when the surface current headed west owing to the onset of the flooding tide (Fig. 3e, f). Suspended sediment concentrations At site B2, a much higher SSC was recorded in the bottom water layer ( g/l; Fig. 4a) than in the middepth and surface layers (<0.10 g/l) at low water (06:00 07:00 on 25 May and 06:00 on 26 May), lower low water (18:00), and high water (11:00 12:00 and 24:00). Shortly before and after lower low water (16:00 17:00; 20:00 21:00), SSCs reached g/l. At all depths, the SSC values at lower low water were 2 10 times as high as those documented during the other tidal phases. At lower low water at site B2, turbidity measurements showed essentially the same pattern as the one recorded for SSC higher turbidity (>230 ppm) in the bottom water, and substantially lower values ( ppm) in the mid-depth and surface waters (Fig. 4b). This finding contrasts with that observed at low water at site B2, showing a similarly high turbidity (>230 ppm) at the bottom but much higher values (>170 ppm) in the mid-depth and surface waters compared to those recorded at lower low water. The SSC depth distribution at lower low water at site C4 was similar to that at site B2. Surface SSC at site C4 was low (0.011 g/l; Table 1), approximating the values measured at maximum ebb at sites C1, C3 and C5 ( g/l; Table 1). SSCs increased strongly from surface and mid-depth waters to bottom waters (0.043 g/ l) at site C4, reaching higher values (factors ) than those recorded in the bottom waters of sites C1, C3 and C5. Discussion and conclusions The results of the present study convincingly demonstrate that, although of brief duration (4 h), the anomalous high-speed current recorded at lower low water in the Changjiang Estuary was important in controlling sediment resuspension, especially in the area of the TM zone in the river mouth (cf. Chen et al. 1988; Shi et al. 1997; Li and Zhang 1998; Shen and Pan 2001; Chen et al. 2003). Less clear, by contrast, are the factors controlling this event. Shen and Pan (2001) reported that the tidal current reaches fastest speeds 2 h before and after low tide, and slackens at high and low tide within the Changjiang Estuary. Off the estuary, by contrast, the tidal current is fastest at high and low tide, and slackens at mid-tide. The time-series data of current distribution documented in the present study at the nearshore site B2 likely result from the superimposition of these two types of tidal currents in and off the Changjiang Estuary. Another possible explanation for the formation of the anomalously fast current could be the sharp density gradient caused by marked changes in salinity and temperature in estuarine fronts, and the Yellow Sea longshore currents constantly heading south from the northern Changjiang coast (Chen et al. 2000). Thus, we contend that the anomalous current off the Changjiang River mouth is probably induced by complex interactions between a number of different physical factors. The high SSC and high turbidity recorded in the bottom water layers off the river mouth during lower low water were closely associated with the occurrence of the high-speed current which could have caused resuspension of bottom sediments. Previous studies have demonstrated that resuspension enhances largely bottom SSC (up to 2 3 g/l), particularly during the winter season, thereby intensifying the TM zone through which fluvial materials are filtered, to subsequently be driven further seawards off the Changjiang Estuary (Shi et al. 1997; Li and Zhang 1998; Shen and Pan 2001). A threshold current speed of m/s (vertical averaged current speed) has been documented in the study area by Li and Zhang (1998). The present study, by contrast, reveals bottom current speeds at lower low water
4 Fig. 2a Twenty-six-hour tidal current speed curve at site B2 on May 2001 (inset indicates tidal levels). 1, 3 Maximum flood, 2, 4 maximum ebb, HW high water, HHW higher high water, LW low water, LLW lower low water. b Temporal variation of vertical current speed at site B2 on May c Anomalous current recorded on 25 and 27 May 2001 at lower low water at sites B2 and A2, compared with the current speed on 26 May 2001 at maximum ebb at site B1. d Anomalous current recorded on 21 May 2001 at lower low water at site C4, compared with the current speed on May 2001 at maximum ebb at sites C5, C3, C1 and B3 (see Fig. 1 for site locations) 255
5 256 Fig. 3a Twenty-six-hour W E current speed curve at site B2 on May b Twenty-six-hour N S current speed curve at site B2 on May c W E depth distribution of vertical current speed at lower low water at site B2 on 25 May d N S depth distribution of vertical current speed at lower low water at site B2 on 25 May e W E depth distribution of vertical current speed at lower low water at site C4 on 21 May f N S depth distribution of vertical current speed at lower low water at site C4 on 21 May W-E-oriented current speeds are indicated by U and N-S-oriented current speeds by V (see Fig. 1 for site locations) reaching m/s at the nearshore site B2, and m/s at the offshore site C4 whereas the values were only m/s at maximum ebb at the other offshore sites C1, C3 and C5. Correspondingly, SSCs in bottom water layers at lower low water at sites B2 and C4 were substantially higher than those at maximum ebb at sites C1, C3 and C5. Presumably, the anomalous current at lower low water serves as a significant mechanism in reworking the seafloor. Chen et al. (2003) reported that highly lami-
