Newtontoppen granitoid rocks, their 
and Rb-Sr age 
A .  M. TEBEN’KOV, Y. OHTA, JU. A .  BALASOV and A. N. SIROTKIN 

geology, chemistry 

Teben’kov, A. M . ,  Ohta, Y., BalaSov, Ju. A. & Sirotkin, A. N. 1996: Newtontoppen granitoid rocks, 
their geology, chemistry and Rb-Sr age. Polar Research 15(1), 67-80. 

A post-tectonic Caledonian granite in southern Ny Friesland has been fully mapped and the following new 
names are proposed: the Chydeniusbreen granitoid suite, consisting of the Raudberget granitoid body in 
the north; the Newtontoppen granitoid body in the middle; and the Ekkoknausane granitoid body in the 
south. 

The contact relationships, internal structures and distribution of various rock types infer an asymmetric 
lopolith or a harpolith-like body, a large sickle-shaped intrusion stretched in the direction of general 
tectonic transport, for the Newtontoppen granitoid body. 

Seven rock types are described in the Newtontoppen granitoid and four emplacement stages are 
recognised. The major rock types seem to have an alkali-calcic to alkalic bulk rock chemistry and show a 
transition between I- and S-type granite derived from anatectic melting of various protoliths under relatively 
high temperature conditions. Possible later K 2 0  introduction modified the earlier formed rock types. 

A Rb-Sr whole rock age of 432 2 10 Ma has been obtained by a seven point isochron with MSDW = 
2.59 and an initial Sr isotope ratio = 0.715. This age is approximately 3 0 M a  older than the previously 
obtained K-Ar whole rock and Rb-Sr biotite ages, ca. 400 Ma, which represents the period of cooling. The 
high initial Sr isotope ratio supports the interpretation of an anatectic origin. 

A .  M. Teben’kou and A .  N .  Sirorkin, Polar Marine Geological Expedition, ul. Pobedy 24, 189510 
Lomonosov, St. Petersburg, Rwsia; Y .  Ohta, Norsk Polarinstitutt, P. 0. Box 5072 Mujorstua, N-0301 Oslo, 
Norway; Ju. A .  Balafov. Geological Institute, Kola Science Centre of Academy of Sciences, ul. Fersman 
14. 184200 Apatity, Russia. 

Introduction 

Three intrusive bodies of granitoid rocks are 
known in southern Ny Friesland and northwestern 
Olav V Land, northeastern Spitsbergen (Fig. 1, 
inserted map, right). The granitic rocks have been 
known from as early as the latter half of last 
century (Drasche 1874; Nordenskiold 1875; Gar- 
wood 1899; Nathorst 1910). Backlund (1908) 
described two rock types and found that these 
granitoid rocks cut the Precambrian Hecla Hoek 
succession. A petrographic summary was made by 
Tyrrell (1922). Oddel (1927) found the northern 
locality in the Raudberget area, where the granitic 
rock is unconformably overlain by Carboniferous 
strata, and thus concluded that the granitoids are 
of Caledonian age. Hjelle (1966) and Kra- 
sil’SCikov (1969) made petrographic studies and 
described another separate locality in the south 
around the Ekkoknausane area, in the upper 
reaches of Nordenskioldbreen. 

These granitoid rocks have been called the 
Chydenius granite (Oddel 1927) or the Chydenius 
batholith (Harland 1959). However, as the place 
name “Chydenius” does not exist, these names 
should be changed according to the suggestion of 
the Norwegian Stratigraphic Committee. Chy- 
deniusfjella is actually outside the distribution 
area of the granitoid rocks. Small nunataks con- 
sisting of the granitoid rocks occur on both sides 
of Chydeniusbreen; therefore, the following new 
names will be introduced here: the Chyden- 
iusbreen granitoid suite for the three bodies 
together, the Raudberget granitoid body for the 
northern occurrence, the Newtontoppen grani- 
toid body for the middle massif, and the Ekko- 
knausane granitoid body for the southern locality 
(Fig. 1 ,  inserted map, right). 

