Weathering

This article is about weathering of rocks and minerals. For weathering of polymers, see Polymer degradation and Weather testing of polymers.
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Weathering is the deterioration of rocks, soils and minerals as well as wood and artificial materials through contact with water, atmospheric gases, and biological organisms. Weathering occurs in situ (on site, with little or no movement), and should not be confused with erosion, which involves the transport of rocks and minerals by agents such as water, ice, snow, wind, waves and gravity.

Weathering processes are divided into physical and chemical weathering. Physical weathering involves the breakdown of rocks and soils through the mechanical effects of heat, water, ice, or other agents. Chemical weathering involves the chemical reaction of water, atmospheric gases, and biologically produced chemicals with rocks and soils. Water is the principal agent behind both physical and chemical weathering,[1] though atmospheric oxygen and carbon dioxide and the activities of biological organisms are also important.[2] Chemical weathering by biological action is also known as biological weathering.[3]

The materials left over after the rock breaks down combine with organic material to create soil. Many of Earth's landforms and landscapes are the result of weathering processes combined with erosion and re-deposition. Weathering is a crucial part of the rock cycle, and sedimentary rock, formed from the weathering products of older rock, covers 66% of the Earth's continents and much of its ocean floor.[4]

Contents
Physical weathering
Chemical weathering
Weathering on the ocean floor
Building weathering
Properties of well-weathered soils
Weathering of non-geological materials
Gallery
See also
References
Other links

Physical weathering

Physical weathering, also called mechanical weathering or disaggregation, is the class of processes that causes the disintegration of rocks without chemical 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 weathering

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Main article: Frost weathering

Frost weathering is 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 is frost wedging, which results from the expansion of pore water when it freezes. However, a growing body of theoretical and experimental work suggests that ice segregation, in which 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 that 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. However, 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 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. This premelted liquid layer has unusual properties, including a strong tendency to draw in water by capillary action from 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 and ice lenses within fractures in the rock, and parallel to the rock surface, that gradually pry the rock apart.[9]

Thermal stress

Thermal stress weathering results 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 shock and thermal 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 in deserts, where there is a large diurnal temperature range, hot in the day and cold at night.[13] As a result, thermal stress weathering is sometimes called insolation 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. Geomorphologists have begun to reemphasize the importance of thermal stress weathering, particularly in cold climates.[12]

Pressure release

See also: Erosion and tectonics
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Pressure release or unloading is a form of physical weathering seen when deeply buried rock is exhumed. Intrusive igneous rocks, such as granite, are formed deep beneath the Earth's surface. They are under tremendous pressure because 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 as exfoliation. Exfoliation due to pressure release is also known as "sheeting".[15]

As with thermal weathering, pressure release is most effective in buttressed rock. Here the differential stress directed towards the unbuttressed surface can be as high as 35 megapascals (5,100 psi), easily enough to shatter rock. This mechanism is also responsible for spalling in 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

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Main article: Haloclasty
"Salt wedging" redirects here. It is not to be confused with Salt wedge (hydrology).

Salt crystallization (also known as salt weathering, salt wedging or haloclasty) causes disintegration of rocks when saline solutions seep into cracks and joints in the rocks and evaporate, leaving salt crystals behind. 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 when pyrite in sedimentary rock is chemically weathered to iron(II) sulfate and gypsum, which then crystallize as salt lenses.[9]

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

Biological effects on mechanical weathering

Living organisms may contribute to mechanical weathering, as well as chemical weathering (see § Biological weathering below). Lichens and mosses grow 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 their hyphae (rootlike attachment structures), a process described as plucking, [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 weathering

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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 original primary minerals in the rock to secondary minerals, remove other substances as solutes, and leave the most stable minerals as a chemically unchanged resistate. 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. However, 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 as hydrolysis. Oxygen is also important, acting to oxidize many minerals, as is carbon dioxide, whose weathering reactions are described as carbonation.[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

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Dissolution (also called simple solution or congruent dissolution) is the process in which a mineral dissolves completely without producing any new solid substance.[23] Rainwater easily dissolves soluble minerals, such as halite or gypsum, but can also dissolve highly resistant minerals such as quartz, given sufficient time.[24] Water breaks the bonds between atoms in the crystal:[25]

The overall reaction for dissolution of quartz is

The dissolved quartz takes the form of silicic acid.

