Eur. J. Mineral., 34, 451–462, 2022
https://doi.org/10.5194/ejm-34-451-2022© Author(s) 2022. This work is distributed under
the Creative Commons Attribution 4.0 License.

Ferri-taramite, a new member of the amphibole supergroup,from the Jakobsberg Mn–Fe deposit, Värmland, Sweden
Dan Holtstam1 , Fernando Cámara2 , Andreas Karlsson1 , Henrik Skogby1 , and Thomas Zack3
1 Department of Geosciences, Swedish Museum of Natural History,

P.O. Box 50007, 10405 Stockholm, Sweden
2 Dipartimento di Scienze della Terra “A. Desio”, Università degli Studi di Milano,

Via Luigi Mangiagalli 34, 20133, Milan, Italy
3 Department of Earth Sciences, University of Gothenburg, P.O. Box 460, 40530 Gothenburg, Sweden

Correspondence: Dan Holtstam (dan.holtstam@nrm.se)
Received: 22 June 2022 – Revised: 9 September 2022 – Accepted: 14 September 2022 – Published: 12 October 2022
W
Abstract. Ferri-taramite (IMA CNMNC 2021-046), ideally A NaB (CaNa)C (Mg3 Fe3+
2 )(Si6 Al2 )O22 (OH)2 , occurs in skarn from the Jakobsberg manganese mine, Värmland, Sweden. Associated minerals are celsian,phlogopite, aegirine-augite, andradite, hancockite, melanotekite, microcline (var. hyalophane), calcite, baryte,prehnite, macedonite and oxyplumboroméite. Conditions of formation, close to peak metamorphism (at circa
650 ◦ C and 0.4 GPa), include silica undersaturation, a slightly peralkaline character and relatively high oxygen fugacities. Ferri-taramite forms poikiloblastic crystals up to 5 mm and is dark brownish black with ayellowish grey streak. The amphibole is brittle with an uneven to splintery fracture. Cleavage parallel to{110} is good. Hardness (Mohs) is ∼ 6, and Dcalc = 3.227(5) g cm−3 . Holotype ferri-taramite has the ex2+
2+
3+
C
perimental unit formula A (Na0.79 K0.16 Pb0.01 )60.96 B (Ca1.26 Na0.72 Mn2+
0.02 )62 (Mg2.66 Mn0.58 Fe0.16 Zn0.02 Fe1.26
Al0.26 Ti0.06 )65.00 T (Al1.86 Si6.14 )68 O22 W (OH)2 , based on chemical analyses (EDS, laser-ablation ICP-MS) andspectroscopic (Mössbauer, infrared) and single-crystal X-ray diffraction data. The mineral is optically biaxial(–), with α = 1.670(5), β = 1.680(5) and γ = 1.685(5) in white light and 2Vmeas = 70(10)◦ and 2Vcalc = 70.2◦ .
Ferri-taramite is distinctly pleochroic in transmitted light, with X pale yellow, Y dark brown, Z yellowish brown
and absorption Y >Z>X. The eight strongest reflections in the X-ray powder pattern (d values (in Å), Irel , hkl)
are 8.44, 60, 110; 3.392, 25, 131; 3.281, 39, 240; 3.140, 100, 310; 2.816, 45, 330; 2.7104, 38, 151; 1.3654, 26,461; and 1.4451, 33, 661. Refined unit-cell parameters from single-crystal diffraction data are a = 9.89596(13),b = 18.015(2), c = 5.32164(7) Å, β = 105.003(13)◦ and V = 916.38(2) Å3 for Z = 2. Refinement of the crystal
structure yielded R = 2.26 % for 2722 reflections with Io >2σ (I ). The Mn2+ and Fe2+ ions show preference for
the M1 and M3 octahedrally coordinated sites, whereas Fe3+ is strongly ordered at M2. The A-group cations,
K and Na, are split over two subsites, A(m) and A(2), respectively.

1

Introduction

Members of the sodium–calcium subgroup oftheamphibolesupergroup(generalformulaAB2 C5 T8 O22 W2 ) associated with the root name taramite(Na(NaCa)Mg3 Al2 (Si6 Al2 )O22 (OH)2 ) are relatively rare.
They typically occur in alkaline igneous rocks and gneisses(e.g. Giret et al., 1980), retrogressed eclogites (Zhang andLiou, 1994), and some felsic lithologies that have experi-

enced ultrahigh-pressure metamorphism (Compagnoni andRolfo, 1999).
Ferrous compositions are the most frequent. The original “taramite”, reported from a nepheline syenite in theVali Tarama ravine, near Mariupol, Ukraine (Morozewicz,
1925), essentially represents a ferro-ferri-taramite in composition, following the current amphibole supergroup classification (Hawthorne et al., 2012). The “ferri-taramite” from
Bancroft, Ontario, Canada, investigated by Hawthorne andPublished by Copernicus Publications on behalf of the European mineralogical societies DMG, SEM, SIMP & SFMC.

452

D. Holtstam et al.: Ferri-taramite, a new member of the amphibole supergroup

Grundy (1978) is also a ferro-ferri-taramite. Other specimens of ferro-taramite and ferro-ferri-taramite have been described in metabasites from the Rakovec Group along thenorthern and eastern boundary of the early Palaeozoic of the
Gemeric Unit in Slovakia, metamorphosed under the highpressure type of greenschist facies (Faryad and Bernhardt,
1996). Similar compositions are reported for retrogressive
amphiboles in eclogites in the Aktyuz area, northern Kyrgyz Tian Shan, Kyrgyzstan (Takasu and Orozbaev, 2009).
Potassic-ferro-taramite from a metamorphosed monzonite,
Sierra de los Filabres, Andalusia, Spain, was described by
Oberti et al. (2008). Chemical analyses corresponding topotassic-ferro-ferri-taramite have been reported for amphiboles rimming arfvedsonite in ilvaite-bearing endoskarn ofheterogeneous nepheline syenitic marginal pegmatites in Ilímaussaq, South Greenland (Graser and Markl, 2008).
Regarding magnesian compositions, the “aluminomagnesiotaramite” from a kyanite–eclogite pod, near Selje,
Vestlandet, Norway, of Oberti et al. (2007a) corresponds
to the present root-name amphibole taramite. Taramite has
also been reported from the ultrahigh-pressure metamorphic
belt of the Dabie Mountains (Wang et al., 2000) as wellas in the Nybø eclogite pod (Norway), formed probably at
0.9–1.3 GPa and 650–720 ◦ C (Ungaretti et al., 1983), and inmetabasites at Cóbdar in Sierra de los Filabres, Andalusia,
Spain (Puga et al., 2002), formed at 550 ◦ C and 0.8 GPa.
Chemical analyses corresponding to potassic-ferri-taramite
have been reported in intergranular spaces of an orthopyroxenite xenolith from the Udachnaya-East kimberlite pipe,
Daldyn kimberlite field, Siberian platform (Rezvukhin et al.,2020), and interpreted as metasomatic, similar to conditionsin the Ilmenogorsky miaskite complex in the South Urals,
Russia (Makagonov et al., 2018).
The present paper is the full scientific characterizationof the C Fe3+ analogue of taramite. Its name, ferri-taramite,is thus dictated by the amphibole nomenclature in force(Hawthorne et al., 2012). The mineral was approved prior
to publication by IMA CNMNC (no. 2021-046). The material used here, a skarn sample from the Jakobsberg manganese mine in Sweden, was once examined by Flink (1914),
who noted the unusual character of the amphibole and described it as a “strange hornblende”. No chemical data werereported for the sample at the time. The holotype material isdeposited in the type mineral collection of the Department ofGeosciences, Swedish Museum of Natural History, P.O. Box
50007, 10405 Stockholm, Sweden, under collection number
GEO-NRM #19221254 (specimen and sections).

