Hydrochemical and Isotopic Characteristics of the Surface ... · Hydrochemical and Isotopic Characteristics of the Surface and Groundwater of the Hydrological Zones of the Ord Stage

C S I R O L A N D a nd WAT E R

Hydrochemical and Isotopic Characteristics of

the Surface and Groundwater of the Hydrological

Zones of the Ord Stage 1 Irrigation Area

Ramsis Salama, Elise Bekele,

Daniel Pollock and Vit Gailitis

Lorraine Bates,

CSIRO Land and Water, Perth

Technical Report 8/02, February 2002

HYDROCHEMICAL AND ISOTOPIC CHARACTERISTICS OF THE SURFACE AND

GROUNDWATER OF THE HYDROLOGICAL ZONES OF THE ORD STAGE I

IRRIGATION AREA

Ramsis Salama, Elise Bekele, Lorraine Bates, Daniel Pollock and Vit Gailitis

Technical Report No 8/02

CSIRO Land and Water Private Bag No 5 PO WEMBLEY

Western Australia 6913

February 2002

Copyright

© 2002 CSIRO Land and Water To the extent permitted by law, all rights are reserved and no part of this publication covered by copyright may be reproduced or copied in any form or by any means except with the written permission of CSIRO Land and Water.

Important Disclaimer

To the extent permitted by law, CSIRO Land and Water (including its employees and consultants) excludes all liability to any person for any consequences, including but not limited to all losses, damages, costs, expenses and any other compensation, arising directly or indirectly from using this publication (in part or in whole) and any information or material contained in it.

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TABLE OF CONTENTS

BACKGROUND.........................................................................................................................1

Location............................................................................................................................. 1

Climate .............................................................................................................................. 1

Soils.................................................................................................................................... 1

Hydrogeology.................................................................................................................... 2

Regional Groundwater Quality ......................................................................................... 3

OBJECTIVES AND METHODOLOGY......................................................................................5

RESULTS.....................................................................................................................................7

Hydrochemistry ................................................................................................................ 7

Relationship between Cl, Na and EC..............................................................................................7

Surface Water..................................................................................................................................7

Shallow Groundwater (<10 m) ....................................................................................................12

Intermediate and Deep Groundwater (>10m) ............................................................................12

Oxygen-18 and Deuterium Isotopic Compositions ........................................................ 12

SURFACE WATER SEEPAGE AND MIXING PATTERNS ......................................................16

Packsaddle Plain .............................................................................................................. 17

Seepage from supply channels.......................................................................................................17

Seepage from drains......................................................................................................................19

Ivanhoe Plain ................................................................................................................... 19

Seepage from the M1- Change in water quality............................................................................19

Seepage from supply channels.......................................................................................................21

Seepage from drains......................................................................................................................21

Cave Spring Gap Area ..................................................................................................... 22

Rainfall recharge .............................................................................................................. 22

SUITABILITY OF GROUNDWATER FOR IRRIGATION........................................................23

CONCLUSIONS ......................................................................................................................24

ACKNOWLEDGEMENTS .......................................................................................................24

REFERENCES ...........................................................................................................................24

APPENDIX 1 ............................................................................................................................27

February 2002

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BACKGROUND

Location

The Ord River Irrigation Area (ORIA) is located in the East Kimberley region of Western

Australia and the Northern Territory. The OBP Regional Irrigation study encompasses

the Packsaddle and Ivanhoe Plains, which cover a total area of approximately 15,000 ha.

Irrigated agriculture commenced in 1963, leading to significant changes in the hydrologic

budget of the aquifers underlying the plains.

Climate

The climate in the region is semi-arid monsoonal with two distinct seasons. Average

annual rainfall varies across the catchment from 780 mm in the north to 450 mm in the

south. Most rainfall occurs during the ‘wet’ season from November through to April due

to cyclonic influences and rain-bearing depressions. Throughout the rest of the year

rainfall is light and it is not unusual to have several consecutive dry months. Daily

temperatures above 40˚C just prior to the wet season are common. The average

temperature range for January is 26–36˚C and for July, the range is 15–30˚C. Pan

evaporation for Kununurra approaches 3,000 mm per year (Ruprecht & Rodgers, 1999;

O’Boy et al., 2001)

Soils

Detailed information relating to soils can be found in survey reports for a number of

general and specific studies conducted in the area since Burvill’s initial work in the Ord

River area (Burvill, 1945; Stoneman, 1972; Aldrick et al., 1990; Burvill, 1991; Schoknecht,

1996; Schoknecht & Grose, 1996). Later surveys found considerable variation in soils and

the presence of ancient river channels, levees, point bar systems and swamps. The soil

type has a significant influence on crop selection and irrigation practices.

The dominant soils are cracking clays from the Cununurra and Aquitane families. Levee

type soils and sands are also present. Cununurra clays occur in several phases including

normal, alkaline and leached. The alkaline phase, consisting of imperfect to poorly drained

brown clays with fine topsoil, covers a large portion of the Ivanhoe Plain. Occurrence is

generally restricted to the area south of the Kimberley Research Station. To the north

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and east, soils of the leached phase occur. These generally have a coarser structure and

higher clay content with poor to very poor drainage. Soils of the minor wetter phase are

located around the margins of swampy soils or in the relatively flat interfluvial areas of

leached phase Cununurra clays. Aquitane soils are bluish-grey to yellow cracking clays

associated with areas subject to prolonged inundation such as swamps. Drainage is

generally very poor. Large areas of Cununurra clay in the normal phase occur on the

Packsaddle Plain. These have a darker colour with medium texture and poor drainage.

Smaller areas of the alkaline and acid phase also occur. Areas of Packsaddle sandy loams

(levee soils) are adjacent to the Cununurra clay. These are better drained and well suited

to intensive horticultural activities. Ord loamy sands are located near the river and light

textured. Cockatoo sands that formed on colluvial deposits are also present (Stoneman,

1972; Aldrick et al., 1990; O’Boy et al., 2001).

Hydrogeology

The Ivanhoe Plain contains superficial sediments resting on a palaeo-topographic surface

of basalt, sandstone and limestone. The geological sequence is comprised of a superficial

sequence consisting of river gravels, sandy, poorly cemented sands or sandstones, silty

clays and clays, and show extreme variation in lateral and vertical distribution (McGowan,

1983). This reflects deposition in a complex sedimentary environment involving two

braided river systems. McGowan (1983) classified the sediments regionally in terms of

two predominant lithotypes: gravels and clays. Very coarse sand sequences show local

association with the gravels. Other sands as well as cemented sands and silts occur within

the clay sequences and are interpreted as thin interbeds or poorly sorted strata. Two

major gravel units have been identified and represent two palaeo-river systems. The

upper unit is less than 10 m thick with an average thickness of 2 m. The thickness of the

lower unit varies between 5–20 m. Both units are present over a considerable area of the

Ivanhoe Plain (McGowan, 1983).

Groundwater exists mainly in the superficial and alluvial deposits within palaeochannels

and depressions of the Ivanhoe and Packsaddle Plains. Due to the nature and thickness of

the gravel and very coarse sand strata, transmissivities of the superficial sediments are

locally very high (>1000 m2d-1) and generally high (>100 m2d-1) where the lower gravel

unit is greater than 5 m thick. The areas in which the upper gravel unit is thickest usually

February 2002

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correspond to areas with the highest transmissivities and good interconnectivity between

the upper and lower gravels (McGowan, 1983). On the other hand, the calculated mean

sand and gravel aquifer transmissivity from aquifer tests in the Ivanhoe Plain is about

2400 m2d-1 and a hydraulic conductivity of 400 md-1, assuming a 6 m thick aquifer (O'Boy,

1997; 1998). The mean transmissivity of the deep gravel aquifer at Packsaddle is about

2000 m2d-1, which gives a hydraulic conductivity of 333 md-1, assuming a 6 m-thick aquifer

(O’Boy, 1997).

Regional Groundwater Quality

The amount of salinity in the groundwater varies widely across the Ord River Irrigation

Area. Groundwater salinities range from fresh (less than 1000 µS/cm in southern areas

near Lake Kununurra) to saline (more than 30000 µS/cm in the northern areas of Green

Location). Low salinity groundwater is associated with recharge from rain, particularly

within the Cave Spring area, the Ord River and the associated irrigation system of supply

channels and drains. In the Ivanhoe Plain, salinity increases gradually along the direction of

groundwater flow from 1000–3000 µS/cm within southern areas to a maximum of

4000 µS/cm at the discharge area along the Ord River (Figure 1). High salinity levels are

associated with groundwater discharge areas. The highest salinity levels are in the

northern areas of Dumas Lookout and the southern areas of Green Location, where

salinities reach a maximum of 100000 µS/cm. In Martins Location, salinity ranges from

1000 µS/cm in the southern part to 3000 µS/cm in the northern part where the

groundwater movement is blocked. In the Cave Spring Zone, groundwater salinity is fairly

uniform and less than 2000 µS/cm along the northeast side. Water from a spring in the

Cave Spring Zone produces the best quality water in the whole ORIA.

In Packsaddle Plain, salinity also increases along the direction of groundwater flow from

the south to the central area, where it reaches a maximum of 7000 µS/cm. Groundwater

salinity in the aquifers south of the Diversion Dam is low and increases in a southerly

direction towards the centre of Packsaddle Plain.

