Limestone is a type ofcarbonatesedimentary rock which is the main source of the materiallime. It is composed mostly of themineralscalcite andaragonite, which are differentcrystal forms ofcalcium carbonateCaCO3. Limestone forms when these mineralsprecipitate out of water containing dissolvedcalcium. This can take place through bothbiological 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 containsfossils which provide scientists with information on ancient environments and on theevolution of life.[3]
About 20% to 25% of sedimentary rock is carbonate rock, and most of this is limestone.[4][3] The remaining carbonate rock is mostlydolomite, a closely related rock, which contains a high percentage of the mineraldolomite,CaMg(CO3)2.Magnesian limestone is an obsolete and poorly defined term used variously for dolomite, for limestone containing significant dolomite (dolomitic limestone), or for any other limestone containing a significant percentage ofmagnesium.[5] Most limestone was formed in shallowmarine environments, such ascontinental shelves orplatforms, 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 slightlysoluble in rainwater, these exposures often are eroded to becomekarst landscapes. Mostcave systems are found in limestone bedrock.
Limestone has numerous uses: as a chemicalfeedstock for the production oflime used forcement (an essential component ofconcrete), as aggregate for the base of roads, as white pigment or filler in products such as toothpaste or paint, as asoil conditioner, and as a popular decorative addition torock gardens. Limestone formations contain about 30% of the world'spetroleum reservoirs.[3]
Limestone is composed mostly of themineralscalcite andaragonite, which are differentcrystal forms ofcalcium carbonate (CaCO3).Dolomite,CaMg(CO3)2, is an uncommon mineral in limestone, andsiderite or othercarbonate minerals are rare. However, the calcite in limestone often contains a few percent ofmagnesium. 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, withclastic sediments (mainly fine-grainedquartz andclay 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 is commonly white to gray in color. Limestone that is unusually rich in organic matter can be almost black in color, while traces ofiron ormanganese can give limestone an off-white to yellow to red color. The density of limestone depends on its porosity, which varies from 0.1% for the densest limestone to 40% for chalk. The density correspondingly ranges from 1.5 to 2.7 g/cm3. Although relatively soft, with aMohs hardness of 2 to 4, dense limestone can have a crushing strength of up to 180MPa.[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]
Grains
Ooids from abeach on Joulter's Cay,The BahamasOoids in limestone of theCarmel Formation (Middle Jurassic) of southwestern Utah.Thin-section view of a MiddleJurassic limestone in southernUtah, U.S. The round grains areooids; 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 ascoral orforaminifera.[16] These organisms secrete structures made of aragonite or calcite, and leave these structures behind when they die. Other carbonate grains composing limestones areooids,peloids, and limeclasts (intraclasts andextraclasts [ca]).[17]
Skeletal grains have a composition reflecting the organisms that produced them and the environment in which they were produced.[18] Low-magnesium calcite skeletal grains are typical of articulatebrachiopods, planktonic (free-floating) foraminifera, andcoccoliths. High-magnesium calcite skeletal grains are typical of benthic (bottom-dwelling) foraminifera,echinoderms, andcoralline algae. Aragonite skeletal grains are typical ofmolluscs, calcareousgreen algae,stromatoporoids,corals, andtube 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 anoolite or sometimes anoolitic limestone. Ooids form in high-energy environments, such as the Bahama platform, and oolites typically showcrossbedding 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.[22] Many are thought to be fecal pellets produced by marine organisms. Others may be produced byendolithic (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 partiallylithified carbonate sediments. Intraclasts are limeclasts that originate close to where they are deposited in limestone, while extraclasts come from outside the depositional area. Intraclasts includegrapestone, 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 aturbidity current.[26]
Mud
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 asmicrite.[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 producesmicrospar, 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 assparry calcite orsparite. 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]
Limestone outcrops are recognized in thefield 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 dilutehydrochloric 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 asclay, sand, organic remains,iron oxide, and other materials) will cause limestones to exhibit different colors, especially withweathered surfaces.
