Soils of the South Central US

It’s sometimes easy to take the soil beneath our feet for granted. Yet soil has always been with us—it is the foundation of our houses and roads, and from the soil comes our food, fiber, and paper. Soil is the interface between living earth and solid rock, between biology and geology. The engineer, the scientist, and the gardener may all look at the soil beneath them in different ways, but perhaps no one has a more integral relationship with soil than a farmer. The economic success of producing crops is intimately tied to the quality of the soil upon which those crops grow, and the most successful farmers are well versed in the science of their soil. Soils store and purify water, and they exchange gasses with the atmosphere. They support agriculture and natural ecosystems and provide a grassy surface for our parks and fodder for our gardens. Everyone, everywhere, every day, depends upon the soil.

What is Soil?

Generally, soil refers to the top layer of earth—the loose surface of earth as distinguished from rock—where vegetation grows. The word is derived (through Old French) from the Latin solum, which means “floor” or “ground.” Soil is one of the most important resources we have—the most basic resource upon which all terrestrial life depends. The South Central has a wide variety of soils, and each type of soil has a story to tell of its origin.

Soils form from the top down, and typically reach a depth of about one meter (3.3 feet) at their more developed stages, although some can reach much deeper. Soils are composed of a mixture of two key ingredients. The first is plant litter, such as dead grasses, leaves, and fallen debris. Worms, bacteria, and fungi do the job of breaking these down into the nutritious organic matter that helps soil to nourish future plant growth. The second important component of soil is the sediment derived from the weathering of rock that is then transported by wind, water, or gravity. Both of these components influence the texture (Figure 8.1) and consistency of the soil, as well as the minerals available for consumption by plants.

All soils might seem alike, but there can be vast differences in soil properties even within small areas! A single acre may contain several different soil types, each with its own assets and drawbacks. Some types of soil are clayey or prone to flooding, while others are stable enough to be used as a foundation for buildings. The most identifiable physical properties of soils are texture, structure, and color, which provide the basis for distinguishing soil horizons. Texture refers to the percentage of sand, silt, and clay that makes up the soil. Soil textures have specific names, as indicated in Figure 8.1.

Figure 8.1: Soil texture triangle.

Generally, the best agricultural soils are those with about equal amounts of clay, silt, and sand. A soil of that type is called a loam. Soils that are mostly sand do not hold water very well and dry quickly, while soils with too much clay may never dry out.

Soil structure refers to the way the soil forms clumps, known as peds. Peds are identified by the shape of the soil clods, which take the form of balls, blocks, columns, and plates. These structures are easiest to see in recently plowed fields, where the soil is often granular and loose or lumpy.

Soil color is its most obvious physical property. The color is influenced by mineral content, the amount of organic material, and the amount of water it routinely holds. The colors are identified by a standard soil color chart called the Munsell chart.

Five main variables affect the characteristics of soil worldwide. In the South Central, all soils are the products of subtle differences among these five factors:

1. Parent material is the original geologic material from which the soil formed. This can be bedrock, preexisting soils, or other materials such as till or loess.

2. Climate strongly determines the temperature regime, amount of moisture, and type of biota that interact with the parent material. This affects the extent of chemical and physical weathering on the soil-forming material.

3. Topography, or landscape, of the area is related to the relative position of the soil on the landscape. This includes the presence or absence of hills and the slopes between high and low areas. Topography influences natural drainage. Gravity moves water down slopes to depressions or streams and pulls free water downward through the soil. Soils on hills tend to be dry, and soils in depressions and valleys are often wet or saturated. Areas with steep slopes that are susceptible to frequent erosion typically have very young soils, as they do not have long to develop before the ingredients are rearranged and the clock is reset. Flatter, more arid areas may have more time to develop, but they have significantly less plant life and will produce a very different soil than will a wetter environment.

