physical properties of soils in the murrumbidgee and ... · and coleambally irrigation areas. csiro...

Physical Properties of Soils in the

Murrumbidgee and Coleambally Irrigation Areas

J. Hornbuckle and E. Christen

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

CSIRO Land and Water, Griffith NSW 2680

Technical Report 17/99 June 1999

II

PHYSICAL PROPERTIES OF SOILS IN THE

MURRUMBIDGEE AND COLEAMBALLY IRRIGATION

AREAS

J. Hornbuckle and E. Christen

CSIRO Land and Water

PMB 3

GRIFFITH NSW 2680

(02) 69 601500

Citation Details:

Hornbuckle, J. and Christen, E.(1999). Physical properties of soils in the Murrumbidgee

and Coleambally Irrigation Areas. CSIRO Land and WaterTechnical Report 17/99.

Copies of this report available from:

Publications or Information

CSIRO Land and Water

GPO Box 1666

CANBERRA ACT 2601

III

SUMMARY

There are over 90 different soil types mapped in the Murrumbidgee Irrigation Area

(MIA) and the Coleambally Irrigation Area (CIA). These soils have different

properties that are important for the design and establishment of irrigation and

farming systems and also for managing and sustaining existing farming systems.

In the past 30 years there have been over 80 studies into the physical properties of

these soils, which are important to manage and utilise the soils to their full extent. The

results of these studies have been documented in published and unpublished forms,

which have been difficult to access easily and quickly, so there was a need to bring all

this information together into a single document. The data from these studies has been

compiled in this report that should prove useful to farmers, farming advisors,

engineers and researchers with an interest in the soils of the region.

The soil properties, which were included in the review, were chosen by discussion

with likely users of the review: e.g., surveyors, resource mangers, farming advisors and

researchers. The soil properties that were included are: bulk density, texture (particle

size analysis ), porosity, infiltration, hydraulic conductivity, plant available water,

soil moisture characteristic, electrical conductivity (salinity), and exchangeable sodium

percent (sodicity). The properties chosen are most important for irrigated agriculture

in terms of water movement and retention.

The report breaks down the large number of individual soil types that occur in the

MIA and CIA into five broad soil groups that are:

1. Clays, which were further divided into self mulching and hard setting

clays

2. Red-brown earths, which were further divided into four subplasticity

classes

3. Transitional red brown earths

4. Sands over clay (solodized solonetz)

5. Deep sandy soils

IV

The soils that occur in each group are listed in the report. Data relating the soils in

each group have been listed and statistical information provided on the data for each

soil group. The information has also been presented in tables and graphs to show the

change in the soil property with depth. Having gathered and analysed all the data for a

particular soil group, a typical set of values for each soil property was established. In

some cases there was very little or no data for a particular soil property and thus a

typical value could not be determined. These typical values are intended to give

readers an indication of the values that might be expected for soils in that group.

These values are not statistically derived but are the authors’ interpretation of all the

data available.

The report also contains two CSIRO reports documenting studies on soil properties in

the CIA and MIA led by John Loveday in 1966 and 1978. The reports contain

valuable soil property information that was used in the review and also data on other

soil properties that were not included the review. A soil property reference list is also

included, as an appendix, showing the soil property information that was contained in

the 78 papers reviewed.

V

ACKNOWLEDGMENTS

Funding of a CSIRO summer studentship that enabled John Hornbuckle to undertake

this work by Mr A. van der Lely, Department of Land and Water Conservation,

Leeton, and Mr A. Parle of Parle Foods Pty. Ltd., Griffith, is gratefully acknowledged

We would also like to thank Mr. Geoff Beecher, NSW Agriculture, Leeton, for his

assistance in providing his bibliography of soils of the Riverina and Dr Warren

Muirhead for his assistance in grouping of soils.

We also would like to thank D. Smith, S. Prathapar and P. Charlesworth of CSIRO

Land and Water, Griffith for providing us with soils data.

We gratefully acknowledge the assistance of D. Skehan in editing this document.

VI

TABLE O F CONTENTS

1 INTRODUCTIO N ........................................................................................................................ 1

2 OBJECTIVE S............................................................................................................................... 3

3 METHODOLO GY ....................................................................................................................... 3

3.1 IDENTIFICATION OF IMPORTANT SOIL PROPERTIES...................................................................... 3

3.1.1 Data collection and selection........................................................................................... 6

3.1.2 Geomorphology of the Area............................................................................................. 7

3.1.3 Description and classification of the soils ....................................................................... 8

3.2 SOIL TYPES SORTED INTO SOIL GROUPS .................................................................................... 16

3.3 DATA ANALY SIS....................................................................................................................... 21

3.3.1 Particle size analysis...................................................................................................... 21

3.3.2 Bulk density and porosity............................................................................................... 21

3.3.3 Infiltration...................................................................................................................... 22

3.3.4 Hydraulic conductivity................................................................................................... 22

3.3.5 Moisture characteristics................................................................................................. 22

3.3.6 Electrical conductivities................................................................................................. 23

3.3.7 Exchangeable sodium percentage.................................................................................. 23

4 SELF MULCHIN G CLAY S...................................................................................................... 24

4.1 PHYSICAL COMPOSITION .......................................................................................................... 24

4.1.2 Water Movement ............................................................................................................ 32

4.1.3 Water Retention / Moisture Characteristic .................................................................... 35

4.1.4 Soil Salinity/Sodicity ...................................................................................................... 41

5 HARD SETTI NG CLAY S......................................................................................................... 45

5.1.1 Physical Composition..................................................................................................... 45

5.1.2 Water Movement ............................................................................................................ 48

5.1.3 Water Retention/Moisture Characteristic ...................................................................... 49


6 TRANSITIONAL RED BROWN EARTH S............................................................................ 53


6.1.2 Water Movement ............................................................................................................ 66



7 RED BROWN EARTH S............................................................................................................ 85

7.1 SOILS OF THE UPPER HILL SLOPES.............................................................................................. 85

7.1.1 Physical composition ..................................................................................................... 85

VII

7.1.2 Water Movement ............................................................................................................ 85

7.2 SOILS OF THE LOWER HILLSLOPES ............................................................................................ 86


7.3 WATER MOVEMENT ................................................................................................................. 90


7.4 SOILS OF THE PLAINS – SUBPLASTIC SUBSOIL GROUP................................................................ 94

7.4.1 Physical composition ..................................................................................................... 94

7.5 SOILS OF THE PLAINS (NORMAL SUBSOIL GROUP)..................................................................... 96


7.5.2 Water Movement .......................................................................................................... 102

7.5.3 Water Retention/Moisture Characteristic .................................................................... 105

7.5.4 Soil Salinity/Sodicity .................................................................................................... 109

8 SANDS OVER CLAY (SOLODIZED SOLONET Z SOILS) ............................................... 111

8.1.1 Physical composition ................................................................................................... 111

8.1.2 Water movement........................................................................................................... 118

8.1.3 Water Retention/Moisture Characteristic .................................................................... 120

8.1.4 Soil Salinity/Sodicity .................................................................................................... 124

9 DEEP SANDY SOIL S.............................................................................................................. 126

9.1.1 Physical Composition................................................................................................... 126

9.1.2 Water movement........................................................................................................... 127

9.1.3 Water Retention/Moisture Characteristic...................................................................... 128

10 TYPICAL S OIL PROPERTIES FOR SOIL GROUPS........................................................ 129

10.1 CLAY S ............................................................................................................................... 129

10.1.1 Self mulching clays....................................................................................................... 129

10.1.2 Hard setting clays ........................................................................................................ 132

10.2 TRANSITIONAL RED BROWN EARTHS.................................................................................. 134

10.2.1 Exchangeable sodium percentage................................................................................ 136

10.3 RED BROWN EARTHS ........................................................................................................ 137

10.3.1 Soils of the upper hillslopes......................................................................................... 137

10.3.2 Soils of the lower hillslopes.......................................................................................... 137

10.3.3 Soils of the plains (subplastic subsoil group)............................................................... 138

10.3.4 Plastic soils of the plains ( normal subsoil group)....................................................... 139

10.4 SANDS OVER CLAY............................................................................................................. 142

10.5 DEEP SANDS....................................................................................................................... 144

11 CONCLUSION......................................................................................................................... 147

12 BIBLIO GRAPHY..................................................................................................................... 148

VIII

TABLE O F FIGURES

FIGURE 1-1 LOCATION OF THE MIA AND CIA .......................................................................................... 1

FIGURE 3-1 DIAGRAMMATIC SCHEME OF THE CHARACTERISTIC SEQUENCE OF SOILS ON THE WIDGELLI

PARNA ............................................................................................................................................. 8

FIGURE 3-2 RELATIONSHIP OF SUBPLASTICITY TO TOPOGRAPHY IN THE BINGAR PARNA. SP(1), FIRST

DEGREE SUBPLASTICITY; SP(11), SECOND DEGREE SUBPLASTICITY; SP(111), THIRD DEGREE

SUBPLASTICITY; SP(111+), HARDPAN; NP, NORMAL PLASTICITY.................................................. 12

FIGURE 4-1 AVERAGE PARTICLE SIZE DISTRIBUTION WITH DEPTH FOR SELF MULCHING CLAYS.............. 27

FIGURE 4-2 CUMULATIVE PROBABILITY DISTRIBUTION OF PARTICLE SIZE OF SELF MULCHING CLAYS IN

THE 0-0.1 M LAYER ....................................................................................................................... 28

FIGURE 4-3 CUMULATIVE PROBABILITY DISTRIBUTION OF PARTICLE SIZE OF SELF MULCHING CLAYS IN

THE 0.2-0.3 M LAYER .................................................................................................................... 29

FIGURE 4-4 BULK DENSITY VARIATION WITH DEPTH FOR SELF MULCHING CLAYS.................................. 31

FIGURE 4-5 MEAN CUMULATIVE INFILTRATION CURVES FOR CLAYS TAKEN FROM VAN DER LELIJ AND

TALSMA (1977)............................................................................................................................. 32

FIGURE 4-6 CUMULATIVE PROBABILITY DISTRIBUTION OF HYDRAULIC CONDUCTIVITY ......................... 34

FIGURE 4-7 VOLUMETRIC MOISTURE CONTENT PROFILES OF A WUNNAMURRA CLAY ............................ 36

FIGURE 4-8 VARIATION OF VOLUMETRIC WATER CONTENTS AT 1500 kPA FOR SELF-MULCHING CLAY S 39

FIGURE 4-9 VARIATION OF VOLUMETRIC WATER CONTENTS AT 10 kPA FOR SELF-MULCHING CLAYS.... 41

FIGURE 4-10 ELECTRICAL CONDUCTIVITY VARIATION WITH DEPTH FOR SELF MULCHING CLAY S........... 42

FIGURE 4-11 ESP VARIATION WITH DEPTH FOR SELF MULCHING CLAYS................................................. 43

FIGURE 5-1 VARIATION OF BULK DENSITY WITH DEPTH FOR HARD SETTING CLAY S ............................... 47

FIGURE 5-2 VARIOUS VOLUMETRIC MOISTURE CONTENTS AT PERMANENT WILTING POINT.................... 50

FIGURE 5-3 VARIATION OF VOLUMETRIC MOISTURE CONTENTS AT FIELD CAPACITY FOR HARD SETTING

CLAYS ........................................................................................................................................... 51

FIGURE 5-4 SOIL MOISTURE CHARACTERISTIC CURVE FOR A BILLABONG CLAY TAKEN FROM SHARMA

(1971) ........................................................................................................................................... 52

FIGURE 6-1 AVERAGE PARTICLE SIZE DISTRIBUTION WITH DEPTH FOR TRANSITIONAL RED BROWN

EARTHS.......................................................................................................................................... 56

FIGURE 6-2 CUMULATIVE PROBABILITY DISTRIBUTION OF PARTICLE SIZE FOR TRANSITIONAL RED BROWN

EARTHS IN THE 0-0.1 M LAYER...................................................................................................... 59

FIGURE 6-3 CUMULATIVE PROBABILITY DISTRIBUTION OF PARTICLE SIZE FOR TRANSITIONAL RED BROWN

EARTHS IN THE 0.2-0.3 M LAYER................................................................................................... 59

FIGURE 6-4 VARIATION OF BULK DENSITY WITH DEPTH FOR TRANSITIONAL RED BROWN EARTHS......... 63

FIGURE 6-5 SHORT-TERM INFILTRATION DURING PONDING ON AN INITIALLY DRY SOIL.......................... 66

FIGURE 6-6 FREQUENCY DISTRIBUTION OF INFILTRATION TOTALS MEASURED OVER A 2-16 WEEK PERIOD

OF PERMANENT PONDING ON TRANSITIONAL RED BROWN EARTHS (VAN DER LELIJ AND TALSMA

1977)............................................................................................................................................. 67

FIGURE 6-7 CUMULATIVE INFILTRATION FOR TRANSITIONAL RED BROWN EARTHS AS MEASURED BY VAN

DER LELIJ AND TALSMA (1977)..................................................................................................... 68

IX

FIGURE 6-8 CUMULATIVE PROBABILITY DISTRIBUTIONS OF HYDRAULIC CONDUCTIVITIES OF

TRANSITIONAL RED BROWN EARTHS, AFTER LOVEDAY ET AL. (1978)............................................ 70

FIGURE 6-9 VARIATION OF VOLUMETRIC WATER CONTENTS AT 1500 kPA FOR TRANSITIONAL RED

BROWN EARTHS............................................................................................................................. 77

FIGURE 6-10 VARIATION OF VOLUMETRIC WATER CONTENTS AT 10 kPA FOR TRANSITIONAL RED BROWN

EARTHS.......................................................................................................................................... 79

FIGURE 6-11 VARIATION OF ELECTRICAL CONDUCTIVITY (MS/CM) WITH DEPTH.................................... 81

FIGURE 6-12 VARIATION OF ESP WITH DEPTH ....................................................................................... 84

FIGURE 7-1 AVERAGE PARTICLE SIZE DISTRIBUTION OF SOILS OF THE LOWER HILL SLOPES.................... 87

FIGURE 7-2 VARIATION OF BULK DENSITY (KG/M3) WITH DEPTH FOR SOIL OF THE LOWER HILLSLOPES.. 89

FIGURE 7-3 VOLUMETRIC MOISTURE CONTENT PROFILE OF A HANWOOD LOAM AS DETERMINED BY

MEYER (1992): “DRY END” = PERMANENT WILTING POINT, “WET END” = FIELD CAPACITY ......... 92

FIGURE 7-4 VOLUMETRIC MOISTURE CONTENT PROFILES OF A JONDARYAN LOAM, TALSMA (1963) ..... 93

FIGURE 7-5 CUMULATIVE PROBABILITY DISTRIBUTION OF PARTICLE SIZE IN PLASTIC SOILS OF THE

PLAINS, 0-0.1 M............................................................................................................................. 99

FIGURE 7-6 CUMULATIVE PROBABILITY DISTRIBUTION OF PARTICLE SIZE IN PLASTIC SOILS OF THE PLAINS

- NORMAL, 0.2-0.3 M................................................................................................................... 100

FIGURE 7-7 VARIATION OF DENSITY WITH DEPTH FOR SOILS OF THE PLAINS - NORMAL........................ 101

FIGURE 7-8 MEAN CUMULATIVE INFILTRATION CURVES (MM) FOR SOILS OF THE PLAINS – NORMAL, VAN

DER LELIJ AND TALSMA (1977)................................................................................................... 103

FIGURE 7-9 VARIATION OF VOLUMETRIC WATER CONTENTS AT 1500 kPA FOR PLASTIC SOILS OF THE

PLAINS......................................................................................................................................... 106

FIGURE 7-10 VARIATION OF VOLUMETRIC WATER CONTENTS AT FIELD CAPACITY............................... 108

FIGURE 7-11 VARIATION OF ESP WITH DEPTH FOR PLASTIC SOILS OF THE PLAIN ................................. 110

FIGURE 8-1 CUMULATIVE PROBABILITY DISTRIBUTION OF PARTICLE SIZE, 0-0.1 M.............................. 115

FIGURE 8-2 CUMULATIVE PROBABILITY DISTRIBUTION OF PARTICLE SIZE, 0.2-0.3 M........................... 115

FIGURE 8-3 VARIATION OF BULK AND AGGREGATE DENSITIES WITH DEPTH OF SANDS OVER CLAY SOILS

.................................................................................................................................................... 117

FIGURE 8-4 MEAN CUMULATIVE INFILTRATION DURING PONDING OF THULABIN AND COBRAM SANDY

LOAMS. FROM VAN DER LELIJ AND TALSMA (1977).................................................................... 118

FIGURE 8-5 VARIATION OF MOISTURE CONTENTS AT 1500 kPA FOR SANDS OVER CLAY ...................... 122

FIGURE 8-6 VARIATION OF MOISTURE CONTENTS AT 10 kPA ............................................................... 123

FIGURE 8-7 VARIATION OF ESP WITH DEPTH FOR SANDS OVER CLAY SOILS......................................... 125

FIGURE 9-1 VOLUMETRIC MOISTURE CONTENT PROFILES OF A BANNA SAND AT 1500 AND 10 kPA..... 128

FIGURE 10-1 AVERAGE PARTICLE SIZE DISTRIBUTION, 0.01 M. ............................................................ 145

FIGURE 10-2 AVERAGE PARTICLE SIZE DISTRIBUTION, 0.2 – 0.3 M. ..................................................... 145

FIGURE 10-3 CUMULATIVE INFILTRATION OVER A SIXTEEN WEEK PERIOD, 1: SOLIDIZED SOLONETZ

SOILS, 2: SELF MULCHING CLAY SOILS, 3: PLASTIC SOILS OF THE PLAINS, 4: TRANSITIONAL SOILS.

(VAN DER LELY AND TALSMA 1977) .......................................................................................... 146

FIGURE 10-4 AVAILA BLE WATER (MM) IN THE TOP 0.3 M OF SOIL FOR SELECTED SOIL GROUPS........... 146

X

LIST O F TABLES

TABLE 3-1 DESCRIPTIONS OF THE SOIL CATEGORIES .............................................................................. 15

TABLE 4-1 RANGES OF PARTICLE SIZE DISTRIBUTION FOR SELF-MULCHING CLAYS (LOVEDAY ET AL.

1966)............................................................................................................................................. 24

TABLE 4-2 RANGES OF PARTICLE SIZE DISTRIBUTION FOR SELF-MULCHING CLAYS (LOVEDAY ET AL.

(1978) ........................................................................................................................................... 25

TABLE 4-3 PARTICLE SIZE ANALYSIS OF SELF MULCHING CLAYS............................................................ 26

TABLE 4-4 STATISTICAL DATA RELATING TO PARTICLE SIZE ANALYSIS OF SELF-MULCHING CLAYS IN THE

0-0.1 M LAYER .............................................................................................................................. 27

TABLE 4-5 STATISTICAL DATA RELATING TO PARTICLE SIZE ANALYSIS OF SELF MULCHING CLAYS IN THE

0.2-0.3 M LAYER ........................................................................................................................... 28

TABLE 4-6 BULK DENSITIES OF SELF-MULCHING CLAYS ......................................................................... 30

TABLE 4-7 STATISTICAL ANALYSIS OF BULK DENSITY DATA OF SELF-MULCHING CLAYS (KG/M3) ........... 31

TABLE 4-8 STATISTICAL ANALYSIS OF HYDRAULIC CONDUCTIVITIES OF SELF-MULCHING CLAYS

(MM/DAY)...................................................................................................................................... 33

TABLE 4-9 HYDRAULIC CONDUCTIVITY FOR SELF-MULCHING CLAY DURING PONDING (MM/DAY).......... 35

TABLE 4-10 RANGES OF 1500 kPA MOISTURE CONTENTS (M 3/M3) OF SELF MULCHING CLAYS, LOVEDAY

ET AL. (1978) ................................................................................................................................. 37

TABLE 4-11 1500 kPA VOLUMETRIC MOISTURE CONTENTS OF SELF-MULCHING CLAY S.......................... 38

TABLE 4-12 STATISTICAL ANALYSIS OF VOLUMETRIC WATER CONTENTS AT 1500 kPA ......................... 38

TABLE 4-13 10 kPA VOLUMETRIC MOISTURE CONTENTS OF SELF-MULCHING CLAY S.............................. 40

TABLE 4-14 STATISTICAL ANALYSIS OF VOLUMETRIC WATER CONTENTS AT 10 kPA ............................. 40

TABLE 4-15 ESP FOR SELF-MULCHING CLAYS........................................................................................ 43

TABLE 4-16 ANALYSIS OF ESP DATA OF SELF-MULCHING CLAYS........................................................... 44

TABLE 5-1 PARTICLE SIZE DISTRIBUTION OF HARD SETTING CLAYS........................................................ 45

TABLE 5-2 BULK DENSITIES OF HARD SETTING CLAYS............................................................................ 46

TABLE 5-3 HYDRAULIC CONDUCTIVITY OF A BILL ABONG CLAY (SHARMA 1972) .................................. 48

TABLE 5-4 PERMANENT WILTING POINT VOLUMETRIC MOISTURE CONTENTS FOR HARD SETTING CLAY S50

TABLE 5-5 VOLUMETRIC MOISTURE CONTENT MEASUREMENTS AT FIELD CAPACITY FOR HARD SETTING

CLAYS ........................................................................................................................................... 51

TABLE 5-6 ELECTRICAL CONDUCTIVITIES OF HARD SETTING CLAYS...................................................... 52

TABLE 6-1 RANGES OF PARTICLE SIZE ANALYSIS FOR TRANSITIONAL RED BROWN EARTHS

LOVEDAY ET AL. (1978)................................................................................................................ 53

TABLE 6-2 RANGES OF PARTICLE SIZE DISTRIBUTION FOR TRANSITIONAL RED BROWN EARTHS, LOVEDAY

ET AL. (1966). ................................................................................................................................ 54

TABLE 6-3 PARTICLE SIZE DISTRIBUTION OF TRANSITIONAL RED BROWN EARTHS.................................. 57

TABLE 6-4 STATISTICAL DATA RELATING TO PARTICLE SIZE ANALYSIS OF TRANSITIONAL RED BROWN

EARTHS FOR THE 0-0.1 M LAYER ................................................................................................... 58

TABLE 6-5 STATISTICAL DATA RELATING TO PARTICLE SIZE ANALYSIS OF TRANSITIONAL RED BROWN

EARTHS FOR THE 0.2-0.3 M LAYER ................................................................................................ 58

XI

TABLE 6-6 BULK DENSITIES OF TRANSITIONAL RED BROWN EARTHS...................................................... 62

TABLE 6-7 STATISTICAL DATA RELATING TO BULK DENSITIES OF TRANSITIONAL RED BROWN EARTHS

(KG/M3) ......................................................................................................................................... 63

TABLE 6-8 POROSITY OF MARAH CLAY L OAM AS FOUND BY MCINTYRE ET AL. (1982) .......................... 64

TABLE 6-9 POROSITY MEASUREMENTS OF TRANSITIONAL RED BROWN EARTHS (M3/M3). LOVEDAY ET AL.