The rock compositions range from clino- 
pyroxene-bearing granodiorite to granosyenite 
(Hjelle 1966; Krasil’SEikov 1969), and the struc- 
ture has been considered a batholith, the three 



\ 
\ 
\ 
\ 

68 A .  M .  Teben’kou et al. 

Fig. 1. Geological map of the Newtontoppen granitoid body, with inserted location maps. Inserted map in the right: RB = 
Raudberget granitoid, N T  = Newtontoppen granitoid, EK = Ekkoknausane granitoid, NB = Nordenskioldbreen, T = 
Terrierfjellet, F = Ferrierfjellet. Key: 1, grey granites; 2, (without ornament) pink-grey granosyenites; 3, granosyenite with aligned 
K-feldspar; 4, pegmatites; 5 ,  aplites (a), quartz-feldspar porphyry (Qp) and lamprophyre (L); 6, estimated outlines of the rock 
types; 7, meta-clastic sediments of the Veteranen Group; 8, marbles of the Akademikerbreen Group; 9, cleavages of the 
metasediments; 10, mesoscopic structures within the granitoid rocks; 11, joints and their general trends; 12, observed and estimated 
boundary of the Newtontoppen granitoid body; 13, estimated boundary between the Veteranen and the Akademikerbreen Groups. 
Dot and Nos. with circle: observation points and sample localities (ref: all tables and Figs. 2, 3, 4, 9 ,  10). 



Newtontoppen granitoid rocks, their geology, chemistry and Rb-Sr age 69 

bodies being considered to be continuous under 
the surface (Harland 1959). The Ekkoknausane 
granitoid has been thought to be the roof of the 
batholith, rich in xenoliths and aplite-pegmatite 
dykes (Hjelle 1966). Krasil'SEikov (1969, 1979) 
considered the exposures in Ekkoknausane to be 
a group of small intrusions. 

The Newtontoppen granitoid body cuts the 
strata of the metasediments of the Lomfjorden 
Supergroup (Harland 1959). The cooling age has 
been given by K-Ar whole rock ages of 385- 
406Ma and Rb-Sr biotite ages of 401-402Ma 
(Hamilton et al. 1962). 

The present paper describes the field occur- 
rences of all three bodies, the bulk rock chemistry, 
and the Rb-Sr whole rock isochron age from the 
Newtontoppen granitoid body. 

Contact relationships 
The contacts of the Newtontoppen granitoids to 
the surrounding metasediments are evidently 
cross-cutting and intrusive. The surrounding 
rocks at the contacts are meta-arenaceous sedi- 
ments of the Veteranen Group on the western 
side, and marbles and meta-pelitic rocks of the 
Akademikerbreen Group to the east, both of the 
Lomfjorden Supergroup of Neoproterozoic age. 
The greenschist-subgreenschist facies metamor- 
phic mineral assemblages in these rocks were 
locally superimposed by middle amphibolite fac- 
ies assemblages in the thermal aureole produced 
by the granitoids, as much as 100m away from 
the contacts. The meta-arenaceous rocks at the 
southwestern contact (Fig. 1, LOC. 6) were con- 
verted into andalusite-cordierite-biotite hornfel- 
ses. The carbonate rocks at the northwestern (Fig. 
1, LOC. 13) and middle eastern (Fig. 1, LOC. 23) 
contacts recrystallised into marbles with 
wollastonite, tremolite and quartz, and the meta- 
arenaceous rocks at LOC. 23 were converted into 
biotite-cordierite-quartz hornfelses. 

The contact surface dips 70-90" in the south 
and west, and 40-60" in the north and east, both 
beneath the granitoid body. Thin aplite veins are 
confined within the body, striking subparallel to 
the contacts, and have not been seen intruding 
the surrounding rocks. No exotic xenolith has 
been found, but preferred alignments of elon- 
gated melanozomes are distinct in the marginal 
part of the body. 

The Raudberget granitoids form a small nun- 

atak which is located ca. 12 km NE of the New- 
tontoppen granitoid body, on the northern side 
of Chydeniusbreen (Fig. 1, inserted map, right), 
and the continuation to the latter is uncertain. 
The granitoid rocks are unconformably covered 
by flat lying Carboniferous strata. 