4. Biota or living organisms that live on or in the material affect soil development through their influence on the amount and distribution of organic matter in the soil. For example, plants contribute significantly to the formation of humus, and animals alter a soil’s characteristics by leaving behind decayed remains and wastes. Decomposers like bacteria and fungi help to free up the nutrients locked away in these remains and wastes, and these freed nutrients are then recycled and used by new life forms within the same soil. In fact, more than 90% of the nutrients used by a forest in a given year are derived from the decomposition of old organic matter fallen to the forest floor. Animal burrows also create spaces in the soil horizons that allow for deeper penetration of air and water, which, in turn, aid plant development. For its part, organic matter impacts the water-holding capacity of the soil, the soil’s fertility, and root penetration.

5. Time is required for soils to develop while the four elements mentioned above interact. Older soils have deeper and thicker subsoils than do younger soils, but only if other soil forming factors remain constant. In west-central Kansas, for example, it takes approximately 500 years to generate a new 2.5 centimeters (1 inch) of topsoil beneath the prairie grass—but it only takes a few years for erosion and weathering to destroy the same amount of unprotected topsoil.

Several types of chemical reactions are important for soil development; of these, acid-base reactions are some of the most important and complex. When carbon dioxide (CO₂) dissolves in water it forms weak carbonic acid. CO₂ found in soil water can come from the atmosphere, where it dissolves in rainwater. Even more CO₂ usually comes from the soil itself, where it is produced by respiring organisms. The amount of CO₂ in soil gases can easily reach levels ten times higher than the amount found in the atmosphere (over 4000 ppm in soil vs. 400 ppm in the atmosphere), making soil water potentially more acidic than rainwater. As this acidic water slowly reacts with fresh minerals, it buffers the soil’s pH and keeps it in a range (6-8) preferred by many organisms. Acid-driven weathering breaks down the soil’s primary igneous minerals, typically transforming them to silica-rich clays. As the soil’s primary minerals are depleted, it loses the ability to buffer acidity, and the pH of highly weathered soil can drop to around 4. These weathered soils tend to be rich in aluminum, iron, and titanium.

In highly weathered settings, soil loses most of its nutrients, and the store of nutrients that remains is mostly found in organic matter. In weathered soils, only the top 25 cm (10 inches) or so may be very biologically active, and rooting depths are very shallow. If this thin layer is lost to erosion, the underlying mineral soil may be infertile and incapable of rapid recovery.

Soil Orders

Just as rocks are classified into different types based on how they formed (igneous, metamorphic, or sedimentary), their mineral composition, and other characteristics, soils also have their own classification scheme. Soil develops in horizons, or layers, whose formation is dependent on the available ingredients, environmental conditions, and the time to mature. More mature soils will develop a variety of horizons unique to their environmental conditions, creating a soil profile. Some horizons are completely absent in certain profiles while others are common to most. Each horizon corresponds to a stage in the weathering of rock and decay of plant matter, and each is found at a specific position beneath the surface (Figure 8.2).

Figure 8.2: A typical soil profile shows the transition from the parent material (horizon C) to the highly developed or changed horizons (O through B). Not every soil profile will have all the horizons present.

Soils can also be categorized by their location (northern vs. southern soils), the type of vegetation growing on them (forest soils vs. desert soils), their topographic position (hilltop soils vs. valley soils), or other distinguishing features. The system used to classify soils based on their properties is called soil taxonomy (Figure 8.3), and it was developed by the United States Department of Agriculture (USDA) with the help of soil scientists throughout the country. It provides a convenient, uniform, and detailed classification of soils throughout the country (Figure 8.4), allowing for an easier understanding of how and why different regions have developed unique soils.

In soil taxonomy, all soils are arranged into one of 12 major units, or soil orders. These 12 orders are defined by diagnostic horizons, composition, soil structures, and other characteristics. Soil orders depend mainly on climate and the organisms within the soil. These orders are further broken down into 64 suborders based on properties that influence soil development and plant growth, with the most important property being how wet the soil is throughout the year. The suborders are, in turn, separated into great groups (300+) and subgroups (2400+). Similar soils within a subgroup are grouped into even more selective families (7500+), and similar soils within families are grouped together into the most exclusive category of all: a series. There are more than 19,000 soil series described in the United States, with more being defined every year.