February 2002

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M1! Bore 2001

Figure 1: Regional groundwater quality in the Ivanhoe and Paddlesack Plains

February 2002

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OBJECTIVES AND METHODOLOGY

The objectives of this hydrochemical and isotopic study for the ORIA are:

1) To review previous relevant studies, and relate the trends to different

management schemes.

2) To investigate the dynamic change in water quality caused by the seepage of

surface water into the shallow aquifer since irrigation started in the area.

3) To clarify the impact of the irrigation and drainage system on the local and regional

groundwater.

4) To use the constructed hydrological response units to clarify mixing patterns.

5) To delineate areas of increased risk based on water quality change due to current

irrigation practices

To accomplish these objectives, water samples were collected and analysed from all of

the Water and Rivers Commission's accessible wells and all newly drilled CSIRO wells, as

well as from most of the operating supply channels and drains during the month of

September 2001 (Plate 1). Electrical conductivity and pH were measured in the field.

Water samples were analysed for the major cations (Ca, Mg, Na and K), anions (Cl, SO4,

HCO3 and NO3) as well as for the stable isotopes deuterium and oxygen-18.

The strategy followed in the study was to use the hydrological zones (Figure 2) that were

created by the irrigation system to analyse the water quality trends within each zone

(Salama et al., 2002). A detailed geochemical modelling, to be completed in May 2002,

will elaborate on the mixing patterns and the resultant water quality to evaluate the

effects of different management schemes on the hydrochemistry.

February 2002

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Figure 2: Hydrological Zones of the Ord

February 2002

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RESULTS

Hydrochemistry

The hydrochemistry of surface water, shallow groundwater and deep groundwater were

plotted on Piper and Stiff diagrams using the RockWare software, HydroChem (Appendix

1). The surface water samples from the Ord River, Diversion Dam, supply channels and

drainage system are all of the temporary hardness type. The chemistry of the surface

water in the Ord River, Diversion Dam and the irrigation system is dominated mainly by

carbonate hardness; secondary alkalinity exceeds 50%.

A large number of water samples from the shallow aquifer are from the alkali carbonate

group with several samples plotting along a line connecting to waters of the temporary

hardness type. This indicates mixing of the surface water with shallow groundwater in

different proportions. The results also show another line of mixing between the surface

water and the saline water in the northern area of Ivanhoe Plain. There are other mixing

lines indicating a mixture of shallow groundwater with deeper groundwater.

Relationship between Cl, Na and EC

Composition diagrams were constructed using pairs of measured constituents to

investigate possible correlations between major ions. The results indicate that there is no

definite correlation between chloride and sodium (R2 = 0.0609) in the surface water

samples collected from the rivers, irrigation channels and drains in the ORIA. The

correlation between chloride and sodium is considerably stronger (R2 = 0.566) in the

groundwater samples from deep WRC bores and the water samples from CSIRO shallow

wells (R2 = 0.9662). There is a strong correlation between EC and Cl for all of the water

samples (R2 = 0.9016). The stronger correlation for shallow groundwater is a clear

indication of evaporative concentration. No significant relationship exists between any of

the other cation and anion pairs.

Surface Water

Surface water sampled from the Ord River indicates very good quality water with EC

ranging from 350 to 450 µS/cm and less than 25 mg/L of chloride (Table 1). The water is

mainly Ca-Na HCO3 water of temporary hardness.

February 2002

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Table 1: Hydrochemistry of the Ord River

Cond Na K Ca Mg Cl SO4 HCO3 NO3 Sample pH TDS

µS/cm Mg/L

D1A1 7.75 238.2 397 22.4 4.6 23.2 11.1 15 3 122 0

D1 7.8 193.8 323 21 4.1 25.5 12.2 14 3 157 1.3

D1/D1A 7.5 183.6 306 21 4.1 25.4 12.1 11 3 157 1.3

D2A1 7.6 186 310 21.4 3.7 25.4 11.7 15 3 155 0.5

D2A1 7.9 179.4 299 21.2 3.5 23.6 11.2 16 3 155 0

D2 8 243.6 406 21.1 3.5 24 11.6 16 3 155 0

D2A 7.95 186 310 20.7 3.7 24.6 12.1 16 3 122 0

D2A 8.15 181.2 302 20.5 3.7 24.3 11.2 16 3 122 0

D2 8.1 176.4 294 19.9 3.1 22.6 11.8 15 3 122 0

D2 8.1 184.8 308 21.1 4.4 23.5 11.9 15 3 122 0

D2/D2C 8 183 305 21 4.3 23.2 11.8 17 4 122 0

D2B 7.7 154.2 257 20.3 3 22.3 11.9 16 3 122 0

D2B 7.87 91.8 153 21.2 3.4 11.7 5.4 18 4 122 0

D2 8 174 290 20.1 3 22.1 11.9 14 3 122 0

D2C 8.05 176.4 294 21.5 3.3 23.7 11.7 15 3 122 0.4

D3 8.6 150.6 251 21.1 3.4 14.9 11.3 16 3 122 0

D3 8.6 144.6 241 21.1 2.8 12.5 11 15 3 122 0

D4 8.21 176.4 294 21.6 3.2 22.1 11.9 19 3 146 0

D4A 8.15 178.2 297 20.7 3.4 22.7 11.7 18 3 155 0

D4A 8.28 177.6 296 20.6 3.4 22.2 11.5 14 3 152 0

D4A1 8.18 190.8 318 23.4 4.9 22.2 12.6 16 3 136 1.2

D4A1 8.22 183.6 306 22.7 4.1 21.8 12.2 14 3 122 0.5

D2B 8.2 205.2 342 23.8 6.6 26.1 13.1 19 3 183 0

D4D 8.27 190.2 317 21.7 3.5 23.1 12.8 18 5 122 0

D4D 8.37 176.4 294 20.2 2.9 21.8 11.8 16 4 122 0

D4C1 8.32 170.4 284 20.4 3.2 21.4 10.9 13 3 122 0

D4C 8.26 179.4 299 20.7 3.4 22.7 11.7 16 3 122 0

D4C1 8.17 183.6 306 22.2 4.2 22.9 11.2 14 4 122 0

D4C 8 194.4 324 21.8 6.6 24.4 12.4 17 3 122 0

D4F 8.29 175.8 293 20.4 2.9 22 11.9 18 3 122 0

D4F 8.34 174 290 20.2 3 22 11.6 16 3 183 0

D5 8.34 176.4 294 20.9 3.3 22.1 11.7 15 4 122 0.1

D5 8.1 180.6 301 21.9 3.9 21.4 12.1 14 3 122 0.1

D6A1 8.15 180 300 21.7 4.7 22.5 11.9 14 3 122 0

D6A1 8.14 177.6 296 21.6 4.5 20.1 12.3 14 3 122 0

D6A 8.28 171.6 286 20.8 3.3 21.1 10.8 14 3 122 0.3

D6 8.26 175.8 293 20.2 3.1 22.2 11.9 17 4 122 0

D6 8.36 174.6 291 20.4 3.1 21.8 11.6 14 8 122 0

D4 8.32 193.2 322 25.6 3.9 22.3 12.5 17 3 122 0.1

D8 8.04 193.2 322 22.5 4.5 23.5 12.9 14 3 122 0

D8 7.98 176.4 294 21.7 4.6 22 12.6 14 3 122 0.1

D7E1A 8.02 178.2 297 22 3.6 21.4 11.5 15 4 122 0.2

D7E2 7.69 223.8 373 24.4 9.9 27.8 16.3 17 3 183 0

D7E2 8.04 168.6 281 21 4 17.7 12.3 16 3 122 0

D7 8.02 191.4 319 22.3 6.1 23.5 13.5 16 3 122 0

D7E1 8.04 187.8 313 21.9 5.8 23.1 12.7 17 3 183 0

February 2002

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Table 1 (continued)


