Data Repository File - Geological Society of America · GSA Data Repository Item 2017403 Data...
Transcript of Data Repository File - Geological Society of America · GSA Data Repository Item 2017403 Data...
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Závada, P., Schulmann, K., Racek, M., Hasalová, P., Jeřábek, P., Weinberg, R.F.,
Štípská, P., and Roberts, A., 2017, Role of strain localization and melt flow on
exhumation of deeply subducted continental crust: Lithosphere,
https://doi.org/10.1130/L666.1.
GSA Data Repository Item 2017403
Data Repository File (Role of strain localization and melt flow on exhumation of deeply
subducted continental crust)
This data repository file presents the additional information about the methodology
and provides extra datasets associated with the manuscript. The first section, the “Image
analysis of melt topology”, explains in detail the image analysis procedure (segmentation) of
the cathodoluminescence image mosaics (Fig. DR1). The second section, “Thermodynamic
modeling of PT equilibria”, includes the details of the phase equilibria modeling for the
pressure and temperature estimations.
“Additional datasets” shows seven phase maps and details of the microstructures in
hand line-drawings alongside the cathodoluminescence images that are also presented as a
shorter version in the Fig.8 of the manuscript (Fig. DR2A-G and DR3A-G). Another panel
(Fig. DR4) reveals the pseudosection calculated using the thermodynamic equilibria
modeling. In addition, the isocon and volume-composition diagrams show the comparison of
the element contents between the studied anatectic samples and are presented in Fig. DR5.
Compositional data for representative mineral paragenesis that were obtained by electron
microanalysis and used later for the P-T calculations (P-T pseudosection in Fig. DR3), are
presented in Table DR1. Whole rock compositional data of the studied samples are shown in
Table DR2. Volume-composition calculations displayed in Fig. DR5, are also shown in Table
DR3.
Image analysis of melt topology
Image analysis processing was performed in order to discern the contrasting phases in
the cathodoluminescence images (CITL Mk5-2) interpreted as new phases that crystallized
from interstitial melt (e.g. Hollness and Sawyer, 2008; Hasalová et al., 2008b; 2011). The
segmentation worked well for albitic overgrowths on plagioclase grains (e.g. in plagioclase
bands, K-feldspar bands or inclusions in quartz) that have contrasting dark purple or dark blue
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colors with respect to pinkish plagioclase and light blue K-feldspar in the optical
cathodoluminescence images (Fig. DR1). Post-processing including manual correction of the
automatically segmented images to obtain best estimate of the modal content of individual
ized in the interstices.
In the first step, a set of cathodoluminescence images (~90-150 pcs) were stitched
together using a software “kolor auto pano GIGA” (www.kolor.com) that included automatic
blending of the sutures between the stitched images and exposure correction. Resulting
images were then subjected to image segmentation in ArcView 10.2.1 using the “Maximum
likelihood classification” method for selected color samples. Resulting classified image was
corrected by smoothing procedure (‘Boundary clean’ function in Spatial Analyst toolbox) and
transformed to a shapefile (‘Raster to Polygon’ conversion tool). Finally, resulting shapefiles
were corrected with ‘Eliminate’ tool to merge small polygons with larger ones to decrease
size of the shapefiles (typically exceeding 100 000 polygons after raster to polygon
conversion). Manual correction by merging and splitting of the individual polygons was
applied in the last step. Melt content and modal analysis from fine-grained samples (EC12-8G
– mylonite; EC12-8C2, EC12-K6 – granofelses), was carried out by manual tracing of
representative areas (at least 500 grains), since automatic segmentation method did not
correctly identify the small melt pockets. Migmatite sample EC12-3C2 was also interpreted
only by manual tracing of pseudomorphed melt pools. Shape preferred orientation of the melt
pockets was obtained by line tracing (2 node lines) of ‘melt films’ primarily in the K-feldspar
aggregates. Shapefiles (line) were then statistically analyzed in Matlab™ using the PolyLX
Matlab™ toolbox (function „prose“) (Lexa et al., 2005).
