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Torcal de Antequera nature reserve of Málaga, Spain
Calcium carbonate: inorganic crystalline calcite or organic calcareous material

Limestone (

crystal forms of CaCO3. Limestone forms when these minerals precipitate out of water containing dissolved calcium. This can take place through both biological and nonbiological processes, though biological processes, such as the accumulation of corals and shells in the sea, have likely been more important for the last 540 million years.[1][2] Limestone often contains fossils which provide scientists with information on ancient environments and on the evolution of life.[3]

About 20% to 25% of sedimentary rock is carbonate rock, and most of this is limestone.

continental shelves or platforms, though smaller amounts were formed in many other environments. Much dolomite is secondary dolomite, formed by chemical alteration of limestone.[6][7] Limestone is exposed over large regions of the Earth's surface, and because limestone is slightly soluble in rainwater, these exposures often are eroded to become karst landscapes. Most cave
systems are found in limestone bedrock.

Limestone has numerous uses: as a chemical

rock gardens. Limestone formations contain about 30% of the world's petroleum reservoirs.[3]


This limestone deposit in the karst of Dinaric Alps near Sinj, Croatia, was formed in the Eocene.

Limestone is composed mostly of the

crystal forms of calcium carbonate (CaCO3). Dolomite, CaMg(CO3)2, is an uncommon mineral in limestone, and siderite or other carbonate minerals are rare. However, the calcite in limestone often contains a few percent of magnesium. Calcite in limestone is divided into low-magnesium and high-magnesium calcite, with the dividing line placed at a composition of 4% magnesium. High-magnesium calcite retains the calcite mineral structure, which is distinct from dolomite. Aragonite does not usually contain significant magnesium.[8] Most limestone is otherwise chemically fairly pure, with clastic sediments (mainly fine-grained quartz and clay minerals) making up less than 5%[9] to 10%[10] of the composition. Organic matter typically makes up around 0.2% of a limestone and rarely exceeds 1%.[11]

Limestone often contains variable amounts of

radiolarians).[12] Fossils are also common in limestone.[3]

Limestone is commonly white to gray in color. Limestone that is unusually rich in organic matter can be almost black in color, while traces of

MPa.[13] For comparison, concrete typically has a crushing strength of about 40 MPa.[14]

Although limestones show little variability in mineral composition, they show great diversity in texture.[15] However, most limestone consists of sand-sized grains in a carbonate mud matrix. Because limestones are often of biological origin and are usually composed of sediment that is deposited close to where it formed, classification of limestone is usually based on its grain type and mud content.[9]


Ooids from a beach on Joulter's Cay, The Bahamas
Ooids in limestone of the Carmel Formation (Middle Jurassic) of southwestern Utah.
Thin-section view of a Middle Jurassic limestone in southern Utah, U.S. The round grains are ooids; the largest is 1.2 mm (0.05 in) in diameter. This limestone is an oosparite.

Most grains in limestone are skeletal fragments of marine organisms such as

peloids, and limeclasts (intraclasts and extraclasts [ca]).[17]

Skeletal grains have a composition reflecting the organisms that produced them and the environment in which they were produced.

stromatoporoids, corals, and tube worms. The skeletal grains also reflect specific geological periods and environments. For example, coral grains are more common in high-energy environments (characterized by strong currents and turbulence) while bryozoan grains are more common in low-energy environments (characterized by quiet water).[19]

Ooids (sometimes called ooliths) are sand-sized grains (less than 2mm in diameter) consisting of one or more layers of calcite or aragonite around a central quartz grain or carbonate mineral fragment. These likely form by direct precipitation of calcium carbonate onto the ooid. Pisoliths are similar to ooids, but they are larger than 2 mm in diameter and tend to be more irregular in shape. Limestone composed mostly of ooids is called an oolite or sometimes an oolitic limestone. Ooids form in high-energy environments, such as the Bahama platform, and oolites typically show crossbedding and other features associated with deposition in strong currents.[20][21]

Oncoliths resemble ooids but show a radial rather than layered internal structure, indicating that they were formed by algae in a normal marine environment.[20]

Peloids are structureless grains of microcrystalline carbonate likely produced by a variety of processes.

endolithic (boring) algae[23] or other microorganisms[24] or through breakdown of mollusc shells.[25] They are difficult to see in a limestone sample except in thin section and are less common in ancient limestones, possibly because compaction of carbonate sediments disrupts them.[23]

