Quick and Dirty Bi-digital Soil Texture Analysis

If a ribbon is formed, and…

if the ribbon is long, flexible, and can sustain its own weight, the soil is a clay
if ribbon is weak, breaks readily, but forms a ball which withstands much handling, the soil is a clay loam
if the clay loam is soapy or slippery feeling, and appears powdery when dry, the soil is silty clay loam
if the clay loam has lots of visible sand, it is a sandy clay loam

If soil will not form a ribbon, but instead gives a broken appearance, and…

If wet soil is friable, somewhat gritty and sticky, the ball handles without breaking, the soil is a loam
if the dry soil feels soft and floury, wet feels slippery, ball does not break, the soil is silt loam
if sand can be seen, and the ball cannot withstand handling without breaking, the soil is a sandy loam

If soil is loose and single grained, and individual grains can be easily seen, and the aggregate crumbles when touched, you have a sand.

Soil Structure - Soil structure refers to the way the soil aggregates, particles, and pore space are arranged with respect to each other. We use shape, size, and strength to define it. Physically, we can describe structure as being platy, block, granular, subangular blocky, etc.

Structure, or even a lack of structure, can affect plant growth in several ways. For example, it affects air exchange with the atmosphere, the speed of water movement into and through the soil. Also, it influences the quantity and size of pores, and the rate and extent of root growth. Structure may be altered for better or worse through sound or poor management.

Organic matter, bacterial and fungal biomass, and clay minerals are the primary agents for binding soil particles together to form aggregates. Sandy, low organic matter soils often lack structure. Incorporation of humic materials - leaf compost, peat, composted sawdust, etc., will generally improve overall soil structure and tilth.

Crusting and compaction often occurs when bare soils are subjected to regular and intense rainfall. The intense rain destroys the surface structure by washing away the clay particles and organic material holding the soil particles together. Without the binding agents, the particles clog up the natural drainage of the surface layer and make it impervious to water coming in and gases going out. Soils can easily be compacted by both natural phenomena and through human activity. Have you ever noticed "deer trails" in and around forested areas? Regular use by deer will cause the trails to become compacted and largely, unvegetated. Schoolyard trails develop in the same way.

Organic matter - Organic matter is the carbon-based residue remaining after processing and decomposition of usable macro-organic matter by soil baceria, fungi and invertebrates. Soil organic matter in the soil matrix is made of humic substances. Humic materials are relatively stable and resistant to rapid breakdown, although over time, decomposition will continue.

The chemical composition of soil organic matter ranges from very simple to very complex chemical compounds, including sugars, starches, carbohydrates, nucleic acids, humic acids, etc. Organic soil amendments, as mentioned previously, tend to improve soil structure. Positive results of increased organic matter in soils, also: (1) enhance development of soil aggregates; (2) inreases pore space; (3) increases infiltration and percolation rates; (4) increases water holding capacity; (5) increases a soil's capacity to hold and release nutrients; (6) improves ease of cultivation (tilth); and (7) most importantly, promotes increased biological activity

Organic matter content of soil is a very dynamic property. For example, excessive cultivation, fertilization and aeration, speeds decomposition and thus lowers organic matter. Soil organic matter is not a "permanent" feature of soils and can diminish quickly in warm, moist climates. However, addition of compost is an effective way of maintaining organic matter at an equilibrium, or even rapidly increasing organic matter. However, in Mississippi's climate, to maintain higher levels of organic annual regular additions have to made.

Soil Atmosphere & Water - Soils have varying levels of pore space - the spaces or voids between soil particles. The porosity affects the ability of soils to maintain aeration and to retain and drain water. The soil "air" is usually somewhat different, particularly in regard to O2/CO2 ratios. Carbon dioxide tends to be somewhat higher in the soil atmosphere, especially in biologically active soils. Pore spaces can also be occupied by water. When water occupies the pore spaces, it displaces the "air", including oxygen. Sustained flooding of a soil can lead to development of anaerobic conditions that are characteristic of wetland soils. In well-drained soils, both gases and water co-exist. Plant-available soil water can also occur as a film over soil particles, and it can be retained in the structure of organic substances and clays. Not only does soil water provide water for plant roots and to soil organisms, it also carries nutrients such as nitrate, calcium, magnesium, phosphate and potassium.

Color - Soil Color is one of the more simple soil properties to test for. It can provide an indirect measurement of soil properties such as drainage and organic matter content. Most minerals which occur in soils are not highly colored. When they become coated with organic matter, iron oxides, or other materials, the soil takes on the color of those materials. Soil Color is described in terms of hue, value and chroma based on the Munsell color system. Hue is the primary rainbow color. Value relates to the relative darkness of the color. Chroma is the intensity of the color. Partially decomposed organic matter is usually brown in color. As the organic matter decompose more it will become black in color. Dark soils tend to have high organic matter (3-6+%). Light soils are usually very low in organic matter (< 1%).