A particularly important form of dissolution is carbonate dissolution, in which atmospheric carbon dioxide enhances solution weathering. Carbonate dissolution affects rocks containing calcium carbonate, such as limestone and chalk. It takes place when rainwater combines with carbon dioxide to form carbonic acid, a weak acid, which dissolves calcium carbonate (limestone) and forms soluble calcium bicarbonate. Despite a slower reaction kinetics, this process is thermodynamically favored at low temperature, because colder water holds more dissolved carbon dioxide gas (due to the retrograde solubility of gases). Carbonate dissolution is therefore an important feature of glacial weathering.[26]

Carbonate dissolution involves the following steps:

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

In unpolluted environments, the pH of rainwater due to dissolved carbon dioxide is around 5.6. Acid rain occurs 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, can become sulfuric acid within rainwater, which can cause solution weathering to the rocks on which it falls.[28]

Hydrolysis and carbonation

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Hydrolysis (also called incongruent 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 a clay mineral.[29] For example, forsterite (magnesium olivine) is hydrolyzed into solid brucite and dissolved silicic acid:

Most hydrolysis during weathering of minerals is acid 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]

This table is only a rough guide to order of weathering. Some minerals, such as illite, are unusually stable, while silica is unusually unstable given the strength of the silicon-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 as carbonation, and can result in weathering of the primary minerals to secondary carbonate minerals.[34] For example, weathering of forsterite can produce magnesite instead of brucite via the reaction:

Carbonic acid is consumed by silicate weathering, resulting in more alkaline solutions because of the bicarbonate. This is an important reaction in controlling the amount of CO2 in the atmosphere and can affect climate.[35]

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

Oxidation

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Within the weathering environment, chemical oxidation of 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 as goethite, limonite, and hematite. 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 of sulfide minerals such as chalcopyrites or CuFeS2 oxidizing to copper hydroxide and iron oxides.[36]

Hydration

Mineral hydration is 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 oxides are converted to iron hydroxides and the hydration of anhydrite forms gypsum.[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 in 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]

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Biological weathering

Mineral weathering can also be initiated or accelerated by soil microorganisms. Soil organisms make up about 10 mg/cm3 of typical soils, and laboratory experiments have demonstrated that albite and muscovite weather twice as fast in live versus sterile soil. Lichens on rocks are among the most effective biological agents of chemical weathering.[33] For example, an experimental study on hornblende granite in New Jersey, USA, demonstrated a 3x – 4x increase in weathering rate under lichen covered surfaces compared to recently exposed bare rock surfaces.[40]

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The most common forms of biological weathering result from the release of chelating compounds (such as certain organic acids and siderophores) 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 CO2 on clay minerals and the very slow diffusion rate of CO2 out of the soil.[41] The CO2 and organic acids help break down aluminium- and iron-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]Decaying remains 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 to podsolisation of soils.[46][47]

The symbiotic mycorrhizal fungi associated 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.

Weathering on the ocean floor

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]

Building weathering

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

Properties of well-weathered soils

Granitic rock, which is the most abundant crystalline rock exposed at the Earth's surface, begins weathering with destruction of hornblende. Biotite then weathers to vermiculite, and finally oligoclase and microcline are 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 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-poor montmorillonite, then to kaolinite. Where leaching is continuous and intense, as in rain forests, the final weathering product is bauxite, the principal ore of aluminium. Where rainfall is intense but seasonal, as in monsoon climates, the final weathering product is iron- and titanium-rich laterite. [55] Conversion of kaolinite to bauxite occurs only with intense leaching, as ordinary river water is in equilibrium with kaolinite.[56]