The Ekkoknausane granitoids (Fig. 1, inserted 
map, right) consist of five nunataks, and are prob- 
ably covered unconformably by the Carbon- 
iferous Nordenskioldbreen Formation. The 
granitoids show sharp intrusive contacts to the 
Veteranen Group quartzites and sandstones at 
Terrierfjellet and Ferrierfjellet, southeast of Nor- 
denskioldbreen. Aplitic and granitic veins 
increase in the surrounding rocks approaching the 
contacts. A 50 m by 100 m granitoid mass cuts a 
quartzite-sandstone succession on the southern 
side of Ferrierfjellet, possibly a stock or a dyke, 
though the boundary is covered by scree. At 
Terrierfjellet, the westernmost part consists of 
gneissic rocks of the Planetfjella Group in fault 
contact with the Veteranen Group which forms 
the eastern part. The granitoid rocks cut a quartz- 
ite-sandstone succession of the latter. 

At the three nunataks of Ekkoknausane, in 
the uppermost reaches of Nordenskioldbreen, the 
granitoid rocks are markedly heterogeneous, con- 
taining quartzo-pelitic xenoliths with cross bed- 
ding and ripple marks, dark patches and seams of 
melanocratic inclusions containing clinopyroxe- 
ne-hornblende aggregates, and irregular blocks 
of gabbroic and gneissose granitic rocks with cat- 
aclastic textures. Some dark inclusions show 
orbicular structures. 

In summary, the Ekkoknausane granitoid body 
is located near the boundary between the Meso- 
proterozoic Planetfjella and Neoproterozoic Vet- 
eranen Groups, and the Newtontoppen granitoid 
body is situated around the boundary between 
the Veteranen and Akademikerbreen Groups. 
The Raudberget granitoid body occurs within the 
Akademikerbreen Group, but near the eastern 
marginal fault zone of the Neoproterozoic met- 
asediments towards the Carboniferous to the east. 

Structure of the Newtontoppen 
granitoid body 
Alignments of K-feldspar phenocrysts and elon- 
gated melanozomes are the main mesoscopic 
structural elements within the Newtontoppen 
granitoid body. These structures are confined to 



70 A .  M. Teben’kou et al. 

the peripheries of the body and are mainly 
oriented subparallel to the margins (Fig. l ) ,  
except for two measurements in the eastern and 
southeastern margins (LOCS. 23 and 27 in Fig. 1). 

The K-feldspar phenocrysts sometimes include 
granulated plagioclase, especially near their rims. 
No granulated plagioclase has been seen in the 
non-porphyritic lithologies. This means that the 
K-feldspar phenocrysts were formed in the granu- 
lated parts of the rocks; thus the K-feldspar por- 
phyritic parts generally show the distribution of 
granulation, which in turn suggest locally granu- 
lated parts in the body during emplacement move- 
ments. The interior of the body is completely 
massive, and a weak planar structure represented 
by preferred arrangement of phenocrysts could 
be measured at only one locality. 

Joints are regularly developed in the body on 
two steep dipping planes, one subparallel and the 
other subperpendicular to the contacts, and on 
one subhorizontal plane (Fig. 1). Small dip-vari- 
ations of the horizontal joints infer a gentle dome- 
like cooling surface over the body. The simple 
joint pattern throughout the body suggests a 
single cooling unit. 

Later aplitic and quartz-feldspar porphyry 
dykes occur along the peripheries within the body 
from the north to the southeastern margin. These 
are obliquely cut by the steep dipping joints. 

A lamprophyre dyke occurs near the south- 
eastern margin. This rock is petrogenetically 
unrelated to the granitoids, but often occurs near 
Caledonian granite intrusions in Svalbard (Lau- 
ritzen & Ohta 1984; Kovalyova & Teben’kov 
1986). 