Limeclasts are fragments of existing limestone or partially lithified carbonate sediments. Intraclasts are limeclasts that originate close to where they are deposited in limestone, while extraclasts come from outside the depositional area. Intraclasts include grapestone, which is clusters of peloids cemented together by organic material or mineral cement. Extraclasts are uncommon, are usually accompanied by other clastic sediments, and indicate deposition in a tectonically active area or as part of a turbidity current.[26]


The grains of most limestones are embedded in a matrix of carbonate mud. This is typically the largest fraction of an ancient carbonate rock.[23] Mud consisting of individual crystals less than 5 μm (0.20 mils) in length is described as micrite.[27] In fresh carbonate mud, micrite is mostly small aragonite needles, which may precipitate directly from seawater,[28] be secreted by algae,[29] or be produced by abrasion of carbonate grains in a high-energy environment.[30] This is converted to calcite within a few million years of deposition. Further recrystallization of micrite produces microspar, with grains from 5 to 15 μm (0.20 to 0.59 mils) in diameter.[28]

Limestone often contains larger crystals of calcite, ranging in size from 0.02 to 0.1 mm (0.79 to 3.94 mils), that are described as sparry calcite or sparite. Sparite is distinguished from micrite by a grain size of over 20 μm (0.79 mils) and because sparite stands out under a hand lens or in thin section as white or transparent crystals. Sparite is distinguished from carbonate grains by its lack of internal structure and its characteristic crystal shapes.[31]

Geologists are careful to distinguish between sparite deposited as cement and sparite formed by recrystallization of micrite or carbonate grains. Sparite cement was likely deposited in pore space between grains, suggesting a high-energy depositional environment that removed carbonate mud. Recrystallized sparite is not diagnostic of depositional environment.[31]

Other characteristics

field by their softness (calcite and aragonite both have a Mohs hardness of less than 4, well below common silicate minerals) and because limestone bubbles vigorously when a drop of dilute hydrochloric acid is dropped on it. Dolomite is also soft but reacts only feebly with dilute hydrochloric acid, and it usually weathers to a characteristic dull yellow-brown color due to the presence of ferrous iron. This is released and oxidized as the dolomite weathers.[9] Impurities (such as clay, sand, organic remains, iron oxide, and other materials) will cause limestones to exhibit different colors, especially with weathered

The makeup of a carbonate rock outcrop can be estimated in the field by etching the surface with dilute hydrochloric acid. This etches away the calcite and aragonite, leaving behind any silica or dolomite grains. The latter can be identified by their

Crystals of calcite,

vugs) in the rock. Vugs are a form of secondary porosity, formed in existing limestone by a change in environment that increases the solubility of calcite.[32]

Dense, massive limestone is sometimes described as "marble". For example, the famous

Portoro "marble" of Italy is actually a dense black limestone.[33] True marble is produced by recrystallization of limestone during regional metamorphism that accompanies the mountain building process (orogeny). It is distinguished from dense limestone by its coarse crystalline texture and the formation of distinctive minerals from the silica and clay present in the original limestone.[34]


Travertine limestone terraces of Pamukkale, Turkey.
carbonate rocks
collectively known as limestone.

Folk classification

carbonate rocks.[35] Based on composition, there are three main components: allochems (grains), matrix (mostly micrite), and cement (sparite). The Folk system uses two-part names; the first refers to the grains and the second to the cement. For example, a limestone consisting mainly of ooids, with a crystalline matrix, would be termed an oosparite. It is helpful to have a petrographic microscope when using the Folk scheme, because it is easier to determine the components present in each sample.[36]

Dunham classification

Robert J. Dunham published his system for limestone in 1962. It focuses on the depositional fabric of carbonate rocks. Dunham divides the rocks into four main groups based on relative proportions of coarser clastic particles, based on criteria such as whether the grains were originally in mutual contact, and therefore self-supporting, or whether the rock is characterized by the presence of frame builders and algal mats. Unlike the Folk scheme, Dunham deals with the original porosity of the rock. The Dunham scheme is more useful for hand samples because it is based on texture, not the grains in the sample.[37]

A revised classification was proposed by Wright (1992). It adds some diagenetic patterns to the classification scheme.[38]

Other descriptive terms

Chalk from the White Cliffs of Dover (Chalk Group), England

hot springs. Such deposits are typically massive, dense, and banded. When the deposits are highly porous, so that they have a spongelike texture, they are typically described as tufa. Secondary calcite deposited by supersaturated meteoric waters (groundwater) in caves is also sometimes described as travertine. This produces speleothems, such as stalagmites and stalactites.[39]