(1966) ........................................................................................................................................... 65

TABLE 6-10 TOTAL POROSITY OF TUPPAL CLAY (M3/M3), TALSMA (1963) ............................................. 65

TABLE 6-11 INFILTRATION RATES (MM/DAY) AS MEASURE BY LOVEDAY ET AL. (1984) ......................... 68

TABLE 6-12 STATISTICAL DATA RELATING TO SATURATED HYDRAULIC CONDUCTIVITIES OF

TRANSITIONAL RED BROWN EARTHS AS DETERMINED BY LOVEDAY ET AL. (1978) ........................ 69

TABLE 6-13 SATURATED HYDRAULIC CONDUCTIVITY (MM/DAY) MEASURED BY LOVEDAY ET AL. (1984)

...................................................................................................................................................... 71

TABLE 6-14 HYDRAULIC CONDUCTIVITY (MM/DAY) AND ITS VARIATION WITH TIME DURING PONDING,

MCINTYRE ET AL. (1982)............................................................................................................... 72

TABLE 6-15 POTENTIAL GRADIENT AND HYDRAULIC CONDUCTIVITY OF A TRANSITIONAL RED BROWN

EARTHS DURING PONDING, VAN DER LELIJ AND TALSMA (1977) .................................................. 72

TABLE 6-16 ESTIMATED HYDRAULIC CONDUCTIVITY OF A WILLBRIGGIE CLAY LOAM WITH A HIGH

WATERTABLE, SIDES ET AL 1993. .................................................................................................. 73

TABLE 6-17 AVAILABLE WATER OF A TUPPAL CLAY, TALSMA (1963) ................................................... 74

TABLE 6-18 RANGES OF 1500 KPA MOISTURE CONTENTS (M3/M3) OF TRANSITIONAL RED BROWN EARTHS,

LOVEDAY ET AL. (1966) ................................................................................................................ 75

TABLE 6-19 RANGES OF 1500 kPA MOISTURE CONTENTS (M 3/M3) FOR TRANSITIONAL RED BROWN

EARTHS, LOVEDAY ET AL. (1978).................................................................................................. 75

TABLE 6-20 1500 kPA MOISTURE CONTENTS (M 3/M3) OF TRANSITIONAL RED BROWN EARTHS............... 76

TABLE 6-21 STATISTICAL DATA RELATING TO 1500 kPA VOLUMETRIC MOISTURE CONTENT STUDIES ON

TRANSITIONAL RED BROWN EARTHS.............................................................................................. 77

TABLE 6-22 10 kPA MOISTURE CONTENTS (M 3/M3) OF TRANSITIONAL RED BROWN EARTHS AS MEASURED

BY LOVEDAY ET AL. (1966) ........................................................................................................... 78

TABLE 6-23 10 kPA VOLUMETRIC MOISTURE CONTENTS (M 3/M3) OF TRANSITIONAL RED BROWN EARTHS

...................................................................................................................................................... 78

TABLE 6-24 STATISTICAL DATA RELATING TO 10 kPA VOLUMETRIC MOISTURE CONTENT (M 3/M3)

STUDIES ON TRANSITIONAL RED BROWN EARTHS .......................................................................... 79

TABLE 6-25 MEAN ELECTRICAL CONDUCTIVITIES (MS/CM) OF TRANSITIONAL RED BROWN EARTHS

LOVEDAY ET AL. (1978)................................................................................................................. 80

TABLE 6-26 STATISTICAL DATA RELATING TO ELECTRICAL CONDUCTIVITY (MS/CM) OF TRANSITIONAL

RED BROWN EARTHS...................................................................................................................... 82

TABLE 6-27 ESP OF TRANSITIONAL RED BROWN EARTHS....................................................................... 83

TABLE 6-28 STATISTICAL DATA RELATING TO ESP OF TRANSITIONAL RED BROWN EARTHS.................. 84

TABLE 7-1 HYDRAULIC CONDUCTIVITIES (MM/DAY) OF SUB-PLASTIC SOILS OF THE UPPER HILLSLOPES,

AFTER VAN DER LELIJ (1974). ....................................................................................................... 86

XII

TABLE 7-2 PARTICLE SIZE DISTRIBUTIONS OF SOILS OF THE LOWER HILLSLOPES.................................... 87

TABLE 7-3 BULK DENSITIES OF SOILS OF THE LOWER HILL SLOPES.......................................................... 88

TABLE 7-4 HYDRAULIC CONDUCTIVITIES (MM/DAY) OF SOILS OF THE LOWER HILL SLOPES, AFTER VAN

DER LELIJ (1974)........................................................................................................................... 91

TABLE 7-5 10 AND 1500 kPA VOLUMETRIC MOISTURE CONTENTS OF JONDARYAN LOAM, TALSMA

(1963) ........................................................................................................................................... 93

TABLE 7-6 PARTICLE SIZE DISTRIBUTION OF PLASTIC SOILS OF THE PLAINS, AFTER SINCLAIR ET AL (1994)

...................................................................................................................................................... 94

TABLE 7-7 MEAN BULK DENSITIES (KG/M3) OF INTACT CORES (0 – 5 CM) AT DISTANCES AWAY FROM THE

VINE ROW FOR PLASTIC SOILS OF THE PLAINS................................................................................ 95

TABLE 7-8 HYDRAULIC CONDUCTIVITIES (MM/DAY) OF SUB SOIL PLASTIC SOILS OF THE PLAINS, AFTER

VAN DER LELIJ (1974). .................................................................................................................. 96

TABLE 7-9 RANGES OF PARTICLE SIZE DISTRIBUTION FOR PLASTIC SOILS OF THE PLAINS LOVEDAY ET AL.

(1966) ........................................................................................................................................... 97

TABLE 7-10 RANGES OF PARTICLE SIZE FOR SOILS OF THE PLAINS, LOVEDAY ET AL. (1978) .................. 97

TABLE 7-11 PARTICLE SIZE DISTRIBUTION OF SOILS OF THE PLAINS – NORMAL ...................................... 98

TABLE 7-12 STATISTICAL DATA RELATING TO SIZE ANALY SIS OF PLASTIC SOILS OF THE PLAINS –

NORMAL, IN THE 0-0.1 M LAYER.................................................................................................... 98

TABLE 7-13 STATISTICAL DATA RELATING TO PARTICLE SIZE ANALY SIS OF SOILS OF THE PLAINS –

NORMAL, IN THE 0.2-0.3 M LAYER................................................................................................. 99

TABLE 7-14 DENSITIES OF PLASTIC SOILS OF THE PLAINS – NORMAL (KG/M3) ...................................... 101

TABLE 7-15 HYDRAULIC CONDUCTIVITY (MM/DAY) OF SOILS OF THE PLAINS – NORMAL, VAN DER LELIJ

AND TALSMA (1977) ................................................................................................................... 104

TABLE 7-16 POTENTIAL GRADIENT AND HYDRAULIC CONDUCTIVITY OF TWO SOILS OF THE PLAINS –

NORMAL, DURING PONDING, VAN DER LELIJ (1974).................................................................... 105

TABLE 7-17 1500 kPA MOISTURE CONTENTS (M 3/M3) OF NORMAL SOILS OF THE PLAINS...................... 106

TABLE 7-18 STATISTICAL DATA RELATING TO STUDIES ON 1500 kPA VOLUMETRIC MOISTURE CONTENTS

FOR NORMAL PLAINS SOILS.......................................................................................................... 107

TABLE 7-19 10 kPA VOLUMETRIC MOISTURE CONTENTS OF PLASTIC SOILS OF THE PLAIN.................... 108

TABLE 7-20 STATISTICAL DATA RELATING TO FIELD CAPACITIES OF PLASTIC SOILS OF THE PLAINS..... 109

TABLE 7-21 ELECTRICAL CONDUCTIVITIES (MS/CM) OF PLASTIC SOILS OF THE PLAINS LOVEDAY ET AL.

(1978) ......................................................................................................................................... 109

TABLE 7-22 ESP OF NORMAL PLAINS SOILS.......................................................................................... 110

TABLE 8-1 RANGES OF PARTICLE SIZE DISTRIBUTION FOR SANDS OVR CLAY SOILS LOVEDAY (1966) .. 111

TABLE 8-2 RANGES OF PARTICLE SIZE DISTRIBUTION FOR SANDS OVER CLAY SOILS LOVEDAY ET AL.

(1978) ......................................................................................................................................... 112

TABLE 8-3 PARTICLE SIZE DISTRIBUTION OF SOLODIZED SOLONETZ SOILS........................................... 113

TABLE 8-4 STATISTICAL DATA RELATING TO PARTICLE SIZE ANALYSIS OF SOLODIZED SOLONETZ SOILS,

0-0.1 M........................................................................................................................................ 114

XIII

TABLE 8-5 STATISTICAL DATA RELATING TO PARTICLE SIZE ANALYSIS OF SOLODIZED SOLONETZ SOILS,

0.2-0.3 M..................................................................................................................................... 114

TABLE 8-6 BULK AND AGGREGATE DENSITIES OF SANDS OVER CLAY SOILS......................................... 116

TABLE 8-7 POTENTIAL GRADIENT AND HYDRAULIC CONDUCTIVITY OF A SANDS OVER CLAY SOIL DURING

PONDING...................................................................................................................................... 119

TABLE 8-8 MEAN HYDRAULIC CONDUCTIVITIES (MM/DAY) OF SANDS OVER CLAY SOILS IN THE

MIRROOL IRRIGATION AREA, VAN DER LELIJ (1974)................................................................... 120

TABLE 8-9 VOLUMETRIC WATER CONTENTS AT 1500 kPA FOR SANDS OVER CLAY .............................. 121

TABLE 8-10 ANALY SIS OF MOISTURE CONTENTS AT 1500 kPA FOR SANDS OVER CLAY ....................... 122

TABLE 8-11 VOLUMETRIC WATER CONTENTS AT 10 kPA ..................................................................... 123

TABLE 8-12 ANALY SIS OF MOISTURE CONTENTS AT 10 kPA................................................................. 124

TABLE 8-13 ELECTRICAL CONDUCTIVITY OF SANDS OVER CLAY SOILS (MS/CM).................................. 124

TABLE 8-14 ESP OF SANDS OVER CLAY SOILS...................................................................................... 125

TABLE 9-1 HYDRAULIC CONDUCTIVITY (MM/DAY) OF A DEEP SANDY SOIL .......................................... 127

TABLE 10-1 TYPICAL VALUES OF PROPERTIES OF SELF MULCHING CLAYS............................................ 132

TABLE 10-2 TYPICAL VALUES OF PROPERTIES OF HARD SETTING CLAY S.............................................. 133

TABLE 10-3 TYPICAL VALUES OF PROPERTIES OF TRANSITIONAL RED BROWN EARTHS........................ 136

TABLE 10-4 TYPICAL VALUES OF PROPERTIES OF SOILS OF THE LOWER HILLSLOPES............................ 138

TABLE 10-5 TYPICAL VALUES OF PROPERTIES OF SUBPLASTIC SOIL OF THE HILL SLOPES...................... 139

TABLE 10-6 TYPICAL VALUES OF NORMAL SOILS OF THE PLAINS.......................................................... 141

TABLE 10-7 TYPICAL VALUES OF PROPERTIES OF SOLODIZED SOLONETZ SOILS.................................... 144

TABLE 10-8 TYPICAL VALUES OF PROPERTIES OF DEEP SANDS............................................................. 144

1

1 INTRODUCTION

The Murrumbidgee Irrigation Area (MIA) and Coleambally Irrigation Area (CIA) lie on

the north eastern region of the Riverine plain. This is part of the Murray Darling Basin,

the major catchment area of New South Wales. The MIA and CIA are irrigated from

water diverted from the Murrumbidgee River, supplied by large catchment dams located

in the Snowy Mountains. A locality map is shown in figure 1.1.

Figure 1-1 Location of the MIA and CIA

Soils are essential for farming, and knowledge of soil physical properties is essential to

manage and utilise soils to their full extent. The MIA and CIA are reliant on farming

enterprises for income, hence knowledge of soil physical properties is important, not only

2

in design and establishment of irrigation systems, but also for managing and sustaining

the farming systems using predictive models and research.

This review has been undertaken to bring together soil physical property data for the MIA

and CIA, previously documented in published and unpublished forms, into a single

publication and to establish, where possible, general ranges of soil physical properties

within soil groups which have similar characteristics.

Information on soil physical properties can be difficult and time consuming to locate, in

many cases the information being located in unpublished reports and technical

memorandums which are difficult to access. Therefore, there existed a need to update this

information and compile it into a more useable format.

3

2 OBJECTIVES

The objectives of this review were to:

1/ Determine what data was available for soil properties in the MIA and CIA.

2/ Determine the soil physical data most useful to end users.

3/ Compile the available data.

4/ Determine characteristic values for properties of soils.

3 METHODOLOGY

3.1 Identification of important soil properties

The soil properties reviewed in this report were selected by correspondence with likely

end users (e.g. surveyors, engineers, researchers and resource managers) of the data, and

through verbal discussion with relevant CSIRO staff, Griffith. The initial facsimile

survey sent to likely end users is included as appendix 1.

The survey tried to identify particular soil physical properties which were of importance

to users of the data, and asked participants to place soil physical properties into three

categories. These were:

• major importance;

• secondary importance;

• not important;

Responses to the surveys were received from seven people also listed in appendix 1.

Responses varied considerably between correspondents, from which it was decided to

review soil properties in four major areas, which were:

4

1/ Soil physical composition

• Particle size analysis

• Bulk density

• Porosity

2/ Water movement

• Infiltration

• Hydraulic conductivity

3/ Water retention/moisture characteristic

• Available water

• Moisture characteristic

4/ Soil salinity/sodicity

• Electrical conductivity

• Exchangeable sodium percentage

The properties chosen above are the most important for irrigated agriculture in terms of

water movement and retention.

Particle size distribution influences qualities such as infiltration, moisture and nutrient

retention, drainage and soil susceptibility to erosion. Knowledge of the particle size

distribution can also give a general indication of other soil properties which may not be

known, such as hydraulic conductivity and moisture characteristics.

The bulk density of soil is important as excessively high bulk densities inhibit root

penetration and impede drainage. Infiltration and permeability rates are also affected by

bulk density.

Porosity refers to the nature and amount of voids between and within particles. An

abundance of large air filled pores is associated with stable aggregates and a productive

5

soil. Porosity also has an effect on other soil properties such as infiltration and hydraulic

conductivity.

Infiltration is a particularly important soil property and serves as a guide to the most

appropriate method of irrigation. It is also important in irrigation design and has a major

control on size of basin or length of furrow and the optimum rate of water application.

Hydraulic conductivity is used to assess waterlogging problems and as the basis of

designing in-field and regional drainage. Knowledge of hydraulic conductivity is also

particularly important in assessing possible problems due to high watertables.

Water retention and moisture characteristics of soils indicate the capacity of a soil to

retain water for plants. Irrigation scheduling depends on the amount of water available to

plants and schedules are based on the amount of water available in particular soils.

Measurements of available water are generally taken as the difference in water content of

the soil between field capacity and permanent wilting point. Field capacity may be

defined as the amount of water held in the soil after drainage under gravity, Dent and

Young (1981). In freely draining soils field capacity is reached within a few hours of

saturation. In silts and clays equilibrium is reached only after a considerable time. For

most crops the lower limit of available water, permanent-wilting point, corresponds to a

soil water tension of 1500 kPa.

Electrical conductivity measurements were included in order to assess the soils possible

salinity problems. It should be remembered however that soil salinity can change rapidly,

it can be reduced by leaching, or can increase by rising groundwater or inadequate

drainage.

Exchange sodium percentages were also included in the review to assess sodicity, which

has a great influence on the stability of the soil and hence hydraulic conductivity and soil

moisture retention.

6

3.1.1 Data collection and selection

In determining available data relating to soil physical properties in the MIA and CIA,

initial searches were conducted on an unpublished soil database being constructed by Mr.

Geoff Beecher at NSW Agriculture, Yanco. The database contained 691 references to soil

studies undertaken in the NSW Riverina. Key search words included each selected soil

property along with associated terms such as Murrumbidgge Irrigation Area,

Coleambally Irrigation Area, soil properties, soil characteristics, soil groups and relevant

authors along with other associated terms. Selected papers were then analysed and those

which documented physical soil properties were collected. Searches of the CSIRO

Structured Information Manager (SIM) database were also made using the keywords

mentioned above.

The results from the searches of SIM and Mr Beechers database were then compiled and

manual searches made on the bibliography of each paper for further references. Sources

of reference material relating to soil properties were also asked for in the fax survey of

potential users of the review, however responses were limited.

Reports and papers were chosen based on the suitability of the material for inclusion in

the review. This was determined on a number of factors:

1/ Accurate identification of the soil type, so that the data could be associated with a

particular soil group. In some cases information on particular soil properties was found

however this information was not linked to a particular soil type.

2/ Soil properties over a range of soil types or a large number of soil properties, in one

paper, were used in the review for one particular soil type.

3/ The purpose of the study was considered, studies which were undertaken for the sole

purpose of determining soil properties, were chosen in preference to those, which

measured limited soil properties to support other research.

7

4/ The methodology used to measure particular soil properties was also considered when

reviewing data and emphasis was placed on collecting reports which were comparable on

a property basis. For example only electrical conductivities of 1:5 solution extracts were

collected.

5/ The relative importance of the soil e.g. area covered, economical importance, was

considered.

In total 78 references of published literature were collected and used in this review along

with some unpublished data from CSIRO staff.

3.1.2 Geomorphology of the Area

The MIA and CIA both lie on the Riverine plain of south eastern Australia across which

the Lachlan, Murrumbidgee, and Murray rivers flow. This alluvial plain is built up of

sediments from ancient streams. These sedimentary deposits are interbedded with wind

blown clay deposits known as parna, Butler and Hutton, (1956).

Butler and Hutton (1956) indicated the occurrence of three periods of parna deposition,

each being followed by a period of soil development. Between each parna deposition

there was a sporadic deposition of riverine materials associated with erosion, but lack of

soil development on these indicated that the riverine phases were followed closely by the

next parna deposition. The lowest and hence oldest deposition and soil forming phase is

called the Cocoparra, van Dijk (1958). The next deposition of parna and its associated

riverine material is called Barellan. The final deposition forms the greater part of the

present day land surface and is called the Widgelli parna and its related riverine material

is called Hanwood. Within the MIA a characteristic phase of the Widgelli parna occurs,

known as the Tabbita phase

.

8

Highly differentiated soils occur on the parna layer and these include brown solodized

soils in the dune zones, red-brown earths on the hills, and red-brown earths and grey and

brown soils of heavy texture on the riverine plains. The variation in soil types is caused

by belts of riverine alluvium of varying width traversing the parna, variations in depth of

the Widgelli parna sheet, fuluviatile-colluvial modifications of varying degree,

differences in age of fluviatile deposits and drainage conditions which determine the

main characteristics of the landscape and its soils, van Dijk (1961). A schematic diagram

of the characteristic sequence of soils on the Widgelli parna is shown in figure 3.1.

Figure 3-1 Diagrammatic scheme of the characteristic sequence of soils on the

Widgelli parna

3.1.3 Description and classification of the soils

The above investigation of the geomorphology of the area and review of the soil surveys

by van Dijk (1958), Stannard (1970), Taylor and Hooper (1938) and van Dijk (1961),

revealed that although there were at least 94 different soil types mapped within the CIA

and MIA, the soils could be grouped together based on morphological similarity and

recurrent patterns of associations. The soils of the area were found to fit into the

9

following five broad soil groups, which were then subdivided on prominent soil

characteristics. These 5 groups were:

1. Clays

2. Red Brown Earths

3. Transitional red brown earths Red Brown Earths

4. Sands over Clay

5. Deep Sands

Typical properties of each of the soil groups are shown in Table 3.1.

3.1.3.1 Clays

There are both grey and brown clays which have been kept together, however, two sub

groups have been made. Those with crumbly calcareous surface horizons (self-mulching

clays) and those with massive non-calcareous surface soils (hard setting clays).

A) Self-mulching clays

These crumbly soils show virtually no change in texture from the surface downward with

approximately 50-60% clay throughout. The fine aggregation of the surface soil gives the

“self-mulching” property and is usually best developed when dry. In some instances the

surface soil may be somewhat crusted but usually the crust is easily broken up. All soil

profiles have in common very aggregated and dense subsoil.

Van Dijk and Talsma (1964) found that lime percentages for the upper limit of 10 gilgai

soils were found to vary between 0.5% and 2%, occasionally reaching 3.5%, with slightly

higher figures for the deeper sub soil. Table 3.1 shows a typical profile of a self-mulching

clay.

10

B) Hard setting clays

The texture of their dense surface clay horizons is slightly lighter than that of the subsoil;

lime concentrations are only encountered in small quantities below 0.45 m. The main soil

type representing this sub group is Riverina clay.

3.1.3.2 Red-brown earths

This group comprises soils with a texture contrast profile, with a loamy or sandy surface

soil more than 0.1 m deep, changing abruptly to clay subsoil. The surface soil may have a

weakly developed bleached zone in the lower part, while the subsoil is relatively dense to

well structured and may be subplastic. A typical profile is shown in table 3.1.

An important characteristic of these soils is a property called subplasticity. Subplastic

clays were described by Butler (1976) who stated: ‘These clays have the consistence

properties of gravels, sands or loams; indeed the farmers refer to them as gravels and in

their influence on drainage they seem to behave as gravels. During the manipulation of

field texturing their apparent clayiness increases progressively until, at the end of five

minutes it fully corroborates the mechanical analysis figures for heavy clay’. The

property of subplasticity when highly developed imparts to the particular soil high

mechanical and chemical stability and hence great resistance to puddling or dispersion.

The implication is that abnormal cementation of particles occurs, McIntyre (1976).

Butler (1976) found that subplastic soils seem to be associated with aeolian clay (parna)

mantles of regional extent, but not all exposures of parna are subplastic: those on the

flatter and poorly drained sites are fully plastic. He also found a variation in the

subplasticity with the age of the parna: there are three successive parna mantles and the

stratigraphically older ones expressed a higher degree of subplasticity than the younger

ones, Butler (1976).

11

In the MIA subplasticity in the soil types is found to be strongly related to success in

irrigated horticulture, Talyor and Hooper, (1938). Therefore a red-brown earth, which has

subplastic properties, is markedly different to a red-brown earth, which is plastic, the

chemical and physical properties differ greatly. In order to group soils, which have

similar physical and chemical properties a greater degree of differentiation between red-

brown earths was required.

Subdivision of subplasticty was done by van Dijk (1958) who defined four degrees:

1/ First degree sub plasticity (SP1): The material works up by one textural grade during

kneading for a few minutes, e.g. from loam to clay loam, or from light to medium clay.

2/ Second degree sub plasticity (SP11): The material works up by two or more textural

grades, e.g. from loam to medium clay.

3/ Third degree subplasticity (SP111): The material feels like grit or coarse sand and can

be puddled by hand only with great difficulty to show its real texture. e.g. medium clay

A fourth degree of subplasticity has also been noted for highly sub plastic materials

SP111+.

These degrees of subplasticity have been used in this report to further differentiate

between red-brown earth soil types.

A high degree of subplasticity occurs only with good internal drainage. The same

material may exhibit normal plastic properties or subplasticity of any degree depending

on the drainage conditions. Therefore soils on hillslopes have a higher degree of

subplasticity than similar soils of the plains. Subplastic soils of a lower degree may

develop on the plains due to smaller micro relief or a thinner underlying parna layer

which is particularly permeable and allows freer drainage of the upper soil layers,

however red-brown earths of the plains rarely exceed a subplasticity degree greater than

SP(1), van Dijk (1958). The relationship between the degree of subplasticity and drainage

12

conditions is shown in figure 3.2. This shows the relationship between subplasticity and

topography in the Bingar parna layer, which underlies the Tabbita parna layer.

Figure 3-2 Relationship of subplasticity to topography in the Bingar parna. SP(1),

first degree subplasticity; SP(11), second degree subplasticity; SP(111), third degree

subplasticity; SP(111+), hardpan; NP, normal plasticity

Therefore three subgroups of red-brown earths were established using subplasticity

degrees as defined by van Dijk (1958). These sub groups were soils of the hillslopes,

soils of the lower hillslopes and soils of the plains. The soils of the plains have further

been divided into those with a lighter subsoil, which may be slightly subplastic and those

with normal subsoil which are fully plastic.

13

Subplastic soils of the upper hillslopes have subplasticity degrees of SP(111) and

SP(111+), while subplastic soils of the lower hillslopes have subplasticty degrees

between SP(11) and SP(111). Plastic soils of the plains, which have a lighter subsoil,

correspond to a subplasticty degree of SP(1), while the normal subsoil subgroup are fully

plastic.

3.1.3.3 Transitional red-brown earths

Transitional red brown earths are soils between clays and red-brown earths. The depth of

the surface horizon of this group is only 0.08-0.1 m. The distribution of lime in the

subsoil is similar to that of red brown earth’s and there is sometimes gypsum in the deep

subsoil, particularly in the west of the CIA, van Dijk and Talsma (1964). The transitional

red brown earths are the dominant soils of the plains, occurring in the highest proportion

in the western and south western sections of the CIA.

3.1.3.4 Sands over clay

The soils of this group are solodized solonetz soils, having a marked texture contrast

between light surface soils and heavy subsoils. The surface soils are quite variable in

texture but are mostly sandy and the subsoils are generally very dense clays. The depth of

the A horizon is variable from 0.13-0.6 m, with 0.2-0.3 m being the most common. Some

surface horizons have a pronounced bleached zone in the lower part.

The characteristic feature of this group is the dense, coarsely structured clay subsoil.

Under dry conditions this tough clay may be broken by wide vertical cracks into columns

with a rounded top and these columns are frequently capped with a thin bleached sandy-

silty layer which is very brittle and powdery when dry, van Dijk and Talsma, (1964).

14

3.1.3.5 Deep sandy soil

The surface sand of these profiles is usually more than 0.9 m deep and the color is

relatively uniform brown or pale grey-brown. A few centimeters at the surface are

somewhat darker owing to the accumulation of organic matter and the brown color of the

subsoil usually becomes more yellow with depth. The subsoil may contain several clay

bands or a single sandy clay layer, there are sometimes slight amounts of lime and there

may be bleached and cemented zones. Some profiles are undifferentiated sand to a depth

of 3-4.5 m and more. The majority of the deep sands are of aeolian origin and occur as

high and low dunes.

15

Table 3-1 Descriptions of the soil categoriesFeature Self-

mulching

clays

Hard setting

clays

Red-brown

earths

Transitional

red brown

earths red-

brown earths

Sands over

Clay

Deep sands

Topsoil Self-

mulching

Hard setting Loam Loam to clay

loam

Sand to

loam

Sand

Depth 5-15cm 5cm or less 10-25cm Less than

10cm

25-100cm 100cm or

more

Subsoil Heavy clay

with lime

Heavy clay Heavy clay Heavy clay Cemented

clayey sand

above a

mottled

medium

clay

Mottled

clayey sand

grading to

light clay

Deep

subsoil

(1-2m)

Medium clay

with

concretionar

y lime

Medium clay,

often with

crystalline

gypsum

Sandy clay,

often

micaceous

Medium clay,

often with

crystalline

gypsum

Medium

clay

sometimes

becoming

more sandy

with depth

Light clay

Example Yooroobla

clay

Riverina clay Cobram

loam

Willbriggie

loam

Danberry

sand

Sandmount

sand

(After personal communication, Muirhead 1998)

16

3.2 Soil types sorted into soil groups

All the soils of the CIA and MIA as surveyed by van Dijk (1958), Stannard (1970),

Taylor and Hooper (1938) and van Dijk (1961) have been placed in the following groups.

