Soil hydrology - Revision history

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	The chemical properties of water govern its behavior in the environment and control many key processes occurring in soils as it interacts with [[organisms]], [[minerals]], and air spaces. As a result of its nonlinear structure and polarity, water is a powerful solvent, allowing it to readily dissolve ionic solids. Water molecules diminish the attractive force of ions by surrounding and forming solvation spheres around them. This allows water to stabilize the charges of both anions and cations, preventing their association.<ref>Sparks, D. L. Environmental Soil Chemistry. 2nd ed. Academic Press, 2003.</ref><ref name=Eisenberg_1969'''Bold text'''>Eisenberg, D. & Kauzmann, W. The Structure and Properties of Water. 296 Oxford University Press, 1969.</ref>		The chemical properties of water govern its behavior in the environment and control many key processes occurring in soils as it interacts with [[organisms]], [[minerals]], and air spaces. As a result of its nonlinear structure and polarity, water is a powerful solvent, allowing it to readily dissolve ionic solids. Water molecules diminish the attractive force of ions by surrounding and forming solvation spheres around them. This allows water to stabilize the charges of both anions and cations, preventing their association.<ref>Sparks, D. L. Environmental Soil Chemistry. 2nd ed. Academic Press, 2003.</ref><ref name=Eisenberg_1969'''Bold text'''>Eisenberg, D. & Kauzmann, W. The Structure and Properties of Water. 296 Oxford University Press, 1969.</ref>

	The ability of water to stabilize charged species in solution allows it to support the flow of electrons in soils. As such, water helps mediate oxidation and reduction (redox) reactions within the soil solution. Water itself may participate in these processes, and it is a product of cellular respiration in soils. In aerobic soils, water is produced from the oxidation of carbon in organic matter for energy production by [[microorganisms]].		The ability of water to stabilize charged species in solution allows it to support the flow of electrons in soils. As such, water helps mediate oxidation and reduction (redox) reactions within the soil solution. Water itself may participate in these processes, and it is a product of cellular respiration in soils. In aerobic soils, water is produced from the oxidation of carbon in [[Organic Matter\|organic matter]] for energy production by [[microorganisms]].

	[[File:Water_liquor.jpg\|300px\|thumb\|left\|]]		[[File:Water_liquor.jpg\|300px\|thumb\|left\|]]

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	Soil hydrology is the study of the movement and distribution of water through [[soil]] and is a subset of the larger field of [[Hydrogeology]]. Hydrologic processes within soil include [[infiltration]], storage, drainage, redistribution, [[evaporation]], and [[transpiration]]. The structural properties of soil (composition, [[porosity]], etc) and the chemical properties of water regulate the flow of water and other materials through soil.		Soil hydrology is the study of the movement and distribution of water through [[soil]] and is a subset of the larger field of [[Hydrogeology]]. Hydrologic processes within soil include [[infiltration]], storage, drainage, redistribution, [[evaporation]], and [[transpiration]]. The structural [[properties]] of soil (composition, [[porosity]], etc) and the chemical properties of water regulate the flow of water and other materials through soil.
	[[File:soil_illustration.jpg\|300px\|thumb\|right\|Illustration of soil water interacting with and flowing through soil minerals and organic matter.<ref>http://www.fao.org/3/a0072e/a0072e07.htm</ref>]]		[[File:soil_illustration.jpg\|300px\|thumb\|right\|Illustration of soil water interacting with and flowing through soil minerals and organic matter.<ref>http://www.fao.org/3/a0072e/a0072e07.htm</ref>]]

