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Weathering

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This article is about weathering of rocks and minerals. For weathering of polymers, seePolymer degradationandWeather testing of polymers.For the public health concept, seeWeathering hypothesis.
Anatural archproduced by erosion of differentially weathered rock in Jebel Kharaz (Jordan)
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Weatheringis the deterioration ofrocks,soilsandminerals(as well aswoodand artificial materials) through contact with water,atmospheric gases,sunlight,and biological organisms. It occursin situ(on-site, with little or no movement), and so is distinct fromerosion,which involves the transport of rocks and minerals by agents such aswater,ice,snow,wind,wavesandgravity.

Weathering processes are either physical or chemical. The former involves the breakdown of rocks and soils through such mechanical effects as heat, water, ice and wind. The latter covers reactions to water, atmospheric gases and biologically produced chemicals with rocks and soils. Water is the principal agent behind both kinds,[1]though atmospheric oxygen and carbon dioxide and the activities of biological organisms are also important.[2]Biological chemical weathering is also called biological weathering.[3]

The materials left after the rock breaks down combine with organic material to createsoil.Many of Earth'slandformsand landscapes are the result of weathering, erosion and redeposition. Weathering is a crucial part of therock cycle;sedimentary rock,the product of weathered rock, covers 66% of theEarth's continentsand much of theocean floor.[4]

Physical[edit]

Physical weathering,also calledmechanical weatheringordisaggregation,is the class of processes that causes the disintegration of rocks without chemical change. Physical weathering involves the breakdown of rocks into smaller fragments through processes such as expansion and contraction, mainly due to temperature changes. Two types of physical breakdown are freeze-thaw weathering and thermal fracturing. Pressure release can also cause weathering without temperature change. It is usually much less important than chemical weathering, but can be significant in subarctic or alpine environments.[5]Furthermore, chemical and physical weathering often go hand in hand. For example, cracks extended by physical weathering will increase the surface area exposed to chemical action, thus amplifying the rate of disintegration.[6]

Frost weathering is the most important form of physical weathering. Next in importance is wedging by plant roots, which sometimes enter cracks in rocks and pry them apart. The burrowing of worms or other animals may also help disintegrate rock, as can "plucking" by lichens.[7]

Frost[edit]

A rock inAbisko,Sweden, fractured along existingjointspossibly by frost weathering or thermal stress
Main article:Frost weathering

Frost weatheringis the collective name for those forms of physical weathering that are caused by the formation of ice within rock outcrops. It was long believed that the most important of these isfrost wedging,which results from the expansion of pore water when it freezes. A growing body of theoretical and experimental work suggests that ice segregation, whereby supercooled water migrates to lenses of ice forming within the rock, is the more important mechanism.[8][9]

When water freezes, its volume increases by 9.2%. This expansion can theoretically generate pressures greater than 200 megapascals (29,000 psi), though a more realistic upper limit is 14 megapascals (2,000 psi). This is still much greater than the tensile strength of granite, which is about 4 megapascals (580 psi). This makes frost wedging, in which pore water freezes and its volumetric expansion fractures the enclosing rock, appear to be a plausible mechanism for frost weathering. Ice will simply expand out of a straight open fracture before it can generate significant pressure. Thus, frost wedging can only take place in small tortuous fractures.[5]The rock must also be almost completely saturated with water, or the ice will simply expand into the air spaces in the unsaturated rock without generating much pressure. These conditions are unusual enough that frost wedging is unlikely to be the dominant process of frost weathering.[10]Frost wedging is most effective where there are daily cycles of melting and freezing of water-saturated rock, so it is unlikely to be significant in the tropics, in polar regions or in arid climates.[5]

