# Dynamic Metasomatism: Stable Isotopes, Fluid Evolution, and Deformation of Albitite and Scapolite Metagabbro (Bamble Lithotectonic Domain, South Norway)

Authors: Ane K. Engvik; Heinrich Taubald; Arne Solli; Tor Grenne; Håkon Austrheim
Journal: Geofluids
 (2018)

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## Abstract

New stable isotopic data from mineral separates of albite, scapolite, amphibole, quartz, and calcite of metasomatic rocks (Bamble lithotectonic domain) give increased knowledge on fluid type, source, and evolution during metamorphism. Albite from a variety of albitites givesδ18OSMOW values of 5.1–11.1‰, while quartz from clinopyroxene-bearing albitite gives 11.5–11.6‰. δ18OSMOW values for calcite samples varies between 3.4 and 12.4‰ and shows more consistent δ13C values of −4.6 to -6.0‰. Amphibole from scapolite metagabbro yields a δ18OSMOW value of 4.3 to 6.7‰ and δDSMOW value of −84 to −50‰, while the scapolite gives δ18OSMOW values in the range of 7.4 to 10.6‰. These results support the interpretation that the original magmatic rocks were metasomatised by seawater solutions with a possible involvement from magmatic fluids. Scapolitisation and albitisation led to contrasting chemical evolution with respect to elements like P, Ti, V, Fe, and halogens. The halogens deposited as Cl-scapolite were dissolved by albitisation fluid and reused as a ligand for metal transport. Many of the metal deposits in the Bamble lithotectonic domain, including Fe-ores, rutile, and apatite deposits formed during metasomatism. Brittle to ductile deformation concurrent with metasomatic infiltration illustrates the dynamics and importance of metasomatic processes during crustal evolution.


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## Body

## 1. Introduction

Metasomatism is the pervasive alteration of rocks with respect to both mineralogical and chemical composition. It results from interaction with fluids, sometimes causing albitisation by replacement of rock units by Na-rich feldspar, and scapolitisation forming scapolite-bearing rocks. These fluids can infiltrate under highly variable geological settings and PT conditions and originate from a meteoric, magmatic, or metamorphic environment. Albitisation is reported in deep weathering profiles [1, 2], in epiclastic sediments during diagenesis and low-grade metamorphism [3], in granitoids during late magmatic alteration [4], and in association with fluid migration in mobile belts [5]. Regional-scale metasomatism is a widely recognized phenomenon in a number of rock types and tectonic settings [6, 7]. Metasomatism is an important guide to hydrothermal ore deposits and represents a characteristic feature of many orogenic gold deposits, iron oxide-apatite (IOA), iron oxide-Cu-Au (IOCG), and U deposits [6, 8–11].The Bamble and Kongsberg-Modum lithotectonic domains of south Norway represent classic high-grade metamorphic terrains [12–18], which contain a series of different metasomatic rocks. An early scapolitisation event, where Cl-rich scapolite coexisted with enstatite, phlogopite, amphibole, and rutile is constrained at 600 to 700°C at mid-crustal levels [19–21]. Mg-Al-rich lithologies such as orthoamphibole-cordierite schists occur together with scapolitised rocks [22]. Subsequently, albitisation transformed scapolite metagabbro and regionally distributed mafic and granitoid rocks to albitites, dominated by albite, with varying amounts of rutile, carbonate, chlorite, and locally prehnite, pumpellyite, and analcime. Albitisation is widespread in the Mesoproterozoic rocks of the Sveconorwegian orogen in southern Scandinavia (Figure 1) [18, 21, 23]. In addition, the Bamble and Kongsberg-Modum lithotectonic domains are characterised by a high density of mineral deposits including the common occurrence of apatite and rutile deposits [23, 24] and a high density of hydrothermal Fe-deposits including veins and breccias of nickeliferous pyrrhotite-apatite, magnetite-apatite, magnetite and hematite, and Fe-oxide skarn deposits [25, 26].Figure 1
(a) Regional geological map of south Norway and Sweden indicating areas of widespread Na-metasomatism [23]. Arrow indicating the study area (Figure 1(b)). B = Bamble lithotectonic domain; K = Kongsberg-Modum lithotectonic domain; RAC = Rogaland Anorthosite Complex; KPFZ = Kristiansand-Porsgrunn Fault Zone; KSFZ = Kongsberg-Sokna Fault Zone; MZ = Mylonite Zone; DBT = Dalsland Boundary Thrust; GZ = Götaelv Zone; SFCZ = Sveconorwegian Frontal Deformation Zone; and LLDZ = Linköping-Lofthammer Deformation Zone. (b) Geological map of the investigated Kragerø area in the Bamble lithotectonic domain with sample localities.
(a)
(b)The metasomatic processes affecting the Bamble lithotectonic domain have locally transformed the rocks so strongly that we cannot trace the precursor, and therefore a full understanding of the processes is still lacking. However, a number of papers have solved various aspects of the metasomatic processes including widespread formation of scapolite metagabbro [19–21, 27] through Mg-Cl metasomatism, replacement textures in apatite [28–30], rutile formation [31], carbonate deposition [32], tourmaline formation [33], and sapphirine-corundum crystallization [34]. While the scapolitisation process with respect to mineral reactions is relatively well understood in the Kragerø region, albitisation is a more complex process and less constrained. Extensive albitisation is seen along veins, as brecciation, as formation of foliated albititic felsites and chlorite schists, as carbonate-rich albitite, and as large-scale albitite bodies [23, 35].In this paper, we present stable O-, H-, and C-isotope data on mineral separates from albitites and scapolite metagabbro with the purpose of constraining the fluid type and source. Different models for fluid evolution are then discussed. Whole rock geochemical data is presented in order to illustrate the chemical changes and discussed relative to mineralogical replacement and mineral deposition. Brittle and ductile structural elements associated with the metasomatism are used to discuss the dynamics of fluid processes.


## 2. Geological Setting

The Sveconorwegian orogenic belt in SW Scandinavia consists of late Palaeoproterozoic to Mesoproterozoic continental crust reworked during the Sveconorwegian orogeny [18, 41, 42]. The orogen is divided into several lithotectonic gneiss domains separated by crustal scale shear zones (Figure 1(a)). The Bamble lithotectonic domain in south Norway shows a SW-NE structural trend and consists of high-grade ortho- and paragneisses and amphibolites [43]. The oldest known rocks are orthogneisses ranging in age from ca. 1570 to 1460 Ma [44–46]. They are intruded by younger plutonic rocks, including a 1294±38 Ma tonalite pluton [20], 1200 to 1150 Ma mafic and felsic plutonic rocks [20, 45, 46], ca. 1060 Ma pegmatite bodies [47], and ca. 990 to 925 Ma Sveconorwegian postcollisional granite plutons [45]. The studied area is located close to the Oslo Rift with abundant magmatic activity in Permian time (Figure 1(a)).Metamorphism in Bamble was associated with regional-scale deformation and the formation of a strong lithological and regional NE-SW tectonic banding. Zircon, monazite, titanite, and rutile U-Pb ages from the area place the high-grade metamorphism as part of an early phase of the Sveconorwegian orogeny in the time interval 1140–1080 Ma [20, 41, 48–50]. The gneisses are dominantly amphibolite-facies, with metamorphic grade increasing to granulite-facies in the Arendal area (P=0.6–0.8 GPa; T = 750–850°C) [13, 16, 51, 52]. In addition, there are several occurrences of rocks with granulite-facies assemblages, including charnockitic gneiss bodies, as well as conformable lenses and layers of sapphirine-bearing rocks [14, 53], which are exposed north of Arendal and Kragerø [17, 54, 55].The Kragerø area (Figure1(b)) consists of a layered complex of mafic rocks and variable gneisses and quartzites. The mafic rocks are amphibolites and metagabbros including bodies of gabbro [56]. Orthogneisses are of granitic, granodioritic, quartzdioritic, and tonalitic composition. Quartzites containing sillimanite are interlayered with garnet amphibolite, felsic gneiss, and garnet- and cordierite-bearing mica gneiss.Na-metasomatism in the form of albitisation is regionally extensive in the Precambrian crust of southern Scandinavia and is particularly widespread in the Bamble and Kongsberg-Modum lithotectonic domains and the Norwegian part of the Mylonite Zone (Figure1(a)) [23]. In the Bamble lithotectonic domain, albitisation is present from the northeastern boundary to the Oslo Rift and southwestwards through the domain. Large bodies of albitite are found in the vicinity of Kragerø and towards Arendal [23, 57–59]. Mg-Cl-metasomatised rocks in the form of scapolite metagabbros occur widespread as part of the mapped amphibolites and metagabbro, commonly in conjunction with the albitites [19, 20, 50].