6 257 Fig. 4a Temporal variations in SSC in surface, mid-depth and bottom (1 m above seafloor) waters on May 2001 at site B2. b Vertical distribution of turbidity at low water (06:00) and lower low water (18:00) on 25 May 2001 at site B2. LW Low water, LLW lower low water, HW high water (see Fig. 1 for site locations) nated sediments periodically interbedded with scouring surfaces prevail in the modern Changjiang pro-delta facies (between E and E), indicating strongly reactivated sedimentation resulting from highspeed sub-bottom tidal current processes. This is consistent with the findings of Sternberg et al. (1985) who witnessed that the threshold of grain motion is exceeded in 65% of all tidal cycles in the region, and that bedload transport is the dominant mode of grain movement, owing to the dominant bottom velocity of tidal currents on the continental shelf of the East China Sea. In addition, the high-speed current documented in the present study may weaken flocculation prevailing in the estuary during lower low water, as suggested by the low SSC and low turbidity recorded in mid-depth and surface waters. Current knowledge of sediment dispersal patterns in and off the Changjiang River mouth, where water depth ranges from 10 to 60 m, is relatively limited. The anomalous current at lower low water investigated here reveals not only active sediment dynamics in association with resuspension, but also a southward sediment transport route. This highlights the need to adequately Table 1 Suspended sediment concentration (SSC) at sites C1, C3, C4 and C5 off the Changjiang River mouth. At sites C1, C3 and C5, SSCs were measured at maximum ebb in the period May The high SSC value at site C4 (italics) at the seafloor was recorded at lower low water on 21 May 2001 Site Water depth SSC (m) (g/l) C Bottom water C Bottom water C Bottom water C Bottom water 0.023
7 258 estimate fine-grained sediment flux from the Changjiang Estuary offshore, as well as erosion/sedimentation rates in the estuary. Such information would be vital for geoengineering projects in the area, especially after completion of the so-called three-gorges dam project in 2009 (Chen et al. 2001). In conclusion, the anomalous high-speed current identified at lower low water is evidently a critical hydrodynamic phenomenon near and off the Changjiang River mouth. Despite its short duration, this event probably plays a prominent role in resuspending estuarine seafloor deposits and in rerouting sediment dispersal from the TM zone offshore. More field observations are needed to further examine the characteristics of this anomalous current, as well as associated processes such as sediment resuspension and dispersal. Acknowledgements Our appreciation goes to Professors Z. Shi, M. Byrnes and R. Kostaschuk for their critical reviews and useful comments. We are grateful to D.C. Chen, T.Y. Wei, H.S. Yao, Y.W. Zhao and L.Q. Li for their painstaking sampling during the investigation. The Shanghai No. 1 Marine Geological Team conducted the sea cruise. This study was supported by the China National Natural Science Foundation (grant no ), APN/ START (grant no ), the Shanghai Priority Academic Discipline, and the Global Environment Research Fund of the Ministry of the Environment, Japan. References Chen JY, Shen HT, Yun CX (1988) Dynamic processes and morphological evolution of the Changjiang estuary (in Chinese). Shanghai Science and Technology Press Chen JY, Li DJ, Chen BL, Hu FX, Zhu HF, Liu CZ (1999) The processes of dynamic sedimentation in the Changjiang Estuary. J Sea Res 41: Chen Z, Song BP, Wang ZH, Cai YL (2000) Late Quaternary evolution of the sub-aqueous Yangtze Delta, China: sedimentation, stratigraphy, palynology, and deformation. Mar Geol 162: Chen Z, Li J, Shen H, Wang Z (2001) Yangtze River of China: historical analysis of discharge variability and sediment flux. Geomorphology 41:77 91 Chen Z, Saito Y, Hori K, Zhao YW, Kitamura A (2003) Early Holocene mud-ridge formation in the Yangtze offshore, China: a tidal controlled estuarine pattern and sea-level implications. Mar Geol 198: He Q, Yun CX, Shi WR (1999) Remote sensing analysis of surface suspended sediment concentration in the Changjiang estuary. Prog Nat Sci 9(6): He Q, Li JF, Li Y, Jin XS, Che Y (2001) Field measurements of bottom boundary layer processes and sediment resuspension in the Changjiang estuary. Sci China Ser B 44 (Suppl):80 86 Li J, Zhang C (1998) Sediment resuspension and implications for turbidity maximum in the Changjiang estuary. Mar Geol 148: Milliman JD, Jin QM (eds) (1985) Sediment dynamics of the Changjiang estuary and the adjacent east China sea. Cont Shelf Res 4(1/2):1 251 Milliman JD, Shen HT, Yang ZS, Meade RH (1985) Transport and deposition of river sediment in the Changjiang estuary and adjacent continental shelf. Cont Shelf Res 4(1/2):37 45 Shen HT, Pan D (2001) Turbidity maximum in the Changjiang estuary (in Chinese). China Ocean Press, Beijing Shen HT, Li JF, Zhu HF, Han MB, Zhou FG (1993) Transport of the suspended sediment in the Changjiang estuary. Int J Sediment Res 7(3):45 63 Shi Z, Ren LF, Zhang SY, Chen JY (1997) Acoustic imaging of cohesive sediment resuspension and re-entrainment in the Changjiang Estuary, East China Sea. Geo-Mar Lett 17(2): Shi Z, Ren LF, Hamilton LJ (1999) Acoustic profiling of fine suspension concentration in the Changjiang estuary. Estuaries 22(3A): Sternberg RW, Larsen LH, Miao YT (1985) Tidally driven sediment transport on the East China Sea continental shelf. Cont Shelf Res 4(1/2): Wu JX, Shen HT, Xiao CY (2001) Sediment classification and estimation of suspended sediment fluxes in the Changjiang estuary, China. Water Resource Res 37(7): Yang CS, Sun JS (1988) Tidal sand ridges on the East China Sea shelf. In: de Boer PL, van Gelder A, Nio SD (eds) Tidalinfluenced sedimentary environments and facies. D Reidel, Dordrecht, pp 23 38
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