Leahtayl at 17:26, 31 March 2022

2022-03-31T17:26:29Z

← Older revision		Revision as of 13:26, 31 March 2022
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	Soil hydrology is the study of the movement and distribution of water through [[soil]] and is a subset of the larger field of [[Hydrogeology]]. Hydrologic processes within soil include infiltration, storage, drainage, redistribution, evaporation, and transpiration. The structural [[properties]] of soil (composition, porosity, etc) and the chemical properties of water regulate the flow of water and other materials through soil.		Soil hydrology is the study of the movement and distribution of water through [[soil]] and is a subset of the larger field of [[Hydrogeology]]. Hydrologic processes within soil include [[infiltration]], storage, drainage, redistribution, [[evaporation]], and [[transpiration]]. The structural properties of soil (composition, [[porosity]], etc) and the chemical properties of water regulate the flow of water and other materials through soil.
	[[File:soil_illustration.jpg\|300px\|thumb\|right\|Illustration of soil water interacting with and flowing through soil minerals and organic matter.<ref>http://www.fao.org/3/a0072e/a0072e07.htm</ref>]]		[[File:soil_illustration.jpg\|300px\|thumb\|right\|Illustration of soil water interacting with and flowing through soil minerals and organic matter.<ref>http://www.fao.org/3/a0072e/a0072e07.htm</ref>]]

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	Liquid water is a key component of the three-phase (solid, liquid, gas) soil system, possibly occupying 50% or more of the total soil volume under saturated conditions. Even under relatively dry conditions, water can be held within soil pores, occupying approximately 5–10% of the soil volume. Particle size is strongly related to how much water soil can retain. Soils with smaller particle sizes, such as [[clay]], will retain more water than soils with larger particles sizes, such as [[sand]]. Liquid water is held in soil due to the adhesive and cohesive forces associated with water's molecular structure.<ref>Hillel, D., 1974. Soil and water. Physical principles and processes.</ref>		Liquid water is a key component of the three-phase (solid, liquid, gas) soil system, possibly occupying 50% or more of the total soil volume under saturated conditions. Even under relatively dry conditions, water can be held within soil pores, occupying approximately 5–10% of the soil volume. Particle size is strongly related to how much water soil can retain. Soils with smaller particle sizes, such as [[clay]], will retain more water than soils with larger particles sizes, such as [[sand]]. Liquid water is held in soil due to the adhesive and cohesive forces associated with water's molecular structure.<ref>Hillel, D., 1974. Soil and water. Physical principles and processes.</ref>

	Three types of water exist in soils- gravitational, adsorbed, and capillary. Gravitational water easily moves through large pore spaces under the influence of gravity and tends not to to be accessible to plants because it moves quickly through the soil. Adsorbed water is held tightly against soil particles due to adhesion, which is the attractive force between water molecules and solid surfaces. This type of water also tends not to be accessible to plants because of the strong adhesive forces binding it to the surface of the soil particle. Capillary water is held in the spaces between soil particles and is generally the most accessible to plants. Capillary water occurs in soil pore spaces due to cohesion, or the attractive force between water molecules. The larger the pore spaces, the more water there is available for plants.		Three types of water exist in soils- gravitational, adsorbed, and capillary. Gravitational water easily moves through large pore spaces under the influence of gravity and tends not to to be accessible to [[plants]] because it moves quickly through the soil. Adsorbed water is held tightly against soil particles due to adhesion, which is the attractive force between water molecules and solid surfaces. This type of water also tends not to be accessible to plants because of the strong adhesive forces binding it to the surface of the soil particle. Capillary water is held in the spaces between soil particles and is generally the most accessible to plants. Capillary water occurs in soil pore spaces due to cohesion, or the attractive force between water molecules. The larger the pore spaces, the more water there is available for plants.

	The interaction between water and soil particles is often visualized with a capillary tube model. Water molecules are more attracted to each other than to air (due to hydrogen bonding and cohesion), which creates surface tension. When combined with adhesion, or the attraction between water molecules and solid surfaces (the capillary tube wall), a meniscus is formed at the water-air interface. Water will rise in the capillary tube until it reaches an equilibrium between the attractive upward force at the interface and the weight of water pulling downward on the meniscus.<ref>Fisher, R.A., 1926. On the capillary forces in an ideal soil; correction of formulae given by W. B. Haines. J. Agric. Sci. 16, 492–505. https://doi.org/10.1017/S0021859600007838</ref>		The interaction between water and soil particles is often visualized with a capillary tube model. Water molecules are more attracted to each other than to air (due to [[hydrogen bonding]] and cohesion), which creates surface tension. When combined with adhesion, or the attraction between water molecules and solid surfaces (the capillary tube wall), a meniscus is formed at the water-air interface. Water will rise in the capillary tube until it reaches an equilibrium between the attractive upward force at the interface and the weight of water pulling downward on the meniscus.<ref>Fisher, R.A., 1926. On the capillary forces in an ideal soil; correction of formulae given by W. B. Haines. J. Agric. Sci. 16, 492–505. https://doi.org/10.1017/S0021859600007838</ref>
	The capillary tube can be used to understand how water behaves in soil pores, and has also been used to understand how management practices such as agricultural tillage that alter pore size distribution can affect soil's ability to hold water.		The capillary tube can be used to understand how water behaves in soil pores, and has also been used to understand how management practices such as [[agricultural tillage]] that alter pore size distribution can affect soil's ability to hold water.