## 3. Analytical Methods

Different types of albitites and scapolite metagabbro were mapped and sampled in the Kragerø area of Bamble lithotectonic domain (Table1; Figure 1). Polished thin sections were studied via optical and scanning electron microscopy (SEM), using a LEO 1450 VP instrument at the Geological Survey of Norway (NGU).Table 1
Key samples with mineral assemblage.
Sample number
E-UTM
N-UTM
Rock/alteration type
Protolith
Locality
Major minerals
Minor minerals
Accessory minerals
Secondary minerals
AE2
530144
6534901
Albitite
Tonalite
Ringsjø
Ab Qz
Cc Chl
Rt
AE21
530891
6535542
Albitite alteration zone
Tonalite
Ringsjø
Ab Qz Chl Cc
Opq
Sercitisation
AE10A
530173
6534951
Albitite alteration zone
Gabbro
Ringsjø
Ab Qz
Rt Ap Opq
AE11A
530173
6534951
Albitite alteration zone
Gabbro
Ringsjø
Ab
1Ø32.80
532200
6536000
Albitite alteration zone
Gabbro
Ødegården verk
Ab Amph Chl
Cc
Rt Ap
AE40
527800
6527900
Albitite, carbonate-rich
Infiltration zone in gabbro
Langøy
Ab Cc Dol
Rt
AE93
527967
6528018
Albitite, carbonate-rich
Infiltration zone in gabbro
Langøy
Ab Cc
Rt Opq
AE99
527967
6528018
Albitite (Ab felsite, Cc-bearing)
Gabbro
Langøy
Ab Cc Amph
Phl
Opq
Chl
AE63
520300
6525650
Cpx-bearing albitite
Åtangen
Ab Qz
Kfsp Cpx
Ttn Ap Zrc Opq
Chl Cc
AE96
520815
6525558
Cpx-bearing albitite
Storkollen
Ab Qz
Kfsp Cpx
Ttn Ap Zrc
Chl Cc
1Ø31.55
532200
6536000
Scp metagabbro
Gabbro
Ødegården verk
Scp Amph
Rt Ap
1Ø47.40
532200
6536000
Scp metagabbro
Gabbro
Ødegården verk
Scp Amph
Rt Ap
2Ø76.40
532200
6536000
Scp metagabbro
Gabbro
Ødegården verk
Scp Amph
Phl En
Rt Ap
AE46
529100
6528700
Scp metagabbro
Gabbro
Langøy
Scp Amph Phl
Rt
AE110
528149
6528140
Scp metagabbro
Gabbro
Langøy
Scp Amph Phl
Cc
RtWhole rock major and trace element analyses (Table2) were carried out at the NGU. Major elements were measured on fused glass beads prepared by 1 : 7 dilution with lithium tetraborate. Trace elements were measured from pressed tablets. The samples were analysed on a PANalytical Axios XRF spectrometre equipped with a 4 kW Rh X-ray end-window tube, using synthetic and international standards for calibration as described by Govindaraju [60]. Rock samples used for whole rock geochemistry were selected as being representative and homogenous, with good control on mineralogy and petrography.Table 2
Whole rock geochemical data, major and trace elements.
(a)
Sample number
Locality
Rock type
Protolith
Major elements (%)
Sum
SiO2
Al2O3
Fe2O3
TiO2
MgO
CaO
Na2O
K2O
MnO
P2O5
LOI
AE7
Ringsjø
Gabbro/metagabbro
Gabbro
45.1
16.6
11.6
1.31
9.59
9.07
3.62
1.22
0.034
0.112
1.58
99.80
AE45A
Langøy
Gabbro/metagabbro
Gabbro
47.1
20.5
8.80
0.770
9.47
10.2
2.65
0.152
0.112
0.078
0.000
99.84
AE45B
Langøy
Gabbro/metagabbro
Gabbro
47.4
21.0
8.73
0.892
8.29
9.92
2.87
0.261
0.119
0.154
0.231
99.86
AE102
Langøy
Gabbro/metagabbro
Gabbro
46.6
17.0
12.1
1.52
7.75
7.67
2.95
1.75
0.136
0.141
2.32
99.9
AE66
Åtangen
Gabbro/metagabbro
Gabbro
47.6
17.4
12.1
1.52
6.12
9.83
3.64
0.574
0.155
0.236
0.596
99.78
AE58
Åtangen
Gabbro/metagabbro
Gabbro
54.3
13.0
4.29
0.872
12.1
8.38
4.84
1.28
0.017
0.179
0.679
99.91
1Ø42.40
Ødegården Verk
Gabbro/metagabbro
Gabbro
45.2
15.8
16.6
3.06
4.44
7.24
3.96
1.63
0.175
0.450
0.931
99.5
2Ø18.20
Ødegården Verk
Gabbro/metagabbro
Gabbro
50.3
13.6
18.2
2.07
2.19
6.50
4.06
1.30
0.255
0.736
0.085
99.3
2Ø30.30
Ødegården Verk
Gabbro/metagabbro
Gabbro
57.6
15.9
5.40
2.30
3.81
6.20
6.88
0.252
0.019
0.547
0.910
99.8
AE22
Fesettjern Ringsjø area
Tonalite
Tonalite
68.6
14.1
4.99
0.330
0.420
3.95
4.94
0.641
0.018
0.051
1.62
99.71
AE71
Fesettjern Ringsjø area
Tonalite
Tonalite
71.6
14.9
0.945
0.355
0.770
4.34
5.45
0.272
0.011
0.077
1.08
99.82
1Ø19.10
Ødegården Verk
Scapolite metagabbro
Gabbro
49.9
16.6
4.17
3.03
7.51
8.91
6.36
0.315
0.017
0.361
1.60
98.8
1Ø18.80
Ødegården Verk
Scapolite metagabbro
Gabbro
49.7
17.5
4.27
2.82
6.26
8.43
6.73
0.391
0.015
0.383
1.55
98.0
1Ø31.55
Ødegården Verk
Scapolite metagabbro
Gabbro
50.4
17.1
3.93
2.88
6.72
8.79
6.85
0.377
0.014
0.352
0.824
98.2
1Ø47.40
Ødegården Verk
Scapolite metagabbro
Gabbro
50.8
18.0
2.66
3.17
6.02
8.13
7.18
0.478
0.013
0.456
1.22
98.1
2Ø74.20
Ødegården Verk
Scapolite metagabbro
Gabbro
49.6
16.7
4.08
3.38
7.04
8.78
6.63
0.471
0.013
0.491
0.803
98.0
2Ø76.60
Ødegården Verk
Scapolite metagabbro
Gabbro
49.6
18.2
2.33
2.74
9.52
5.36
6.31
2.27
<0.01
0.514
1.52
98.3
AE43
Langøy
Scapolite metagabbro
Gabbro
42.7
19.9
7.99
0.192
12.4
11.4
3.12
0.676
0.108
0.028
1.37
99.88
AE46
Langøy
Scapolite metagabbro
Gabbro
44.9
17.9
8.82
0.695
11.3
9.52
4.12
1.07
0.076
0.069
1.32
99.79
AE49
Langøy
Scapolite metagabbro
Gabbro
46.2
20.3
6.47
0.760
8.86
9.64
4.65
1.20
0.051
0.109
1.62
99.85
AE103
Langøy
Scapolite metagabbro
Gabbro
44.7
16.0
12.4
1.41
7.59
8.76
4.35
1.69
0.036
0.134
1.31
98.3
AE110
Langøy
Scapolite metagabbro
Gabbro
45.7
17.3
5.78
1.31
9.17
10.1
5.21
0.816
0.053
0.189
2.68
98.3
AE 146
Åtangen
Albitite
Unknown
65.4
18.8
0.809
0.283
0.800
1.51
10.5
0.097
0.030
0.060
1.02
99.3
AE 143
Åtangen
Albitite
Unknown
78.1
12.3
0.471
0.150
0.260
0.315
7.15
0.073
<0.01
0.027
0.420
99.3
AE 144
Åtangen
Albitite
Unknown
76.5
13.0
0.517
0.197
0.274
1.19
6.97
0.248
<0.01
0.039
1.12
100
AE98C
Storkollen
Albitite
Unknown
75.8
13.3
0.536
0.137
0.334
0.722
7.47
0.101
0.014
0.012
0.765
99.2
AE2
Ringsjø
Albitite
Tonalite
72.4
14.9
0.407
0.389
0.359
1.71
7.94
0.165
<0.01
0.086
1.39
99.77
AE16
Ringsjø
Albitite
Tonalite
72.9
14.6
1.07
0.366
0.368
1.17
8.09
0.139
0.014
0.056
1.14
99.83
AE21
Fesettjern Ringsjø area
Albitite
Tonalite
69.9
13.1
5.12
0.337
0.099
2.23
6.74
0.334
<0.01
0.048
1.88
99.77
AE 73
Ringsjø
Albitite
Gabbro/metagabbro
60.5
18.3
2.28
2.18
2.55
1.46
9.19
0.369
0.015
0.023
2.80
99.7
AE10A
Ringsjø
Albitite
Gabbro/metagabbro
63.2
20.3
0.286
3.59
0.326
0.525
9.90
0.963
<0.01
0.127
0.795
99.92
AE11A
Ringsjø
Albitite
Gabbro/metagabbro
67.7
19.8
0.062
0.381
0.011
0.178
11.5
0.080
<0.01
<0.01
0.253
100.0
AE10B
Ringsjø
Albitite
Gabbro/metagabbro
52.4
18.2
2.14
3.12
3.50
5.62
7.35
0.901
0.013
0.586
5.45
99.33
AE11C
Ringsjø
Albitite
Gabbro/metagabbro
55.2
17.5
3.04
3.69
5.66
4.31
7.13
0.954
0.012
0.299
1.99
99.84
1Ø17.10
Ødegården Verk
Albitite
Gabbro/metagabbro
58.0
19.9
1.62
0.488
3.94
3.96
7.91
0.726
0.013
0.476
2.67
99.8
1Ø32.80
Ødegården Verk
Albitite
Gabbro/metagabbro
50.6
15.1
3.29
4.04
7.68
9.65
5.28
0.456
0.015
0.784
2.61
99.4
1Ø17.30
Ødegården Verk
Albitite
Gabbro/metagabbro
53.5
16.0
2.76
4.31
6.51
7.97
5.93
0.336
0.015
0.526
1.90
99.8
AE93
Langøy
Albitite Cc-rich
Infiltration zone
55.9
9.52
2.70
0.744
3.76
9.37
5.39
0.132
0.039
0.171
12.1
99.9
AE40
Langøy
Albitite Cc-rich
Infiltration zone
49.0
6.68
4.30
0.504
6.25
11.8
3.69
0.150
0.055
0.101
17.3
99.86
AE99
Langøy
Albitite Cc-rich
Gabbro/metagabbro
58.2
11.9
3.56
1.35
6.52
8.05
6.80
0.263
0.017
0.196
3.21
100
AE100
Langøy
Albitite Cc-rich
Gabbro/metagabbro
52.7
13.9
4.98
0.910
10.6
5.96
4.65
2.86
0.014
0.166
3.08
99.8
AE63
Åtangen
Albitite Cpx-bearing
Unknown
76.4
13.2
1.23
0.173
0.255
1.16
6.92
0.407
0.014
0.027
0.182
99.92
AE96
Storkollen
Albitite Cpx-bearing
Unknown
75.5
14.0
0.559
0.175
0.379
1.43
7.35
0.384
0.012
0.026
0.386
100
(b)
Sample number
Locality
Rock type
Protolith
Trace elements (mg/kg)
Ba
Br
Ce
Co
Cr
Cu
Ga
La
Nb
Nd
Ni
Pb
Rb
Sc
Sn
Sr
Th
V
Y
Zn
Zr
AE7
Ringsjø
Gabbro/metagabbro
Gabbro
56
<2
31
51.2
179
2.7
21.8
<10
1.9
22
141
3.2
24.9
23.3
5.2
114
<4
160
28
5
79
AE45A
Langøy
Gabbro/metagabbro
Gabbro
35
<2
<20
50.7
66.8
17.1
15.8
<10
<1
13
181
<3
3.4
7.6
<5
261
<4
83
11
51
45
AE45B
Langøy
Gabbro/metagabbro
Gabbro
64
4.7
22
48.6
24.0
19.7
17.6
11
1.1
<10
158
<3
7.3
8.1
7.2
280
<4
96
18
60
77
AE102
Langøy
Gabbro/metagabbro
Gabbro
194
<2
<20
49.6
90.7
32.5
18.5
<10
1.3
<10
107
13.5
29.1
24.2
9.7
144
<4
193
27.6
43.0
86.8
AE66
Åtangen
Gabbro/metagabbro
Gabbro
111
2.7
31
45.6
145
88.0
20.4
13
8.5
18
71.4
<3
13.5
21.2
7.1
268
<4
169
29
57
124
AE58
Åtangen
Gabbro/metagabbro
Gabbro
22
<2
47
11.9
43.2
<2
14.6
18
8.6
27
44.3
3.1
53.8
13.2
6.8
63.3
8
85
33
2
163
1Ø42.40
Ødegården Verk
Gabbro/metagabbro
Gabbro
510
<2
54
46.1
60.1
38.3
24.2
23
5.5
33
52.4
12.7
42.3
22.9
14.4
312
<4
228
40.9
85.6
171
2Ø18.20
Ødegården Verk
Gabbro/metagabbro
Gabbro
753
4.0
133
17.1
<4
11.8
25.3
51
16.1
71
<2
9.9
18.6
37.2
13.5
267
6.1
18.3
78.2
93.4
644
2Ø30.30
Ødegården Verk
Gabbro/metagabbro
Gabbro
71
2.1
103
15.7
<4
<2
30.0
40
16.6
69
18.7
9.6
1.8
39.8
13.5
145
4.5
74.3
114
4.4
586
AE22
Fesettjern Ringsjø area
Tonalite
Tonalite
135
3.5
193
<4
<4
2.2
30.2
89
20.8
81
5.1
<3
19.5
6.7
6.9
425
14
<5
95
2
654
AE71
Fesettjern Ringsjø area
Tonalite
Tonalite
34
<2
118
<4
<4
<2
31.1
55
19.3
57
5.6
<3
4.1
6.0
5.7
283
16
6
89
2
655
1Ø19.10
Ødegården Verk
Scapolite metagabbro
Gabbro
66
51.5
42
10.7
102
<2
33.6
18
6.0
43
204
9.9
3.1
22.6
12.1
105
<4
402
99.0
9.4
151
1Ø18.80
Ødegården Verk
Scapolite metagabbro
Gabbro
86
68.7
42
11.5
52.1
<2
30.5
<10
4.8
41
162
11.1
5.1
20.0
14.7
126
<4
322
84.3
10.1
155
1Ø31.55
Ødegården Verk
Scapolite metagabbro
Gabbro
48
51.3
45
13.4
24.6
<2
29.9
17
4.7
45
125
9.6
2.8
22.6
12.6
113
<4
352
92.0
5.2
170
1Ø47.40
Ødegården Verk
Scapolite metagabbro
Gabbro
49
73.6
55
8.7
87.7
<2
28.6
20
5.1
48
96.5
9.0
10.4
24.4
10.1
84.4
<4
644
132
8.5
179
2Ø74.20
Ødegården Verk
Scapolite metagabbro
Gabbro
31
61.5
55
12.9
118
<2
30.5
12
6.1
50
149
10.5
3.0
20.0
11.6
82.9
<4
391
96.8
4.0
201
2Ø76.60
Ødegården Verk
Scapolite metagabbro
Gabbro
81
71.5
30
9.0
123
<2
32.8
11
5.0
22
218
10.4
93.1
16.6
10.7
75.7
<4
525
32.3
5.9
130
AE43
Langøy
Scapolite metagabbro
Gabbro
42
9.1
<20
59.5
48.0
<2
11.4
<10
<1
<10
351
3.7
13.5
<5
5.2
101
<4
23
3
53
12
AE46
Langøy
Scapolite metagabbro
Gabbro
44
28.0
22
55.5
135
19.7
12.8
<10
<1
<10
201
3.2
32.7
11.1
5.1
133
<4
86
11
23
35
AE49
Langøy
Scapolite metagabbro
Gabbro
56
34.8
35
36.7
55.3
6.9
13.6
<10
<1
10
162
3.6
40.1
9.1
<5
182
<4
88
11
22
53
AE103
Langøy
Scapolite metagabbro
Gabbro
100
32.8
45
48.0
90.6
8.2
16.9
20
1.5
20
95.0
15.9
16.3
24.9
15.1
87.7
<4
187
28.0
15.0
84.3
AE110
Langøy
Scapolite metagabbro
Gabbro
29
29.5
33
43.8
37.8
4.0
15.7
16
2.1
19
157
14.4
18.3
10.5
13.7
137
<4
111
23.3
21.1
95.7
AE 146
Åtangen
Albitite
Unknown
12
56
<4
<5
<5
19.1
22
17.2
34
<5
<5
<5
<5
<5
43.7
19.4
42.4
66.6
<5
215
AE 143
Åtangen
Albitite
Unknown
<10
78
<4
6.8
<5
22.1
28
11.5
48
<5
<5
<5
<5
<5
10.7
8.4
13.5
94.3
<5
190
AE 144
Åtangen
Albitite
Unknown
10
30
<4
<5
<5
25.4
<15
18.3
21
<5
<5
<5
<5
<5
22.1
11.1
14.2
98.3
<5
281
AE98C
Storkollen
Albitite
Unknown
<10
<2
<20
<4
<4
<2
25.6
<10
6.8
<10
<2
12.0
1.3
<5
9.8
9.6
10.2
<5
7.7
7.8
130
AE2
Ringsjø
Albitite
Tonalite
46
2.8
123
<4
<4
<2
28.0
46
20.9
89
5.1
3.9
2.1
7.5
10.5
57.9
11
18
84
3
696
AE16
Ringsjø
Albitite
Tonalite
11
2.5
74
<4
<4
<2
29.4
19
23.7
63
11.5
<3
1.3
6.7
5.5
22.8
10
40
117
4
640
AE21
Fesettjern Ringsjø area
Albitite
Tonalite
30
2.5
134
<4
5.1
<2
26.5
56
20.2
63
3.4
4.0
10.4
6.5
5.2
119
13
9
73
2
585
AE 73
Ringsjø
Albitite
Gabbro/metagabbro
29
19
8.8
98.3
<5
19.5
<15
8.2
<10
29.1
<5
8.3
22.9
<5
104
<3
111
22.5
16.9
135
AE10A
Ringsjø
Albitite
Gabbro/metagabbro
19
<2
<20
<4
29.0
<2
16.7
<10
22.0
<10
2.1
<3
31.7
5.2
7.2
44.6
<4
89
6
2
120
AE11A
Ringsjø
Albitite
Gabbro/metagabbro
<10
2.4
<20
<4
4.5
<2
16.4
<10
3.9
<10
<2
3.0
<1
<5
5.9
20.6
<4
13
2
<1
113
AE10B
Ringsjø
Albitite
Gabbro/metagabbro
30
3.0
39
7.3
61.1
<2
20.3
11
4.8
27
47.6
3.2
32.1
42.9
5.7
98.9
<4
233
64
5
118
AE11C
Ringsjø
Albitite
Gabbro/metagabbro
35
2.6
28
9.7
54.8
<2
20.5
16
6.8
27
55.7
<3
28.8
30.3
6.0
144
<4
307
66
4
144
1Ø17.10
Ødegården Verk
Albitite
Gabbro/metagabbro
129
<2
33
<4
25.1
<2
27.6
17
<1
25
33.3
8.6
12.8
7.2
10.2
207
<4
117
32.0
14.9
247
1Ø32.80
Ødegården Verk
Albitite
Gabbro/metagabbro
103
4.0
49
10.2
33.4
<2
32.0
25
8.6
52
163
9.4
8.7
38.9
12.2
126
<4
446
99.2
10.1
286
1Ø17.30
Ødegården Verk
Albitite
Gabbro/metagabbro
51
<2
34
8.1
23.8
<2
33.0
12
6.7
45
141
9.8
5.4
38.5
10.3
150
<4
416
85.1
5.9
236
AE93
Langøy
Albitite Cc-rich
Infiltration zone
<10
<2
26
<4
24.5
<2
8.4
<10
6.2
18
5.9
9.6
1.3
<5
12.7
14.6
5.1
51.9
20.8
<1
131
AE40
Langøy
Albitite Cc-rich
Infiltration zone
<10
<2
<20
<4
24.3
<2
6.2
<10
4.3
<10
10.9
3.5
<1
<5
<5
15.2
<4
45
16
1
152
AE99
Langøy
Albitite Cc-rich
Gabbro/metagabbro
19
<2
83
<4
39.3
<2
10.3
16
17.8
86
22.4
15.5
4.4
9.5
15.0
9.6
10.8
82.1
133
4.9
304
AE100
Langøy
Albitite Cc-rich
Gabbro/metagabbro
119
<2
29
9.0
40.9
<2
15.1
15
8.2
23
47.9
11.2
50.2
11.2
11.9
55.2
<4
88.4
22.5
2.8
188
AE63
Åtangen
Albitite Cpx-bearing
Unknown
17
<2
65
<4
<4
<2
22.4
28
12.4
31
3.3
4.0
2.8
<5
6.8
36.1
14
5
81
4
202
AE96
Storkollen
Albitite Cpx-bearing
Unknown
27
<2
<20
<4
<4
<2
24.3
<10
12.5
13
3.2
12.5
3.8
<5
12.9
31.8
12.1
6.9
61.7
1.1
200Stable isotopic data are presented in Table3. The oxygen isotope composition (16O, 17O, and 18O) of handpicked mineral separates of albite, scapolite, amphibole, and quartz was measured at the University of Tübingen using a method similar to that described by Sharp [61] and Rumble III and Hoering [62], which is described in more detail in Kasemann et al. [63]. Between 2 to 4 mg of sample was loaded onto a small Pt sample holder, which was pumped to a vacuum of about 10−6 mbar. After prefluorination of the sample chamber overnight, the samples were heated with a CO2-laser in 50 mbars of pure F2. Excess F2 was separated from the O2 using KCl at 150°C by producing KF and releasing Cl2. The extracted O2 was collected quantitatively by adsorption on a molecular sieve (13X) at liquid nitrogen temperature in a sample vial. Subsequently the vial was removed from the line and heated to room temperature; thus, O2 is released as a gas and eventually analysed isotopically using a Finnigan MAT 252 isotope ratio mass spectrometer. Oxygen isotope compositions are given in the standard δ-notation and expressed relative to SMOW (Vienna Standard Mean Ocean Water) in permil (‰). Replicate oxygen isotope analyses of the standards, using NBS-28 quartz and UWG-2 garnet [64], generally have an average precision of ±0.1‰ for δ18O. The accuracy of δ18O values is commonly better than 0.2‰ compared to the accepted δ18O values for NBS-28 of 9.64‰ and UWG-2 of 5.8‰.Table 3
Stable isotopic data.
Sample number
Mineral
Rock type
Protolith
Locality
δ
18
O
S
M
O
W (‰)
δ
D
S
M
O
W (‰)
δ
13
C
P
D
B (‰)
CO3 (%  CaCO3)
AE 2
Albite
Albitite
Tonalite
Ringsjø
8.5
AE 21
Albite
Albitite alteration zone
Tonalite
Ringsjø
10.8
AE 10A
Albite
Albitite alteration zone
Gabbro
Ringsjø
5.1
AE 11A
Albite
Albitite alteration zone
Gabbro
Ringsjø
7.7
1Ø32.80
Albite
Albitite alteration zone
Gabbro
Ødegården Verk
8.4
AE 40
Albite
Albitite, carbonate-rich
Infiltration in gabbro
Langøy
7.0
AE 93
Albite
Albitite, carbonate-rich
Infiltration in gabbro
Langøy
6.3
AE 99
Albite
Albitite (Ab felsite, Cc-rich)
Gabbro
Langøy
5.5
AE 63
Albite
Cpx-bearing albitite
(Unknown)
Åtangen
10.8
AE 96
Albite
Cpx-bearing albitite
(Unknown)
Storkollen
11.1
AE 63
Quartz
Cpx-bearing albitite
(Unknown)
Åtangen
11.6
AE 96
Quartz
Cpx-bearing albitite
(Unknown)
Storkollen
11.5
AE 2
Calcite
Albitite
Tonalite
Ringsjø
4.5
-
5.7
1.6
AE 21
Calcite
Albitite alteration zone
Tonalite
Ringsjø
10.5
-
6.0
6.1
AE 40
Calcite
Albitite, carbonate-rich
Infiltration in gabbro
Langøy
5.8
-
5.0
1.0
AE 93
Calcite
Albitite, carbonate-rich
Infiltration in gabbro
Langøy
12.4
-
5.6
2.0
AE 99
Calcite
Albitite (Ab felsite, Cc-rich)
Gabbro
Langøy
3.4
-
4.6
28.1
1Ø31.55
Scapolite
Scp metagabbro
Gabbro
Ødegården Verk
9.1
1Ø47.40
Scapolite
Scp metagabbro
Gabbro
Ødegården Verk
8.4
2076.40
Scapolite
Scp metagabbro
Gabbro
Ødegården Verk
10.6
AE 46
Scapolite
Scp metagabbro
Gabbro
Langøy
8.2
AE 110
Scapolite
Scp metagabbro
Gabbro
Langøy
7.4
1Ø31.55
Amphibole
Scp metagabbro
Gabbro
Ødegården Verk
4.3
-
51
1Ø47.40
Amphibole
Scp metagabbro
Gabbro
Ødegården Verk
6.2
-
51
2Ø76.40
Amphibole
Scp metagabbro
Gabbro
Ødegården Verk
6.7
-
59
AE 46
Amphibole
Scp metagabbro
Gabbro
Langøy
4.3
-
57
AE 110
Amphibole
Scp metagabbro
Gabbro
Langøy
5.6
-
84
Overall analytical precision for O: ±0.2; overall analytical precision for H: ±2.0; overall analytical precision for C: ±0.1.For the D/H analysis of the minerals, an extraction line as described in [65] was used. Depending on the water content, a sufficient amount of hydrous minerals was loaded into 12 cm long quartz tubes in order to obtain >1 mg H2O. Water was released by heating the minerals in the tubes using a torch. H2O was then converted to H2 using Zn (see also Vennemann and O’Neil [65] for further details). H2 was then subsequently measured by a Finnigan MAT 252 Mass Spectrometer, using the dual inlet device. External precision is typically ±2‰, and all values are reported relative to SMOW.Stable isotope analysis (C, O) of carbonate samples was performed using a Finnigan MAT 252 gas source mass spectrometer combined with a Thermo Finnigan GasBench II/CTC Combi-Pal autosampler. Both devices are connected using the continuous flow technique with a He stream as carrier gas. About 0.1 mg dried sample powder is loaded into a 10 ml glass exetainer, sealed with rubber septum. The exetainers are placed in an aluminium tray and set to 72°C. After purging with pure He gas, 4–6 drops of 100% phosphoric acid are added. After a reaction time of about 90 minutes, the released CO2 is transferred (using a GC gas column to separate other components) to the mass spectrometer using a He carrier gas. The sample CO2 is measured relative to an internal laboratory tank gas standard, which is calibrated against internal and international carbonate standards (e.g., Laser marble, NBS-19). All values are given in ‰ relative to PDB (Vienna Pee Dee Belemnite) for C and SMOW/PDB for O. The external precision calculated over 10–15 standards is typically in the range of 0.05–0.06‰ for δ13C and 0.06–0.08‰ for δ18O. For further details see Spötl and Vennemann [66].