Ice segregation is a less well characterized mechanism of physical weathering.[8]It takes place because ice grains always have a surface layer, often just a few molecules thick, that resembles liquid water more than solid ice, even at temperatures well below the freezing point. Thispremelted liquid layerhas unusual properties, including a strong tendency to draw in water bycapillary actionfrom warmer parts of the rock. This results in growth of the ice grain that puts considerable pressure on the surrounding rock,[11]up to ten times greater than is likely with frost wedging. This mechanism is most effective in rock whose temperature averages just below the freezing point, −4 to −15 °C (25 to 5 °F). Ice segregation results in growth of ice needles andice lenseswithin fractures in the rock and parallel to the rock surface, which gradually pry the rock apart.[9]

Thermal stress[edit]

Thermal stress weatheringresults from the expansion and contraction of rock due to temperature changes. Thermal stress weathering is most effective when the heated portion of the rock is buttressed by surrounding rock, so that it is free to expand in only one direction.[12]

Thermal stress weathering comprises two main types,thermal shockandthermal fatigue.Thermal shock takes place when the stresses are so great that the rock cracks immediately, but this is uncommon. More typical is thermal fatigue, in which the stresses are not great enough to cause immediate rock failure, but repeated cycles of stress and release gradually weaken the rock.[12]

Thermal stress weathering is an important mechanism indeserts,where there is a largediurnaltemperature range, hot in the day and cold at night.[13]As a result, thermal stress weathering is sometimes calledinsolation weathering,but this is misleading. Thermal stress weathering can be caused by any large change of temperature, and not just intense solar heating. It is likely as important in cold climates as in hot, arid climates.[12]Wildfires can also be a significant cause of rapid thermal stress weathering.[14]

The importance of thermal stress weathering has long been discounted by geologists,[5][9]based on experiments in the early 20th century that seemed to show that its effects were unimportant. These experiments have since been criticized as unrealistic, since the rock samples were small, were polished (which reduces nucleation of fractures), and were not buttressed. These small samples were thus able to expand freely in all directions when heated in experimental ovens, which failed to produce the kinds of stress likely in natural settings. The experiments were also more sensitive to thermal shock than thermal fatigue, but thermal fatigue is likely the more important mechanism in nature.Geomorphologistshave begun to reemphasize the importance of thermal stress weathering, particularly in cold climates.[12]

Pressure release[edit]

See also:Erosion and tectonics
Exfoliated granite sheets in Texas, possibly caused by pressure release

Pressure releaseorunloadingis a form of physical weathering seen when deeply buried rock isexhumed.Intrusive igneous rocks, such asgranite,are formed deep beneath the Earth's surface. They are under tremendouspressurebecause of the overlying rock material. When erosion removes the overlying rock material, these intrusive rocks are exposed and the pressure on them is released. The outer parts of the rocks then tend to expand. The expansion sets up stresses which cause fractures parallel to the rock surface to form. Over time, sheets of rock break away from the exposed rocks along the fractures, a process known asexfoliation.Exfoliation due to pressure release is also known assheeting.[15]

As with thermal weathering, pressure release is most effective in buttressed rock. Here the differential stress directed toward the unbuttressed surface can be as high as 35 megapascals (5,100 psi), easily enough to shatter rock. This mechanism is also responsible forspallingin mines and quarries, and for the formation of joints in rock outcrops.[16]

Retreat of an overlying glacier can also lead to exfoliation due to pressure release. This can be enhanced by other physical wearing mechanisms.[17]

Salt-crystal growth[edit]

TafoniatSalt Point State Park,Sonoma County, California
Main article:Haloclasty
"Salt wedging" redirects here. Not to be confused withSalt wedge (hydrology).

