Introduction

There are currently (2020) two minerals with a kaersutite root-name:
Ferri-kaersutite - registered from 7 localities in mindat (2020)
Kaersutite - registered from 216 localities in mindat (2020)
In addition, a named amphibole ferro-kaersutite is registered from 9 localities in mindat (2020).

The kaersutite minerals are typical for upper mantle rocks. It is common, and even a major constituent of alkali-magmas under high pressures between 25-35 kbar. On surface it can be found as sub mm grains in alkaline volcanic rocks, such as basanites and mugearites, or in alkaline plutonic rocks. Under certain circumstances, titanian amphiboles can also be formed at lower pressures, and it seems as the presence of F^- may increase the stability field of kaersutitic amphiboles even at close to atmospheric pressure.

Kaersutite crystals can form when the magma fractionates and allow larger crystals to form. It is believed that this is a very slow process, taking maybe thousands of years under constant pressure and temperature to form a 1 cm crystal. The crystal then must be transported to the surface to be frozen as a crystal (megacryst, porfyroblast) in a fine-grained volcanic matrix. The long time it takes to form a large kaersutite-series mineral makes the large, well developed crystals from some of the Czech locations truly remarkable, whether they are kaersutite proper or not.

Kaersutite minerals may also be fomed in volcanic dikes. This is the case for the type locality Qaersut and some of the other localities listed in this article. In these cases, the kaersutite minerals grow rather rapidly, only 25 days is estimated for the up to 4 in. long crystals found near the Hoover Dam in the US. The mechanisms causing the growth of large kaersutite crystals in these dikes has been compared to how pegmatites are formed. The Qaersut occurance has sometimes been referred to as a "kaersutite-pegmatite".

In this article, the term kaersutitic amphibole is used for amphiboles closely resembling kaersutite in chemistry and mode of occurrence. The name is used as a common name for amphiboles with a high (>0.35 apfu) Ti content with compositions falling in the pargasite, hastingsite, oxo-pargasite, oxo-hastingsite, ferri-sadanagaite, kaersutite and/or ferri-kaersutite field. This has been a useful term for two reasons:

1) It is not uncommon to find amphiboles near the borderline for one or more of the minerals listed above, and two or more of these minerals can be found at the same locality, and even within the same crystal.

2) Even analyzed amphiboles will have uncertainties in their ID, since H and Fe³⁺ is rarely measured. For O, the ^wO₂ content is normally assumed to be twice the Ti content, thus discarding that Fe is often oxidized in these amphiboles following the Fe²⁺(OH) -> Fe³⁺O reaction. The Fe³⁺ content is calculated with a rather large error margin when comparing calculated values with actual measured Fe3+ content. Both these approximations result in erroneous naming of analyzed amphiboles.

I therefore find the term kearsutitic amphibole useful as it allows the (almost) inevitable uncertainty in the identification, yet still providing the reader a reasonably accurate understanding of the composition of the amphibole. The Czech and German amphiboles included in this article are good examples of kaersutitic amphiboles. Probably only a very few of these amphiboles are kaersutite sensu strictu. For all the entries in the article, the compositional space of the amphiboles from the different amphiboles are given.

The kaersutite amphiboles are not particularly sought after by collectors, whether museums or private, as they are rarely much for the eye, and notoriously difficult to identify. For petrologists and scientists with an interest in mantle processes or special volcanic events, kaersutitic amphiboles are more interesting, and there is quite a lot of literature available describing the genesis and chemistry of these amphiboles. Kaersutitic amphiboles are also much studied to understand the relationship between ferrous and ferric iron as well as the role of Titanium in the amphibole molecule.

Australia

Eastern Hill, Mount Anakie, Anakie, City of Greater Geelong, Victoria, Australia

Mount Anakie belongs to the Newer Basalt Province in Victoria and South Australia. This province hosts a large variety of magma types, seemingly without any clear compositional progression. Some of the magmas are characterized by the occurrence of megacrysts in the form of sometimes “unusually large crystals”, believed to have formed in fractionation of liquid magma in mantel conditions.