## 4. Na- and Mg-Cl-Metasomatic Rocks

### 4.1. Field and Structural Relations

In the Kragerø area, Mg-Cl-metasomatised scapolite-bearing rocks occur widespread as a part of the mapped amphibolite, metagabbro, and gabbro lithologies [19, 20, 23] and have been studied in detail at Ødegården Verk, Ringsjø, Åtangen, Valberg, and Langøy localities (Figure 1(b)). At Langøy and Ødegården Verk, transformation of pristine gabbro to scapolite metagabbro is observed along fluid fronts (Figure 2(a)). Medium-grained dark gabbro including olivine and pyroxenes is transformed into a medium- to coarse-grained scapolite metagabbro. The scapolite metagabbro occurs as an equigranular massive rock originally named ødegårdite [57]. Frequently, the scapolite metagabbro displays veining in the form of 0.5–2 cm wide veins, which are composed of the major rock-forming minerals scapolite, amphibole (edenite, pargasite, and actinolite), or phlogopite (Figures 2(b)–2(d)). Locally, this veining occurs with a high density initiating a layered structure in the rock (Figure 2(c)). The veining and banded structure develops during progressive deformation and formation of the rock foliation (Figure 2(d)). At the Åtangen locality, dynamic scapolitisation through synchronous brecciation is observed, where amphibolite and banded host schist are found as inclusions in a matrix of scapolite (Figures 2(e)–2(g)). White scapolite forms veins, or a scapolite-amphibole assemblage forms the groundmass in evolved breccias with rounded clasts. The veined and brecciated structure undergoes flattening (Figure 2(g)), evolving to a foliated scapolite-bearing amphibolitic rock (Figure 2(h)).Figure 2
Field photos of scapolite metagabbro and dynamic scapolitisation. (a) Gabbro with scapolitisation front. Locality Langøy. (b) Scapolite metagabbro with veining filled by scapolite and amphibole. Field of view is approximately one metre wide. Locality Langøy. (c) Scapolite metagabbro with a high density of scapolite veining resulting in a layered structure in the rock [20]. Field of view is approximately one metre wide. Locality Langøy. (d) Scapolite metagabbro with amphibole veining and flattened foliation [20]. Locality Langøy. (e) Brecciated amphibolite with a thin scapolite vein filling and rounded clasts. Locality Åtangen. (f) Intensive scapolitisation of an evolved breccia with amphibole veins, amphibole + scapolite matrix, and rounded clasts. Locality Åtangen. (g) Brecciated amphibolite with scapolite veins undergoing flattening. Locality Åtangen. (h) Foliated scapolite-bearing amphibolites. Locality Åtangen.
(a)
(b)
(c)
(d)
(e)
(f)
(g)
(h)Albitisation affects both mafic and granitoid lithologies in the Kragerø area, usually associated with the scapolite-bearing rocks, and normally postdating the scapolitisation. Albitisation takes place along veins and in breccias. Albite is the dominant mineral in foliated felsites, in chlorite schist, in carbonate-rich albitite, and in large-scale albitite bodies [23, 50]. Albitisation has been studied in detail in the Ringsjø-Ødegården Verk area [20, 35]. Both mafic (gabbro, scapolite metagabbro, and amphibolite) and granitoid protolith are transformed to albitite along veining, where the central vein consists of nearly pure albite (Figures 3(a)-3(b)). The replacement zone to the mafic host rock shows a widespread replacement of the mafic phases to chlorite (Figure 3(c)). Intensive albitisation affects part of the area resulting in a 0.5×2 km albitite body (Figure 1(b)).Figure 3
Field photos of albitites and dynamic albitisation. (a) Albitisation vein in metagabbro transforming the dark mafic rock to nearly pure albite. Locality Ringsjø. (b) Albitisation (red color) of tonalite (light color) along veining. Locality Fesettjern, Ringsjø area. (c) Vein albitisation (red color) causing chloritisation (greenish color) of scapolite metagabbro (dark grey). Locality Ringsjø. (d) Carbonate-rich albitite forming an approximate 5-metre wide vein deposit in the metagabbro. Locality Langøy. (e) Breccia containing clasts of albitised metagabbro in the matrix of a carbonate-rich albitite deposit. Field of view is approximately four metres wide. Locality Langøy. (f) Albitisation of metagabbro along veining with transformation to foliated albitic felsites. Locality Langøy. (g) Foliated albititic felsites with alternating light carbonate-albite and green-grey chlorite-schist bands. Locality Langøy. (h) Banded clinopyroxene-bearing albitite. Locality Åtangen.
(a)
(b)
(c)
(d)
(e)
(f)
(g)
(h)At the Langøy locality, albitite extends over a 3 × 2 km area and follows a mapped vein-pattern through gabbro, metagabbro, and scapolite metagabbro rocks (Figure1(b)). It includes massive carbonate-rich albitite, brecciated and altered host rock with albite-carbonate groundmass, and foliated albitic felsites. The massive carbonate-rich albitite usually occurs as several-meter thick deposits (Figure 3(d)) with the largest albitite body being more than 150 m wide and 1500 m long (Figure 1(b)). They are brecciated along their margins (Figure 3(e)) to the scapolite metagabbro with a gradational contact. The initial transformation and disintegration of the metagabbro protolith are observed along and adjacent to the individual albititic veins (Figure 3(f)). Progressive deformation and infiltration caused brecciation, with an albititic groundmass infiltrating angular clasts of greenish-grey, retrograded mafic rock, and progressively developing a foliation fabric. These foliated albite-rich felsites are rocks with layers of light carbonate-albite dominated bands layered with green-grey chlorite schist, after veined, brecciated, and flattened metagabbro (Figure 3(g)).In the Storkollen-Åtangen area, west of the town of Kragerø, large-scale albititic bodies covering >1 km2 are enveloped by amphibolites, metagabbro, and scapolite metagabbro. The albitite is clinopyroxene- and titanite-bearing. It characteristically takes the form of a medium-grained, granoblastic, light grey, or pink leucocratic rock (Figure 3(h)). It is either massive or has a gneissic banding formed by alternating leucocratic and amphibole-bearing melanocratic layers. The clinopyroxene-bearing albitite and its melanocratic layers show replacement to rutile-bearing, light pink, fine-grained albitite. The contact to the enveloping amphibolite unit is associated with a greenish-grey transformation of mafic phases. Analysed amphiboles show edenitic, pargasitic, and actinolitic compositions. In addition, Dahlgren et al. [32] report dolomite-dominated deposits in this area with veining and brecciation of the metagabbro and amphibolites.