Salt crystallization(also known assalt weathering,salt wedgingorhaloclasty) causes disintegration of rocks whensalinesolutions seep into cracks and joints in the rocks and evaporate, leaving saltcrystalsbehind. As with ice segregation, the surfaces of the salt grains draw in additional dissolved salts through capillary action, causing the growth of salt lenses that exert high pressure on the surrounding rock. Sodium and magnesium salts are the most effective at producing salt weathering. Salt weathering can also take place whenpyritein sedimentary rock is chemically weathered toiron(II) sulfateandgypsum,which then crystallize as salt lenses.[9]

Salt crystallization can take place wherever salts are concentrated by evaporation. It is thus most common inaridclimates where strong heating causes strong evaporation and along coasts.[9]Salt weathering is likely important in the formation oftafoni,a class of cavernous rock weathering structures.[18]

Biomechanical relationship[edit]

Living organisms may contribute to mechanical weathering, as well as chemical weathering (see§ Biological weatheringbelow).Lichensandmossesgrow on essentially bare rock surfaces and create a more humid chemical microenvironment. The attachment of these organisms to the rock surface enhances physical as well as chemical breakdown of the surface microlayer of the rock. Lichens have been observed to pry mineral grains loose from bare shale with theirhyphae(rootlike attachment structures), a process described asplucking,[15]and to pull the fragments into their body, where the fragments then undergo a process of chemical weathering not unlike digestion.[19]On a larger scale, seedlings sprouting in a crevice and plant roots exert physical pressure as well as providing a pathway for water and chemical infiltration.[7]

Chemical[edit]

Comparison of unweathered (left) and weathered (right) limestone

Most rock forms at elevated temperature and pressure, and the minerals making up the rock are often chemically unstable in the relatively cool, wet, and oxidizing conditions typical of the Earth's surface. Chemical weathering takes place when water, oxygen, carbon dioxide, and other chemical substances react with rock to change its composition. These reactions convert some of the originalprimaryminerals in the rock tosecondaryminerals, remove other substances as solutes, and leave the most stable minerals as a chemically unchangedresistate.In effect, chemical weathering changes the original set of minerals in the rock into a new set of minerals that is in closer equilibrium with surface conditions. True equilibrium is rarely reached, because weathering is a slow process, and leaching carries away solutes produced by weathering reactions before they can accumulate to equilibrium levels. This is particularly true in tropical environments.[20]

Water is the principal agent of chemical weathering, converting many primary minerals to clay minerals or hydrated oxides via reactions collectively described ashydrolysis.Oxygen is also important, acting tooxidizemany minerals, as is carbon dioxide, whose weathering reactions are described ascarbonation.[21]

The process of mountain block uplift is important in exposing new rock strata to the atmosphere and moisture, enabling important chemical weathering to occur; significant release occurs of Ca2+and other ions into surface waters.[22]

Dissolution[edit]

Limestonecore samplesat different stages of chemical weathering, from very high at shallow depths (bottom) to very low at greater depths (top). Slightly weathered limestone shows brownish stains, while highly weathered limestone loses much of its carbonate mineral content, leaving behind clay. Limestone drill core taken from the carbonate West Congolian deposit inKimpese,Democratic Republic of Congo.

Dissolution (also calledsimple solutionorcongruent dissolution) is the process in which a mineral dissolves completely without producing any new solid substance.[23]Rainwater easily dissolves soluble minerals, such ashaliteorgypsum,but can also dissolve highly resistant minerals such asquartz,given sufficient time.[24]Water breaks the bonds between atoms in the crystal:[25]

Hydrolysis of a silica mineral

The overall reaction for dissolution of quartz is

SiO2+ 2 H2O → H4SiO4

The dissolved quartz takes the form ofsilicic acid.

A particularly important form of dissolution is carbonate dissolution, in which atmosphericcarbon dioxideenhances solution weathering. Carbonate dissolution affects rocks containingcalcium carbonate,such aslimestoneandchalk.It takes place when rainwater combines with carbon dioxide to formcarbonic acid,aweak acid,which dissolves calcium carbonate (limestone) and forms solublecalcium bicarbonate.Despite a slowerreaction kinetics,this process is thermodynamically favored at low temperature, because colder water holds more dissolved carbon dioxide gas (due to the retrogradesolubilityof gases). Carbonate dissolution is therefore an important feature of glacial weathering.[26]

Carbonate dissolution involves the following steps:

