Approaching Tahlee

We walked through fields that had been cleared by convicts one hundred and eighty years ago ……. now it’s a forest again!

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Tide and the Salt Marsh (for the technical)

This study was conducted by Gareth Davies from the University of Wollongong. He has given us permission to publish.

Vignettes > Flow in a microtidal channel during within-bank and over-bank tides: Yalimbah Creek, South Eastern Australia.

Flow in a microtidal channel during within-bank and over-bank tides: Yalimbah Creek, South Eastern Australia.

Gareth Davies
University of Wollongong

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Continent: Australia
Country: Australia
State/Province:New South Wales
City/Town: Karuah
UTM coordinates and datum: none


Climate Setting: Humid
Tectonic setting: Passive Margin
Type: Process, Computation

Location map of Yalimbah Creek. a) The location of Yalimbah Creek (black box) in Port Stephens, Australia. b) Map of Yalimbah Creek, with major landform categories and measurement sites. Coordinates are in UTM Zone 56H. Created by the author of the page containing this file. Details
Three intertidal environments of increasing elevation. a) Number One cove, which is usually completely inundated except during very low tides. b) Mangrove forest in the lower elevation vegetated intertidal regions. c) Mixed mangrove and salt marsh in an upstream, higher elevation intertidal area. Created by the author of the page containing this file. Details
Time series of water levels and velocities at the ‘velocity measurement’ site depicted in Figure 1b). The horizontal line in the water level time series approximately divides within-bank and overbank tides at this site. Notice how the velocity peaks are much higher during overbank tides than within-bank tides. Details
A comparison of the measured and predicted water velocities at the ‘velocity measurement’ site (Figure 1b), using Equation 1. The water level data used for prediction was measured near the seaward edge of the channel (Figure 1b). The first day of velocity and stage data was used to estimate F(h), using linear regression. F(h) was estimated as a third order polynomial, because increasing the order of the polynomial did not significantly change the predictions. Created by the author of the page containing this file. Details


The study of tidal hydrodynamics plays an important role in geomorphic studies of tidal channels. While the hydrodynamic properties of the landform are largely controlled by its morphology, these flows also drive sediment transport in the creek and its intertidal flats. They thus have a major influence on the evolution of the landform. This vignette will examine a velocity time series from a tidal channel, and consider the extent to which a simple model, based on the conservation of water mass, can explain the observations.

Yalimbah Creek is a microtidal channel (tidal range usually < 2 m), situated in the north western corner of Port Stephens, a large natural harbour in South Eastern Australia (Figure 1a). The channel is largely sheltered from wave processes, and its small catchment has no inflowing river channel. For most of its length, the channel meanders through a narrow valley filled with intertidal marsh (Figures 1b, 2b,2c), the elevation of which gradually decreases downstream. At its most downstream end, the channel flows into an unvegetated intertidal cove (Number One cove, Figure 1b, 2a), where it gradually shallows until it is no longer clearly distinct from the rest of the cove. The channel is formed largely in unconsolidated muddy sediments, consisting of organic rich silt and clay, with some fine and very fine sand. In many places it is also partly bound by bedrock.

Vegetated intertidal flats are known to exert a strong influence on tidal channel hydrodynamics (e.g. Wolanski et al., 1980; Lessa and Masselink, 1995). As the tide overtops the channel banks, the flats are flooded, and the volume of water stored in the channel/flats system increases rapidly with tidal stage. The flow velocities on the flats tend to be much lower than in the channel, because the former have smaller depths and a greater hydrodynamic drag (induced by vegetation) (Wolanski et al., 1980; Furukawa, 1997). Hence, most water in the channel/flats system is transported via the channel. During overbank tides, velocities in the channel must increase in order to transport these larger volumes of water.

These ‘mass conservation’ type effects are complicated by ‘momentum conservation’ effects. When the intertidal flats are inundated, the propagating tidal wave is also slowed and deformed (Aucan and Ridd, 2000; Fortunato and Oliveira, 2005). This can produce temporarily high water surface slopes (i.e. spatial differences in water levels), both along the channel and between the channel and the flats. These water surface slopes can induce strong accelerations in flow velocities.

Figure 3 shows a water level and velocity time series from a site in Yalimbah Creek, collected in October 2008 (Figure 1b). Notice how the peak velocities are much higher during overbank tides than within bank tides. We will now develop a crude model of this data set, based only on mass conservation considerations.