µS/cm Mg/L

D7E1 7.91 190.2 317 21.6 5.1 23.9 12.5 15 3 122 0

Lake Argyle 8.1 178.2 297 20.3 3.9 24.1 11.7 13 3 122 0

Dunham river 8.17 199.2 332 23.9 3.3 23.9 15.7 16 3 183 0.2

Diversion Dam 8.06 178.2 297 20.3 3.4 24.8 11.9 14 3 183 0

M1 near Co9a 8.17 177.6 296 20.1 3.2 24.4 11.9 14 3 122 0

HDP1 U 8.01 185.4 309 20.6 4.2 25.1 12.2 17 3 122 0

DP1D 7.86 201.6 336 22.3 4.8 26.9 13.6 15 5 122 0.5

DP2D 7.9 190.2 317 23.6 4 24.1 12.3 18 3 122 0

DP3U 8 181.2 302 20.2 3.3 24.7 12 14 3 122 0

DP3D 8.05 180.6 301 20.1 3.2 24.9 12 13 3 122 0

DP4D 8.09 183.6 306 21.1 3.5 26.5 12.2 17 3 122 0.1

DP3AAU 8.02 198 330 21.1 8.2 25.4 13.5 15 3 183 0

DP3AAD 7.79 199.8 333 21.1 7.6 25.5 13.7 18 3 183 0

DP6D 8.05 204 340 26.3 3.7 25.4 13.7 19 4 122 0

DP10D 8.15 177.6 296 20.1 3.2 24.4 11.3 14 3 122 0

DP12D 8.06 189.6 316 22 5.1 26.3 11.3 19 5 122 0.1

DP8U 7.97 186 310 20.9 3.6 24.8 12 14 3 183 0

DP8D 8.17 182.4 304 20.5 3.4 27.3 11.9 15 2 122 0

SP1A 8.25 181.2 302 20.2 3.3 24.4 11.8 16 3 183 0

S28 8.32 196.2 327 20.9 4.8 24.9 12.4 16 3 183 0

1C 8.16 256.2 427 25.4 4.9 31.1 21.2 16 3 183 0.1

CS1A/78 7.57 33.3 55.5 6 2.7 2.3 0.8 15 3 0 0

HI1/78 8.28 660.6 1101 154.7 2.1 13.8 35.9 140 2 305 0

HI3/78 8.1 2334 3890 808 2 22.5 52.1 1295 23 427 0.4

ORD1 (CG3) 7.82 487.2 812 37.7 6.4 52.2 42.3 210 4 122 0.9

ORD3 (CG5) 8.18 1542 2570 443.7 5 35.9 72.3 665 64 305 0.3

ORD4 8.09 2478 4130 1011 6.4 10.4 35.4 595 290 671 0.1

ORD5 (CG1) 7.94 1824 3040 442.6 7.3 8.6 100 770 80 61 0.9

ORD6 (CG2) 8.15 648 1080 60.4 4 31.4 41.1 140 9 244 0.4

ORD8 8.14 850.2 1417 198.2 4.5 23.3 51.8 245 34 244 0

ORD13 (PS14) 8.49 498.6 831 137.8 1.4 21.4 15.1 70 3 244 0

ORD14 (PS15) 8.12 687.6 1146 154.3 2.4 16.1 29.7 175 6 305 0.2

ORD15 (PS12) 8.25 1008 1680 87.9 2.7 91 79 525 5 61 0.2

ORD27 (PS3) 8.44 481.8 803 34.2 1.6 28.9 26.7 70 4 122 0.8

ORD28 (PS1) 7.89 557.4 929 46.5 2.2 33.9 40.9 140 5 122 1.7

ORD29 8.26 577.8 963 152.8 2.1 14.1 21.5 105 2 244 0.8

P2 8.45 858 1430 352 3.8 11.6 12 70 3 671 0.1

P7 8.38 942.6 1571 296.9 1.1 20.3 22.8 455 2 183 1.3

P13 8.23 1411.2 2352 526.6 10.1 12.4 17.3 350 19 732 0.2

P14 8.2 368.4 614 91.6 0.8 13.1 11.8 19 2 244 2.1

P17 8.08 2922 4870 1220 9 5.2 12.3 1050 43 1281 0.4

P18 8.06 442.8 738 103.7 5.6 11.3 10.9 25 3 244 0

P20 8.39 1644 2740 387.4 33.7 3 3.2 280 9 732 0.1

PB2M2 7.9 939 1565 163.4 9.2 28.2 49.6 350 5 122 5

PN2D 8.05 2634 4390 1034 7.7 12.1 40.7 840 198 732 0.3

PN2S 8.55 2178 3630 951 4.2 10 20.5 140 238 1159 0.4

February 2002

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Table 1 (continued)


µS/cm Mg/L

PN3S 8.57 728.4 1214 289.3 0.8 5.5 4.6 70 16 427 2.8

PN5D 7.92 1347 2245 298.6 4.2 28.4 81.5 630 27 244 1

PN5S 8.27 517.8 863 101 1.6 39.1 26.7 105 8 183 0.3

PN6D 8.21 718.2 1197 227 6.6 21.1 11.8 175 14 305 0.5

PN6S 8.35 1542 2570 601 2 14.2 16.3 630 24 610 0.9

PN7S 8.02 750 1250 266 54.3 6.4 15.4 35 22 549 0

PN8D 7.64 560.4 934 93.3 4.5 30 23.3 175 2 122 3.6

PN9D 7.68 888 1480 137.3 3.1 47.9 55.3 420 5 183 2.1

PN9S 7.77 850.8 1418 144.7 4.6 34.1 51 210 19 122 35.8

PN12D 7.96 2112 3520 518.8 58.5 81.4 98.8 910 222 183 4.5

PN13D 7.78 3558 5930 698 34.8 288 205 2135 107 183 0.3

PN13S 8.17 645 1075 177.6 1.5 8.7 15.1 21 5 366 7.8

PN14S 7.85 110.4 184 9.7 4.1 0.7 1.3 12 0.5 20.9 2.8

PS1/78 8.1 765 1275 284 0.3 7.2 14.5 210 6 427 0

PS2/78 8 429.6 716 133.3 1.7 18 14.3 35 2 366 0.1

PS5(P6?) 8.22 4332 7220 1880 4.8 4.2 14.1 2030 65 1281 17.2

CO1A 8.03 5208 8680 1860 3.9 20.4 172 2695 321 366 0

CO1B 8.1 199.8 333 2995 3.9 0 400 4235 496 366 0.4

CO2 8.14 4482 7470 1249 2.6 26.9 134 2415 4 366 3.9

CO4 8.28 1854 3090 590 0.9 7.2 46.6 875 22 488 0

CO5A 8.7 939.6 1566 407.4 0.9 2 2.2 35 11 854 0

CO5B 8.6 1206.6 2011 561 1.3 1.9 3.4 175 14 915 0

CO5C 8.56 3990 6650 1837 5.5 5.6 25.5 1680 76 2013 0

CO6 8.12 562.2 937 110.9 2.6 29.9 15.5 19 19 244 0

CO7 8.12 296.4 494 26.3 2.3 17.7 30.9 15 2 183 0.5

CO8A 8.57 343.2 572 13.7 4.1 22.8 29.2 14 1 183 0.6

CO8B 8.22 266.4 444 48.5 4.2 17.9 20.7 14 2 183 0

CO8C 8.47 313.2 522 121.3 2.4 3.6 4 23 2 244 0.4

CO9A 8.27 235.2 392 17.3 4.9 24.6 19 14 3 183 1.4

CO9B 8.33 624.6 1041 191.8 10.3 12.3 32.6 14 2 427 1.8

CO9C 8.17 396.6 661 59.6 7 17.1 36.9 27 0.5 305 0

CO10 8.39 495 825 193.9 5.2 7.8 7.3 15 3 427 0.8

CO11A 8.41 382.8 638 126.9 2.4 10.4 5.8 35 3 244 0.6

CO11B 8.1 271.8 453 36.3 4.7 26.2 19.2 105 2 183 0.9

CO11C 8.21 429.6 716 86.5 4 17.7 24 350 2 183 0

CO11D 8.25 839.4 1399 188.1 3.4 20.4 10.3 14 3 366 1

CO12 7.95 5094 8490 1637 5.4 11.7 179 2975 7 427 0.2

CO13A 8.19 210.6 351 20 3.6 27.2 10.6 16 3 122 0

CO13B 8.07 211.2 352 16 4.7 26.8 19 12 2 215 0

CO13C 8.09 261.6 436 23.4 6.8 18.1 25.9 17 2 244 0

CO13D 8.48 594.6 991 32.6 256 8.2 22.5 11 7 427 2.9

CO14A 8.34 506.4 844 136.4 1.7 12.4 20 46 8 427 0

CO14B 8.15 307.2 512 81 1.1 16.3 10.3 17 8 244 0.1

CO14C 8.21 511.2 852 131.3 2.3 14.5 19.8 70 12 244 2.2

CO14D 8.24 377.4 629 63.9 3.5 13.5 17.2 35 3 244 0.4

CO15A 8.24 1134.6 1891 407.7 2.8 16.6 12.5 525 17 305 0.2

CO15B 8.39 744 1240 280.2 1.2 9.2 6.8 140 10 366 0

February 2002

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Table 1 (continued)