Thermodynamic modeling of PT equilibria
In order to get constraints on the P-T conditions of coupled deformation and melt flux,
the P-T pseudosection was calculated for the representative sample of the banded orthogneiss
(sample EC12-K1), the results of the modelling were then compared with the observed
mineral assemblage and corresponding mineral chemistry, namely of muscovite and garnet
(see Table DR1 for representative analyses). The P-T pseudosection was calculated using the
software Perple_X (Connolly, 2005, version Perple_X 07) with dataset 5.5 (Holland &
Powell, 1998, November 2003 upgrade), in the system MnO–Na2O–CaO–K2O–FeO–MgO–
Al2O3–SiO2–H2O–TiO2 (MnNCKFMASHT). The following activity models were used: Mn-
bearing model for cordierite is a combination of formulations by Mahar et al. (1997) and
Holland & Powell (1998), garnet is from White et al. (2007), biotite from White et al. (2005),
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silicate melt from White et al. (2007), muscovite and paragonite from Coggon & Holland
(2002), plagioclase and K-feldspar from Holland & Powell (2003). Ilmenite is considered to
be an ideal solution of Fe–Mg–Mn endmembers; albite, titanite, rutile, kyanite, sillimanite,
and quartz are considered as pure endmembers. The whole rock composition used for the
modelling was obtained by standard wet chemical methods in the Bureau Veritas laboratories
(Vancouver, Canada). Since it cannot be assumed that the studied metagranitic rocks were
metamorphosed in H2O-saturated conditions, it was necessary to estimate the H2O content
used for the calculations. This was done based on modal proportions of present H2O bearing
minerals (muscovite and biotite) and their composition, which resulted in 1.5 mol.% of H2O.
The microanalyses of the rock forming minerals were done at the Laboratory of
electron microscopy and microanalysis at the Institute of Petrology and Structural Geology
(Faculty of Science, Charles University, Prague, Czech Republic). They were acquired using
the FEG-EPMA JXA-8530F (manufactured by Jeol) under following analytical conditions:
accelerating voltage 15 kV, beam current 20 nA. Garnet was analyzed with focused beam,
feldspars and micas were analyzed with beam defocused to diameter of 5µm. The same
equipment was used for acquisition of the map of Ca distribution (Fig. DR1b), which was
acquired with 15 kV and 40 nA (step size 8 µm, dwell time 40 ms per point).
The mineral abbreviations follow the abbreviations used in the THERMOCALC (see:
http://www.metamorph.geo.uni-mainz.de/thermocalc/documentation/abbreviations/index.html),
following definitions of end-members and ratios are used for characterization of mineral
chemistry: XFe = Fetot/(Fetot + Mg), Alm = Fetot/(Fetot + Mg + Ca + Mn), Py = Mg/(Fetot + Mg
+ Ca + Mn), Grs = Ca/(Fetot + Mg + Ca + Mn), Sps = Mn/(Fetot + Mg + Ca + Mn), Ab =
Na/(Na+ Ca + K), An = Ca/(Na+ Ca + K), Or = K/(Na+ Ca + K), apfu = atoms per formula
unit. Coupled cathodoluminescence imaging and compositional mapping in selected areas
were acquired using the JXA 8530F (Jeol) at IPSG (Prague) equipped with five wavelength
dispersive spectrometers, energy dispersive spectrometer and a cathodoluminescence
spectrometer.
The chemical analyses of major and trace elements in the selected samples were
carried out in order to correlate the element content between the different types of anatectic
rocks for possible melt flux related element transfer. The samples were crushed with a jaw
crusher and pulverized in an agate mill in the Laboratories of the Czech Geological Survey
(Prague, Czech Republic). Pulverized and homogenized samples were analyzed in the Bureau
Veritas Mineral Laboratories (Vancouver, Canada). The total whole rock characterization
(code LF202, see http://acmelab.com/pdfs/FeeSchedule-2016.pdf) was done using the lithium
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borate fusion ICP-ES (major and minor elements, code LF302) the lithium borate fusion ICP-
MS (trace elements, code LF100), and Aqua Regia ICP-ES/MS (trace elements, code AQ200)
methods.