Weak post-consolidation movements have 
been recorded as slips along joint surfaces near 
the western margin (LOC. 8 in Fig. l), where the 
surfaces are covered by chlorite. A 3 m-wide shear 
zone with hematite has been observed at Val- 
letteknausen, on the southern side of Chy- 
deniusbreen (LOC. 13 in Fig. l), separating the 
porphyritic granite from Carboniferous white- 
grey limestones, without any thermal effect. 

The Newtontoppen granitoid body is assumed 
to be an asymmetric lopolith or a harpolith-like 
shape; a large sickle-shaped intrusion elongated 
in general tectonic transport direction, based on 
the following evidence: (1) steep dips of the con- 
tact surfaces beneath the body in the southwest 
and moderate dips from north to southeast, (2) 
relatively rich melanozomes in the south and 
southwest, and (3) the distribution of aplite dykes 

from the southeast to the northern margin. This 
suggests that the body has a steep root in the 
southwest and an extended thinner tongue to the 
east and north. The exposed thickness of the 
body is about 900 to 1OOOm in the southern to 
southwestern parts. The roof of the harpolith-like 
body has been removed by erosion. The contact 
hornfelses having andalusite-cordierite assem- 
blages infer low pressure conditions at a relatively 
shallow depth. 

Petrography 
Backlund (1908) described porphyritic and non- 
porphyritic varieties from the granitoid rocks, 
while Oddel (1927) wrote that these varieties are 
caused by various degrees of surface weathering. 
Hjelle (1966) reported that the modal com- 
positions of the rocks range from granodiorite to 
granosyenite. The following rock types have been 
recognised in the Newtontoppen granitoid body 
in the field, with their field names, referring to 
Streckeisen (1976): 

1. melanozomes and dark grey granosyenites, 
2. pink-grey granosyenites and pink quartz 

3. grey granites, 
4. granosyenite with aligned K-feldspar pheno- 

5. aplitic veins, 
6. pegmatites, 
7. quartz-feldspar porphyry. 

monzonites, 

crysts, 

Melanozomes and dark grey granosyenites 

These rocks are represented by melanozomes and 
dark varieties of the more common pink-grey 
granosyenites. The melanozomes (sample nos. 1, 
2 in Tables 1 , 2  and Figs. 2-4) occur as inclusions 
in various types of granosyenites near the margin 
of the body, as round and/or elongated patches 
and seams of several cm to 4-5 m in length, with 
partly diffused margins. They contain more mafic 
minerals and less quartz than the host rocks, with 
modal compositions of melanocratic granosyen- 
ite. Their constituent minerals are the same as 
other granosyenites and they are considered to 
be cognate inclusions. Some gabbroic inclusions 
found in the Ekkoknausane body could be similar 
in origin. The melanozomes contain as much as 
10 modal % clinopyroxene which is always sur- 



Newtontoppen granitoid rocks, their geology, chemistry and Rb-Sr age 71 

. 5  

4 
F 

3 0  

2 

1 

Ab Or 50 4 0  30 20 

Fig. 2. CIPW normative ratios, Q-Or-Ab diagram. Key: solid 
triangles = melanozomes and dark grey granosyenites; solid 
circles = pink-grey granosyenites; crosses = grey granites; 
oblique crosses = pink quartz monzonites; open triangles = 
granosyenite with aligned K-feldspar; open squares = aplites; 
circle with dot = quartz-feldspar porphyry. These symbols are 
the same in all figures, except for Figs. 9 and 10. Broken curves: 
eutectic minimums at various vapour pressures. Nos. refer to 
the first column of Table 1. 

60 60 

Fig. 3. AFM diagram. TH-CA dividing curve: Irvine & Baragar 
(1971); between the two broken curves: common C A  field 
(Ringwood 1974). Same nos. and symbols as Fig. 2. 

rounded by green prismatic hornblende (ca 15 
modal %). Brown biotite occupies ca. 10 to 15 
modal % of the rock. K-feldspar occurs inter- 
stitially in most rocks, but it is locally phenocrystic 
and includes many grains of prismatic plagioclase 
and mafic minerals. 