	=== Darcy's Law ===		=== Darcy's Law ===

Leahtayl at 17:22, 31 March 2022

2022-03-31T17:22:42Z

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	The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>		The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>

	~~{{nowrap\|''~~Q~~'' {{~~=~~}} ''~~KA~~''}}~~		Q = KA(dH/dL)

	When applied to soils, Darcy's law states that the flow rate (Q) of water is equal to the hydraulic conductivity of the soil (K) times the cross-sectional area (A) times the hydraulic gradient (dH/dL), which is the change in head over the change in length of interest. This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>		When applied to soils, Darcy's law states that the flow rate (Q) of water is equal to the hydraulic conductivity of the soil (K) times the cross-sectional area (A) times the hydraulic gradient (dH/dL), which is the change in head over the change in length of interest. This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>

	=== Temperature Regulation ===		=== Temperature Regulation ===
	~~The prevalence of water~~ within the soil system also ~~drives~~ terrestrial temperature dynamics. When ~~liquid~~ water enters the soil matrix, it displaces the soil ~~gas phase~~. Water requires a relatively large energy input or loss (heat capacity, 4.18 kJ kg-1 K-1) to change its temperature because of strong interactions (hydrogen bonding) between ~~dipolar~~ water molecules. Alternately, weak inter-molecular interactions in soil gases allow ~~soil~~ temperatures to change readily with a small energy input or loss~~. Furthermore, because soil water can exist in liquid, gas (vapor) and solid (ice) phases, latent heat loss or gain from soil associated with phase change also impacts the thermal regime~~. In moist environments with ample soil water, water vapor loss from soil through evaporation requires a large energy input (heat of vaporization, 2449 kJ kg-1) without accompanying temperature change because of the large energy input required to disrupt the hydrogen bonds between liquid water molecules. Similarly, a large latent heat loss is required for soil freezing due to the high heat of fusion (334 kJ kg-1) associated with the more rigid, low-density structure of ice. Thermal properties of water within soil mediate environmental conditions for the biological community and regulate the thermodynamics of biogeochemical reactions.<ref>Campbell, G. S. & Norman, J. M. An Introduction to Environmental Biophysics. Vol. second 286 Springer-Verlag, 1998.</ref>		Water within the soil system also influences terrestrial temperature dynamics. When water enters the soil matrix, it displaces gas in the soil. Water requires a relatively large energy input or loss (heat capacity, 4.18 kJ kg-1 K-1) to change its temperature because of strong interactions (hydrogen bonding) between water molecules. Alternately, weak inter-molecular interactions in soil gases allow temperatures to change readily with a small energy input or loss. In moist environments with ample soil water, water vapor loss from soil through evaporation requires a large energy input (heat of vaporization, 2449 kJ kg-1) without accompanying temperature change because of the large energy input required to disrupt the hydrogen bonds between liquid water molecules. Similarly, a large latent heat loss is required for soil freezing due to the high heat of fusion (334 kJ kg-1) associated with the more rigid, low-density structure of ice. Thermal properties of water within soil mediate environmental conditions for the biological community and regulate the thermodynamics of biogeochemical reactions.<ref>Campbell, G. S. & Norman, J. M. An Introduction to Environmental Biophysics. Vol. second 286 Springer-Verlag, 1998.</ref>