Soil formation requires between 100 and 1000 years, a very brief interval in geologic time. As a result, some formations show numerous paleosol (fossil soil) beds. For example, the Willwood Formation of Wyoming contains over 1000 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 as Archean (over 2.5 billion years in age). However, paleosols 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 the chemical index of alteration, defined as 100 Al2O3/(Al2O3 + CaO + Na2O + K2O). This varies from 47 for unweathered upper crust rock to 100 for fully weathered material.[59]

Weathering of non-geological materials

Wood can be physically and chemically weathered by hydrolysis and other processes relevant to minerals, but in addition, wood is highly susceptible to weathering induced by ultraviolet radiation from sunlight. This induces photochemical reactions that degrade the wood surface.[60] Photochemical reactions are also significant in the weathering of paint[61] and plastics.[62]

See also

References

  1. Leeder, M. R. (2011). Sedimentology and sedimentary basins : from turbulence to tectonics (2nd ed.). Chichester, West Sussex, UK: Wiley-Blackwell. p. 4. ISBN9781405177832 .
  2. Blatt, Harvey; Middleton, Gerard; Murray, Raymond (1980). Origin of sedimentary rocks (2d ed.). Englewood Cliffs, N.J.: Prentice-Hall. pp. 245–246. ISBN0136427103 .
  3. Gore, Pamela J. W. "Weathering". Georgia Perimeter College. Archived from the original on 2013-05-10.
  4. Blatt, Harvey; Tracy, Robert J. (1996). Petrology : igneous, sedimentary, and metamorphic (2nd ed.). New York: W.H. Freeman. p. 217. ISBN0716724383 .
  5. Blatt, Middleton & Murray 1980, p. 247.
  6. Leeder 2011, p. 3.
  7. Blatt, Middleton & Murray 1980, pp. 249–250.
  8. Murton, J. B.; Peterson, R.; Ozouf, J.-C. (17 November 2006). "Bedrock Fracture by Ice Segregation in Cold Regions". Science. 314 (5802): 1127–1129. Bibcode:2006Sci...314.1127M. doi:10.1126/science.1132127. PMID17110573 . S2CID37639112 .
  9. Leeder 2011, p. 18.
  10. Matsuoka, Norikazu; Murton, Julian (April 2008). "Frost weathering: recent advances and future directions". Permafrost and Periglacial Processes. 19 (2): 195–210. doi:10.1002/ppp.620.
  11. Dash, J. G.; Rempel, A. W.; Wettlaufer, J. S. (12 July 2006). "The physics of premelted ice and its geophysical consequences". Reviews of Modern Physics. 78 (3): 695–741. Bibcode:2006RvMP...78..695D. doi:10.1103/RevModPhys.78.695.
  12. Hall, Kevin (1999), "The role of thermal stress fatigue in the breakdown of rock in cold regions", Geomorphology, 31 (1–4): 47–63, Bibcode:1999Geomo..31...47H, doi:10.1016/S0169-555X(99)00072-0
  13. Paradise, T. R. (2005). "Petra revisited: An examination of sandstone weathering research in Petra, Jordan". Special Paper 390: Stone Decay in the Architectural Environment. 390. pp. 39–49. doi:10.1130/0-8137-2390-6.39. ISBN0-8137-2390-6 .
  14. Shtober-Zisu, Nurit; Wittenberg, Lea (March 2021). "Long-term effects of wildfire on rock weathering and soil stoniness in the Mediterranean landscapes". Science of the Total Environment. 762: 143125. Bibcode:2021ScTEn.762n3125S. doi:10.1016/j.scitotenv.2020.143125. PMID33172645 . S2CID225117000 .
  15. Blatt, Middleton & Murray 1980, p. 249.