Mount Anakie is the largest and northernmost of 4 aligned eruption points over a distance of 5km and is considered the most interesting of these scoria cones due to the presence of kaersuite megacrysts in nepheline mugearite host rock.
Deer et al.(1997) publish an analysis of kaersutite from here, showing 0.632 apfu Ti.

Czech Republic

Lukov outcrop, Lukov, Teplice District, Ústí nad Labem Region, Czech Republic

Macroscopic (>2 mm) kaersutitc amphibole phenocrysts can be found at several localities in the area. The largest phenocrysts reaching sizes up to several cm. Kaersutitic amphiboles are mostly found in the alkaline basaltic rocks, and is found in more than 70% of the more than 1000 alkaline dykes radially arranged to the main volcanic center of the České Středohoří Mts.
J. Ulrych (Pers. Com 2012) has provided analytical data from Lukov and several other localities related to the České Středohoří Mts. volcanic center. The Ti content ranges from 4.24-5.29wt% placing these amphiboles at or near the titanian pargasite-kaersutite borderline of 0.5 (atoms per formula unit) apfu Ti. Data from Ulrych et al (2018) show that the compositions of kaersutitic amphiboles range from ca 0.3 apfu to 0.7 apfu Ti,. The larger crystals rarely contain enough Ti to qualify as kaersutite but the majority of large crystals are more likely to be pargasite or hastingsite root name amphiboles. As the crystals must be analyzed individually to set a correct ID, the term kaersutitic amphibole are consequently used for these amphiboles in this article.

Suletice (Sulotice; Sulotitz; Sulloditz), Homole u Panny, Ústí nad Labem District, Ústí nad Labem Region, Czech Republic

Plundrichovy Hůrky (Plundrichs Kuppe), Suletice (Sulotice; Sulotitz; Sulloditz), Homole u Panny, Ústí nad Labem District, Ústí nad Labem Region, Czech Republic

Several localities near the Suletice village was described by Hibsch (1934). He is listing references back to 1903 for kaersutitic amphibole, but the knowledge of these localities may predate even these early references.
“Plundrichs Kuppe” Hill

The Plundrichs Kuppe Hill locality (SE of Suletice) is one of many localities for kaersutitic amphibole of the Ceske Stredohori Mts. The amphibole crystals are concentrated especially in the marginal porous part of the basaltic body.
Free kaersutitic amphibole and clinopyroxene crystals (“augites”) were collected in 1970’s on the fields below the Plundrich’s Kuppe Hill near the road to Homole village. The size of perfect columnar crystals of kaersutitic amphibole are up to 2.5 cm.
“Mückenhübel” ( Mückenkübel, Mickenhübel)

The Mückenhübel locality (ESE of Suletice) is one of the most traditional localities of kaersutitic amphiboles and clinopyroxenes (“augites”) up to more than 1 cm large in the Ceske Stredohori Mts. They originate from the tuffaceous (?) marginal part of a tephritic flow (Hibsch 1934).

The locality Mückenhübel was lost for a long time, but it was re-discovered by a coincident in 1996, when amphibole crystals were found in soil outside badger burrows. A more systematic approach revealed well-formed crystals of kaersutititc amphibole and clinopyroxenes in tuff outcrops in a 20 by 40 m area. The amphibole crystals are unevenly distributed in the rock.
The amphibole is here much more common than clinopyroxene and also reaches larger sizes. The size of the crystals varies from several mm to 2 cm, rarely up to 3-4 cm. In contrast, the size of clinopyroxene crystals exceeding 1 cm.
This is currently (2012) one of the more productive localities for kaersutitic amphibole and recent specimens from here are represented in collections across the central Europe.