µS/cm Mg/L

CO15C 7.82 249 415 19.7 3 29.3 15.6 15 3 183 0

CO16A 7.88 657 1095 108.2 14.3 37.7 48.1 280 5 244 4.4

CO16B 8.25 1032 1720 248.6 10 22.4 52.6 490 2 305 1.2

CO16C 8.45 373.8 623 54.1 5 26.6 26.3 35 6 244 0.4

CO16D 8.36 599.4 999 237.2 2.2 8.3 5 13 19 427 22.5

CO17A 8.16 7158 11930 2398 7.8 183 358 3220 778 244 2.7

CO17B 8.23 2688 4480 887 3.8 27.1 60.5 945 234 366 0.6

CO17C 8.26 2016 3360 669 4.2 64.4 59.1 420 325 305 0

CO17D 8.14 3330 5550 1233 5.4 29.6 87.3 1260 356 549 0.1

CO18A 7.58 15420 25700 4823 52.2 551 1667 6860 2313 183 0.5

CO18B 8.15 5406 9010 1612 16 52.4 253 1785 744 305 0.2

CO18C 7.61 17280 28800 5130 43.7 826 1959 8470 1726 183 2.8

CO18D 8.05 3546 5910 926 11.4 68.1 114 875 424 305 0.1

CO18E 7.49 17340 28900 5213 54.2 607 1706 7770 2484 244 0

CO19A 8.56 718.8 1198 127.9 15.1 11.4 24.4 35 22 305 1.6

CO19B 8.23 5622 9370 2059 48.6 14.3 261 1925 917 488 2.4

CO19C 7.86 5298 8830 1195 62.8 0 504 2520 589 244 1.6

CO20A 8.29 1340.4 2234 178.8 0.5 2.4 2.1 17 5 427 4.7

CO20B 8.27 561 935 181.3 1.1 11 21 35 7 366 7

CO20C 8.17 451.2 752 87.5 1.7 12.2 32.6 18 4 427 1.1

CO20D 8.21 253.2 422 27 3 23.2 15.6 14 4 183 1.7

CO21 8.24 1048.2 1747 237 2 14.9 26.7 315 8 366 2.5

CO24A 8.36 607.2 1012 241.7 1 6.6 3.8 35 12 366 21.2

CO24B 8.38 302.4 504 109.5 0.8 2.9 1 17 8 305 1.3

CO24C 8.47 422.4 704 176.3 1 4.3 2.4 35 11 305 4.8

CO25A 8.59 513 855 195.3 1.2 8.4 6.2 18 10 427 1.6

CO25B 8.54 427.8 713 149 1.4 9.2 7.8 21 6 366 0

CO25C 8.33 1461.6 2436 535.6 3 9.4 26.6 525 58 549 12.2

CO27A 8.46 558.6 931 123.5 4.4 13.6 29.7 70 4 366 4.8

CO27B 8.57 535.8 893 109.6 3.7 12 38.6 35 7 366 0.4

CO27C 8.52 345.6 576 67.4 1.8 18.2 19.5 22 3 366 2.8

CO28A 8.13 377.4 629 93.7 1 14.6 10.7 15 4 305 1.1

CO28B 8.28 566.4 944 233.4 0.9 5.7 4.2 15 28 488 1.5

CO28C 8.35 477.6 796 179.6 1.3 6.9 5.5 35 9 427 0

CO29A 8.24 922.2 1537 249.4 3.5 13.8 44.4 175 36 427 14.7

CO29B 8.38 858.6 1431 191.4 4.1 17.4 44.2 175 25 305 20

CO29C 8.36 623.4 1039 197.6 1.3 15.3 17.5 56 15 427 14.7

CO29D 8.14 603 1005 163.4 2.1 15.2 23.9 105 12 366 3.4

CO30A 8.84 1626 2710 659 1.5 8.1 19.8 665 9 793 0

CO30B 8.48 3672 6120 1618 3.8 2.3 48.4 1715 12 1708 0

Ivanhoe Crossing 20/1001 8.33 522.6 871 31.1 2.2 30.2 29.9 105 5 183 0

Ivanhoe Crossing temp 19/1001 8.16 462.6 771 27.6 1.9 33.9 29.4 105 3 244 0.1

Unknown sample possibly Ord 12 8.27 605.4 1009 221.3 49 3.2 0.4 210 5 305 0.1

Cave Spring 8.64 40.5 67.5 2.5 0.9 0.3 0.2 3 1 0 0.1

J Kirby 8.12 407.4 679 20.5 2.1 33.8 28.2 35 8 244 0.7

J Kirby bore near shed 8.28 386.4 644 16.5 2.6 31.2 22.6 35 5 183 2.6

February 2002

– 12 –

Shallow Groundwater (<10 m)

The following description of shallow groundwater (less than 10 m depth below surface) is

based on samples from CSIRO wells in the ORIA collected in September 2001. The

electrical conductivity of shallow groundwater is quite variable; measured EC values for

the majority of groundwater samples range from 500 to 3000 µS/cm. Salinity increases

from the south to the north in both the Packsaddle and the Ivanhoe Plains. In addition to

this trend, salinity increases from the M1 towards the Ord River in the southern part of

the Ivanhoe Plain (Zones G and F). Few samples in Zones C and B have very high EC

values (above 25000 µs/cm). The highest salinity values were measured in the northern

part of Zone D and extending into Zone C, especially at the junction of the D4 and D7.

In the low salinity areas, groundwater composition is mainly Na-Ca HCO3 of temporary

hardness, which indicates direct seepage from the surface water system. As the amount

of mixing with groundwater from the shallow aquifer increases, the water composition

becomes alkali carbonate dominated. Sulphate and chloride are the dominant ions in the

water samples with high measured EC and salinity.

Intermediate and Deep Groundwater (>10m)

Groundwater sampled from the WRC bores is from deeper aquifers than the CSIRO

bores. The deep aquifers generally have lower salinities than the overlying shallow

aquifer. A good indication of direct recharge of surface water to the deep aquifer comes

from a deep groundwater sample from 1C. The groundwater composition is

predominantly alkali carbonate-rich (Ca, Na, HCO3) or saline (SO4, Cl) with few samples

of permanent hardness.

In Zone A (Martins Location), a significant decrease in EC, greater than 1000 µS/cm was

reported between 1990 and 1996 (O’Boy et al., 2001). This was attributed to the gradual

influx of relatively fresh groundwater from recharge mounds (Yesertener, 1997).

Oxygen-18 and Deuterium Isotopic Compositions

The isotopic compositions (δ18O, δD) of surface water, WRC and CSIRO groundwater

samples were plotted relative to the meteoric line of Darwin precipitation to investigate

the probable source of the waters (Table 2; Figures 3, 4 & 5).

February 2002

– 13 –

Table 2: Stable Isotope data from surface and groundwater of the Ivanhoe and Packsaddle Plains

WRC Bores CSIRO Bores Surface Water Bores

ID Oxygen-18 Deuterium ID Oxygen-18 Deuterium ID Oxygen-18 Deuterium

1C -5.34 -45.3 CO1A -4.39 -33.7 D1A1 -4.72 -43.7

CS1A/78 -6.15 -41.3 CO1B -4.00 -30.5 D1 -6.20 -49.1

HI1/78 -4.49 -36.1 CO2 -5.76 -43.7 D1/D1A -6.28 -50.7

HI3/78 -4.67 -36.8 CO4 -2.88 -28.0 D2A1 -6.24 -49.2

ORD1 (CG3) -4.11 -35.5 CO5A -2.70 -31.0 D2A1 -6.13 -48.1

ORD3 (CG5) -5.12 -38.2 CO5B -2.06 -31.5 D2 -6.15 -49.2

ORD4 -1.83 -20.7 CO5C -1.76 -20.2 D2A -6.11 -49.0

ORD5 (CG1) -5.17 -39.1 CO6 -2.69 -26.8 D2A -6.08 -48.2

ORD6 (CG2) -5.67 -42.1 CO7 -5.73 -47.8 D2 -6.41 -50.8

ORD8 -5.56 -40.8 CO8A -6.90 -49.4 D2 -6.17 -49.4

ORD13 (PS14)

-1.05 -16.4 CO8B -2.65 -23.8 D2/D2C -6.15 -49.4

ORD14 (PS15)

-1.45 -18.9 CO8C -2.32 -25.5 D2B -6.35 -50.1

ORD15 (PS12)

-3.41 -30.3 CO9A -6.63 -53.2 D2B -0.56 -22.8

ORD27 (PS3) -4.45 -33.9 CO9B -3.30 -30.4 D2 -6.28 -51.6

ORD28 (PS1) -3.64 -31.3 CO9C -6.88 -51.2 D2C -6.04 -49.7

ORD29 -2.01 -23.9 CO10 -6.66 -46.3 D3 -5.10 -45.2

P2 -5.53 -42.3 CO11A -1.80 -19.2 D3 -5.04 -45.3

P7 -3.24 -27.8 CO11B -6.86 -55.0 D4 -5.75 -47.2

P13 -5.53 -42.4 CO11C -5.33 -45.7 D4A -6.04 -49.1

P14 -3.22 -30.4 CO11D -2.60 -26.5 D4A -6.06 -48.6

P17 -5.74 -42.8 CO12 -4.40 -32.3 D4A1 -5.88 -48.8

P18 -3.92 -37.9 CO13A -6.28 -53.0 D4A1 -6.00 -49.1

P20 -5.52 -42.6 CO13B -6.56 -52.6 D2B -4.88 -44.4

PB2M2 -4.79 -36.9 CO13C -5.10 -42.5 D4D -5.93 -50.5

PN2D -5.93 -46.0 CO13D -6.53 -52.7 D4D -6.23 -49.6

PN2S -2.44 -22.6 CO14A -3.78 -33.6 D4C1 -5.98 -49.1

PN3S -2.33 -25.2 CO14B -2.77 -27.5 D4C -6.04 -49.1

PN5D -2.90 -26.3 CO14C -4.95 -39.6 D4C1 -5.71 -47.2

PN5S -4.02 -34.9 CO14D -4.47 -37.6 D4C -5.67 -46.5

PN6D -3.65 -33.5 CO15A -3.60 -31.4 D4F -6.18 -50.4

PN6S -5.09 -41.1 CO15B -3.19 -30.0 D4F -6.17 -50.9

PN7S -7.33 -52.4 CO15C -6.41 -52.2 D5 -5.83 -51.1

PN8D -2.91 -28.1 CO16A -4.74 -35.0 D5 -5.66 -49.4

PN9D -3.08 -28.8 CO16B -3.37 -29.8 D6A1 -4.94 -45.3

PN9S -2.81 -26.4 CO16C -5.05 -45.5 D6A1 -5.59 -47.4

PN12D -2.23 -23.3 CO16D -3.68 -32.0 D6A -5.79 -47.1

PN13D -6.67 -49.4 CO17A -3.48 -29.1 D6 -6.19 -50.9

PN13S -3.03 -28.9 CO17B -2.48 -25.5 D6 -6.03 -49.3

PN14S -4.90 -38.3 CO17C -2.08 -25.1 D4 -5.75 -47.8

PS1/78 -2.78 -27.1 CO17D -2.96 -26.9 D8 -5.88 -48.5

PS2/78 -1.19 -19.9 CO18A -3.35 -27.1 D8 -5.86 -48.7

PS5(P6?) -2.10 -21.5 CO18B -1.91 -21.0 D7E1A -5.59 -46.6

CO18C -3.60 -27.8 D7E2 -4.79 -43.2

CO18D -1.67 -18.8 D7E2 -5.85 -48.5

CO18E -3.55 -27.7 D7 -5.57 -46.9

CO19A -5.18 -42.2 D7E1 -5.77 -47.9

CO19B -6.31 -45.5 D7E1 -5.54 -47.8

CO19C -5.82 -42.7 Lake Argyle -6.21 -51.9

CO20A -4.98 -41.2 Dunham River -5.04 -42.5

February 2002

– 14 –

Table 2 (continued)