CO2+ H2O → H2CO3
carbon dioxide + water → carbonic acid
H2CO3+ CaCO3→ Ca(HCO3)2
carbonic acid + calcium carbonate → calcium bicarbonate

Carbonate dissolution on the surface of well-jointed limestone produces a dissectedlimestone pavement.This process is most effective along the joints, widening and deepening them.[27]

In unpolluted environments, thepHof rainwater due to dissolved carbon dioxide is around 5.6.Acid rainoccurs when gases such as sulfur dioxide and nitrogen oxides are present in the atmosphere. These oxides react in the rain water to produce stronger acids and can lower the pH to 4.5 or even 3.0.Sulfur dioxide,SO2,comes from volcanic eruptions or from fossil fuels, and can becomesulfuric acidwithin rainwater, which can cause solution weathering to the rocks on which it falls.[28]

Hydrolysis and carbonation[edit]

Olivineweathering toiddingsitewithin amantlexenolith

Hydrolysis(also calledincongruent dissolution) is a form of chemical weathering in which only part of a mineral is taken into solution. The rest of the mineral is transformed into a new solid material, such as aclay mineral.[29]For example,forsterite(magnesiumolivine) is hydrolyzed into solidbruciteand dissolved silicic acid:

Mg2SiO4+ 4 H2O ⇌ 2 Mg(OH)2+ H4SiO4
forsterite + water ⇌ brucite + silicic acid

Most hydrolysis during weathering of minerals isacid hydrolysis,in which protons (hydrogen ions), which are present in acidic water, attack chemical bonds in mineral crystals.[30]The bonds between different cations and oxygen ions in minerals differ in strength, and the weakest will be attacked first. The result is that minerals in igneous rock weather in roughly the same order in which they were originally formed (Bowen's Reaction Series).[31]Relative bond strength is shown in the following table:[25]

Bond Relative strength
Si–O 2.4
Ti–O 1.8
Al–O 1.65
Fe+3–O 1.4
Mg–O 0.9
Fe+2–O 0.85
Mn–O 0.8
Ca–O 0.7
Na–O 0.35
K–O 0.25

This table is only a rough guide to order of weathering. Some minerals, such asillite,are unusually stable, while silica is unusually unstable given the strength of thesilicon–oxygen bond.[32]

Carbon dioxide that dissolves in water to form carbonic acid is the most important source of protons, but organic acids are also important natural sources of acidity.[33]Acid hydrolysis from dissolved carbon dioxide is sometimes described ascarbonation,and can result in weathering of the primary minerals to secondary carbonate minerals.[34]For example, weathering of forsterite can producemagnesiteinstead of brucite via the reaction:

Mg2SiO4+ 2 CO2+ 2 H2O ⇌ 2 MgCO3+ H4SiO4
forsterite + carbon dioxide + water ⇌ magnesite + silicic acid in solution

Carbonic acidis consumed bysilicateweathering, resulting in morealkalinesolutions because of thebicarbonate.This is an important reaction in controlling the amount of CO2in the atmosphere and can affect climate.[35]

Aluminosilicatescontaining highly soluble cations, such as sodium or potassium ions, will release the cations as dissolved bicarbonates during acid hydrolysis:

2 KAlSi3O8+ 2 H2CO3+ 9 H2O ⇌ Al2Si2O5(OH)4+ 4 H4SiO4+ 2 K++ 2 HCO3−
orthoclase(aluminosilicate feldspar) + carbonic acid + water ⇌kaolinite(a clay mineral) + silicic acid in solution + potassium and bicarbonate ions in solution

Oxidation[edit]

Apyritecube has dissolved away from host rock, leavinggoldparticles behind.
Oxidizedpyritecubes