The dark grey granosyenites (sample nos. 3 , 4 ,  
5 in Tables 1, 2 and Figs. 2-4) are more coarse- 

1 .  I 
75 

65 sio2 ’O 
55 60 

Fig. 4 .  N a 2 0  + K 2 0  and CaO vs. S O L  diagram, in weight 
percent. Alkali-subalkali division: Irvine & Baragar (1971). The 
alkali-lime index is roughly estimated between 56 and 47. Same 
nos. and symbols as Fig. 2. 

grained than the melanozomes, having similar 
modal compositions, locally with K-feldspar por- 
phyritic texture. They show a gradational tran- 
sition contact with the pink-grey granosyenites. 

Syenites, monzonites and granites 

The differences in modal compositions of quartz 
and mafic minerals and the colour of K-feldspar 
discriminate these rock types; pink-grey grano- 
syenites (sample nos. 6 t o  9 in Tables 1, 2 and 
Figs. 2 - 4 ,  pink quartz monzonites (sample nos. 
15 to 17 in Tables 1, 2 and Figs. 2-4) and grey 
granites (sample nos. 10 to 14 in Tables 1, 2 and 
Figs. 2-4). 

These rocks occupy ca.90% of the New- 
tontoppen granitoid body. The grey granite occu- 
pies the center of the body, while the other two 
rock types are irregularly mixed and occur around 
the grey granite. No cross-cutting relationship has 
been observed between them and the borders are 
gradational. 

All of these rocks are K-feldspar porphyritic; 
phenocrysts are 4 4  cm in size and occupy ca. 4 s  
50 modal % of the rocks. K-feldspar always 
exceeds plagioclase, and microcline twins are dis- 
tinct in the K-feldspars of the granosyenites and 
quartz monzonites, while not distinct in the grey 
granites. The matrices of all three rock types show 
a coarse-grained, hypidiomorphic texture and 
consist of K-feldspar, quartz and plagioclase in 
similar amounts (5-20 modal % each), biotite and 
hornblende (5-20 modal % each) and cli- 
nopyroxene. Clinopyroxene is absent in the grey 



72 A .  M. Teben’kov et al. 

Table 1. Major element compositions of granitord rocks from the Newtontoppen granitoid body. The first numbers in the second 
column correspond t o  the locality numbers in Fig. 1. Melanozomes and dark grey granosyenites: 1-5; pink-grey granosyenites: b 
9; grey granites. 1G-14; pink quartz monzonites: 15-17; granosyenite with aligned K-feldspar: 18; aplites: 19 and 20; quartz 
porphyry: 21. No. 17 is a quartz monzonite from the Raudberget granitoid body. The sample numbers are common in all tables 
and figures. I = average I-type granite, S = average S-type granite from Taylor & McLennan (1985) 

LOC. 
No. In No. in 
Figs. 2-5 Fig. 1 S i 0 2  TiO, Al2O3 F e 2 0 3  FeO MnO MgO CaO N a 2 0  K,O P 2 0 s  ig. loss Total 

1 
2 
3 
4 
5 
6 
7 
8 
9 

10 
11 
12 
13 
14 
15 
16 
17 
18 
19 
20 
21 
I 
S 

1-3 60.40 1.00 13.66 0.97 
5-2 59.68 1.20 13.26 1.00 
8-1 60.64 0.93 13.52 0.65 

23-2 60.39 1.06 12.76 1.37 
5-1 61.55 0.95 12.40 1.02 
9-1 61.20 0.88. 14.67 0.89 

11-1 60.03 0.95 15.30 0.95 
8-2 62.42 0.68 13.74 1.90 
X-3 59.85 0.84 14.91 0.65 
1-1 69.13 0.40 14.12 0.32 

18-1 69.33 0.50 13.74 0.08 
19-1 71.01 0.40 13.68 0.22 
20-1 66.83 0.60 14.14 0.85 

1-2 68.94 0.50 12.83 0.72 
13-8 63.16 0.83 14.73 0.06 
15-1 64.62 0.65 15.64 0.70 
34-1 63.66 0.68 14.90 1.33 
28-2 63.49 0.68 14.84 1.12 

