Determinazione del contenuto di umidità del suolo
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Overview
Fonte: Laboratori del Dr. Ian Pepper e del Dr. Charles Gerba – Università dell’Arizona
Autore dimostrativo: Bradley Schmitz
I terreni normalmente contengono una quantità finita di acqua, che può essere espressa come “contenuto di umidità del suolo”. Questa umidità esiste all’interno degli spazi dei pori tra gli aggregati del suolo (spazio dei pori inter-aggregati) e all’interno degli aggregati del suolo (spazio dei pori intra-aggregato) (Figura 1). Normalmente questo spazio dei pori è occupato da aria e / o acqua. Se tutti i pori sono occupati dall’aria, il terreno è completamente asciutto. Se tutti i pori sono riempiti d’acqua, si dice che il terreno sia saturo.
Figura 1. Spazio dei pori nel terreno.
Principles
Negli ambienti naturali all’aperto, l’acqua viene aggiunta al suolo attraverso la pioggia o l’irrigazione deliberata delle piante. In entrambi i casi, l’umidità del suolo aumenta man mano che più pori si riempiono di acqua a scapito dell’aria. Se tutti i pori si riempiono d’acqua, l’acqua in eccesso ora si percola verso il basso (Figura 2) attraverso i pori continui del suolo, fino a quando la pioggia o l’irrigazione cessano. La lisciviazione continuerà fino a quando i film d’acqua all’interno dei pori saranno trattenuti dalla tensione superficiale dei colloidi del suolo contro la forza di gravità. Tale situazione è indicata come il suolo che si trova a “capacità di campo” rispetto all’umidità del suolo. Un terreno a capacità di campo ha pori parzialmente riempiti d’aria, circondati da film di umidità del suolo. Normalmente un terreno a capacità di campo è ottimale per la crescita delle piante e i microrganismi aerobici del suolo, poiché sono disponibili sia aria che acqua. Al contrario, un terreno saturo creerà condizioni anaerobiche impigliate d’acqua che possono uccidere le piante e sopprimere i microbi aerobici del suolo, stimolando i microbi anaerobici.
Figura 2. Lisciviazione dei nutrienti nel terreno.
Considera un campione di terreno umido all’interno di un contenitore come un becher. Il peso del terreno umido è costituito dal peso delle particelle di terreno secco più il peso dell’acqua all’interno del terreno. Se più acqua viene aggiunta al terreno, il peso umido del terreno aumenta. Il peso secco delle particelle di terreno all’interno del campione è fisso, cioèun peso che è il peso secco. Al contrario, ci sono un numero infinito di pesi umidi, a seconda di quanta acqua viene aggiunta al terreno. Per questo motivo, quando si fanno esperimenti di laboratorio con il suolo, il contenuto di umidità del terreno è normalmente espresso su una base di peso secco, perché il peso secco è costante nel tempo, mentre il peso umido o umido può cambiare nel tempo. Quando si esprimono i risultati di un esperimento come il contenuto di nutrienti di un terreno, l’uso della base del peso secco fornisce la standardizzazione del risultato finale.
Procedure
Results
Calculate the soil moisture content for each of the replicate samples using the following equation:
% moisture content (MC) = 
(dry wt. basis)
Example Calculations:
M = 102 g
D = 90 g
∴ % MC = 
MC = 13.3%
With the addition of 5 g of water, new M = 107 and D still equals 90
∴ % MC = 
New MC = 18.9%
Applications and Summary
Knowledge of the moisture content of a soil on a dry weight basis is useful in a number of ways. For example, if the experiments are conducted with soil that should be amended with a known concentration of ammonium fertilizer (for example 50 μg/g), then the moisture content on a dry weight basis must be determined. If the calculation was completed on a wet weight basis, the amount of fertilizer to be added would depend on the moisture content (and therefore the moist weight) of the soil sample. Likewise, if potted plants are considered, the moisture content must be known in order to make sure that the soil isn’t too dry (not enough moisture for plant growth) or too wet (waterlogged and anaerobic). In a field situation, knowledge of the soil moisture content can prevent excess irrigation and leaching of soil nutrients.
Transcript
The amount of water held in soil is an important component of biological and ecological processes, and is used in applications such as farming, erosion prevention, flood control, and drought prediction.