In addition kaersutitic amphibole crystals can be found in other localities near Suletice ( 5-20km away), such as:

- Kostomlaty pod Milesovkou (up to 7 cm large crystals but often quickly disintegrating) in altered dyke (about 10 m) exposed in an abandoned coal pit

- Holomer in Usti nad Labem in altered volcanic breccia of a volcanic chimney

- Kaersutiteic amphiboles occur commonly in phenocrysts (2 to 30 mm) of prevailing part of alkaline dyke rocks (lamprophyre, semi-lamptrophyre, leucocratic derivatives as bostonite) forming swarms (~1000 dykes) radially arranged to the main intrusive center of the Ceske Stredohori Mts. in Roztoky (e.g., Techlovice and Dobkovice quarries)

Vlčí hora, Černošín, Tachov District, Plzeň Region, Czech Republic

The Vlčí Hora Hill (704 m) locality lies by Černošín close to Stříbro is a complex volcanic body in Western Bohemia formed in Miocene (11.7 Ma).

Two coexisting cogenetic volcanic series have been recognized in the broad area of West Bohemia: (i) weakly alkaline series basanite – trachybasalt – (basaltic) trachyandesite – trachyte – rhyolite (15.9-11.4 Ma) and (ii) strongly alkaline series olivine nephelinite – tephrite (16.5-8.3 Ma).

Vlčí Hora Hill belongs to the weakly alkaline series, and kaersutitic amphibole has been found both in basanitic rocks (prevalently xenocrysts) and their tuffs (free perfect crystals) often together with clinopyroxene (“augite” de facto diopside) crystals. Smaller crystal of kaersutitic amphibole occur also near the village Resanov in breccia filling of a chimney. Phenocrysts of kaersutitic amphibole occur also in trachyandesitic rocks of the weakly alkaline series.

The quantity, size and near perfect form of the kaersutitic amphibole and clinoporyxene crystals has made this locality known by collectors and scientists alike. Perfectly developed, slightly molted and pitted kaersutitic amphiboles in sizes up to 15 cm has been found, normally rimmed by clinopyroxene and titanian magnetite. Kaersutitic amphibole is usually found as single crystals, however, random intergrowths of several crystals may be found.

The kaersutitic amphiboles from Vlčí Hora is amongst the most oxidized amphiboles known, with Fe³⁺/Fe²⁺ ratios between 7-37. They are also rich in titanium, containing between 4.28-4.63 wt% thus being intermediate between ferroan oxo-pargasite, oxo-hastingsite and kaersutite with many minerals present. It is very tempting to follow J. Ulrych’s thoughts that the Ti>0,5apfu requirement in the definition of kaersutite sets an arbitrary line and “separates genetically uniform hornblendes even within one locality into several minerals. Hence, the adoption of a limit characterized by 0.35 apfu Ti seems to be at some localities more suitable”

Pyroxene (augite) is very often mineral at this locality. It forms up to circa 8 cm long crystals, often grown into polycrystalline aggregates.

Partly altered/transformed? olivine (forsterite) is characteristic mineral for the locality. It occurs as up to 3 cm large well-developed crystals which are often grown into the augite crystals. Other macroscopic minerals at the locality are: phlogopite , hyalite, phillipsite and aragonite.”

Greenland

Østerfjeld, Qaarsut, Nuussuaq Peninsula, Avannaata, Greenland

Qaersut is a small, remote village on the east coast of Greenland, and the type locality of kaersutite. The Qaersut amphibole was first described as a new mineral by Lorenzen (1884) on the account of its high Ti content. It took some time before kaersutite was acknowledged as a separate species as its optical properties was inseparable from other amphiboles, and chemistry was, at the time, one of many characteristics defining a mineral species.

Kaersutite was found in a nearly horizontal, 50m thick peridotite (picrite) sill penetrating Devonian sandstone. The peridotite sill is not homogenous, having some layers enriched in augite and a 1-2m wide doleritic band in the center. Benson (1939) describe numerous segregations of kaersutite-bearing pegmatite comprising a horizontal sheet 35-40cm thick traversing the upper portion of the sill” .

Kaersuitte is found as several cm long elongated crystals embedded in feldspar. Published analytical data from this rather unusual occurrence shows a Ti content between 0,9 and 1,2 apfu or +/- 10%wt TiO₂.

