{"id":201,"date":"2021-09-16T19:28:53","date_gmt":"2021-09-16T19:28:53","guid":{"rendered":"https:\/\/pressbooks.ccconline.org\/physicalgeology\/chapter\/5-4-weathering-and-the-formation-of-soil-physical-geology-2nd-edition\/"},"modified":"2021-09-16T19:43:02","modified_gmt":"2021-09-16T19:43:02","slug":"5-4-weathering-and-the-formation-of-soil-physical-geology-2nd-edition","status":"publish","type":"chapter","link":"https:\/\/pressbooks.ccconline.org\/physicalgeology\/chapter\/5-4-weathering-and-the-formation-of-soil-physical-geology-2nd-edition\/","title":{"raw":"5.4 Weathering and the Formation of Soil -- Physical Geology – 2nd Edition","rendered":"5.4 Weathering and the Formation of Soil — Physical Geology – 2nd Edition"},"content":{"raw":"\n\n
\n \n \"""\"\n <\/a>\n
Figure 5.4.1 This diagram applies only to the mineral component of soils, and the names are textural descriptions, not soil classes.<\/div>\n <\/div>\n

Soil forms through accumulation and decay of organic matter and through the mechanical and chemical weathering processes described above. The factors that affect the nature of soil and the rate of its formation include climate (especially average temperature and precipitation amounts, and the consequent types and intensity of vegetation), the type of parent material, the slope of the surface, and the amount of time available.<\/p>\n

Climate<\/h1>\n

Soils develop because of the weathering of materials on Earth\u2019s surface, including the mechanical breakup of rocks, and the chemical weathering of minerals. Soil development is facilitated by the downward percolation of water. Soil forms most readily under temperate to tropical conditions (not cold) and where precipitation amounts are moderate (not dry, but not too wet). Chemical weathering reactions (especially the formation of clay minerals) and biochemical reactions proceed fastest under warm conditions, and plant growth is enhanced in warm climates. Too much water (e.g., in rainforests) can lead to the leaching of important chemical nutrients and hence to acidic soils. In humid and poorly drained regions, swampy conditions may prevail, producing soil that is dominated by organic matter. Too little water (e.g., in deserts and semi-deserts), results in very limited downward chemical transportation and the accumulation of salts and carbonate minerals (e.g., calcite) from upward-moving water. Soils in dry regions also suffer from a lack of organic material (Figure 5.4.2).<\/p>\n

\n \"\"\n
Figure 5.4.2 Poorly developed soil on wind-blown silt (loess) in an arid part of northeastern Washington State. The thickness shown is about 1 m, and the \u201csoil\u201d is just the upper 2 or 3 cm.<\/div>\n <\/div>\n

Parent Material<\/h1>\n

Soil parent materials can include all different types of bedrock and any type of unconsolidated sediments, such as glacial deposits and stream deposits. Soils are described as residual soils<\/span><\/strong> if they develop on bedrock, and transported soils if they develop on transported material such as glacial sediments. Other sources may use the term \u201ctransported soil\u201d to imply that the soil itself has been transported, but in this text \u201ctransported soil\u201d is soil that is developed on transported materials, like the very thin soil shown in Figure 5.4.2. When referring to such soil, it is better to be specific and say \u201csoil developed on unconsolidated material,\u201d because that distinguishes it from soil developed on bedrock.<\/p>\n

Quartz-rich parent material, such as granite, sandstone, or loose sand, leads to the development of sandy soils. Quartz-poor material, such as shale or basalt, generates soils with little sand.<\/p>\n

Parent materials provide important nutrients to residual soils. For example, a minor constituent of granitic rocks is the calcium-phosphate mineral apatite (Ca5<\/sub>(PO4<\/sub>)3<\/sub>(F,Cl,OH)), which is a source of the important soil nutrient phosphorus. Basaltic parent material tends to generate very fertile soils because it also provides phosphorus, along with significant amounts of iron, magnesium, and calcium.<\/p>\n

Some unconsolidated materials, such as river-flood deposits, make for especially good soils because they tend to be rich in clay minerals. Clay minerals have large surface areas with negative charges that are attractive to positively charged elements like calcium, magnesium, iron, and potassium\u2014important nutrients for plant growth.<\/p>\n

Slope<\/h1>\n

Soil can only develop where surface materials remain in place and are not frequently moved away by mass wasting. Soils cannot develop where the rate of soil formation is less than the rate of erosion, so steep slopes tend to have little or no soil.<\/p>\n

Time<\/h1>\n

Even under ideal conditions, soil takes thousands of years to develop. Virtually all of southern Canada was still glaciated up until 14 ka, and most of the central and northern parts of B.C., the prairies, Ontario, and Quebec were still glaciated at 12 ka. Glaciers still dominated the central and northern parts of Canada until around 10 ka, and so, at that time, conditions were still not ideal for soil development even in the southern regions. Therefore, soils in Canada, and especially in central and northern Canada, are relatively young and not well developed.<\/p>\n

The same applies to soils that are forming on newly created surfaces, such as recent deltas or sand bars, or in areas of mass wasting.<\/p>\n

Soil Horizons<\/h1>\n

The process of soil formation generally involves the downward movement of clay, water, and dissolved ions, and a common result of that is the development of chemically and texturally different layers known as soil horizons<\/span><\/strong>. The typically developed soil horizons, as illustrated in Figure 5.4.3, are:<\/p>\n