### 4.2. Petrography and Mineral Chemistry

Petrography and mineral chemistry of the metasomatic rocks have been described in detail by Engvik et al.: albitisation of granitoid [35], scapolite metagabbro and vein-related albitisation of mafic rock [20, 29], albite-carbonate-rich deposits and albitic felsites [23], and scapolite metagabbro, clinopyroxene-bearing albitite, and rutile-albitite [50].


#### 4.2.1. Scapolite Metagabbro

The scapolite metagabbro is dominated by a Cl-rich marialitic scapolite (Me19–42) and edenitic, pargasitic, and actinolitic amphibole (Mg# = 0.79–0.87; Cl < 0.24 a.p.f.u.), and it locally contains a high phlogopite content (Mg# < 0.95) (Figures 4(a)-4(b)). The Ti-bearing phase is normally rutile. At Ødegården Verk, the scapolite metagabbro shows in addition a high chlorapatite and enstatite (En95-96Fs3-4, Mg# = 0.94–0.95) content. Sapphirine is formed during replacement of the former plagioclase by scapolite [34].Figure 4
Photomicrographs of representative petrography from metasomatised rocks (mineral abbreviations after Whitney and Evans [36]). (a) Scapolite metagabbro dominated by scapolite and amphibole with accessory rutile. Locality Ødegården Verk, sample 2Ø91.45. (b) Phlogopite-bearing scapolite metagabbro. Locality Langøy, sample AE46. (c) Rutile-bearing albitite from veining in an amphibolite. Locality Ringsjø, sample AE10A. (d) Calcite-rich albitite (albitite vein deposit) with rutile. Locality Langøy, sample AE93. (e) Banded albitite felsites with the foliation outlined by chlorite. Locality Langøy, sample AE87. (f) Clinopyroxene-bearing albitite with quartz and titanite. Locality Storkollen, sample AE96.
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(f)Scapolite from the Kragerø area is Cl-rich, that is, 0.80–0.97 a.p.f.u. (marialite), although Cl values down to 0.69 a.p.f.u. have been measured. It is low in S (S < 0.07 a.p.f.u.), combined with the measured Cl-level, indicating a C-content varying up to 0.4 a.p.f.u. [20, 50]. Scapolite in metagabbros is replaced by albite and analcime during albitisation, releasing CO2 and precipitating calcite (see Engvik et al. [50], Figures 4(a)–4(d)).


#### 4.2.2. Rutile-Bearing Albitite

Rutile-bearing albitite forms as vein replacement in mafic (including scapolite-bearing rocks) and granitoid protoliths, and pervasive albitisation results in large-scale albitite bodies (Figure1(b)). Albitite is composed of nearly pure albite (Ab98-99) with accessory rutile, formed from a mafic protolith, and occurs in extreme transformed localities (Figure 4(c)). In the protolith-albitite transition zones, remnants after mafic phases are present in variable amounts. Partly transformed amphibole remnants (edenite-pargasite-actinolite; Mg# = 0.81–0.88), chlorite (Mg# = 0.82–0.87), calcite, and minor prehnite and pumpellyite are observed locally. Albitite, formed from a granitoid protolith, is dominated by albite (Ab99), quartz, with rutile as the accessory Ti-phase, and minor chlorite (Mg# = 0.82), epidote, and calcite locally.


#### 4.2.3. Carbonate-Rich Albitite and Albitite Felsite

The carbonate-rich albitite consists of fine to medium grains of near end-member albite (Ab97–100), calcite, and dolomite (Figure 4(d)). Minor quartz and chlorite are present with rutile and Fe-oxides as accessories. The albitite host clasts consist of mafic, greenish-grey, fine-grained, and retrograded metagabbro, partly replaced by albitite and characterised by a higher content of chlorite and Fe-oxide. In the related, banded, albite-rich felsitic schist, the light bands are composed of fine-grained albite, calcite, chlorite (Mg# = 0.85–0.89), and amphibole. The darker bands also contain clinopyroxene and some phlogopite (Mg# = 0.82), with rutile, apatite, zircon, and magnetite as accessory phases. In addition to the banding, reflected by modal variation, a parallel fabric is defined by planar-oriented phlogopite and chlorite (Figure 4(e)).


#### 4.2.4. Clinopyroxene-Bearing Albitite

The clinopyroxene-bearing albitite is a leucocratic granoblastic, fine- to medium-grained rock, dominated by albite (Ab94–96) and quartz, with minor amounts of clinopyroxene (En30–36Fs12–23; Na = 0.12–0.15 a.p.f.u.; Mg# = 0.57–0.75); (Figure 4(f)). Amphibole (actinolite or magnesiohornblende; Mg# = 0.67–0.79) occurs locally related to, and partly replacing, clinopyroxene in melanocratic layers. The albitite is relatively rich in titanite and has in addition apatite and zircon as accessory minerals. Its replacement to rutile-bearing albitite is petrographically evident by formation of a porous albite chessboard (Ab98–100An0–2), by replacement of clinopyroxene by chlorite (Mg# < 0.80) and calcite, and by replacement of titanite by aggregates of rutile + calcite + quartz.


### 4.3. Whole Rock Geochemistry

Whole rock geochemical data from the gabbro/metagabbro and tonalite protolith, together with the metasomatic scapolite-bearing metagabbro and albitites, are presented in Table2 and Figure 5. While scapolite metagabbro has a gabbro protolith, the albitites are derived from a variety of rocks including a gabbro or scapolite metagabbro protolith for the samples with SiO2 < 70, whereas for albitites with SiO2 > 70 a granitoid or unknown protolith is inferred (Table 2). For the major elements, systematic geochemical changes are seen for the elements Na, Ca, Fe, and Mg in the metasomatic rocks compared to the protoliths. For scapolite metagabbro and albitite derived from gabbro, Na2O increases and CaO decreases with increasing SiO2 (Figures 5(a) and 5(b)). For a specific content of SiO2, the Na2O is higher for the scapolite metagabbro than for the albite, which reflects that the Na : Si ratio in marialite is 2 : 1, while the same ratio for albite is 1 : 1. We regard the two trends, defined by increasing Na2O with increasing SiO2 for scapolite metagabbro and albitites with SiO2 < 70, to represent increasing degree of scapolitisation and albitisation. Fe2O3 (Figure 5(c)) is generally lower in the scapolite metagabbro compared to the gabbro/metagabbro and shows especially low values in the albitites. MgO (Figure 5(d)) decreases with increasing SiO2 for both albitite and scapolite metagabbros. An increase of P2O5 with increasing degree of scapolitisation (increasing SiO2) is apparent for the scapolite metagabbros, while for albitites the P2O5 decreases with albitisation (Figure 5(e)). The concentration of the trace elements Zn and Cu (Figures 5(f) and 5(g)) decreases with increasing degree of scapolitisation and both elements are below 15 ppm for all albitites, while one of the gabbro samples contains around 90 ppm for both Zn and Cu (Table 2). Bromine which is absent in the protolith rocks increases with increasing degree of scapolitisation up to a level of 80 ppm, while this element is below the detection limit in the albitites (Figure 5(h)). No analyses of Cl are available, but we assume, based on the mineralogical evolution and mineral chemistry, that Cl must parallel the evolution of Br at a much higher level. Like P2O5, TiO2 increases with increasing degree of scapolitisation (Figure 5(i)). Albitites with low SiO2 values contain the highest TiO2 content (ca 4 wt%), while increasing the degree of albitisation apparently results in decreasing the TiO2 content. Vanadium, an element that typically follows Ti, displays a clear increase with degree of scapolitisation and a reduction during progressive albitisation (Figure 5(j)). For most of the metasomatised samples analysed, there is a negative correlation between TiO2 and Fe2O3, while for the gabbro an overall positive correlation between these two oxides exists (Figure 5(k)). TiO2 values up to 4.31 wt% are found in some of the scapolite metagabbros and albitites.Figure 5
Plots of whole rock geochemical data: (a) Na2O-SiO2; (b) CaO-SiO2; (c) Fe2O3-SiO2; (d) MgO-SiO2; (e) P2O5-SiO2; (f) Zn-SiO2; (g) Cu-SiO2; (h) Br-SiO2; (i) TiO2-SiO2; (j) V-SiO2; (k) TiO2-Fe2O3; and (l) V-TiO2.
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## 4.1. Field and Structural Relations

In the Kragerø area, Mg-Cl-metasomatised scapolite-bearing rocks occur widespread as a part of the mapped amphibolite, metagabbro, and gabbro lithologies [19, 20, 23] and have been studied in detail at Ødegården Verk, Ringsjø, Åtangen, Valberg, and Langøy localities (Figure 1(b)). At Langøy and Ødegården Verk, transformation of pristine gabbro to scapolite metagabbro is observed along fluid fronts (Figure 2(a)). Medium-grained dark gabbro including olivine and pyroxenes is transformed into a medium- to coarse-grained scapolite metagabbro. The scapolite metagabbro occurs as an equigranular massive rock originally named ødegårdite [57]. Frequently, the scapolite metagabbro displays veining in the form of 0.5–2 cm wide veins, which are composed of the major rock-forming minerals scapolite, amphibole (edenite, pargasite, and actinolite), or phlogopite (Figures 2(b)–2(d)). Locally, this veining occurs with a high density initiating a layered structure in the rock (Figure 2(c)). The veining and banded structure develops during progressive deformation and formation of the rock foliation (Figure 2(d)). At the Åtangen locality, dynamic scapolitisation through synchronous brecciation is observed, where amphibolite and banded host schist are found as inclusions in a matrix of scapolite (Figures 2(e)–2(g)). White scapolite forms veins, or a scapolite-amphibole assemblage forms the groundmass in evolved breccias with rounded clasts. The veined and brecciated structure undergoes flattening (Figure 2(g)), evolving to a foliated scapolite-bearing amphibolitic rock (Figure 2(h)).Figure 2
Field photos of scapolite metagabbro and dynamic scapolitisation. (a) Gabbro with scapolitisation front. Locality Langøy. (b) Scapolite metagabbro with veining filled by scapolite and amphibole. Field of view is approximately one metre wide. Locality Langøy. (c) Scapolite metagabbro with a high density of scapolite veining resulting in a layered structure in the rock [20]. Field of view is approximately one metre wide. Locality Langøy. (d) Scapolite metagabbro with amphibole veining and flattened foliation [20]. Locality Langøy. (e) Brecciated amphibolite with a thin scapolite vein filling and rounded clasts. Locality Åtangen. (f) Intensive scapolitisation of an evolved breccia with amphibole veins, amphibole + scapolite matrix, and rounded clasts. Locality Åtangen. (g) Brecciated amphibolite with scapolite veins undergoing flattening. Locality Åtangen. (h) Foliated scapolite-bearing amphibolites. Locality Åtangen.
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(h)Albitisation affects both mafic and granitoid lithologies in the Kragerø area, usually associated with the scapolite-bearing rocks, and normally postdating the scapolitisation. Albitisation takes place along veins and in breccias. Albite is the dominant mineral in foliated felsites, in chlorite schist, in carbonate-rich albitite, and in large-scale albitite bodies [23, 50]. Albitisation has been studied in detail in the Ringsjø-Ødegården Verk area [20, 35]. Both mafic (gabbro, scapolite metagabbro, and amphibolite) and granitoid protolith are transformed to albitite along veining, where the central vein consists of nearly pure albite (Figures 3(a)-3(b)). The replacement zone to the mafic host rock shows a widespread replacement of the mafic phases to chlorite (Figure 3(c)). Intensive albitisation affects part of the area resulting in a 0.5×2 km albitite body (Figure 1(b)).Figure 3
Field photos of albitites and dynamic albitisation. (a) Albitisation vein in metagabbro transforming the dark mafic rock to nearly pure albite. Locality Ringsjø. (b) Albitisation (red color) of tonalite (light color) along veining. Locality Fesettjern, Ringsjø area. (c) Vein albitisation (red color) causing chloritisation (greenish color) of scapolite metagabbro (dark grey). Locality Ringsjø. (d) Carbonate-rich albitite forming an approximate 5-metre wide vein deposit in the metagabbro. Locality Langøy. (e) Breccia containing clasts of albitised metagabbro in the matrix of a carbonate-rich albitite deposit. Field of view is approximately four metres wide. Locality Langøy. (f) Albitisation of metagabbro along veining with transformation to foliated albitic felsites. Locality Langøy. (g) Foliated albititic felsites with alternating light carbonate-albite and green-grey chlorite-schist bands. Locality Langøy. (h) Banded clinopyroxene-bearing albitite. Locality Åtangen.
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(h)At the Langøy locality, albitite extends over a 3 × 2 km area and follows a mapped vein-pattern through gabbro, metagabbro, and scapolite metagabbro rocks (Figure1(b)). It includes massive carbonate-rich albitite, brecciated and altered host rock with albite-carbonate groundmass, and foliated albitic felsites. The massive carbonate-rich albitite usually occurs as several-meter thick deposits (Figure 3(d)) with the largest albitite body being more than 150 m wide and 1500 m long (Figure 1(b)). They are brecciated along their margins (Figure 3(e)) to the scapolite metagabbro with a gradational contact. The initial transformation and disintegration of the metagabbro protolith are observed along and adjacent to the individual albititic veins (Figure 3(f)). Progressive deformation and infiltration caused brecciation, with an albititic groundmass infiltrating angular clasts of greenish-grey, retrograded mafic rock, and progressively developing a foliation fabric. These foliated albite-rich felsites are rocks with layers of light carbonate-albite dominated bands layered with green-grey chlorite schist, after veined, brecciated, and flattened metagabbro (Figure 3(g)).In the Storkollen-Åtangen area, west of the town of Kragerø, large-scale albititic bodies covering >1 km2 are enveloped by amphibolites, metagabbro, and scapolite metagabbro. The albitite is clinopyroxene- and titanite-bearing. It characteristically takes the form of a medium-grained, granoblastic, light grey, or pink leucocratic rock (Figure 3(h)). It is either massive or has a gneissic banding formed by alternating leucocratic and amphibole-bearing melanocratic layers. The clinopyroxene-bearing albitite and its melanocratic layers show replacement to rutile-bearing, light pink, fine-grained albitite. The contact to the enveloping amphibolite unit is associated with a greenish-grey transformation of mafic phases. Analysed amphiboles show edenitic, pargasitic, and actinolitic compositions. In addition, Dahlgren et al. [32] report dolomite-dominated deposits in this area with veining and brecciation of the metagabbro and amphibolites.