2

Figure 1. Type specimen, GEO-NRM #19221254, of ferri-taramite(brownish black aggregate on top) with mostly phlogopite (brown)
and celsian–baryte (whitish). Field of view 60 × 100 mm. Torbjörn Lorin photo.

banded skarn–carbonate masses (Magnusson, 1929). It is
one of the dolomitic marble-hosted Fe–Mn–(Ba–Pb–As–Sb–
Be) Långban-type deposits (Moore, 1970), in the Palaeoproterozoic Bergslagen ore region. They occur withinsupracrustal rocks predominated by ∼ 1.9 Ga rhyolitic
volcanic–volcaniclastic units, altogether regionally metamorphosed under amphibolite-facies conditions (with a peakat 600–650 ◦ C, 0.3–0.4 GPa) and to some extent also thermally affected by 1.85–1.78 Ga Svecokarelian intrusions(Björck, 1986; Sandström and Holtstam, 1999; Stephens andJansson, 2020). Genetically, Långban-type deposits constitute metamorphic equivalents of exhalative Mn–Fe deposits
in shallow marine environments (Boström et al., 1979; Holtstam and Mansfeld, 2001).
Ferri-taramite occurs as partly poikiloblastic, subhedral
crystals up to 5 mm, forming a dense aggregate in a mediumgrained skarn (Fig. 1). Associated minerals in the rock arecelsian, phlogopite, aegirine-augite, andradite, hancockite,melanotekite, microcline (var. hyalophane), calcite, baryte,prehnite, macedonite and oxyplumboroméite (Fig. 2). Celsian has largely suffered from alteration phenomena, leading
to heterogeneous aggregates of various Ba phases with poor
crystallinity (Fig. 3). Some portions are similar to cymrite(BaAl2 Si2 (O,OH)8 · H2 O) in composition, but this mineral
could not be confirmed by powder X-ray diffraction. Similar Ba–Pb–Mn–Fe skarn samples from Jakobsberg have been
described in the past (Holtstam and Langhof, 1994; Holtstam
et al., 2021), but no amphibole was detected, and hence ferritaramite might be considered relatively rare at the deposit.

Occurrence

At the Jakobsberg deposit (59.83◦ N, 14.11◦ E; 190 m a.s.l.),
1 km southeast of the Nordmark mine field, Filipstad,
Värmland, Sweden, separate hausmannite–braunite andmagnetite–hematite ores form distinct bodies adjacent toEur. J. Mineral., 34, 451–462, 2022

3

Physical and optical properties

Ferri-taramite has a short prismatic habitus, along [001]. The
colour of the crystals is dark brownish black (greenish yelhttps://doi.org/10.5194/ejm-34-451-2022

D. Holtstam et al.: Ferri-taramite, a new member of the amphibole supergroup

Figure 2. BSE-SEM image of ferri-taramite (Ftrm), with phlogopite (Phl), hancockite (Hnc) and melanotekite (Mtk). The atoll-likehancockite grain contains calcite and baryte (red arrow). The whitearrow points to prehnite. White specks in the amphibole crystal are
inclusions of macedonite. Sample GEO-NRM #19221254.

low to brown in splinters), with a yellowish grey streak. The
lustre is vitreous and semi-transparent, and no fluorescenceis observed under UV light. The amphibole is brittle withan uneven to splintery fracture. Cleavage parallel to {110}is good. Hardness (Mohs) is ∼ 6. Vickers hardness numbers
were obtained on a polished section of ferri-taramite using
a micro-hardness tester loaded with a 200 g weight, giving amean value of 919 (9.0 GPa) for a range of 733–1190 fromeight indentations. The density was not measured becauseof frequent inclusions of heavier minerals (e.g. macedonite);a calculated value is 3.227(5) g cm−3 based on the unit-cellvolume and atom contents. Ferri-taramite is slightly attracted
by a neodymium magnet. It is insoluble in HCl and HNO3 .
The optical character is biaxial (−), with α = 1.670(5),β = 1.680(5) and γ = 1.685(5) in white light and 2Vmeas =70(10)◦ and 2Vcalc = 70.2◦ . Pleochroism is strong in transmitted light, with X pale yellow, Y dark brown, Z yellowish
brown and absorption Y >Z>X.

4

Chemical composition

The chemical composition (Table 1) was primarily determined using an FEI Quanta 650 field-emission scanning electron microscope, fitted with an 80 mm2 X-MaxN Oxford Instruments EDS detector (20 kV, beam size >1 µm, working
distance 10 mm). The beam current was calibrated on Co
metal, with the instrument calibrated against metal and mineral standards for each element. The number of point analyses is 10. F and Cl were below detection. Contents of major,
minor and other trace elements (Table 2) were also determined with laser-ablation ICP-MS analysis (an NWR 213 nm
laser coupled to an Agilent 8800 MS/MS) at the University
of Gothenburg, with 16 analysed spots. Element oxide quanhttps://doi.org/10.5194/ejm-34-451-2022453

tification was performed by normalizing to 100 wt %, assuming 2 wt % H2 O and the Fe2+ / Fe3+ ratio from Mössbauer
data. We used a multi-standard approach, with measuringcalibration factors for each major element from a wide spectrum of known standard materials: NIST SRM 610, ATHOG, BCR-2G, BHVO-2G, GSC-1G, GSD-1G, Kakanui amphibole, NKT-G, T1-G and TB-1G (all data from the GeoReM database, except for Kakanui amphibole, which is from
unpublished electron microprobe data). Consistency of calibration factors is generally better than 4 %, confirming an
excellent accuracy when compared with EDS data (Table 1).
NIST SRM610 was used as the only primary standard fortrace element quantification. The elements P, Cl, Br, Cs, W,
Tl, Ta, Bi, Th and U were found to be at or below the level ofdetection.
The empirical formula of ferri-taramite derived from
EDS data and calculated on the basis of 24 (O, OH) is
2+
A (Na
B
0.79 K0.16 Pb0.01 )6=0.96 (Ca1.26 Na0.72 Mn0.02 )6=2
2+
2+
3+
C (Mg
2.66 Mn0.58 Fe0.16 Zn0.02 Fe1.26 Al0.26 Ti0.06 )6=5.00
T (AlW
1.86 Si6.14 )6=8 O22 (OH)2 . The ideal formula is3+
Na(NaCa)(Mg3 Fe2 )(Si6 Al2 )O22 (OH)2 ,corresponding
to the composition SiO2 41.01 wt %, Al2 O3 11.60 wt %,Fe2 O3 18.16 wt %, MgO 13.75 wt %, CaO 6.38 wt %,Na2 O 7.05 wt % and H2 O 2.05 wt %, totalling 100.00 wt %.
5
5.1