Coquina is a poorly consolidated limestone composed of abraded pieces of coral, shells, or other fossil debris. When better consolidated, it is described as coquinite.[40]

Chalk is a soft, earthy, fine-textured limestone composed of the tests of planktonic microorganisms such as foraminifera, while marl is an earthy mixture of carbonates and silicate sediments.[40]


Limestone forms when calcite or aragonite precipitate out of water containing dissolved calcium, which can take place through both biological and nonbiological processes.[41] The solubility of calcium carbonate (CaCO3) is controlled largely by the amount of dissolved carbon dioxide (CO2) in the water. This is summarized in the reaction:

CaCO3 + H2O + CO2 → Ca2+ + 2HCO3

Increases in temperature or decreases in pressure tend to reduce the amount of dissolved CO2 and precipitate CaCO3. Reduction in salinity also reduces the solubility of CaCO3, by several orders of magnitude for fresh water versus seawater.[42]

Near-surface water of the earth's oceans are oversaturated with CaCO3 by a factor of more than six.

ooids likely form through purely inorganic processes, the bulk of CaCO3 precipitation in the oceans is the result of biological activity.[44] Much of this takes place on carbonate platforms

An aerial view of a whiting event precipitation cloud in Lake Ontario.

The origin of carbonate mud,[30] and the processes by which it is converted to micrite,[45] continue to be a subject of research. Modern carbonate mud is composed mostly of aragonite needles around 5 μm (0.20 mils) in length. Needles of this shape and composition are produced by calcareous algae such as Penicillus, making this a plausible source of mud.[46] Another possibility is direct precipitation from the water. A phenomenon known as whitings occurs in shallow waters, in which white streaks containing dispersed micrite appear on the surface of the water. It is uncertain whether this is freshly precipitated aragonite or simply material stirred up from the bottom, but there is some evidence that whitings are caused by biological precipitation of aragonite as part of a bloom of cyanobacteria or microalgae.[47] However, stable isotope ratios in modern carbonate mud appear to be inconsistent with either of these mechanisms, and abrasion of carbonate grains in high-energy environments has been put forward as a third possibility.[30]

Formation of limestone has likely been dominated by biological processes throughout the Phanerozoic, the last 540 million years of the Earth's history. Limestone may have been deposited by microorganisms in the Precambrian, prior to 540 million years ago, but inorganic processes were probably more important and likely took place in an ocean more highly oversaturated in calcium carbonate than the modern ocean.[48]


Diagenesis is the process in which sediments are compacted and turned into solid rock. During diagenesis of carbonate sediments, significant chemical and textural changes take place. For example, aragonite is converted to low-magnesium calcite. Diagenesis is the likely origin of pisoliths, concentrically layered particles ranging from 1 to 10 mm (0.039 to 0.394 inches) in diameter found in some limestones. Pisoliths superficially resemble ooids but have no nucleus of foreign matter, fit together tightly, and show other signs that they formed after the original deposition of the sediments.[49]

Chert nodule within soft limestone at Akçakoca, Turkey
Stylolites in limestone

Silicification occurs early in diagenesis, at low pH and temperature, and contributes to fossil preservation.[50] Silicification takes place through the reaction:[50]

Fossils are often preserved in exquisite detail as chert.[50][51]

Cementing takes place rapidly in carbonate sediments, typically within less than a million years of deposition. Some cementing occurs while the sediments are still under water, forming

hardgrounds. Cementing accelerates after the retreat of the sea from the depositional environment, as rainwater infiltrates the sediment beds, often within just a few thousand years. As rainwater mixes with groundwater, aragonite and high-magnesium calcite are converted to low-calcium calcite. Cementing of thick carbonate deposits by rainwater may commence even before the retreat of the sea, as rainwater can infiltrate over 100 km (60 miles) into sediments beneath the continental shelf.[52]

As carbonate sediments are increasingly deeply buried under younger sediments, chemical and mechanical compaction of the sediments increases. Chemical compaction takes place by pressure solution of the sediments. This process dissolves minerals from points of contact between grains and redeposits it in pore space, reducing the porosity of the limestone from an initial high value of 40% to 80% to less than 10%.[53] Pressure solution produces distinctive stylolites, irregular surfaces within the limestone at which silica-rich sediments accumulate. These may reflect dissolution and loss of a considerable fraction of the limestone bed. At depths greater than 1 km (0.62 miles), burial cementation completes the lithification process. Burial cementation does not produce stylolites.[54]