WRC Bores CSIRO Bores Surface Water Bores

ID Oxygen-18 Deuterium ID Oxygen-18 Deuterium ID Oxygen-18 Deuterium

CO20B -4.07 -36.0 Diversion Dam -5.99 -49.4

CO20C -5.59 -46.8 M1 -6.24 -50.1

CO20D -6.15 -51.5 HDP1 U -6.41 -50.3

CO21 -2.35 -23.0 DP1D -6.22 -50.5

CO24A -2.17 -25.0 DP2D -4.32 -41.7

CO24B -4.14 -36.3 DP3U -6.39 -51.7

CO24C -2.36 -26.4 DP3D -6.30 -50.4

CO25A -3.79 -33.3 DP4D -6.26 -50.6

CO25B -4.71 -40.2 DP3AAU -6.31 -50.4

CO25C -2.56 -23.3 DP3AAD -6.24 -50.6

CO27A -3.42 -30.7 DP6D -2.09 -31.4

CO27B -3.13 -29.6 DP10D -6.35 -50.6

CO27C -3.47 -31.5 DP12D -5.09 -45.7

CO28A -6.05 -49.5 DP8U -5.77 -49.7

CO28B -4.22 -38.2 DP8D -6.08 -51.0

CO28C -3.87 -34.7 SP1A -6.21 -52.0

CO29A -2.41 -23.1 S28 -6.04 -51.0

CO29B -3.71 -33.7

CO29C -1.60 -21.0

CO29D -1.80 -20.5

CO30A -5.44 -40.6

CO30B -3.34 -25.4

-9 -8 -7 -6 -5 -4 -3 -2 -1

-60

-50

-40

-30

-20

-10

0

D1A1

D4

D2B

D5

D7

Lake ArgyleS28

Surface WaterMeteoric LineSurface evaporationMixing Line

D2B

DP6D

DP2D

DP8U

D2AD2A1

D2B

SP1A

D2

DP3U

D3

DP12D

D7E2Dunham River

δD

δ18O

Figure 3: Isotopic Composition - Surface Water Bores

February 2002

– 15 –

-9 -8 -7 -6 -5 -4 -3 -2 -1

-60

-50

-40

-30

-20

-10

0

1C

HI3/78

ORD4

ORD28 (PS1)

ORD29

P14

P18

PN2D

PN3SPN5D

PN5SPN6D

PN6S

PN7S

PN8D

PN13D

PN14S

PS1/78

PS2/78PS5(P6?)

PN9S

ORD14 (PS15)

ORD13 (PS14)

PN13S

PN12DPN2S

PN9DP7

ORD15

ORD1H11/78

PB2M2

ORD27

ORD5ORD3

ORD8P13

P2P17

ORD6P20

CS1A/78

WRCMeteoric LineMixing Line

δ2H = 6.00514 * δ18O -20.80939)

R2 = 0.96944Surface Evaporation

δ2H = 4.75167 * δ18O -10.19178)

R2 = 0.98134

δD

δ18O

Figure 4: Isotopic Composition - WRC Water Bores

-9 -8 -7 -6 -5 -4 -3 -2 -1

-60

-50

-40

-30

-20

-10

0

CO8A

CO9B

CO9C

CO10

CO11B

CO13A

CO16A

CO16C

CO16D

CO17A

CO17C

CO18A

CO18D

CO20A

CO20C

CO20D

CO24B

CO24C

CO25B

CO28A

CO28B

CO28CCO29B

CO29C

CO1A

CO2

CO4

CO5A CO5B

CO5C

CO7

C012

CO19A

CO19B

CO19C

CO21

CO30A

CO30B

CSIROMeteoric LineSurface Evaporation

δ2H = 6.00514 * δ18

O -20.80939)

R2

= 0.96944Mixing Line

δ2H = 4.75167 * δ18

O -10.19178)

R2

= 0.98134

δ18O

CO13BCO9A

CO13CCO11C

CO14CCO14D

CO20B

CO27C

CO14ACO1B

CO17B

CO8C

CO29A

CO8BCO25C

CO29DCO18B

CO11A

δD

Figure 5: Isotopic Composition - CSIRO Water Bores

February 2002

– 16 –

The isotopic composition of surface water samples from Lake Argyle, the Diversion Dam,

M1, supply channels and drains all plot below the meteoric line and along a trajectory

indicating secondary fractionation caused by evaporation. The surface water becomes

more enriched with increasing evaporation. The trajectory for evaporated surface water

is δD = 4.7085*δ18O - 21.011 with R2 = 0.9568.

All ground water samples plot below the local meteoric water line and along a slope that

indicates secondary fractionation by evaporation of the surface water prior to infiltration.

Groundwater samples from the shallow wells plot slightly farther away from the meteoric

line compared to the deep groundwater, which could indicate that the deep groundwater

originated from a meteoric source, but during a different climatic regime.

The shallow groundwater follows the line: δD = 6.253*δ18O - 9.6142 with R2 = 0.9392.

The deep groundwater follows another line: δD = 5.5535*δ18O - 11.428 with

R2 = 0.9672, which is very similar to the shallow groundwater, but with a less depleted

fraction. The phenomenon of isotope enrichment is well reported in the literature as

occurring under several possible conditions: a delay of water near the surface before

infiltration (Gat & Tzur, 1967), infiltration of recycled irrigation waters that have been

evaporated repeatedly, and evaporation of soil water from the uppermost soil layers

(Zimmermann et al., 1967; Dincer et al., 1974).

In this case, the different trajectory for the shallow aquifer is due to mixing of infiltrated

irrigation water that has been subjected to evaporation with older groundwater that has

not evaporated to the same degree. The isotopically lighter deep groundwater, although

less depleted, seems to have been subjected to evaporation near the surface or while

infiltrating or could also have been recharged during slightly different climate conditions

than present.

SURFACE WATER SEEPAGE AND MIXING PATTERNS

A detailed study of groundwater mixing patterns was conducted using the chemistry and

isotopic results of the constructed sections in the Ivanhoe and Packsaddle Plains

(Appendix 1).

February 2002

– 17 –

In Packsaddle Plain the regional trends in the isotopic composition show that the area

monitored by wells ORD13 and ORD14 contain the most depleted waters. Water from

these two bores will be considered to represent the local original groundwater in the area

prior to irrigation and can be used as an end-member for estimating the amount of mixing.

Water from the Diversion Dam is the other end-member. All of the samples plot along a

line given by δD = 6.0734*δ18O - 9.7295 (R2 = 0.9787), which defines different amounts

of mixing between surface water and the original groundwater (Figure 3).

Packsaddle Plain

The construction of the Diversion Dam restricted the northward flow of groundwater and

water samples upstream of the dam from wells CO21 and CO4 show some mixing with

surface water, but less than the expected proportion; perhaps this is due to the trapping

of the original groundwater behind the dam. The extraordinary result is that water

samples from upstream of the irrigation area from ORD27 and ORD28 show more mixing

with surface water than water sampled from the central irrigation area. This might be due

to better connections through highly transmissive palaeochannel sediments.

Seepage from supply channels

Section CO5 was constructed around the main supply channels SP1 and SP1B in

Packsaddle Plain to study changes in water quality due to seepage from the supply

channels. The isotopic data show that there is minor seepage from the supply channels

(Table 3). This is mainly because a thick mudstone layer extends to about 10 m below the

surface and hinders vertical infiltration. Dilution effects are observed a few hundred

meters west at site P18, due to greater seepage in the area. The mixing pattern is rather

complicated; site CO5A consists of a mixture of surface water and groundwater; site

CO5B indicates a component of water depleted in the heavier isotopes, whereas site

CO5C represents water from a completely different origin. The water quality indicates

that the extent of mixing between surface water and groundwater is greater at site P18

than at sites CO5A and CO5B with the lowest rates of mixing at site CO5C. The water

at sites P15, CO5A and CO5B is alkali carbonate type, whereas the water at CO5C is

saline with high total soluble salts.

February 2002

– 18 –

Table 3: Types of water and degree of mixing in the study sections

Section Groundwater Surface water – Groundwater Mixing Fraction of surface

water in the mixture CO1 Primary salinity CO1A

CO1B 0.52 0.42

CO5 Carbonate alkali Mixing along the weak acids line in 5A and 5B. Less mixing in 5C

CO5A CO5B CO5C

0.43 0.44 0.11

CO8 Carbonate alkali Mixing along the weak acids line. 8A mainly surface water CO8A CO8B CO8C

0.97 0.22 0.27

CO9 Carbonate alkali Mixing along the weak acids line. 9A & 9C mainly surface water

CO9A CO9B CO9C

0.92 0.42 0.97

CO11 11C and 11B Primary salinity, 11A and 11D Carbonate alkali

11A and 11D are mixing along the weak acids line. 11B and 11C are mixing along the alkaline earths line.