Fig. DR1. Cathodoluminescence images (A,C), compositional map (B) and image
segmentation result of image shown in (D) for a migmatite sample 3A2 (Fig. DR2b). EPMA
image (A) and corresponding compositional map of relative calcium content (B) contain an
overlay of hatched polygons with interpreted topology of pools interpreted as crystallized
interstitial melt (also indicated with white fields on grey background in inset of (B)). An
optical cathodoluminescence image (C) of the same area was used for the image
segmentation resulting in a phase map (D) including post-processing in ArcGIS 10.2.1. Note
an inset in (B) showing schematically the melt topology with white patches. Mineral
abbreviations: pl—plagioclase; q—quartz; ksp—potassium feldspar, g—garnet.
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Fig. DR2. Optical cathodoluminscence (CITL Mk5) images of selected representative
microstructures and line-drawings showing distribution of individual phases and interpreted
melt topology (on the right side of each image). Line-drawings and related images
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correspond to small insets in Fig.8 of the manuscript. Note that the prefix "EC12-" is not
included in the sample labels. Note relatively thick interstitial grains in K-feldspar bands (a)
and corroded shape of garnet showing embayments and holes, where melt precipitated as
quartz, K-feldspar and plagioclase (banded orthogneiss, sample EC12-A); (b) anatectic
orthogneiss (sample EC12-3A2) with corroded quartz band containing numerous inclusions
of feldspars that are also interpreted as precipitates from interstitial melt; (c) large pools in
granular framework of a metatexite sample (sample EC12-3C2), note the irregular thick
overgrowths of albite (dark purple color) in an elongate pool in the middle part of the image.
Banded mylonite sample EC-8G shows K-feldspar band with numerous albite (dark blue and
pinkish colors in CITL images on left) and quartz (black) interstitial grains (d); granofels
sample with small pools and transgranular cracks, indicated by white triangles (e); banded
orthogneisses EC12-K1, where melt topology was influenced by fold axial crenulation
cleavage (f) and shows pockets oriented primarily at high angles to the layer (parallel to fold
axial cleavage); granofels sample EC12-K6 showing only isolated melt pockets on boundaries
of feldspar grains that are oriented obliquely to the shape preferred orientation of the grains.
Scalebars are 1 mm long.
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Fig. DR3. Cathodoluminiscence images (EPMA) of the migmatite and a granofels are shown
in (a) and (b), respectively. Same images with interpreted topology of pseudomorphs after
melt are highlighted by hatched fields in (c) and (d). Estimated melt volumes (ϕ) are
indicated. Schematic map of interpreted melt topology as white fields on grey background is
shown also in inset (c, d). Mineral abbreviations: pl—plagioclase; q—quartz; ksp—potassium
feldspar, bi—biotite, mu—muscovite, g—garnet.
Additional datasets
P-T conditions and maximum melt volume produced in situ
In order to estimate the pressure-temperature (P-T) conditions of the deformation and
pervasive melt flux and estimate the potential of the banded orthogneisses to produce melt, a
PT pseudosection was calculated (Fig. DR4) for a sample EC12-K1/K1 (Fig. DR2f, sample
shown in Fig. 7C (manuscript); composition (K1) shown in Table DR2). The rock-forming
minerals K-feldspar, plagioclase, quartz, biotite, muscovite and garnet are accompanied by
rutile, occasionally rimmed by ilmenite. Accessory phases are represented by apatite, zircon
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and monazite. Garnet forms grains up to 0.5 mm in diameter and shows compositional zoning
represented by increase of almandine and spessartine and decrease of pyrope and grossular
components from core to rim (Alm72→79; Py11→8; Grs16→11; Sps2→3; XFe = 87→91). Muscovite
composition varies mainly with respect to Si (3.16−3.28 apfu) and Ti contents (0.08−0.11
apfu). Biotite has XFe ratio 0.71 and Ti content of 0.18 apfu, K-feldspar has composition of
Or86−90, Ab10−14 and An0, while plagioclase corresponds to oligoclase (Ab86−90, An10−13, Or1)
and has albite-rich rims in places (Ab96, An3, Or1).