Soils typically contain a finite amount of water, which can be expressed as the soil moisture content. Moisture exists in soil within the pore spaces between soil aggregates, called inter-aggregate pore space, and within pores in the soil aggregates themselves, called intra-aggregate pore space. If the pore space is occupied entirely by air, the soil is completely dry. If all of the pores are filled with water, the soil is saturated.
The measurement of the amount of water held within the soil, or the soil moisture content, is essential to the understanding of soil characteristics and the types of plants and microorganisms that reside in it.
This video will introduce the basics of soil moisture content, and demonstrate the procedure for determining moisture content in the laboratory.
In outdoor environments, water is added to soil naturally through rainfall or deliberately with the irrigation of plants. As the pores in the soil become filled with water at the expense of air, the soil moisture increases. When all of the pores are filled with water, the soil is saturated. If the soil at the surface is saturated, excess water will leach downward through pores into deeper soil. Leaching continues until there is not enough water to saturate all of the pore space. At this point pores contain some air and thin films of moisture. The water films within the pores are held by the surface tension of soil colloids, thus water stops leaching.
After leaching stops, and excess water has drained from the soil, the soil is described as being at field capacity. Soil at field capacity has pores that are partially filled with air, surrounded by films of moisture. Soil at field capacity is optimal for plant growth and aerobic soil microorganisms, since both air and water are available. In contrast, saturated soil, where all pores are filled with water, will create an anaerobic environment that can kill plants and suppress aerobic soil microbes.
The mass of moist soil consists of the mass of the dry soil particles, plus the mass of the water within the soil. The dry mass of the soil particles is fixed, whereas the amount of water within moist soil can vary. Therefore, moisture content is calculated on a dry basis, rather than a total mass basis, to ensure consistency. The moisture content of soil is described as the ratio of the mass of water held in the soil to the dry soil. The mass of water is determined by the difference before and after drying the soil.
The following experiment will demonstrate how to measure soil moisture content in the laboratory using these principles.
To begin, collect soil samples and transfer them into the laboratory. Samples of soil can be collected in the field using a soil auger, or a trowel. Use of a soil auger allows for the soil to be sampled to specific depths. Transfer them into the laboratory. Weigh two aluminum dishes, and accurately record the weight of each dish. Aliquot approximately 20 g of the moist soil into each aluminum dish, then reweigh the dish. Subtract the weight of the empty dish from the full dish to acquire the moist soil weight.
Next, dry the soil overnight in an oven set to 105 °C. On the next day, carefully remove the soil samples from the oven using tongs. Place the soil samples on the bench top to cool. When the dry soil samples are cool, reweigh them and record the total weight. Subtract the weight of the aluminum dish, and record the dry soil weight.
Calculate the moisture content of the soil by subtracting the weight of the dry soil from the weight of the moist soil, and then dividing by the weight of the dry soil.
Although the measurement is simple, it is important to determine soil moisture content in order to better understand soil characteristics.
Soil moisture content plays a large roll in environmental concerns, especially when considering soil runoff that may contain fertilizers and pesticides. In this example, soil runoff was analyzed using a simulated rainfall study in order to determine the retention of a compound in moist soil.
Soil, containing urea, was packed into soil boxes and assembled under a rainfall simulator. Soil runoff was collected, and the concentration of urea in the runoff water calculated. The amount of urea in the soil runoff was higher for soils that had higher moisture content, indicating that urea is better absorbed in drier soil, than in moist.
The fate of chemicals in soil can also be analyzed by direct pore water sampling, using a lysimeter, as shown in this example. In this experiment, lysimeters, or long metal tubing, were installed in soil with turf grass to analyze pore water in vegetative soil.
The pore water sampler was then installed, and water pumped from the lysimeter after applying chemicals to the soil. The collected water was then analyzed, and the concentration of applied chemicals correlated to soil depth and moisture content.
The results demonstrated that the concentration of the herbicide monosodium methyl arsenate, or MSMA, was the highest in the top 2 cm of soil.
You’ve just watched JoVE’s introduction to soil moisture content. You should now understand how to accurately measure soil moisture content in the laboratory. Thanks for watching!