## 4.2. Petrography and Mineral Chemistry

Petrography and mineral chemistry of the metasomatic rocks have been described in detail by Engvik et al.: albitisation of granitoid [35], scapolite metagabbro and vein-related albitisation of mafic rock [20, 29], albite-carbonate-rich deposits and albitic felsites [23], and scapolite metagabbro, clinopyroxene-bearing albitite, and rutile-albitite [50].


### 4.2.1. Scapolite Metagabbro

The scapolite metagabbro is dominated by a Cl-rich marialitic scapolite (Me19–42) and edenitic, pargasitic, and actinolitic amphibole (Mg# = 0.79–0.87; Cl < 0.24 a.p.f.u.), and it locally contains a high phlogopite content (Mg# < 0.95) (Figures 4(a)-4(b)). The Ti-bearing phase is normally rutile. At Ødegården Verk, the scapolite metagabbro shows in addition a high chlorapatite and enstatite (En95-96Fs3-4, Mg# = 0.94–0.95) content. Sapphirine is formed during replacement of the former plagioclase by scapolite [34].Figure 4
Photomicrographs of representative petrography from metasomatised rocks (mineral abbreviations after Whitney and Evans [36]). (a) Scapolite metagabbro dominated by scapolite and amphibole with accessory rutile. Locality Ødegården Verk, sample 2Ø91.45. (b) Phlogopite-bearing scapolite metagabbro. Locality Langøy, sample AE46. (c) Rutile-bearing albitite from veining in an amphibolite. Locality Ringsjø, sample AE10A. (d) Calcite-rich albitite (albitite vein deposit) with rutile. Locality Langøy, sample AE93. (e) Banded albitite felsites with the foliation outlined by chlorite. Locality Langøy, sample AE87. (f) Clinopyroxene-bearing albitite with quartz and titanite. Locality Storkollen, sample AE96.
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(f)Scapolite from the Kragerø area is Cl-rich, that is, 0.80–0.97 a.p.f.u. (marialite), although Cl values down to 0.69 a.p.f.u. have been measured. It is low in S (S < 0.07 a.p.f.u.), combined with the measured Cl-level, indicating a C-content varying up to 0.4 a.p.f.u. [20, 50]. Scapolite in metagabbros is replaced by albite and analcime during albitisation, releasing CO2 and precipitating calcite (see Engvik et al. [50], Figures 4(a)–4(d)).


### 4.2.2. Rutile-Bearing Albitite

Rutile-bearing albitite forms as vein replacement in mafic (including scapolite-bearing rocks) and granitoid protoliths, and pervasive albitisation results in large-scale albitite bodies (Figure1(b)). Albitite is composed of nearly pure albite (Ab98-99) with accessory rutile, formed from a mafic protolith, and occurs in extreme transformed localities (Figure 4(c)). In the protolith-albitite transition zones, remnants after mafic phases are present in variable amounts. Partly transformed amphibole remnants (edenite-pargasite-actinolite; Mg# = 0.81–0.88), chlorite (Mg# = 0.82–0.87), calcite, and minor prehnite and pumpellyite are observed locally. Albitite, formed from a granitoid protolith, is dominated by albite (Ab99), quartz, with rutile as the accessory Ti-phase, and minor chlorite (Mg# = 0.82), epidote, and calcite locally.


### 4.2.3. Carbonate-Rich Albitite and Albitite Felsite

The carbonate-rich albitite consists of fine to medium grains of near end-member albite (Ab97–100), calcite, and dolomite (Figure 4(d)). Minor quartz and chlorite are present with rutile and Fe-oxides as accessories. The albitite host clasts consist of mafic, greenish-grey, fine-grained, and retrograded metagabbro, partly replaced by albitite and characterised by a higher content of chlorite and Fe-oxide. In the related, banded, albite-rich felsitic schist, the light bands are composed of fine-grained albite, calcite, chlorite (Mg# = 0.85–0.89), and amphibole. The darker bands also contain clinopyroxene and some phlogopite (Mg# = 0.82), with rutile, apatite, zircon, and magnetite as accessory phases. In addition to the banding, reflected by modal variation, a parallel fabric is defined by planar-oriented phlogopite and chlorite (Figure 4(e)).


### 4.2.4. Clinopyroxene-Bearing Albitite

The clinopyroxene-bearing albitite is a leucocratic granoblastic, fine- to medium-grained rock, dominated by albite (Ab94–96) and quartz, with minor amounts of clinopyroxene (En30–36Fs12–23; Na = 0.12–0.15 a.p.f.u.; Mg# = 0.57–0.75); (Figure 4(f)). Amphibole (actinolite or magnesiohornblende; Mg# = 0.67–0.79) occurs locally related to, and partly replacing, clinopyroxene in melanocratic layers. The albitite is relatively rich in titanite and has in addition apatite and zircon as accessory minerals. Its replacement to rutile-bearing albitite is petrographically evident by formation of a porous albite chessboard (Ab98–100An0–2), by replacement of clinopyroxene by chlorite (Mg# < 0.80) and calcite, and by replacement of titanite by aggregates of rutile + calcite + quartz.


## 4.2.1. Scapolite Metagabbro

The scapolite metagabbro is dominated by a Cl-rich marialitic scapolite (Me19–42) and edenitic, pargasitic, and actinolitic amphibole (Mg# = 0.79–0.87; Cl < 0.24 a.p.f.u.), and it locally contains a high phlogopite content (Mg# < 0.95) (Figures 4(a)-4(b)). The Ti-bearing phase is normally rutile. At Ødegården Verk, the scapolite metagabbro shows in addition a high chlorapatite and enstatite (En95-96Fs3-4, Mg# = 0.94–0.95) content. Sapphirine is formed during replacement of the former plagioclase by scapolite [34].Figure 4
Photomicrographs of representative petrography from metasomatised rocks (mineral abbreviations after Whitney and Evans [36]). (a) Scapolite metagabbro dominated by scapolite and amphibole with accessory rutile. Locality Ødegården Verk, sample 2Ø91.45. (b) Phlogopite-bearing scapolite metagabbro. Locality Langøy, sample AE46. (c) Rutile-bearing albitite from veining in an amphibolite. Locality Ringsjø, sample AE10A. (d) Calcite-rich albitite (albitite vein deposit) with rutile. Locality Langøy, sample AE93. (e) Banded albitite felsites with the foliation outlined by chlorite. Locality Langøy, sample AE87. (f) Clinopyroxene-bearing albitite with quartz and titanite. Locality Storkollen, sample AE96.
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(f)Scapolite from the Kragerø area is Cl-rich, that is, 0.80–0.97 a.p.f.u. (marialite), although Cl values down to 0.69 a.p.f.u. have been measured. It is low in S (S < 0.07 a.p.f.u.), combined with the measured Cl-level, indicating a C-content varying up to 0.4 a.p.f.u. [20, 50]. Scapolite in metagabbros is replaced by albite and analcime during albitisation, releasing CO2 and precipitating calcite (see Engvik et al. [50], Figures 4(a)–4(d)).


## 4.2.2. Rutile-Bearing Albitite

Rutile-bearing albitite forms as vein replacement in mafic (including scapolite-bearing rocks) and granitoid protoliths, and pervasive albitisation results in large-scale albitite bodies (Figure1(b)). Albitite is composed of nearly pure albite (Ab98-99) with accessory rutile, formed from a mafic protolith, and occurs in extreme transformed localities (Figure 4(c)). In the protolith-albitite transition zones, remnants after mafic phases are present in variable amounts. Partly transformed amphibole remnants (edenite-pargasite-actinolite; Mg# = 0.81–0.88), chlorite (Mg# = 0.82–0.87), calcite, and minor prehnite and pumpellyite are observed locally. Albitite, formed from a granitoid protolith, is dominated by albite (Ab99), quartz, with rutile as the accessory Ti-phase, and minor chlorite (Mg# = 0.82), epidote, and calcite locally.


## 4.2.3. Carbonate-Rich Albitite and Albitite Felsite

The carbonate-rich albitite consists of fine to medium grains of near end-member albite (Ab97–100), calcite, and dolomite (Figure 4(d)). Minor quartz and chlorite are present with rutile and Fe-oxides as accessories. The albitite host clasts consist of mafic, greenish-grey, fine-grained, and retrograded metagabbro, partly replaced by albitite and characterised by a higher content of chlorite and Fe-oxide. In the related, banded, albite-rich felsitic schist, the light bands are composed of fine-grained albite, calcite, chlorite (Mg# = 0.85–0.89), and amphibole. The darker bands also contain clinopyroxene and some phlogopite (Mg# = 0.82), with rutile, apatite, zircon, and magnetite as accessory phases. In addition to the banding, reflected by modal variation, a parallel fabric is defined by planar-oriented phlogopite and chlorite (Figure 4(e)).


## 4.2.4. Clinopyroxene-Bearing Albitite

The clinopyroxene-bearing albitite is a leucocratic granoblastic, fine- to medium-grained rock, dominated by albite (Ab94–96) and quartz, with minor amounts of clinopyroxene (En30–36Fs12–23; Na = 0.12–0.15 a.p.f.u.; Mg# = 0.57–0.75); (Figure 4(f)). Amphibole (actinolite or magnesiohornblende; Mg# = 0.67–0.79) occurs locally related to, and partly replacing, clinopyroxene in melanocratic layers. The albitite is relatively rich in titanite and has in addition apatite and zircon as accessory minerals. Its replacement to rutile-bearing albitite is petrographically evident by formation of a porous albite chessboard (Ab98–100An0–2), by replacement of clinopyroxene by chlorite (Mg# < 0.80) and calcite, and by replacement of titanite by aggregates of rutile + calcite + quartz.


## 4.3. Whole Rock Geochemistry

Whole rock geochemical data from the gabbro/metagabbro and tonalite protolith, together with the metasomatic scapolite-bearing metagabbro and albitites, are presented in Table2 and Figure 5. While scapolite metagabbro has a gabbro protolith, the albitites are derived from a variety of rocks including a gabbro or scapolite metagabbro protolith for the samples with SiO2 < 70, whereas for albitites with SiO2 > 70 a granitoid or unknown protolith is inferred (Table 2). For the major elements, systematic geochemical changes are seen for the elements Na, Ca, Fe, and Mg in the metasomatic rocks compared to the protoliths. For scapolite metagabbro and albitite derived from gabbro, Na2O increases and CaO decreases with increasing SiO2 (Figures 5(a) and 5(b)). For a specific content of SiO2, the Na2O is higher for the scapolite metagabbro than for the albite, which reflects that the Na : Si ratio in marialite is 2 : 1, while the same ratio for albite is 1 : 1. We regard the two trends, defined by increasing Na2O with increasing SiO2 for scapolite metagabbro and albitites with SiO2 < 70, to represent increasing degree of scapolitisation and albitisation. Fe2O3 (Figure 5(c)) is generally lower in the scapolite metagabbro compared to the gabbro/metagabbro and shows especially low values in the albitites. MgO (Figure 5(d)) decreases with increasing SiO2 for both albitite and scapolite metagabbros. An increase of P2O5 with increasing degree of scapolitisation (increasing SiO2) is apparent for the scapolite metagabbros, while for albitites the P2O5 decreases with albitisation (Figure 5(e)). The concentration of the trace elements Zn and Cu (Figures 5(f) and 5(g)) decreases with increasing degree of scapolitisation and both elements are below 15 ppm for all albitites, while one of the gabbro samples contains around 90 ppm for both Zn and Cu (Table 2). Bromine which is absent in the protolith rocks increases with increasing degree of scapolitisation up to a level of 80 ppm, while this element is below the detection limit in the albitites (Figure 5(h)). No analyses of Cl are available, but we assume, based on the mineralogical evolution and mineral chemistry, that Cl must parallel the evolution of Br at a much higher level. Like P2O5, TiO2 increases with increasing degree of scapolitisation (Figure 5(i)). Albitites with low SiO2 values contain the highest TiO2 content (ca 4 wt%), while increasing the degree of albitisation apparently results in decreasing the TiO2 content. Vanadium, an element that typically follows Ti, displays a clear increase with degree of scapolitisation and a reduction during progressive albitisation (Figure 5(j)). For most of the metasomatised samples analysed, there is a negative correlation between TiO2 and Fe2O3, while for the gabbro an overall positive correlation between these two oxides exists (Figure 5(k)). TiO2 values up to 4.31 wt% are found in some of the scapolite metagabbros and albitites.Figure 5
Plots of whole rock geochemical data: (a) Na2O-SiO2; (b) CaO-SiO2; (c) Fe2O3-SiO2; (d) MgO-SiO2; (e) P2O5-SiO2; (f) Zn-SiO2; (g) Cu-SiO2; (h) Br-SiO2; (i) TiO2-SiO2; (j) V-SiO2; (k) TiO2-Fe2O3; and (l) V-TiO2.
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## 5. Stable Isotopic Compositions

