| Igneous rock | |
.jpg) Kimberlite from the United States | |
| Composition | |
|---|---|
| Forsteritic olivine and carbonate minerals, with trace amounts of magnesian ilmenite, chromium pyrope, almandine-pyrope, chromium diopside, phlogopite, enstatite and titanium-poor chromite. Sometimes containsdiamonds. |
Kimberlite is anigneous rock and a rare variant ofperidotite. It is most commonly known to be the main host matrix fordiamonds. It is named after the town ofKimberley inSouth Africa, where the discovery of an 83.5-carat (16.70 g) diamond called theStar of South Africa in 1869 spawned adiamond rush and led to the excavation of theopen-pit mine called theBig Hole. Previously, the term kimberlite has been applied to olivine lamproites as Kimberlite II, however this has been in error.
Kimberlite occurs in the Earth'scrust in vertical structures known askimberlite pipes, as well as igneousdykes and can also occur as horizontalsills. Kimberlite pipes are the most important source of mined diamonds today. The consensus on kimberlites is that they are formed deep withinEarth's mantle. Formation occurs at depths between 150 and 450 kilometres (93 and 280 mi), potentially from anomalously enriched exotic mantle compositions, and they are erupted rapidly and violently, often with considerablecarbon dioxide and othervolatile components. It is this depth of melting and generation that makes kimberlites prone to hosting diamondxenocrysts.
Despite its relative rarity, kimberlite has attracted attention because it serves as a carrier of diamonds andgarnet peridotite mantlexenoliths to the Earth's surface. Its probable derivation from depths greater than any otherigneous rock type, and the extrememagma composition that it reflects in terms of lowsilica content and high levels ofincompatibletrace-element enrichment, make an understanding of kimberlitepetrogenesis important. In this regard, the study of kimberlite has the potential to provide information about the composition of the deep mantle and melting processes occurring at or near the interface between thecratonic continentallithosphere and the underlying convectingasthenospheric mantle.
Many kimberlite structures are emplaced as carrot-shaped, vertical intrusions termed "pipes". This classic carrot shape is formed due to a complex intrusive process of kimberlitic magma, which inherits a large proportion of CO2 (lower amounts of H2O) in the system, which produces a deep explosive boiling stage that causes a significant amount of vertical flaring.[1] Kimberlite classification is based on the recognition of differing rockfacies. These differing facies are associated with a particular style of magmatic activity, namely crater, diatreme andhypabyssal rocks.[2][3]
Themorphology of kimberlite pipes and their classical carrot shape is the result of explosivediatremevolcanism from very deepmantle-derived sources. These volcanic explosions produce vertical columns of rock that rise from deep magma reservoirs. The eruptions forming thesepipes fracture the surrounding rock as it explodes, bringing up unalteredxenoliths of peridotite to surface. Thesexenoliths provide valuable information to geologists about mantle conditions and composition.[4][5] The morphology of kimberlite pipes is varied, but includes a sheeted dyke complex of tabular, vertically dipping feeder dykes in the root of the pipe, which extends down to the mantle. Within 1.5–2 km (4,900–6,600 ft) of the surface, the highly pressured magma explodes upwards and expands to form a conical to cylindricaldiatreme, which erupts to the surface. The surface expression is rarely preserved but is usually similar to amaar volcano. Kimberlite dikes and sills can be thin (1–4 meters), while pipes range in diameter from about 75 meters to 1.5 kilometers.[6]
Both the location and origin of kimberlitic magmas are subjects of contention. Their extreme enrichment and geochemistry have led to a large amount of speculation about their origin, with models placing their source within the sub-continental lithospheric mantle (SCLM) or even as deep as the transition zone. The mechanism of enrichment has also been the topic of interest with models including partial melting, assimilation of subducted sediment or derivation from a primary magma source.
Historically, kimberlites have been classified into two distinct varieties, termed "basaltic" and "micaceous" based primarily on petrographic observations.[7] This was later revised by C. B. Smith, who renamed these divisions "group I" and "group II" based on the isotopic affinities of these rocks using theNd,Sr, and Pb systems.[8] Roger Mitchell later proposed that these group I and II kimberlites display such distinct differences, that they may not be as closely related as once thought. He showed that group II kimberlites show closer affinities tolamproites than they do to group I kimberlites. Hence, he reclassified group II kimberlites as orangeites to prevent confusion.[9]
Group-I kimberlites are of CO2-richultramafic potassic igneous rocks dominated by primaryforsteritic olivine and carbonate minerals, with a trace-mineral assemblage of magnesianilmenite, chromiumpyrope,almandine-pyrope, chromiumdiopside (in some cases subcalcic),phlogopite,enstatite and of Ti-poorchromite. Group I kimberlites exhibit a distinctive inequigranular texture caused by macrocrystic (0.5–10 mm or 0.020–0.394 in) to megacrystic (10–200 mm or 0.39–7.87 in) phenocrysts of olivine, pyrope, chromian diopside, magnesian ilmenite, and phlogopite, in a fine- to medium-grained groundmass.[10]
The groundmass mineralogy, which more closely resembles a true composition of the igneous rock, is dominated by carbonate and significant amounts of forsteritic olivine, with lesser amounts of pyrope garnet, Cr-diopside, magnesian ilmenite, andspinel.