When overlying beds are eroded, bringing limestone closer to the surface, the final stage of diagenesis takes place. This produces secondary porosity as some of the cement is dissolved by rainwater infiltrating the beds. This may include the formation of vugs, which are crystal-lined cavities within the limestone.[54]

Diagenesis may include conversion of limestone to dolomite by magnesium-rich fluids. There is considerable evidence of replacement of limestone by dolomite, including sharp replacement boundaries that cut across bedding.[55] The process of dolomitization remains an area of active research,[56] but possible mechanisms include exposure to concentrated brines in hot environments (evaporative reflux) or exposure to diluted seawater in delta or estuary environments (Dorag dolomitization).[57] However, Dorag dolomitization has fallen into disfavor as a mechanism for dolomitization,[58] with one 2004 review paper describing it bluntly as "a myth".[56] Ordinary seawater is capable of converting calcite to dolomite, if the seawater is regularly flushed through the rock, as by the ebb and flow of tides (tidal pumping).[55] Once dolomitization begins, it proceeds rapidly, so that there is very little carbonate rock containing mixed calcite and dolomite. Carbonate rock tends to be either almost all calcite/aragonite or almost all dolomite.[57]


About 20% to 25% of sedimentary rock is carbonate rock,

sea floor spreading, which removes magnesium from ocean water. The modern ocean and the ocean of the Mesozoic have been described as "aragonite seas".[62]

Most limestone was formed in shallow marine environments, such as

continental shelves or platforms. Such environments form only about 5% of the ocean basins, but limestone is rarely preserved in continental slope and deep sea environments. The best environments for deposition are warm waters, which have both a high organic productivity and increased saturation of calcium carbonate due to lower concentrations of dissolved carbon dioxide. Modern limestone deposits are almost always in areas with very little silica-rich sedimentation, reflected in the relative purity of most limestones. Reef organisms are destroyed by muddy, brackish river water, and carbonate grains are ground down by much harder silicate grains.[63] Unlike clastic sedimentary rock, limestone is produced almost entirely from sediments originating at or near the place of deposition.[64]

El Capitan, an ancient limestone reef in Texas

Limestone formations tend to show abrupt changes in thickness. Large moundlike features in a limestone formation are interpreted as ancient reefs, which when they appear in the geologic record are called bioherms. Many are rich in fossils, but most lack any connected organic framework like that seen in modern reefs. The fossil remains are present as separate fragments embedded in ample mud matrix. Much of the sedimentation shows indications of occurring in the intertidal or supratidal zones, suggesting sediments rapidly fill available accommodation space in the shelf or platform.[65] Deposition is also favored on the seaward margin of shelves and platforms, where there is upwelling deep ocean water rich in nutrients that increase organic productivity. Reefs are common here, but when lacking, ooid shoals are found instead. Finer sediments are deposited close to shore.[66]

The lack of deep sea limestones is due in part to rapid

calcite compensation depth of 4,000 to 7,000 m (13,000 to 23,000 feet). Below this depth, foraminifera tests and other skeletal particles rapidly dissolve, and the sediments of the ocean floor abruptly transition from carbonate ooze rich in foraminifera and coccolith remains (Globigerina ooze) to silicic mud lacking carbonates.[67]

Mønsted is the largest limestone mine in the world.

In rare cases, turbidites or other silica-rich sediments bury and preserve benthic (deep ocean) carbonate deposits. Ancient benthic limestones are microcrystalline and are identified by their tectonic setting. Fossils typically are foraminifera and coccoliths. No pre-Jurassic benthic limestones are known, probably because carbonate-shelled plankton had not yet evolved.[68]

Limestones also form in freshwater environments.

charophyte (stonewort), a form of freshwater green algae, are characteristic of these environments, where the charophytes produce and trap carbonates.[71]

Limestones may also form in

depositional environments.[72][73] Calcite is one of the first minerals to precipitate in marine evaporites.[74]

Limestone and living organisms

Coral reef at Nusa Lembongan, Bali, Indonesia

Most limestone is formed by the activities of living organisms near reefs, but the organisms responsible for reef formation have changed over geologic time. For example,

stromatolites are mound-shaped structures in ancient limestones, interpreted as colonies of cyanobacteria that accumulated carbonate sediments, but stromatolites are rare in younger limestones.[75] Organisms precipitate limestone both directly as part of their skeletons, and indirectly by removing carbon dioxide from the water by photosynthesis and thereby decreasing the solubility of calcium carbonate.[71]