CO11A CO11B CO11C CO11D

0.08 0.89 0.87 0.30

CO13 13D Carbonate alkali, 13A, B & C Secondary alkalinity

13A, B & D are mainly surface water, 13D mixing along the weak acids line


0.93 0.94 0.77 0.93

CO14 Carbonate Alkali All samples show mixing along the weak acids line CO14A CO14B CO14C CO14D

0.51 0.33 0.69 0.63

CO15 15A & 15B Primary salinity, 15C Secondary alkalinity

15C is mainly surface water, 15A and 15B groundwater with <50% surface water

CO15A CO15B CO15C

0.45 0.40 0.94

CO16 16A & 16B Primary salinity, 16C Carbonate alkali, and 16D Secondary alkalinity

16C is mainly surface water, 16D is mixing along the weak acid line. 16A & 16B slightly mixing along the alkaline earths.


0.56 0.40 0.86 0.46

CO17 Primary salinity, high TDS

Less than 40% surface water in 17A and less than 30% in 17B and 17C


0.38 0.27 0.26 0.31

CO18 Primary salinity, high TDS

Minimum mixing in 18B & D, slightly higher in A, C and E CO18A CO18B CO18C CO18D CO18E

0.32 0.14 0.34 0.07 0.34

CO19 19B & 19C Primary salinity, high TDS. 19A Carbonate alkali

19A mixing along the weak acids line CO19A CO19B CO19C

0.77 0.87 0.78

CO20 Carbonate alkali 20D & C mainly surface water, 20A, B & C mixing along the weak acids line


0.74 0.58 0.90 0.96

CO24 Carbonate alkali Slight mixing along the weak acids line CO24A CO24B CO24C

0.25 0.59 0.30

CO25 25A & B Carbonate alkali, 25C Primary salinity

A & C slight mixing along the weak acids line CO25A CO25B CO25C

0.50 0.71 0.21

CO27 Carbonate alkali Mixing along the weak acids line CO27A CO27B CO27C

0.43 0.39 0.45

CO28 Carbonate alkali Mixing along the weak acids line CO28A CO28B CO28C

0.98 0.65 0.54

CO29 29C Carbonate alkali, 29A, B & D is NaHCO3

Only 29B show some mixing with 50% surface water CO29A CO29B CO29C CO29D

0.20 0.51 0.14 0.12

CO30 Primary Salinity 30A is mainly drain water CO30A CO30B

0.72 0.27

February 2002

– 19 –

Seepage from drains

Water from DP3, discharging in to Packsaddle Creek along the west side, shows that the

surface water in the drain mixed with a small quantity of rainwater that fell during the

night before sample collection occurred. The samples from the monitoring bores show

some degree of mixing between resident groundwater and surface water with less surface

water influence away from the drain.

The water in the drain is mainly Ca, Mg, HCO3 type, whereas the groundwater in the

area is mainly saline (Na, Cl) with high total dissolved salts. Groundwater near the drain

has lower soluble salts than farther away from the drain, mainly due to dilution by the

seeping drain water.

Results from DP8 drain cross-section are analogous to the results for DP3, but the surface

water fraction in the groundwater is much lower than in DP3. This is attributed to the

fact that the DP8 drain is deeper than DP3. The resident groundwater is of relatively

good quality and mainly Ca, Mg HCO3-type water with a higher proportion of Na than

surface water. Groundwater samples from ORD14 indicate mixing with more saline

water.

Ivanhoe Plain

Seepage from the M1- Change in water quality

Changes in water quality caused by seepage from the M1 were monitored using several

cross-sections that extend from downstream of the Diversion Dam (CO8 and CO9) to

the northwest corner of Green Location Zone A (CO15). The stable isotope results from

sites CO8 and CO9 near the airport indicate that seepage from the M1 is not uniformly

distributed; there is more seepage along the eastern side, although the gradients on the

western side are steeper. The isotopic signature indicates that water from 8A, 9A and 9C

are mainly surface water; however, water from 8C, 8B and 9B consists of different

amounts of surface water mixing in the proportions 27%, 22% and 42%, respectively

(Table 3). These results are similar to the Piper diagram results, which show that water

from 8C and 9B represent one end-member of alkali carbonate-type water, while water

February 2002

– 20 –

from the M1, 8A and 9A are of the temporary hardness type and water from 9C and 8B

comprises part of a mixing line between the two end-members.

Further downstream at site CO11, similar results are obtained, where groundwater near

the M1 (11B and 11C) is mainly of the surface water type. Groundwater from wells

farther away (11A and 11D) is only 8% and 30% surface water. A deeper well (1C)

which is farther away from the M1 and near to 11A, which is only 16% surface water,

showed a similar surface water proportion to wells near the M1, which indicates that the

base of the M1 is in direct connection with transmissive palaeochannel deposits at depth.

This direct hydraulic connectivity between the M1 and the deep palaeochannel deposits

might explain the continuous rise of water levels in these aquifers although the top layer is

not very conductive. This direct connection would have been established during

construction of the M1 by removal of the top clayey layers.

At site CO13, all the wells show that most of the area is saturated with surface water;

with only CO13C, showing some mixing with original groundwater, but even there the

proportion of groundwater is only 23%. A groundwater mound has occurred in this area

since 1965 when the M1 was first flooded and the mound continues to be a trouble spot

today.

Most of the water around the M1 and the supply channels is of the temporary hardness

type; however, it changes to alkali carbonate type farther away from the M1. Total

soluble salts also increase away from the M1.

Sites CO14, CO15 and CO29 were constructed along the M1 in Zone A (Martins

Location) to study surface water leakage patterns in this area where the water levels are

known to be near the surface. At site CO29 in the central part of Zone A, the water

levels are less than 2 m from the surface, but the isotopic signature of the groundwater

indicates an unexpectedly low proportion of surface water in the monitoring wells with

51% in 29B, 20% in 29A, 12% in 29D and 14% in 29C. This indicates that the rising

groundwater is replacing infiltrated surface water due to the fact that Zone A is a closed

basin with no outlet for groundwater. The isotopic signature of CO29C also indicates

some fractionation caused by the evaporation of shallow groundwater. The water is

predominantly Na-HCO3 type with evidence of mixing and an evaporation trend. Site

February 2002

– 21 –

CO14 has a similar water type and mixing trends, where the isotopic signature indicates

percentages of surface water of 69%, 63%, 51% and 33% in 14C, 14D, 14A and 14B,

respectively. Similarly, the same trend is observed in section CO15 with only CO15C in

the embankment of the supply channel showing higher percentage of surface water

component (94%), while the other wells showed about 45% and 40% of surface water

component in CO15A and CO15B respectively.

Seepage from supply channels

Four sections (CO3, CO20, CO25 and CO28) were constructed to study the influence of

seepage from supply channels on the water quality. In section CO20, the isotopic

signature of groundwater from wells 20C and 20D, upstream of the supply channel

underpass, is mainly derived from surface water. On the other hand, wells downstream

of the supply channel show a small groundwater component ranging from 26% (20A) in

the area near the sugar cane field to 42% in the other well (20B) on the other side of the

road. The water type is mainly Na-HCO3.

Similar trends were observed in sections CO25 and CO28; however, the percentage of

surface water in the groundwater decreases to the west. This is associated with an

increase in depth to groundwater occurring in the same direction. Both observations are

attributed to the increase in hydraulic gradient towards the discharge zones in the Ord

(Salama et al., 2002). This is best illustrated by the fact that wells drilled in section CO3

did not encounter water except below a depth of 10 m from the surface.

Seepage from drains

Sections CO23 and CO24 were constructed to study water quality change due to seepage

from D3. Sections CO17, CO18 and CO19 were constructed to study water quality and

change in chemistry due to seepage from the D4 and D7. The groundwater in the vicinity

of CO17, CO18 and CO19 is mainly NaCl water with very high TDS. Seepage from the

drains is not expected to be significant because this area is already a groundwater

discharge area and the water levels are near to the surface. This is indicated at site CO17;

however, farther downstream where the water levels are deeper, the areas adjacent to

the drains show some mixing. At the confluence of D4 and D7 at site CO19, the isotopic

signature indicates that there is more seepage from the drains. Nevertheless, it seems

February 2002

– 22 –

that the seeping water interacts with the original groundwater to produce saline type

water (Table 3).

Cave Spring Gap Area

The chemical analysis of groundwater from the shallow aquifer is similar to irrigation

water from a borehole near the supply channel, which suggests that there is seepage

occurring from the supply channel in the Cave Spring Gap area. Water from the borehole

on the eastern side of the Cave Spring Gap does not show seepage from the drain; this

might be because local hydraulic gradients do not promote groundwater flow in this

direction. The groundwater flow direction as shown by the constructed section is from

the west to the east. The results also show that there are three separate areas with

different water qualities: the water near the western drain is mainly sodium chloride type

and the water near the supply channel is mainly magnesium bicarbonate type, whereas the

water near the eastern drain is mainly sodium bicarbonate type.

The deuterium and oxygen-18 plot shows the mixing pattern in more detail (Appendix 1).

