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Formula: Na(AlSi2O6).H2O
Tectosilicate (framework silicate),
zeolite group, feldspathoid, forms series
with pollucite and with wairakite
(ZW).
Crystal System: Triclinic
Specific gravity: 2.24 to 2.29 measured, 2.271 calculated
Hardness: 5 to 5½
Streak: White
Colour: White, colourless, gray, pink, greenish, yellowish; colourless in thin section.
Solubility: Moderately soluble in hydrochloric acid
Environments:
Igneous environments
Pegmatites
Sedimentary environments
Basaltic cavities
Analcime occurs as a primary mineral in some
igneous rocks; it is the only
zeolite that crystallises directly from molten rock. In pegmatites and
miarolytic cavities
cesium-rich analcime forms from 250° to 150°C. Analcime phenocrysts crystallise in deep basaltic magma chambers
at temperatures
between 600 and 640°C, and at
pressures from 5 to 13 kilobars. Rapid vertical transport to the surface is required for analcime to survive the decrease
in temperature and pressure.
A slow decrease in temperature and pressure would allow the analcime to react with the basaltic magma to produce
albite
(ZW).
Analcime is also the product of hydrothermal action in the
filling of basalt cavities, where analcime phenocrysts crystallise in deep
basaltic magma chambers at temperatures between 600oC and 640oC, and pressure between 5 and
13 kbar, in association with
prehnite, calcite and
zeolites such as chabazite,
thomsonite and stilbite
(DHZ 4 p346).
Geothermal wells have been drilled through a thick series of basalt flows in
western Iceland, where it was found that
analcime crystallised at temperatures from to 300oC at depths between 72m and 1600m
(ZW).
Analcime may occur in mafic rocks such
as aegirine-analcime-nepheline
syenite.
In saline alkaline lakes, analcime forms near the centre of the lake, where the water is highly saline with pH 9 to 10
(strongly alkaline), and in
these conditions analcime, K-feldspar,
trona and borosilicates
are dominant. Analcime forms at a higher pH (more alkaline) by dissolving
phillipsite,
erionite, chabazite, or silica-rich
heulandite that crystallised when the pH was lower (less strongly alkaline)
(ZW).
In deep sea sediments phillipsite and
heulandite alter
to analcime over a period of millions of years
(ZW).
In lake beds, analcime may be altered
from pyroclastics or clay minerals, or it may be a
primary precipitate. It is authigenic (formed in place) in
sandstone and
siltstone.
Analcime crystallises in the isometric system, point group 4/m 3 2/m,
and crystals usually have the form {211} (trapezohedron)
Mindat Image
Localities
In Western Tasmania, Australia, analcime occurs as a late stage
primary
mineral with
gonnardite-natrolite and as an
alteration product of feldspar. It also occurs in
basaltic cavities
( AJM 10.2.62-63 ).
In the Marron Volcanics of the Olalla Area, South-Central British Columbia, Canada, analcime is found lining many of the
vesicles in the road cuts at Yellow Lake. These are clear to translucent, colourless crystals, commonly overgrown by a transparent to
pinkish second generation analcime
(R&M 96.6.519).
In the vicinity of Meshkinshahr, Ardabil Province, Iran, crystals of analcime are found embedded in small amygdules
in potassium-rich basalt, associated with
chabazite, mesolite and/or
thomsonite. The analcime originated hydrothermally
(R&M 92.6.541).
At Mount Kahoven, Semnan Province, Iran, orange coloured crystals of analcime are found on perched on
vesicular basalt
(R&M 92.6.542).
In the alkaline rocks of the Kola peninsula, Russia, analcime is associated with
aegirine and may be either
primary
or secondary after sodalite
or aegirine
(DHZ 4 p345).
At Palabora, Limpopo, South Africa, analcime is an early phase in the deepest parts of the dyke fracture zone.
Crystal cores may have
originally been wairakite overgrown by analcime, then later
hydrothermal alteration converted wairakite to
laumontite. A later generation of analcime occurs on
fluorapophyllite
(R&M 92.5.433).
At Copthill Quarry, Stanhope, County Durham, England, UK, crystals of analcime on dolerite
have been found
(JRS 21.6).
At Cambokeels Mine, Westgate, Stanhope, County Durham, England, UK, analcime crystals typically up to 2 mm across occurred coating surfaces
of dolerite. In many specimens the analcime was accompanied, and locally overgrown by,
small crystals of apophyllite, and in a few specimens was
also accompanied by crystals of calcite up to 2 mm across
(JRS 21.6).
At the High Force Quarry, Forest and Frith, County Durham, England, UK, analcime crystals up to 1 mm across were found in samples as crusts
up to 12 cm across coating joint surfaces of dolerite pegmatite. In some examples the
analcime was accompanied by a few crystals of chabazite up to 2 mm across. Exactly similar
small analcime crystals were also noted in situ in narrow stilbite - bearing veins in slightly
chloritised dolerite pegmatite exposed in the quarry
(JRS 21.6).
At Croft quarry, Croft, Leicestershire, England, UK, analcime has been found in a
zeolite-filled fissure in tonalite, together with
chabazite. The first generation of analcime occurs as crystals to 1mm associated with
quartz.
The second generation analcime crystals were numerous and larger, up to 13 mm across, associated with
calcite, marcasite,
chalcopyrite or galena. It is
suggested that the
analcime was produced by the action of water on feldspar:
plagioclase + water
→ analcime + laumontite + quartz
Both generations of analcime may enclose, or be coated with, hematite.