The P-T conditions derived from intersection of the compositional isopleths
corresponding to the garnet core composition (Alm72; Py11; Grs16; Sps2; XFe = 87) indicate c.
720 °C and 13 kbar, in the stability field of g+bi+mu+pl+kfs+q+ru+liq, consistent with the
observed mineral assemblage. The isopleth of maximum Si content in muscovite (3.28 apfu)
is located in slightly higher pressure (c. 14 kbar). The composition of the garnet rim points to
lower P-T conditions (680 °C and 10 kbar), which also corresponds to minimum Si content in
muscovite (3.16 apfu) and being located right at the low-temperature boundary of the
g+bi+mu+pl+kfs+q+ilm+liq field, representing the solidus line. In result, the garnet core
composition is supposed to represent the peak P-T conditions 720°C and 13−14 kbar
(corresponding to granulite-eclogite facies transition) recorded by the banded orthogneiss
sample, while the garnet rims, low-Si muscovite and ilmenite are connected presumably with
later retrograde re-equilibration in upper amphibolite facies (680 °C and 10 kbar) during
exhumation of the ECC.
Since the textural characteristics of the observed metagranitic rocks indicate that they
are connected with partial melting (Fig. 8, manuscript), it is important to estimate what
volume of melt can be generated in such granitic rock at the calculated P-T conditions. The
core composition of garnet corresponds to conditions close to the low-T limit of the
g+bi+mu+pl+ksp+q+ru+liq, where melt forms only ~1 vol.% of the rock. Even if we were to
assume that garnet composition was partially re-equilibrated during retrogression and that the
temperature is slightly underestimated, the study of large number of samples shows that they
(except for the granulites) probably never left the stability field of muscovite. This constrains
the upper temperature to c. 800 °C (at 13 kbar) and the maximum melt content, to less than c.
6 vol. %. We therefore infer that most of the interstitial melt in these rocks must have come
from external sources.
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Fig. DR4. P-T pseudosection calculated by thermodynamic equilibria modeling for the
layered orthogneiss sample EC12-K1/K1 (see Fig. 7d in the manuscript, Fig. DR2F, and
Table DR2 for hand specimen, microstructure overview and composition, respectively).
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(Figure continues on next page)
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Fig. DR5. Isocon diagrams of Grant (1986) and diagrams of Potdevin (Potdevin and
Marquer, 1987) displaying the loss-gain relationships for a range of elements for five pairs of
selected samples. The volume-composition relationships displayed in the diagrams of
Potdevin (diagrams on the right side) were calculated using a freeware Microsoft Excel
macro created by López-Moro (2012). See the Table DR2 and Table DR3 for the whole rock
composition data and the results of these calculations, respectively. The Fv volume factor in
the diagrams of Potdevin is given by the volume ratio between the transformed rock and the
initial one. The difference in relative abundance of specific element (i) is expressed by:
∆𝑚𝑖 = 𝐹𝑣 . (𝜌𝑎
𝜌0) 𝐶𝑎
𝑖 − 𝐶0𝑖 mi is the relative gain or loss of mass, and 𝐶0
𝑖 and 𝐶𝑎𝑖 are the
initial and final concentrations and 0 and a the densities of these rocks, respectively. Note,
that the relative gain or loss of mass is normalized by the initial mass 𝑚0𝑖 in the volume-
composition diagrams. Shaded area corresponds to an artificial fluctuation range, for which
the elements are considered as relatively immobile. Note, that while isocon diagrams (Grant,
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1986) on the left display the comparison of only major elements, the composition-volume
diagrams on the right (Diagrams of Potdevin; Gresens, 1967; Potdevin and Marquer, 1987)
show the selected 32 major and minor elements, including the REE (Rare Earth Elements).