Within the weathering environment, chemicaloxidationof a variety of metals occurs. The most commonly observed is the oxidation of Fe2+(iron) by oxygen and water to form Fe3+oxides and hydroxides such asgoethite,limonite,andhematite.This gives the affected rocks a reddish-brown coloration on the surface which crumbles easily and weakens the rock. Many other metallic ores and minerals oxidize and hydrate to produce colored deposits, as does sulfur during the weathering ofsulfide mineralssuch aschalcopyritesor CuFeS2oxidizing tocopper hydroxideandiron oxides.[36]

Hydration[edit]

Mineral hydrationis a form of chemical weathering that involves the rigid attachment of water molecules or H+ and OH- ions to the atoms and molecules of a mineral. No significant dissolution takes place. For example,iron oxidesare converted toiron hydroxidesand the hydration ofanhydriteformsgypsum.[37]

Bulk hydration of minerals is secondary in importance to dissolution, hydrolysis, and oxidation,[36]but hydration of the crystal surface is the crucial first step in hydrolysis. A fresh surface of a mineral crystal exposes ions whose electrical charge attracts water molecules. Some of these molecules break into H+ that bonds to exposed anions (usually oxygen) and OH- that bonds to exposed cations. This further disrupts the surface, making it susceptible to various hydrolysis reactions. Additional protons replace cations exposed on the surface, freeing the cations as solutes. As cations are removed, silicon-oxygen and silicon-aluminium bonds become more susceptible to hydrolysis, freeing silicic acid and aluminium hydroxides to be leached away or to form clay minerals.[32][38]Laboratory experiments show that weathering of feldspar crystals begins at dislocations or other defects on the surface of the crystal, and that the weathering layer is only a few atoms thick. Diffusion within the mineral grain does not appear to be significant.[39]

A freshly broken rock shows differential chemical weathering (probably mostly oxidation) progressing inward. This piece ofsandstonewas found inglacial driftnearAngelica, New York.

Biological[edit]

Mineral weathering can also be initiated or accelerated by soil microorganisms. Soil organisms make up about 10 mg/cm3of typical soils, and laboratory experiments have demonstrated thatalbiteandmuscoviteweather twice as fast in live versus sterile soil.Lichenson rocks are among the most effective biological agents of chemical weathering.[33]For example, an experimental study on hornblende granite in New Jersey, US, demonstrated a 3x – 4x increase in weathering rate under lichen covered surfaces compared to recently exposed bare rock surfaces.[40]

Biological weathering ofbasaltbylichen,La Palma

The most common forms of biological weathering result from the release ofchelatingcompounds (such as certain organic acids andsiderophores) and of carbon dioxide and organic acids by plants. Roots can build up the carbon dioxide level to 30% of all soil gases, aided by adsorption of CO2on clay minerals and the very slow diffusion rate of CO2out of the soil.[41]The CO2and organic acids help break downaluminium- andiron-containing compounds in the soils beneath them. Roots have a negative electrical charge balanced by protons in the soil next to the roots, and these can be exchanged for essential nutrient cations such as potassium.[42]Decayingremains of dead plants in soil may form organic acids which, when dissolved in water, cause chemical weathering.[43]Chelating compounds, mostly low molecular weight organic acids, are capable of removing metal ions from bare rock surfaces, with aluminium and silicon being particularly susceptible.[44]The ability to break down bare rock allows lichens to be among the first colonizers of dry land.[45]The accumulation of chelating compounds can easily affect surrounding rocks and soils, and may lead topodsolisationof soils.[46][47]

The symbioticmycorrhizal fungiassociated with tree root systems can release inorganic nutrients from minerals such as apatite or biotite and transfer these nutrients to the trees, thus contributing to tree nutrition.[48]It was also recently evidenced that bacterial communities can impact mineral stability leading to the release of inorganic nutrients.[49]A large range of bacterial strains or communities from diverse genera have been reported to be able to colonize mineral surfaces or to weather minerals, and for some of them a plant growth promoting effect has been demonstrated.[50]The demonstrated or hypothesised mechanisms used by bacteria to weather minerals include several oxidoreduction and dissolution reactions as well as the production of weathering agents, such as protons, organic acids and chelating molecules.