The surface water represents one end-member and the groundwater from well 16B

represents the other end-member. The results indicate a steady decrease of the surface

water component moving away from the supply channel, with the highest degree of

seepage occurring near the supply channel. The isotopic signature near the eastern drain

shows some rain influence.

A water sample from a spring located near a cave has the lowest EC in the whole area.

Moreover, the isotopic signature indicates less fractionation than the M1 and the

Diversion Dam. The results of the chemistry and isotope analyses indicate that the spring

water is mainly derived from rainwater, which infiltrates through fractures in the cliffs

bordering the irrigation plain.

Rainfall recharge

The only areas that show less isotopic fractionation than the surface water, and shallow

and deep groundwater are the spring in Cave Spring area, the two wells from the west

side of the Ord River in Kirby property and the wells drilled in a depression near the

Ivanhoe Crossing. All of these areas indicate recharge from rainwater in addition to

seepage from the irrigation system, except the Cave Spring sample, which has no surface

water component.

February 2002

– 23 –

SUITABILITY OF GROUNDWATER FOR IRRIGATION

The sodium adsorption ratio (SAR) measures the degree to which sodium in irrigation

water replaces the adsorbed (Ca + Mg) in the soil clays, and thus damages the soil

structure. Irrigation waters are usually classified in terms of salinity hazard (conductivity

or TDS) and sodium hazard (Richards, 1969). The salinity hazard dividing points are 250,

750 and 2250 µohms, resulting in four categories: C1, C2, C3 and C4 respectively. The

sodium hazard is a function of both SAR and salinity. The resulting four categories are S1

to S4, which represents low, medium, high and very high sodium hazard respectively. The

salinity hazard points of the surface and groundwater were calculated using the WATEVAL

computer program (Hounslow, 1995) and the results are shown in Table 4. The results

indicate that most of the groundwater from the shallow and deep aquifers of the Ivanhoe

and Packsaddle Plains has a high to very high sodium adsorption ratio. Although the

surface water from the M1 is in C2S1 category, all of the water mixtures from the shallow

aquifers are in the C3S1 and C3S2 classes which makes it unsuitable for irrigation. Most

of the other shallow and deep groundwater are very saline and exceed the classification.

Table 4: SAR – Conductivity classes of the Ord shallow and deep groundwater

C1S1 C2S1 C2S2 C2S3 C3S1 C3S2 C3S3 C3S4 C4S2 C4S3 C4S4 off graph PN14S 1C CO11A CO24B CO13D CO11D CO10 P2 CO15A ORD3 CO17B C12 CO11B CO25B CO24C CO14A CO16B CO16D PN3S CO15B ORD5 CO17C CO12 CO11C CO8C CO14C CO20B CO25A CO20A PN12D CO25C CO17A CO13A CO16A CO21 CO28C CO24A CO30A CO17D CO13B CO19A CO29A P7 CO28B CO4 CO18A CO13C CO20C CO29B PN7S PN5D HI3/78 CO18B CO14B CO27A CO29C PS1/78 P13 CO18C CO14D CO27B CO29D PN6S CO18D CO15C CO6 CO9B CO18E CO16C HI1/78 ORD29 CO19B CO20D IV1 ORD8 CO19C CO27C IV2 PN13S CO1A CO28A ORD1 PN6D CO1B CO7 ORD13 CO2 CO8A ORD14 CO30B CO8B ORD15 CO5A CO9A ORD27 CO5B CO9C ORD28 CO5C K1 ORD6 CS1A K2 PB2M2 ORD4 M1 PN5S P17 P14 PN8D P20 P18 PN9D PN13D PS2/78 PN9S PN2D PN2S PS5(P6)

February 2002

– 24 –

CONCLUSIONS

Preliminary results of this study indicate that surface water throughout the irrigation

system, including the Diversion Dam, Lake Kununurra, M1, supply channels and drains,

are seeping and mixing with the shallow and deep groundwater of the Ivanhoe and

Packsaddle Plains. The amount of seepage and mixing is taking place in different

proportions, depending on the hydraulic gradients and permeability of the formations. All

of the surface water in the irrigation system, including the drains, is of low salinity. Most

of the shallow and deep groundwater in the aquifers is unsuitable for irrigation due to the

high SAR and high soluble salts in the northern part of the Ivanhoe Plain. The continuous

seepage and groundwater movement might eventually improve the quality of the near

surface shallow groundwater. This will be studied in detail in the next phase of the

project.

ACKNOWLEDGEMENTS

The authors acknowledge funding from the Ord Bonaparte Program through Land &

Water Australia (Project 3.3B: "Best Utilisation of Water Resources for the Ord Irrigation

Area") and the Australian Centre for International Agricultural Research (ACIAR) under

Project LWR1/1998/130: "Water Resources and Salinity Management in Agricultural Areas

of Inland, Northern China and Northern Australia".

REFERENCES

Aldrick, J.M., Clarke, A.J., Moody, P.W., van Cuylenburg, M.H.R. & Wren B.A. (1990).

Soils of the Ivanhoe Plain, East Kimberley, Western Australia. Western Australian

Department of Agriculture; Technical Bulletin No 82.

Burvill, G.H. (1945). Soil surveys Kimberley Division Western Australia map. National

Mapping Office/Western Australian Department of Agriculture.

February 2002

– 25 –

Burvill, G.H. (1991). Soil surveys and related investigations in the Ord River area, East

Kimberley, 1944. Western Australian Department of Agriculture; Technical Bulletin

No 80.

Gat, J.R. & Tzur, Y. (1967). Modification of the isotopic composition of rainwater by

processes which occur before groundwater recharge. Isotopes in Hydrology (Proc.

IAEA Symp, Vienna, 1966): 49.

Dincer, T., Al-Mugrin, A. & Zimmermann, U. (1974). Study of the infiltration and

recharge through the sand dunes in arid zones with special reference to the stable

isotopes and thermonuclear tritium. Journal of Hydrology, 23(79).

Drever, 1988 (depends on whether you want to include the sentence I added).

Hounslow, A.W. (1995). Water quality data: analysis and interpretation. CRC Press.

McGowan, R.J. (1983). Ord River Irrigation Area. Analysis and Interpretation of Drilling

and Hydraulic Testing Programme - Ivanhoe Plains, 1983. Interim Report.

Geological Survey of Western Australia: Hydrogeology Report No. 2513

(unpublished).

O'Boy, C.A. (1997). Ord River Irrigation Area Test Pumping. Water and Rivers

Commission: Hydrogeology Report No. 48.

O'Boy, C.A. (1998). Ord River Irrigation Area Long-Term Test Pumping. Water and

Rivers Commission: Hydrogeology Report No 125.

O'Boy, C.A., Tickell, S.J., Yestertener, D.P., Commander, D.P., Jolly, P. & Laws, A.T.

(2001). Hydrogeology of the Ord Irrigation Area. Water and Rivers Commission:

Hydrogeological Record Series Report HG 7.

Richards, L.A. (1969). Diagnosis and improvement of saline and alkali soils. US Salinity

Laboratory, Agriculture Handbook No 60. US Government Printing Office,

Washington, DC.

Ruprecht, J.K. & Rodgers, S.J. (1999). Hydrology of the Ord River. Water and Rivers

Commission: Water Resources Technical Series No. WRT 24.

February 2002

– 26 –

Salama, R.B., Bekele, E., Pollock, D., Bates, L.E., Byrne, J.D., Hick, W., Watson, G.D. &

Bartle, G. (2002). Hydrological response units of the Ord Stage I Irrigation Area and

the dynamic filling of the aquifers of the Ivanhoe and Packsaddle Plains. CSIRO Land

and Water report, February, 78pp.

Schoknecht, N. & Grose, C. (1996). Soils of the Ivanhoe West Bank, East Kimberley,

Western Australia. Agriculture WA: Resource Management Technical Report 155.

Schoknecht, N. (1996). Assessment of the suitability for horticulture of the Packsaddle

Infill Area, Kununurra. Agriculture WA: Resource Management Technical Report

157.

Stoneman, T.C. (1972). Packsaddle Plains Soil Survey. Western Australian Department of

Agriculture: Technical Bulletin No 55

Yesertener, C. (1997). Review of groundwater monitoring data in the Ord River Irrigation

Area 1996. Water and Rivers Commission: Hydrogeology Report HR 60.

Zimmermann, U., Ehhalt, D. & Munnich, K.O. (1967). Soil water movement and

evapotranspiration: Change in the isotopic composition of the water. Isotopes in

Hydrology (Proc. IAEA Symp. Vienna, 1966): 567.