The horticultural soils are shown with an ‘H’ and the codes following some soils are the

Northcote codes (Northcote, 1979) to which the soils have been mapped by various

authors.

1) Clays:

1a) Self mulching clays:

Coleambally Clay Ug5.24, Ug5.28

Gogeldrie Clay

Gundaline Clay

Toganmain clay

Wunnamurra Clay Ug5.24, Ug 5.28, Ug5.34

Yooroobla Clay. Ug 5.34

These clays have a heavier surface texture and calcareous surface horizon which breaks

down to small aggregates under wetting and drying

1b) Hard setting clays:

Billabong Clay

Crommelin Clay

Goolgumbla Clay

Riverina Clay. Ug5.6, Ug5.5

Wandook Clay

17

These are clays which have the texture of their dense surface horizons slightly lighter

than that of the subsoil. Lime concentrations are not encountered until depths below 0.45

m

2) Red Brown Earths:

2a) Soils of the upper hillslopes:

Ballingall loam H

Lakeview loam H

Merungle loam H

Tharbogang loam H

Wyangan loam H

These soils have subplasticity classes SP(111) and SP(111+)

2b) Soils of the lower hillslopes:

Bilbul clay loam H

Griffith clay loam H

Hanwood sandy loam and loam H

Jondaryan loam and clay loam H

Stanbridge sandy loam and loam H

Yenda sandy loam and loam H

Type 9 H

These soils have subplasticity classes SP(11) and SP(111)

2c) Soils of the plains:

Subplastic group:

Bilbul loam H

Fivebough sandy loam H

Griffith loam H

18

Mirrool loam H

Willimbong loam H

Yoogali loam H

Thulablin clay loam

These are plastic soils of the plains with subplasticity SP(1), the lighter subsoil group

Normal group:

Beelbangera clay loam

Camarooka clay loam H

Camarooka sandy loam H

Leeton clay loam H

Types 8,12,13 H

Birganbigill cl ay loam

Birganbigil sandy loam Dr1.13, Dr1.33, Dr2.23

Birarbigill loam

Bundure loam

Cobram sandy loam Dr2.23

Danberry clay loam

Finley loam

Marah sandy loam

Moira loam

Mundiwa sandy loam

Thulabin loam

Thulabin sandy loam Dr2.23

Tuppal loam

Willbriggie loam Dr1.33

These are plastic soils of the plains without subplasicity, they are the ‘normal’ subsoil

group

19

3) Transitional Red Brown Earths:

Coree loam

Coree clay loam

Marah loam Dr2.13

Marah clay loam Dr2.13, Dr2.33

Morago clay

Morago clay loam

Mundiwa clay loam

Tuppal clay

Tuppal clay loam Dd1.33, Dy2.3

Willbri ggie clay Dr2

Willbriggie clay loam Dr1.13, Dr2.13, Db1.1, Db1.13

Yamma loam

These are transitional red brown earths between grey and brown clays and the red brown

earths

4) Sands over clay:

Boona sandy loam

Cobram sandy loam

Danberry sand

Danberry sandy loam

Danberry loamy sand Db2.33

Finley sandy loam

Hyandra sandy loam H

Mycotha sand

Pullega sand

Pullega loamy sand

Tenningerie sand

Tenningerie sandy loam

Thulabin sand

20

Tubbo sand

Types 7,10,14 H

Wamoon sand

Whymoul sand

Whymoul loamy sand

Yambil sandy loam H

Yandera loam H

Yandera sandy loam H

These are soils which have marked texture contrast between light surface soils and heavy

cemented subsoils

5) Deep Sandy Soils:

Banna sand H

Banandera sand

Boona sand

Eulo sand

Jurambula sand

Sandmount sand

Utona sand

Yarangery sand

These are soils which have a surface sand profile deeper than 1m.

21

3.3 Data analysis

3.3.1 Particle size analysis

Studies of particle size analysis rarely specified the method used, however where possible

the methods used have been recorded with the associated data and included in the results

section of this review. Most studies undertaken included the analysis of coarse sand (CS),

fine sand (FS), silt (Si) and clay (C). Clay size fractions are commonly taken to be

<0.002 mm, silt 0.002-0.02 mm, fine sand 0.02-0.2 mm and coarse sand >0.2 mm. In some

cases only limited data such as the clay content was given with no indication of silt of

sand size fractions and in others sand fractions have simply been given rather than coarse

and fine sand fractions. Ranges of coarse sand, fine sand, silt and clay have been

compiled in most cases to depths of 0.3 m and comparisons of these results undertaken

with average values, standard deviations, coefficient of variation, medians and geometric

means. At depths greater than 0.3 m results from specific studies have been listed.

3.3.2 Bulk density and porosity

Density values have been recorded with associated moisture contents were possible,

however in many studies moisture contents were not reported. In sandier soils moisture

content does not affect bulk density dramatically but in clay soils the effect is more

pronounced. In one particular study by Loveday et al. (1966) volumetric moisture

contents have been calculated from aggregate densities, not bulk densities. In some cases

for particular soil groups bulk density data was not plentiful hence aggregate densities

were recorded. It should be noted that the bulk density of aggregates will be greater than

that of the soil due to pore spaces between the clods Marshall and Holmes, (1979). All

bulk densities have been converted to units of kg/m3.

22

Studies that undertook porosity measurements were difficult to find however, one major

study undertaken by Loveday et al. (1966) contained a number of porosity measurements

taken at various sites in the CIA. This report has been included as appendix 2.

3.3.3 Infiltration

Infiltration of water into soils had been measured in numerous ways using different

instrumentation. The method used to measure infiltration was documented together with

the results. Infiltration measurements included in this report have come largely from

ponding of the soil over extended time periods. Measurements of infiltration on dry soil

were not well represented, and is difficult to measure particularly on cracking clay soils.

Infiltration measurements have been converted to units of mm/day.

3.3.4 Hydraulic conductivity

Measurements of hydraulic conductivity were made in either the field or laboratory.

Laboratory measurements were on either packed cores or on undisturbed cores taken

from the soil profile. Field measurements were taken through the use of infiltration data

and potential measurements made by tensiometers or piezometers. The results section of

hydraulic conductivity have been divided into field and laboratory sections, with specific

methods noted. Hydraulic conductivities have been reported in units of mm/day.

3.3.5 Moisture characteristics

Studies of moisture characteristics were varied with different interpretations on what

value of suction best represents permanent wilting point and field capacity. There was

also a large variation of units used to represent suctions. All measurements of suction

were converted to units of kilopascals (kPa) which is equivalent to a kilonewton per

square meter (kN/m2). Units commonly used were Bars and these were converted using

23

1Bar = 105 Pascals and pF which was converted by kPa = (10pF/100)*9.8. It was assumed

that 1500 kPa suctions were representative of permanent wilting point and 10 kPa

suctions representative of field capacity.

Measurements of field capacities and permanent wilting points were also taken using

direct field measurements, moisture contents of the soil when plants showed moisture

stress and moisture contents of the soil after irrigation.

All moisture content measurements have been converted to a volumetric basis (m3/m3)

using associated bulk density measurements. In the particular case of moisture contents at

10 and 1500 kPa suctions measured by Loveday et al. (1966) moisture contents have

been converted to a volumetric basis using aggregate densities not bulk densities.

3.3.6 Electrical conductivities

Measurements of electrical conductivities have been restricted to those measured in a 1:5

water suspensions and are reported in mS/cm, equivalent to dS/m.

3.3.7 Exchangeable sodium percentage

Exchangeable sodium percentage (ESP) was not commonly reported in the literature,

however in one particular report by Loveday et al. (1978) a number of measurements of

exchangeable cations were undertaken. From these measurements exchangeable sodium

percentage (ESP) was calculated from the following formula given in Dent and Young

(1987).

ESP = (exchangeable Na*100)/ CEC

where CEC is the cation exchange capacity and all measurements are in milliequivalents

per litre.

The data from the various reports found are reported in the following sections according

to the grouping reported earlier.

24

4 SELF MULCHING CL AYS

4.1 Physical Composition

4.1.1.1 Particle size analysis

Loveday et al. (1966) conducted particle size analysis for two self-mulching clays,

Wunnamurra and Yooroobla clay, on five different sites in the CIA. Particle size analysis

was undertaken using normal mechanical analysis. Sodium tripolyphoshate was used as

the dispersing agent and silt and clay contents were determined using a plummet balance.

Three different depths were analysed, with these being 0-0.025, 0.025-0.1 and 0.2-0.3 m.

Ranges of particle size distributions are shown in table 4.1.

Table 4-1 Ranges of particle size distribution for self-mulching clays (Loveday et al.

1966)

Part iclesize Low H igh Low H igh Low H igh

CS % 4 9 3 9 3 18F S % 15 28 15 27 15 24Si % 7 15 8 16 7 15C % 52 72 51 72 60 73

0.2-0.3 mDepth (m)

0-0.025 m 0.025-0.1 m

Loveday et al. (1978) also conducted particle size analysis on four MIA self-mulching

clays, Wunnamurra, Gogeldrie, Coleambally and Yooroobla clays. Particle size analysis

was undertaken using normal mechanical analysis methods. Sodium tripolyphosphate

was used as the dispersing agent and silt and clay contents were determined using the

plummet balance. Samples from seven sites were taken at two depths, 0-0.1 m and 0.2-

0.3 m. Ranges of particle size distribution are shown in table 4.2.

25

Table 4-2 Ranges of particle size distribution for self-mulching clays (Loveday et al.

(1978)

Part ic lesize L o w H ig h L o w H ig h

C S % 5 15 4 9F S % 2 2 2 7 2 0 2 5Si % 6 12 6 11C % 5 3 6 3 5 9 6 8

0-0 .1 m 0 .2 -0 .3 mD ep t h (m )

van der Lelij and Talsma (1977) also determined clay contents of self mulching clay soils

and found a mean clay content of Yooroobla, Gogeldrie and Wunnamurra clays of 63 %

at depths of 0.2-0.3 m during investigation of infiltration of self mulching clays.

Christen (1994) also undertook particle size analysis on a Wunnamurra clay located in

the MIA during investigations into mole drainage. Particle size analysis was carried out at

depth intervals of 0.1-0.16 and 0.55-0.7 m. Results from the study are presented in table

4.3.

Stace et al. (1968) published particle size analysis data undertaken by Sleeman for a

Yooroobla clay located in the MIA to a 1.8 m depth. Results from the study are shown in

table 4.3.

Lattimore et al. (1994) also undertook particle size analysis on a Gogeldrie clay located

in the MIA. Results from the particle size analysis are shown in figure 4.3.

Smith (unpublished) also determined particle size analysis of a Wunnamurra clay at 0.1

m intervals to a 1 m depth. Results from the study are presented in table 4.3.

Average particle size distribution with depth as calculated from all samples is shown in

figure 4.1.

26

Table 4-3 Partic le size analysis of self mulching clays

Soil Depth (m) AuthorType 0.025 0.1 0.2 0.3 0.4 0.5 0.6 0.7 0.8 0.9 1 1.2 1.3 1.5 1.7 1.8Yooroo bla CS % 8 7 7 Lovedayclay FS % 23 22 19 1966

Si % 11 12 11 (average 3)C % 59 60 63

Wunnamurra CS % 5 5 6 Lovedayclay FS % 17 16 16 1966

Si % 10 10 10 (average 2)C % 68 69 69

Gogeldrie CS % 8 9 Lovedayclay FS % 23 20 1978

Si % 12 9C % 57 62

Wunnamurra CS % 10 7 Lovedayclay FS % 25 22 1978

Si % 9 7 (average 3)C % 57 65

Coleambally CS % 8 6 Lovedayclay FS % 24 22 1978

Si % 10 9 (average 2)C % 58 64

Yooroo bla CS % 6 5 Lovedayclay FS % 26 24 1978

Si % 10 10C % 58 61

Yooroo bla CS % 7 6 6 5 4 9 7 4 4 5 Staceclay FS % 20 19 19 19 19 27 26 26 25 26 1968

Si % 6 4 4 5 8 9 8 10 9 7C 55 62 63 63 65 51 54 56 57 54

Wunnamurra CS % 8 7 7 9 8 5 6 7 6 6 Smithclay FS % 27 22 21 22 21 22 22 22 22 22

Si % 15 14 15 14 15 18 17 15 16 17C % 50 57 57 55 55 55 55 56 55 55

Wunnamurra CS % 7 6 Christenclay FS % 22 15 1994

Si % 14 10C % 57 70

Gogeldrie CS % 8 8 10 LattimoreClay FS % 20 18 18 1994

Si % 12 8 10C % 60 66 62

27

The bracketed average in the author column indicates how many sites were surveyed and

results shown are the average of those sites for that particular soil type.

Figure 4-1 Average particle size distribution with depth for self mulching clays

Analysis of all particle size distributions of all studies at depths between 0-0.1 m and 0.2-

0.3 m has been undertaken. Statistical analysis of particle size distribution is listed

between 0-0.1 m depths in table 4.4 and for 0.2-0.3 m depths in table 4.5. Figures 4.2 and

4.3 shown cumulative probability distributions of the particle size analysis in the 0-0.1

and 0.2-0.3 m depth layers.

Table 4-4 Statistical data relating to particle size analysis of self mulching clays in

the 0-0.1 m layer

CS % FS % Si % C %Average 7 21 11 61L owest value 3 15 6 50Highest value 15 28 16 72Standard deviat ion 2 4 2 6Coeff iecient of var iat ion 33 18 22 9M edian 7 21 11 61Geomean 7 21 10 61Number of samples 50 50 50 50

0

0.2

0.4

0.6

0.8

1

1.2

1.4

1.6

1.8

2

0 10 20 30 40 50 60 70

%

Dep

th (

m)

AverageCoarsesandAverageFine sand

AverageSilt

AverageClay

28

Table 4-5 Statistical data relating to particle size analysis of self mulching clays in

the 0.2-0.3 m layer

CS % F S % Si % C %Average value 6 19 10 65Lowest value 3 14 6 59Highest value 18 25 15 73Standard deviation 3 3 2 4Coef f ic ient of variation 43 15 23 6M edian 6 20 10 64Geomean 6 19 10 65Number of of samples 30 30 30 30

00.10.20.30.40.50.60.70.80.9

1

0 10 20 30 40 50 60 70 80

%

Pro

babi

lity

of E

xcee

denc

e

CoarseSand

FineSand

Silt

Clay

Figure 4-2 Cumulative probability distribution of particle size of self mulching clays

in the 0-0.1 m layer

29

0

0.1

0.2

0.3

0.4

0.5

0.6

0.7

0.8

0.9

1

0 10 20 30 40 50 60 70 80

%

Pro

babi

lity

of e

xcee

denc

e

CoarseSand

FineSand

Silt

Clay

Figure 4-3 Cumulative probability distribution of particle size of self mulching

clays in the 0.2-0.3 m layer

4.1.1.2 Bulk density

Bulk density analysis for self-mulching clays has been undertaken by Loveday et al.

(1978) for Wunnamurra, Gogeldrie, Coleambally and Yooroobla clays. The bulk density

data was obtained from post irrigation sampling of soils from large area farms in the

MIA. Seven different sites were used with 2 samples being taken at each site. Variation

in bulk densities ranged from a low of 1240 kg/m3 at 0-0.1 m depth to 1620 kg/m3 at 0.6-

0.8 m depth. Moisture contents at sampling were not given however the soil was sampled

at a post irrigation stage.

Bulk density determinations were also carried out by Christen (1994) for a Wunnamurra

clay at depths between 0.01 to 0.16 m and 0.55 to 0.7 m, bulk density was found to be

1400 kg/m3 and 1510 kg/m3 for the respective depths. McIntyre et al. (1976) also

conducted bulk density determination at a depth greater than 0.8 m on a self mulching

clay located in the MIA and found the bulk density at 3m to be 1850 kg/m3.

30

Loveday et al. (1966) also undertook aggregate density measurements on five sites

consisting of Wunnamurra and Yooroobla clays. Aggregate densities were determined at

10 kPa and moisture contents reported in table 4.6.

Table 4-6 Bulk densities of self mulching clays

S oil Dep th (m ) A u th orType 0.025 0.1 0.2 0.3 0.4 0.6 0.8 3

Go g eld r ie 1245 1500 1495 1540 1570 1585 Lovedayc lay 1978

W un n am u rra 1272 1402 1402 1476 1505 1517 (average 3)c lay

Co leam b ally 1248 1440 1448 1488 1523 1540 (average 2)c lay

Yo o ro ob la 1250 1350 1430 1520 1560 1530c lay

W un n am u rra 1400 1510 Christenc lay 1994

Self m u lc h in g 1650 1850 Lovedayc lay 1976

Yo o ro ob la {1380} {1423} {1438} {1473} Lovedayc lay [0 .349] [0 .371] [0 .395] 1966

(average 3)

W un n am u rra {1268} {1305} {1378} {1363} (average 2)c lay [0 .384] [0 .404] [0 .416]

* Aggregate densities are shown in {}.

Moisture contents are shown in [ ]

Statistical analysis of bulk densities of self mulching clays to a 0.8 m depth from results

in the above studies are presented in table 4.7 and variation of bulk density with depth is

shown in figure 4.4.

31

Table 4-7 Statistical analysis of bulk density data of self mulching clays (kg/m3)

Depth (m) Average value

Lowest value

Highest value

Standard deviation

Coefficient of variation

Median Geomean No. ofsamples

0-0.1 1268 1130 1400 79 6 1250 1267 14

0.1-0.2 1427 1350 1510 59 4 1430 1430 13

0.2-0.3 1435 1360 1520 52 4 1450 1439 13

0.3-0.4 1490 1450 1530 25 2 1490 1491 13

0.4-0.6 1534 1460 1650 48 3 1520 1531 15

0.6-0.8 1537 1470 1620 42 3 1530 1533 13

0

0 . 1

0 . 2

0 . 3

0 . 4

0 . 5

0 . 6

0 . 7

0 . 8

0 . 9

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

B u lk D e n s i t y ( k g / m 3 )

Dep

th (

m)

Figure 4-4 Bulk density variation with depth for self mulching clays

32

4.1.2 Water Movement

4.1.2.1 Infiltration studies

Infiltration studies have been carried out by van der Lelij and Talsma (1977) during

prolonged ponding of soil at various sites in the MIA and CIA on Yooroobla,

Wunnamurra and Gogeldrie clays. Infiltration rates during ponding were measured at 16

sites using large, buffered ring infiltrometers for each field. Measurements were restricted

to infiltration between 1-16 weeks. Mean cumulative infiltration for the 16 sites varied

from 12 mm at 2 weeks to 148 mm at 16 weeks, with the curve being slightly S shaped as

shown in the figure 4.5. Mean infiltration rate near the end of ponding was calculated to

be 1.4 mm/day.

Figure 4-5 Mean cumulative infiltration curves for clays taken from van der Lelij

and Talsma (1977)

33

Talsma and Van der Lelij (1976) also carried out infiltration studies in the CIA on a

Wunnamurra clay. Both small ring infiltrometers and large buffered infiltrometers were

used to measure infiltration over a seven week period. Results from the three large ring

infiltrometers had a median value of 3.7 mm/day between 50-125 days after ponding and

for the small ring 1.6 mm/day. Mean infiltration rates over most of the ponding period

were found to fluctuate considerably.

4.1.2.2 Hydraulic conductivity

Laboratory measurement

Studies on hydraulic conductivities of self mulching clays have been undertaken by

Loveday et al. (1978) for four self mulching clays, Wunnamurra, Gogeldrie, Coleambally

and Yooroobla. Ground soil was repacked into columns and saturated hydraulic

conductivity measured with a falling head permeameter. Saturated hydraulic

conductivities between 0-0.2 m depths have been measured at both 24 and 48 hr periods,

10 samples from seven different sites were taken in the study. Average values of recorded

saturated hydraulic conductivitys are listed in table 4.8 along with a cumulative

probability distribution of the data for both 24 and 48 hr time periods in figure 4.6.

Table 4-8 Statistical analysis of hydraulic conductivities of self mulching clays

(mm/day)

Time Average value

Lowest value

Highest value

Standard deviation

Coef f icienof variation

Median Geomean No. of samples

24hr 42 24 64 18 42 38 38 1048hr 37 24 49 14 38 44 34 10

34

0

0.25

0.5

0.75

1

0 10 20 30 40 50 60 70

Hydraulic cond uctivty (mm/day)

Pro

babi

lity

of e

xcee

denc

e

24 hr

48 hr

Figure 4-6 Cumulative probability distribution of hydraulic conductivity

Field measurements

Hydraulic conductivity during prolonged ponding of self-mulching clays were

undertaken by van der Lelij and Talsma (1977). Hydraulic conductivities were calculated

from infiltration rates and potential gradients. Topsoil (0-0.45 m) unsaturated hydraulic

conductivitys as calculated by infiltration and potential gradient measurements at 16 sites

on self mulching clays gave an average hydraulic conductivity of 2.7 mm/day over a

period of 10-100 days during ponding of the soil average potential gradient was found to

be 0.73. Subsoil (1.2-1.5 m) saturated hydraulic conductivities for the study gave an

average value of 1.11 mm/day at a potential gradient of 1.8, again calculated from

infiltration measurements and potential gradients. Hydraulic conductivity at 100 days

after ponding at one site on a self mulching clay was estimated to a 3 m depth from

measurements of infiltration rate and potential gradient measured at the site. Results are

presented in table 4.9, taken from van der Lelij and Talsma (1977).

35

Table 4-9 Hydraulic conductivity for self mulching clay during ponding (mm/day)

D e p t h in t e r v a l ( m )

G r a d ie n t H y d r a u lic c o n d u c t iv it y ( m m /d a y )

0 - 0 .5 0 .0 6 2 0 .80 .5 - 1 0 .1 6 7 .81 - 1 .5 0 .9 4 1 .31 .5 - 2 1 .7 6 0 .72 - 3 .0 5 0 .8 6 1 .5

Hydraulic conductivities of a Wunnamurra clay, Talsma and Van der Lelij (1976), were

also estimated using measurements of infiltration and piezometer readings. Hydraulic

conductivity was found to vary between 0.5 and 9.7 mm/day measured at depths between

0.2 and 0.3 m with mean moisture potentials of –0.61 and –0.48 m at respective depths of

0.2 and 0.4 m, during a study of prolonged ponding of the soil on 16 sites. Hydraulic

conductivity of a slurried top soil from the site was also conducted and ranged between

8.9 mm/day and 1.4 mm/day for respective depths of 0.02 m to 0.22 m.

4.1.3 Water Retention / Moisture Characteristic

Studies relating to moisture characteristics of self-mulching clay profiles have been

undertaken by Loveday et al. (1977). Available water was calculated from the difference

between capacity to hold water between 10 kPa and 1500 kPa suctions. The study was

undertaken on five sites, which included Wunnamurra and Yooroobla clays. Available

water for the five samples taken ranged between 0.08-0.10 m for the top 0.6 m with an

average of 0.094 m of available water for the top 0.6 m of soil. Loveday et al. (1966) also

undertook moisture characteristic studies on five sites in the CIA on Wunnamurra and

Yooroobla clays. Moisture contents at 10 kPa and at 1500 kPa were determined, and the

difference used as an approximation to available moisture. Clods were used for the 10

kPa determination and 1500 kPa moisture contents were determined using sieved soil in a

pressure membrane. Available water was then estimated from the aggregate densities and

10 kPa and 1500 kPa moisture contents. The average available water for the five sites

36

was found to be 0.037 m for the top 0.3 m depth, with the highest recorded value being

0.046 m and the lowest 0.027 m for the top 0.3 m.

Field determinations of permanent wilting points and field capacity of a Wunnamurra

clay have been undertaken by Loveday et al. (1977). Moisture contents were taken when

the crop showed signs of moisture stress and then again after irrigation, figure 4.7. The

difference between the two moisture contents was taken to represent the available water.

1500 kPa moisture content were also undertaken on the profiles, figure 4.7, taken from

Loveday et al. (1977).

Figure 4-7 Volumetric moisture content profiles of a Wunnamurra clay

Measurements of moisture contents at 1500 kPa suctions were also made by Loveday et

al. (1966) at depths of 0-0.025, 0.025-0.1 and 0.2-0.3 m. Volumetric water contents from

these measurements were then calculated from aggregate densities and volumetric water

contents. Volumetric water contents varied from 0.2-0.30 m3/m3 in the 0-0.025 m layer,

0.2-0.3 m3/m3 in the 0.025-0.1 m layer and 0.23-0.34 m3/m3 in the 0.2-0.3 m layer.