For locations of the selected samples see Figs. 5,6,7 (manuscript).
g - rim g - rim g - core g - core mu mu mu bi ksp pl pl-rim
Na2O 0.00 0.00 0.00 0.00 0.35 0.25 0.33 0.20 1.15 10.44 11.70
MgO 2.07 2.13 2.81 2.80 2.22 2.18 1.71 5.57 0.00 0.00 0.00
Al2O3 20.75 20.87 21.07 21.02 28.70 28.31 29.91 15.90 18.45 21.77 20.19
SiO2 37.08 37.05 37.62 37.50 48.13 48.13 46.27 36.48 65.71 66.46 69.21
K2O 0.00 0.00 0.00 0.00 10.94 10.79 10.85 9.51 15.12 0.41 0.17
CaO 3.80 3.77 5.72 5.55 0.01 0.00 0.00 0.00 0.01 2.36 0.57
TiO2 0.00 0.00 0.00 0.00 1.70 1.73 1.68 2.91 0.00 0.00 0.00
MnO 1.10 1.11 0.78 0.67 0.00 0.00 0.00 0.24 0.00 0.00 0.00
FeO 35.34 34.77 32.22 32.63 2.89 2.72 3.13 24.51 0.01 0.03 0.01
BaO 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.95 0.07 0.00 0.00
F 0.00 0.00 0.00 0.00 1.07 1.05 0.69 0.25 0.00 0.00 0.00
Cl 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00
Total 100.14 99.70 100.21 100.17 96.01 95.16 94.56 96.52 100.51 101.48 101.85
Na 0.00 0.00 0.00 0.00 0.05 0.03 0.04 0.03 0.10 0.88 0.97
Mg 0.25 0.26 0.33 0.33 0.22 0.22 0.17 0.65 0.00 0.00 0.00
Al 1.98 1.99 1.98 1.98 2.29 2.27 2.42 1.46 0.99 1.11 1.02
Si 3.00 3.00 3.00 3.00 3.26 3.28 3.17 2.84 3.01 2.88 2.97
K 0.00 0.00 0.00 0.00 0.94 0.94 0.95 0.95 0.88 0.02 0.01
Ca 0.33 0.33 0.49 0.48 0.00 0.00 0.00 0.00 0.00 0.11 0.03
Ti 0.00 0.00 0.00 0.00 0.09 0.09 0.09 0.17 0.00 0.00 0.00
Mn 0.08 0.08 0.05 0.05 0.00 0.00 0.00 0.02 0.00 0.00 0.00
Fe 2.39 2.35 2.15 2.18 0.16 0.16 0.18 1.60 0.00 0.00 0.00
Ba 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.03 0.00 0.00 0.00
F 0.00 0.00 0.00 0.00 0.23 0.23 0.15 0.06 0.00 0.00 0.00
Cl 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00
XFe 0.91 0.90 0.87 0.87 0.42 0.41 0.51 0.71
Alm 0.79 0.78 0.71 0.72
Py 0.08 0.09 0.11 0.11
Grs 0.11 0.11 0.16 0.16
Sps 0.02 0.03 0.02 0.01
Ab 0.10 0.87 0.96
An 0.00 0.11 0.03
Or 0.89 0.02 0.01
Table DR1. Representative compositional data used for thermodynamic modeling of
metamorphic equilibrium for the sample K1. Corresponding P-T pseudosection is presented
in Fig. DR4.
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Lithology
Banded
Orthog.
Banded
Orthog.