	== '''Chemical Properties''' ==		== '''Chemical Properties''' ==

	=== As a Solvent ===		=== As a Solvent ===
	The chemical properties of water govern its behavior in the environment and control many key processes occurring in soils as ~~the aqueous phase~~ interacts with [[organisms]], ~~mineral surfaces~~, and air spaces. As a result of its nonlinear structure and ~~dipole moment~~, water ~~has a high dielectric constant (80.1 at 20°C), which~~ is ~~a measure of a substance's ability to minimize the force of attraction between oppositely charged species.~~		The chemical properties of water govern its behavior in the environment and control many key processes occurring in soils as it interacts with [[organisms]], [[minerals]], and air spaces. As a result of its nonlinear structure and polarity, water is a powerful solvent, allowing it to readily dissolve ionic solids. Water molecules diminish the attractive force of ions by surrounding and forming solvation spheres around them. This allows water to stabilize the charges of both anions and cations, preventing their association.<ref>Sparks, D. L. Environmental Soil Chemistry. 2nd ed. Academic Press, 2003.</ref><ref name=Eisenberg_1969'''Bold text'''>Eisenberg, D. & Kauzmann, W. The Structure and Properties of Water. 296 Oxford University Press, 1969.</ref>
	~~This unique property of water also makes it~~ a powerful solvent, allowing it to readily dissolve ionic solids. Water ~~acts to dissipate~~ the attractive force of ions by forming solvation spheres around them. ~~The polar nature of the~~ water ~~molecules allow them~~ to ~~surround and~~ stabilize the charges of both anions and cations, preventing their association.<ref>Sparks, D. L. Environmental Soil Chemistry. 2nd ed. Academic Press, 2003.</ref><ref name=Eisenberg_1969'''Bold text'''>Eisenberg, D. & Kauzmann, W. The Structure and Properties of Water. 296 Oxford University Press, 1969.</ref>

	~~[[File:Water_liquor.jpg\|300px\|thumb\|left\|]]~~

	~~=== PH Regulation ===~~
	Another particularly important chemical property of water that impacts processes occurring within the soil solution is that it is amphoteric, meaning that it can act as either an acid or a base. Due to its polarity, water readily undergoes ionic dissociation into protons and hydroxide ions. When it reacts with a strong base, water acts as an acid, releasing protons. When it reacts with a strong acid, water acts as a base, accepting protons.

	The amphoteric behavior of water facilitates the acid-base chemistry and dictates the potential pH range of aqueous solutions, thereby imparting [[soil pH]] — a "master variable" of soils that influences soil formation, plant growth, and environmental quality.

	The ability of water to stabilize charged species in solution allows it to support the flow of electrons in soils. As such, water helps mediate oxidation and reduction (redox) reactions within the soil solution. Water itself may participate in these processes, and it is a product of cellular respiration in soils. In aerobic soils, water is produced from the oxidation of carbon in organic matter for energy production by [[microorganisms]].		The ability of water to stabilize charged species in solution allows it to support the flow of electrons in soils. As such, water helps mediate oxidation and reduction (redox) reactions within the soil solution. Water itself may participate in these processes, and it is a product of cellular respiration in soils. In aerobic soils, water is produced from the oxidation of carbon in organic matter for energy production by [[microorganisms]].

			[[File:Water_liquor.jpg\|300px\|thumb\|left\|]]

			=== pH Regulation ===
			Another particularly important chemical property of water is that it is amphoteric, meaning that it can act as either an acid or a base. Due to its polarity, water readily dissociates into protons and hydroxide ions. When it reacts with a strong base, water acts as an acid, releasing protons. When it reacts with a strong acid, water acts as a base, accepting protons. This amphoteric behavior of water facilitates the acid-base chemistry and dictates the potential pH range of aqueous solutions, thereby imparting [[soil pH]] — a "master variable" of soils that influences soil formation, plant growth, and environmental quality.