X-ray diffraction data and structure refinement
Powder data

Powder X-ray diffraction (pXRD) data were collectedwith a PANalytical X’Pert3 powder diffractometer equippedwith an X’Celerator silicon-strip detector and operated
at 40 mA and 45 kV (CuKα radiation, λ = 1.5406 Å).
The monoclinic, space group C2/m unit-cell parameters refined from the powder data (29 reflections in the2θ range 9–70◦ ), using least squares with minimization on
Q = 1/d 2 (Holland and Redfern, 1997), are a = 9.9019(9) Å,
b = 18.0316(16) Å, c = 5.3248(9) Å, β = 105.008(8)◦ andV = 918.31(16) Å3 for Z = 2. The complete set of X-ray
powder diffraction data is shown in Table 3.
5.2

Crystal structure refinement

A single-crystal X-ray diffraction (SC-XRD) study was doneon a 146×213×342 µm fragment (Fig. 4) using a Rigaku Oxford Diffraction XtaLAB Synergy diffractometer, equippedwith a PhotonJet (Mo) X-ray source operating at 50 kV and
1 mA, with monochromatized MoKα radiation and equippedwith a HyPix detector working at 62 mm from the crystal. A
combination of ω scans at different values of φ, χ and θ positions, with a step scan of 0.5◦ and exposure time of 2 s perframe, was used to maximize redundancy and data coverage.
High-resolution data were collected (up to 0.46 Å).

Eur. J. Mineral., 34, 451–462, 2022

454

D. Holtstam et al.: Ferri-taramite, a new member of the amphibole supergroup

Table 1. Chemical data (in wt %) for ferri-taramite obtained with EDS and laser-ablation (LA) ICP-MS analyses.
EDS, n = 10

LA-ICP-MS, n = 16

Constituent

Mean

2σ

Range

Mean

2σ

Range

Na2 O
MgO
Al2 O3
SiO2
K2 O
CaO
TiO2
MnO
Fe2 O3 *
FeO∗
ZnO
PbO
BaO
H2 Ocalc

5.26
12.06
12.15
41.43
0.83
7.92
0.50
4.81
11.30
1.32

0.18
0.28
1.22
0.62
0.06
0.29
0.12
0.22
0.45
0.06

5.11–5.42
11.90–12.40
11.61–13.25
40.71–41.73
0.77–0.89
7.53–8.04
0.37–0.58
4.64–4.98
11.07–11.73
1.28–1.36

0.22
0.35
0.59
0.65
0.05
0.27
0.06
0.19
0.44
0.06
0.01
0.16
0.005

5.50–5.87
11.90–12.38
11.09–12.05
40.55–41.76
0.80–0.87
7.78–8.22
0.39–0.51
4.35–4.68
11.11–11.90
1.47–1.58
0.13–0.16
0.22–0.52
0.05–0.06

2.02

5.66
12.14
11.59
41.25
0.84
8.01
0.46
4.57
11.51
1.53
0.15
0.27
0.05
2.02

Total

99.60

100.00∗ The Fe2+ / Fe3+ ratio is derived from Mössbauer data. H O is calculated on the basis of OH = 2 apfu.
2Figure 3. Ferri-taramite with phlogopite, andradite (Adr) and macedonite (Mce). The irregular brighter areas correspond to altered Bafeldspar. Sample GEO-NRM #19221254.
Figure 4. Crystal fragment of ferri-taramite used for SC-XRD
study. Sample GEO-NRM #19221254.

The crystal structure of ferri-taramite was refined starting from the atom coordinates of sample Q99-3 of Oberti etal. (2007a) (named “alumino-magnesiotaramite” in the paper). Scattering curves for fully ionized chemical species
were used at sites where chemical substitutions occur; neutral vs. ionized scattering curves were used at the T (2)and anion sites. Scattering at T (1) sites was fixed at the
54 : 46 Si4+ : Al3+ ratio as deduced form application of theequation of Oberti et al. (2007b) and in agreement withchemistry. Scattering curves for neutral and fully ionizedatoms were taken from International Tables for Crystallography (Wilson, 1992). Splitting of the electron density
at site A was observed and added to the model as A(2)Eur. J. Mineral., 34, 451–462, 2022

and A(m) sites. Full-matrix least-squares refinement on F 2
yielded Robs = 2.26 % (2722 reflections with Io >2σ (I )) andRall = 2.54 % (2983 reflections) using SHELXL (Sheldrick,2015). See Table 4 for experimental details. Refined atom
coordinates, site scattering and equivalent isotropic displacement parameters are reported in Table 5. Selected interatomic
distances and bond angles are given in Table 6. Site populations for ferri-taramite have been derived from the unit formula and the results of the structure refinement (Table 7).
There is an excellent agreement between the refined valuesof site scattering (ss, electrons per formula unit) and meanhttps://doi.org/10.5194/ejm-34-451-2022

D. Holtstam et al.: Ferri-taramite, a new member of the amphibole supergroup
Table 2. Trace element composition of ferri-taramite (µg g−1 ).

As
B
Be
Ce
Co
Cr
Cu
Ga
Ge
Hf
In
La
Li
Lu
Mo
Nb
Ni
Rb
Sb
Sc
Sn
Sr
V
Y
Zr

Table 3. X-ray powder diffraction data (d in Å) for ferri-taramite.

Mean(2σ )

Min

Max

Iobs

Icalc

dobs

dcalc

h

k

l

19(1)
5.5(8)
84(5)0.4(1)
114(2)
294(19)13(7)17(1)
1.2(0.3)
0.9(1)
0.07(1)0.08(1)72(4)0.09(1)1.7(1)
0.04(1)231(7)
1.8(2)
5.1(7)52(1)0.5(1)
17(1)
6.1(2)
1.5(1)
37(2)

18
4.1
75
0.3
109
242
6
15
0.7
0.6
0.06
0.06
66
0.07
1.5
0.02
216
1.5
3.8
49
0.3
15
5.7
1.2
34

21
7.2
91
0.4
117
309
28
18
1.9
1.3
0.09
0.10
81
0.11
1.9
0.06
244
2.0
6.3
54
0.6
18
6.4
1.6
42

5
60
8
4
25
39
100
20
45
20
38
23
17
8
24
17
11
24
8
17
14
5
5
26
13
9
10
13
33
13

32
89
23
2
66
29
66
30
20
34
100
53
66
4
42
12
18
35
15
18
6
4
2
13
4
13
13
10
31
5

9.01
8.44
4.51
4.22
3.392
3.281
3.140
2.951
2.816
2.750
2.71042.59492.55792.38852.34732.33982.29692.16542.03302.02181.90211.86551.82241.65403
1.63997
1.61565
1.54585
1.50261
1.445141.36983

9.02
8.45
4.51
4.22
3.391
3.280
3.139
2.950
2.816
2.749
2.71012.59482.55802.38862.34732.33822.29712.16522.03322.02171.9022
1.86561.82281.65396
1.640111.61568
1.54594
1.502631.445021.36989

0
1
0
2
1
2
3
2
3
3
1
0
2
3
3
4
3
2
4
3
5
1
5
4
4
1
6
0
6
5

2
1
4
2
3
4
1
2
3
3
5
6
0
5
5
2
1
6
0
5
1
9
3
6
8
11
0
12
6
1

0
0
0
0
1
0
0
1
0
1
1
1
2
0
1
1
2
1
2
1
0
1
0
1
0
0
2
0
1
2

bond lengths (mbl’s, Å) and those calculated based on the
proposed site populations. A crystallographic information
file (CIF) containing observed structure factors has been deposited in the Supplement.