37

Stace et al. (1968) also compiled moisture content determinations at 1500 kPa suctions

measured by Sleeman on a Yooroobla clay in the MIA. Results are shown in table 4-10.

Loveday et al. (1978) also determined moisture contents at 1500 kPa suctions for

Wunnamurra, Gogeldrie, Coleambally and Yooroobla clays located at seven sites in the

MIA, Table 4.11 shows all the data found in this study.

Statistical data relating to all 1500 kPa moisture contents is shown in table 4.12 along

with variation of moisture content with depth from all studies at 1500 kPa shown in

figure 4.8.

Table 4-10 Ranges of 1500 kPa moisture contents (m3/m3) of self mulching clays,

Loveday et al. (1978)

0.4-0.6 mLow High Low High Low High Low High Low High

Volumetric water 0.231 0.288 0.264 0.323 0.268 0.335 0.294 0.352 0.28 0.356cont ent

Depth (m)0-0.1 m 0.2-0.3 m 0.3-0.4 m 0.6-0.8 m

38

Table 4-11 1500 kPa volumetric moisture contents of self mulching clays

Author0.025 0.1 0.3 0.4 0.6 0.8

Yooroobla 0.230 0.245 0.266 Lovedayclay 1966

(average 3)

Wunnamurra 0.282 0.284 0.303 (average 2)clay

Gogeldrie 0.242 0.268 0.283 0.296 0.291 Lovedayclay 1978

Wunnamurra 0.259 0.296 0.320 0.330 0.339 (average 3)clay

Coleambally 0.267 0.295 0.298 0.315 0.323 (average 2)clay

Yooroobla 0.231 0.271 0.293 0.315 0.319clay

Yooroobla 0.23 0.23 0.25 0.27 Staceclay 1968

Depth ( m)

Table 4-12 Statistical analysis of volumetric water contents at 1500 kPa

Depth (m)

Average value

Lowest value

Highest value

Standard deviation

Coeff icient of variation


0.025 0.251 0.207 0.301 0.032 12.56 0.251 0.249 100.1 0.256 0.229 0.323 0.022 8.70 0.255 0.255 250.3 0.283 0.230 0.341 0.026 9.02 0.281 0.282 250.4 0.301 0.250 0.335 0.026 8.70 0.299 0.300 150.6 0.315 0.270 0.352 0.022 6.91 0.312 0.315 150.8 0.325 0.280 0.356 0.020 6.30 0.326 0.324 14

39

Figure 4-8 Variation of volumetric water contents at 1500 kPa for self-mulching

clays

Determinations of 10 kPa moisture contents were carried out by Loveday et al. (1966) at

five sites on Wunnamurra and Yooroobla clays. Moisture contents at 10 kPa suctions

were measured at depths of 0-0.025, 0.025-0.1 and 0.2-0.3 m in order to approximate the

field capacity of the soils. Moisture contents ranged from 0.32-0.40 m3/m3 in the 0-0.025

m layer, 0.33-0.43 m3/m3 in the 0.025-0.1 m layer and 0.38-0.43 m3/m3. Stace et al.

(1968) also compiled 10 kPa moisture content determinations measured by Sleeman in

the MIA. Results from the study are shown in table 4.13.

0

0.2

0.4

0.6

0.8

0 0.1 0.2 0.3 0.4Mois tu re Con tent (m 3/m 3)

Dep

th (

m)

40

Table 4-13 10 kPa volumetric moisture contents of self mulching clays

Depth (m)Soil type 0.025 0.1 0.2 0.3 0.6 Author

Yooroobla 0.349 0.371 0.395 Lovedayclay 1966

(average 3)

Wunnamu rra 0.384 0.404 0.416 (average 2)clay

Yooroobla 0.37 0.33 0.39 0.4 Staceclay 1968

Statistical data relating to 10 kPa moisture contents for all mentioned studies is shown in

table 4.14 along with variation of volumetric moisture content at 10 kPa suction with soil

depth, also shown in figure 4-9.

Table 4-14 Statistical analysis of volumetric water contents at 10 kPa


Lowest value

Highest value

Standard deviation

Coefficienof v ariation


0.025 0.363 0.321 0.397 0.0224 6.19 0.363 0.362 100.1 0.382 0.33 0.429 0.0257 6.73 0.383 0.382 110.2 0.330 0.33 0.33 0.33 0.33 10.3 0.402 0.383 0.427 0.0142 3.54 0.403 0.402 110.6 0.4 1

41

Figure 4-9 Variation of volumetric water contents at 10 kPa for self-mulching clays

4.1.4 Soil Salinity/Sodicity

Electrical conductivities for self mulching clay profiles have been undertaken by

Loveday et al. (1978) for Wunnamurra, Yooroobla, Coleambally and Gogeldrie clays on

seven sites in the MIA. Electrical conductivity analysis was undertaken in a 1:5 water

suspension on ten samples from the sites at depths of 0.1, 0.2, 0.3, 0.4, 0.6 and 0.8 m.

Loveday et al. (1983) also undertook electrical conductivity analysis on four self

mulching clays to 0.8 m. Variation of electrical conductivity with depth is shown in

figure 4.10.

0

0.2

0.4

0.6

0.8

0 0.1 0.2 0.3 0.4 0.5Mois ture Content (m 3/m 3)

Dep

th (

m)

42

0

0.2

0.4

0.6

0.8

0 0.5 1 1.5 2 2.5EC (mS/cm)

Dep

th (

m)

Figure 4-10 Electrical conductivity variation with depth for self mulching clays

Exchangeable sodium percentages (ESP) of self mulching clays have been calculated

from exchangeable cation data recorded by Loveday et al. (1966) and Loveday et al.

(1978). Loveday et al. (1966) determined exchangeable cations at profile depths of 0-

0.025, 0.025-0.1 and 0.2-0.3 m on five sites of Yooroobla and Wunnamurra clays located

in the CIA. ESP ranged from 0.08-0.6 % in the 0-0.025 m layer, 0.06-3.96 % in the

0.025-0.1 m layer and 0.48-3.96 % in the 0.2-0.3 m layer.

Loveday et al. (1978) also determined exchangeable cations for Wunnamurra,

Yooroobla, Gogeldrie and Coleambally clays at seven sites in the MIA. ESP was

calculated from these results at 0-0.1 and 0.2-0.3 m depths and ranged from 0.055-6.6 %

in the 0-0.1 m layer and 1.03-15.6 % in the 0.2-0.3 m layer. ESP for the various soil type

is shown in table 4.15.

Variation of ESP with depth for all the above mentioned studies is shown in figure 4.11

and statistical analysis of all studies in table 4.16.

43

Table 4-15 ESP for self-mulching clays

SoilType 0.025 0.1 0.3 Au thor

Yoo roob la 0.48 0.80 1.90 Lovedayc lay 1966

(average 3)

W unna m urr a 0.26 0.92 2.51 Lovedayc lay 1966

(average 2)

W unna m urr a 2.94 10.16 Lovedayc lay 1978

(average 3)

Goge ld rie 0.59 1.55 Lovedayc lay 1978

Yoo roob la 4.40 3.72 Lovedayc lay 1978

Coleam bally 2.24 4.73 Lovedayc lay 1978

(average 2)

Depth (m )

0

0.05

0.10.15

0.2

0.25

0.30.35

0.4

0 5 10 15 20 25

ESP

Dep

th (

m)

Figure 4-11 ESP variation with depth for self mulching clays

44

Table 4-16 Analysis of ESP data of self mulching clays

Depth (m)

Average value

Lowest value

Highest value

Standard deviation



0.025 0.35 0.08 0.6 0.244 70.43 0.46 0.25 50.1 1.62 0.055 6.6 1.745 107.67 1.06 0.86 330.3 3.92 0.48 15.6 3.828 97.65 2.36 2.72 34

45

5 HARD SETTING CL AYS

5.1.1 Physical Composition


Loveday et al. (1978) conducted particle size analysis on a Riverina clay located in the

MIA on a large area farm. The sampled site was in an annual pasture phase of the cereal

(rice, wheat, barley) pasture rotation. Two determinations of particle size distribution

were made at depths between 0-0.1 and 0.2-0.3 m, results from the study are shown in

table 5.1. Loveday et al. (1983) also conducted particle size analysis on four hard setting

clays located in the MIA and CIA. Individual names of the clays were not given however

it was indicated that the particular clays were hard setting not self mulching. Particle size

distributions for this study however were only conducted at 0-0.1 m depths. Particle size

distribution ranged from 4-6 % coarse sand, 19- 32 % fine sand, 14-20 % silt and 36-55 %

clay. Average values are given in table 5.1.

Table 5-1 Partic le size distribution of hard setting clays

Soil Depth (m)Type 0.1 0.3 Author

Hard CS % 6 Lovedaysett ing FS % 28 1983clays Si % 18 (average 4)

C % 48

Riverina CS % 6 3 LovedayClay FS % 20 20 1978

Si % 12 11C % 62 66

46


Bulk density analysis of hard setting clays has been undertaken by Loveday et al. (1978)

at depths between 0-0.8 m at one site in the MIA on Riverina clay. Two replicates were

taken post irrigation, with cores of 0.046 m diameter, Table 5.2.

Loveday and Scotter (1966) also undertook bulk density determinations on Riverina and

Billabong clays at 3 sites in the MIA. Bulk densities were determined on 0.051 m

diameter cores taken after the sites had been irrigated. Bulk densities ranged between

1290-1430 kg/m3 for 0-0.1 m depths and between 1510-1580 kg/m3 for 0.2-0.3 m depths,

table 5.2.

Sharma (1971) also measured bulk densities of a Billabong clay at depths of 0.1, 0.3, 0.4

and 0.6 m. Bulk densities were determined from core samples of 0.048 m diameter which

were collected three days after irrigation. Results from the study are shown in table 5.2.

Variation of bulk density with depth for hard setting clays is shown in figure 5.1.

Table 5-2 Bulk densities of hard setting clays

Soil Depth (m) AuthorType 0.1 0.2 0.3 0.4 0.6 0.8

Riverina 1130 1270 1350 1410 1515 1480 Lovedayclay 1978

Riverina 1320 1510 Lovedayclay and

Scotter

Billa bong 1390 1565 (average 2)clay

Billa bong 1510 1540 1580 1570 Sharmaclay 1972

47

0

0.2

0.4

0.6

0.8

1000 1200 1400 1600 1800

Bu lk d ens ity

Dep

th (

m)

Figure 5-1 Variation of bulk density with depth for hard setting clays

5.1.1.3 Porosity

Loveday and Scotter (1966) have undertaken aggregate porosity measurements of a

Billabong clay during an investigation into the emergence response of subterranean

clover. Total porosity was determined on air-dried surface clods at the conclusion of the

experiment and was found to be 0.26 m3/m3.

Sedgley (1962) also conducted porosity determinations on a Billabong clay. Porosity was

calculated from E = (1-(Wod/ρsVod).100 where E is porosity, Wod the weight of oven dry

soil, Vod the volume of oven dry soil and ρs the density of solid particles assumed to be

2.65. Volumes of soil samples were determined using the kerosene displacement

technique. Seven samples from a 0.1-0.15 m layer gave a mean porosity of 0.343 m3/m3

with a standard deviation of 0.002.

48



Laboratory measurements

Hydraulic conductivity measurements were undertaken by Sharma (1971) for a Billabong

clay. The hydraulic conductivity of uniformly packed 1-2 mm air dry aggregates was

measured with a falling head permeameter. The value of hydraulic conductivity was

recorded at 4 hr intervals for a 24 hr period on aggregates from three depths in the profile.

Mean hydraulic conductivitys at the end of the 24 hr period are shown in table 5.3.

Table 5-3 Hydraulic conductivity of a Billabong clay (Sharma 1972)

Aggregate samp le depths

Hydraulic conduct iv ityaf ter 24 hr (mm/da y)

0-0.075 14400.075-0.15 290.15-0.3 40.3-0.45 6

Loveday et al. (1978) also undertook laboratory determinations of saturated hydraulic

conductivity for a hardsetting clay, Riverina clay, on two samples taken at depths

between 0-0.2 m in the Warrawidgee area of the MIA. Ground soil was packed into

columns and saturated hydraulic conductivity measured with a falling head permeameter.

Hydraulic conductivitys for the two samples at 24 hr periods were found to be 3.84

mm/day and at 48 hrs were 2.64 mm/day.

49

5.1.3 Water Retention/Moisture Characteristic

Determinations of available water for hard setting clays have been undertaken by

Loveday et al. (1977) for a Riverina clay. Only one determination was made and the

available water in the profile was found to be 0.058 m for the top 0.6 m of soil as

calculated from the difference between post and pre irrigation samplings.

Loveday and Scotter (1966) also undertook available water measurements on Riverina

and Billabong clays located in the Warrawidgee area of the MIA. Available water for the

top 0.4 m of soil was calculated from laboratory measurements of moisture contents of

aggregates at 10 kPa (field capacity) and 1500 kPa (wilting point) from depths of 0-0.03,

0.03-0.1, 0.1-0.2, 0.2-0.3 and 0.3-0.4 m. Three determinations were made and the

available water to a 0.4 m depth was found to be 0.05 and 0.054 m for the two sites on

Billabong clays and 0.056 m for the Riverina clay.

Field determinations of moisture contents at permanent wilting points and field capacity

of hard settings clays has been undertaken by Loveday et al. (1977) for two hardsetting

clays, Billabong and Riverina. Moisture content determinations were obtained initially

when the crops grown on the various sites showed moisture stress and again after

irrigation. The difference between the two measured moisture curves of the soil was

taken to represent the available water in the soil profile.

The results for the permanent wilting point moisture contents when plants showed initial

signs of stress are shown in table 5.4, along with 1500 kPa moisture contents which were

determined from laboratory measurements on the same Riverina clay profile.

Loveday et al. (1978) also undertook laboratory determinations of 1500 kPa moisture

contents of a Riverina clay located in the MIA. Two replicates were taken at the site and

the mean 1500 kPa moisture content is shown in table 5.4. Moisture content profiles are


50

Table 5-4 Permanent wilting point volumetric moisture contents for hard setting

clays

Soil Depth (m) AuthorType 0.05 0.075 0.1 0.15 0.2 0.25 0.3 0.35 0.4 0.6 0.8

Billa bong {0.1} {0.21} {0.26} {0.29} {0.31} Lovedayclay 1977

Riverina {0.17} {0.18} {0.22} {0.23} {0.27} {0.29}clay

Riverina 0.22 0.275 0.28 0.29 0.3clay

Riverina 0.258 0.301 0.32 0.349 0.295 Lovedayclay 1978

Values determined from moisture contents in the field are shown in brackets.

00.10.20.30.40.50.60.70.8

0 0.1 0.2 0.3 0.4

Volumetric moisture content (m3/m3)

Dep

th (

m)

F ield

1500kPa

Figure 5-2 Various volumetric moisture contents at permanent wilting point.

51

Field capacity determinations as found by Loveday et al. (1977) on Billabong and

Riverina clays from moisture content sampling after irrigation are shown in table 5.5 and

also graphically in figure 5.3.

Table 5-5 Volumetric moisture content measurements at field capacity for hard

setting clays

Soil Depth (m) AuthorType 0.05 0.075 0.1 0.15 0.25 0.35 0.4 0.6

Billa bong 0.31 0.33 0.32 0.32 0.32 Lovedayclay 1977

Riverina 0.47 0.42 0.38 0.3 0.3 0.29clay

0

0.1

0.2

0.3

0.4

0.5

0.6

0 0.1 0.2 0.3 0.4 0.5

Volumetric moisture content (m3/m3)

Dep

th (

m)

Figure 5-3 Variation of volumetric moisture contents at field capacity for hard

setting clays

Soil moisture characteristic curves for a Billabong clay have also been constructed by

Sharma (1971) over a range of water potentials, figure 5.4.

52

Figure 5-4 Soil moisture characteristic curve for a Billabong clay taken from

Sharma (1971)


Electrical conductivity determinations for hard setting clay profiles have been undertaken

by Loveday et al. (1978) on a Riverina clay and by Sharma (1966) for a Billabong clay,

table 5.6. Measurements of exchangeable cations have been undertaken by Loveday et al.

(1978) for a Riverina clay located in the MIA. ESP was calculated to be 8.2 % in the 0-

0.1 m layer and 12.45 % in the 0.2-0.3 m layer.

Table 5-6 Electrical conductivities of hard setting clays

Soil Depth (m) AuthorType 0.075 0.1 0.15 0.2 0.3 0.4 0.45 0.6 0.8

Bill abong 0.246 0.373 0.749 1.173 2.613 Sharmaclay 1971

Riverina Lovedayclay 0.135 0.135 0.18 0.255 0.315 1.49 1978

53

6 TRANSITIONAL RED BROWN EA RTHS



Loveday et al. (1978) conducted particle size analysis on four transitional red brown

earths, Willbriggie clay, Willbriggie clay loam, Marah loam, and Marah clay loam

located on large area farms in the MIA. The studies were undertaken on 13 different sites

with two samples being taken per site up to 20 m apart. Particle size analysis was

undertaken using normal mechanical analysis. Sodium tripolyphoshate was used as the

dispersing agent and silt and clay contents were determined using a plummet balance.

Two different depths were analysed, being 0-0.1 and 0.2-0.3 m. Ranges of particle size

distributions for transitional red brown earths measured in the study are shown in table

6.1.

Table 6-1 Ranges of particle size analysis for transitional red brown

earths, Loveday et al. (1978)

D e p t h (m )P a r t ic le 0 -0 .1 0 .2 -0 .3s iz e L o w H ig h L o w H ig h

C S % 5 2 4 2 1 5F S % 2 8 5 5 1 7 3 0S i % 6 1 7 4 1 2C % 2 1 5 7 5 1 7 3

Loveday et al. (1966) also conducted particle size analysis on three transitional red brown

earths, Willbriggie clay loam, Willbriggie loam and Tuppal clay loam at 9 sites in the

CIA. Particle size analysis was undertaken using the same method as specified above.

54

Samples from the nine sites were taken from three different depths, being 0-0.025, 0.025-

0.1 and 0.2-0.3 m, table 6.2.

Table 6-2 Ranges of particle size distribution for transitional red brown earths,

Loveday et al. (1966).

Depth (m)

Particle 0-0.025 0.025-0.1 0.2-0.3

size Low High Low High Low High

CS % 10 20 8 21 3 12

FS % 28 43 25 42 11 21

Si % 13 21 14 22 5 12

C % 19 46 17 49 61 76

Loveday et al. (1970) also undertook particle size determinations on Marah clay loam

during an investigation into soil and cotton responses to tillage. Particle size analysis was

undertaken at three depth ranges, being 0-0.05, 0.1-0.2 and 0.5-0.6 m, table 6.3.

Blackwell et al. (1990) reported particle size analysis for a Mundiwa clay loam located in

the Whitton area of the MIA, table 6.3. Clay contents of a Marah clay loam have also

been determined by Jayawardane et al. (1984) to a 1 m depth from soil samples taken at

Benerembah. Clay contents only were determined at 0.1 m depth intervals, in table 6.3.

Kowalik et al. (1977) also determined only clay contents of a Marah clay loam at

Benerembah in the MIA, table 6.3.

During investigations into mole drainage in the MIA, Christen (1994) also undertook

particle size analysis on two transitional red brown earths, Morago and Mundiwa clay

loams located in the Whitton area, table 6.3.

55

Soil analysis undertaken on bore holes on transitional red brown has also been carried out

on a Willbriggie clay loam located in the CIA to depths of 3 m by Sleeman and Stanad

(1983). Particularly high clay contents were found. Results from the analysis are

presented in table 6.3.

Unpublished particle size analysis on two transitional red brown earth soils Willbriggie

clay and Mundiwa clay loam was provided by Mr. David Smith, CSIRO Griffith. Particle

size distributions were determined at 0.1 m intervals to a depth of 1.4 m for the Mundiwa

clay loam profile and to a 1 m depth for the Willbriggie clay loam profile. Both profiles

were located in the MIA and results are presented in table 6.3, with the Mundiwa clay

loam analysis is an average of three replicates.

Average coarse sand, fine sand, silt and clay percentages from all of the above studies are

shown graphically in figure 6.1.

Data analysis of particle size distributions in the 0-0.1 and 0.2-0.3 m layers for all

transitional red brown earths profiles is shown in tables 6.4 and 6.5 respectively.

Cumulative probability distributions for particle size distributions of transitional red

brown earths has also been undertaken for depth ranges between 0-0.1 and 0.2-0.3 m are

shown in figures 6.2 and 6.3 respectively.

56

0

0.5

1

1.5

2

2.5

3

3.5

0 20 40 60 80%

Dep

th (

m)

Coarsesand

Finesand

Silt

Clay

Figure 6-1 Average particle size distribution with depth for transitional red brown

earths

57

Table 6-3 Particle size distribution of transitional red brown earths

Soil Depth (m) AuthorType 0.025 0.1 0.2 0.3 0.4 0.5 0.6 0.7 0.8 0.9 1 1.1 1.2 1.3 1.4 1.5 2.5 3

W illbriggie CS % 15 14 6 Lovedayclay FS % 36 34 15 1966loam Si % 18 18 7 (average 5)

C % 31 34 71

Tuppal CS % 15 14 7 (average 2)clay FS % 32 30 16loam Si % 16 17 10

C % 37 39 68

W illbriggie CS % 20 17 7 (average 2)loam FS % 39 36 14

Si % 20 21 8C % 22 26 72

W illbriggie CS % 14 7 Lovedayclay FS % 36 23 1978loam Si % 11 6 (average 8)

C % 38 65

W illbriggie CS % 7 3clay FS % 32 21

Si % 9 5C % 54 71

Marah CS % 11 4 (average 2)clay FS % 36 24loam Si % 15 10

C % 40 62

Marah CS % 14 7 (average 2)loam FS % 49 22

Si % 14 5C % 24 67

Marah CS % 11 4 3 Lovedayclay FS % 43 20 24 1970loam Si % 21 10 15

C % 25 66 58

Mundiwa Sand % 60 26 Blackwellclay Si % 24 14 1990loam C % 17 62

Mundiwa CS % 22 13 11 10 10 12 13 14 14 11 9 8 8 8 Smithclay FS % 35 22 19 19 19 20 21 21 22 21 21 20 20 21 unpublishedloam Si % 18 14 14 14 13 13 12 13 12 14 14 15 15 15

C % 24 51 57 57 58 56 52 51 52 54 56 58 56 56

W illbriggie CS % 14 9 7 7 8 9 9 9 10 10clay FS % 44 33 28 29 32 30 30 27 32 29

Si % 11 11 10 10 9 10 12 14 12 14C % 31 47 55 55 51 51 50 50 46 47

Marah C % 44 54 59 56 52 49 47 46 45 46 47 50 Jayawardaneclay 1983loam

58

Marah C % 38 60 54 47 45 49 50 Kowalikclay 1978loam

Willbriggie CS % 2 2 3 3 3 3 4 9 12 Sleemanclay FS % 17 14 18 20 20 20 20 18 14 and loam Si % 6 5 8 3 5 10 11 9 8 Stannard

C % 78 82 76 79 78 72 70 70 67 1983

Marago CS % 13 5 Christenclay FS % 33 17 1994loam Si % 9 16

C % 45 63

Mundiwa CS % 21 8clay FS % 39 12loam Si % 24 15

C % 17 65

Table 6-4 Statistical data relating to particle size analysis of transitional red brown

earths for the 0-0.1 m layer

CS % FS % Si % C %Average value 14 36 16 36Lowest value 5 25 6 17Highest value 24 55 22 57Standard dev iation 4 5 4 9Coeffient of variation 27 15 25 24Median 14 36 16 35Geomean 13 35 15 35No. of samples 73 73 73 73

Table 6-5 Statistical data relating to particle size analysis of transitional red brown

earths for the 0.2-0.3 m layer

CS % FS % Si % C %Average value 6 20 7 67Lowest value 2 11 4 51Highest value 15 30 12 76Standard deviation 3 5 2 6Coefficient of variation 45 25 28 8Median 6 20 7 68Geomean 6 19 7 67No. of samples 53 53 53 53

59

0

0.25

0.5

0.75

1

0 10 20 30 40 50 60

%

Pro

babi

lity

of e

xcee

denc

e

CoarseSand

FineSand

Silt

Clay

Figure 6-2 Cumulative probability distribution of particle size for transitional red

brown earths in the 0-0.1 m layer

0

0.25

0.5

0.75

1

0 20 40 60 80%

Pro

babi

lity

of e

xcee

denc

e

CoarseSand

FineSand

Silt

Clay

Figure 6-3 Cumulative probability distribution of particle size for transitional red

brown earths in the 0.2-0.3 m layer

60


Determinations of bulk density for transitional red brown earths has been undertaken by

Loveday et al. (1978) for four transitional red brown earth soils, Willbriggie clay,

Willbriggie clay loam, Marah loam and Marah clay loam at 15 sites in the MIA. Two

samples were taken from each site and bulk densities were recorded to 0.8 m. Moisture

contents were not given. Samples were obtained from post irrigation coring of sites in the

annual pasture phase of the cereal (rice, wheat, and barley) - pasture rotation. Cores of

0.046 m diameter were used for sampling. Results from the study are presented in table

6.6.