Banded
Orthog. Granofels Granofels Migmatite
S1
leucos. Leucosomes
Leucos.
average Sample EC27 K1 2B K2 2H EC86 2E
slab E,
S1
slab E,
S2
slab D,
S1
slab D,
S2
SiO2 68.86 70.95 74.37 72.41 73.90 72.88 74.28 71.73 71.45 69.74 71.50 71.11
TiO2 0.48 0.38 0.27 0.31 0.51 0.26 0.12 0.20 0.17 0.10 0.19 0.17
Al2O3 16.02 14.52 13.24 14.00 12.62 13.98 13.31 14.72 15.08 16.01 14.97 15.20
Fe2O3 3.18 2.97 2.26 2.46 3.07 2.22 1.60 2.23 2.09 1.34 1.92 1.90
MnO 0.06 0.04 0.03 0.03 0.03 0.06 0.03 0.03 0.03 0.01 0.02 0.02
MgO 0.9 0.63 0.41 0.52 0.90 0.45 0.18 0.29 0.25 0.17 0.29 0.25
CaO 1.3 1.10 0.76 1.02 1.01 0.72 0.60 0.97 1.06 0.73 0.90 0.92
Na2O 3.01 2.61 2.41 2.56 3.10 2.74 1.94 3.04 3.41 2.99 3.03 3.12
K2O 5.03 5.46 5.17 5.55 3.49 5.35 6.94 6.28 6.08 8.61 6.74 6.93
P2O5 0.271 0.25 0.21 0.22 0.22 0.21 0.25 0.12 0.10 0.10 0.12 0.11
As 10.30 1.50 1.40 1.90 1.70 13.00 1.10 2.20 1.50 2.00 2.60 2.08
Cs 10.57 12.90 6.40 8.60 7.50 9.50 6.50 4.00 4.40 8.40 6.80 5.90
Rb 201.84 258.10 242.30 246.00 199.10 305.50 277.60 239.00 229.70 320.90 267.50 264.28
Ba 725.19 411.00 312.00 443.00 237.00 345.00 229.00 471.00 405.00 714.00 543.00 533.25
Sr 107.5 67.00 57.30 81.30 64.10 59.40 54.60 89.60 94.70 110.80 103.60 99.68
Pb 33.21 1.40 1.30 1.10 1.70 18.90 3.80 13.70 7.60 17.40 11.10 12.45
Ni 6.87 5.10 2.60 4.00 11.00 7.70 1.20 3.90 1.80 4.90 3.20 3.45
V 39.47 28.00 25.00 24.00 42.00 21.00 10.00 15.00 11.00 8.00 12.00 11.50
Ga 20.78 19.50 16.30 15.80 16.50 18.20 14.70 16.50 16.20 15.50 16.10 16.08
Zn 48.65 32.00 31.00 27.00 50.00 82.00 8.00 13.00 17.00 12.00 24.00 16.50
U 4.41 2.70 2.00 2.10 1.90 4.90 1.60 1.60 1.70 1.20 2.50 1.75
Zr 83.82 181.10 129.00 147.30 1.90 121.00 36.60 101.70 93.80 40.00 84.10 79.90
Hf 2.60 4.80 4.50 4.00 3.80 3.70 1.40 3.00 2.90 1.00 2.60 2.38
Y 56.51 49.50 40.20 46.80 28.60 37.00 29.90 36.00 29.90 14.00 25.50 26.35
Nb 46.18 12.10 9.10 9.60 8.50 7.90 6.10 11.50 25.80 3.60 29.70 17.65
Ta 1.04 1.20 0.70 1.00 0.50 0.50 0.60 1.30 12.50 0.60 14.20 7.15
Th 18.65 17.50 12.90 11.00 9.90 13.40 2.00 6.90 5.60 6.90 24.30 10.93
La 33.83 24.90 19.20 22.60 20.50 16.50 11.50 15.40 15.00 14.40 21.70 16.63
Ce 79.16 53.40 41.60 49.70 45.00 37.10 26.70 32.60 29.00 28.00 46.40 34.00
