Why is there a sandwave and why is it not there all the time?
Shortcut URL: https://serc.carleton.edu/36033
Location
Continent: Australia
Country: Australia
State/Province:NSW
City/Town:
UTM coordinates and datum: none
Setting
Climate Setting:
Tectonic setting:
Type: Process
Figure 1: Aerial photo from 2006 showing the northern shoreline of Port Stephens (NSW, Australia). Details
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Description
It is widely known that beaches erode because of the effect of storms. However, this is not always the case; this vignette presents an area that seems to grow the most when affected by severe storms. For this vignette, we are using the term sandwave to refer to a shoreline-attached sandwave which is a sandy protrusion of the shoreline as shown in Figure 1. We are showing the decadal and monthly evolution of a shoreline-attached sandwave that appears in the study area, migrates and disappears again, and that also undergoes accumulation under severe storms.
Port Stephens (NSW, Australia) is a ria-like drowned river valley estuary that is located 230 km north of Sydney (NSW, Australia). Its northern shoreline (Figure 1) is a highly dynamic environment that includes Jimmy's beach and Winda Woppa peninsula, both of them form a sand spit that deflects the mouth of the Myall River and forms its southern boundary [for more information see the other vignette by the same author]. Further eastwards there is a shoreline-attached sandwave, a dynamic morphologic feature that modifies the morphodynamics of the surrounding beach. Features of this scale have been described in several coastal settings and have been given different names, the presence of sandwaves in estuarine environments has been described in the literature but the mechanisms related to their formation and evolution remain mostly unknown.
The evolution of the sandwave during past decades can be assessed using georectified aerial photos in a Geographic Information Systems (GIS). Figure 2 shows aerial photos of the area where the sandwave (if present) is located in 1968, 1986, 1993 and 2006; measurements of the sandwave taken in April 2008 using a Real Time Kinematic Global Navigation Satellite System (RTK-GNSS) are also represented on the 2006 photo. It can be seen how the sandwave was absent in 1968 and how sediment seem to be transported to the NW in 1986; a sandwave is present in 1993, 2006 and 2008.
Before going any further we should introduce some of the forcing mechanisms that control the geomorphologic evolution of the area:
- Port Stephens is a tide-dominated estuary which is located in a wave dominated coast. It has an entrance that is 1.24 km wide and a deep well defined channel (tide-dominated). Due to its location on a wave-dominated coast, and the fact that the entrance is quite wide, it is possible for waves to propagate inside the estuary.
- The wave climate is moderate with mean significant wave heights (Hs) of 1.5 m and 8 s wave period (T). Waves from the NE dominate during summer and E-SE waves are prevalent for the rest of the year; although SE storms may occur at any time of the year, they are more frequent between April and September.
- Tides in the area are semidiurnal (two high-low tidal cycles per day) and microtidal (tidal range is less than 2 m) with mean tidal ranges of 1.6 m and 1.3 m for spring and neap tides respectively.
To assess the decadal evolution of the sandwave we can use a Geographic Information System (GIS). This enables us to then measure the instantaneous shorelines (i.e., the contact between the sand and the water) to represent the sandwave (Figure 3). We can also determine across-shore transects to measure shoreline progradation and retreat in relation to an arbitrary line (Figure 3). The sandwave underwent overall accumulation between 1968 and 1986. Between 1986 and 1993 there was erosion on both ends of the sandwave and accumulation on its central part (transects 4 to7). There was again overall accumulation between 1993 and 2001. The periods between 2001-06 and 2006-08 were characterised by opposite behaviour, there was accumulation on the external transects (T1 to T4) and erosion on the remaining transects during the first period; followed by erosion in T1-T4 with accumulation in the remaining of the sandwave in the second period (Figure 3).
To better understand the morphodynamics of the sandwave, we have been measuring it since March 2007 using standard surveying techniques such as total station and RTK-GNSS. The period was characterised by a cluster of storms occurring during June and July, in the Austral winter of 2007 (significant wave heights, Hs, were from 3.5 m to greater than 6 m). During the rest of the study period there were several low-energy high frequency storms (Hs between 3 and 3.5 m). The largest erosion of the sandwave occurred during these low-energy high frequency storms. On the other hand, during the severe storms of June-July 2007, the sandwave underwent an overall sediment accumulation (Figure 4).
The analyses of the decadal evolution agree with previous studies by Cholinski (2004) and suggest that the sandwave was first recorded in the 1980s and that there was a period up until the mid 1990s where westward sediment transport caused sandwave formation and migration towards the inner parts of the estuary. Since then, the sandwave migration slowed down, remaining relatively stable with some further migration between 2006 and 2008. Short term studies suggest that sandwave accretion episodes occur under severe SE storms.
There are still too many unknowns with respect to the evolution and behaviour of the sandwave. Several sandwaves were identified since 1980s but none between 1968 and 1981. On the other hand, cartography of Port Stephens, drawn during the visit of the Beagle in 1835-36, clearly shows a protrusion in the location where the sandwave exists at present; this only adds more questions to the puzzle: why is there a sandwave and why is it not there all the time?
