Soil profiles and horizons at Higher Level: The same profile and horizons as SL, with different real cases. At HL you also classify soils by their whole profile and link them to biomes, on their own pages.
The HL cases
- Ukraine's black chernozem.
- Dutch soils built by farmers.
- Australia's ancient soils.
Practise this as you read
- Read a profile from the top down: organic to inorganic.
- Explain each horizon by the processes that made it.
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Layers from the surface to the rock: Dig a pit and look at its wall: the soil is in layers. The whole set of layers is the soil profile; each layer is a horizon.
The points to remember
- A soil profile is the soil seen from the surface down to the rock, as in the wall of a pit.
- It is made of layers called horizons, each with its own colour, texture and make-up.
- Organic at the top: dead leaves and dark humus.
- Inorganic below: paler mineral soil, then broken rock, then solid rock.
- The layers are stable: once formed, they keep their order for a long time.
Read it from the top down: Colour is the clue: dark means humus, pale or orange means mineral soil, stones mean the parent rock is near.
Real example: the chernozem soils of Ukraine formed under grassland. Their dark, humus-rich top layer can be up to about a metre deep, so they are among the most fertile soils on Earth.
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Soil scientists label the horizons with letters, from the top down. Learn them in order: O, A, B, C, R.
The horizons, top to bottom
- O: fallen leaves and other dead matter, rotting on the surface.
- A (topsoil): dark, humus mixed with minerals; most roots and soil life.
- B (subsoil): lighter; minerals and clay washed down from above build up here.
- C: broken, weathered pieces of the parent rock; little organic matter.
- R: the solid parent rock (bedrock) underneath.
- The A horizon matters most for plant growth, and it is the easiest to lose.
Remember it as: O on top, A for the roots, B below, C is broken rock, R is solid rock.
| Horizon | Colour | Organic matter | What happens there |
|---|---|---|---|
| O | Brown to black | Very high | Leaves fall and start to rot |
| A (topsoil) | Dark brown | High | Humus mixes with minerals; most roots |
| B (subsoil) | Lighter, often orange | Low | Minerals and clay washed down collect |
| C | Pale, stony | Very low | Parent rock breaks up |
| R | Rock colour | None | Solid bedrock |
Real example: in the Netherlands, farmers for centuries spread sods mixed with manure on their fields. This built a dark A horizon more than half a metre thick: a horizon made by people.
Made by the soil system itself: The horizons form from interactions inside the soil: dead matter added at the top, water carrying minerals down, animals mixing, rock breaking up at the bottom. It takes hundreds to thousands of years.
How the layers form
- Dead leaves fall and decay at the top: humification makes humus.
- Earthworms and other animals mix humus into the top mineral layer.
- Rainwater soaking down leaches dissolved minerals out of the upper layers.
- Fine clay is washed down too (eluviation) and builds up lower down (illuviation).
- At the base, weathering keeps breaking the parent rock into fragments.
- It is slow: about 1 cm of soil every 100 to 1,000 years, so lost soil is not replaced in a lifetime.
- Humification
- dead matter being broken down into humus.
- Leaching
- water carrying dissolved minerals down through the soil.
- Eluviation
- fine particles such as clay being washed out of an upper layer.
- Illuviation
- those particles being laid down in a lower layer, usually the B horizon.
Real example: large parts of Australia have not been covered by ice or new rock for millions of years. Their soils have been weathered and leached for so long that many are deep but poor in nutrients.
Renewable, but not in a lifetime: Soil does form again, but at about 1 cm per 100 to 1,000 years. Topsoil lost to erosion in a few years cannot be replaced in a human lifetime, so treat it as non-renewable.
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You can compare two soils yourself. Dig to the B horizon at two sites, one managed by people and one natural, and run the same tests on both samples.
What to test
- Take both samples from the B horizon: one from a garden or field, one from a natural ecosystem.
- Texture: rub it between your fingers, or shake it in a jar of water and let the layers settle.
- Nutrients: a test kit for nitrogen (N), phosphorus (P) and potassium (K).
- Drainage: time how fast water poured on the soil drains through.
- Water retention: weigh the soil wet, dry it, weigh it again.
- Organic matter: dry it, weigh it, burn it, weigh it again: the loss on ignition.
Organic matter by loss on ignition: % organic matter = (mass lost on burning ÷ dry mass) × 100
How to do it
- Dry the soil in an oven until its mass stops changing, then weigh it.
- Heat it strongly in a crucible until the organic matter has burned off.
- Weigh it again: the mass lost is the organic matter that burned.
- Divide by the dry mass, multiply by 100, and write the % sign.
Worked example: Woodland soil: mass lost = 20.0 - 18.6 = 1.4 g. % organic matter = (1.4 ÷ 20.0) × 100 = 7.0%.
Check it: the garden sample gives (0.8 ÷ 20.0) × 100 = 4.0%, less than the wood, because dead plants are cleared from a garden and the soil is dug.
Make it a fair test: Same horizon, same mass, both dried until the mass stops changing. Drying first matters: otherwise the mass lost on burning would include water, not just organic matter.
How this comes up: Paper 2, Section A: a table from a soil investigation, then a calculation and short parts.
A student in Ireland compared B-horizon soil from a wheat field and from an old hedgerow beside it. Figure 1 shows the results of burning each dry sample.
(a) Calculate the percentage of organic matter in the hedgerow sample.
(b) Suggest two reasons why the hedgerow soil holds more organic matter than the wheat-field soil.
(c) Outline why each sample was dried before it was burned.
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