Mineral separates from the scapolite metagabbro and albitites have been analysed for the stable isotopes of O (δ18O), H (δD), and C (δ13C; Table 3). Albite separates from different types of albitites, quartz separates from clinopyroxene-bearing albitites, calcite separates from carbonate-rich albitite, and scapolite separates from scapolite metagabbros have been analysed with respect to δ18O. The albite, calcite, and scapolite are presumed to have formed during metasomatism, while the quartz equilibrated with these minerals during the same event. The stable isotopic composition of these minerals should give constraints on the infiltrating fluid chemistry, but O in the silicate crystal structure should also retain information regarding the origin of the rock.In addition, theδD composition of amphibole separates from the scapolite metagabbro is presented. The amphibole crystallized during the metasomatic alteration of the dry gabbro by the infiltration of an external fluid [20]. Consequently, the δD-values give direct information on the chemistry of the metasomatising fluid. Carbon, in the form of CO2, was also supplied externally during the metasomatic event resulting in the formation of calcite, which was analysed for δ13C.Albite mineral separates from the Ringsjø-Ødegården Verk area giveδ18OSMOW values of 5.1 to 8.4‰ for samples of albitite originating from a mafic/gabbro protolith and 8.5 to 10.8‰ for samples originating from a granitoid/tonalite. Albite, from carbonate-bearing albitite samples from Langøy, gives a δ18OSMOW of 5.5 to 7.0‰. Albite from a clinopyroxene-bearing albitite in the Åtangen-Storkollen area yields a δ18OSMOW of 10.8 to 11.1‰, while quartz from the same samples gives a δ18OSMOW of 11.5 to 11.6‰. Scapolite separates from a scapolite metagabbro sampled at the Ødegården Verk and Ringsjø localities give δ18OSMOW values in the range of 7.4 to 10.6‰. Calcite from different albitites shows a wide range in δ18OSMOW between 3.4 and 12.4‰, but with a quite consistent δ13C of −4.6 to -6.0‰ (Figure 6). Amphibole separates from the same scapolite metagabbro samples yield δ18OSMOW from 4.3 to 6.7‰ and δDSMOW of −84 to -50‰.Figure 6
(a) Back-scattered electron (BSE) image of replacement of ilmenite by rutile in a scapolite metagabbro. Square indicates image in Figure6(b). Sample 2Ø88.80, locality Ødegården Verk (photo: A. Korneliussen). (b) Detail of incomplete alteration of ilmenite (white) to rutile (light grey) and titanite (grey) (photo: A. Korneliussen). (c) BSE image of Cl and hydroxyapatite in scapolite metagabbro. Sample 2Ø78.20, locality Ødegården Verk.
(a)
(b)
(c)


## 6. Discussion

### 6.1. Metasomatism and Mineralisation

Metasomatism is extensive in south Norway [18, 23]. Earlier work in the Bamble lithotectonic domain has shown that scapolitisation transforms mafic rocks into scapolite metagabbros by infiltration of Cl-Mg-rich solutions and that albitites form from both mafic and granitoid protoliths by Na-rich solutions [20, 35]. As expected, Na2O increases and CaO decreases during albitisation. Addition of albite to a gabbroic protolith will dilute the nonadded elements in equal proportion. Although the overall trend displayed by Figure 5 can be explained by addition of albite and scapolite to a gabbroic protolith, the TiO2-Fe2O3 relationship shown in Figure 5(k) strongly indicates that addition of albite and scapolite alone cannot explain the chemical evolution displayed and that other elements must have been mobile. The strong reduction in Fe2O3 suggests that this oxide is removed during albititisation and to some extent during scapolitisation. The measured variation in Br and Cl which is assumed to parallel Br suggests that these elements are added during the scapolitisation but were removed from the rock during albitisation. The mineralogical evolution, where Cl-scapolite formed during scapolitisation and later broke down during albitisation, suggests that halogens will be present in the fluid also during albitisation and are available for complexing with metals (e.g., Fe, Cu, and Zn). We suggest that such a complexing can explain the many ore deposits in the area and in particular the Langøy Fe-mines.The Bamble lithotectonic domain is characterised not only by widespread metasomatic alteration, but also by a high density of mineral deposits (Geological Survey of Norway Ore Database [24–26]). The high density of apatite and rutile deposits follows the regional distribution of metasomatic alteration in the Bamble lithotectonic domain [23]. While ilmenite is the main Ti-bearing mineral in the gabbro protolith, Ti occurs as rutile (Figures 6(a)-6(b)) and in amphibole (<0.34 a.p.f.u.) and biotite (<0.69 a.p.f.u.) within the scapolite metagabbro [20]. Replacement of ilmenite by rutile is illustrated in Figures 6(a)-6(b). During albititisation, biotite and amphibole break down and Ti is released as titanite [20, 31]. The whole rock geochemical data (Figures 5(i) and 5(j)) illustrates that TiO2 and V increased during scapolitisation and decreased during albitisation. The high values of TiO2 in some of the albitites are probably inherited from the scapolite enrichment. Fe2O3 decreases during scapolitisation and albitisation and the TiO2-Fe2O3 relationships (Figure 5(k)) cannot be the result of pure dilution by adding albite and scapolite but suggest that Fe is removed.The whole rock geochemistry in Figure5(e) illustrates the P, which is increased during scapolitisation and that the P resources at Ødegården Verk owe their existence to this event rather than the albitisation event which leads to a reduction of P. This is in accordance with earlier works which show that scapolite metagabbros commonly have both a high apatite content in the Bamble lithotectonic domain and host vein-related apatite deposits (Figure 6(c)) [19, 28, 29]. Scapolitisation and albitisation are documented as having formed chlorapatite and hydroxyfluorapatite at Ødegården Verk in Bamble (Figure 6(c)) [19, 28, 29].As discussed above, metasomatism of the gabbro causes extensive Fe-depletion (Figure5(c)) [20]. In addition, the whole rock geochemistry shows that the concentration of Cu and Zn is lowered during the scapolitisation of the gabbro/metagabbro (Figures 5(f)-5(g)) and is nearly completely depleted during albitisation of the same protolith. The fluid mobilization of these elements could have caused the widespread occurrences of metal deposits in the Bamble lithotectonic domain [23]. Fe-oxide ores are present as hematite-carbonate veins in the rutile-rich albitites in the Kragerø area and are widespread in the Bamble lithotectonic domain [23, 58], as hematite-rich albitites, orthoamphibole-hematite veins, and albite-magnetite veins. Cu-Zn-bearing base metal deposits are frequent in the Kragerø-Bamble area (Geological Survey of Norway Ore Database). The association of Fe-ores with albitites and altered granites has been reported worldwide, for example, as in magnetite-apatite deposits from the Lyon Mountain area, Adirondacks, New York, USA [67].


### 6.2. Stable Isotopic Results: Fluid and Rock Origin

The stable isotopic composition of silicate mineral separates can reflect the origin of both the rocks and the infiltrating fluid [68, 69]. It will retain information from the protolith phases, but, depending on the degree of alteration and replacement, the isotopic composition will undergo a shift during fluid infiltration. Oxygen is already present in significant concentrations in the silicate minerals. To shift the δ18O composition in a silicate mineral will require large amounts of infiltrating fluids. This must be the case for the albitite rocks in the Bamble lithotectonic domain, which have undergone complete alteration to a new mineralogy, involving large chemical changes [20, 23, 50].Aδ18OSMOW composition of 5.1 to 8.4‰ is seen for the albite separates from albitite formed from a gabbroic protolith (Table 3). Results for albite from a carbonate-rich albitite deposited in metagabbro at Langøy fall in the same range. A δ18OSMOW composition of 8.5 to 10.8‰ is obtained for albite, which originated from a granitoid protolith in the Ringsjø-Ødegården Verk area. From a clinopyroxene-bearing albitite in the Åtangen-Storkollen area, the albite gives a δ18OSMOW composition of 10.8 to 11.1‰ and the quartz 11.5 to 11.6‰. The results from measured albitites from both mafic and tonalitic magmatic precursors are in accordance with the original values from such protoliths [70] coupled with the influence of a fluid with both a magmatic and seawater origin [69]. Depending on the temperature, the reported O-isotopic signature could originate from a magmatic fluid, although a magmatic fluid would normally give a higher value. Seawater could explain the reported values since it could lower the isotopic ratio relative to the magmatic protolith values. As metasomatic fluid infiltration is often spatially inhomogeneous, this could possibly also explain variations in the resulting values. A meteoric water source can clearly be ruled out, as meteoric water would have led to a significantly lower δ18OSMOW composition of about +2 to -10‰. Mark and Foster [71] document a similar δ18OSMOW composition associated with albitisation in the Cloncurry district, Australia, and concluded that it is due to magmatic processes.Amphiboles in scapolite metagabbros were produced during fluid infiltration into the dry protolith gabbro [20, 29]. This implies that the H-isotopic content of the amphiboles, in contrast to the O-isotopes, will give more accurate information regarding the metasomatic fluid. The δD-composition of the amphibole from the scapolite metagabbro generally varies between −50 and -59‰ and is in accordance with an igneous precursor [70] infiltrated by magmatic or metamorphic H2O [69, 72]. A hydrothermal saline solution would not affect the δD-composition, as it will give similar δD-values compared to magmatic and metamorphic fluids. Again, a meteoric water origin can be excluded as it would give significantly lower values for the δD composition down to −90 to -140‰. The stable isotopic composition of scapolite-bearing rocks is known from Mary Kathleen, Queensland, Australia [73], where the scapolitisation is interpreted to have been caused by magmatic fluids, and the Greenville Province, Ontario, Canada [74], where scapolitisation was caused by metamorphic fluids originating from a carbonate source.For the carbonate-rich albitite, theδ18OSMOW values show values similar to silicate rocks, indicating a magmatic source for C (Figure 7). This is supported by the δ13CPDB values, which fall between −6.0 and -4.6‰ and give signatures similar to those for carbonatitic magma. Our petrographic investigations show in addition that breakdown of scapolite during albitisation produces carbonate [50]. Dahlgren et al. [32] described vein deposited dolomite marbles giving δ18O = 9.6 to 10.7‰, δ13C = −8.5 to -6.2‰, and high 87Sr/86Sr ratios of 0.706 to 0.709, which overlaps the values reported from these studies (Figure 6) and values from the Bamble hyperites [37] and vein carbonates [40]. Dahlgren et al. [32] suggested that the dolomite marbles were formed from hydrothermal solutions that were channeled into a large degassing zone, which now takes the form of a deformed, regional zone with hydrothermal dolomite deposits, albitites, apatite-veins, and widespread scapolitisation. These authors speculated that the fluids were derived from charnockite intrusions in the region.Figure 7
δ
18
O
S
M
O
W versus δ13CPDB plot: circles indicate data from this study (Table 3) and diamonds indicate data from dolomite marble deposits/veins and a calcite + albite + quartz dike in the Kragerø area by Dahlgren et al. [32]. BG = Bamble hyperites [37]; CBT = world carbonatites [38]; PC = nonmetamorphic proterozoic carbonates [39]; VC = vein carbonate [40].As mentioned above, while metasomatism is able to significantly alter the chemical composition of the precursor rock, this alteration may vary spatially. This also applies to the isotope composition of the rocks. Probably this is due to varying temperatures as well as the different water/rock (w/r) ratios that caused the alteration. The variable oxygen isotope composition in all altered rock types from this study, in combination with relatively homogeneous H- and C-isotope ratios, corroborates this assumption. Varying degrees of alteration, variableT, and variable w/r ratios can produce isotopic signatures that reflect the values that we have measured and are shown in Table 3. In addition, fluid compositions can also have been varied, even on a local scale, and scales of equilibrium might also have been local, regardless of the widespread regional occurrence of the metasomatic rocks.For the sampled localities, Engvik et al. [20] reported a Cl- and B-rich environment, Sr-signatures in the scapolite with an initial 87Sr/86Sr ranging from 0.704 to 0.709, and a regional distribution of lithologies, indicating that the fluid originated from evaporites that were mobilized during regional metamorphism. Our new data on the stable isotopic composition of the albitites and scapolite metagabbro support the interpretation that the original magmatic mafic and granitoid rocks were metasomatised by fluids reflecting a seawater origin or with a possible magmatic component. Depending on T, w/r, and the degree of alteration, both fluid types (seawater and magmatic) may lead to the same approximate pattern. What can be ruled out from the H and O stable isotope data is meteoric water as it would have led to significantly lower δ18OSMOW and δDSMOW values and also to different δ13CPDB values.Other stable isotopic constraints in the Kragerø area of the Bamble lithotectonic domain support a mixture of magmatic and metamorphic fluid signatures coupled with seawater as being responsible for the metasomatism. Bast et al. [33] analysed B isotope compositions in tourmaline in order to constrain the possible sources of and the evolution of hydrothermal fluids. δ11B values were found to range from −5 to +27‰ (relative to SRM-951), which suggests marine evaporites interlayered with continental detritus and pelagic clay as a possible B source reservoir. Negative δ11B values were explained by the influence of pneumatolytic fluids associated with granitic pegmatites. Variations in δ11B on a regional km-scale, with small local variations, were explained by fluid infiltration during several generations of pulses.Measurements ofδ37Cl, together with F, Cl, Br, and I concentrations, were used to trace the metasomatic evolution of gabbroic bodies and to understand the interplay between localized and pervasive fluid flow [27, 30]. The reported Br/Cl and I/Cl ratios (3 × 10−3 and 25 × 10−6) overlap with the range of ratios measured for marine pore fluids. The unaltered gabbro has δ37Cl values near 0% and a similar value is inferred for the infiltrating fluid. Minimally altered samples have negative δ37Cl values (average = –0.6±0.1‰). δ37Cl values increase (up to +1‰) with increasing evidence of fluid-rock interaction. Measured Cl-stable isotope values of individual apatite grains are heterogeneous and range from −1.2 to +3.7‰. Highδ37Cl values are generally correlated with OH-rich zones formed during fluid-aided metasomatic alteration of the chlorapatite, whereas lowδ37Cl values, measured in the host chlorapatite, are interpreted to have been of magmatic origin.