  16. Leeder 2011, p. 19.
  17. Harland, W. B. (1957). "Exfoliation Joints and Ice Action". Journal of Glaciology. 3 (21): 8–10. doi:10.3189/S002214300002462X.
  18. Turkington, Alice V.; Paradise, Thomas R. (April 2005). "Sandstone weathering: a century of research and innovation". Geomorphology. 67 (1–2): 229–253. Bibcode:2005Geomo..67..229T. doi:10.1016/j.geomorph.2004.09.028.
  19. Fry, E. Jennie (July 1927). "The Mechanical Action of Crustaceous Lichens on Substrata of Shale, Schist, Gneiss, Limestone, and Obsidian". Annals of Botany. os-41 (3): 437–460. doi:10.1093/oxfordjournals.aob.a090084.
  20. Blatt, Middleton & Murray 1980, pp. 245–246.
  21. Blatt, Middleton & Murray 1980, pp. 246.
  22. Hogan, C. Michael (2010) "Calcium", in A. Jorgenson and C. Cleveland (eds.) Encyclopedia of Earth, National Council for Science and the Environment, Washington DC
  23. Birkeland, Peter W. (1999). Soils and geomorphology (3rd ed.). New York: Oxford University Press. p. 59. ISBN978-0195078862 .
  24. Boggs, Sam (2006). Principles of sedimentology and stratigraphy (4th ed.). Upper Saddle River, N.J.: Pearson Prentice Hall. p. 7. ISBN0131547283 .
  25. Nicholls, G. D. (1963). "Environmental Studies in Sedimentary Geochemistry". Science Progress (1933- ). 51 (201): 12–31. JSTOR43418626 .
  26. Plan, Lukas (June 2005). "Factors controlling carbonate dissolution rates quantified in a field test in the Austrian alps". Geomorphology. 68 (3–4): 201–212. Bibcode:2005Geomo..68..201P. doi:10.1016/j.geomorph.2004.11.014.
  27. Anon. "Geology and geomorphology". Limestone Pavement Conservation. UK and Ireland Biodiversity Action Plan Steering Group. Archived from the original on 7 August 2011. Retrieved 30 May 2011.
  28. Charlson, R. J.; Rodhe, H. (February 1982). "Factors controlling the acidity of natural rainwater". Nature. 295 (5851): 683–685. Bibcode:1982Natur.295..683C. doi:10.1038/295683a0. S2CID4368102 .
  29. Boggs 2006, pp. 7–8.
  30. Leeder 2011, p. 4.
  31. Blatt, Middleton & Murray 1980, p. 252.
  32. Blatt, Middleton & Murray 1980, p. 258.
  33. Blatt, Middleton & Murray 1980, p. 250.
  34. Thornbury, William D. (1969). Principles of geomorphology (2d ed.). New York: Wiley. pp. 303–344. ISBN0471861979 .
  35. Berner, Robert A. (31 December 1995). White, Arthur F; Brantley, Susan L (eds.). "Chapter 13. CHEMICAL WEATHERING AND ITS EFFECT ON ATMOSPHERIC CO2 AND CLIMATE". Chemical Weathering Rates of Silicate Minerals: 565–584. doi:10.1515/9781501509650-015. ISBN9781501509650 .
  36. Boggs 2006, p. 9.
  37. Boggs 1996, p. 8. sfn error: no target: CITEREFBoggs1996 (help)
  38. Leeder 2011, pp. 653–655.
  39. Berner, Robert A.; Holdren, George R. (1 June 1977). "Mechanism of feldspar weathering: Some observational evidence". Geology. 5 (6): 369–372. Bibcode:1977Geo.....5..369B. doi:10.1130/0091-7613(1977)5<369:MOFWSO>2.0.CO;2.
  40. Zambell, C.B.; Adams, J.M.; Gorring, M.L.; Schwartzman, D.W. (2012). "Effect of lichen colonization on chemical weathering of hornblende granite as estimated by aqueous elemental flux". Chemical Geology. 291: 166–174. Bibcode:2012ChGeo.291..166Z. doi:10.1016/j.chemgeo.2011.10.009.
