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Posted 13 March 2008
Figure 1. Inferred groundwater flow from bedrock to alluvium (Broughton 1994). There are currently very few groundwater monitoring bores in bedrock so hydraulic connections are uncertain.
Dr Wendy Timms
Consultant Senior Engineer-Scientist, UNSW Water Research Laboratory
Professor Ian Acworth
Gary Johnston Chair of Water Management at UNSW
Wendy Timms was an Independent Expert to the Caroona Coal Community Consultative Committee appointed for the Exploration Phase.
Recent WRL reviews and recommendations on groundwater aspects of coal exploration in the area have been made available by the Committee at: http://www.caroonacoalccc.com.au
For example, WRL Technical Report 2007/07 (presented to the committee in April 2007) provides 9 recommendations for the proposed groundwater investigations and monitoring for the exploration phase. The recommendations can be read in full in this report download (http://www.caroonacoalccc.com.au/client_images/357367.pdf). The responses by BHP Billiton and their consultants to the Independent reviews are also available on the website.
Aquifers used for irrigation are frequently embedded in clay rich sediments known as aquitards. These aquitards are low permeability units that dominate the large volume of alluvial sediments on the Liverpool Plains. Aquitards can act as a 'barrier' to groundwater flow.
Understanding aquifers and aquitards typically requires 'muddy' investigation work in the paddock in addition to desk top or computer studies. Investigations can be relatively expensive because of the need to drill test holes. Investigation 'tools' used by the Water Research Laboratory include state-of-the-art geophysical logging techniques, aquifer hydraulic testing, geotechnical and chemical analysis of sediment cores, intensive automated monitoring of groundwater levels and water quality studies. Realistic computer models of flow and contaminant transport are then developed to assess various management scenarios.
A combination of these investigative tools have been applied as required at sites around the Caroona area including Claremont, Yarramanbah, Hudson, Connamara, Pullaming, Breeza, Native Dog Gully and at several spring sites west and south of Lake Goran.
Understanding of local groundwater processes commenced with work by George Gates (1980) and progressed during the early 1990s through a number of catchment 'snapshot' studies: Broughton (1994); the Liverpool Plains Water Quality Project (Timms 1997; Mawhinney 1998); Lavitt (1998); Coram (1999); the CSIRO team (Stauffacher et al. 1997; Dawes et al. 2000). In the last 10 years, work by Acworth and Timms at the UNSW Water Research Laboratory has further progressed our understanding and has been of international interest.
The work by WRL has shown that aquitards play a hitherto unappreciated role in the groundwater system.
Alluvial sediments include both clays (aquitards) and sands and gravels (aquifers) and mixed sediments. High yielding aquifers in the Liverpool Plains are found in sand and gravel lenses. These lenses can be thought of as old river beds that weave their way through finer grained mud deposits. They are therefore variable in thickness and prone to rapidly change direction. This conceptual model is in contrast to the rather simple layer or blanket type aquifer deposits often incorporated in groundwater models. The Gunnedah Formation is an unofficial geological title sometimes given to the deepest, thickest deposit of gravel and sand.
There are substantial high yield/low salinity aquifers east of the Mooki River at 90m to 130m below the land surface. Recharge of these aquifers is from a combination of diffuse infiltration on the footslopes of the surrounding hills, infiltration from gravel outcrops in stream beds, and from leakage through the clay strata underlying the floodplain.
Groundwater flow is naturally to the north and west, flowing from high pressure to low pressure (usually downhill). In the area of alluvium east of Caroona, flow rates have been estimated to be of the order of 2m to 10m per annum. Flows (and flow rates) are constricted at the Breeza gap, and the high levels of extraction between Breeza and Carroll/Gunnedah have resulted in a reversal of groundwater flow direction in the north of the area, such that groundwater is now believed to flow south from the Namoi. Groundwater age, measured by various isotopes, is of the order of tens of thousands of years. This means that current pumping may be mining the aquifer! Falling groundwater levels are clearly seen at some sites (Fig. 3).