Germany

Radersberg quarry, Dreis-Brück, Daun, Vulkaneifel, Rhineland-Palatinate, Germany

Rothenberg Quarry, Bell, Mendig, Mayen-Koblenz, Rhineland-Palatinate, Germany

Korretsberg, Kruft, Pellenz, Mayen-Koblenz, Rhineland-Palatinate, Germany

The Eifel area lies in Western Germany, near the borders to Belgium and Luxembourg. This region is one of the most interesting areas in Europe for collectors of microcrystals. This is due to relatively recent tectonic events (the last 430.000 years), leading both to rifting and volcanic activity. There are several volcanoes in the area, with the Laacher See (13000 years old) as the youngest. An annual land-lift of 1-2mm shows that the area may still be active.

Several of these lavas contain phenocrysts of well-formed crystals. Although pyroxenes are most common, also titanian amphiboles can be found as phenocrysts in the volcanic rocks in the Eifel lavas. These amphiboles where originally termed “basaltic hornblende”, and modern analyses show that their composition falls within the titanian (oxo-)pargasite, (ferri-)kaersutite or titanian (oxo-) magnesio-hastingsite compositional fields. Mayer (2013) provides analytical data for several amphibole phenocrysts from the Röhn area. His data show a Ti content varying from roughly 0.45 to 0.6 apfu, with average slightly higher than 0.5 apfu. Also, the ferric iron content is variable, and some of his analyzed samples can be classified as ferri-kaersutite or (oxy)-hastingsites. Mayer also presents an aggregated formula: Na_0.3-0.5 K_0.3 Ca_1.7-1.9Na_0.3-0.1) ₂ (Mg_2.9-3.2Fe_1.1-1.3Al_0.2Ti_0.5-0.6 ) ₅ (Al_2.2 Si_5.8O₂₂)(O,OH_F0.1-0.5)₂ and concludes that he will call these amphiboles kaersutite.

Rothenberg Quarry, Bell, Mendig, Mayen-Koblenz, Rhineland-Palatinate, Germany

Caspar quarry, Ettringen, Vordereifel, Mayen-Koblenz, Rhineland-Palatinate, Germany

Nickenicher Sattel, Nickenich, Pellenz, Mayen-Koblenz, Rhineland-Palatinate, Germany

Ferri-kaersutite occurs as shiny dark brown to black prismatic crystals to a few mm. The mineral is identified by EMPA and SXRD. It occurs in vugs in lava xenoliths in several of the quarries in the Volcanic Eifel area. This type of occurrence is very unusual for a kaersutite-mineral, and it is speculated that a F-content can help stabilize kaersutite at the relatively low PT conditions where it formed.

Italy

Mount Etna, Etna Volcanic Complex, Metropolitan City of Catania, Sicily, Italy

Mt Etna is the largest active volcano in Europe today. The volcano reaches and altitude of 3315m and it's lavas covers 1260 km². The 600 000-year volcanic history is divided in four main evaluation stages:

1st stage: (580 to 225 ka) tholeiitic basalts which today can be found in outcrops out as pillow-lavas, hyaloclastites and sills along the Ionian Sea coast north of Catania.
2nd stage: (220 to 96 ka) The lava composition changes from tholeiitic to Na-alkaline (Branca et al. 2004). Several central volcanoes (Ancient Alkaline Centers or Timpe Volcanoes) were constructed over a time span of about 100 ka (172 to 96 ka), and their remnants mainly crop out along the present-day margin of Etna. It is in these ancient lavas kaersutitic amphibole can be found as well-formed crystals. Published data by Rruff.org of an amphibole crystal gives a kaersutite composition w/ Ti= 0,64afu.
3rd stage: (80-60ka) A series of effusive and explosive eruptions built a series of successive cones Successively, the so-called Trifoglietto unit
4th stage: (60ka-present): The building of the current stratovolacano.

During the various eruptive stages, the composition of the amphiboles has changed, from kaersutitic amphiboles in the ancient stage 2, via pargasites to magnesio-hastingsite in the latest 2001/2002 eruption.