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 theirrhombohedral shape.[9]
Crystals of calcite,quartz,dolomite orbarite may line small cavities (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 famousPortoro "marble" of Italy is actually a dense black limestone.[33] Truemarble is produced by recrystallization of limestone during regionalmetamorphism 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]
Robert L. Folk developed a classification system that places primary emphasis on the detailed composition of grains and interstitial material incarbonate 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 apetrographic microscope when using the Folk scheme, because it is easier to determine the components present in each sample.[36]
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
Travertine is a term applied to calcium carbonate deposits formed in freshwater environments, particularlywaterfalls, cascades andhot 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 astufa. Secondary calcite deposited bysupersaturatedmeteoric waters (groundwater) in caves is also sometimes described as travertine. This producesspeleothems, such asstalagmites andstalactites.[39]
Coquina is a poorly consolidated limestone composed of abraded pieces ofcoral,shells, or other fossil debris. When better consolidated, it is described ascoquinite.[40]
Chalk is a soft, earthy, fine-textured limestone composed of the tests of planktonic microorganisms such as foraminifera, whilemarl is an earthy mixture of carbonates and silicate sediments.[40]
Formation
Limestone forms when calcite or aragoniteprecipitate 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 dissolvedcarbon dioxide (CO2) in the water. This is summarized in the reaction:
CaCO3 + H2O + CO2 → Ca2+ + 2 HCO−3
Increases in temperature or decreases in pressure tend to reduce the amount of dissolvedCO2 and precipitateCaCO3. Reduction in salinity also reduces the solubility ofCaCO3, by several orders of magnitude for fresh water versus seawater.[42]
Near-surface water of the earth's oceans are oversaturated withCaCO3 by a factor of more than six.[43] The failure ofCaCO3 to rapidly precipitate out of these waters is likely due to interference by dissolved magnesiumions withnucleation of calcite crystals, the necessary first step in precipitation. Precipitation of aragonite may be suppressed by the presence of naturally occurring organic phosphates in the water. Althoughooids likely form through purely inorganic processes, the bulk ofCaCO3 precipitation in the oceans is the result of biological activity.[44] Much of this takes place oncarbonate 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 asPenicillus, making this a plausible source of mud.[46] Another possibility is direct precipitation from the water. A phenomenon known aswhitings 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 abloom ofcyanobacteria ormicroalgae.[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 thePhanerozoic, the last 540 million years of the Earth's history. Limestone may have been deposited by microorganisms in thePrecambrian, 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
Diagenesis is the process in which sediments are compacted andturned 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 ofpisoliths, 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 atAkçakoca, TurkeyStylolites 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, forminghardgrounds. 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 bypressure 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 distinctivestylolites, 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 producessecondary porosity as some of the cement is dissolved by rainwater infiltrating the beds. This may include the formation ofvugs, 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 ofdolomitization 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]
Occurrence
About 20% to 25% of sedimentary rock is carbonate rock,[3] and most of this is limestone.[17][3] Limestone is found in sedimentary sequences as old as 2.7 billion years.[59] However, the compositions of carbonate rocks show an uneven distribution in time in the geologic record. About 95% of modern carbonates are composed of high-magnesium calcite and aragonite.[60] The aragonite needles in carbonate mud are converted to low-magnesium calcite within a few million years, as this is the most stable form of calcium carbonate.[28] Ancient carbonate formations of thePrecambrian andPaleozoic contain abundant dolomite, but limestone dominates the carbonate beds of theMesozoic andCenozoic. Modern dolomite is quite rare. There is evidence that, while the modern ocean favors precipitation of aragonite, the oceans of the Paleozoic and middle to late Cenozoic favored precipitation of calcite. This may indicate a lower Mg/Ca ratio in the ocean water of those times.[61] This magnesium depletion may be a consequence of more rapidsea 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 ascontinental shelves orplatforms. 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]
Limestone formations tend to show abrupt changes in thickness. Large moundlike features in a limestone formation are interpreted as ancientreefs, which when they appear in the geologic record are calledbioherms. 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 availableaccommodation 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 rapidsubduction of oceanic crust, but is more a result of dissolution of calcium carbonate at depth. The solubility of calcium carbonate increases with pressure and even more with higher concentrations of carbon dioxide, which is produced by decaying organic matter settling into the deep ocean that is not removed byphotosynthesis in the dark depths. As a result, there is a fairly sharp transition from water saturated with calcium carbonate to water unsaturated with calcium carbonate, thelysocline, which occurs at thecalcite 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 limestonemine 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 theirtectonic 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.[69] These limestones are not unlike marine limestone, but have a lower diversity of organisms and a greater fraction of silica and clay minerals characteristic ofmarls. TheGreen River Formation is an example of a prominent freshwater sedimentary formation containing numerous limestone beds.[70] Freshwater limestone is typically micritic. Fossils ofcharophyte (stonewort), a form of freshwater green algae, are characteristic of these environments, where the charophytes produce and trap carbonates.[71]