Cai et al. (1994) also undertook bulk density determinations for a Mundiwa clay loam

during the modeling of leaching and recharge. Bulk density was found to vary between

1370 kg/m3 at a 0-0.1 m depth and 1530 kg/m3 at a 1-2.4 m depth, table 6.6.

Bulk density determinations have been undertaken to 4.6 m by Kowalik et al. (1978) on a

Marah clay loam located at Benerembah in the MIA. Bulk density was found to vary

between 1460 kg/m3 at 0.2-0.3 m, to 1800 kg/m3 at a depth of 4.6 m, table 7.6.

Loveday et al. (1970) undertook bulk density determinations on Marah sandy clay loams

and Marah clay at depths between 0-0.1 m and 0.2-0.3 m. Measurements were taken on 4

cores, each of 0.051 m diameter, after irrigation of the soil, table 7.6. During a

preliminary sampling of the Whitton common Loveday et al. (1984) also measured bulk

density of a Mundiwa clay loam at three profile depths on two sites. Five cores of 0.075

m diameter and 0.6 m long were used to determine the mean bulk density at each of the

three depths. Mean bulk densities of the two sites at respective depths were then

calculated, table 6.6. Determinations of bulk density were also undertaken by Christen

(1994), table 6.6.

Talsma (1963) also determined bulk density measurements on a Tuppal clay located in

the MIA during investigations into the control of saline groundwater. Results from the

study are presented in table 6.6.

61

Statistical data relating to bulk densities of transitional red brown earths calculated from

the previously mentioned studies is shown in table 6.7 the variation of bulk density with

depth to 0.8 m for transitional red brown earths is shown in figure 6.4.

62

Table 6-6 Bulk densities of transitional red brown earths

Soil Depth (m) AuthorType 0.05 0.1 0.2 0.3 0.4 0.6 0.8 1.1 1.5 2 3.2 4.6

Willbriggie 1383 1497 1456 1506 1528 1536 Lovedayclay 1978loam (average 7)

Marah 1415 1558 1405 1448 1503 1540 (average 2)loam

Willbriggie 1230 1450 1375 1445 1505 1505clay

Marah 1363 1493 1475 1535 1578 1590 (average 2)clayloam

Mundiwa 1370 1430 1430 1450 1450 1500 1530 Caiclay 1994loam

Marah 1460 1630 1630 1620 1680 1710 1860 1800 Kowalikclay 1978loam

Marah 1460 1570 Lovedayfine sandy 1970clay loam (average 2)

Marah 1380 1510clay

Mundiwa 1545 1430 1455 Lovedayclay [0.25] [0.39] [0.29] 1984loam (average 2)

Marago 1360 1460 Christenclay 1994loam

Mundiwa 1360 1460clayloam

Tuppal 1440 1490 1470 1580 1590 Talsma clay 1963

63

0

0.2

0.4

0.6

0.8

1000 1200 1400 1600 1800 2000

B u lk Den s it y (kg /m3)D

epth

(m

)

Figure 6-4 Variation of bulk density with depth for transitional red brown earths

Table 6-7 Statistical data relating to bulk densities of transitional red brown earths

(kg/m3)

Depth (m)

Average value

Lowest value

Highest value

Standard deviation



0.05 1545 1545 1545 10.1 1369 1180 1620 93 7 1375 1366 300.2 1480 1310 1630 75 5 1460 1478 310.3 1444 1340 1560 63 4 1450 1443 300.4 1495 1370 1630 68 5 1500 1493 300.6 1528 1390 1630 64 4 1540 1526 310.8 1541 1440 1640 56 4 1540 1540 311.1 1599 1580 1619 20 1 1599 1599 31.5 1600 1530 1680 75 5 1590 1599 32 1710 13.2 1860 14.6 1800 1

64

6.1.1.3 Porosity

Porosity measurements of transitional red brown earths have been undertaken by

McIntyre et al. (1982). Total porosity was estimated from the initial bulk density and

corrected for measured final vertical swelling on two sites of Marah clay loam at

Benerembah in the MIA after the site had been ponded, table 6.8.

Table 6-8 Porosity of Marah clay loam as found by McIntyre et al. (1982)

D e p t h ( m ) P o r o s it yP lo t 1 P lo t 2

0 . 1 0 . 5 0 . 50 . 2 5 0 . 4 80 . 5 5 0 . 4 5 0 . 4 20 . 8 5 0 . 4 2 0 . 4 21 0 . 41 . 5 0 . 4 0 . 3 91 . 7 5 0 . 3 82 0 . 3 82 . 1 0 . 3 82 . 7 0 . 3 6 0 . 3 73 . 3 0 . 3 63 . 9 0 . 3 44 . 5 0 . 3 6

Loveday et al. (1966) also conducted determinations on total porosity and air filled

porosity at nine sites in the CIA consisting of Willbriggie clay loam Willbriggie loam,

and Tuppal clay loam. Measurements were made on core samples of 0.0372 and 0.0496

m diameter taken from a depth of between 0-0.1 m. Cores were taken at 24 hr and 48 hr

periods after the plots had received 50mm of water, table 6.9.

65

Table 6-9 Porosity measurements of transitional red brown earths (m3/m3). Loveday

et al. (1966)

Po ros ity RangeA v erage Low High

To ta l p o ro s ity a f te r 24h r 0.51 0 .44 0 .6A ir f illed p o ro s ity a f te r 24hr 0.29 0 .21 0 .48To ta l p o ro s ity a f te r48h r 0.50 0 .29 0 .59A ir f illed p o ro s ity a f te r 48hr 0.31 0 .22 0 .34

Total porosity determinations were also undertaken by Talsma (1963), the amount of

water held at saturation was used to measure total porosity to a depth of 1.6 m, table 6.10.

Table 6-10 Total porosity of Tuppal clay (m3/m3), Talsma (1963)

D e p t h ( m ) T o t a l p o r o s i t y

0 - 0 . 2 0 . 4 30 . 2 - 0 . 4 5 0 . 4 30 . 4 5 - 0 . 7 0 . 4 50 . 7 - 1 0 . 4 11 - 1 . 3 0 . 41 . 3 - 1 . 6 0 . 4

Determinations of aggregate porosity have also been made by Loveday and Scotter

(1966) for aggregates of Willbriggie clay loams. Total porosity was determined on air-

dry surface aggregates and was found to vary between 0.33-0.45 m3/m3.

66


6.1.2.1 Infiltration studies

McIntyre et al. (1982) conducted infiltration studies on a bare, ponded Marah clay loam

at Benerembah in the MIA. Short-term infiltration measurements on the control were

undertaken with three ring infiltrometers and also estimated from soil moisture changes

during the ponding period. The control plot had a ploughed layer of heterogeneous

material consisting of dry clods and finer soil. Short term infiltration on the control plot

was found to vary dramatically, figure 6.5, the rather large shorter term infiltration

recorded by the second infiltrometer was caused by water breakthrough to a crack.

Figure 6-5 Short-term infiltration during ponding on an initially dry soil

Rapid flow through infiltrometer two was caused by a water break through to a crack.

However, the rapid flow ceased after 90 min and the infiltration was similar to the other

infiltrometers after 90 min. Long term infiltration for the control plot during ponding was

determined by measurements form two ring infiltrometers. Mean cumulative infiltration

67

was found to be 276mm for a 379-day period. Infiltration rates during ponding were

found to be 5.3 mm/day during the first week of ponding, 1 mm/day from 2-5 weeks and

0.7 mm/day after a 16-week period.

van der Lelij and Talsma (1977) also undertook infiltration determinations on Willbriggie

and Mundiwa clay loams in both the MIA and CIA irrigation areas. Studies of infiltration

during prolonged ponding were made with 23 infiltrometers on several sites. The

distribution of infiltration totals within transitional red brown earths as measured at the

23 sites is shown in figure 6.6 for a 2-16 week period from the start of permanent

ponding.

Figure 6-6 Frequency distribution of infiltration totals measured over a 2-16 week

period of permanent ponding on transitional red brown earths (van der Lelij and

Talsma 1977)

Mean cumulative infiltration from the 23 infiltrometers over a 16-week period is shown

in figure 6.7. Mean infiltration rate at the end of 16 weeks was found to be 0.25 mm/day.

68

Figure 6-7 Cumulative infiltration for transitional red brown earths as measured by

van der Lelij and Talsma (1977)

Loveday et al. (1984) also undertook infiltration measurements on a Mundiwa clay loam

at two sites in the Whittion area of the MIA. Two plots were ponded with water for a

one-week period and then drained and covered for several days before sampling.

Infiltration rates were determined using 0.3 m diameter rings at the surface and at

surfaces exposed at 0.3 and 0.6 m depths after the rings had stood ponded for 24 hours.

Four determinations of infiltration rate were made at the three depths for the two soil

profiles. Mean infiltration rates are shown in table 6.11.

Table 6-11 Infiltration rates (mm/day) as measure by Loveday et al. (1984)

Depth (m) Infiltration rate (mm/day)

surface 16.8

0.3 2.7

0.6 7.1

69


Laboratory measurements

Laboratory determinations of saturated hydraulic conductivity on transitional red brown

earth soils have been carried out by Loveday et al. (1978) at nine sites in the MIA,

consisting of Willbriggie clay loams, Willbriggie clays, Marah clay loams and Marah

loams. Saturated hydraulic conductivity was determined on ground soil repacked into

columns taken from the sites at 0-0.2 m depths. Two samples were taken from each site

and saturated hydraulic conductivity’s measured after 24 and 48-hour periods. Results

from the study are presented in table 6.12 together with a cumulative probability

distribution shown in figure 6.8.

Table 6-12 Statistical data relating to saturated hydraulic conductivities of

transitional red brown earths as determined by Loveday et al. (1978)

Time Average value

Lowest value

Highest value

Standard deviation



24 hr 20 4 65 18 90 14 14 1248 hr 14 3 57 16 109 8 9 12

70

0

0.25

0.5

0.75

1

0 50 100 150Hydraulic conduct ivity (mm/day)

Pro

babi

lity

of e

xcee

denc

e

24hr

48hr

Figure 6-8 Cumulative probability distributions of hydraulic conductivities of

transitional red brown earths, after Loveday et al. (1978)

Loveday et al. (1970) also undertook hydraulic conductivity determinations on a Marah

clay loam located in the MIA. Eight cores of 0.073 m diameter and 0.05 m long were

taken from a 0.05-0.1 m depth on a Marah clay loam, which had been ploughed. Mean

equilibrium hydraulic conductivity was found to be 166 mm/day with a standard error of

72 mm/day. Six core samples were also taken from a 0.3-0.35 m depth and mean

hydraulic conductivity was found to be 5.52 mm/day with a standard error of 8.64

mm/day, highlighting the difference between surface and subsoil hydraulic conductivity

after cultivation.

Saturated hydraulic conductivity determinations of a Mundiwa clay loam have been

undertaken by Loveday et al. (1984) on two sites in the Whitton area. Two plots were

ponded with water for a one week period and drained and covered for several days before

sampling. Six cores of 0.075 m diameter and 0.05 m long were taken at three profile

depths and results for the two plots are shown in table 6.13.

71

Table 6-13 Saturated hydraulic conductivity (mm/day) measured by Loveday et al.

(1984)

Hydraulic conductivit y (mm/da y)Depth (m) Plot 1 Plot 2

Average Low Hi gh Average Low High

0-0.05 1189 12 6500 96 24 2830.3-0.35 <0.2 <0.2 <0.2 <0.2 <0.2 <0.20.6-0.65 <0.2 <0.2 <0.2 <0.2 <0.2 <0.2

The rather large saturated hydraulic conductivity recorded at plot one was not explained,

however if the highest measurement of 6500 mm/day is ignored then the average

hydraulic conductivity for plot 1 in the 0-0.05 m layer is 128 mm/day.

van der Lelij and Talsma (1977) also undertook laboratory determinations on large

undisturbed core samples from a 0-0.3 m depth on a transitional red brown earths which

had been ponded and found the saturated hydraulic conductivity to be 0.018 mm/day after

a 100 day ponding period.

Field determinations

Field determination of hydraulic conductivity has been undertaken by McIntyre et

al. (1982) for a Marah clay loam. Hydraulic conductivities were determined when

moisture contents had reached their maximum value from infiltration and pressure

potential data measured with a neutron moisture meter and tensiometers. Hydraulic

conductivity variation with time during ponding is shown in the table 6.14 after McIntyre

et al. (1982).

72

Table 6-14 Hydraulic conductivity (mm/day) and its variation with time during

ponding, McIntyre et al. (1982)

Depth Days of pondinginterval (m) 111 141 190 254 308 379

0.1-0.25 0.2 0.15 0.1 0.073 0.091 0.110.25-0.55 0.16 0.13 0.097 0.07 0.035 0.0260.55-0.85 0.34 0.29 0.21 0.15 0.062 0.0560.85-1.50 0.21 0.2 0.12 0.151.5-2.10 0.31

van der Lelij and Talsma (1977) also undertook field determinations of hydraulic

conductivity of Willbriggie and Mundiwa clay loams located in the MIA and CIA during

periods of extended ponding. Hydraulic conductivity was calculated from fluxes and

gradients, in the top soil and sub soil during a ponding period of 10-100 days, table 6.15.

Sides et al. (1993) also undertook hydraulic conductivity measurements of a Willbriggie

clay loam during ponding in order to estimate recharge. Nested piezometers were used at

three profile depth ranges to estimate hydraulic conductivity, table 6.16.

Table 6-15 Potential gradient and hydraulic conductivity of a transitional red brown

earths during ponding, van der Lelij and Talsma (1977)

Ponding Topsoil (0-0.3 m) Subsoil (0.3-1.2 m)period Infiltration v Gradient Hydraulic Gradient Hydraulic Potential

conductivity conductivity(days) (mm/day) (mm/day) (mm/day) (cm h2O)

10-100 0.14 5.9 0.023 0.7 0.21 -136

73

Table 6-16 Estimated hydraulic conductivity of a Willbriggie clay loam with a high

watertable, Sides et al 1993.

Estimated hydraulic conductiv ityEffective layerwidth (m)

Minimum Maximum Average Standard dev iation

0.2-0.5 2 8.5 4.8 2.30.7-1.0 3.5 10 5.9 1.61.2-1.5 10 45 21.7 13.6

Measurements of hydraulic conductivity on Tuppal clay have also been undertaken by

Talsma (1963) using the auger hole method over successive depths. Saturated hydraulic

conductivity was found to be 169 mm/day with an error of 51 mm/day for 10

measurements made between depths of 0.2-1.4 m.


Determinations of available water for transitional red brown earths have been made by

Loveday and Scotter (1966) for Marah clay and Marah sandy clay loams in the

Warrawidgee area of the MIA. Available water was determined from laboratory

measurements of moisture contents of aggregates at 10kpa and 1500 kPa, taken from

depths of 0-0.03, 0.03-0.1, 0.1-0.2, 0.2-0.3 and 0.3-0.4 m. From these measurements

available water for the top 0.4 m of soil was calculated. For the three samples available

water was calculated to be 0.056, 0.056 and 0.055 m for the top 0.4 m of soil.

Loveday et al. (1977) also determined available water for 14 sites on Willbriggie and

Marah clay loams. Sites were sampled before irrigation and then between 1-3 days after

irrigation. Moisture contents at 1500 kPa were then determined from samples and the

difference between 1500 kPa moisture content and post irrigation moisture content values

reported as the available water. For the 14 samples average available water to 0.6 m was

found to be 0.078 m with a maximum of 0.103 m, minimum of 0.053 m.

74

Talsma (1963) also undertook available water determination to a 1.6 m depth of a Tuppal

clay. Available water was determined from differences between 10 and 1500 kPa

moisture contents and results from the study are presented in table 6.17.

Table 6-17 Available water of a Tuppal clay, Talsma (1963)

Soil layer

(m)

Available water

(m)

0-0.3 0.045

0.3-0.5 0.026

0.5-0.7 0.036

0.7-1.1 0.059

1.1-1.4 0.051

1.4-1.6 0.037

0-1.6 0.255

Loveday et al. (1966) also undertook determinations of available water for Willbriggie

clay loams, Willbriggie loams and Tuppal clays loams in the CIA. Available water for a

depth between 0-0.3 m was calculated from measurements of 10 and 1500 kPa moisture

content samples taken at depths of 0-0.025, 0.025-0.1 and 0.2-0.3 at nine sites, which

ranged from a low of 0.029 m to a high of 0.041m with a mean of 0.035 m for the top 0.3

m of soil.

Water content profiles to a depth of 0.6 m have been carried out by Loveday et al. (1977)

for a Marah clay loam and sandy clay loam. Water contents were determined when stress

symptoms first appeared in subterranean clover growing on the soil and then again after

the same profile had been irrigated. It was not specified how many days after irrigation or

what volume of water had been applied, however the difference between the post and pre

irrigation sampling was used as an approximation of the available water. 1500 kPa

moisture content determinations were also made on the profiles, table 6.20.

75

1500 kPa suctions for transitional red brown earth soils have been carried out by Loveday

et al. (1966) for Willbriggie clay loams, Willbriggie loams and Tuppal clay loams at nine

sites in the CIA with two replicates were undertaken at each site, table 6.18.

Table 6-18 Ranges of 1500 kPa moisture contents (m3/m3) of transitional red brown


Depth (m) 0-0.025 0.025-0.1 0.2-0.3Low High Low High Low High

Volumetric water 0.099 0.181 0.093 0.214 0.287 0.383content

Loveday et al. (1978) also determined moisture content at 1500 kPa suctions for

Willbri ggie clay loams, Willbriggie clays, Marah clay loams and Marah loams at 15 sites

in the MIA, two replicates were taken at each site, table 6.19.

Table 6-19 Ranges of 1500 kPa moisture contents (m3/m3) for transitional red brown


Depth (m) 0-0.1 0.2-0.3 0.3-0.4 0.4-0.6 0.6-0.8Low High Low High Low High Low High Low High

Volumetricwater 0.178 0.259 0.274 0.349 0.283 0.363 0.285 0.374 0.249 0.36content

Determinations of permanent wilting point on a Mundiwa clay loam at Whitton in the

MIA have also been undertaken by Loveday et al. (1984), table 6.20.

Variation of 1500 kPa moisture content determinations from all studies with depth are

shown in figure 6.9 along with statistical data relating to all studies found on transitional

red brown earths in table 6.21.

76

Table 6-20 1500 kPa moisture contents (m3/m3) of transitional red brown earths

Soil Depth (m) AuthorType 0.025 0.05 0.1 0.3 0.4 0.6 0.8 0.9 1.2 1.6

Willbriggie 0.136 0.150 0.339 Lovedayclay 1966loam (average 5)

Willbriggie 0.095 0.098 0.337 (average 2)loam

Tuppal 0.12 0.152 0.34 (average 2)clayloam

Willbriggie 0.225 0.302 0.310 0.316 0.313 Lovedayclay 1978loam (average 5)

Marah 0.190 0.305 0.317 0.306 0.265 (average 2)loam

Marah 0.231 0.296 0.306 0.318 0.304 (average 3)clayloam

Willbriggie 0.224 0.32 0.351 0.36 0.358clay

Tuppal 0.235 0.24 0.277 0.244 0.226 0.204 Talsmaclay 1963

Mundiwa 0.1 0.31 0.27 Lovedayclay 1984loam (average 2)

Marah 0.155 0.26 0.27 0.28 Lovedayclay {0.08} {0.23} {0.25} {0.29} 1977loam (average 2)

{ } indicates field determination

77

0

0.2

0.4

0.6

0.8

1

1.2

1.4

1.6

0 0.1 0.2 0.3 0.4 0.5 0.6

M o is tu re Con te n t (m 3/m 3)D

epth

(m

)

Figure 6-9 Variation of volumetric water contents at 1500 kPa for transitional red

brown earths

Table 6-21 Statistical data relating to 1500 kPa volumetric moisture content studies

on transitional red brown earths

Depth (m)

Average value

Lowest value

Highest value

Standard dev iation

Coeff icient of v ariation


0.025 0.128 0.084 0.181 0.029 23 0.129 0.125 160.05 0.128 0.100 0.155 0.039 31 0.128 0.124 20.1 0.188 0.092 0.259 0.050 26 0.198 0.181 390.3 0.314 0.265 0.390 0.030 9 0.309 0.313 390.4 0.310 0.240 0.363 0.022 7 0.311 0.310 230.6 0.315 0.270 0.374 0.026 8 0.312 0.314 240.8 0.306 0.249 0.360 0.034 11 0.305 0.304 220.9 0.244 11.2 0.226 11.6 0.204 1

10 kPa moisture content determinations have been undertaken by Loveday et al. (1966)

for Willbri ggie clay loams, Willbriggie loams and Tuppal clay loams at nine sites in the

CIA, two replicates were taken, table 6.22. Average moisture contents of each soil are

shown in table 6.23.

78

Table 6-22 10 kPa moisture contents (m3/m3) of transitional red brown earths as

measured by Loveday et al. (1966)

Depth (m)0-0.025 0.025-0.1 0.2-0.3

Low High Low High Low High

Volumetricwater 0.213 0.305 0.225 0.314 0.397 0.471content

Loveday et al. (1984) also undertook moisture content determinations at 10 kPa suctions

on a Mundiwa clay loam at Whitton in the MIA, table 6.23. Talsma (1963) also

undertook 10 kPa moisture content determinations on a Tuppal clay, table 6.23. Variation

of 10 kPa moisture contents from the above studies are shown in figure 6.10, and

statistical data in table 6.24.

Table 6-23 10 kPa volumetric moisture contents (m3/m3) of transitional red brown

earths


Will brigg ie 0.267 0.264 0.447 Lovedayclay 1966loam (average 5)

Tuppal 0.279 0.294 0.414 (average 2)clayloam

Willbrigg ie 0.229 0.240 0.453 (average 2)loam

Mund iwa 0.3 0.45 0.41 Lovedayclay 1984loam

Tuppal 0.367 0.377 0.374 0.355 0.348 0.351 Talsmacaly 1963

79

0

0.2

0.4

0.6

0.8

1

1.2

1.4

1.6

0 0.1 0.2 0.3 0.4 0.5

M o is tu r e Co n ten t (m 3/m 3)

Dep

th (

m)

Figure 6-10 Variation of volumetric water contents at 10 kPa for transitional red

brown earths

Table 6-24 Statistical data relating to 10 kPa volumetric moisture content (m3/m3)

studies on transitional red brown earths

Depth (m) Average Lowest Highest Standard dev iation

Coeff icienof v ariation

Median Geomean No. ofsamp les

0.025 0.285 0.226 0.340 0.026 11.48 0.291 0.284 240.05 0.300 10.1 0.271 0.238 0.314 0.025 10.67 0.268 0.270 120.3 0.444 0.397 0.520 0.022 5.65 0.442 0.443 240.4 0.377 10.6 0.407 0.360 0.450 0.028 7.89 0.405 0.406 120.9 0.355 11.2 0.348 11.6 0.351 1

80


Electrical conductivity studies for transitional red brown earths have been undertaken by

Loveday et al. (1978) for Willbriggie and Marah clay loams and Marah loams at 15 sites

in the MIA., with two replicates at each site, table 6.25.

Table 6-25 Mean electrical conductivities (mS/cm) of transitional red brown earths

Loveday et al. (1978)

Depth interval (m) Mean electrical cond uct iv ity (1:5)

0-0.1 0.1180.1-0.2 0.0960.2-0.3 0.150.3-0.4 0.2230.4-0.6 0.3780.6-0.8 0.636

Christen (1994) also undertook electrical conductivity measurements of Morago and

Mundiwa clay loams at Whitton in the MIA. Electrical conductivity of a saturated paste

measured at depths of 0.1-0.16 and 0.55-0.7 m were 0.14 -0.1 mS/cm and 1.23-1.05

mS/cm respectively. Loveday et al. (1984) also determined electrical conductivity in a

1:5 water suspension for a Mundiwa clay loam to a 1 m depth at 0.1 m intervals. Ten

replicates were made at each depth and mean electrical conductivity ranged from a low of

0.04 mS/cm at a 0-0.1m depth to a maximum of 0.25 mS/cm at 0.9-1 m.

Electrical conductivities of a Willbriggie clay loam to a depth of 3 m have been

determined by Sleeman and Stannard (1983), ranging from 0.49 mS/cm at a 0.05-0.15 m

depth to a maximum of 1.7 mS/cm at 1-1.5 m before decreasing to 1.1 mS/cm at 2.6-3 m.

Loveday et al. (1974) also undertook electrical conductivity determinations of a Marah

clay loam to 5 m. Mean electrical conductivity ranged from a low of 0.48 mS/cm at 0.25

m to a high of 2.12 mS/cm at 1.5 m before decreasing to 1.55 mS/cm at 5 m.