Changes to aquitards can result in increased transmissivity or leakage. Aquitards will leak more when they are:
The leakage through the aquifer can be beneficial to management, for example, if it counteracts rising saline groundwater, but it can also increase the vulnerability of the aquifers to contamination
Weathered basalt slopes and drainage channels are found near the Liverpool Ranges where most recharge occurs to the alluvial aquifers (Fig. 5). However, the hydrogeology of these slopes is very different to sandstone hill slopes. Sandstone hill slopes found at Pine Ridge, Spring Ridge, and near Caroona are not as important to recharge. For example, at one sandstone hill slope, monitoring and investigation found that groundwater levels were lower under the ridge than on the plains and that almost no recharge occurred. Rainfall on the sandstone ridges appears to be lost mainly to evaporation with minor runoff. However, further investigation is needed to confirm this.
Salt has been accumulated in the soil and clay aquitards over tens of thousands of years by wet and dry deposition. Deep clay cores have shown that only about 10% to 20% of total salts is stored in the upper 3m to 6 m depth where it is detected by soil surveys. There is also evidence of saline playa lakes in the sediments, suggesting that Lake Goran may be the remnant of a larger salt lake system. Erosion of these sediments, or release of salts by drying and increased flushing, will have implications for achieving river salinity targets downstream. Proposed mining activity must therefore be planned to minimize or eliminate the release of additional salt to the surface drainage system.
Recent work has caused a re-think of conceptual models describing groundwater flow and discharge in valleys south of Caroona (Timms and Acworth, 2006, 2005). In this case, new field data was used in a computer model of flow and contaminant transport to show that salt has diffused downwards through a 30 m thick aquitard over at least ten thousand years. The very low permeability of clay below the surface cracked and fractured zone, combined with almost no hydraulic gradient means that upward discharge of water is extremely slow with water possibly moving only about 5m in 10,000 years. This means that the clays can effectively become barriers if used appropriately.
The increased weight of moisture in the soil zone causes water pressure changes deep within the compressible clay even though no physical recharge occurred. A small increase of groundwater levels in the gravel aquifer at 50 m depth, confined by the clay aquitard was observed about 70 days after rainfall increased storage weight near the ground surface. Groundwater hydrographs need to be re-examined in the light of this finding because a rise in the hydrograph has previously been taken to imply direct downward movement of groundwater.
Work by UNSW-WRL has shown that salinisation is not due to discharge and evaporative concentration of fresh groundwater from deep aquifers. Instead, the evidence indicates that shallow and deep groundwater systems are often poorly connected (Timms and Acworth, 2005, 2006). Clay-rich sediments must be managed to prevent release of salts that have been deposited and accumulated over geological time.
Knowledge about groundwater can be utilised in forward planning for mine management, mine closure and mine rehabilitation. The geochemical reaction of water (groundwater or rainfall) with mine spoils and rejects can produce contaminants. After mining, salt can be concentrated by evaporation in pit lakes that are left behind. Non-permeable barriers can be constructed to prevent leakage of contaminants through alluvium to rivers and streams. Alternatively, it may be possible to utilize buffer zones of natural clay aquitards as a barrier between mining and rivers or alluvial aquifers.
Based on the extensive research that has been carried out in the past 10 years, we believe that coal mining on the Liverpool Plains will impact on the groundwater system used for irrigation, stock and domestic use if mining is carried out beneath the flat-lying plains. Management strategies on the Liverpool Plains are currently addressing the adverse impacts that irrigation development has had on the groundwater system. If coal mining is to proceed, the additional impacts on groundwater recharge, groundwater levels and water quality will require careful investigation and management.
1. Alluvial aquifers
2. Clay aquitards
3. Water quality in pit lakes & mine voids
The relative size and impacts of proposed mine sites should be considered in the regional context of environmental and socio-economic factors. A transparent process of regulatory checks and approvals together with peer-review by suitably experienced professionals is recommended.
Published by Liverpool Plains Land Management Committee, Plains Talk, June 2006, No. 33
Wendy Timms is currently an Independent Expert to the Caroona Coal Community Consultative Committee appointed. Recent reviews and recommendations on groundwater aspects of coal exploration in the area have been made available by the Committee at:
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