Limestone shows the same range of

playa lakes, which lack the burrowing organisms.[76] Limestones also show distinctive features such as geopetal structures, which form when curved shells settle to the bottom with the concave face downwards. This traps a void space that can later be filled by sparite. Geologists use geopetal structures to determine which direction was up at the time of deposition, which is not always obvious with highly deformed limestone formations.[77]


green alga Eugamantia sacculata and the fungus Ostracolaba implexa.[78]

Micritic mud mounds

Micricitic mud mounds are subcircular domes of micritic calcite that lacks internal structure. Modern examples are up to several hundred meters thick and a kilometer across, and have steep slopes (with slope angles of around 50 degrees). They may be composed of peloids swept together by currents and stabilized by

mangroves. Bryozoa may also contribute to mound formation by helping to trap sediments.[79]

Mud mounds are found throughout the geologic record, and prior to the early Ordovician, they were the dominant reef type in both deep and shallow water. These mud mounds likely are microbial in origin. Following the appearance of frame-building reef organisms, mud mounds were restricted mainly to deeper water.[80]

Organic reefs

Organic reefs form at low latitudes in shallow water, not more than a few meters deep. They are complex, diverse structures found throughout the fossil record. The frame-building organisms responsible for organic reef formation are characteristic of different geologic time periods:

rudists (a form of bivalve mollusc).[81][82][83] The extent of organic reefs has varied over geologic time, and they were likely most extensive in the middle Devonian, when they covered an area estimated at 5,000,000 km2 (1,900,000 sq mi). This is roughly ten times the extent of modern reefs. The Devonian reefs were constructed largely by stromatoporoids and tabulate corals, which were devastated by the late Devonian extinction.[84]

Organic reefs typically have a complex internal structure. Whole body fossils are usually abundant, but ooids and interclasts are rare within the reef. The core of a reef is typically massive and unbedded, and is surrounded by a talus that is greater in volume than the core. The talus contains abundant intraclasts and is usually either floatstone, with 10% or more of grains over 2mm in size embedded in abundant matrix, or rudstone, which is mostly large grains with sparse matrix. The talus grades to planktonic fine-grained carbonate mud, then noncarbonate mud away from the reef.[81]

Limestone landscape

The Cudgel of Hercules, a tall limestone rock in Poland (Pieskowa Skała Castle in the background)
igneous rocks, but more resistant than most other sedimentary rocks. It is therefore usually associated with hills and downland, and occurs in regions with other sedimentary rocks, typically clays.[85][86]

Karst regions overlying limestone bedrock tend to have fewer visible above-ground sources (ponds and streams), as surface water easily drains downward through joints in the limestone. While draining, water and organic acid from the soil slowly (over thousands or millions of years) enlarges these cracks, dissolving the calcium carbonate and carrying it away in solution. Most cave systems are through limestone bedrock. Cooling groundwater or mixing of different groundwaters will also create conditions suitable for cave formation.[85]

Coastal limestones are often eroded by organisms which bore into the rock by various means. This process is known as

fossil record.[87]

Bands of limestone emerge from the Earth's surface in often spectacular rocky outcrops and islands. Examples include the

Lijiang River and Guilin city in China.[96]

The Florida Keys, islands off the south coast of Florida, are composed mainly of oolitic limestone (the Lower Keys) and the carbonate skeletons of coral reefs (the Upper Keys), which thrived in the area during interglacial periods when sea level was higher than at present.[97]

Unique habitats are found on alvars, extremely level expanses of limestone with thin soil mantles. The largest such expanse in Europe is the Stora Alvaret on the island of Öland, Sweden.[98] Another area with large quantities of limestone is the island of Gotland, Sweden.[99] Huge quarries in northwestern Europe, such as those of Mount Saint Peter (Belgium/Netherlands), extend for more than a hundred kilometers.[100]


Globigerina limestone was, for a long time, the only building material available, and is still very frequently used on all types of buildings and sculptures.[105]

Limestone can be processed into many various forms such as brick, cement, powdered/crushed, or as a filler.[102] Limestone is readily available and relatively easy to cut into blocks or more elaborate carving.[101] Ancient American sculptors valued limestone because it was easy to work and good for fine detail. Going back to the Late Preclassic period (by 200–100 BCE), the Maya civilization (Ancient Mexico) created refined sculpture using limestone because of these excellent carving properties. The Maya would decorate the ceilings of their sacred buildings (known as lintels) and cover the walls with carved limestone panels. Carved on these sculptures were political and social stories, and this helped communicate messages of the king to his people.[106] Limestone is long-lasting and stands up well to exposure, which explains why many limestone ruins survive. However, it is very heavy (density 2.6[107]), making it impractical for tall buildings, and relatively expensive as a building material.