Predazzo, Trento Province (Trentino), Trentino-Alto Adige (Trentino-South Tyrol), Italy

The Predazzo Intrusive Complex (PIC) is a ring-like shaped multi-pulse intrusion of 237.3 ± 1.0 Ma Age. It is composed by a several small intrusive bodies with an overall volume of about 4.5km 3. PIC rocks are grouped in three main units with different geochemical features, Shoshonitic Silica Saturated (SS, 3.1 km³), Granitic Unit (GU, 1.1 km³)173 and Shoshonitic Silica Undersaturated (SU, 0.3 km³). In addition, a swarm of lamprophyre dykes were emplaced around 20 Myr after the main intrusive event.
Amphiboles are present in the SS unit (magnesio-hornblende/actinolite), the SU unit (pargasite/hastingsite) and the lamprophyre dykes (kaersutitic amphibole). The lamprophyres are 20–200 cm in thickness and can be easily distinguished by their greenish color and the presence of up to 5 cm large, euhedral dark brown to black kaersutitic amphibole crystals. Amphiboles are a main constituent in the lamprophyres (35-55 vol%) and their composition is extremely variable between the less and the more differentiated samples, and varies from pargasite to ferri-kaersutite, Ti-rich magnesio-hastingsite and Ti-rich ferro-ferri-sadanagaite. Casetta et al. (2019) provides a detailed description and chemical analyses of a wide range of amphiboles in the lamprophyres. They differentiate between 5 different types, where their type 5 is most interesting for collectors, as this type includes the up to 5 cm large well-formed crystals. Unfortunately, only one of them are analyzed, but with a highly interesting result: “Sample MA1…. have (a) dark brown Ti-rich ferri-sadanagaitic to Ti-rich ferro-ferri-sadanagaitic core and pale brown Ti-rich magnesio-hastingsitic rim.”.

As these amphiboles are generally considered “kaersutite”, they are included in this article, and considered a kaersutitic amphibole. However, their composition can be highly variable and several other Ti-rich amphibole species may be present even in a single crystal.

Portugal

Sintra Complex, Sintra, Lisbon, Portugal

Ferri-kaersutite occurs in Late Cretaceous alkaline magmatism on the West Iberian Margin (WIM). The alkaline cycle took place in a post-rift setting, after oceanic break-up, and is contemporaneous of the opening of the Bay of Biscay and 35º counterclockwise rotation of Iberia.
Onshore, this cycle includes the Sintra, Sines and Monchique igneous complexes, the extrusive Lisbon Volcanic Complex as well as several other minor intrusions scattered in the Lusitanian and Algarve basins. The amphibole compositions in these igneous complexes are quite homogeneous, and analytical data provided in Miranda (2010) generally corresponds to ferri-kaersutite using Locock (2014) for normalizing the formula.

The Sintra igneous complex outcrops approximately 25 km west of Lisbon, having an emerged area of approximately 40 km². It extends underwater. The complex can be considered as being constituted by three main units, as follows: i) the Sintra granite, ii) the Cabo da Roca complex, a unit located in the western part of the complex and formed by amphibole rich gabbros (mafraites), quartz diorites, quartz syenites and igneous breccias and iii) the surrounding complex of dykes.

Ferri-kaersutite occurs in the gabbros and some of the dykes, both as groundmass composition and as phenocrysts, and the amphibole crystals can locally reach “pegmatitic” size.

Surprizingly, the amphibole composition in all Late Cretaceous alkaline magmatism on the Western Iberian Margin (WIM) is fairly homogenous and almost all analyzes (Miranda 2010) for amphiboles in Sintra, Sines and Monchique igneous complexes, the extrusive Lisbon Volcanic Complex as well as several other minor intrusions scattered in the Lusitanian and Algarve basins fall within the ferri-kaersutite compositional space.

Green, second generation amphiboles show a composition near the actinolite-edenite-magnesio-hornblende join.

Monte Suímo Mine, Queluz e Belas, Sintra, Lisbon, Portugal

This locality has been mined for pyrope garnets since Roman time, and ferri-kaersutite is found as megacrysts up to 6 cm in volcanic rocks belonging to the Lisbon Volcanic Complex.