81

Loveday et al. (1970) also conducted measurements of electrical conductivity on a Marah

clay loam at depths of 0-0.05, 0.1-0.2 and 0.5-0.6 m. Electrical conductivity was found to

be 0.15, 0.24 and 1.04 mS/cm for the respective depths. Table 6.26 shows the statistical

data relating to electrical conductivity in 1:5 suspension from all of the above mentioned

studies. Variation of electrical conductivity with depth from the studies is shown in figure

6.11.

0

0.1

0.2

0.3

0.4

0.5

0.6

0.7

0.8

0 0.5 1 1.5 2 2.5 3EC (mS/cm)

De

pth

(m

)

Figure 6-11 Variation of electrical conductivity (mS/cm) with depth

82

Table 6-26 Statistical data relating to electrical conductivity (mS/cm) of transitional

red brown earths

Depth (m)

Average Lowest Highes t Standard dev iation



0.1 0.128 0.040 0.490 0.078 61 0.120 0.115 290.2 0.135 0.030 0.860 0.167 124 0.090 0.094 280.3 0.146 0.030 0.450 0.094 64 0.120 0.121 260.4 0.253 0.030 1.200 0.240 95 0.180 0.183 270.6 0.457 0.060 1.430 0.359 79 0.300 0.347 290.8 0.654 0.120 2.800 0.637 97 0.360 0.465 270.9 0.190 11 1.178 0.250 1.830 0.735 62 1.315 0.922 41.5 2.120 12.5 1.523 1.050 2.000 0.468 31 1.520 1.467 43 1.205 1.100 1.310 0.148 12 1.205 1.200 24 1.480 15 1.550 1

Exchangeable sodium percentages of transitional red brown earths soil profiles have been

calculated from exchangeable cation data recorded by Loveday et al. (1966) for

Willbri ggie clay loams, Willbriggie clays and Tuppal clay loams at nine sites in the CIA.

ESP was also calculated from exchangeable cations measured by Loveday et al. (1978)

on Willbriggie clay loams, Willbriggie clay, Marah clay loams and Marah loams, table

6.27. ESP has also been determined by Blackwell et al. (1990) for a Mundiwa clay loam,

table 6.27.

McIntyre et al. (1982) also determined ESP for a Marah clay, table 6.27.

Loveday and Scotter (1966) also determined ESP of two transitional red brown earths

during an experiment into the emergence response of subterranean clover to dissolved

gypsum, table 6.27. Variation of ESP with depth from results of the above studies is

shown in figure 6.12. Statistical data relating to ESP for transitional red brown earths is

shown in table 6.28.

83

Table 6-27 ESP of transitional red brown earths

Soil Depth (m) AuthorType 0.025 0.1 0.3 0.6

Willbriggie 2.8 6.8 Lovedayclay 1978loam (average 8)

Marah 0.7 3.3 (average 2)loam

Willbriggie 1.8 4.7clay

Marah 5.7 13.6 (average 2)clayloam

Willbriggie 1.9 2.5 8.1 Lovedayclay 1966loam (average 5)

Tuppal 1 2.4 5.1 (average 2)clayloam

Willbriggie 1.2 1.4 7.9 (average 2)loam

Mundiwa 2 4.7 Blackwellclay 1990loam

Willbriggie 13 Lovedayclay and

Scotter

Marah 18.8 18.8 McIntyreclay 1982loam

84

0

0.1

0.2

0.3

0.4

0.5

0.6

0 5 10 15 20 25

ESPD

epth

(m

)

Figure 6-12 Variation of ESP with depth

Table 6-28 Statistical data relating to ESP of transitional red brown earths

Depth (m)

Average Lowest Highest Standard dev iation



0.025 2.3 0.8 9.3 2.3 101 1.9 1.8 120.1 3.0 0.0 20.0 3.0 101 2.3 2.0 280.3 7.3 0.6 19.0 4.0 55 6.7 6.1 270.6 18.8 1

85

7 RED BROWN EARTHS

7.1 Soils of the upper hillslopes

7.1.1 Physical composition


Particle size analysis for a Ballingall loam located in the Tharbogang area has been

undertaken by Norrish and Tiller (1976). Particle size analysis on a sample from a 0.8-0.9

m depth found 47 % sand, 17% silt and 23 % clay.



Studies on hydraulic conductivity of soils of the upper hillslopes has been compiled by

van der Lelij (1974) for Ballingall, Tharbogang and Wyangan loams located in the

Mirrool irrigation area. The auger hole method was used to determine hydraulic

conductivity on 121, 65 and 36 sites respective of the soil types listed above. Average

hydraulic conductivity for the soils as calculated by van der Lelij (1974) are listed in table

7.1 and have been further divided based on watertable (WT) depth with normal

watertables (Nor. WT) between 0.75 and 1.05 m below the surface, deep watertables

(Deep WT) deeper than 1.05 m and high watertables (High WT) within 0.75 m of the

surface.

86

Table 7-1 Hydraulic conductivities (mm/day) of sub-plastic soils of the upper

hillslopes, after van der Lelij (1974).

SoilType

Mean hydraulic Mean hydraulic Mean hydraulic

0.5-0.9 m 0.9-1.4 m 1.4-1.9 mcond uctivity Conduc tivity cond uctivity

(Nor. WT) (High WT) (Deep WT)

Ballingall loam 945 1530 1128 1097 1097 1097

Tharbogang loam 1326 307 1021 1097 1097 1097

Wyangan loam 677 887 722 725 725 725

Average hydraulic cond uctivity

7.2 Soils of the lower hillslopes



Particle size analysis on red-brown earths of the lower hillslopes have been carried out

by Smith (unpublished) for a Hanwood loam to a 1.5 m depth. Particle size analysis was

carried out at 0.1 m intervals with four replicates, table 7.2. Prathapar (pers comms)

compiled results of particle size analysis undertaken by Blackmore on a Hanwood loam,

table 7.2. Talsma (1963) undertook particle size analysis of a Jondaryan loam located at

farm 151 Koonadan in the MIA, table 7.2. Particle size analysis has also been undertaken

on a Hanwood loam at CSIRO Griffith, by Charlesworth (unpublished data) in the MIA,

table 7.2. Average particle size distribution of soils of the lower hillslopes to a 0.8 m

depth is shown in figure 7.1.

87

0

0.1

0.2

0.3

0.4

0.5

0.6

0.7

0.8

0 10 20 30 40 50 60 70%

Dep

th (

m)

Sand

Silt

Clay

Figure 7-1 Average particle size distribution of soils of the lower hillslopes

Table 7-2 Particle size distributions of soils of the lower hillslopes

Soil Depth (m) AuthorType 0.1 0.2 0.3 0.4 0.5 0.6 0.7 0.8 0.9 1 1.1 1.2 1.3 1.4 1.5

Hanwood CS % 15 15 11 7 5 6 6 7 7 6 7 8 11 6 4 Smithloam FS % 39 38 36 28 31 29 24 26 24 28 31 33 23 37 43 (unpublished)

Si % 15 13 13 16 29 31 29 28 28 26 25 22 22 23 22C % 31 34 40 49 32 31 36 37 35 34 30 30 29 25 25

Hanwood CS % 10 10 11 10 8 7 6 5 6 3 Charlesworthloam FS % 62 60 61 61 50 47 55 60 61 67 (unpublished)

Si % 6 8 7 6 5 7 9 11 9 8C % 22 22 21 23 37 39 30 24 26 22

Hanwood Sand %54 43 34 Prathaparloam Si % 16 8 24 (unpublished)

C % 30 49 45

Jondaryan Sand %73 33 35 41 43 43 Talsma loam Si % 9 11 14 16 20 20 1963

C % 18 56 52 43 37 37

88


Talsma (1963) undertook bulk density determinations on a Jondaryan loam located in the

MIA, with four replicates at each depth, table 7.3.

Meyer (1992) also conducted bulk density determination of a Hanwood loam during

calibration of Neutron and Gamma probes, three replicates at each depth, table 7.3.

Prathapar (unpublished) also compiled bulk density data undertaken on a Hanwood loam,

table 7.3. Variation of bulk density with depth has been plotted for the above mentioned

studies in figure 7.2.

Table 7-3 Bulk densities of soils of the lower hillslopes

Soil Depth (m) AuthorType 0.1 0.2 0.3 0.4 0.6 0.8 1 1.2 1.4 1.6

Hanwood 1500 1560 1550 1380 1510 1470 1400 1560 1600 Meyerloam 1992

Jondaryan 1600 1410 1460 1540 1570 1550 Talsmaloam 1963

Hanwood 1450 1350 1340 Prathaparloam (unpublished)

89

0

0.2

0.4

0.6

0.8

1

1.2

1.4

1.6

1.8

1000 1200 1400 1600 1800 2000

B ulk dens ity (kg /m3)D

epth

(m

)

Figure 7-2 Variation of bulk density (kg/m3) with depth for soil of the lower

hillslopes

7.2.1.3 Porosity

Porosity measurements of soils of the lower hillslopes has been undertaken by Talsma

(1963) during investigations into the control of saline groundwater. Total porosity was

estimated from the amount of water held at saturation at depths of 0.1, 0.305, 0.61, 0.915,

1.22 and 1.525 m. Results from the study gave total porosity as 0.532, 0.42, 0.454, 0.408,

0.361 and 0.346 m3/m3 for the respective depths.

90

7.3 Water Movement


Measurements of hydraulic conductivity have been documented by van der Lelij (1974)

for five subplastic soils of the hillslopes in the Mirrool Irrigation Area. The soil type

included in the report were Hanwood loam and sandy loam, Yenda loam, Type 9, Bilbul

clay loam, Jondaryan loam and Griffith clay loam. Hydraulic conductivity’s documented

in the study were by the auger hole method conducted on 206, 149, 36, 118, 221 and 96

sites for the respective soil types. Auger holes were bored to depths between 1.8-1.2 m.

Averages hydraulic conductivities for the soils are shown in table 7.4, and have been

further divided based on watertable depth with normal watertables (Nor. WT) being

between 0.75 and 1.05 below the surface, low watertables (Deep WT) deeper than 1.05 m

and high watertables (High WT) within 0.75 m of the surface.

91

Table 7-4 Hydraulic conductivities (mm/day) of soils of the lower hill slopes, after

van der Lelij (1974).

Soil Average hydraulic conductivityType

Mean hydraulic Mean hydraulic Mean hydraulic

conductivity conductivity conductivity 0.5-0.9 m 0.9-1.4 m 1.4-1.9 m

(Nor. WT) (High WT) (Deep WT)

Hanwood 692 573 415 274 969 415

loam

Hanwood 539 448 290 223 607 290

sandy loam

Yenda 421 597 347 1039 494 347

loam

Type 9 216 232 116 271 317 116

Bilbul 213 351 85 768 341 85

clay loam

Jondaryan 146 149 110 131 131 131

loam

Griffith 91 223 58 549 125 58

clay loam

Hydraulic conductivity of a Hanwood loam have also been documented by Prathapar

(unpublished data). Saturated hydraulic conductivity was found to be 180 mm/day at 0-

0.1 m and 90mm/day at depths of 0.25-0.35 and 0.6-0.7 m.

Talsma (1963) undertook measurements of saturated hydraulic conductivity of Jondaryan

loam at depths between 0.3-0.9 and 0.9-1.5 m using the auger hole method. Saturated

hydraulic conductivity was found to be 43 mm/day and 76 mm/day at the respective

depths.

92


Water content profiles for soils of the lower hillslopes have been carried out by Meyer

(1992) for a Hanwood loam. Soil water content profiles were measured from samples

after a wheat crop had died from water deficiency ( permanent wilting point) to a profile

depth of 1.87 m and then five days after the same profile had been fully wetted and

allowed to drain (field capacity). Gravimetric soil water contents were multiplied by field

bulk densities to obtain volumetric soil water profiles with the difference between the two

representing the available water. Figure 7.3 shows the water content profiles taken from

Meyer (1992).

Figure 7-3 Volumetric moisture content profile of a Hanwood loam as determined

by Meyer (1992): “dry end” = permanent wilting point, “wet end” = field capacity

93

Talsma (1963) also undertook determinations of moisture contents of a Jondaryan loam at

suctions of 10 and 1500 kPa, for field capacity and permanent wilting point, table 7.5 and

figure 7.4.

Table 7-5 10 and 1500 kPa volumetric moisture contents of Jondaryan Loam,

Talsma (1963)

Depth (m) 10 kPa 1500 kPa

0.1 0.26 0.0940.305 0.35 0.2790.61 0.406 0.2830.915 0.348 0.2621.22 0.33 0.2221.525 0.305 0.211

0

0.2

0.4

0.6

0.8

1

1.2

1.4

1.6

1.8

0 0.1 0.2 0.3 0.4 0.5

Vol umetr i c moi sture content (m3/m3)

Dep

th (

m)

1500kPa

10kPa

Figure 7-4 Volumetric moisture content profiles of a Jondaryan loam, Talsma

(1963)

94

7.4 Soils of the plains - subplastic subsoil group


7.4.1.1 Particle size distribution

Particle size distribution measurement on subplastic soils of the plains were undertaken at

three sites in the MIA by Sinclair et aI (1994), see Table 7-6.

Table 7-6 Particle size distribution of plastic soils of the plains, after Sinclair et al

(1994)

Soil Type Depth (m)

0 - 10 10 - 20 20 - 30 30 - 50

Bilbul CS % 5 5 3 1

loam FS % 54 45 48 48

Si % 10 13 4 12

C % 31 37 45 43

Bilbul CS % 5 7 6 2

loam FS % 46 56 42 33

Si % 10 10 7 5

C % 29 27 45 60

Griffith CS % 8 6 7 5

loam FS % 45 40 33 32

Si % 12 12 5 8

C % 35 42 55 55

95


Bulk density measurement were undertaken at the same three sites by Sinclair et aI

(1994), see Table 7-7.

Table 7-7 Mean bulk densities (kg/m3) of intact cores (0 – 5 cm) at distances away

from the vine row for plastic soils of the plains

Soil type Distance away from the base of the vine row (cm)

0 40 60 80 100 120 140

Bilbul loam 1120 1340 1290 1260 1230 1320 1340

Bilbul loam 1390 1400 1580 1450 1460 1500 1360

Griffith loam 1240 1300 1440 1320 1340 1420 1460


Studies on hydraulic conductivity of plastic plains soils with a subplastic subsoil have

been undertaken by van der Lelij (1974) for Bilbul, Griffith, Mirrool and Yoogali loams

located in the Mirrool irrigation area. The auger hole method was used to determine

hydraulic conductivity on 146, 182, 65 and 113 respectively sites of the soil types listed

above. Average hydraulic conductivity for the soils are listed in table 7.8 and have been

further divided based on watertable depth with normal watertables (Nor. WT) being

between 0.75 and 1.05 m below the surface, low watertables (Deep WT) deeper than 1.05

m and high watertables (High WT) within 0.75 m of the surface.

96

Table 7-8 Hydraulic conductivities (mm/day) of sub soil plastic soils of the plains,

after van der Lelij (1974).

Soil Average hydraulic conduc tivityType Mean hydraulic Mean hydraulic Mean hydraulic

condu ctivity Conduc tivity condu ctivity 0.5-0.9 m 0.9-1.4 m 1.4-1.9 m(Nor. WT) (High WT) (Deep WT)

Bilbul loam

375 360 155 320 594 155

Griff ith loam

259 299 155 396 363 155

Mirrool loam

195 299 104 561 287 104

Yoogali loam

174 219 201 192 192 192

7.5 Soils of the Plains (normal subsoil group)



Particle size analysis of plastic red brown earth’s of the plains has been undertaken by

Loveday et al. (1966) for three Birganbigil fine sandy loams located in the CIA, with four

replicates per site, ranges of particle size distribution found in the study are shown in

table 7.9.

97

Table 7-9 Ranges of particle size distribution for plastic soils of the plains Loveday

et al. (1966)

Particlesize Low High Low High Low High

CS % 14 31 15 33 7 16FS % 37 56 34 56 15 32Si % 16 20 14 18 4 11C % 10 18 11 22 48 65

0-0.025 0.025-0.1 0.2-0.3Depth (m)

Loveday et al. (1978) also undertook particle size analysis on plastic red brown earths of

the plains located in the MIA, two sites of Birganbigil fine sandy loam, table 7.10.

Table 7-10 Ranges of particle size for soils of the plains, Loveday et al. (1978)

Particlesize Low High Low High

CS % 24 29 12 13FS % 40 47 23 29Si % 9 12 2 5C % 17 24 54 63

Depth (m)0-0.1 0.2-0.3

Particle size analysis for a Birganbigil clay loam has also been carried out by Thompson

(1978), table 7.11. van der Lelij and Talsma (1977) found a mean clay content of 56% at

a 0.2-0.3 m depths for Cobram, Thulabin and Birganbigil loams during investigation into

infiltration and water movement in these soils. Talsma (1963) undertook particle size

analysis of a Camarooka clay loam located in the MIA, table 7.11.

98

Table 7-11 Particle size distribution of soils of the plains - normal

Soil Depth (m) AuthorType 0.025 0.1 0.15 0.3 0.6 0.9 1 1.2 1.5

Birganbigil CS % 16 16 8 Lovedayfine FS % 54 55 29 1966sandy Si % 17 17 8 (average)loam C % 13 12 55

Birganbigil CS % 26 12 Lovedayfine FS % 44 26 1978sandy Si % 11 3 (average)loam C % 20 59

Camarooka Sand % 51 40 44 43 44 45 Talsmaclay Si % 10 12 9 8 6 6 1963loam C % 39 48 47 49 50 49

Birganbigil CS % 12 9 9 Thompsonclay FS % 28 21 20 1978loam Si % 13 5 10

C % 47 65 61

Analysis of all the above studies at depths between 0-0.1 and 0.2-0.3 m are shown in

tables 7.12 and 7.13 respectively, with cumulative probability distribution in figures 7.5

and 7.6.

Table 7-12 Statistical data relating to size analysis of plastic soils of the plains –

normal, in the 0-0.1 m layer


99

Table 7-13 Statistical data relating to particle size analysis of soils of the plains –

normal, in the 0.2-0.3 m layer


0

0.25

0.5

0.75

1

0 10 20 30 40 50 60%

Pro

babi

lity

of E

xcee

denc

e

CoarseSand

FineSand

Silt

Clay

Figure 7-5 Cumulative probability distribution of particle size in plastic soils of the

plains, 0-0.1 m

100

0

0.25

0.5

0.75

1

0 10 20 30 40 50 60 70%

Pro

abili

ty o

f Exc

eede

nce

CoarseSand

FineSand

Silt

Clay

Figure 7-6 Cumulative probability distribution of particle size in plastic soils of the

plains - normal, 0.2-0.3 m


Loveday et al. (1978) undertook bulk density determinations on two Birganbigil fine

sandy loams located in the MIA, table 7.14. Talsma (1963) conducted bulk density

determinations on a Camarooka clay loam located in the MIA, table 7.14. Determinations

of aggregate densities of plastic soils of the plains have been undertaken by Loveday et

al. (1966) at three sites in the CIA on Birganbigil fine sandy loam, table 7.14. Variation

of densities of plastic soils of the plains with depth are shown in figure 7.7.

101

Table 7-14 Densities of plastic soils of the plains – normal (kg/m3)

Soil Depth (m) AuthorTypes 0.025 0.1 0.2 0.3 0.4 0.6 0.8 0.9 1.2 1.5

Birganbigil {1550} {1664} {1688} {1504} Lovedayfine sandy 1966loam (average)

Birganbigil 1589 1680 1509 1550 1593 1580 Lovedayfine sandy 1978loam (average)

Camarooka 1510 1320 1480 1560 1620 1620 Talsmaclay loam 1963

0

0.2

0.4

0.6

0.8

1

1.2

1.4

1.6

1000 1200 1400 1600 1800 2000

B u lk d e n is ty (k g /m 3 )

Dep

th (

m)

A ggre gatede ns i ty

B u lk de ns i t y

H o r t i c u l tur a ls o i l

Figure 7-7 Variation of density with depth for soils of the plains - normal

7.5.1.3 Porosity

Measurements of porosity of a Camarooka clay loam have been undertaken by Talsma

(1963). Porosity was calculated from the amount of water held at saturation. Porosity

measurements were undertaken at depths of 0.15, 0.305, 0.61, 0.915, 1.22 and 1.525 m

102

and found to be 0.454, 0.493, 0.429, 0.419, 0.389 and 0.389 m3/m3 for the respective

depths.

Loveday et al. (1966) also undertook measurements of total and air filled porosity of

three Birganbigil fine sandy loams at three sites in the CIA. Porosity was measured on

0.0372 m diameter cores taken from depths between 0-0.1 m after the site had been

irrigated. Porosity was then measured at intervals of 24 and 48 hrs. Average total porosity

at both 24 and 48 hr was found to be 0.44 m3/m3 and average air filled porosity at 24 and

48 hr was found to be 0.23 m3/m3 and 0.24 m3/m3 respectively.


7.5.2.1 Infiltration

Studies on infiltration of normal red brown earth’s of the plains have been undertaken by

van der Lelij and Talsma (1977). Infiltration on 14 sites of Cobram, Thulabin and

Birganbigil loams was determined by use of large buffered ring infiltrometers. Infiltration

over a 16 week ponding period was measured and mean infiltration over the time period

is shown in figure 7.8, taken from van der Lelij and Talsma. Mean infiltration rate at the

end of ponding was found to be 0.43 mm/day.

103

Figure 7-8 Mean cumulative infiltration curves (mm) for soils of the plains - normal,

van der Lelij and Talsma (1977)


Laboratory determinations

Laboratory determinations of hydraulic conductivity have been undertaken by Loveday et

al. (1978) for two Birganbigil sandy clay loams located in the MIA. Hydraulic

conductivity was measured on cores 0.046 m diameter between depths of 0-0.2m with

two replicates being undertaken at each site. Hydraulic conductivity was measured at 24

and 48 hour periods, the 24 hour period hydraulic conductivity was found to be 73.2 and

58.32 mm/day from samples of the two sites. Hydraulic conductivity after a 48 hour

period on the same samples was found to be 43.2 and 24.96 mm/day respectively.

104


Field determinations of hydraulic conductivity have been undertaken by Talsma (1963)

using the auger hole method for a Camarooka clay loam. Saturated hydraulic conductivity

measurements were made at depths of 0.7-1.2 and 1.4-2 m. Hydraulic conductivity for the

respective depths was found to be 81 and 65 mm/day.

Van der Lelij (1974) also documented values of hydraulic conductivity as found by the

auger hole method on Beelbangera clay loams and Camarooka sandy loams located in the

Mirrool irrigation area. Hydraulic conductivity on 179 sites for Beelbangera clay loams

and 177 sites for Camarooka sandy loams were used to determine mean hydraulic

conductivity for the soil types, table 7.15. These have been further divided based on

watertable depth with normal watertables (Nor. WT) being between 0.75 and 1.05 m

below the surface, low watertables (Deep WT) deeper than 1.05 m and high watertables

within 0.75 m of the surface.

Table 7-15 Hydraulic conductivity (mm/day) of soils of the plains – normal, van der

Lelij and Talsma (1977)

Soil Average hydraulic conductivityType Mean hydraulic Mean hydraulic Mean hydraulic

conductivity conductivity conductivity 0.5-0.9 m 0.9-1.4 m 1.4-1.9 m(Nor. WT) (High WT) (Deep WT)

Beelbangera clay loam

131 186 70 328 192 70

Camarooka sandy loam

125 168 64 274 186 64

van der Lelij and Talsma (1977) also undertook field determinations of hydraulic

conductivity on Cobram, Thulabin and Birganbigil loams during extended ponding.

Hydraulic conductivity was determined from measured infiltration and potential gradients

measured at two sites for the topsoil and subsoil at 100 days after the site had been

ponded. Results from the study are presented in table 7.16.

105

Table 7-16 Potential gradient and hydraulic conductivity of two soils of the plains –

normal, during ponding, van der Lelij (1974).

Pond ingperiod Inf iltration Gradient Hydraulic Gradient Hydraulic Potent ial

conduct iv ity conduct iv ity(days) (mm/da y) (mm/da y) (mm/da y) (cm H2O)

at 100 1.1 2.4 0.46 1.2 0.89 -65at 100 0.4 3.5 0.11 0.9 0.43 -108

Subso il (0.6-2.3 m)Topso il (0-0.47)


Determinations of available water for plastic red brown earths have been carried out by

Loveday et al. (1966). Available water was calculated for the top 0.3 m soil depths for

three Birganbigil fine sandy loams and a Birganbigil sandy clay loam located in the CIA.

Two replicates were taken on each site and average available water for the top 0.3 m of

soil was 0.032 m with a high of 0.046 m and a low of 0.028 m. Approximations of

permanent wilting points for plastic soils of the plains have been carried out by Loveday

et al. (1966) for Birganbigil fine sandy loam. Water contents were measured at 1500 kPa

suctions, table 7.17. Loveday et al. (1978) determined 1500 kPa moisture content for two

Birganbigil fine sandy loams located in the MIA, table 7.17. Talsma (1963) determined

1500 kPa moisture content of a Camarooka clay loam located in the MIA, table 7.17.