February 2002

– 27 –

APPENDIX 1

(a) Isotope data of water samples in cross sections

(b) Piper trilinear diagrams

(c) Stiff diagrams

February 2002

– 28 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

DD

P17

CO1ACO1B

DP3U

M1DP3D

δD

δ18O

Cross Section 1

(b)

Ord River

Section CO1Piper Diagram

C A T I O N S A N I O N S%meq/l

Na+K HCO +CO3 3 Cl

Mg SO4

CaCalcium (Ca) Chloride (Cl)

Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium(K

)

Sulfate(S

O4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20

Total Dissolved Solids(Parts Per Million)

0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

DD

DD

DD

M1

M1

M1

P17 P17

P17

CO1ACO1A

CO1A

CO1B

CO1B

CO1B

DDM1P17CO1ACO1B

February 2002

– 29 –

(c)

Ord RiverSection CO1 Stiff Diagram

Cations meq/l Anions125 100 75 50 25 25 50 75 100 125

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+KDD

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+KM1

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+KP17

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+KCO1A

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K CO1B

February 2002

– 30 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

DD

CO5B

CO5C

P18

CO5A

M1

δD

δ18O

Cross Section 5

(b)

Ord River

Section CO5 Piper Diagram


Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

DD

DD

DD

M1

M1

M1

P18

P18

P18

CO5ACO5A

CO5A

CO5BCO5B

CO5B

CO5CCO5C

CO5C

DDM1P18CO5ACO5BCO5C

February 2002

– 31 –

(c)


Cations meq/l Anions80 70 60 50 40 30 20 10 10 20 30 40 50 60 70 80

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+KDD

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+KM1

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

P18

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

CO5A

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

CO5B

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K CO5C

February 2002

– 32 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

CO8C

CO9B

CO10CO7

δD

δ18O

CO9A

DDM1CO9C

CO8A

CO8B

Cross Sections 8 & 9

(b)

Ord River

Section CO8 &CO9 Piper Diagram


Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

DD

DD

DD

M1

M1

M1

CO8A

CO8A

CO8A

CO8B

CO8B

CO8B

CO8C

CO8C

CO8CCO9A

CO9A

CO9A

CO9B

CO9B

CO9B

CO9C

CO9C

CO9C

CO10CO10

CO10

CO7

CO7

CO7

DDM1CO8ACO8BCO8CCO9ACO9BCO9CCO10CO7

February 2002

– 33 –

(c)


Cationsmeq/l

Anions

February 2002

– 34 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

DD

CO11A

CO11B

CO11C

CO11D

M1

1C

δD

δ18O

Cross Section 11

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

DD

DD

DD

M1

M1

M1

1C

1C

1C

CO11A

CO11A

CO11A

CO11B

CO11B

CO11B

CO11C

CO11C

CO11C

CO11D

CO11D

CO11D

DDM11CCO11ACO11BCO11CCO11D

February 2002

– 35 –

(c)


February 2002

– 36 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

DD

CO13A

CO13C

CO13D

CO13BM1

δD

δ18O

Cross Section 13

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

DD

DD

DD

M1

M1

M1

CO13A

CO13A

CO13A

CO13B

CO13B

CO13B

CO13C

CO13C

CO13C

CO13D

CO13D

CO13D

DDM1CO13ACO13BCO13CCO13D

February 2002

– 37 –

(c)


February 2002

– 38 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

DD

CO14A

CO14B

CO14CCO14D

M1

δD

δ18O

Cross Section 14

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

DD

DD

DD

M1

M1

M1

CO14A

CO14A

CO14A

CO14BCO14B

CO14B

CO14C

CO14C

CO14C

CO14D

CO14D

CO14D

DDM1CO14ACO14BCO14CCO14D

February 2002

– 39 –

(c)


February 2002

– 40 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

D4

CO15B

CO15CDD

D4D

CO15A

δD

δ18O

Cross Section 15

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

CO15ACO15A

CO15A

CO15BCO15B

CO15B

CO15C

CO15C

CO15C

DD

DD

DD

M1

M1

M1

CO15ACO15BCO15CDDM1

February 2002

– 41 –

(c)


February 2002

– 42 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

DD

CO16B

CO16C

CO16D

ORD1 (CG3)CO16A

M1

δD

δ18O

Cross Section 16

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

ORD1

ORD1

ORD1

CO16A

CO16A

CO16A

CO16B

CO16B

CO16B

CO16C

CO16C

CO16C

CO16D CO16D

CO16D

DD

DD

DD

M1

M1

M1

ORD1CO16ACO16BCO16CCO16DDDM1

February 2002

– 43 –

(c)


February 2002

– 44 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

DD

CO17A

CO17CCO17D

CO17B

M1

δD

δ18O

Cross Section 17

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

CO17A

CO17A

CO17A

CO17BCO17B

CO17B

CO17C

CO17C

CO17C

CO17D

CO17D

CO17D

DD

DD

DD

M1

M1

M1

CO17ACO17BCO17CCO17DDD

M1

February 2002

– 45 –

(c)


February 2002

– 46 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

DD

CO18D

D7E2

D7

CO18ECO18A

CO18C

M1

CO18B

δD

δ18O

Cross Section 18

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium

(Na)+P

otassium(K

)

Sulfate(S

O4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

D7E2

D7E2

D7E2

D7E2

D7E2

D7E2

D7

D7

D7

CO18A

CO18A

CO18A

CO18B CO18B

CO18B

CO18C

CO18C

CO18C

CO18D

CO18D

CO18D

CO18ECO18E

CO18E

DD

DD

DD

M1

M1

M1

D7E2D7E2D7CO18ACO18BCO18CCO18DCO18EDDM1

February 2002

– 47 –

(c)


February 2002

– 48 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

D7

CO19A

D4DD

CO19B

CO19C

δD

δ18O

Cross Section 19

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

D4

D4

D4

D7

D7

D7

CO19A

CO19A

CO19A

CO19B

CO19B

CO19B

CO19C

CO19C

CO19C

DD

DD

DD

M1

M1

M1

D4D7CO19ACO19BCO19CDDM1

February 2002

– 49 –

(c)


Cations meq/l Anions90 80 70 60 50 40 30 20 10 10 20 30 40 50 60 70 80 90

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

D4

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

D7

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

CO19A

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

CO19B

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

CO19C

February 2002

– 50 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

DD

CO20A

CO20B

CO20CD6

CO20D

δD

δ18O

D6A

Cross Section 20

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

D6

D6

D6

D6

D6

D6

CO20ACO20A

CO20A

CO20B

CO20B

CO20B

CO20C

CO20C

CO20C

CO20D

CO20D

CO20D

DD

DD

DD

M1

M1

M1

D6D6CO20ACO20BCO20CCO20DDDM1

February 2002

– 51 –

(c)


Cations meq/l Anions10 5 5 10

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

D6

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

CO20A

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

CO20B

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

CO20C

Cl

HCO3+CO3

SO4

SiO2

NO3

Mn

Al

Cu

Fe

Mg

Ca

Na+K

CO20D

February 2002

– 52 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

DD

CO24A

CO24B

CO24C

M1

δD

δ18O

Cross Section 24

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

CO24ACO24A

CO24A

CO24B CO24B

CO24B

CO24CCO24C

CO24C

DD

DD

DD

M1

M1

M1

CO24ACO24BCO24CDDM1

February 2002

– 53 –

(c)

February 2002

– 54 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

CO25A

CO25B

CO25C

DD

J Kirby

M1

δD

δ18O

Cross Section 25

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

CO25A CO25A

CO25A

CO25B CO25B

CO25B

CO25C

CO25C

CO25C

DD

DD

DD

M1

M1

M1

CO25ACO25BCO25CDDM1

February 2002

– 55 –

(c)


February 2002

– 56 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

D8

CO27C

ORD14

CO4

ORD28 (PS1)ORD27 (PS3)

CO27ACO27B

DDM1

δD

δ18O

Cross Section 27

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

ORD14

ORD14

ORD14

ORD27

ORD27

ORD27

ORD28

ORD28

ORD28

CO4

CO4

CO4

CO5ACO5A

CO5ACO27A

CO27A

CO27A

CO27B

CO27B

CO27B

CO27C

CO27C

CO27C

DD

DD

DD

M1

M1

M1

ORD14ORD27ORD28CO4CO5ACO27ACO27BCO27CDDM1

February 2002

– 57 –

(c)


February 2002

– 58 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

CO29A

CO29B

CO29C

Cross Section 29δD

δ18O

DDM1

CO29D

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

CO28A

CO28A

CO28A

CO28B

CO28B

CO28B

CO28C

CO28C

CO28C

DD

DD

DD

M1

M1

M1

CO28ACO28BCO28CDDM1

February 2002

– 59 –

(c)


February 2002

– 60 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

CO29A

CO29B

CO29C

Cross Section 29δD

δ18O

DDM1

CO29D

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

CO29A

CO29A

CO29A

CO29B

CO29B

CO29B

CO29C

CO29C

CO29C

CO29D

CO29D

CO29D

DD

DD

DD

M1

M1

M1

CO29ACO29BCO29CCO29DDDM1

February 2002

– 61 –

(c)


February 2002

– 62 –

(a)

-8 -7 -6 -5 -4 -3 -2 -1 0

-60

-50

-40

-30

-20

-10

0

DD

CO30A

CO30B

M1

δD

δ18O

Cross Section 30

(b)

Ord River



Na+K HCO +CO3 3 Cl

Mg SO4


Sul

fate

(SO

4)+C

hlor

ide(

Cl)

Calcium

(Ca)+M

agnesium(M

g)

Car

bona

te(C

O3)

+Bic

arbo

nate

(HC

O3)

Sodium(N

a)+Potassium

(K)

Sulfate(SO4)M

agne

sium

(Mg)

80 60 40 20 20 40 60 80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

20

40

60

80

20

40

60

80

80

60

40

20

80

60

40

20


0 1,00

0

2,00

0

3,00

0

4,00

0

5,00

0

CO30ACO30A

CO30A

CO30B

CO30B

CO30B

DD

DD

DD

M1

M1

M1

CO30ACO30BDDM1

February 2002

– 63 –

(c)


Documents

Hydrochemical and Isotopic Characteristics of the Surface ... · Hydrochemical and Isotopic Characteristics of the Surface and Groundwater of the Hydrological Zones of the Ord Stage