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 ofcyanobacteria 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 ofsedimentary structures found in other sedimentary rocks. However, finer structures, such aslamination, are often destroyed by the burrowing activities of organisms (bioturbation). Fine lamination is characteristic of limestone formed inplaya lakes, which lack the burrowing organisms.[76] Limestones also show distinctive features such asgeopetal 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]
ThecyanobacteriumHyella balani can bore through limestone; as can thegreen algaEugamantia sacculata and thefungusOstracolaba 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 byThalassia grass ormangroves. Bryozoa may also contribute to mound formation by helping to trap sediments.[79]
Mud mounds are found throughout the geologic record, and prior to theearly 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:Archaeocyathids appeared in theearly Cambrian; these gave way to sponges by thelate Cambrian; later successions included stromatoporoids, corals, algae, bryozoa, andrudists (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 andtabulate corals, which were devastated by thelate 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 atalus that is greater in volume than the core. The talus contains abundant intraclasts and is usually eitherfloatstone, with 10% or more of grains over 2mm in size embedded in abundant matrix, orrudstone, 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 is partially soluble, especially in acid, and therefore forms many erosional landforms. These includelimestone pavements,pot holes,cenotes, caves and gorges. Such erosion landscapes are known askarsts. Limestone is lessresistant to erosion than mostigneous rocks, but more resistant than most othersedimentary rocks. It is therefore usually associated with hills anddownland, 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 throughjoints 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 insolution. Mostcave 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 asbioerosion. It is most common in the tropics, and it is known throughout thefossil record.[87]
TheFlorida Keys, islands off the south coast ofFlorida, are composed mainly ofoolitic limestone (the Lower Keys) and the carbonate skeletons ofcoral 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 onalvars, extremely level expanses of limestone with thin soil mantles. The largest such expanse in Europe is theStora Alvaret on the island ofÖland, 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]
Limestone is a raw material that is used globally in a variety of different ways including construction, agriculture and as industrial materials.[102] Limestone is very common in architecture, especially in Europe and North America. Many landmarks across the world, including theGreat Pyramid and its associatedcomplex inGiza, Egypt, were made of limestone. So many buildings inKingston, Ontario, Canada were, and continue to be, constructed from it that it is nicknamed the 'Limestone City'.[103] Limestone, metamorphosed by heat and pressure produces marble, which has been used for many statues, buildings and stone tabletops.[104] On the island ofMalta, a variety of limestone calledGlobigerina 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), theMaya 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 aslintels) 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 afaçade on some skyscrapers, but only in thin plates for covering, rather than solid blocks. In the United States, Indiana, most notably theBloomington area, has long been a source of high-quality quarried limestone, calledIndiana limestone. Many famous buildings in London are built fromPortland limestone. Houses built inOdesa inUkraine in the 19th century were mostly constructed from limestone and the extensive remains of the mines now form theOdesa 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 is the raw material for production of lime, primarily known for treating soils, purifying water andsmelting copper. Lime is an important ingredient used in chemical industries.[110] Limestone and (to a lesser extent) marble are reactive to acid solutions, makingacid rain a significant problem to the preservation of artifacts made from this stone. Many limestone statues and building surfaces have suffered severe damage due to acid rain.[111][112] Likewise limestone gravel has been used to protect lakes vulnerable to acid rain, acting as apH buffering agent.[113] Acid-based cleaning chemicals can also etch limestone, which should only be cleaned with a neutral or mildalkali-based cleaner.[114]
A limestone plate with a negative map ofMoosburg in Bavaria is prepared for alithography print.Plastic bag "made mainly from limestone"[clarification needed]
As an additive toothpaste, paper, plastics, paint, tiles, and other materials as both white pigment and a cheap filler.[118]
Asrock dust, to suppress methane explosions in underground coal mines.[119]
Purified, it is added to bread and cereals as a source of calcium.[120]
As a calcium supplement in livestock feed, such as for poultry (when ground up).[121]
For remineralizing and increasing the alkalinity of purified water to prevent pipe corrosion and to restore essential nutrient levels.[122]
Inblast furnaces, limestone binds with silica and other impurities to remove them from the iron.[123]
It can aid in the removal of toxic components created from coal burning plants and layers of polluted molten metals.[110]
Many limestoneformations are porous and permeable, which makes them importantpetroleum 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. Thelead-zinc deposits ofMissouri and theNorthwest Territories are examples of ore deposits hosted in limestone.[59]
Scarcity
Limestone is a major industrial raw material that is in constant demand. This raw material has been essential in theiron andsteel 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]
Powdered limestone as a food additive isgenerally 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 causecorneal abrasions. Because limestone contains small amounts of silica, inhalation of limestone dust could potentially lead tosilicosis orcancer.[129]
Removinggraffiti from weathered limestone is difficult because it is a porous and permeable material. The surface is fragile, therefore usual abrasion methods run the risk of severe surface loss. Since it is an acid-sensitive stone, some cleaning agents cannot be used due to adverse effects.[132]
Gallery
Astratigraphic section ofOrdovician limestone exposed in centralTennessee, U.S. The less-resistant and thinner beds are composed ofshale. The vertical lines are drill holes for explosives used during road construction.
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