Figure 8.3: Soil taxonomy.

Figure 8.4: Dominant soil orders of the United States.

The 12 soil orders

Dominant Soils of the South Central

Eight soil orders are found in the South Central, with the greatest diversity found within the Coastal Plain.

Alfisols are partially leached soils with a high degree of fertility that form primarily in forested regions. These soils tend to develop in cooler, more forested environments, and they commonly form a band separating more arid areas from humid areas. They are found throughout the South Central region, particularly in the Coastal Plain and Central Lowland (Figure 8.5).

Aridisols are very dry soils that form in arid environments, such as the Basin and Range region (Figure 8.6). Water content is very low or even nonexistent for most of the year, leading to limited leaching. The lack of leaching means that there is abundant calcium carbonate in the soils, which makes them quite alkaline. This soil type is unsuitable for plants that are not adapted to store water or to survive extreme drought.

Entisols are soils of recent origin with poorly developed horizons, typically formed near floodplains. They are not common in the South Central, but they are found in all five of its regions (Figure 8.7).

Histosols are carbon-rich soils, where half or more of the upper 80 centimeters (32 inches) is organic. They contain high concentrations of organic matter, due to their development in wetland environments with poor drainage and a slow rate of decomposition. They are saturated year round, and are often called bogs, moors, peats, or mucks. In the South Central, they are found along the coast of Louisiana in the Coastal Plain (Figure 8.8).

Inceptisols are soils with poorly developed horizons that are associated with steep slopes and resistant parent material. They are located in cool to very warm, humid, and subhumid regions. They often overlie erosion-resistant bedrock and are scattered around most regions of the South Central (Figure 8.9).

Figure 8.5: Alfisols of the South Central.

Figure 8.6: Aridisols of the South Central.

Figure 8.7: Entisols of the South Central.

Figure 8.8: Histosols of the South Central.

Figure 8.9: Inceptisols of the South Central.

Figure 8.10: Mollisols of the South Central.

Figure 8.11: Ultisols of the South Central.

Figure 8.12: Vertisols of the South Central.

Mollisols are the dominant soils of grasslands. The thick, black A horizon makes these soils extremely productive and valuable to agriculture. They are one of the most abundant soil types in the South Central (Figure 8.10).

Ultisols are soils with clay accumulations below the surface (often red, due to iron oxides) and low native fertility. They form in humid areas and, like Alfisols, have a clay-enriched subsoil. Ultisols often support forest vegetation, so they are most common in the forested areas of the South Central (Figure 8.11).

Vertisols are very dark soils, rich in swelling clays. Their distinguishing feature is that they form deeply cracked surfaces during dry periods, but they swell again in the wet season, which seals all the cracks. As a result, they are very difficult soils to build roads or other structures on. Vertisols are found primarily in the Coastal Plain region (Figure 8.12).

Geology of the South Central: Parent Material

The South Central is home to a variety of parent materials—the minerals and organic matter from which its soils are derived (Figure 8.13). The floodplain and delta of the Mississippi River provide alluvial sediments: silt- and clay-rich parent materials that produce agriculturally rich soils. In fact, the Mississippi River floodplain and delta together represent the largest contiguous set of alluvial deposits in the US (Figure 8.14). Many of these deposits result from glacial outwash.

Although the South Central was not subjected to the degree of glaciation experienced by more northern regions of the US, the pre-Illinoian glacial advance did reach the northern part of Missouri and the northwest portion of Kansas. This glaciation lead to the accumulation of loess deposits (Figure 8.15), carried by wind and deposited by river systems, that are responsible for the development of some of the extremely productive agricultural soils found there today.

Weathered sedimentary rock is perhaps the most ubiquitous parent material in the South Central. Sandstone, siltstone, limestone, and shale are among the most common bedrocks across the South Central States; over time, erosional processes have contributed to the formation of soils from all of these sedimentary substrates.

Figure 8.13: Physiographic and regolith map of the South Central.