Limestone was most popular in the late 19th and early 20th centuries. Railway stations, banks and other structures from that era were made of limestone in some areas. It is used as a

Odesa Catacombs.[108]

Limestone was also a very popular building block in the Middle Ages in the areas where it occurred, since it is hard, durable, and commonly occurs in easily accessible surface exposures. Many medieval churches and castles in Europe are made of limestone.

Beer stone was a popular kind of limestone for medieval buildings in southern England.[109]

  • Limestone quarry at Cedar Creek, Virginia, US
    Limestone quarry at
    Cedar Creek, Virginia
    , US
  • Nordkalk's limestone quarry in Pargas, Finland
    Nordkalk's limestone quarry in Pargas, Finland
  • Cutting limestone blocks at a quarry in Gozo, Malta
    Cutting limestone blocks at a quarry in Gozo, Malta
  • Limestone as building material
    Limestone as building material
  • Limestone is used worldwide as building material.
    Limestone is used worldwide as building material.

Limestone is the raw material for production of lime, primarily known for treating soils, purifying water and

pH buffering agent.[113] Acid-based cleaning chemicals can also etch limestone, which should only be cleaned with a neutral or mild alkali-based cleaner.[114]

Moosburg in Bavaria is prepared for a lithography
Plastic bag "made mainly from limestone"[clarification needed]

Other uses include:

Many limestone formations are porous and permeable, which makes them important petroleum reservoirs.[124] About 20% of North American hydrocarbon reserves are found in carbonate rock. Carbonate reservoirs are very common in the petroleum-rich Middle East,[59] and carbonate reservoirs hold about a third of all petroleum reserves worldwide.[125] Limestone formations are also common sources of metal ores, because their porosity and permeability, together with their chemical activity, promotes ore deposition in the limestone. The lead-zinc deposits of Missouri and the Northwest Territories are examples of ore deposits hosted in limestone.[59]


Limestone is a major industrial raw material that is in constant demand. This raw material has been essential in the iron and steel industry since the nineteenth century.[126] Companies have never had a shortage of limestone; however, it has become a concern as the demand continues to increase[127] and it remains in high demand today.[128] The major potential threats to supply in the nineteenth century were regional availability and accessibility.[126] The two main accessibility issues were transportation and property rights. Other problems were high capital costs on plants and facilities due to environmental regulations and the requirement of zoning and mining permits.[104] These two dominant factors led to the adaptation and selection of other materials that were created and formed to design alternatives for limestone that suited economic demands.[126]

Limestone was classified as a critical raw material, and with the potential risk of shortages, it drove industries to find new alternative materials and technological systems. This allowed limestone to no longer be classified as critical as replacement substances increased in production; minette ore is a common substitute, for example.[126]

Occupational safety and health

NFPA 704
safety square

Powdered limestone as a food additive is generally recognized as safe[130] and limestone is not regarded as a hazardous material. However, limestone dust can be a mild respiratory and skin irritant, and dust that gets into the eyes can cause corneal abrasions. Because limestone contains small amounts of silica, inhalation of limestone dust could potentially lead to silicosis or cancer.[129]

United States

The Occupational Safety and Health Administration (OSHA) has set the legal limit (permissible exposure limit) for limestone exposure in the workplace as 15 mg/m3 (0.0066 gr/cu ft) total exposure and 5 mg/m3 (0.0022 gr/cu ft) respiratory exposure over an 8-hour workday. The National Institute for Occupational Safety and Health (NIOSH) has set a recommended exposure limit (REL) of 10 mg/m3 (0.0044 gr/cu ft) total exposure and 5 mg/m3 (0.0022 gr/cu ft) respiratory exposure over an 8-hour workday.[131]


Removing graffiti from weathered limestone is difficult because it is a porous and permeable material. The surface is fragile so usual abrasion methods run the risk of severe surface loss. Because it is an acid-sensitive stone some cleaning agents cannot be used due to adverse effects.[132]


See also


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Further reading