Thompson (1978) determined 1500 kPa moisture content, table 7.17. Variation of

moisture contents at 1500 kPa are shown in figure 7.9. Statistical data relating to 1500

kPa moisture content determinations are shown in table 7.18.

106

Table 7-17 1500 kPa moisture contents (m3/m3) of normal soils of the plains

Soil Depth (m) AuthorType 0.025 0.1 0.2 0.3 0.4 0.6 0.8 0.9 1 1.2 1.5

Birganbigil 0.08 0.09 0.09 0.26 Lovedayfine sandy 1966loam (average 3)

Birganbigil 0.14 0.25 0.29 0.288 0.258 Lovedayfine sandy 1978loam (average 2)

Camarooka 0.227 0.255 0.26 0.287 0.297 0.278 Talsmaclay loam 1963

Birganbigil 0.192 0.27 0.27 Thompsonclay loam 1978

0

0.25

0.5

0.75

1

1.25

1.5

0 0.05 0.1 0.15 0.2 0.25 0.3 0.35

Moisture content (m3/m3)

Dep

th (

m) Hortic ultural

soil

Figure 7-9 Variation of volumetric water contents at 1500 kPa for plastic soils of the

plains

107

Table 7-18 Statistical data relating to studies on 1500 kPa volumetric moisture

contents for normal plains soils


Lowest value

Highest value

Standard deviation

Coefficientof v ariation

Median Geomean No. ofSamples

0.025 0.078 0.071 0.087 0.006 8 0.077 0.078 80.1 0.114 0.069 0.227 0.050 44 0.103 0.105 130.2 0.103 0.072 0.192 0.043 41 0.086 0.098 70.3 0.263 0.216 0.310 0.030 11 0.261 0.262 130.4 0.285 0.270 0.299 0.012 4 0.288 0.285 50.6 0.282 0.260 0.297 0.017 6 0.291 0.282 50.8 0.258 0.235 0.275 0.020 8 0.262 0.258 40.9 0.287 11 0.270 11.2 0.297 11.5 0.278 1

Approximations of field capacity of plastic soils of the plains by 10 kPa suction have

been undertaken by Loveday et al. (1966) for three Birganbigil fine sandy loams located

in the CIA, table 7.19. Talsma (1963) also undertook on a Camarooka clay loam 10 kPa

suctions, table 7.19. Thompson (1978) also estimated moisture content at field capacity

by measuring water content of a Birganbigil clay loam 24 hours after the soil had been

saturated by irrigation, table 7.19. Variation of 10 kPa moisture content determinations

with depth are shown in figure 7.10. Statistical data relating plastic plains soils is shown

in table 7.20.

108

Table 7-19 10 kPa volumetric moisture contents of plastic soils of the plain


Birganbigil 0.199 0.209 0.193 0.385 Lovedayfine sandy 1966loam (average 3)

Camarooka 0.367 0.377 0.374 0.355 0.348 0.351 Talsmaclay loam 1963

Birganbigil {0.334} {0.387} {0.41} Thompsonclay loam 1978

{ } indicates moisture content after 24 hours of drainage

0

0.2

0.4

0.6

0.8

1

1.2

1.4

0 0.1 0.2 0.3 0.4 0.5

W ater Content (m3/m3)

Dep

th (

m)

10 kPa

Horticulturalsoil

Fielddetermination

Figure 7-10 Variation of volumetric water contents at field capacity

109

Table 7-20 Statistical data relating to field capacities of plastic soils of the plains

Depth (m)

Average value

Lowest value

Highest value

Standard deviation



0.025 0.20 0.18 0.22 0.01 6.48 0.20 0.20 80.1 0.23 0.19 0.37 0.05 24.29 0.21 0.22 90.2 0.21 0.18 0.33 0.05 25.74 0.19 0.21 70.3 0.38 0.34 0.44 0.04 9.34 0.38 0.38 90.4 0.39 10.6 0.37 10.9 0.36 11.2 0.35 11.5 0.35 1


Electrical conductivity measurements for plastic soils of the plains have been carried by

Loveday et al. (1978) for two Birganbigil sandy loams, table 7.21.

Table 7-21 Electrical conductivities (mS/cm) of plastic soils of the plains Loveday et

al. (1978)

Depth (m ) Elect rical conduct iv ity (mS/cm)

0.1 0.12 0.18 0.15 0.120.2 0.06 0.06 0.06 0.060.3 0.06 0.06 0.06 0.060.4 0.06 0.18 0.06 0.060.6 0.24 0.24 0.06 0.120.8 0.27 0.3 0.18 0.18

Measurements of exchangeable cations of normal soils of the plains have been

undertaken by Loveday et al. (1966) on three Birganbigil fine sandy loams located in the

CIA. Exchangeable cations were also measured by Loveday et al. (1978) on two

110

Birganbigil fine sandy loams at 0-0.1 and 0.2-0.3 m depths, ESP was calculated from

these studies, table 7.22. Variation of ESP with depth is shown in figure 7.11.

Table 7-22 ESP of normal plains soils

Soil Depth (m ) Au thorType 0.025 0.1 0.3

Birganbig il Lovedayf ine sandy 1.57 0.87 7.29 1966loam (average 3)

Birganbig il Lovedaysandy 0.92 3.61 1978loam (average 2)

0

0.05

0.1

0.15

0.2

0.25

0.3

0.35

0 5 10 15 20

ESP

Dep

th (

m)

Figure 7-11 Variation of ESP with depth for plastic soils of the plain

111

8 SANDS OVER CLAY (SOLODIZED SOLONETZ SOILS)


8.1.1.1 Particle size distribution

Particle size analysis of sands over clay soils have been undertaken by Loveday et al.

(1966) for two Danberry loamy sands and a Cobram sandy loam located in the CIA, table

8.1.

Table 8-1 Ranges of particle size distribution for sands ovr clay soils Loveday (1966)

Particlesize Low High Low High Low High

CS % 33 52 33 52 18 33FS % 25 31 27 32 14 27Si % 8 21 9 22 2 19C % 4 16 4 18 25 52

Depth (m)0-0.025 0.025-0.1 0.2-0.3

Loveday et al. (1978) also undertook particle size analysis on a Thulabin sandy loam and

a Cobram sandy loam located in the MIA, table 8.2.

112

Table 8-2 Ranges of particle size distribution for sands over clay soils Loveday et al.

(1978)

P a rtic les iz e L o w Hig h L o w Hig h

C S % 1 4 5 2 7 3 9F S % 2 9 4 8 1 7 3 7S i % 6 1 7 2 1 2C % 1 2 2 1 3 8 5 1

D e p th (m )0 -0 .0 2 5 0 .0 2 5 -0 .1

Prathapar (unpublished) also compiled particle size analysis for a Thulabin sand, table

8.3. Smith (unpublished) also conducted particle size analysis on a Thulabin sand to a 1

m depth at intervals of 0.1 m, table 8.3. Particle size analysis on a solodized solonetz soil,

Yandera loam, has been undertaken by Talsma (1963), table 8.3. Analysis of particle size

distribution data at 0-0.1 and 0.2-0.3 m depths from all studies is shown in tables 8.4 and

8.5. Cumulative probability distributions of particle size from all studies at depths

between 0-0.1 and 0.2-0.3 m are shown in figures 8.1 and 8.2.

113

Table 8-3 Particle size distribution of solodized solonetz soils

Soil Depth (m) AuthorType 0.025 0.1 0.2 0.3 0.4 0.5 0.6 0.7 0.8 0.9 1 1.2 1.5

Danberry CS % 50 51 30 Lovedayloamy FS % 28 28 16 1966sand Si % 12 13 6 (average 2)

C % 10 8 49

Cobram CS % 35 34 22sandy FS % 31 31 23loam Si % 20 20 17

C % 15 16 39

Thulabin CS % 51 38 Lovedaysandy FS % 30 19 1978loam Si % 8 4

C % 13 45

Cobram CS % 15 9sandy FS % 48 36loam Si % 17 10

C % 21 47

Thulabin Sand % 78 56 50 Prathaparsand Si % 9 2 10

C % 13 42 40

Thulabin CS % 22 23 10 9 13 16 19 23 27 28 Smithsand FS % 40 39 22 15 16 21 27 27 35 37

Si % 9 11 39 10 4 12 10 11 10 11C % 29 27 58 67 67 52 44 39 28 25

Yandera Sand % 67.5 53.8 60.7 66 60.5 60.7 Talsma loam Si % 11.3 11.2 15.1 12.3 15.8 12.7 1963

C % 21.2 35 24.2 21.7 23.7 26.6

114

Table 8-4 Statistical data relating to particle size analysis of solodized solonetz soils,

0-0.1 m


Table 8-5 Statistical data relating to particle size analysis of solodized solonetz soils,

0.2-0.3 m


115

0

0 .1

0 .2

0 .3

0 .4

0 .5

0 .6

0 .7

0 .8

0 .9

1

0 20 40 60%

Pro

babi

lity

of e

xcee

denc

e

C oarseS and

F inesand

S ilt

C lay

Figure 8-1 Cumulative probability distribution of particle size, 0-0.1 m

0

0.1

0 .2

0 .3

0 .4

0 .5

0 .6

0 .7

0 .8

0 .9

1

0 20 40 60%

Pro

babi

lity

of e

xcee

denc

e

C oarseS and

F ineS and

S ilt

C lay

Figure 8-2 Cumulative probability distribution of particle size, 0.2-0.3 m

116

8.1.1.2 Bulk Density

Loveday et al. (1978) undertook bulk density determinations of two sands over clay soils,

Thulabin sandy loam and Cobram sandy loam at two sites located in the MIA, table 8.6.

Talsma (1963) also undertook bulk density determinations of a Yandera loam during

investigations into the control of saline groundwater in the MIA, table 8.6.

Prathapar (unpublished) also compiled bulk density data for a Thulabin sand, table 8.6.

Aggregate densities at 10 kPa moisture suctions of two sands over clay soils, Cobram

sandy loam and Danberry loamy sand have been determined by Loveday et al. (1966).

Two replications were taken at each of the three sites, two of Danberry loamy sand and

one of Cobram sandy loam. Variation of bulk and aggregate densities with depth from

results of all the above studies is shown in figure 8.3.

Table 8-6 Bulk and aggregate densities of sands over clay soils


Thulabin 1555 1770 1535 1570 1650 1670 Lovedaysandy 1978loam

Cobram 1390 1740 1750 1770 1690 1590sandy loam

Yandera 1530 1390 1460 1610 1500 1560 Talsmaloam 1963

Thulabin 1250 1440 1360 Prathaparsandy

Danberry {1547} {1535} {1743} {1595} Lovedayloamy 1966sandy (average 2)

Cobram {1565} {1665} {1665} {1715}sandy loam

{ } indicates aggregate density

117

0

0.2

0.4

0.6

0.8

1

1.2

1.4

1.6

1000 1200 1400 1600 1800 2000

Bulk density (kg/m3)

Dep

th (

m)

Hor ticulturals oil

Aggregatedens ities

B ulkdens ities

Figure 8-3 Variation of Bulk and aggregate densities with depth of sands over clay

soils

8.1.1.3 Porosity

Total porosity measurements as calculated from the amount of water held at saturation for

a Yandera loam has been undertaken by Talsma (1963). Total porosity was measured on

four replicates at depths of 0.15, 0.35, 0.61, 0.915, 1.22 and 1.525 m and average porosity

for the respective depths were found to be 0.389, 0.475, 0.449, 0.392, 0.433 and 0.412

m3/m3.

Loveday et al. (1966) also undertook total porosity and air filled porosity determinations

of two sands over clay soils, Danberry loamy sand and Cobram sandy loam, located in

the CIA. Porosity was measured in 0.0372 m diameter cores taken from depths between

0-0.1 m after the site had been irrigated. Porosity was then measured at intervals of 24

and 48 hours. Average total porosity was found to be 0.49 and 0.48 m3/m3 at 24 and 48

hours after irrigation and average air filled porosity was found to be 0.3 and 0.31 m3/m3

at 24 and 48 hours after irrigation.

118

8.1.2 Water movement

8.1.2.1 Infiltration

Studies on infiltration of sands over clay soils have been undertaken by van der Lelij and

Talsma (1977) at seven sites consisting of Cobram and Thulabin sandy loams. Infiltration

over a sixteen week period during ponding of the soil was measured with large buffered

ring infiltrometers. Mean infiltration is shown in figure 8.4, mean infiltration rate at the

end of ponding was calculated to be 2.9 mm/day.

Figure 8-4 Mean cumulative infiltration during ponding of Thulabin and Cobram

sandy loams. From van der Lelij and Talsma (1977)

119


Laboratory determinations

Laboratory determinations of hydraulic conductivity have been undertaken by Loveday et

al. (1978) for two sands over clay soils, Thulabin and Cobram sandy loams, located in the

MIA. Saturated hydraulic conductivity was measured on ground soil from 0-0.2 m

depths, which had been packed in cores of 0.046 m diameter. Saturated hydraulic

conductivity was measured at 24 and 48 hour periods for the two sites and for the

Thulabin sandy loam hydraulic conductivity was found to be 230.4 mm/day and 242.9

mm/day for 24 and 48 hour periods respectively. Hydraulic conductivity for the Cobram

sandy loam varied from 5.52 mm/day at a 24 hour period to 3.6 mm/day for a 48 hour

period.


Field determination of hydraulic conductivity of sands over clay soils have been

undertaken by van der Lelij and Talsma (1977) on Cobram and Thulabin sandy loams

located in the MIA and CIA. Hydraulic conductivity, between a period of 10-110 days

during ponding on one site, was estimated from measurements of infiltration and

hydraulic gradient, table 8.7.

Table 8-7 Potential gradient and hydraulic conductivity of a sands over clay soil

during ponding

Pond ingperiod Inf iltration v Gradient Hydraulic Gradient Hydraulic Potent ial

conduct iv ity conduct iv ity(days) (mm/da y) (mm/da y) (mm/da y) (cm H2O)

10-110 13.3 1.3 10.2 1 13.3 -25

Subso il (0.5-0.7m)Topso il (0-0.5m)

120

Talsma (1963) also undertook determinations of hydraulic conductivity of a sands over

clay soil, Yandera loam by the auger hole method and calculated at depth intervals of 0.5-

2, 1-2, 1.5-2 and 2-2.5 m. Average hydraulic conductivity was found to be 820, 610, 410

and 220 mm/day for the respective depth intervals.

van der Lelij (1974) also compiled hydraulic conductivity measurements sands over clay

soils by the auger hole method. Hydraulic conductivity measurements of Hyandra sandy

loam and Yambil sandy loam were compiled from a total of 146 and 169 sites

respectively in the Mirrool irrigation area. Average hydraulic conductivity’s for the soils

are listed in table 8.8 and have been further divided based on watertable depth with

normal watertables (Nor. WT) being between 0.75 and 1.05 m below the surface, low

watertables (Deep WT) deeper than 1.05 m and high watertables (High WT) within 0.75

m of the surface.

Table 8-8 Mean Hydraulic conductivities (mm/day) of sands over clay soils in the

Mirrool irrigation area, van der Lelij (1974).

Soil Average hydraulic conduct ivityType Mean hydraulic Mean hydraulic Mean hydraulic

conductivity Conductivity conductivity 0.5-0.9 m 0.9-1.4 m 1.4-1.9 m(Nor. WT) (High WT) (Deep WT)

Yambil 158 274 76 564 241 76sandy loam

Hyandra 226 274 125 396 326 125sandy loam


Determinations of available water for sands over clay soils have been carried out by

Loveday et al. (1966) for two Danberry loamy sands and a Cobram sandy loam located in

121

the CIA. Available water was calculated from moisture contents determined at 10 kPa

and 1500 kPa and aggregate densities. Two replicates were undertaken at each site and

average available water for a 0-0.3 m depth for the two Danberry loamy sands was found

to be 0.0315 m and for the Cobram sandy loam 0.0405 m.

Determined water contents at 1500 kPa suctions, on two Danberry loamy sands and a

Cobram sandy loam located in the CIA, table 8.9. Loveday et al. (1978) detailed 1500

kPa moisture contents for a Thulabin sandy loam and Cobram sandy loam located in the

MIA, table 8.9. Talsma (1963) conducted 1500 kPa moisture contents of a Yandera loam

located in the MIA, table 8.9. Variations of 1500 kPa moisture content with depth from

the above mentioned studies is shown in figure 8.5. The statistical data compiled from all

studies is shown in table 8.10.

Table 8-9 Volumetric water contents at 1500 kPa for sands over clay


Danberry 0.072 0.068 0.256 Lovedayloamy 1966sand (average 2)

Cobram 0.095 0.103 0.222sandy loam

Thulabin 0.076 0.207 0.296 0.275 0.288 Lovedaysandy loam 1978

Cobram 0.186 0.233 0.244 0.255 0.24sandy loam

Yandera 0.15 0.207 0.184 0.177 0.187 0.15 Talsmaloam 1963

122

0

0.2

0.4

0.6

0.8

1

1.2

1.4

0 0.1 0.2 0.3 0.4

M o is tu re C on te n t (m 3/m 3)D

epth

(m

)

Horticulturalsoil

Figure 8-5 Variation of moisture contents at 1500 kPa for sands over clay

Table 8-10 Analysis of moisture contents at 1500 kPa for sands over clay

Depth (m)

Average value

Lowest value

Highest value

Standard deviation

Coeff icientof v ariation


0.025 0.080 0.069 0.097 0.012 15 0.074 0.079 60.1 0.090 0.062 0.186 0.040 44 0.075 0.085 90.2 0.150 0.150 0.150 10.3 0.235 0.182 0.295 0.030 13 0.233 0.233 90.4 0.261 0.207 0.329 0.051 20 0.253 0.257 40.6 0.247 0.184 0.303 0.049 20 0.251 0.243 40.8 0.272 0.240 0.304 0.032 12 0.272 0.271 30.9 0.177 11.2 0.187 11.5 0.150 1

123

Loveday et al. (1966) for two Danberry loamy sands and a Cobram sandy loam located in

the CIA detailed moisture contents at 10 kPa suctions, table 8.11.

Talsma (1963) for a Yandera loam located in the MIA, detailed moisture contents at a 10

kPa suction, table 8.11. Variation of moisture contents at 10 kPa suctions from the above

studies is shown in figure 8.6. Statistical data relating to all studies is shown in table 8.12.

Table 8-11 Volumetric water contents at 10 kPa


Danberry 0.176 0.171 0.343 Lovedayloamy 1966sand (average 2)


Yandera 0.301 0.338 0.364 0.325 0.358 0.334 Talsma loam 1963

0

0.2

0.4

0.6

0.8

1

1.2

1.4

0 0.1 0.2 0.3 0.4 0.5

Moisture Content (m3/m3)

De

pth

(m

)

Horticulturalsoil

Figure 8-6 Variation of moisture contents at 10 kPa

124

Table 8-12 Analysis of moisture contents at 10 kPa

Depth (m)

Average value

Lowest value

Highest value

Standard deviation



0.025 0.18 0.13 0.23 0.03 18 0.18 0.18 70.1 0.19 0.16 0.25 0.03 16 0.18 0.18 70.2 0.30 10.3 0.36 0.33 0.40 0.03 7 0.35 0.36 70.4 0.34 10.6 0.36 10.9 0.33 11.2 0.36 11.5 0.33 1


Electrical conductivity measurements of sands over clay soils have been undertaken by

Loveday et al. (1978) for Cobram and Thulabin sandy loams located in the MIA. Two

replications were undertaken at each site and mean electrical conductivity of a 1:5 water

suspension to a 0.8 m depth is shown in table 8.13.

Table 8-13 Electrical conductivity of sands over clay soils (mS/cm)

Soil Depth (m) AuthorType 0.1 0.2 0.3 0.4 0.6 0.8

Thulabin 0.135 0.03 0.045 0.06 0.09 0.225 Lovedaysandy loam 1978

Cobram 0.105 0.09 0.075 0.135 0.39 0.73sandy loam

125

Exchangeable sodium percent (ESP) of sands over clay soils have been calculated from

measurements made of exchangeable cations made by Loveday et al. (1966) for two

Danberry loamy sands and a Cobram sandy loam located in the CIA and Loveday et al.

(1978) for a Thulabin sandy loam and Cobram sandy loam located in the MIA, table 8.14.

Variation of ESP with depth for all of the above mentioned studies is shown in figure 8.7.

Table 8-14 ESP of sands over clay soils

Soil Depth (m) AuthorType 0.025 0.1 0.3

Danberry 0.42 0.2 Lovedayloamy 1966sand (average 2)


Thulabin 2.31 Lovedaysandy loam 1978

Cobram 5.2 16.02sandy loam

0

0.05

0.1

0.15

0.2

0.25

0.3

0.35

0 5 10 15 20 25ESP

Dep

th (

m)

Figure 8-7 Variation of ESP with depth for sands over clay soils

126

9 DEEP SANDY SOILS



Particle size analysis on a deep sandy soil, Banna sand, has been undertaken by Talsma

(1963) at depths of 0.15, 0.305, 0.61, 0.915, 1.22 and 1.525 m. Four replicates were taken

at each depth and the average sand percentage was found to be 81.6, 82.6, 50.9, 45.3,

51.3 and 44.5 % for the respective depths. Average silt percent was found to be 4.5, 3.1,

10.3, 11.5, 8.8 and 7.8 % for the respective depths and average clay content was found to

be 13.9, 13.3, 38.8, 43.2, 39.9 and 47.7 %.


Determinations of bulk density for a Banna sand has been undertaken at depths of 0.15,

0.305, 0.61, 0.915, 1.22 and 1.525 m by Talsma (1963). Bulk densities for the respective

depths were found to be 1530, 1530, 1420, 1410, 1470 and 1490 kg/m3.

9.1.1.3 Porosity

Porosity determinations of a Banna sand have been undertaken by Talsma (1963) at

depths of 0.15, 0.305, 0.61, 0.905, 1.22 and 1.525 m. Total porosity was estimated from

saturation measurements taken on soil samples form the above mentioned depths. Total

porosity was found to be 0.389, 0.475, 0.449, 0.392, 0.433 and 0.412 m3/m3 for the

respective depths.

127

9.1.2 Water movement



Hydraulic conductivity of a Banna sand has been determied by van der Lelij (1974).

Hydraulic conductivity was measured by the auger hole method from 181 sites in the

Mirrool irrigation area, table 9.1 and have been further divided based on the watertable

depth with normal watertables being between 0.75 and 1.05 m below the surface, low

watertables deeper than 1.05 m and high watertables within 0.75 m of the surface.

Table 9-1 Hydraulic conductivity (mm/day) of a deep sandy soil

Soil Average hydraulic conductivityType Mean hydraulic Mean hydraulic Mean hydraulic

conductivity Conductivity conductivity 0.5-0.9 m 0.9-1.4 m 1.4-1.9 m(Nor. WT) (High WT) (Deep WT)

Banna 286 408 113 713 460 113sand

Talsma (1963) also conducted hydraulic conductivity determination using the auger hole

method on a Banna sand located in the MIA. Hydraulic conductivity at a depth interval of

1.3-1.8 m was found to be 268 mm/day.

128

9.1.3 Water retention/Moisture characteristic

Talsma (1963) has undertaken determinations of available water for a Banna sand.

Available water was calculated from 10 and 1500 kPa moisture content determinations

undertaken on the Banna sand. The available water to a 1.6 m depth was found to be

0.207 m.

Permanent wilting points were estimated from 1500 kPa moisture content determinations

at depths of 0.15, .0305, 0.61, 0.905, 1.22 and 1.525 m. Moisture contents were found to

be 0.058, 0.067, 0.249, 0.261, 0.282 and 0.280 m3/m3.

Field capacity of the soil was also estimated from 10 kPa moisture content determinations

and found to be 0.294, 0.257, 0.354, 0.359, 0.358 and 0.364 m3/m3 for the respective

depths. Figure 9.1 shows the permanent wilting point and field capacity moisture content

profiles as found by Talsma (1963).

Figure 9-1 Volumetric moisture content profiles of a Banna sand at 1500 and 10 kPa

0

0.2

0.4

0.6

0.8

1

1.2

1.4

1.6

0.15 0.2 0.25 0.3 0.35 0.4

M oisture Content

Dep

th (

m)

1500 kPa 10 kPa

129

10 TYPICAL SOIL PROPERTIES FOR SOIL GROUPS

This section summarises soil properties of the major soil groups. These properties are:

particle size, bulk density, porosity, electrical conductivity, exchangeable sodium, and

moisture content.

10.1 Clays

10.1.1 Self mulching clays

Physical property data relating to self mulching clays was well represented in the

papers collected for the review.

Particle size analysis

Particle size distributions for self mulching clays indicated a uniform particle

distribution to 0.3 m with average coarse sand, fine sand, silt and clay being

comparable at 0-0.1 and 0.2-0.3 m depths with an average of 61 % clay in the 0-0.1 m

layer and 65 % in the 0.2-0.3 m layer. Average particle size distributions for the 0-0.1

m layer are shown in figure 10.1 for the 0-0.1 m layer and in figure 1.2 for the 0.2-0.3

m layer. Particle size distributions were not well documented below 0.3 m, however

studies which were found did show particle size distributions to be relatively constant

to 1.8 m with a clay content of around 50-60 %.