### 6.3. Fluid Evolution

Changes in fluid conditions will affect the geochemical and mineralogical evolution during metasomatism. Fluids with a high Mg- and Cl-content cause scapolitisation and phlogopite formation [20, 29], while Na-rich solutions cause albitisation [12, 20, 21, 23]. The replacement of scapolite by albite during the albitisation also releases Cl into the albitisation fluid. Metasomatism is enhanced by Cl, which has been shown to be an effective ligand for transporting Fe [75, 76]. A high CO2 concentration in the fluid enhances carbonitisation [32]. The complexity and evolution of metasomatic fluids penetrating the Kragerø area can be explained by a series of different possible models, which include (1) phase separation of volatiles; (2) internal recycling; and (3) external infiltration, which are further expanded as follows.(1) Phase Separation of Volatiles. Fluid composition evolves as a function of changes in physical conditions. A decrease in temperature will affect separation of volatiles into different phases [77, 78]. Separation of hydrous and CO2-dominated fluid phases and brines could possibly explain the complex pattern in the spatial distribution of metasomatic rocks containing scapolite metagabbros, different varieties of albitites, and carbonate deposits in the Bamble lithotectonic domain.(2) Internal Recycling. Albitisation can be controlled by internal recycling of fluids. The observed fluid composition and mineralogical reactions can be an effect of local replacement reactions. Mineral reactions can both release and consume fluid components and solutes, and dissolved elements in one reaction can be used in another reaction. The scapolite gabbro in the Kragerø area is composed mostly of major Cl-CO2-dominated scapolite and Ti-, Fe-, and Cl-bearing amphibole. During albitisation, both minerals break down and disappear as the rock is transformed into albitite. During these reactions, all CO2, H2O, and Cl are released as fluids [50].Breakdown of scapolite during albitisation results in albite, CO2, and Cl via the following reactions:(1)Scapolite=2Albite+2CaO+2Al2O3+CO2+ClHere CaO and CO2 react to form calcite (Engvik et al. [50], Figures 4(a)–4(d)) and Cl can be reused as a ligand for metal complexing and transport. Also, replacement of rutile and scapolite by titanite releases CO2 and Cl, whereas replacement of ilmenite and scapolite will also release Fe: (2)2Rutile+Scapolite=2Titanite+Na2O+3Al2O3+4SiO2+Cl+CO2or(3)2Ilmenite+Scapolite=2Titanite+Na2O+3Al2O3+4SiO2+2FeO+Cl+CO2Breakdown of amphibole during albitisation occurs in two stages: (4)Amphibole+3H2O=Chlorite+Rutile+FeO+3SiO2+12Al2O3+12H2O+12CaO+14Na2O+Cl(5)Chlorite=5MgO+FeO+3SiO2+Al2O3+4H2OBreakdown of the Cl-bearing amphibole and, subsequently, chlorite releases H2O and Cl. Titanium from amphibole crystallizes as rutile [35], while Fe is either deposited as nanoinclusions of magnetite or hematite in the albite [79] or transported and deposited as ores associated with the albitite [23]. Excess Na, Al, and Si are used to produce albite or Al-Si-rich phases [34], and the Ca is incorporated into the calcite.(3) External Infiltration. Metasomatism can be controlled by an influx of external fluids. As discussed above, this work, combined with earlier isotopic studies in the Kragerø area [20, 27, 30, 32, 33], indicates a mixture of magmatic and evaporitic/seawater signatures. This is in agreement with the regional lithological distribution, which consists of a mixed gneiss region with magmatic rocks and metasedimentary sequences [43, 80] metamorphosed during the late Sveconorwegian tectonometamorphic event [20, 50]. Remobilized volatiles in sediments, possibly together with fluids derived during magmatic activity, were behind the regional metasomatism.Engvik et al. [50] discuss the variety in lithology, mineral assemblages, and replacement related to albitisation, indicating changing physical conditions during albitisation, which possibly occurred in several stages over a longer time interval. Similar metasomatic processes have been also reported in other regions such as Australia [5, 81, 82], which have been affected by various tectonic processes and crustal movements. The scapolitisation of dry gabbro requires the infiltration of an external fluid. The breakdown of a scapolite-amphibole-dominated metagabbro to albitite could possibly contribute a substantial amount of the necessary fluids. The question as to whether metasomatism occurred in an open or closed system therefore depends on the scale, that is, if we regard the metagabbro rim zone capable of producing reactive solutions, which cause local albitisation in a closed system, or if the large-scale Bamble lithotectonic domain can be considered as a closed system, including both magmatic and metasedimentary sequences.


### 6.4. On the Dynamics of Fluid Infiltration

As described above, scapolitisation and albitisation have occurred not only as static replacement of rocks, but also throughout those parts, which consist of dynamic deformed veining, breccias, and foliated schists. Fluid infiltration and metasomatic replacement both occur as a pervasive replacement of larger rock volumes as observed in the scapolitisation of gabbros. In addition, a high fluid pressure will cause fracturing, which channelizes the fluids, resulting in metasomatism that is widespread in a brittle deformed structure as single veins, networks of veins, and breccias (Figures2 and 3) resulting in structurally complex albitites and scapolite-bearing rocks. The reported local banded structure in scapolite metagabbros and albitites is interpreted to have been caused by veins (Figures 2(b)–2(d)) produced during metasomatic infiltration. A localized, high fluid pressure, resulting in brecciation of host rock, has been mapped out with both a scapolite-filling (Figures 2(e)–2(g)) at Åtangen and an albitite filling (Figures 3(e)-3(f)) at Langøy. The brittle fracturing and brecciation structures show a progressive deformation into the foliated schist. Here, the brecciated rocks are surrounded by scapolite-bearing schists and amphibolites (Figure 2(h)) or albite-dominated chlorite schists (Figure 4(e)) and carbonate-rich albitic felsites/schists (Figures 3(f)-3(g)). In addition, the role of deformation, as well as existing lithological contacts and lineaments, will affect the spatial distribution of the metasomatic rocks. Concurrent metasomatic infiltration and deformation caused a progression of the resulting foliation into the major regional structure, a process which was synchronous with a regional tectonometamorphic event.Formation of metasomatic scapolite metagabbros in the Kragerø area is constrained at 600 to 700°C at mid-crustal levels [19]. Formation of the clinopyroxene-bearing albitite in the Kragerø area is calculated to 410–420°C by Engvik et al. [50], while Mark and Foster [71] constrain similar albitites to 450–550°C from the Cloncurry district in Australia [71]. The local presence of prehnite, pumpellyite, and analcime indicates a low-grade albitisation event at temperatures < 350°C. The tectonometamorphic setting indicates that the albitisation processes occurred over a time span at middle to upper crustal levels. Although the scapolitisation conditions refer to a ductile crustal regime, fracturing and formation of breccias caused by high fluid pressure [83–85] have been described as a precursor stage for ductile deformation in the lower crust [86, 87]. A variation in fluid pressure can possibly explain the change between brittle and ductile deformation during metasomatism. The ductile formation of foliation in both the scapolite metagabbro and scapolite-bearing amphibolites at Åtangen, following scapolite-cemented brecciation, and similar formation of foliated albitic felsites and chlorite schists at Langøy, illustrate that the deformation changed from brittle to ductile during metasomatism. Both breccias and ductile rock fabrics are well known elsewhere in albitised and scapolitised crust [5, 20].In the Kragerø area, single, metasomatised, large (>1 km2) albitites and scapolite metagabbro bodies have been mapped. These replacement zones, resulting from metasomatic infiltration, are widespread on the regional scale similar to features mapped in the Modum area [21]. Age dating of the metasomatism indicates that these processes were part of the regional Sveconorwegian amphibolite-facies, tectonometamorphic phase. These ages are constrained by U-Pb ages from metasomatically generated rutile, titanite, and monazite between 1100 and 1070 Ma in the Bamble area [50] and by a U-Pb titanite age of 1080 Ma in the Modum area [21]. A later event connected to Permian Oslo Rift activity is evidenced by Ar-Ar age dating of metasomatically produced K-feldspar [88] and can possibly reflect the low-grade albitisation stage. Fluid infiltration during the Permian is indicated by alteration in the Bohus granite east of the Oslo Rift [89].The progressive development of albitised schists and scapolite-bearing amphibolites described above illustrates the importance of metasomatic processes during crustal evolution. These mineral phases and lithologies have a widespread occurrence, extending outside the mapped albitites in Figure1(b). Although not yet quantified, our results indicate the importance and extent of metasomatic influences on rock formation and structure on a regional scale.


## 6.1. Metasomatism and Mineralisation

Metasomatism is extensive in south Norway [18, 23]. Earlier work in the Bamble lithotectonic domain has shown that scapolitisation transforms mafic rocks into scapolite metagabbros by infiltration of Cl-Mg-rich solutions and that albitites form from both mafic and granitoid protoliths by Na-rich solutions [20, 35]. As expected, Na2O increases and CaO decreases during albitisation. Addition of albite to a gabbroic protolith will dilute the nonadded elements in equal proportion. Although the overall trend displayed by Figure 5 can be explained by addition of albite and scapolite to a gabbroic protolith, the TiO2-Fe2O3 relationship shown in Figure 5(k) strongly indicates that addition of albite and scapolite alone cannot explain the chemical evolution displayed and that other elements must have been mobile. The strong reduction in Fe2O3 suggests that this oxide is removed during albititisation and to some extent during scapolitisation. The measured variation in Br and Cl which is assumed to parallel Br suggests that these elements are added during the scapolitisation but were removed from the rock during albitisation. The mineralogical evolution, where Cl-scapolite formed during scapolitisation and later broke down during albitisation, suggests that halogens will be present in the fluid also during albitisation and are available for complexing with metals (e.g., Fe, Cu, and Zn). We suggest that such a complexing can explain the many ore deposits in the area and in particular the Langøy Fe-mines.The Bamble lithotectonic domain is characterised not only by widespread metasomatic alteration, but also by a high density of mineral deposits (Geological Survey of Norway Ore Database [24–26]). The high density of apatite and rutile deposits follows the regional distribution of metasomatic alteration in the Bamble lithotectonic domain [23]. While ilmenite is the main Ti-bearing mineral in the gabbro protolith, Ti occurs as rutile (Figures 6(a)-6(b)) and in amphibole (<0.34 a.p.f.u.) and biotite (<0.69 a.p.f.u.) within the scapolite metagabbro [20]. Replacement of ilmenite by rutile is illustrated in Figures 6(a)-6(b). During albititisation, biotite and amphibole break down and Ti is released as titanite [20, 31]. The whole rock geochemical data (Figures 5(i) and 5(j)) illustrates that TiO2 and V increased during scapolitisation and decreased during albitisation. The high values of TiO2 in some of the albitites are probably inherited from the scapolite enrichment. Fe2O3 decreases during scapolitisation and albitisation and the TiO2-Fe2O3 relationships (Figure 5(k)) cannot be the result of pure dilution by adding albite and scapolite but suggest that Fe is removed.The whole rock geochemistry in Figure5(e) illustrates the P, which is increased during scapolitisation and that the P resources at Ødegården Verk owe their existence to this event rather than the albitisation event which leads to a reduction of P. This is in accordance with earlier works which show that scapolite metagabbros commonly have both a high apatite content in the Bamble lithotectonic domain and host vein-related apatite deposits (Figure 6(c)) [19, 28, 29]. Scapolitisation and albitisation are documented as having formed chlorapatite and hydroxyfluorapatite at Ødegården Verk in Bamble (Figure 6(c)) [19, 28, 29].As discussed above, metasomatism of the gabbro causes extensive Fe-depletion (Figure5(c)) [20]. In addition, the whole rock geochemistry shows that the concentration of Cu and Zn is lowered during the scapolitisation of the gabbro/metagabbro (Figures 5(f)-5(g)) and is nearly completely depleted during albitisation of the same protolith. The fluid mobilization of these elements could have caused the widespread occurrences of metal deposits in the Bamble lithotectonic domain [23]. Fe-oxide ores are present as hematite-carbonate veins in the rutile-rich albitites in the Kragerø area and are widespread in the Bamble lithotectonic domain [23, 58], as hematite-rich albitites, orthoamphibole-hematite veins, and albite-magnetite veins. Cu-Zn-bearing base metal deposits are frequent in the Kragerø-Bamble area (Geological Survey of Norway Ore Database). The association of Fe-ores with albitites and altered granites has been reported worldwide, for example, as in magnetite-apatite deposits from the Lyon Mountain area, Adirondacks, New York, USA [67].