Ocean floor[edit]

Weathering of basaltic oceanic crust differs in important respects from weathering in the atmosphere. Weathering is relatively slow, with basalt becoming less dense, at a rate of about 15% per 100 million years. The basalt becomes hydrated, and is enriched in total and ferric iron, magnesium, and sodium at the expense of silica, titanium, aluminum, ferrous iron, and calcium.[51]

Buildings[edit]

Concrete damaged byacid rain

Buildings made of any stone, brick or concrete are susceptible to the same weathering agents as any exposed rock surface. Alsostatues,monuments and ornamental stonework can be badly damaged by natural weathering processes. This is accelerated in areas severely affected byacid rain.[52]

Accelerated building weathering may be a threat to the environment and occupant safety. Design strategies can moderate the impact of environmental effects, such as using of pressure-moderated rain screening, ensuring that the HVAC system is able to effectively control humidity accumulation and selecting concrete mixes with reduced water content to minimize the impact of freeze-thaw cycles.[53]

Soil[edit]

Granitic rock, which is the most abundant crystalline rock exposed at the Earth's surface, begins weathering with destruction ofhornblende.Biotitethen weathers tovermiculite,and finallyoligoclaseandmicroclineare destroyed. All are converted into a mixture of clay minerals and iron oxides.[31]The resulting soil is depleted in calcium, sodium, and ferrous iron compared with the bedrock, and magnesium is reduced by 40% and silicon by 15%. At the same time, the soil is enriched in aluminium and potassium, by at least 50%; by titanium, whose abundance triples; and by ferric iron, whose abundance increases by an order of magnitude compared with the bedrock.[54]

Basaltic rock is more easily weathered than granitic rock, due to its formation at higher temperatures and drier conditions. The fine grain size and presence of volcanic glass also hasten weathering. In tropical settings, it rapidly weathers to clay minerals, aluminium hydroxides, and titanium-enriched iron oxides. Because most basalt is relatively poor in potassium, the basalt weathers directly to potassium-poormontmorillonite,then tokaolinite.Where leaching is continuous and intense, as in rain forests, the final weathering product isbauxite,the principal ore of aluminium. Where rainfall is intense but seasonal, as in monsoon climates, the final weathering product is iron- and titanium-richlaterite.[55]Conversion of kaolinite to bauxite occurs only with intense leaching, as ordinary river water is in equilibrium with kaolinite.[56]

Soil formationrequires between 100 and 1,000 years, a very brief interval in geologic time. As a result, someformationsshow numerouspaleosol(fossil soil) beds. For example, theWillwood Formationof Wyoming contains over 1,000 paleosol layers in a 770 meters (2,530 ft) section representing 3.5 million years of geologic time. Paleosols have been identified in formations as old asArchean(over 2.5 billion years in age). They are difficult to recognize in the geologic record.[57]Indications that a sedimentary bed is a paleosol include a gradational lower boundary and sharp upper boundary, the presence of much clay, poor sorting with few sedimentary structures, rip-up clasts in overlying beds, and desiccation cracks containing material from higher beds.[58]

The degree of weathering of a soil can be expressed as thechemical index of alteration,defined as100 Al2O3/(Al2O3+ CaO + Na2O + K2O).This varies from 47 for unweathered upper crust rock to 100 for fully weathered material.[59]

Wood, paint and plastic[edit]

Wood can be physically and chemically weathered by hydrolysis and other processes relevant to minerals and is highly susceptible toultravioletradiation from sunlight. This induces photochemical reactions that degrade its surface.[60]These also significantly weather paint[61]and plastics.[62]

Gallery[edit]

See also[edit]

References[edit]

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External links[edit]

The WikibookHistorical Geologyhas a page on the topic of:Mechanical weathering and erosion
The WikibookHistorical Geologyhas a page on the topic of:Chemical weathering
Look upweatheringin Wiktionary, the free dictionary.
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