Analcime and
calcite may form pseudomorphs
after laumontite
(JRS 20.6-9, RES p185 to 190).
At Enderby Warren Quarry, Enderby, Blaby, Leicestershire, England, UK, analcime occurs in
quartz-diorite and
tonalite associated with
laumontite
(JRS 20.9).
At the Emmons pegmatite, Greenwood, Oxford county, Maine, USA, analcime has been identified in the central portion of
lepidolite veins cutting pollucite masses.
After pollucite has formed no more cesium is available, thus only analcime can
form. The Emmons pegmatite is an example of a highly evolved
boron-lithium-cesium-tantalum
enriched pegmatite
(R&M 94.6.503).
The Central Mine, Central, Keweenaw county, Michigan, USA, initially targeted a series of sub-parallel mineralised
fissure veins where the most copper-rich portion of the vein was close to the
base of the main greenstone flow.
Analcime from the Central mine occurs only as mediocre, opaque cream to white crystals up to 2 cm, commonly
associated with other zeolites. Some Central mine analcime crystals
contain inclusions of copper and/or
hematite
(MinRec 54.1.53-81).
At the Copper Falls Mine, Copper Falls, Keweenaw county, Michigan, USA, mineralisation occurs primarily in hydrothermal veins
cutting preexisting lavas and as amygdules in the Ashbed flow.
Analcime is a fairly common zeolite mineral here; reddish crystals to 1 cm or so have been
found in most of the veins at Copper Falls, sometimes associated with natrolite. These
red analcime crystals were known from as early as the 1800s. White crystals, more typical for the species, are also not
uncommon. Analcime with copper inclusions is also known from this locality
(MinRec 54.1.94-95).
The Cliff Mine, Phoenix, Keweenaw county, Michigan, USA, is situated at the base of a roughly 70-metre
basalt cliff. A curious feature of the impressive thickness of the
greenstone flow here is that it contains zones of “pegmatoid”: areas
where
slow cooling in the core of the lava flow allowed for large feldspar crystals
exceeding 1 cm to grow. Such features are normally only observed in intrusive igneous rocks and are almost unheard of
in basalt flows.
The Cliff mine primarily exploited rich copper mineralisation in the Cliff
fissure (vein). Although mineralised with copper to some extent along its
entire length, the part of the vein just below the greenstone flow
carried the richest copper mineralisation by far. A significant amount of the
copper recovered at the Cliff mine came from amygdaloids in the tops of 13
basalt flows which were cut by the Cliff vein. The discovery and mining
of this vein proved that the veins were the source of the large masses of float
copper that were already well known, and proved that the
primary ore mineral in the district was native
copper, not sulphides, as had been suspected earlier.
Analcime is an uncommon mineral in the Cliff fissure, occurring as white or colourless crystals with typical
trapezohedral habit to 1 or 2 cm. It is typically associated with quartz,
prehnite, datolite,
apophyllite, laumontite and
copper (which is sometimes included in the analcime)
(MinRec 54.1.25-49).
At the Phoenix Mine, Phoenix, Keweenaw county, Michigan, USA, mineralisation occurs primarily in hydrothermal veins cutting
pre-existing Portage Lake basalts as well as in amygdules in the Ashbed
basalt flow, and the vast majority of collectible minerals occur in the
hydrothermal veins.
Superb examples of analcime associated with well crystallised copper,
silver, calcite and a host of other minerals
have been found here. Analcime is a common late-stage zeolite species in the
veins. It typically occurs as opaque white trapezohedral crystals, exceptionally to 4 cm, on a matrix of other minerals. The
analcime crystals often contain visually striking inclusions of other minerals, most notably native
copper and hematite. Analcime
crystals with oriented hematite inclusions and/or
apophyllite coatings are a particular Phoenix mine specialty, as are the
complex crystals with re-entrant edges which were first described (incorrectly) as twins; they are actually oriented
overgrowths of colourless analcime on pre-existing white analcime crystals. These seem to be unique to the
Phoenix mine
(MinRec 54.1.125-130).
At the Bearpaw Mountains, Montana, USA, analcime occurs in cavities in igneous rock, associated with
axinite, prehnite and
datolite
(DHZ 4 p345).
The Purple Diopside Mound, Rose Road, Pitcairn, St. Lawrence county, New York, USA, is situated in
marble. The development of veins of large crystals probably occurred as
a result of fluid penetration from a concurrent intrusion. Many of the minerals of interest to collectors formed during
this primary event, with additional species resulting from the
subsequent alteration of scapolite. There seems to be little, if any,
secondary, late-stage mineralisation present.
Analcime occurs uncommonly as white, crude trapezohedral crystals in the walls of the
scapolite vein. It most likely formed as an alteration of
marialite
(R&M 96.6.548).
The analcime fluoresces pale yellow under long wave UV
(R&M 97.5.442).
Alteration
analcime to jadeite and H2O
Na(AlSi2O6).H2O → NaAlSi2O6 + H2O
At high temperature analcime changes to jadeite
(ZW)
analcime and quartz to
albite and H2O
Na(AlSi2O6).H2O + SiO2 ⇌ Na(AlSi3O8) +
H2O
High temperature favours the forward reaction
(JVW p 144, ZW).
nepheline and H4SiO4 (silicic acid) to analcime and H2O
NaAlSiO4 + H4SiO4 ⇌ Na(AlSi2O6).H2O
+ H2O
(http://citeseerx.ist.psu.edu/viewdoc/download?doi=10.1.1.613.9474&rep=rep1&type=pdf)
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