  41. Fripiat, J. J. (1974). "Interlamellar Adsorption of Carbon Dioxide by Smectites". Clays and Clay Minerals. 22 (1): 23–30. Bibcode:1974CCM....22...23F. doi:10.1346/CCMN.1974.0220105. S2CID53610319 .
  42. Blatt, Middleton & Murray 1980, pp. 251.
  43. Chapin III, F. Stuart; Pamela A. Matson; Harold A. Mooney (2002). Principles of terrestrial ecosystem ecology ([Nachdr.] ed.). New York: Springer. pp. 54–55. ISBN9780387954431 .
  44. Blatt & Tracy 1996, p. 233.
  45. Blatt, Middleton & Murray 1980, pp. 250–251.
  46. Lundström, U. S.; van Breemen, N.; Bain, D. C.; van Hees, P. A. W.; Giesler, R.; Gustafsson, J. P.; Ilvesniemi, H.; Karltun, E.; Melkerud, P. -A.; Olsson, M.; Riise, G. (2000-02-01). "Advances in understanding the podzolization process resulting from a multidisciplinary study of three coniferous forest soils in the Nordic Countries". Geoderma. 94 (2): 335–353. Bibcode:2000Geode..94..335L. doi:10.1016/S0016-7061(99)00077-4. ISSN0016-7061 .
  47. Waugh, David (2000). Geography : an integrated approach (3rd ed.). Gloucester, U.K.: Nelson Thornes. p. 272. ISBN9780174447061 .
  48. Landeweert, R.; Hoffland, E.; Finlay, R.D.; Kuyper, T.W.; van Breemen, N. (2001). "Linking plants to rocks: Ectomycorrhizal fungi mobilize nutrients from minerals". Trends in Ecology & Evolution. 16 (5): 248–254. doi:10.1016/S0169-5347(01)02122-X. PMID11301154 .
  49. Calvaruso, C.; Turpault, M.-P.; Frey-Klett, P. (2006). "Root-Associated Bacteria Contribute to Mineral Weathering and to Mineral Nutrition in Trees: A Budgeting Analysis". Applied and Environmental Microbiology. 72 (2): 1258–66. Bibcode:2006ApEnM..72.1258C. doi:10.1128/AEM.72.2.1258-1266.2006. PMC1392890 . PMID16461674 .
  50. Uroz, S.; Calvaruso, C.; Turpault, M.-P.; Frey-Klett, P. (2009). "Mineral weathering by bacteria: ecology, actors and mechanisms". Trends Microbiol. 17 (8): 378–87. doi:10.1016/j.tim.2009.05.004. PMID19660952 .
  51. Blatt, Middleton & Murray 1960, p. 256. sfn error: no target: CITEREFBlattMiddletonMurray1960 (help)
  52. Schaffer, R. J. (2016). Weathering of Natural Building Stones. Taylor and Francis. ISBN9781317742524 .
  53. "Design Discussion Primer - Chronic Stressors"(PDF) . BC Housing. Retrieved 13 July 2021.
  54. Blatt, Middleton & Murray, p. 253. sfn error: no target: CITEREFBlattMiddletonMurray (help)
  55. Blatt, Middleton & Murray, p. 254. sfn error: no target: CITEREFBlattMiddletonMurray (help)
  56. Blatt, Middleton & Murray, p. 262. sfn error: no target: CITEREFBlattMiddletonMurray (help)
  57. Blatt, Middleton & Murray, p. 233. sfn error: no target: CITEREFBlattMiddletonMurray (help)
  58. Blatt & Tracy 1996, p. 236.
  59. Leeder, 2011 & 11. sfn error: no target: CITEREFLeeder201111 (help)
  60. Williams, R.S. (2005). "7". In Rowell, Roger M. (ed.). Handbook of wood chemistry and wood composites. Boca Raton: Taylor & Francis. pp. 139–185. ISBN9780203492437 .
  61. Nichols, M.E.; Gerlock, J.L.; Smith, C.A.; Darr, C.A. (August 1999). "The effects of weathering on the mechanical performance of automotive paint systems". Progress in Organic Coatings. 35 (1–4): 153–159. doi:10.1016/S0300-9440(98)00060-5.
  62. Weathering of plastics : testing to mirror real life performance. [Brookfield, Conn.]: Society of Plastics Engineers. 1999. ISBN9781884207754 .