Pr 9.24 5.99 4.59 5.72 4.97 4.31 3.23 3.50 3.17 2.88 4.87 3.61
Nd 33.83 23.70 17.70 20.70 18.80 17.30 12.60 11.60 11.50 10.70 18.20 13.00
Sm 7.85 4.54 3.58 4.84 4.05 3.95 3.06 2.69 2.65 2.35 3.22 2.73
Eu 0.96 0.59 0.41 0.58 0.49 0.37 0.33 0.49 0.48 0.74 0.64 0.59
Gd 7.49 5.60 4.40 5.64 4.42 4.14 3.73 3.43 3.18 2.30 3.59 3.13
Tb 1.41 1.15 0.83 1.13 0.83 0.86 0.75 0.75 0.65 0.45 0.68 0.63
Dy 9.14 7.74 6.15 7.44 5.03 5.70 4.88 5.00 4.64 2.38 4.11 4.03
Ho 2.09 1.55 1.26 1.53 1.05 1.26 0.99 1.12 1.06 0.48 0.90 0.89
Er 5.86 5.30 4.10 4.78 2.90 3.30 3.00 3.38 3.23 1.25 2.48 2.59
Tm 0.81 0.76 0.60 0.74 0.43 0.54 0.45 0.50 0.47 0.18 0.34 0.37
Yb 5.05 5.12 3.87 4.40 2.84 3.45 3.21 3.11 2.74 1.18 2.49 2.38
Lu 0.7 0.67 0.53 0.63 0.34 0.50 0.46 0.44 0.39 0.20 0.31 0.34
LOI 1.11 1.00 0.80 0.80 1.10 1.00 0.70 0.30 0.20 0.10 0.20 0.20
Table DR2. Whole rock compositional data for selected samples and leucosomes oriented
parallel to S1 and S2 fabrics, respectively (see slab D, E, Fig. 7).
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Sample
pair K1/K2 2B/2E 2B/2H K1-EC86
K1/avg.
leucosomes
Gain/Loss Gain/Loss Gain/Loss Gain/Loss Gain/Loss
rel. to
Ci0
wt.% or
ppm
rel. to
Ci0
wt.% or
ppm
rel. to
Ci0
wt.% or
ppm
rel. to
Ci0
wt.% or
ppm
rel. to
Ci0
wt.% or
ppm
ΔCi/C
i0 ΔC
i ΔC
i/C
i0 ΔC
i ΔC
i/C
i0 ΔC
i ΔC
i/C
i0 ΔC
i ΔC
i/C
i0 ΔC
i
SiO2 0.03 1.81 0.00 0.19 0.01 0.81 0.03 1.98 0.02 1.12
TiO2 -0.18 -0.07 -0.55 -0.15 0.92 0.25 -0.32 -0.12 -0.56 -0.21
Al2O3 -0.03 -0.45 0.01 0.12 -0.03 -0.40 -0.04 -0.53 0.06 0.88
Fe2O3 -0.17 -0.50 -0.29 -0.65 0.38 0.86 -0.25 -0.75 -0.35 -1.05
MnO -0.25 -0.01 0.00 0.00 0.02 0.00 0.50 0.02 -0.43 -0.02
MgO -0.17 -0.11 -0.56 -0.23 1.23 0.51 -0.29 -0.18 -0.60 -0.38
CaO -0.07 -0.08 -0.21 -0.16 0.35 0.27 -0.34 -0.38 -0.16 -0.17
Na2O -0.01 -0.04 -0.19 -0.46 0.31 0.74 0.05 0.13 0.21 0.55
K2O 0.02 0.12 0.35 1.80 -0.31 -1.62 -0.02 -0.11 0.29 1.56
P2O5 -0.12 -0.03 0.19 0.04 0.07 0.01 -0.16 -0.04 -0.55 -0.14
As 0.27 0.41 -0.21 -0.30 0.24 0.33 7.67 11.51 0.40 0.60
Cs -0.33 -4.26 0.02 0.12 0.19 1.23 -0.26 -3.39 -0.54 -6.92
Rb -0.04 -10.90 0.15 36.35 -0.16 -39.75 0.18 47.63 0.04 9.75
Ba 0.08 34.17 -0.26 -82.14 -0.23 -70.89 -0.16 -65.74 0.32 129.47
Sr 0.22 14.70 -0.04 -2.49 0.14 7.91 -0.11 -7.56 0.51 34.02