6
6.1

455

Spectroscopic data
Micro-Raman spectroscopy

A Raman spectrum of ferri-taramite (Fig. 5) was collected from a randomly oriented, polished crystal on a
LabRAM HR 800 micro-spectrometer, using a 514 nm Arion laser source at < 1 mW power, a Peltier-cooled (−70 ◦ C)
1024 × 256 px CCD detector (Synapse), an Olympus MPlan
N 100×/0.9 NA objective and a laser spot of ca. 3 µm. A
600 grooves cm−1 grating was used, and the resolution isabout 1 cm−1 . Spectral positions were corrected against the
Raman band at 789 cm−1 of a SiC-6H crystal measured on{0001}. Instrument control and data acquisition (range 50–
4000 cm−1 , 10 s exposure time in 20 cycles) were made with
the LabSpec 5 software.
The Raman band at ca. 3700 cm−1 is related to O–Hstretching vibration modes. Multiple bands in the region
800–1000 cm−1 are ascribed to Si–O and T Al–O symmetricand antisymmetric stretching. The peak at ca. 680 cm−1 ishttps://doi.org/10.5194/ejm-34-451-2022

Note: the seven strongest Bragg reflections are in bold.

assigned to C Al–O stretching, whereas the one at 669 cm−1
corresponds the bending of Si–O–Si bridges (see Waeselmann et al., 2020). The strong peak at 536 cm−1 (with ashoulder at ca. 500 cm−1 ) is tentatively assigned to stretching vibrations of Fe3+ –O octahedra and the one at 370 cm−1
to Mg–O vibrations.
6.2

Fourier-transform infrared (FTIR) spectroscopy

Polarized single-crystal FTIR spectra were collected in therange 2000–10000 cm−1 at a spectral resolution of 2 cm−1 on
a 50×100 µm raster, with a Bruker Vertex 70 spectrometer attached to a Bruker Hyperion 2000 IR microscope. Measurements were done from a 58 µm thick doubly polished singlecrystal fragment oriented parallel (010). The spectra (Fig. 6)
show a distinct absorption band at 3713 cm−1 pronounced
in the X direction and caused by O–H-stretching vibrationsof the OH dipole at the O(3) position, typical of local A Na–
MgMgMg–SiAl atomic nearest-neighbour and next-nearestneighbour arrangements of cations around the O(3) atom
Eur. J. Mineral., 34, 451–462, 2022

456

D. Holtstam et al.: Ferri-taramite, a new member of the amphibole supergroup

Table 4. Crystal data and experimental conditions for SC-XRD study of ferri-taramite.
Temperature
Wavelength
Crystal system
Space group
Unit-cell dimensions

Unit-cell volume
Z
Absorption coefficient
Absorption correction
F (000)θ range for data collection
Index ranges
Reflections collected
Independent reflections
Completeness to θ = 25.24◦
Refinement method
Data/restraints/parameters
Goodness of fit on F 2Final R indices (I >2σ (I ))R indices (all data)
Largest diff. peak and hole298(2) K
0.71073 Å
Monoclinic
C2/m (no. 12)
a = 9.89596(13) Å
b = 18.015(2) Å
β = 105.003(13)◦c = 5.32164(7) Å
916.38(2) Å3
2
2.69 mm−1
Multi-scan873
2.26 to 40.64◦−18 ≤ h ≤ 18, −32 ≤ k ≤ 32, −9 ≤ l ≤ 5
17 7092983 (Rint = 2.43)
100 %Full-matrix least squares on F 2
2983/1/121
1.049
R1 = 0.0226, wR2 = 0.0610
R1 = 0.0254, wR2 = 0.0625
1.27 and −0.99 e− Å−3

Figure 5. Raman spectrum of ferri-taramite, obtained with a 514 nm
laser.

(Hawthorne and Della Ventura, 2007). The interatomic distance from the H atom to the O(7) receptor of 2.67 Å is ingood agreement with the main band at 3700 cm−1 , basedon the known empirical correlations (Libowitsky, 1999). The
shoulder band at ca. 3670 cm−1 is possibly related to the partial vacancies at the A site. Local A Na–MnMgMg–SiAl arrangements as a substitution of Mg by Mn2+ at M(1,3) is expected to cause a band shift of at least −15 cm−1 (see Reece
et al., 2002; Hawthorne and Della Ventura, 2007), which may
contribute to the observed spectrum.

Eur. J. Mineral., 34, 451–462, 2022

Figure 6. Polarized single-crystal FTIR spectra of ferri-taramite.
Sample thickness is 58 µm.

6.3

Optical absorption spectroscopy

Polarized optical absorption spectra (Fig. 7) were measured on an X–Z crystal section of ferri-taramite (same asused for FTIR). The spectra were recorded in the visible
range (350–800 nm) with an AvaSpec-ULS2048x16 spectrometer attached to a Zeiss Axiotron UV microscope. A
xenon lamp (75 W) was the light source, and Zeiss Ultrafluar 10× lenses were used as the objective and condenser.
The size of the aperture was 30 µm in diameter on the sample. A Glan–Thompson calcite prism served as the polarizer.
The spectra show a significant absorption edge towards thehttps://doi.org/10.5194/ejm-34-451-2022

D. Holtstam et al.: Ferri-taramite, a new member of the amphibole supergroup

457

Table 5. Refined atom coordinates and equivalent isotropic displacement parameters.
Atom

Site occ.

x/a

y/b

z/c

Ueq

O(1)

O0 0.23(4)O= 0.77(4)0.10680(6)0.08981(3)0.21568(11)0.00961(10)O(2)

O0 0.35(4)O= 0.65(4)0.12045(6)0.17356(3)0.73542(11)0.00916(10)O(3)

O0 0.62(6)O= 0.38(6)0.10932(9)00.71219(17)0.01082(14)O(4)

O0 0.49(3)O= 0.51(3)0.36651(6)0.25032(3)0.79146(11)0.01046(10)O(5)

O0 0.35(4)O= 0.65(4)0.35070(6)0.13886(4)0.10716(11)0.01279(11)O(6)

O0 0.38(4)O= 0.62(4)0.34315(6)0.11678(4)0.60895(12)0.01264(11)O(7)

O0 0.25
O= 0.75

0.33796(10)00.27754(19)0.01561(16)T (1)Si4+ 0.54
Al3+ 0.45

0.28047(2)0.08614(2)0.30215(4)0.00604(5)T (2)Si0 0.41(2)Si4+ 0.59(2)0.29088(2)0.17277(2)0.81262(4)0.00648(5)M(1)

Mn2+ 0.216(3)Mg2+ 0.784(3)00.08949(2)1/2

0.00755(10)M(2)

Fe3+ 0.680(2)Mg2+ 0.320(2)00.17851(2)00.00750(6)M(3)

Mn2+ 0.270(3)Mg2+ 0.730(3)

0

0

0

0.00689(12)M(4)

Ca2+ 0.601(2)Na+ 0.399(2)00.28056(2)1/2

0.00992(10)A(m)