Bulk density

Bulk density data for self mulching clays was particularly varied in the 0-0.1 m layer

between 1130-1400 kg/m3 . Reasons for the large variation are due to soil tillage,

which can radically change bulk densities or variations in soil moisture content. At

depths below 0.1 m bulk densities were less varied and typical values, shown in table

10.1.

130

Infiltration

Infiltration measurements on self-mulching clays were few. Studies by van der Lelij

and Talsma (1977) indicated that infiltration rates during prolonged ponding were

between 1.4 and 3.7 mm/day, however it was also noted that infiltration rates over

most of the ponding period fluctuated considerably. Comparisons of cumulative

infiltration with other soil groups as measured by van der Lelij and Talsma (1977) is


Hydraulic conductivity

Hydraulic conductivities of self-mulching clays were varied as were the methods used

to measure hydraulic conductivity. Laboratory measurements on ground soil from 0-

0.2 m depths in repacked cores had saturated hydraulic conductivities between 24-49

mm/day after 48 hours with an average of 37mm/day.

Field estimates of unsaturated hydraulic conductivity taken by van der Lelij and

Talsma (1977) indicated a hydraulic conductivity at a depth interval between 0-0.5 m

to be 20.8 mm/day which is comparable to measurements made on repacked soil

cores.

Hydraulic conductivity at depth was very much lower, at depths of 1.5-2 m saturated

hydraulic conductivities as found by van der Lelij and Talsma were between 0.7-1.1

mm/day and indicated that hydraulic conductivities of self mulching soils tended by

decrease with depth.

Moisture characteristics

1500 kPa moisture contents for self-mulching clay soils did vary however ranges of

1500 kPa moisture content with depth were reasonably consistent. Typical values of

1500 kPa moisture contents are shown in table 10.1. 10 kPa moisture contents were

also relatively constant with depth again increasing slightly down the profile; typical

results are shown in table 10.1. From the results it also indicates that average moisture

contents between 10 kPa and 1500 kPa are reasonably representative of the self

mulching clay group and indeed gave a representation of moisture characteristics of

self mulching clays to a depth of 0.3 m. Average available water for the top 0.3 m

131

calculated from average 10 and 1500 kPa moisture contents are shown in figure 10.4

at the end of this section. It was also interesting to note that both particle size analysis,

10 and 1500 kPa moisture contents were fairly constant with profile depth.

Electrical conductivity

Electrical conductivity of self mulching clays increased with depth from an average of

0.167 mS/cm at 0.1 m to 0.724 mS/cm at 0.8 m. Loveday et al. (1984) stated

moderate salinity occurred at EC1:5 > 0.6 mS/cm and high salinity EC1:5 > 1.2 mS/cm,

hence findings from the data collected indicated that self mulching clay profiles

tended to be saline or moderately saline at depths to 0.8.

Exchangeable sodium percentages

Exchangeable sodium percentages for self-mulching clays were mostly calculated

from measurements of exchangeable cations measured by Loveday.

Loveday (1974) indicated that soils can be thought of as sodic at ESP > 5-6. From the

data collected average ESP ranged from 0.37 % in the 0.025 m layer to 4.1 % in the

0.2-0.3 m layer and indicated that self mulching clays are not particularly sodic at

least to a depth of 0.3 m.

132

Table 10-1 Typical values of properties of self mulching clays

Depth (m) CS % FS % Si % C % Bulk Density (kg/m3)

1500kPa(m3/m3)

10 kPa(m3/m3)

EC 1:5(mS/cm)

ESP

0-0.025 7 20 11 64 0.251 0.3630.025-0.1 7 21 11 61 1268 0.256 0.382 0.167 0.370.1-0.2 7 21 9 60 1427 0.33* 0.205 1.980.2-0.3 6 19 10 65 1435 0.283 0.402 0.251 4.10.3-0.4 9* 22* 14* 55* 1490 0.301 0.4* 0.3820.4-0.6 6 19 11 63 1534 0.315 0.5820.6-0.8 7* 22* 15* 56* 1537 0.325 0.7240.8-1 9* 27* 9* 51*1-1.5 4* 26* 9* 57*1.5-2.5 5* 26* 7* 54*2.5-3 1850*

* Indicates limited data

10.1.2 Hard setting clays

Data relating to physical properties of hard setting clays was limited.

Particle size distribution

Particle size distribution was relatively constant with depth at least until 0.3 m,

however the upper 0-0.1 m had slightly lower clay contents. Average values of

particle size distribution are show in figure 10.1 for the 0-0.1 m layer and figure 10.2

for the 0.2-0.3 m layer.

Bulk density

Bulk densities were not well represented and values were distributed over a wide

range typical bulk densities are shown in table 10.2, however in most cases only three

samples at each depth were taken.

Porosity

Only one determination on a hard setting clay was found and is shown in table 10.2.

133


Hydraulic conductivities were only measured on repacked soil cores and

measurements taken are comparable indicating a hydraulic conductivity around 4

mm/day for cores packed from soil at profile depth between 0-0.2 m, however the

sample size was limited to three studies.


Moisture characteristics were not well documented and only one 1500 kPa moisture

content profile determination could be found. This is presented in table 10.2.


From the limited information collected hard setting clays tended to become

moderately to highly saline with depth with an EC of 0.19 mS/cm at 0-0.025 m to

2.05 mS/cm at 0.8 m.

Exchangeable sodium percentage

Hard setting clays appeared to be prone to being sodic, however only limited data was

collected.

Table 10-2 Typical values of properties of hard setting clays


Porosity(m3/m3)

1500kPa(m3/m3)

10kPa(m3/m3)

EC 1:5(mS/cm)

ESP

0-0.0250.05-0.1 6 24 15 55 1338 0.258* 0.190.1-0.2 1270* 0.343* 0.2540.2-0.3 3 20 11 66 1491 0.301* 0.260.3-0.4 1495 0.32* 0.255*0.4-0.6 1543 0.349* 2.050.6-0.8 1480* 0.295*


134

10.2 Transitional red brown earths

Data relating to soil physical properties of transitional red brown earths was well

represented in the papers collected for this review.


Particle size distributions for transitional red brown earths had a marked texture

contrast between 0-0.1 m and 0.2-0.3 m depths with mean clay contents at 0-0.1 m

depths being 36 % while at a 0.2-0.3 m depth 67 %, which was higher on average than

self mulching clays. Also high clay contents were particularly evident at depths below

0.3 m in the transitional red brown earths, which occurred in the CIA. From the two

studies conducted in the CIA, clay contents were in most cases above 70 %, Sleeman

and Stannard (1983) recorded clay contents as high as 83 % at 0.6 m depth on a

Willbriggie clay loam in the CIA. Clay contents in the MIA were all on average

below 70 % at depths greater than 0.3 m apart from one determination on Willbriggie

clay, which had a clay content of 71 % at a 0.3 m depth. Average particle size

distributions are shown in figure 10.1 for 0-0.1 m and in figure 10.2 for 0.2-0.3 m.

Bulk density

Bulk density data for transitional red brown earths varied considerably and

particularly in the 0-0.1 m layer, which varied between 1180-1620 kg/m3. The large

difference in bulk densities may be due to variations in moisture contents during

sampling as moisture contents were rarely given with measured bulk densities, or due

to soil tillage conditions.

Porosity

Porosity determinations on transitional red brown earths showed total porosity to be

between 0.45-0.5 m3/m3 in the 0-0.1 m layer decreasing steadily with depth to 0.35-

0.4 m3/m3 at a 1-1.5 m depth, typical values are shown in table 10.3.

135

Infiltration

Infiltration measurements on transitional red brown earths have been mostly carried

out by ponding of the soil for prolonged periods of time. From the limited information

available it is difficult to draw conclusions, however it does appear that infiltration

during ponding on transitional red brown earths is very low when compared to other

soil groups, infiltration rates could be around 0.25 mm/day as measured by van der

Lelij and Talsma (1977) over a 16 week ponding period comparisons of cumulative

infiltration over a 16 week ponding period with other soil groups is shown in figure

10.2.


Measurements of hydraulic conductivity in transitional red brown earths were

extremely varied, however it was apparent that between a depth of 0.2-0.6 m the

hydraulic conductivity was lowest and increased around 0.6 m. This has been shown

in studies undertaken by McIntyre et al. (1982), van der Lelij and Talsma (1977) and

Sides (1993). Hydraulic conductivities in the 0.2-0.6 m depth range varied from 0.026

to 10 mm/day, with lower values more common.

Moisture characteristic

1500 kPa moisture contents of transitional red brown earths were found to vary

considerably particularly in the 0.1 m layer and would be due to tillage affecting the

porosity. There was a marked change in 1500 kPa moisture contents between the

upper 0.2 m and the lower profile 0.3-0.8 m. This may be due to the higher clay

content which appears in the profile at around 0.2-0.3 m depths and causes the marked

contrast between the surface soil and the lower soil profile. Typical values are shown

in table 10.3. 10 kPa moisture content determinations on transitional red brown earths

were not well documented. From the data collected a change in 10 kPa moisture

content occurred at around a 0.2-0.3 m depth similar in shape to the 1500 kPa

moisture content curve. Typical values are shown in table 10.4 and average available

water for the top 0.3 m of soil calculated from average 10 and 1500 kPa moisture

contents is shown in figure 10.3.

136


Electrical conductivity of transitional red brown earths tended to be low in the upper

0.6 m, however becoming moderate to highly saline with depth, with high EC

occurring below 1 m depths. Typical values are shown in table 10.3.

10.2.1 Exchangeable sodium percentage

Exchangeable sodium percentages tended to indicate higher sodicity with ESP in the

0.3 m layer being on average 7.3 indicating sodic soils. ESP was not well documented

below 0.3 m.

Table 10-3 Typical values of properties of transitional red brown earths


Porosity (m3/m3)

1500kPa(m3/m3)

10 kPa(m3/m3)

EC 1:5(mS/cm)

ESP

0-0.025 17 36 18 30 1545* 0.128 0.285 2.30.05-0.1 14 36 16 36 1369 0.49 0.188 0.271 0.118 30.1-0.2 9 25 12 55 1480 0.0960.2-0.3 6 20 7 67 1444 0.46* 0.314 0.444 0.15 7.30.3-0.4 9 24 12 56 1495 0.31 0.377* 0.2230.4-0.6 7 21 12 60 1528 0.43* 0.315 0.407 0.378 18.8*0.6-0.8 12 24 14 49 1541 0.42* 0.306 0.6360.8-1 11 25 14 49 1599 0.4* 0.244* 0.355* 1.1781-1.5 4* 20* 11* 57* 1600 0.39* 0.21* 0.35* 2.12*1.5-2.5 9* 18* 9* 70* 1710* 0.38* 1.5*2.5-3 12* 14* 8* 67* 1860* 0.34* 1.2*


137

10.3 Red brown earths

10.3.1 Soils of the upper hillslopes

Little information was available on soils of the upper hillslopes and from the limited

data no trends could be concluded apart from one particle size distribution measured

in the 0.8-0.9 m layer and hydraulic conductivity’s measured by van der Lelij (1974)

which are shown in the results section.

10.3.2 Soils of the lower hillslopes

Information relating to soils of the hillslopes was limited and mostly came from

unpublished data collected during the review.


Particle size distributions tended to vary with depth with silt and fine sand fractions

increasing with depth, while coarse sand and clay fractions in general decreased with

depth. It did appear however that the clay contents tended to peak around a 0.3-0.6 m

depth before then decreasing with depth. Average particle size distributions are shown

in figure 10.1 for the 0-0.1 m layer and figure 10.2 for the 0.2-0.3 m layer.

Bulk density

Bulk density data for soils of the lower hillslopes was not well documented and from

the three studies undertaken variation was great typical values, which may be

expected, are shown in table 10.4.


Hydraulic conductivity measured by the auger hole method were well documented by

van der Lelij (1974), however during statistical investigations of hydraulic

138

conductivity by van der Lelij it was concluded that mean hydraulic conductivities

measured by the auger hole method on the same soil types were significantly different

in some cases from each other, hence hydraulic conductivities within this soil group

vary considerably from 58 mm/day to 1039 mm/day. For a more detailed discussion

see van der Lelij (1974).


Moisture characteristics of soils of the lower hillslopes have only been documented in

two studies by Meyer (1992) and Talsma (1963) the shape of the two profiles are very

similar and variations of moisture contents at 10 and 1500 kPa with depth show

similar patterns, however the amount of available water at depths greater than 0.8 m

are very different. Typical values of 10 and 1500 kPa moisture contents are shown in

table 10.4. No information relating to soil salinity or sodicity of subplastic soils of the

hillslopes was found.

Table 10-4 Typical values of properties of soils of the lower hill slopes


Porosity (m3/m3)

1500 kPa(m3/m3)

10 kPa(m3/m3)

0-0.0250.025-0.1 13 51 11 27 15170.1-0.2 13 49 11 28 1560* 0.532* 0.094 0.2660.2-0.3 11 49 10 31 14370.3-0.4 9 45 11 36 1380* 0.42* 0.279 0.350.4-0.6 7 38 19 35 1437 0.454* 0.283 0.4060.6-0.8 6 43 20 31 1470*0.8-1 5 48 17 28 1470 0.408* 0.262 0.331-1.5 4* 43* 22* 25* 1575 0.346* 0.211 0.305


10.3.3 Soils of the plains (subplastic subsoil group)

Little information was available on plastic soils of the plains with lighter subsoil apart

from hydraulic conductivity measurements measured by the auger hole method

139

reported by van der Lelij (1974). Hydraulic conductivities were found to vary between

104-396 mm/day.

Table 10-5 Typical values of properties of subplastic soil of the hillslopes

Depth

(m)

CS

%

FS

%

Si

%

C% Bulk

Density

(kg/m3)

Porosity

(m3/m3)

EC 1:5

(mS/m)

ESP

0-0.025

0.025-0.1 6 48 11 32 1360 0.54 0.12 1.6

0.1-0.2 6 47 12 35 0.09 2.5

0.2-0.3 5 41 5 48 0.14 3.7

0.3-0.4 3 38 8 53

0.4-0.6 3 38 8 53 0.3 5.9

0.6-0.8

0.8-1 0.09

1-1.5

1.5-2.5

(This table is based on limited data)

10.3.4 Plastic soils of the plains ( normal subsoil group)

Particle size distribution

Particle size distributions for plastic plains soils indicated a marked texture contrast

between the 0-0.1 and 0.2-0.3 m soil profile layer with an average clay content of 15

% in the 0-0.1 m layer and 57 % in the 0.2-0.3 m layer. Clay contents appeared from

the limited data available to remain relatively constant with depth however only

limited data at a depth below 0.3 m was found. Average particle size distributions are

shown in figure 10.1 for a 0-0.1 m depth and figure 10.2 for a 0.2-0.3 m depth.

140

Bulk densities

Bulk densities were also varied and from the limited amount of data available

indicated that ranges of bulk densities did remain relatively constant with depth.

Typical values are shown in table 10.6.

Infiltration

Infiltration measurements on normal soils of the plains were not well documented and

only one study of infiltration during prolonged ponding was found. This study was

undertaken by van der Lelij and Talsma (1977) and found the infiltration rate at the

end of a 16 week ponding period to be 0.43 mm/day which is low in comparison to

some soil groups. Comparisons between cumulative infiltration over a 16 week

ponding period are shown in figure 10.3.


Determinations of hydraulic conductivity were extremely varied and depended largely

on the method used. It was also evident that the horticultural soils of this group had a

greater hydraulic conductivity than non horticultural soils of this group, with

horticultural soils having hydraulic conductivities between 64-328 mm/day as

measured by the auger hole method while non horticultural soil had hydraulic

conductivity’s between 0.11-0.89 mm/day measured during ponding.


1500 kPa moisture contents varied with depth and this is due possibly to the textural

change of the soils. It was evident that the horticultural soil of this group, Camarooka

clay loam had a higher moisture content at 1500 kPa than the non horticultural soils in

the upper soil profile, however only one measurement of 1500 kPa moisture content

of a horticultural plastic plain soil was found. Typical values are shown in table 10.6.

Moisture contents at 10 kPa were limited. 10 kPa moisture contents did show a

marked variation with depth and increased rather dramatically after a 0.2 m depth. It

was also apparent that the horticultural soil, Camarooka clay loam, had a much greater

141

moisture content at 10 kPa compared to the non horticultural soils. Typical values are

shown in table 10.6 and average available water has also been calculated to a 0.3 m

depth and is shown in figure 10.4.


Electrical conductivity measurements of normal soils of the plains were not well

documented. From the data collected it did not appear that plastic soils of the plains

were saline at least until a 0.8 m depth.


Exchangeable sodium percentages increased with depth and sodicity was evident a 0.3

m depth with an ESP of 7.3 %.

Table 10-6 Typical values of normal soils of the plains


Porosity (m3/m3)

1500kPa(m3/m3)

10 kPa(m3/m3)

EC 1:5(mS/cm)

ESP

0-0.025 16* 54* 17* 13* 1589 0.078 0.2 1.20.025-0.1 22 48 16 15 1680 0.104 0.23 0.14 2.20.1-0.2 10 39 1510 0.454* 0.119 0.21 0.06 7.3*0.2-0.3 11 25 7 57 1435 0.263 0.38 0.060.3-0.4 1593 0.285 0.39* 0.090.4-0.6 9* 47* 1530 0.493* 0.282 0.37* 0.170.6-0.8 8* 49* 1560* 0.429* 0.258 0.36* 0.230.8-1 9* 20* 10* 61* 0.419* 0.287*1-1.5 6* 49* 1620* 0.389* 0.27* 0.35*1.5-2.5 0.288*

51

44*43*

45*

∗ Indicates limited data

142

10.4 Sands over clay


Sands over clay soils were found to have a marked texture contrast between 0-0.1 and

0.2-0.3 m depths with average clay contents in the 0-0.1 m layer being 12 % while in

the 0.2-0.3 m layer 45 %. Particle size distribution at depths below 0.3 m were few,

however it appears from the limited data that sand fractions increased after 0.4-0.5 m

becoming sandier with depth, however only three studies on particle size distributions

below 0.3 m depth were found. Average particle size distribution is shown in figure

10.1 for a 0-0.1 m depth and figure 10.2 for a 0.2-0.3 m depth.

Bulk density

Bulk density data for sands over clay soils was limited, however it did appear from

the limited data that at a depth range between 0.1-0.3 m bulk densities increased

slightly before decreasing after this depth range. This may be due to the presence of a

cemented layer in some soil types in this group. It was also apparent that the bulk

density of the horticultural soil Yandera loam was lower than non horticultural

solodized solonetz soils and this can be seen graphically in the results section.

Infiltration

Infiltration measurements on sands over clay soils were not well documented. It did

appear from the studies undertaken on infiltration during ponding that infiltration on

soil types of this group were high, cumulative infiltration in comparison to other soil

groups can be seen in figure 10.3.


There was also a large variation in hydraulic conductivity measurements of soils of

this group with two distinct ranges. These were the horticultural soils of the group

which had high hydraulic conductivities (>100 mm/day) measured by the auger hole

143

method and the non horticultural soils of the group which had a lower hydraulic

conductivity range (<15 mm/day) estimated from infiltration and potential

measurements during prolonged ponding.


Moisture contents at 1500 kPa for sands over clay soils varied particularly in the

lower soil profile. It was also apparent that the horticultural soil, Yandera loam, had a

lower moisture content at 1500 kPa compared to the non horticultural soils, this can

be seen graphically in the results section.

Moisture contents at 10 kPa were not well documented and only to 0.3 m depth apart

from one study. 10 kPa moisture contents increased rapidly with depth between 0.1 to

0.3 m and this may be due to the texture contrast between these depths. Average

available water has been calculated for the upper 0.3 m soil profile from average 10

and 1500 kPa moisture contents and is shown in figure 10.4.

Electrical conductivities

Electrical conductivity measurements for sands over clay soils indicated that profiles

are not saline at least until a 0.8 m depth. Typical values are shown in table 10.7.


Exchangeable sodium percentages were also moderate to a 0.3 m depth, however there

was some rather high ESP measurements in this group. Typical values are shown in

table 10.6.

144

Table 10-7 Typical values of properties of solodized solonetz soils

Depth (m) CS % FS % Si % C % Bulk Density(kg/m3)

Porosity(m3/m3)

1500kPa(m3/m3)

10 kPa(m3/m3)

EC(mS/cm)

1:5 ESP

0-0.025 43 30 16 13 0.08 0.18 0.390.025-0.1 43 30 14 12 1398 0.09 0.19 0.12 2.70.1-0.2 23* 39* 11* 27* 1680 0.389* 0.15 0.3 0.06 5.50.2-0.3 26 20 9 45 1575 0.235 0.36 0.060.3-0.4 9* 15* 10* 67* 1577 0.475* 0.261 0.34* 0.010.4-0.6 16* 21* 12* 52* 1540 0.449* 0.247 0.36* 0.240.6-0.8 23* 27* 11* 39* 1630 0.272 0.34* 0.480.8-1 28* 37* 11* 25* 1610* 0.392* 0.177* 0.33*1-1.5 12* 27* 1560* 0.412* 0.15*61*


10.5Deep sands

Soil physical property data for deep sands were not well documented in the papers

collected for the review apart from one study undertaken by Talsma (1963) on a

Banna sand hence it is difficult to associate trends to this soil group. Typical values

are shown in table 10.8.

Table 10-8 Typical values of properties of Deep sands

Depth (m) CS% FS % Si % C % Bulk Density (kg/m3)

Porosity(m3/m3)

1500 kPa(m3/m3)

10 kPa(m3/m3)

0-0.0250.025-0.1 5* 13* 1530* 0.389* 0.058* 0.294*0.1-0.20.2-0.30.3-0.4 4* 13* 1530* 0.475* 0.067* 0.257*0.4-0.6 10* 39* 1420* 0.449* 0.249* 0.354*0.6-0.80.8-1 12* 43* 1410* 0.392* 0.261* 0.359*1-1.5 8* 47* 1490* 0.412* 0.28* 0.364*45*

82*

83*51*

45*


145

0

10

20

30

40

50

60

70

Solodized solonetz soils Hard setting clays Subplastic hillslopesoils

Plastic soi ls of the plain Self mulching clays Transitional soils

Soil groups

%

Coarse sand

Fine sand

Silt

Clay

Figure 10-1 Average particle size distribution, 0.01 m.

0

10

20

30

40

50

60

70

80

Solodized solonetz soils Hard setting clays Subplastic hillslopesoils

Plastic soi ls of the plain Self mulching clays Transitional soils

Soil groups

%

Coarse sand

Fine sand

Silt

Clay

Figure 10-2 Average particle size distribution, 0.2 – 0.3 m.

146

Figure 10-3 Cumulative infiltration over a sixteen-week period, 1: Solidized

solonetz soils, 2: Self mulching clay soils, 3: Plastic soils of the plains,

4: Transitional soils. Insert, scale for Solodised solonetz soils. (van der Lely

and Talsma 1977)

0

5

10

15

20

25

30

35

40

45

50

Solodized solonetz soils Subplastic hillslope soils Plastic soils of the plains Self mulching clays Transitional soils

Soil groups

Ava

ilabl

e w

ater

(m

m)

in to

p 0.

3 m

of s

oil

Figure 10-4 Available water (mm) in the top 0.3 m of soil for selected soil groups

147

11 CONCLUSION

This review has brought together most of the available data on soil physical properties

in the MIA and CIA. Much of this data is either unpublished or in CSIRO technical

reports that have not been formally published.

The different soil groups identified have resulted in quite consistent data for each

group and there appears to be good separation in textural properties between groups.

Several soil groups had limited data available, they were: subplastic soils of the upper

hillslopes, plastic soils of the plains (lighter subsoil group), and deep sands.

The typical soil properties that were derived for each soil group represent the values

that may be expected for soils in that group, but are not in any way definitive as there

is variation within any group. These typical values were not derived using statistical

procedures due to the variation in type and quantity of data available.

This report contains little comparison between soil groups and no assessment of soil

capability or property correlations that would be useful. It is hoped that this aspect can

be developed in future.

It is hoped that this document is the first step in building a comprehensive reference of

soil physical attributes of soils in the MIA and CIA. As such, any contributions to

future editions are welcome.

148

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Appendix 1

Appendix 2

Please refer to:

1.

Technical Memorandum 2/1978CSIRO Division of Soils, 1978

DATA RELATING TO SOME IRRIGATED SOILS OF THE M.I.A.,NEW SOUTH WALES, AND CORRELATIONS BETWEEN SOME OFTHEIR PROPERTIES.

By J. Loveday, H.J. Beatty and G.A. Steward

2.

Technical Memorandum 25/66CSIRO Division of Soils, 1966

FIELD AND LABORATORY DATA RELATING TO SOMECOLEAMBALLY SOILS

By J. Loveday, D.S. McIntyre and H.J. Beatty

Appendix 3

These data sheets (60 pages A4) are available in hard copy from theCSIRO Land and Water Library.

physical properties of soils in the murrumbidgee and ... · and coleambally irrigation areas. csiro...

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