	==References==		==References==
	{{reflist}}		{{reflist}}

Leahtayl at 01:49, 29 March 2022

2022-03-29T01:49:47Z

← Older revision		Revision as of 21:49, 28 March 2022
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	Liquid water is a key component of the three-phase (solid, liquid, gas) soil system, possibly occupying 50% or more of the total soil volume under saturated conditions. Even under relatively dry conditions, water can be held within soil pores, occupying approximately 5–10% of the soil volume. Particle size is strongly related to how much water soil can retain. Soils with smaller particle sizes, such as [[clay]], will retain more water than soils with larger particles sizes, such as [[sand]]. Liquid water is held in soil due to the adhesive and cohesive forces associated with water's molecular structure.<ref>Hillel, D., 1974. Soil and water. Physical principles and processes.</ref>		Liquid water is a key component of the three-phase (solid, liquid, gas) soil system, possibly occupying 50% or more of the total soil volume under saturated conditions. Even under relatively dry conditions, water can be held within soil pores, occupying approximately 5–10% of the soil volume. Particle size is strongly related to how much water soil can retain. Soils with smaller particle sizes, such as [[clay]], will retain more water than soils with larger particles sizes, such as [[sand]]. Liquid water is held in soil due to the adhesive and cohesive forces associated with water's molecular structure.<ref>Hillel, D., 1974. Soil and water. Physical principles and processes.</ref>

	The interaction between water and ~~the~~ soil ~~solid matrix~~ is often visualized with a capillary tube model. ~~Liquid water at the water-gas interface exhibits a meniscus. The inward pull of liquid water~~ molecules ~~from~~ hydrogen bonding (cohesion) ~~is unbalanced at the liquid-gas interface~~, which ~~is referred to as~~ surface tension. ~~In combination~~ with the ~~polar~~ attraction of water molecules ~~for a wettable soil~~ solid ~~matrix~~ (~~adhesion to~~ the capillary tube wall), ~~this cohesion creates concave curvature~~. Water ~~rises~~ in the tube ~~to reach~~ equilibrium between the attractive upward force at the interface and the weight of water pulling downward on the meniscus.<ref>Fisher, R.A., 1926. On the capillary forces in an ideal soil; correction of formulae given by W. B. Haines. J. Agric. Sci. 16, 492–505. https://doi.org/10.1017/S0021859600007838</ref>		Three types of water exist in soils- gravitational, adsorbed, and capillary. Gravitational water easily moves through large pore spaces under the influence of gravity and tends not to to be accessible to plants because it moves quickly through the soil. Adsorbed water is held tightly against soil particles due to adhesion, which is the attractive force between water molecules and solid surfaces. This type of water also tends not to be accessible to plants because of the strong adhesive forces binding it to the surface of the soil particle. Capillary water is held in the spaces between soil particles and is generally the most accessible to plants. Capillary water occurs in soil pore spaces due to cohesion, or the attractive force between water molecules. The larger the pore spaces, the more water there is available for plants.
	The ~~analog of the~~ capillary tube ~~for~~ soil pores also ~~has~~ been used to understand ~~wetting above the water table and~~ how management practices that alter pore size distribution~~, such as agricultural tillage,~~ can affect soil's water ~~holding capacity~~.
			The interaction between water and soil particles is often visualized with a capillary tube model. Water molecules are more attracted to each other than to air (due to hydrogen bonding and cohesion), which creates surface tension. When combined with adhesion, or the attraction between water molecules and solid surfaces (the capillary tube wall), a meniscus is formed at the water-air interface. Water will rise in the capillary tube until it reaches an equilibrium between the attractive upward force at the interface and the weight of water pulling downward on the meniscus.<ref>Fisher, R.A., 1926. On the capillary forces in an ideal soil; correction of formulae given by W. B. Haines. J. Agric. Sci. 16, 492–505. https://doi.org/10.1017/S0021859600007838</ref>
			The capillary tube can be used to understand how water behaves in soil pores, and has also been used to understand how management practices such as agricultural tillage that alter pore size distribution can affect soil's ability to hold water.

	=== Darcy's Law ===		=== Darcy's Law ===

	The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref> When applied to soils, Darcy's law states that the flow rate (Q) of water is equal to the hydraulic conductivity of the soil (K) times the cross-sectional area (A) times the hydraulic gradient (dH/dL), which is the change in head over the change in length of interest. This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>		The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>

			{{nowrap\|''Q'' {{=}} ''KA''}}

			When applied to soils, Darcy's law states that the flow rate (Q) of water is equal to the hydraulic conductivity of the soil (K) times the cross-sectional area (A) times the hydraulic gradient (dH/dL), which is the change in head over the change in length of interest. This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>

