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Variability of Dissolved CO in the Pang and Lambourn Chalk Rivers 2

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Hydrol.J. Griffiths, Earth J. Nutter, Syst. A. Sci., Binley, 11(1), N. Crook,328339 A., Young 2007 and J. Pates www.hydrol-earth-syst-sci.net/11/328/2007 © Author(s) 2007. This work is licensed under a Creative Commons License. Variability of dissolved CO in the Pang and Lambourn Chalk 2 rivers J. Griffiths1, J. Nutter2, A. Binley3, N. Crook4, A. Young1 and J. Pates3 1Centre for Ecology and Hydrology, Wallingford, UK 2Wallingford Hydrological Solutions, Wallingford, UK 3Department of Environmental Science, Lancaster University, UK 4Department of Geophysics, Stanford University. California, USA Email for corresponding author: [email protected] Abstract This paper presents the results of a two-year field campaign to determine the spatial and temporal variability of groundwater interaction with surface waters in two Cretaceous Chalk catchments (the Pang and Lambourn) in the Upper Thames in Berkshire, UK, based on measurement of dissolved carbon dioxide (CO ). Average stream water concentrations of dissolved CO were up to 35 times the concentration at atmospheric 2 2 equilibrium. Mean groundwater concentrations of 85 and 70 times the atmospheric equilibrium were determined from borehole water sampled in the Pang and Lambourn respectively. Diurnal and seasonal variation of in-stream concentration of dissolved CO is not significant enough 2 to mask the signal from groundwater inputs. Keywords: chalk, river, groundwater, alkalinity, pH, carbon dioxide, Pang, Lambourn, LOCAR Introduction at a rate determined by the dimensional characteristics of Analysis of stream and groundwater chemistry has been used the water-body, the amount of disturbance or turbulence in to assess the extent of groundwater interaction with surface the water and external interferences such as wind-speed waters (Neal et al., 1990; Hill and Neal, 1997; James et al., (Genereux and Hemond, 1992; Raymond and Cole, 2001). 2000; Cook et al., 2003; Malcolm et al., 2004; Rodgers et Once at the surface, the concentration of CO in the water 2 al., 2004). Such methods provide relatively quick and may be affected by photosynthetic and respirative processes inexpensive descriptions of the spatial and temporal of biological organisms in surface sediments and in the water distribution of surface-groundwater interactions. For a column. Such processes make the interpretation of surface- naturally occurring substance to be used as an indicator of water CO concentrations for calculation of the rate and 2 groundwater, its concentration in groundwater must be extent of groundwater inputs more difficult (Schurr and relatively consistent over both space and time, as well as Ruchti, 1977; Simonsen and Harremoes, 1978). For significantly different from that of stream water. Initially, measurements of dissolved CO to be useful as reliable 2 dissolved CO is captured from the atmosphere by rainfall. indicators of surface-groundwater interaction therefore, the 2 Processes of organic material decomposition in the soil potential magnitude of extraneous sources and sinks of CO 2 column further increase the CO concentration of this water must first be quantified. 2 as it percolates through the soil. Resulting levels of dissolved Worrall and Lancaster (2005), observed significant intra- CO in groundwater are, therefore, higher than those found annual variation in groundwater-dissolved CO , and between 2 2 in surface waters (Neal et al., 2000), making it a good different aquifers. While physically-based models for candidate for use as a groundwater tracer. simulation of conservative natural tracers may be used as a When groundwater emerges at an interface with a surface- starting point in the context of CO (e.g. Choi et al., 1998), 2 water body, dissolved CO in the groundwater starts to degas parameterisation of such models is difficult (Genereux and 2 328 Variability of dissolved CO in the Pang and Lambourn Chalk rivers 2 Hemond, 1992) and extraneous processes of CO 2 Site description production, CO degassing and carbonate precipitation are 2 Covering areas of 170.9 km2 and 234.1 km2 respectively, still not addressed. Indeed, Finlay (2003), suggests that even the Pang and Lambourn catchments are located on the the presence of canopy cover above streams can affect the northern side of the Thames basin (Fig. 1) and each temporal dynamics of dissolved CO significantly. 