To do this, assume that: 1) the water surface elevation in the channel/flat system is constant in space; 2) that the flats receive all their water from nearby parts of the channel, and 3) that there is no inflowing fluvial discharge. Although these assumptions are a strong simplification of reality in many situations, they lead to simple calculations, and are accurate in some situations (see below).

At any cross-section in the creek, the discharge in the channel Q_c must be equal to the rate of change in water volume upstream (dVol/dt). Thus,
Q_c= dVol/dt = (dVol/dh)*(dh/dt)
where the last step follows from the ‘chain rule’ for differentiation. Because the average velocity at this site in the creek is v_c = Q_c/A_c (where A_c is the channel cross-sectional area), it follows that:
v_c = [ (dVol/dh) / A_c ]*(dh/dt) = F(h)*dh/dt
where F(h) = [(dVol/dh) / A_c]. The assumptions mean that F(h) is purely a function of h (and the location of the cross-section). Qualitatively, this equation says that the velocity in the creek can be predicted purely from a water elevation time series, by estimating dh/dt (the rate of change of the water level), and F(h). Although the latter is unknown, it can potentially be estimated with morphological data, or statistically as a high order polynomial of h (using a time series of water levels, and velocity at the site).

Does this work for Yalimbah Creek? Figure 4 shows the predicted and measured water velocities over a few tides at the ‘velocity measurement’ site in Figure 1b, using water level data from a site in Number One cove (Figure 1b). The model does a decent job of predicting the velocities during smaller, within channel tides. It also qualitatively predicts the velocity peaks during overbank tides. However, it incorrectly estimates the magnitude of the flood velocity peaks, and the final ebb velocity peak. It also poorly estimates the timing of the ebb velocity peaks.

These results are consistent with the hydrodynamic theory reviewed above. During within channel tides, water slope effects are relatively slight, and so the ‘flat water surface’ model does a good job at predicting the within channel velocities. During overbank tides, the model is able to qualitatively fit the velocity peaks as the flow goes overbank. However, momentum effects make the simple ‘flat water surface’ approximation rather crude at this time, and the velocity is not simply a function of h and dh/dt at the mouth. Thus, the results are not as good. Another likely source of error is the assumption that the measured velocity time series reflects the mean within-channel velocity. In reality, variations in velocity over the cross-section mean that this will not always be a good approximation.

However, continuity-based models have the advantage of simplicity. They can also be extended to two dimensional flows (Fagherazzi, 2002; Fagherazzi et al., 2003). Results from the latter studies also suggest that they perform well in some situations. However, it is important to realise that some basic features of tidal hydrodynamics cannot be explained while ignoring flow momentum conservation. This includes the asymmetry of tidal currents. While much is known about such processes, to understand them you will need to consider the principles of momentum conservation, as well as mass conservation.


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Estuarine Shore Crabs


Find out about them here! Click above.

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The Road to Tahlee

The first part of the road to Tahlee was made up of raised stony road. The rock had been quarried from the hillside and used to raise the road above the level of the saltmarsh. This was the most overgrown part of the road and finished at what children of half a century before called “the black swamp”.

Today it was still a bit swampy, but it didn’t scare anyone!

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Crossing the Creek

For 130 years there was a bridge here. It was burned down about 50 years ago. So this was the first time since then that such a party had crossed here!

We could only do it with the help of our gallant skipper Gordon Latimore who brought his punt up the creek just to be our ferryman.

It was abit tricky, but one of the highlights of the trip!

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The Yalimbah Creek Salt Marsh

The Old AACo Road crosses a fragile salt marsh which is sometimes partially covered by tidal water. The road here is made up of timber slabs, rock and corduroy – branches laid across the road. At high tide, it’s a bit muddy (but fun!). Beside the road live lots of interesting things.

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Into the trees

From The Karuah Bridge to the start of the salt marsh at Yalimbah Creek is about one and a half kilometres of flat road under a forest canopy.

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Across the River

On Sunday 7th November, a little after noon, a very strong tide was running out. The tide had been very high and had peaked about one and a half hours previously. Now it was running out fiercely and frothing as it raced against the wind. The movement made for interesting pictures

The River in Action
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Sir Edward Parry

Sir Edward Parry

Sir Edward Parry


Sir Edward Parry was a noted polar explorer and for fifty years was the leader of an expedition that reached closer to the north pole than any other. His time as Commissioner of the Australian Agricultural Company saw him travel through Karuah (then Sawyers Point) on many occasions both by boat and by horseback.

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