Port Stephens (NSW, Australia) is a ria-like drowned river valley estuary that is located 230 km north of Sydney (NSW, Australia). Its northern shoreline (Figure 1) is a highly dynamic environment that includes Jimmy's beach and Winda Woppa peninsula, both of them form a sand spit that deflects the mouth of the Myall River and forms its southern boundary [for more information see the other vignette by the same author]. Further eastwards there is a shoreline-attached sandwave, a dynamic morphologic feature that modifies the morphodynamics of the surrounding beach. Features of this scale have been described in several coastal settings and have been given different names, the presence of sandwaves in estuarine environments has been described in the literature but the mechanisms related to their formation and evolution remain mostly unknown.
The evolution of the sandwave during past decades can be assessed using georectified aerial photos in a Geographic Information Systems (GIS). Figure 2 shows aerial photos of the area where the sandwave (if present) is located in 1968, 1986, 1993 and 2006; measurements of the sandwave taken in April 2008 using a Real Time Kinematic Global Navigation Satellite System (RTK-GNSS) are also represented on the 2006 photo. It can be seen how the sandwave was absent in 1968 and how sediment seem to be transported to the NW in 1986; a sandwave is present in 1993, 2006 and 2008.
Before going any further we should introduce some of the forcing mechanisms that control the geomorphologic evolution of the area:
- Port Stephens is a tide-dominated estuary which is located in a wave dominated coast. It has an entrance that is 1.24 km wide and a deep well defined channel (tide-dominated). Due to its location on a wave-dominated coast, and the fact that the entrance is quite wide, it is possible for waves to propagate inside the estuary.
- The wave climate is moderate with mean significant wave heights (Hs) of 1.5 m and 8 s wave period (T). Waves from the NE dominate during summer and E-SE waves are prevalent for the rest of the year; although SE storms may occur at any time of the year, they are more frequent between April and September.
- Tides in the area are semidiurnal (two high-low tidal cycles per day) and microtidal (tidal range is less than 2 m) with mean tidal ranges of 1.6 m and 1.3 m for spring and neap tides respectively.
To assess the decadal evolution of the sandwave we can use a Geographic Information System (GIS). This enables us to then measure the instantaneous shorelines (i.e., the contact between the sand and the water) to represent the sandwave (Figure 3). We can also determine across-shore transects to measure shoreline progradation and retreat in relation to an arbitrary line (Figure 3). The sandwave underwent overall accumulation between 1968 and 1986. Between 1986 and 1993 there was erosion on both ends of the sandwave and accumulation on its central part (transects 4 to7). There was again overall accumulation between 1993 and 2001. The periods between 2001-06 and 2006-08 were characterised by opposite behaviour, there was accumulation on the external transects (T1 to T4) and erosion on the remaining transects during the first period; followed by erosion in T1-T4 with accumulation in the remaining of the sandwave in the second period (Figure 3).
To better understand the morphodynamics of the sandwave, we have been measuring it since March 2007 using standard surveying techniques such as total station and RTK-GNSS. The period was characterised by a cluster of storms occurring during June and July, in the Austral winter of 2007 (significant wave heights, Hs, were from 3.5 m to greater than 6 m). During the rest of the study period there were several low-energy high frequency storms (Hs between 3 and 3.5 m). The largest erosion of the sandwave occurred during these low-energy high frequency storms. On the other hand, during the severe storms of June-July 2007, the sandwave underwent an overall sediment accumulation (Figure 4).
The analyses of the decadal evolution agree with previous studies by Cholinski (2004) and suggest that the sandwave was first recorded in the 1980s and that there was a period up until the mid 1990s where westward sediment transport caused sandwave formation and migration towards the inner parts of the estuary. Since then, the sandwave migration slowed down, remaining relatively stable with some further migration between 2006 and 2008. Short term studies suggest that sandwave accretion episodes occur under severe SE storms.
There are still too many unknowns with respect to the evolution and behaviour of the sandwave. Several sandwaves were identified since 1980s but none between 1968 and 1981. On the other hand, cartography of Port Stephens, drawn during the visit of the Beagle in 1835-36, clearly shows a protrusion in the location where the sandwave exists at present; this only adds more questions to the puzzle: why is there a sandwave and why is it not there all the time?
Associated References
- Cholinski, M.P., 2004. Sandwave Morphodynamics at Port Stephens, N.S.W. Honours Thesis, University of Sydney, Sydney, Australia, 150 pp.
- Short, A.D., 1985. Rip-current type, spacing and persistence, Narrabeen Beach, Australia. Marine Geology, 65(1-2): 47-71.
- Short, A.D. and Trenaman, N.L., 1992. Wave climate of the Sydney region, an energetic and highly variable ocean wave regime. Australian Journal of Marine and Freshwater Research, 43: 765-791.
- Thom, B.G., Sheperd, M., Ly, C.K., Roy, P.S., Bowman, G.M. and Hesp, P.A., 1992. Coastal geomorphology and quaternary geology of the Port Stephens-Myall Lakes area. Dept. of Biogeography and Geomorphology, Australian National University, Canberra, 407 pp.
- Vila-Concejo, A., Short, A.D., Hughes, M.G. and Ranasinghe, R., 2007. Shoreline implications of flood-tide delta morphodynamics. The case of Port Stephens (SE Australia). Coastal Sediments. ASCE, New Orleans, pp. 1417-1430.
- Vila-Concejo, A., Short, A.D., Hughes, M.G. and Ranasinghe, R., 2009. Formation and evolution of a sandwave on an estuarine beach. Journal of Coastal Research, SI 56: 153-157. http://www.geosci.usyd.edu.au/research/re_portstephens.shtml