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ORZC2

Site ORZC2 Landscape

Sites ORZC1 & ORZC2

A1	0-10 cm	Brown (7.5YR4/4); light clay; moderate to strong, medium to fine polyhedral structure; earthy fabric; very weak consistence (dry); strong effervescence; contains minor amounts of iron sandstone floaters (20 cm in size); also contains worm casts; pH 8.4:	Site ORZC2 Profile
Subsoil
B21	10-20 cm	Brown (7.5YR4/4); light medium clay; weak blocky structure; earthy fabric; firm consistence (dry); pH 8.9:
B22	20-45 cm	Brown (10YR4/3); light medium clay; weak coarse blocky structure; very firm consistence (dry); contains bands of quartz sand; pH 9.0; clear change to:
B23k	45-60 cm	Yellowish brown (10YR5/4) with light brown (7.5YR6/4) and dark greyish brown (10YR4/2) mottles as well as infill of a darker soil; medium clay; strong coarse prismatic structure; strong consistence (dry); contains few (5%) fine earth carbonates as well as pockets of sand; pH 9.3:
B24	60-120 cm	Light yellowish brown (10YR6/4); medium clay; lenticular structure with slickensides; very firm consistence (moist); contains sand grains throughout; pH 9.4:
B25	120+ cm	Light brown (7.5YR6/4) with light brownish grey (10YR6/2) and reddish yellow (5YR6/6) mottles; medium heavy clay; firm consistence (moist); pH 9.3.

• Gradual increase in clay content with depth.
• Vertic properties (i.e. slickensides and lenticular peds) in deeper subsoil.
• Soil profile calcareous throughout.

• Management strategies for all soils should include: increasing organic matter levels in the surface soil, minimising the degradation of soil aggregates and porosity, promoting the development of stable biopores, improving the calcium status of the cation exchange complex (particularly when sodium is a significant part), and breaking up any hardpans. Less frequent tillage, using less aggressive implements and working the soil at optimum moisture content can all assist in maintaining soil aggregation and porosity as well as reducing the breakdown of organic matter.

• Most of the soil profile is strongly to extremely alkaline throughout. This indicates that phosphorus and trace elements such as iron, manganese, copper and zinc may be poorly available to plants.

• The original gilgai microrelief is caused due to the vertic properties of the soil and the resultant shrinking and swelling in response to drying and wetting cycles. This forces ‘blocks’ of soil material gradually upward to form mounds (or ‘puffs’). The soil in the mounds will be different to soils in the depressions. Mound soils tend to be lighter in colour and have higher calcium carbonate contents. Salinity is also often higher in the upper profile in the mounds as well as boron levels. Continuous cultivation results in the smoothing out of many of these gilgai formations. The forces that created them, however, are still operating as is evident by displacement of fence posts; and if the land is left undisturbed over a number of wetting and drying seasons they will continue to develop.

• The surface soil has a high cation exchange capacity with relatively high levels of exchangeable calcium and potassium.

• Tillage of clayey soils like these should be avoided if the soil is wet (i.e. wetter than the plastic limit). At such moisture conditions, excessive tillage, trafficking or over-stocking could result in some structural damage (e.g. compaction). Ideally, tillage should take place on clayey soils when the soil is drier than the plastic limit – down to at least the tillage depth.

• The surface soil has a weak consistence when dry and is reasonably friable. This is well suited as a seed-bed.

• The upper subsoil is sodic but does not disperse. The deeper subsoil becomes strongly sodic and disperses, which is likely to result in restricted root and water movement in the deeper subsoil. The high level of exchangeable sodium in the deeper subsoil can also result in nutrient imbalances and may even have a toxic effect on some plants.

• Boron levels are lower for this depression component of the gilgai microrelief (compared to the nearby gilgai mounds) in the upper part of the subsoil. Boron levels increase below 40 cm depth to levels that are likely to affect the growth of boron-sensitive species (including cereals, pulses, pasture legumes). Concentrations as low as 10 ppm, for example, can reduce lentil yield. Limited data estimates that the threshold level of soluble boron for cereals is 15 mg/kg (Cartwright et al., 1984). Other work at VIDA indicates that where there are low levels of soluble salts, boron tolerance can be comparatively high, with little reduction in wheat yield at levels of up to 45 ppm (Quinlan, 2001).

• The level of soluble salts is low in the upper subsoil. Levels increase to high in the deeper subsoil (i.e. from 40 cm depth) to levels which will restrict the growth of salt-sensitive species. Excessive soil salinity can affect the plant's ability to take up water and can also have a toxic effect on plants.

• The deeper subsoil displays vertic properties (i.e. slickensides and lenticular peds). This indicates that significant shrinking and swelling occurs during wetting and drying cycles. This may disturb the roots of some plant species and has engineering implications (e.g. disturbance to fencelines).

• Surface cracking not evident.

References:

Cartwright, B, Zarcinas, BA, and Mayfield, AH (1984), Toxic concentrations of boron in a red-brown earth at Gladstone, South Australia, Australian Journal of Soil Research 22, 261-72.

Hobson, K (2001), Boron Tolerant Lentils, In On The Pulse pamphlet, NRE.

Quinlan, J (2001), Sorting out the Boron Problem, Wimmera Farming & Landcare Newsletter, 19-20.

Rengasamy, P and Churchman, GJ (1999), Cation Exchange Capacity, Exchangeable Cations and Sodicity, In: Soil Analysis – An Interpretation Manual, (eds. Peverill, KI et al.), CSIRO Publishing.

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