K+ 0.030(5)0.048(3)1/2

0.097(5)0.042(6)A2

K+ 0.033(7)Na+ 0.437(7)00.4809(2)00.0544(17)H

10.194(4)00.769(6)0.064(10)UV, most pronounced in the Z direction. A set of absorption bands caused by spin-forbidden electronic d–d transitions are superimposed on the background. Narrow bands located at ca. 24 500 and 23 000 cm−1 mark field-independenttransitions in Mn2+ and Fe3+ , respectively. Broader bands
at higher wavelengths, ca. 14 000 cm−1 , could be related
to Fe2+ → Fe3+ or Fe2+ → Ti4+ charge transfer between
neighbouring amphibole octahedra (Burns, 1993).
6.4

Mössbauer spectroscopy

An 57 Fe transmission Mössbauer spectrum (Fig. 8) was obtained from a 20 mg powder absorber using 57 Co γ rahttps://doi.org/10.5194/ejm-34-451-2022

diation and a constant-acceleration spectrometer (WissEl).
Two-mirror image spectra (± 4.28 mm s−1 ) were collected
at 54.7◦ “magic angle” geometry to avoid texture effects,
during 70 h over 1024 channels, and calibrated against a
25 µm thick α-iron foil. The baseline of the resulting folded
spectrum halted at 6.94 × 106 counts. The MossA software(Prescher et al., 2012) was employed for spectrum analysis, under the assumption of Lorentzian line shapes and a“thin” absorber. A pair of doublets is dominant, with a centroid shift (CS) of 0.388(5) mm s−1 and quadrupole splitting(QS) of 0.53(2) and 0.79(2) mm s−1 , indicative of Fe3+ at
an octahedrally coordinated cation site (M(2)) with varying nearest-neighbour cation arrangements. A small contri-

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458

D. Holtstam et al.: Ferri-taramite, a new member of the amphibole supergroup

Table 6. Selected interatomic distances (Å) and angles (◦ ) in ferritaramite.
T (1)–O(1)T (1)–O(5)T (1)–O(6)T (1)–O(7)1.6614(6)1.6838(6)1.6825(6)1.6695(4)T (2)–O(2)T (2)–O(4)T (2)–O(5)T (2)–O(6)1.6293(6)1.6025(6)1.6432(6)1.6584(6)hT (1)–Oi

1.674

hT (2)–Oi

1.633

M(1)–O(1) ×2
M(1)–O(2) ×2
M(1)–O(3) ×2
hM(1)–Oi
M(3)–O(1) ×4
M(3)–O(3) ×2
hM(3)–Oi

A(2)–O(5) ×2
A(2)–O(6) ×2
A(2)–O(7) ×2
hA(2)–Oi
A(m)–O(5) ×2
A(m)–O(5) ×2
A(m)–O(6) ×2
A(m)–O(7)A(m)–O(7)hA(m)–Oi

2.0577(6)2.1238(6)2.1005(6)2.094

M(2)–O(1) ×2
M(2)–O(2) ×2
M(2)–O(4) ×2
hM(2)–Oi

2.0880(6)2.0689(6)1.9651(6)2.040

2.0133(6)2.0914(6)M(4)–O(2) ×2
M(4)–O(4) ×2

2.4359(6)2.3497(6)2.099

M(4)–O(5) ×2
M(4)–O(6) ×2

2.6574(7)2.5752(7)2.757(3)2.857(3)2.4396(10)hM(4)–Oi

2.505

A(2)–A(2)A(2)–A(m)A(m)–A(m)0.689(8)0.69(3)
1.20(6)

O(3)–H

0.81(4)2.694
3.180(17)3.002(12)2.677(18)2.50(2)2.53(2)

T (1)–O(5)–T (2)T (1)–O(6)–T (2)T (1)–O(7)–T (1)133.90(4)137.29(4)136.70(6)O(5)–O(6)–O(5)O(6)–O(7)–O(6)162.72(8)100.46(8)2.845

bution, ca. 12 % of total absorption as determined from area
ratios (with identical recoil-free fractions assumed for all
Fe sites), emanating from another doublet at CS = 1.11(1)and QS = 2.60(2) mm s−1 is attributed to Fe2+ in octahedral
coordination (M(1) and M(3) sites). Line widths (FWHM)
were in the range 0.28(2)–0.35(2) mm s−1 , with a χ 2 valueof 0.9 for the fitting result.

7
7.1

Figure 7. Polarized single-crystal optical spectra of ferri-taramite.

Discussion
Crystal structure and chemistry

Site populations (Hawthorne et al., 1995) were calculated
based on present knowledge of amphibole crystal chemistry.
The results are reported in Table 7. Here we describe the different cation and anion groups.
T sites. The observed hT (1)–Oi distance is in perfectagreement with the calculated values using the equations ofOberti et al. (2007b; see Tables 6 and 7) and the chemical
analyses. Therefore, the 54 : 46 Si4+ : Al3+ ratio was fixed atEur. J. Mineral., 34, 451–462, 2022

Figure 8. Transmission 57 Fe Mössbauer spectrum of ferri-taramite.
Subspectra no. 1 (59 %) and no. 2 (29 %) correspond to M2 Fe3+ ,and no. 3 corresponds to M1,M3 Fe2+ (12 %).

the last stages of refinement. The limited presence of Al in
the T (2) sites assumed in Table 7 (2 % per site) is observedin high-temperature high-T Al amphiboles, in agreement withpeak conditions for its crystallization (see paragenesis section).
C-group cation sites. On the basis of the observed meanbond lengths, for C Mn2+ the following (strong) site preference is inferred: M(1) = M(3)  M(2). This is similar towhat is expected for C Fe2+ according to present knowledgeof amphibole crystal chemistry (see the review in Oberti etal., 2007b), and it is related to the structural relaxation ofM(1) and M(3) sites as a consequence of the size reductionof the adjacent M(2) sites. As in other taramitic amphibole
samples (Oberti et al., 2007a), the observed mean octahedral
distances are larger than the calculated values, although in
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D. Holtstam et al.: Ferri-taramite, a new member of the amphibole supergroup

459

Table 7. Site occupancies for ferri-taramite with site scattering (ss) and mean bond lengths (mbl’s).
Site

Site population (apfu)

T (1)
T (2)
M(1)
M(2)
M(3)

2.14 Si4+ + 1.86 Al3+

ss (epfu)
Refined6 C cations
B cations
A cations
W anions

Calculated

RefinedCalculated

29.62
43.04
15.52

29.83
43.16
15.65

1.675
1.633
2.094
2.040
2.099

1.675∗
1.633
2.096
2.025
2.101

88.18
32.81
12.02

88.64
33.62
12.55

3.92 Si4+ + 0.08 Al3+
1.56 Mg2+ + 0.33 Mn2+ + 0.11 Fe2+
1.26 Fe3+ + 0.37 Mg2+ + 0.26 Al +0.06 Ti4+ + 0.04 Mn2+ + 0.01 Fe2+
0.73 Mg2+ + 0.21 Mn2+ + 0.04 Fe2+ + 0.02 Zn2+
1.26 Ca2+ + 0.72 Na + 0.02 Mn2+
0.79 Na+ + 0.16 K+ + 0.01 Pb2+2 OH−

mbl (Å)∗ Using the equation of Oberti et al. (2007b).