Pb -0.21 -0.29 1.93 2.51 0.33 0.43 12.51 17.51 8.01 11.22
Ni -0.21 -1.08 -0.54 -1.40 3.30 8.59 0.51 2.61 -0.31 -1.60
V -0.14 -3.88 -0.60 -14.96 0.71 17.73 -0.25 -6.98 -0.58 -16.34
Ga -0.19 -3.62 -0.09 -1.54 0.03 0.49 -0.07 -1.29 -0.16 -3.21
Zn -0.15 -4.87 -0.74 -22.97 0.64 19.87 1.56 50.06 -0.48 -15.28
U -0.22 -0.59 -0.20 -0.39 -0.03 -0.07 0.82 2.20 -0.34 -0.93
Zr -0.18 -33.08 -0.72 -92.26 -0.99 -127.07 -0.33 -60.01 -0.55 -100.12
Hf -0.16 -0.78 -0.69 -3.09 -0.14 -0.63 -0.23 -1.10 -0.50 -2.39
Y -0.05 -2.47 -0.25 -10.19 -0.28 -11.10 -0.25 -12.47 -0.46 -22.79
Nb -0.20 -2.45 -0.33 -2.98 -0.05 -0.45 -0.35 -4.19 0.48 5.79
Ta -0.16 -0.20 -0.14 -0.10 -0.27 -0.19 -0.58 -0.70 5.04 6.05
Th -0.37 -6.45 -0.84 -10.89 -0.22 -2.83 -0.23 -4.09 -0.37 -6.43
La -0.09 -2.19 -0.40 -7.66 0.09 1.66 -0.34 -8.39 -0.32 -8.05
Ce -0.06 -3.46 -0.36 -14.80 0.10 4.18 -0.30 -16.27 -0.35 -18.94
Pr -0.04 -0.24 -0.29 -1.35 0.10 0.47 -0.28 -1.68 -0.39 -2.34
Nd -0.12 -2.90 -0.29 -5.05 0.08 1.43 -0.27 -6.39 -0.44 -10.52
Sm 0.07 0.32 -0.14 -0.51 0.15 0.54 -0.13 -0.59 -0.39 -1.78
Eu -0.01 -0.01 -0.19 -0.08 0.22 0.09 -0.37 -0.22 0.01 0.01
Gd 0.01 0.07 -0.15 -0.66 0.02 0.10 -0.26 -1.46 -0.43 -2.43
Tb -0.01 -0.01 -0.09 -0.08 0.02 0.01 -0.25 -0.29 -0.44 -0.51
Dy -0.03 -0.26 -0.20 -1.25 -0.17 -1.03 -0.26 -2.04 -0.47 -3.65
Ho -0.01 -0.01 -0.21 -0.27 -0.15 -0.19 -0.19 -0.29 -0.42 -0.65
Er -0.09 -0.50 -0.27 -1.09 -0.28 -1.15 -0.38 -2.00 -0.51 -2.68
Tm -0.02 -0.02 -0.25 -0.15 -0.27 -0.16 -0.29 -0.22 -0.50 -0.38
Yb -0.14 -0.70 -0.17 -0.65 -0.25 -0.98 -0.33 -1.67 -0.53 -2.71
Lu -0.06 -0.04 -0.13 -0.07 -0.35 -0.18 -0.25 -0.17 -0.49 -0.33
LOI -0.20 -0.20 -0.12 -0.10 0.40 0.32 0.00 0.00 -0.80 -0.80
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Table DR3. Results of volume-composition data calculations, where ∆𝐶𝑖is the difference
between the original and altered (e.g. modified by reactive melt flow) rock, 𝐶0𝑖 represents the
initial concentration of the element i in the unaltered rock. Note that the positive and negative
values represent the gain and loss, respectively, of each element in the altered rock in
contrast to the unaltered rock.
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