New Zealand

Kakanui North & South Heads, Kakanui, Otago Region, New Zealand

Kaersutite constitutes an important part of the ultramafic inclusions in the mineral-breccia at Kakanui. It is associated with garnet, clinopyroxene and magnetite. The mineral-breccia is a mantle-sourced diatreme with associated marine reworked volcaniclastics. Mantle xenoliths include lherzolite and garnet pyroxenites occurring with megacrysts of garnet, clinopyroxene, kaersutite, and feldspar.

Kaersutite usually occurs as irregular crystals enclosed in the matrix. Occasionally, rounded, seemingly “polished” crystals up to 5 cm in diameter and 15 cm length can be found. The “polished“ surface is probably due to friction in the mineral breccia.
Analytical data suggest that the Ti content in the kaersutite lies between 4,98 and 5,87 wt% TiO₂

USA

Unnamed Kaersutite occurrence [1], Hoover Dam area, Minnesota Mining District, Mohave County, Arizona, USA

Kaersutite can be found as up to 10cm large megacrysts in camponite dikes. The best-known dyke, and also the source of most of the Hoover (Boulder) Dam kaersutites come from, is a road cut some 12-13km south of the dam itself. The dyke is more than a meter wide and the near vertical orientation give a four m exposure in the road cut. Kaersutite can also be found in other camptonite dikes in the area.

The kaersutite megacrysts gets larger towards the center of the dyke. It is believed that rapid cooling towards the walls of the dyke trapped the volatile elements within the dyke, thus allowing larger kaersutites to form towards the center of the dyke. The kaersutite seems to have grown rather rapidly. Campell and Schenk (1950) suggests 25 days.
Published data seems to indicate a Ti content ranging from 5,49-5,78%wt TiO2

References

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Ulrych, J., Novák, J., Lloyd, F., Balogh, K., & Buda, G. (2002). Rock-forming minerals of alkaline volcanic series associated with the Cheb-Domazlice Graben, West Bohemia. Acta Mineralogica-Petrographica, 43, 1-18.

Ulrych, J., Krmíček, L., Teschner, C., Skála, R., Adamovič, J., Ďurišová, J., ... & Radoň, M. (2018). Chemistry and Sr-Nd isotope signature of amphiboles of the magnesio-hastingsite–pargasite–kaersutite series in Cenozoic volcanic rocks: Insight into lithospheric mantle beneath the Bohemian Massif. Lithos, 312, 308-321.

Viccaro, M., Ferlito, C., & Cristofolini, R. (2007). Amphibole crystallization in the Etnean feeding system: mineral chemistry and trace element partitioning between Mg-hastingsite and alkali basaltic melt. European Journal of Mineralogy, 19(4), 499-511.

Wallace, R. C. (1977). Anorthoclase-calcite rodding within a kaersutite xenocryst from the Kakanui mineral breccia, New Zealand. American Mineralogist, 62(9-10), 1038-1041.

Wilkinson, J. F. G., & Hensel, H. D. (1991). An analcime mugearite-megacryst association from north-eastern New South Wales: implications for high-pressure amphibole-dominated fractionation of alkaline magmas. Contributions to Mineralogy and Petrology, 109(2), 240-251.

Yagi, K., Hariya, Y., Onuma, K., & Fukushima, N. (1975). Stability relation of kaersutite. Journal of the Faculty of Science, Hokkaido University. Series 4, Geology and mineralogy= 北海道大學理學部紀要, 16(4), 331-342.

Bilina town association of Nature Sciences
M. Fillippi: http://home.gli.cas.cz/filippi/pwww/mineralogie/suletice.html (Mückenhübel locality only)
Personal communication . J. Ulrych and M. Fillippi,

Mindat mineral pages, locality pages and photo captions

Revision History

Revision History

Revision no date description editor 1.0 2011 First Draft Olav Revheim 2.0 2020 Rewritten and reformatted Olav Revheim

Latest photo reviewed: 1037525