Olivine lamproites were previously called group II kimberlite or orangeite in response to the mistaken belief that they only occurred in South Africa. Their occurrence and petrology, however, are identical globally and should not be erroneously referred to as kimberlite.[11] Olivine lamproites areultrapotassic,peralkaline rocks rich in volatiles (dominantly H2O). The distinctive characteristic of olivine lamproites isphlogopite macrocrysts and microphenocrysts, together with groundmass micas that vary in composition from phlogopite to "tetraferriphlogopite" (anomalously Al-poor phlogopite requiring Fe to enter the tetrahedral site). Resorbed olivine macrocrysts and euhedral primary crystals of groundmass olivine are common but not essential constituents.
Characteristic primary phases in the groundmass include zoned pyroxenes (cores of diopside rimmed by Ti-aegirine), spinel-group minerals (magnesianchromite to titaniferousmagnetite), Sr- andREE-richperovskite, Sr-richapatite, REE-rich phosphates (monazite, daqingshanite), potassian barianhollandite group minerals, Nb-bearingrutile and Mn-bearingilmenite.
Kimberlites are peculiar igneous rocks because they contain a variety of mineral species with chemical compositions that indicate they formed under high pressure and temperature within the mantle. These minerals, such as chromium diopside (apyroxene), chromium spinels, magnesian ilmenite, and pyrope garnets rich in chromium, are generally absent from most other igneous rocks, making them particularly useful as indicators for kimberlites.
 | This sectionneeds additional citations forverification. Please helpimprove this article byadding citations to reliable sources in this section. Unsourced material may be challenged and removed.(October 2007) (Learn how and when to remove this message) |
Kimberlites exhibit unique geochemical characteristics that distinguish them from other igneous rocks, reflecting their origin deep within the Earth's mantle. These features provide insights into the mantle's composition and the processes involved in the formation and eruption of kimberlite magmas.
Kimberlites are classified as ultramafic rocks due to their highmagnesium oxide (MgO) content, which typically exceeds 12%, and often surpasses 15%. This high MgO concentration indicates a mantle-derived origin, rich inolivine and other magnesium-dominant minerals. Additionally, kimberlites are ultrapotassic, with a molar ratio ofpotassium oxide (K2O) toaluminum oxide (Al2O3) greater than 3, suggesting significant alterations or enrichment processes in their mantle source regions.
Characteristic of kimberlites is their abundance in near-primitive elements such asnickel (Ni), chromium (Cr), and cobalt (Co), with concentrations often exceeding 400ppm for Ni, 1000 ppm for Cr, and 150 ppm for Co. These high levels reflect the primitive nature of their mantle source, having undergone minimal differentiation.
Kimberlites show enrichment inrare earth elements (REEs),[12] which are pivotal for understanding their genesis and evolution. This enrichment in REEs, along with a moderate to high large-ionlithophile element (LILE)[13] enrichment (more than 1,000 ppm) includingpotassium, barium, and strontium, points to a significant contribution frommetasomatized mantle sources, where the rock composition has been altered by fluids.
A defining feature of kimberlites is their high volatile content, particularly of water (H2O) and carbon dioxide (CO2). The presence of these volatiles influences the explosivity of kimberlite eruptions and facilitates the transport of diamonds from deep within the mantle to the Earth's surface. The high levels of H2O and CO2 are indicative of a deep mantle origin, where these compounds are more abundant.[14]
Kimberlite exploration techniques encompass a multifaceted approach that integrates geological, geochemical, and geophysical methodologies to locate and evaluate potential diamond-bearing deposits.[15]
Exploration techniques for kimberlites primarily hinge on the identification and analysis of indicator minerals associated with the presence of kimberlite pipes and their potential diamond content. Sediment sampling is a fundamental approach, where kimberlite indicator minerals (KIMs) are dispersed across landscapes due to geological processes like uplift, erosion, and glaciations. Loaming and alluvial sampling are utilized in different terrains to recover KIMs from soils and stream deposits, respectively. Understanding paleodrainage patterns and geological cover layers aids in tracing KIMs back to their source kimberlite pipes. In glaciated regions, techniques such asesker sampling,till sampling, and alluvial sampling are employed to recover KIMs buried beneath thick glacial deposits. Once collected, heavy minerals are separated and sorted by hand to identify these indicators. Chemical analysis confirms their identity and categorizes them. Techniques likethermobarometry help understand the conditions under which these minerals formed and where they came from in the Earth's mantle. By analyzing these indicators and geological curves, scientists can estimate the likelihood of finding diamonds in a kimberlite pipe. These methods help prioritize where to drill in the search for valuable diamond deposits.[16][17]
