Porosity

\phi = rac{V_p}{V_m}

where V_p is the non-solid volume ( Pores and liquid) and V_m is the total volume of material, including the solid and non-solid parts. Both

\phi

and

n

are used to denote porosity.

Porosity is a fraction between 0 and 1, typically ranging from less than 0.01 for solid Granite to more than 0.5 for Peat and Clay , although it may also be represented in percent terms by multiplying the fraction by 100%.

The porosity of a rock, or sedimentary layer, is an important consideration when attempting to evaluate the potential volume of Hydrocarbons it may contain. Sedimentary porosities are a complex function of many factors, including but not limited to: rate of burial, depth of burial, the nature of the connate fluids, the nature of overlying sediments (which may impede fluid expulsion). One commonly used relationship between porosity and depth is given by the Athy (1930) equation:

:

\phi(z) = \phi_0 e^{-kz}

where φ₀ is the surface porosity, k is the compaction coefficient (m^-1) and z is depth (m).

A value for porosity can be calculated from the Bulk Density and Particle Density .

POROSITY AND HYDRAULIC CONDUCTIVITY

Porosity is indirectly related to hydraulic conductivity; for two similar Sandy aquifers, the one a higher porosity will typically have a higher hydraulic conductivity (more open area for the flow of water), but there are many complications to this relationship. Clays, which typically have very low hydraulic conductivity also have very high porosities (due to the structured nature of Clay Minerals ), which means clays can hold a large volume of water per volume of bulk material, but they do not release water very quickly.

SORTING AND POROSITY

Well Sorted (grains of approximately all one size) materials have higher porosity than similarly sized poorly sorted materials (where smaller particles fill the gaps between larger particles). The graphic illustrates how some smaller grains can effectively fill the pores (where all water flow takes place), drastically reducing porosity and hydraulic conductivity, while only being a small fraction of the total volume of the material. For tables of common porosity values for earth materials, see .

POROSITY OF ROCKS

Consolidated rocks (e.g. Sandstone , Shale , Granite or Limestone ) potentially have more complex "dual" porosities, as compared with alluvial sediment. The rock itself may have a certain (low) porosity, and the fractures (cracks and joints), or dissolution features may create a second (higher) porosity. The interaction of these porosities is complex and often makes simple models highly inaccurate.

POROSITY OF SOIL

Porosity of surface soil typically decreases as particle size increases. This is due to soil aggregate formation in finer textured surface soils when subject to Soil Biological processes. Aggregation involves particulate adhesion and higher resistance to compaction. Typical bulk density of sandy soil is between 1.5 and 1.7 g/cm³. This calculates to a porosity between .43 and .36. Typical bulk density of clay soil is between 1.1 and 1.3 g/cm³. This calculates to a porosity between .58 and .51. This seems counterintuitive because clay soils are termed ''heavy'', implying ''lower'' porosity. Heavy apparently refers to a gravitational moisture content effect in combination with terminology that harkens back to the relative force required to pull a Tillage implement through the clayey soil at field moisture content as compared to sand.

Porosity of subsurface soil is lower than in surface soil due to compaction by gravity. Porosity of 0.20 is considered normal for unsorted gravel size material at depths below the Biomantle . Porosity in finer material below the aggregating influence of Pedogenesis can be expected to approximate this value.

Soil porosity is complex. Traditional models regard porosity as continuous. This fails to account for anomalous features and produces only approximate results. Furthermore it cannot help model the influence of environmental factors which affect pore geometry. A number of more complex models have been proposed, including Fractal s, Bubble theory, Cracking theory, Boolean grain process, packed sphere, and numerous other models.

TYPES OF POROSITY

Primary porosity is the main or original porosity system in a Rock or unconfined Alluvial Deposit .

Secondary porosity is a subsequent or separate porosity system in a rock, often enhancing overall porosity of a rock. This can be a result of chemical leeching of minerals or the generation of a fracture system. This can replace the primary porosity or coexist with it (see dual porosity below).

Fracture porosity is porosity associated with a fracture system or faulting. This can create secondary porosity in rocks that otherwise would not be reservoirs for hydrocarbons due to their primary porosity being destroyed (for example due to depth of burial) or of a rock type not normally considered a reservoir (for example igneous intrusions or metasediments).

Vuggy porosity is secondary porosity generated by dissolution of large features (such as macrofossils) in carbonate rocks leaving large holes, Vug s, or even Cave s.

Effective porosity (also called ''open porosity'') refers to the fraction of the total volume in which fluid flow is effectively taking place (this excludes dead-end pores or non-connected cavities). This is very important in solute transport.

Dual porosity refers to the conceptual idea that there are two overlapping reservoirs which interact. In fractured rock aquifers, the rock mass and fractures are often simulated as being two overlapping but distinct bodies. Delayed yield, and leaky aquifer flow solutions are both mathematically similar solutions to that obtained for dual porosity; in all three cases water comes from two mathematically different reservoirs (whether or not they are physically different).

MEASURING POROSITY

There are several ways to estimate the porosity of a given material or mixture of materials, which is called your material matrix.

The Volume/Density method is fast and surprisingly accurate (normally within 2 % of the actual porosity). To do this method you pour your material into a beaker, cylinder or some other container of a known Volume . Weigh your container so you know its empty weight, then pour your material into the container. Tap the side of the container until it has finished settling and measure the volume in the container. Then weigh your container full of this material, so you can subtract the weight of the container to know just the weight of just your material. So now you have both the volume and the Weight of the material. The weight of your material divided by the Density of your material gives you the volume that your material takes up, minus the pore volume. (The assumed density of most rocks, sand, glass, etc. is assumed to be 2.65 g/cm³. If you have a different material, you may look up its density) So, the pore volume is simply equal to the total volume minus the material volume, or more directly (pore volume) = (total volume) - (material volume).

Water Saturation Method is slightly harder to do, but it more accurate and more direct. Again, take a known volume of your material and also a known volume of water. (Make sure the beaker or container is large enough to hold your material as well.) Slowly dump your material into the water and let it saturate as you pour it in. Then seal the beaker (with a piece of Parafilm tape or if you don't have parafilm tape a plastic bag tied around the beaker will do.) and let it sit for a few hours to insure the material is fully saturated. Then remove the unsaturated water from the top of the beaker and measure its volume. The total volume of the water originally in the beaker minus the amount of water not Saturated is the volume of the pore space, or again more directly (pore volume) = (total volume of water) - (unsaturated water).

Water Evaporation Method is the hardest to do, but is also the most accurate. Take a fully saturated, known volume of your material with no excess water on top. Weigh your container with the material and water and then place your container into a heater to dry it out. Drying out your sample may take several days depending on the heat applied and the volume of your sample. Then weigh your dried sample. Since the density of water is 1 g/cm³, the difference of the weights of the saturated versus the dried sample is equal to the volume of the water removed from the sample (assuming you are measuring in grams), which is exactly the pore volume. So once again, (pore volume in cubic centimeters) = (weight of saturated sample in grams) - (weight of dried sample in grams).

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Porosity