2 catchment consists of predominantly Upper and Middle This paper investigates the potential of using simple Cretaceous Chalk. The Upper Chalk is approximately 75 m surface/groundwater ratios of dissolved CO to describe the 2 thick and outcrops extensively on the dip slopes of both spatial and temporal distribution of surfacegroundwater catchments. The Middle Chalk is up to 60 m thick and is interaction in groundwater catchments. The influence of slightly more argillaceous than the Upper Chalk, (Allen et streamflow and in-stream vegetation on the seasonal and al., 1997; Aldiss et al., 2002). Due to the highly permeable diurnal variability of in-stream dissolved CO has been 2 nature of Chalk aquifers, rivers in both catchments are assessed using water sampled at nine surface water and five groundwater fed. The Lambourn, for example, has an groundwater locations, over a three-year period in the Pang average stream gauge baseflow index (BFI) of 0.93, whilst and Lambourn Chalk catchments in Berkshire, UK. the Pang has average BFI of 0.867 (Gustard et al., 1992). In The Pang and Lambourn catchments are key sites of the addition to groundwater springs, there are several sink holes Lowland Catchment Research project (LOCAR) which aims in both catchments, the most significant one being in the to develop a better understanding of hydrological, geo- lower Pang catchment (Banks et al., 1995; Maurice et al., chemical and ecological processes in permeable lowland 2006). Significant impermeable Tertiary (Eocene) catchments. In this research new interdisciplinary science formations are also found in the lower Pang, including and improved modelling tools were developed to meet the Reading Beds and London Clay. Geological variation challenges of integrated catchment management as defined between the two catchments is reflected in contrasting by the Water Framework Directive (Wheater and Peach, landscape features and topography. The river valley of the 2004). s e m Lambourn a h T Pang r Lynch Wood e v i R !( L1 P1 !( !( L2 !( !( L3 P2 !( L4 Pangbourne !( e n r P3!( P9 L5 u !( o b L6 !( r !( te !( P8 n L7 i !( !( !( P7 W P4 P5 P6 !( !( L8 L9 R Blue Pool iver K enn et Shaw Newbury Fig. 1. Location of water sampling sites within the Pang and Lambourn catchments. Position of Thames, Kennet and Winterbourne Rivers also shown. 329 J. Griffiths, J. Nutter, A. Binley, N. Crook, A. Young and J. Pates Lambourn, for example, is relatively narrow (typically Dissolved CO in Chalk streams 250500 m) with sharp gradient sides. The Pang, by 2 In Chalk catchments, CO in groundwater is the result of comparison, is characterised by wide river valleys (up to 2 calcium carbonate (calcite) acid dissolution due to 2 km width) with less-defined sides of lower topographic microbiological activity; this generates carbonic acid and gradient. Consequently, dry-valley landscape-features that nitrogen transformations. The rates of these reactions are intersect the main river-valley, and which are thought to determined by CO concentrations and the degree of mineral promote convergence of subsurface flow (Grapes et al., 2 unsaturation in the water, and the availability of individual 2005), are more prevalent in the Lambourn catchment. minerals, especially those that dissolve rapidly, such as Grapes et al. (2006) also identified a localised alluvial gravel calcite and other carbonate-based minerals. Upper and aquifer in the Lambourn valley which is probably associated middle Chalk consists of relatively pure calcium carbonate with a number of small wetland areas in the main river valley. such as the mineral calcite but may still contain impurities, Larger regional-scale controls on groundwater movement including Mg, Sr, Mn and Fe. in the two catchments include major hydrological sinks (the The chemistry of percolating rainwater in Chalk Thames and Kennet valleys), geological boundaries (Pewsey catchments will change gradually as it passes through Anticline) and the stratigraphic position relative to sea level different subsurface layers. Chalk soils are typically less (Bradford, 2002). Hard-grounds and harder bands in the than one metre in depth and, whilst well drained, have Chalk, associated with more cleanly fractured areas of relatively slow infiltration times of about a metre per year. deeper Chalk, may also promote the formation of preferential The production of CO by biological activity in such soils flow pathways (Brettal, 1971). 2 results in the CO concentration of percolating rainfall The River Lambourn flows in a predominantly south- 2 increasing from 340 ppm in the open-air to up to 6000 ppm easterly direction throughout its course and covers a distance (Edmunds et al., 1992). The rate of CO production through of 20 km from its source at Lynch Wood to its confluence 2 biological activity in the soil is linearly related to with the larger River Kennet at Newbury. The River temperature, but the relationship is also dependent on the Lambourn has a mean annual flow of 1.76 m3 s1 (1962 type of vegetation and will be greater for natural vegetation 2003), at the Shaw gauging station, situated 2 km upstream than for wheat crops, for example. of Newbury (NRFA, 2004a). From spring to summer, the Beneath the soil layer, in the unsaturated zone of the Chalk, seasonal head of the river rises from outcrops of Middle moisture moves in what is essentially a dual-porosity Chalk in Lynch Wood at the top of the catchment. Stream medium comprising the saturated micro-pores of the Chalk levels generally peak and begin to recede from the end of rock matrix, and a largely unsaturated fissure network that May. Summer streamflow recession is then followed by a runs through the Chalk.
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