this case the differences are within 0.002 Å, probably related
to the fact that the presence of Fe3+ in M(2) does not allow
for a strong relaxation of this site. In fact, the observed meanoctahedral bond length for M(2) site is larger than the calculated value (Table 7). At any rate, the very good agreement
between observed and calculated site scattering (a remarkable one) is obtained considering some disordering of Mn2+
and Fe2+ among the C sites, probably due to the relatively
high T of crystallization in the amphibolite facies (see thefollowing).
B-group cation sites. The M(4) site shows the typical y/bcoordinate of a Ca and/or Na populated site. No evident
residual electron density has been found around the M(4)sites in agreement with the absence of Mg and negligible
Mn2+ at the B-group sites, based on the chemical analyses.
A-group cation sites. The A cations are preferentially ordered, with K at the A(m) site (0.066 apfu of K) and Na(0.873 apfu of Na and minor 0.06 apfu of K) at the A(2)subsite (0.57 and 10.87 epfu, respectively). Both K and Na
contents agree reasonably well with the chemical analysis (Na0.79 K0.16 Pb0.01 ). The main preference for A(2) (seeFigs. 9 and 1 of Oberti et al., 2007a, for comparison) is also
observed in ferro-taramite and taramite related to the preferred local arrangement M(4) Ca–O(3) OH–A(2) Na, althoughhigher occupancy of A(m) sites would be expected due tothe local arrangement M(4) Na–O(3) OH–A(m) Na. This might
be due to the absence of O(3) F, responsible for ordering at
the A(m) sites observed in fluoro-taramite (Oberti et al.,2007a). When the A site is dominantly populated by K, likein potassic-ferro-taramite, strong ordering of K at the A(m)site is also observed even in the absence of F at O(3) (Oberti
et al., 2008).
W anion sites. Despite a relatively high Ti content of
0.06 apfu, there is no indication of deprotonation and existence of an oxy-component (W O2− ) in ferri-taramite, whichis consistent with the metamorphic origin of ferri-taramite(see Oberti et al., 2015b).

https://doi.org/10.5194/ejm-34-451-2022

Figure 9. A section of the Fo map calculated parallel to (201) andcentred at 0, 1/2, 0 for ferri-taramite, showing the distribution of
the electron density within the A cavity. The b axis is horizontal,−1
and contours are drawn with steps of 1 e Å starting from 1.

7.2

Trace elements

Ferri-taramite from Jakobsberg is low in most trace elements.
Increased levels, compared to the continental-crust average,
are however seen for Be, As, Sb and Pb, which can be considered a Långban-type signature reflecting the general enrichment of these elements in the skarn (Holtstam and Mansfeld,
2001). There is also a significant concentration of the transition elements Sc, Cr, Co, Ni and Zn. Global comparisons
are hampered by the fact that comprehensive trace element
data for amphiboles of an unmistakable non-igneous origin
are very rare. Cr and Co concentrations are slightly enrichedcompared to an amphibolite-grade hornblende from the Njurundukan mafic complex, Baikal, Russia (samples 487, 499,
23 and 54/3 in Skublov and Drugova, 2003). Concentrations for other elements available for comparison, such as
Eur. J. Mineral., 34, 451–462, 2022

460

D. Holtstam et al.: Ferri-taramite, a new member of the amphibole supergroupY, La, Ce, Lu, Hf and Ta, are significantly lower in ferritaramite. This effect can possibly be explained (in the case ofREE) by the coeval crystallization of ferri-taramite with hancockite that has an epidote-type structure. Amphibole in amagmatic-influenced skarn can show considerably higher Sr,
Rb, Sn and Ta contents but is generally lower in the period4 transition elements (e.g. Žáček, 2007) than seen for ferritaramite. The partitioning behaviour of trace elements amongmajor skarn-forming minerals (where there is no melt phasepresent) is, however, essentially unexplored.
7.3

Paragenesis

Amphibole in Mn skarn assemblages is common inLångban-type deposits and mostly occurs as sodic–calcic,
aluminium-poor members, 6T ∼ 8Si, of the richterite–
potassic–richterite series (Sundius, 1945; Holtstam et al.,2019a). Although hastingsitic and pargasitic members(6T ∼ 6Si + 2Al) are reported as well (e.g. Christy and
Gatedal, 2005; Hålenius and Bosi, 2012), they are less frequently encountered. Specimens are Mn-bearing to various
extents, with Mn2+ acting as both B- and C-group cations.
In the case of rare hjalmarite, B Mn > B Ca (Holtstam et al.,2019b).
The rock with ferri-taramite formed during regional metamorphism as is the case for the above-mentioned amphiboles
in general. In a possible scenario, precipitates of Fe–Mn(hydroxy-)oxides, Ca–Mg–Ba–Pb carbonates and siliceous
material of hydrothermal origin were mixed with aluminous detritus and reacted to eventually form a skarn assemblage of amphibole, mica, feldspar, clinopyroxene and Pb
silicates. The alkali metals have probably originally been
derived from metasomatic alteration of the felsic volcanic
units (see Magnusson, 1930). Conditions for ferri-taramite
formation, close to peak-metamorphism (at circa 650 ◦ C and
0.4 GPa), demonstrably included silica undersaturation, aslightly peralkaline character and relatively high oxygen fugacities of the system. Obviously, hydrous alteration has affected the Jakobsberg skarn at some point, but the amphibole
shows little sign of breakdown (limited prehnite formation).
Katophorite, also a rare species (Oberti et al.,2015a), can be considered an intermediate amphibole composition between richterite and taramite,
related by the exchange C Mg5 +T Si8 → C (Mg4 Al)+T (AlSi7 ) →C (Mg3 Al2 ) +T (Al2 Si6 ) (or with C Fe3+
instead of C Al, for the “ferri-” members). It is however not
known from the Långban-type deposits. Although the properbulk compositions could likely be achieved in the rocks
present, katophoritic amphiboles seem to belong to a highpressure domain (Harlow and Sorensen, 2005; Pirard andHermann, 2015; Oberti et al., 2015a). Ferri-taramite must
be a rare composition since we have found very few verified
analyses elsewhere in the literature (see Schumacher, 2007).
In addition, the present specimen is the first example ofa taramitic amphibole from a skarn, not associated with
Eur. J. Mineral., 34, 451–462, 2022

rock types of magmatic origin. The closest composition toferri-taramite has been reported from eclogites in the Aktyuz
area, northern Kyrgyz Tian Shan, Kyrgyzstan (Takasu
and Orozbaev, 2009), but without a direct Fe2+ / Fe3+
determination and with very similar Fe3+ and AlV I content,
it is difficult to discern if these samples are ferri-taramite
or taramite. In the Ilmenogorsky complex in the South
Urals, analysis no. 49 of Nikandrov et al. (2000) can be alsoclassified as ferri-taramite, although it is richer in Fe3+ thanour sample from the type locality. Similar compositions arereported by Makagonov et al. (2018) from the same locality,
but Ca at the B site of the amphibole is 1.49 apfu, and theamphibole is therefore very close to magnesio-hastingsite incomposition.

Data availability. A CIF file is deposited in the Supplement below.

Supplement. The supplement related to this article is available online at: https://doi.org/10.5194/ejm-34-451-2022-supplement.

Author contributions. DH and AK measured optical and physicalproperties. DH and HS obtained and interpreted spectroscopic data.
AK and TZ performed the chemical analyses. FC collected singlecrystal X-ray diffraction data and executed the structural refinement. DH and FC wrote the manuscript, in consultation with all
authors.