Geophysical methods are particularly useful in areas where direct detection of kimberlites is challenging due to significantoverburden or weathering. These methods leverage physical property contrasts between kimberlite bodies and their surrounding host rocks, enabling the detection of subtle anomalies indicative of potential kimberlite deposits. Airborne and ground surveys, including magnetics, electromagnetics, and gravity surveys, are commonly employed to acquire geophysical data over large areas efficiently. Magnetic surveys detect variations in the Earth's magnetic field caused by magnetic minerals within kimberlites, which typically exhibit distinct magnetic signatures compared to surrounding rocks. Electromagnetic surveys measure variations in electrical conductivity, with conductive kimberlite bodies producing anomalous responses. Gravity surveys detect variations in gravitational attraction caused by differences in density between kimberlite and surrounding rocks. By analyzing and interpreting these geophysical anomalies, geologists can delineate potential kimberlite targets for further investigation, such as drilling. However, the interpretation of geophysical data requires careful consideration of geological context and potential masking effects from surrounding geology, highlighting the importance of integrating geophysical results with other exploration techniques for accurate targeting and successful diamond discoveries.[15][18]
Three-dimensional (3D) modeling offers a comprehensive framework for understanding the internal structure and distribution of key geological features within potential diamond-bearing deposits. This process begins with the collection and integration of various datasets, including drill-hole data, ground geophysical surveys, and geological mapping information. These datasets are then integrated into a cohesive digital platform, often utilizing specialized software packages tailored for geological modeling. Through advanced visualization techniques, geologists can create detailed 3D representations of the subsurface geology, highlighting the distribution and geometry of kimberlite bodies alongside other significant geological features such as faults, fractures, and lithological boundaries. Within the model, efforts are made to accurately depict the internal phases of kimberlite pipes, incorporating differentfacies, country rock xenoliths, and mantle xenoliths identified through careful interpretation of drill-core data and geophysical surveys. Once validated, the 3D model serves as a valuable decision-making tool, offering insights into potential diamond-bearing potential, identifying high-priority drilling targets, and guiding exploration strategies to maximize the chances of successful diamond discoveries.[19][20]
Kimberlites are a valuable source of information about the composition of the Earth's mantle and the dynamic processes that occur within it. The study of kimberlites has contributed to our understanding of the Earth’s deep geochemical cycles and the mechanism ofmantle plumes, which are upwellings of abnormally hot rock within the Earth's mantle.[21]
Moreover, kimberlites are unique in their ability to transport material from the Earth's mantle to its surface. This process, known as xenolith transport, provides geologists with samples of the Earth's mantle, which are otherwise inaccessible. Analyzing these samples has led to significant advances in our knowledge of the Earth's deep interior, including its physical conditions, composition, and the evolutionary history of the planet.
The role of kimberlites in diamond exploration cannot be overstated. Diamonds are formed under the high-pressure, high-temperature conditions of the Earth's mantle. Kimberlites act as carriers for these diamonds, transporting them to the Earth's surface. The discovery of diamond-bearing kimberlites in the 1870s in Kimberley sparked adiamond rush, transforming the area into one of the world’s largest diamond-producing regions. Since then, the association between kimberlites and diamonds has been crucial in the search for new diamond deposits around the globe.[22][23]
Kimberlites also serve as a window into the Earth's past, offering clues about the formation of continents and the dynamic processes that shape our planet. Their distribution and age can provide insights into ancient continental movements and the assembly and breakup ofsupercontinents.[24]
Kimberlites are the most important source of primarydiamonds. Many kimberlite pipes also produce richalluvial oreluvial diamondplacer deposits. As of 2014[update] about 6,400 kimberlite pipes are known on Earth including about 900 that have been found to contain diamonds, with mining of diamonds occurring at about 30 pipes.[25]
The discovery of diamond-rich kimberlite pipes in northern Canada during the early 1990s serves as a prime example of how challenging these deposits can be to locate, as their surface features are often subtle. In this case, the pipes were hidden beneath ice-covered shallow ponds, which filled depressions formed by the softer kimberlite rock eroding slightly faster than the surrounding harder rock.[26]
The deposits occurring atKimberley,South Africa, were the first recognized and the source of the name. The Kimberleydiamonds were originally found inweathered kimberlite, which was colored yellow bylimonite, and so was called "yellow ground". Deeper workings encountered less altered rock,serpentinized kimberlite, which miners call "blue ground". Yellow ground kimberlite is easy to break apart and was the first source of diamonds to be mined. Blue ground kimberlite needs to be run throughrock crushers to extract the diamonds.[27]
See alsoMir Mine andUdachnaya pipe, both in theSakha Republic,Siberia.
The blue and yellow ground were both prolific producers of diamonds. After the yellow ground had been exhausted, miners in the late 19th century accidentally cut into the blue ground and found gem-quality diamonds in quantity. The economic situation at the time was such that, with a flood of diamonds being found, the miners undercut each other's prices and eventually decreased the diamonds' value down to cost in a short time.[28]