## 6.2. Stable Isotopic Results: Fluid and Rock Origin

The stable isotopic composition of silicate mineral separates can reflect the origin of both the rocks and the infiltrating fluid [68, 69]. It will retain information from the protolith phases, but, depending on the degree of alteration and replacement, the isotopic composition will undergo a shift during fluid infiltration. Oxygen is already present in significant concentrations in the silicate minerals. To shift the δ18O composition in a silicate mineral will require large amounts of infiltrating fluids. This must be the case for the albitite rocks in the Bamble lithotectonic domain, which have undergone complete alteration to a new mineralogy, involving large chemical changes [20, 23, 50].Aδ18OSMOW composition of 5.1 to 8.4‰ is seen for the albite separates from albitite formed from a gabbroic protolith (Table 3). Results for albite from a carbonate-rich albitite deposited in metagabbro at Langøy fall in the same range. A δ18OSMOW composition of 8.5 to 10.8‰ is obtained for albite, which originated from a granitoid protolith in the Ringsjø-Ødegården Verk area. From a clinopyroxene-bearing albitite in the Åtangen-Storkollen area, the albite gives a δ18OSMOW composition of 10.8 to 11.1‰ and the quartz 11.5 to 11.6‰. The results from measured albitites from both mafic and tonalitic magmatic precursors are in accordance with the original values from such protoliths [70] coupled with the influence of a fluid with both a magmatic and seawater origin [69]. Depending on the temperature, the reported O-isotopic signature could originate from a magmatic fluid, although a magmatic fluid would normally give a higher value. Seawater could explain the reported values since it could lower the isotopic ratio relative to the magmatic protolith values. As metasomatic fluid infiltration is often spatially inhomogeneous, this could possibly also explain variations in the resulting values. A meteoric water source can clearly be ruled out, as meteoric water would have led to a significantly lower δ18OSMOW composition of about +2 to -10‰. Mark and Foster [71] document a similar δ18OSMOW composition associated with albitisation in the Cloncurry district, Australia, and concluded that it is due to magmatic processes.Amphiboles in scapolite metagabbros were produced during fluid infiltration into the dry protolith gabbro [20, 29]. This implies that the H-isotopic content of the amphiboles, in contrast to the O-isotopes, will give more accurate information regarding the metasomatic fluid. The δD-composition of the amphibole from the scapolite metagabbro generally varies between −50 and -59‰ and is in accordance with an igneous precursor [70] infiltrated by magmatic or metamorphic H2O [69, 72]. A hydrothermal saline solution would not affect the δD-composition, as it will give similar δD-values compared to magmatic and metamorphic fluids. Again, a meteoric water origin can be excluded as it would give significantly lower values for the δD composition down to −90 to -140‰. The stable isotopic composition of scapolite-bearing rocks is known from Mary Kathleen, Queensland, Australia [73], where the scapolitisation is interpreted to have been caused by magmatic fluids, and the Greenville Province, Ontario, Canada [74], where scapolitisation was caused by metamorphic fluids originating from a carbonate source.For the carbonate-rich albitite, theδ18OSMOW values show values similar to silicate rocks, indicating a magmatic source for C (Figure 7). This is supported by the δ13CPDB values, which fall between −6.0 and -4.6‰ and give signatures similar to those for carbonatitic magma. Our petrographic investigations show in addition that breakdown of scapolite during albitisation produces carbonate [50]. Dahlgren et al. [32] described vein deposited dolomite marbles giving δ18O = 9.6 to 10.7‰, δ13C = −8.5 to -6.2‰, and high 87Sr/86Sr ratios of 0.706 to 0.709, which overlaps the values reported from these studies (Figure 6) and values from the Bamble hyperites [37] and vein carbonates [40]. Dahlgren et al. [32] suggested that the dolomite marbles were formed from hydrothermal solutions that were channeled into a large degassing zone, which now takes the form of a deformed, regional zone with hydrothermal dolomite deposits, albitites, apatite-veins, and widespread scapolitisation. These authors speculated that the fluids were derived from charnockite intrusions in the region.Figure 7
δ
18
O
S
M
O
W versus δ13CPDB plot: circles indicate data from this study (Table 3) and diamonds indicate data from dolomite marble deposits/veins and a calcite + albite + quartz dike in the Kragerø area by Dahlgren et al. [32]. BG = Bamble hyperites [37]; CBT = world carbonatites [38]; PC = nonmetamorphic proterozoic carbonates [39]; VC = vein carbonate [40].As mentioned above, while metasomatism is able to significantly alter the chemical composition of the precursor rock, this alteration may vary spatially. This also applies to the isotope composition of the rocks. Probably this is due to varying temperatures as well as the different water/rock (w/r) ratios that caused the alteration. The variable oxygen isotope composition in all altered rock types from this study, in combination with relatively homogeneous H- and C-isotope ratios, corroborates this assumption. Varying degrees of alteration, variableT, and variable w/r ratios can produce isotopic signatures that reflect the values that we have measured and are shown in Table 3. In addition, fluid compositions can also have been varied, even on a local scale, and scales of equilibrium might also have been local, regardless of the widespread regional occurrence of the metasomatic rocks.For the sampled localities, Engvik et al. [20] reported a Cl- and B-rich environment, Sr-signatures in the scapolite with an initial 87Sr/86Sr ranging from 0.704 to 0.709, and a regional distribution of lithologies, indicating that the fluid originated from evaporites that were mobilized during regional metamorphism. Our new data on the stable isotopic composition of the albitites and scapolite metagabbro support the interpretation that the original magmatic mafic and granitoid rocks were metasomatised by fluids reflecting a seawater origin or with a possible magmatic component. Depending on T, w/r, and the degree of alteration, both fluid types (seawater and magmatic) may lead to the same approximate pattern. What can be ruled out from the H and O stable isotope data is meteoric water as it would have led to significantly lower δ18OSMOW and δDSMOW values and also to different δ13CPDB values.Other stable isotopic constraints in the Kragerø area of the Bamble lithotectonic domain support a mixture of magmatic and metamorphic fluid signatures coupled with seawater as being responsible for the metasomatism. Bast et al. [33] analysed B isotope compositions in tourmaline in order to constrain the possible sources of and the evolution of hydrothermal fluids. δ11B values were found to range from −5 to +27‰ (relative to SRM-951), which suggests marine evaporites interlayered with continental detritus and pelagic clay as a possible B source reservoir. Negative δ11B values were explained by the influence of pneumatolytic fluids associated with granitic pegmatites. Variations in δ11B on a regional km-scale, with small local variations, were explained by fluid infiltration during several generations of pulses.Measurements ofδ37Cl, together with F, Cl, Br, and I concentrations, were used to trace the metasomatic evolution of gabbroic bodies and to understand the interplay between localized and pervasive fluid flow [27, 30]. The reported Br/Cl and I/Cl ratios (3 × 10−3 and 25 × 10−6) overlap with the range of ratios measured for marine pore fluids. The unaltered gabbro has δ37Cl values near 0% and a similar value is inferred for the infiltrating fluid. Minimally altered samples have negative δ37Cl values (average = –0.6±0.1‰). δ37Cl values increase (up to +1‰) with increasing evidence of fluid-rock interaction. Measured Cl-stable isotope values of individual apatite grains are heterogeneous and range from −1.2 to +3.7‰. Highδ37Cl values are generally correlated with OH-rich zones formed during fluid-aided metasomatic alteration of the chlorapatite, whereas lowδ37Cl values, measured in the host chlorapatite, are interpreted to have been of magmatic origin.


## 6.3. Fluid Evolution

Changes in fluid conditions will affect the geochemical and mineralogical evolution during metasomatism. Fluids with a high Mg- and Cl-content cause scapolitisation and phlogopite formation [20, 29], while Na-rich solutions cause albitisation [12, 20, 21, 23]. The replacement of scapolite by albite during the albitisation also releases Cl into the albitisation fluid. Metasomatism is enhanced by Cl, which has been shown to be an effective ligand for transporting Fe [75, 76]. A high CO2 concentration in the fluid enhances carbonitisation [32]. The complexity and evolution of metasomatic fluids penetrating the Kragerø area can be explained by a series of different possible models, which include (1) phase separation of volatiles; (2) internal recycling; and (3) external infiltration, which are further expanded as follows.(1) Phase Separation of Volatiles. Fluid composition evolves as a function of changes in physical conditions. A decrease in temperature will affect separation of volatiles into different phases [77, 78]. Separation of hydrous and CO2-dominated fluid phases and brines could possibly explain the complex pattern in the spatial distribution of metasomatic rocks containing scapolite metagabbros, different varieties of albitites, and carbonate deposits in the Bamble lithotectonic domain.(2) Internal Recycling. Albitisation can be controlled by internal recycling of fluids. The observed fluid composition and mineralogical reactions can be an effect of local replacement reactions. Mineral reactions can both release and consume fluid components and solutes, and dissolved elements in one reaction can be used in another reaction. The scapolite gabbro in the Kragerø area is composed mostly of major Cl-CO2-dominated scapolite and Ti-, Fe-, and Cl-bearing amphibole. During albitisation, both minerals break down and disappear as the rock is transformed into albitite. During these reactions, all CO2, H2O, and Cl are released as fluids [50].Breakdown of scapolite during albitisation results in albite, CO2, and Cl via the following reactions:(1)Scapolite=2Albite+2CaO+2Al2O3+CO2+ClHere CaO and CO2 react to form calcite (Engvik et al. [50], Figures 4(a)–4(d)) and Cl can be reused as a ligand for metal complexing and transport. Also, replacement of rutile and scapolite by titanite releases CO2 and Cl, whereas replacement of ilmenite and scapolite will also release Fe: (2)2Rutile+Scapolite=2Titanite+Na2O+3Al2O3+4SiO2+Cl+CO2or(3)2Ilmenite+Scapolite=2Titanite+Na2O+3Al2O3+4SiO2+2FeO+Cl+CO2Breakdown of amphibole during albitisation occurs in two stages: (4)Amphibole+3H2O=Chlorite+Rutile+FeO+3SiO2+12Al2O3+12H2O+12CaO+14Na2O+Cl(5)Chlorite=5MgO+FeO+3SiO2+Al2O3+4H2OBreakdown of the Cl-bearing amphibole and, subsequently, chlorite releases H2O and Cl. Titanium from amphibole crystallizes as rutile [35], while Fe is either deposited as nanoinclusions of magnetite or hematite in the albite [79] or transported and deposited as ores associated with the albitite [23]. Excess Na, Al, and Si are used to produce albite or Al-Si-rich phases [34], and the Ca is incorporated into the calcite.(3) External Infiltration. Metasomatism can be controlled by an influx of external fluids. As discussed above, this work, combined with earlier isotopic studies in the Kragerø area [20, 27, 30, 32, 33], indicates a mixture of magmatic and evaporitic/seawater signatures. This is in agreement with the regional lithological distribution, which consists of a mixed gneiss region with magmatic rocks and metasedimentary sequences [43, 80] metamorphosed during the late Sveconorwegian tectonometamorphic event [20, 50]. Remobilized volatiles in sediments, possibly together with fluids derived during magmatic activity, were behind the regional metasomatism.Engvik et al. [50] discuss the variety in lithology, mineral assemblages, and replacement related to albitisation, indicating changing physical conditions during albitisation, which possibly occurred in several stages over a longer time interval. Similar metasomatic processes have been also reported in other regions such as Australia [5, 81, 82], which have been affected by various tectonic processes and crustal movements. The scapolitisation of dry gabbro requires the infiltration of an external fluid. The breakdown of a scapolite-amphibole-dominated metagabbro to albitite could possibly contribute a substantial amount of the necessary fluids. The question as to whether metasomatism occurred in an open or closed system therefore depends on the scale, that is, if we regard the metagabbro rim zone capable of producing reactive solutions, which cause local albitisation in a closed system, or if the large-scale Bamble lithotectonic domain can be considered as a closed system, including both magmatic and metasedimentary sequences.


## 6.4. On the Dynamics of Fluid Infiltration

As described above, scapolitisation and albitisation have occurred not only as static replacement of rocks, but also throughout those parts, which consist of dynamic deformed veining, breccias, and foliated schists. Fluid infiltration and metasomatic replacement both occur as a pervasive replacement of larger rock volumes as observed in the scapolitisation of gabbros. In addition, a high fluid pressure will cause fracturing, which channelizes the fluids, resulting in metasomatism that is widespread in a brittle deformed structure as single veins, networks of veins, and breccias (Figures2 and 3) resulting in structurally complex albitites and scapolite-bearing rocks. The reported local banded structure in scapolite metagabbros and albitites is interpreted to have been caused by veins (Figures 2(b)–2(d)) produced during metasomatic infiltration. A localized, high fluid pressure, resulting in brecciation of host rock, has been mapped out with both a scapolite-filling (Figures 2(e)–2(g)) at Åtangen and an albitite filling (Figures 3(e)-3(f)) at Langøy. The brittle fracturing and brecciation structures show a progressive deformation into the foliated schist. Here, the brecciated rocks are surrounded by scapolite-bearing schists and amphibolites (Figure 2(h)) or albite-dominated chlorite schists (Figure 4(e)) and carbonate-rich albitic felsites/schists (Figures 3(f)-3(g)). In addition, the role of deformation, as well as existing lithological contacts and lineaments, will affect the spatial distribution of the metasomatic rocks. Concurrent metasomatic infiltration and deformation caused a progression of the resulting foliation into the major regional structure, a process which was synchronous with a regional tectonometamorphic event.Formation of metasomatic scapolite metagabbros in the Kragerø area is constrained at 600 to 700°C at mid-crustal levels [19]. Formation of the clinopyroxene-bearing albitite in the Kragerø area is calculated to 410–420°C by Engvik et al. [50], while Mark and Foster [71] constrain similar albitites to 450–550°C from the Cloncurry district in Australia [71]. The local presence of prehnite, pumpellyite, and analcime indicates a low-grade albitisation event at temperatures < 350°C. The tectonometamorphic setting indicates that the albitisation processes occurred over a time span at middle to upper crustal levels. Although the scapolitisation conditions refer to a ductile crustal regime, fracturing and formation of breccias caused by high fluid pressure [83–85] have been described as a precursor stage for ductile deformation in the lower crust [86, 87]. A variation in fluid pressure can possibly explain the change between brittle and ductile deformation during metasomatism. The ductile formation of foliation in both the scapolite metagabbro and scapolite-bearing amphibolites at Åtangen, following scapolite-cemented brecciation, and similar formation of foliated albitic felsites and chlorite schists at Langøy, illustrate that the deformation changed from brittle to ductile during metasomatism. Both breccias and ductile rock fabrics are well known elsewhere in albitised and scapolitised crust [5, 20].In the Kragerø area, single, metasomatised, large (>1 km2) albitites and scapolite metagabbro bodies have been mapped. These replacement zones, resulting from metasomatic infiltration, are widespread on the regional scale similar to features mapped in the Modum area [21]. Age dating of the metasomatism indicates that these processes were part of the regional Sveconorwegian amphibolite-facies, tectonometamorphic phase. These ages are constrained by U-Pb ages from metasomatically generated rutile, titanite, and monazite between 1100 and 1070 Ma in the Bamble area [50] and by a U-Pb titanite age of 1080 Ma in the Modum area [21]. A later event connected to Permian Oslo Rift activity is evidenced by Ar-Ar age dating of metasomatically produced K-feldspar [88] and can possibly reflect the low-grade albitisation stage. Fluid infiltration during the Permian is indicated by alteration in the Bohus granite east of the Oslo Rift [89].The progressive development of albitised schists and scapolite-bearing amphibolites described above illustrates the importance of metasomatic processes during crustal evolution. These mineral phases and lithologies have a widespread occurrence, extending outside the mapped albitites in Figure1(b). Although not yet quantified, our results indicate the importance and extent of metasomatic influences on rock formation and structure on a regional scale.



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