Competing interests. The contact author has declared that none of
the authors has any competing interests.

Disclaimer. Publisher’s note: Copernicus Publications remains
neutral with regard to jurisdictional claims in published maps andinstitutional affiliations.

Acknowledgements. Torbjörn Lorin is thanked for the colour photograph of ferri-taramite in Fig. 1.

Financial support. This research has been supported by the grantRicerca Locale 2020; Università di Milano; and the Italian Ministry of Education, University and Research (MIUR) through the
project “Dipartimenti di Eccellenza 2018–2022”. Publication costs
were covered by the Finneman fund.

Review statement. This paper was edited by Rossella Arletti andreviewed by two anonymous referees.

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D. Holtstam et al.: Ferri-taramite, a new member of the amphibole supergroup
References
Björck, L.: Beskrivning till berggrundskartan Filipstad NV, Sver.
Geol. Undersök., Swedish Geological Survey, series Af, 147, 1–
110, 1986.
Boström, K., Rydell, H., and Joensuu, O.: Långban – An exhalative sedimentary deposit?, Econ. Geol., 74, 1002–1011,
https://doi.org/10.2113/gsecongeo.74.5.1002, 1979.
Burns, R. G.: Mineralogical applications of crystal field
theory (No. 5), Cambridge University Press, 551 pp.,https://doi.org/10.1017/CBO9780511524899, 1993.
Christy, A. G. and Gatedal, K.: Extremely Pb-rich rock-forming silicates including a beryllian scapolite and associated minerals ina skarn from Långban, Värmland, Sweden. Mineral. Mag., 69,
995–1018, https://doi.org/10.1180/0026461056960304, 2005.
Compagnoni, R. and Rolfo, F.: Characteristics of UHP pelites,
gneisses, and other unusual rocks, Internat. Geol. Rev., 41, 552–
570, https://doi.org/10.1080/00206819909465157, 1999.
Faryad, S. W. and Bernhardt, H.-J.: Taramite-bearing metabasites
from Rakovec (Gemeric unit, the western Carpathians), Geol.
Carpathica, 47, 349–357, 1996.
Flink, G.: Bidrag till Sveriges mineralogi III, Ark. Kem. Mineral.
Geol., 5, 1–273, 1914.
Giret, A., Bonin, B., and Leger, J. M.: Amphibole compositional
trends in oversaturated and undersaturated alkaline plutonic ringcomposition, Can. Mineral., 18, 481–495, 1980.
Graser, G. and Markl, G.: Ca-rich ilvaite–epidote–hydrogarnet endoskarns: a record of late-magmatic fluid influx into the persodic
Ilímaussaq Complex, South Greenland, J. Petrol., 49, 239–265,
https://doi.org/10.1093/petrology/egm079, 2008.
Hålenius, U. and Bosi, F.: Cation ordering in Pb2+ -bearing, Mn3+ rich pargasite from Långban, Sweden. Am. Mineral., 97, 1635–
1640, https://doi.org/10.2138/am.2012.4137, 2012.
Harlow, G. E. and Sorensen, S. S.: Jade (nephrite and jadeitite) andserpentinite: metasomatic connections, Inter. Geol. Rev, 47, 113–
146, https://doi.org/10.2747/0020-6814.47.2.113, 2008.
Hawthorne, F. C. and Grundy, H. D.: The crystal chemistry of
the amphiboles, VII. The crystal structure and site chemistry ofpotassian ferri-taramite, Can. Mineral., 16, 53–62, 1978.
Hawthorne, F. C. and Della Ventura, G.: Short range order in amphiboles, in: Amphiboles: Crystal chemistry, occurrence and healthissues, edited by: Hawthorne, F. C., Oberti, R., Della Ventura, G.
and Mottana, A., Rev. Mineral. Geochem., 67, 173–222, 2007.
Hawthorne, F. C., Ungaretti, L., and Oberti, R.: Site populations
in minerals: Terminology and presentation of results of crystalstructure refinement, Can. Mineral., 33, 907–911, 1995.
Hawthorne, F. C., Oberti, R., Harlow, G. E., Maresch, W. V., Martin, R. F., Schumacher, J. C., and Welch, M. D.: Nomenclature of the amphibole supergroup, Am. Mineral., 97, 2031–2048,
https://doi.org/10.2138/am.2012.4276, 2012.
Holland, T. J. B. and Redfern, S. A. T.: Unit cell refinement from powder diffraction data: the use ofregression diagnostics, Mineral. Mag., 61, 65–77,
https://doi.org/10.1180/minmag.1997.061.404.07, 1997.
Holtstam, D. and Langhof, J.: Hancockite from Jakobsberg, Filipstad, Sweden: the second world occurrence, Mineral. Mag.,58, 172–174, https://doi.org/10.1180/minmag.1994.058.390.18,
1994.

https://doi.org/10.5194/ejm-34-451-2022

461

Holtstam, D. and Mansfeld, J.: Origin of a carbonate-hosted Fe-Mn(Ba-As-Pb-Sb-W) deposit of Långban-type in Central Sweden,
Mineral. Dep., 36, 641–657, 2001.
Holtstam, D., Cámara, F., Skogby, H., Karlsson, A., and Langhof, J.:
Description and recognition of potassic-richterite, an amphibole
supergroup mineral from the Pajsberg ore field, Värmland, Sweden, Mineral. Petrol., 113, 7–16, https://doi.org/10.1007/s00710018-0623-6, 2019a.
Holtstam, D., Cámara, F., Skogby, H., and Karlsson, A.: Hjalmarite,a new Na–Mn member of the amphibole supergroup, from Mn
skarn in the Långban deposit, Värmland, Sweden, Eur. J. Mineral., 31, 565–574, https://doi.org/10.1127/ejm/2019/0031-2822,
2019b.
Holtstam, D., Cámara, F., and Karlsson, A.: Instalmentof the margarosanite group, and data on walstromite–margarosanite solid solutions from the Jakobsberg Mn–Fe
deposit, Värmland, Sweden, Mineral. Mag., 85, 224–232,
https://doi.org/10.1180/mgm.2021.15, 2021.
Libowitzky, E.: Correlation of OH stretching frequencies andOH. . . O hydrogen bond lengths in minerals, Monatsh. Chem.,
130, 1047–1059, https://doi.org/10.1007/BF03354882, 1999.
Magnusson, N. H.: Nordmarks malmtrakt: geologisk beskrivning,
Sver. Geol. Undersök, Swedish Geological Survey, series Ca, 13,
1–98, 1929.
Magnusson, N. H.: Långbans malmtrakt, Sver. Geol. Undersök,
Swedish Geological Survey, series Ca, 23, 1–111, 1930.
Makagonov, E. P., Kotlyarov, V. A., and Korinevsky, E. V.: Amphiboles of alkaline rocks of the Ilmenogorsky Complex and country
metamorphic rocks, South Urals, Mineralogiya, 4, 8–26, 2018 (inRussian).
Moore, P. B.: Mineralogy & chemistry of Långban-type deposits in
Bergslagen, Sweden, Mineral. Record, 1, 154–172, 1970.
Morozewicz, J.: Über einige Eisenalkali-amphibole, Tscher. Miner.
Petrog., 38, 210–222, https://doi.org/10.1007/BF02993932,
1925.
Nikandrov, S. N., Kobyashev, Y. S., and Valizer, P. M.: Amphibolesof the Ilmenogorsky complex. IGZ UB RAS (Ilmensky State Reserve, Ural branch of the Russian Academy of Sciences), Miass,
Russia, 120 pp., 2000 (in Russian).
Oberti, R., Boiocchi, M., Smith, D. C., and Medenbach, O: Aluminotaramite, alumino-magnesiotaramite, and fluoro-aluminomagnesiotaramite: Mineral data and crystal chemistry, Am.
Mineral., 92, 1428–1435, https://doi.org/10.2138/am.2007.2529,
2007a.
Oberti, R., Hawthorne, F. C., Cannillo, E., and Cámara, F.: Longrange order in amphiboles, in: Amphiboles: Crystal chemistry,occurrence and health issues, edited by: Hawthorne, F. C., Oberti,R., Della Ventura, G., and Mottana, A., Rev. Mineral. Geochem.,
67, 125–172, https://doi.org/10.2138/rmg.2007.67.4, 2007b.
Oberti, R., Boiocchi, M., Smith, D. C., Medenbach, O.,
and Helmers, H.: Potassic-aluminotaramite from Sierrade los Filabres, Spain. Eur. J. Mineral., 20, 1005–1010,
https://doi.org/10.1127/0935-1221/2008/0020-1837, 2008.
Oberti, R., Boiocchi, M., Hawthorne, F. C., Ball, N. A., andHarlow, G. E.: Katophorite from the Jade Mine Tract, Myanmar: mineral description of a rare (grandfathered) endmember of the amphibole supergroup, Mineral. Mag., 79, 355–363,
https://doi.org/10.1180/minmag.2015.079.2.13, 2015a.