	=== Temperature Regulation ===		=== Temperature Regulation ===

Leahtayl: /* Darcy's Law */

2022-03-21T20:11:10Z

Darcy's Law

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	=== Darcy's Law ===		=== Darcy's Law ===

	The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>When applied to soils, Darcy's law states that the flow rate (Q) of water is equal to the hydraulic conductivity of the soil (K) times the cross-sectional area (A) times the hydraulic gradient (dH/dL), which is the change in head over the change in length of interest. This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>		The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref> When applied to soils, Darcy's law states that the flow rate (Q) of water is equal to the hydraulic conductivity of the soil (K) times the cross-sectional area (A) times the hydraulic gradient (dH/dL), which is the change in head over the change in length of interest. This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>

	=== Temperature Regulation ===		=== Temperature Regulation ===

Leahtayl: /* Darcy's Law */

2022-03-21T20:10:02Z

Darcy's Law

← Older revision		Revision as of 16:10, 21 March 2022
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	=== Darcy's Law ===		=== Darcy's Law ===

	~~{{math\| 1}}~~		The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>When applied to soils, Darcy's law states that the flow rate (Q) of water is equal to the hydraulic conductivity of the soil (K) times the cross-sectional area (A) times the hydraulic gradient (dH/dL), which is the change in head over the change in length of interest. This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>

	The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>When applied to soils, Darcy's law states that the ~~flux~~ (q) of water is ~~proportionate~~ to the hydraulic conductivity of the soil (k) ~~and~~ the ~~pressure gradient (\delta H) for a given~~ cross-sectional area ~~and length~~ (L). This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>

	=== Temperature Regulation ===		=== Temperature Regulation ===

Leahtayl: /* Darcy's Law */

2022-03-21T20:01:14Z

Darcy's Law

← Older revision		Revision as of 16:01, 21 March 2022
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	=== Darcy's Law ===		=== Darcy's Law ===

	<math~~>\delta</math>~~		{{math\| 1}}

	The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>When applied to soils, Darcy's law states that the flux (q) of water is proportionate to the hydraulic conductivity of the soil (k) and the pressure gradient (\delta H) for a given cross-sectional area and length (L). This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>		The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>When applied to soils, Darcy's law states that the flux (q) of water is proportionate to the hydraulic conductivity of the soil (k) and the pressure gradient (\delta H) for a given cross-sectional area and length (L). This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>

Leahtayl: /* Darcy's Law */

2022-03-21T20:00:06Z

Darcy's Law

← Older revision		Revision as of 16:00, 21 March 2022
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	=== Darcy's Law ===		=== Darcy's Law ===

	{{math~~\|''q''{{=}}''K''''&~~delta~~;''H~~/~~L}}~~		<math>\delta</math>

	The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>When applied to soils, Darcy's law states that the flux (q) of water is proportionate to the hydraulic conductivity of the soil (k) and the pressure gradient (\delta H) for a given cross-sectional area and length (L). This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>		The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>When applied to soils, Darcy's law states that the flux (q) of water is proportionate to the hydraulic conductivity of the soil (k) and the pressure gradient (\delta H) for a given cross-sectional area and length (L). This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>

Leahtayl: /* Darcy's Law */

2022-03-21T19:58:23Z

Darcy's Law

← Older revision		Revision as of 15:58, 21 March 2022
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	=== Darcy's Law ===		=== Darcy's Law ===

	<math>q=K(\delta)H/L~~</math>~~		{{math\|''q''{{=}}''K''''δ''H/L}}

	The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>When applied to soils, Darcy's law states that the flux (q) of water is proportionate to the hydraulic conductivity of the soil (k) and the pressure gradient (\delta H) for a given cross-sectional area and length (L). This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>		The movement of liquids through porous media was first described mathematically by Henry Darcy in 1856 and is known as Darcy's law.<ref>Darcy, H. (1856). Les fontaines publiques de la ville de Dijon. Paris: Dalmont.</ref>When applied to soils, Darcy's law states that the flux (q) of water is proportionate to the hydraulic conductivity of the soil (k) and the pressure gradient (\delta H) for a given cross-sectional area and length (L). This equation is commonly used when applying soil biogeochemical and hydraulic models.<ref>Hillel, D., 1998. Environmental soil physics. Academic Press, San Diego, CA.</ref>