Eur. J. Mineral., 34, 451–462, 2022

462

D. Holtstam et al.: Ferri-taramite, a new member of the amphibole supergroup

Oberti, R., Boiocchi, M., Hawthorne, F. C., Cámara, F., Ciriotti, M.
E., and Berge, S. A.: Ti-rich fluoro-richterite from Kariåsen (Norway): the oxo-component and the use of Ti4+ as a proxy, Can.
Mineral., 53, 285–294, https://doi.org/10.3749/canmin.1400086,
2015b.
Pirard, C. and Hermann, J.: Experimentally determined stability of alkali amphibole in metasomatised dunite at
sub-arc pressures, Contrib. Mineral. Petrol., 169, 1–26,
https://doi.org/10.1007/s00410-014-1095-2, 2015.
Prescher, C., McCammon, C., and Dubrovinsky, L.: MossA: a program for analyzing energy-domain Mössbauer spectra from conventional and synchrotron sources, J. Appl. Cryst., 45, 329–331,
https://doi.org/10.1107/S0021889812004979, 2012.
Puga, E., Ruiz-Cruz, M. D., and Diaz de Federico, A.: Polymetamorphic amphibole veins in metabasalts from the betic ophiolitic association at Cóbdar, southeastern Spain: relics of oceanfloor metamorphism preserved through the alpine orogeny, Can.
Mineral., 40, 67–83, https://doi.org/10.2113/gscanmin.40.1.67,
2002.
Reece, J. J., Redfern, S. A. T., Welch, M. D., Henderson, M. B., andMcCammon, C. A.: Temperature-dependent Fe2+ –Mn2+ order–
disorder behaviour in amphiboles, Phys. Chem. Minerals, 29,
562–570, https://doi.org/10.1007 s−1 00269-002-0267-1, 2002.
Rezvukhin, D. I., Alifirova, T. A., Golovin, A. V., and Korsakov, A. V.: A plethora of epigenetic minerals reveals amultistage metasomatic overprint of a mantle orthopyroxenite from the Udachnaya Kimberlite, Minerals, 10, 264,https://doi.org/10.3390/min10030264, 2020.
Sandström, F. and Holtstam, D.: Geology of the Långban deposit,
in: Långban: the mines, their minerals, geology and explorers, edited by: Holtstam, D. and Langhof, J., Naturhistoriska
riksmuseet and Raster Förlag, Stockholm, ISBN 91 87214 881,
1999.
Schumacher, J. C.: Metamorphic amphiboles: compositionand coexistence, Rev. Mineral. Geochem., 67, 359–416,
https://doi.org/10.2138/rmg.2007.67.10, 2007.
Sheldrick, G. M.: Crystal structure refinement with SHELXL, Acta
Cryst., C71, 3–8, https://doi.org/10.1107/S2053229614024218,
2015.
Skublov, S. and Drugova, G.: Patterns of trace-element
distribution in calcic amphiboles as a function ofmetamorphic grade, Can. Mineral., 41, 383–392,
https://doi.org/10.2113/gscanmin.41.2.383, 2003.

Eur. J. Mineral., 34, 451–462, 2022

Stephens, M. B. and Jansson, N. F.: Paleoproterozoic (1.9–1.8 Ga)
syn-orogenic magmatism, sedimentation and mineralization in
the Bergslagen lithotectonic unit, Svecokarelian orogen, Geol.
Soc. Mem., 50, 155–206, https://doi.org/10.1144/M50-2017-40,
2020.
Sundius, N.: The position of richterite in the amphibole group, Geol. Fören. Stock. För., 67, 266–270,
https://doi.org/10.1080/11035894509446100, 1945.
Takasu, A. and Orozbaev, R.: Variety of chemical compositions ofamphiboles from eclogites in the Aktyuz area, northern Kyrgyz
Tien-Shan, Geoscience Report Shimane Univ., Shimane University, 28, 51–63, 2009.
Ungaretti, L., Smith, D. C., and Rossi, G.: Crystal-chemistry by Xray structure refinement and electron microprobe analysis of aseries of sodic-calcic to alkali-amphiboles from the Nybö eclogite pod, Norway, Bull. Minéral., 104, 400–412, 1983.
Waeselmann, N., Schlüter, J., Malcherek, T., Della Ventura, G.,
Oberti, R., and Mihailova, B.: Nondestructive determinationof the amphibole crystal-chemical formulae by Raman spectroscopy: One step closer, J. Raman Spectrosc., 51, 1530–1548,
https://doi.org/10.1002/jrs.5626, 2020.
Wang, R., Xu, S., and Xu, S.: First occurrence of preiswerkite in the
Dabie UHP metamorphic belt, Chinese Sci. Bull., 45, 748–750,
https://doi.org/10.1007/BF02886183, 2000.
Wilson, A. J. C.: International Tables for Crystallography, Volume
C: Mathematical, physical and chemical tables, Kluwer Academic, Dordrecht, Netherlands, 883 pp., ISBN 0-792-3-16-38X,
1992.
Žáček, V.: Potassian hastingsite and potassichastingsite from garnet hedenbergite skarn at Vlastejovice, Czech Republic, Neues
Jb. Miner. Abh., 2007, 161–168, https://doi.org/10.1127/00777757/2007/0089, 2007.
Zhang, R. Y. and Liou, J. G.: Coesite-bearing eclogite inHenan Province, central China: detailed petrography, glaucophane stability and PT-path, Eur. J. Mineral., 9, 217–234,
https://doi.org/10.1127/ejm/6/2/0217, 1994.

https://doi.org/10.5194/ejm-34-451-2022