1-4 71.74 0.33 14.11 0.35 
23-3 76.96 0.11 13.07 0.10 

1-5 67.15 0.50 16.16 0.55 
69.17 0.43 14.33 - 
70.27 0.48 14.10 - 

4.08 0.13 5.02 4.30 2.17 
4.11 0.10 7.12 2.86 1.94 
4.29 0.10 4.41 3.72 2.37 
4.07 0.13 5.39 4.27 2.04 
3.60 0.08 4.21 3.72 2.45 
3.90 0.10 4.41 3.44 2.57 
4.11 0.10 4.51 3.29 2.13 
3.06 0.07 3.78 2.83 2.56 
5.11 0.11 4.04 3.81 2.56 
2.14 0.05 1.30 1.86 3.57 
3.03 0.05 1.41 2.15 3.47 
2.10 0.04 1.41 1.43 3.29 
2.70 0.07 2.41 2.58 2.71 
1.93 0.05 1.90 1.72 3.13 
3.54 0.06 3.21 3.01 3.45 
3.06 0.07 1.10 2.44 3.01 
2.81 0.08 2.80 3.23 2.96 
2.88 0.08 2.45 3.54 2.96 
1.89 0.03 0.80 1.43 2.97 
0.29 - - 0.62 3.22 
2.16 0.04 1.20 1.72 3.23 
3.23 0.07 1.40 3.20 3.13 
3.37 0.06 1.42 2.03 2.41 

6.47 0.37 
5 62 0.60 
6.64 0.47 
7.06 0.32 
7.11 0 4 5  
6.01 0.45 
6.22 0.46 
6.30 0.37 
5.81 0.38 
5.17 0.22 
4.88 0.26 
5.02 0.22 
5.46 0.35 
6.06 0.29 
5.34 0.41 
6.20 0.37 
5.72 0.28 
6.60 0.12 
5.00 0.16 
5.72 0.22 
5.60 0.22 
3.40 0.11 
3.96 0.15 

1.35 99.92 
2.41 99.90 
2.35 100.09 
1.26 100.12 
1.71 99.25 
1.54 100.06 
1.77 99.82 
2.09 99.86 
1.45 99.61 
1.67 99.95 
1.03 99.93 
1.23 100.05 
1.28 99.98 
1.65 99.72 
2.14 99.94 
1.91 99.77 
1.14 99.59 
1.06 99.86 
1.15 99.96 
0.42 100.53 
1.48 100.01 
- 98.47 
- 98.25 

Table 2. Trace element analyses. I and S: same as in Table 1. 

No. in No. in 
Figs. 2-5 Fig. 1 Li Rb Cs Sr Ba Sc Y Zr V Cr Co Ni Cu Ga 

1 
2 
3 
4 
5 
6 
7 

10 
11 
12 
13 
14 
15 
16 
17 
18 
19 
20 
21 
I 
S 

1-3 - 
5-2 33 
8-1 40 

5-1 23 
9-1 33 

11-1 41 
1-1 62 

18-1 - 
19-1 31 
20-1 48 

1-2 47 
13-8 18 
15-1 - 
34-1 - 
28-2 23 

1-4 - 
23-3 - 

1-5 - 

23-2 - 

- 

- 

- 

373 
289 

329 
278 
286 
335 

251 
324 
317 
262 

- 

- 

- 

- 
278 
- 

- 

- 

132 
- 

- 100 470 
7 520 1800 

15 500 1600 
- 200 800 

7 560 1300 
11 560 2000 
11 660 2200 
1s 350 700 
- 560 580 
11 440 900 
11 640 900 
13 390 800 
12 520 1200 
- 470 1400 
- 500 1500 
11 780 1800 
- 100 320 
- <loo <loo 
- 200 300 
- 253 520 
- 139 480 

13 21 
13 22 
10 20 
9 22 
9 22 

14 18 
13 22 
5 14 
5 14 
6 13 
8 19 
5 13 

10 18 
8 19 

10 12 
8 16 

14 10 
<5 <5 
<5 13 
15 27 
14 32 

560 
1100 
430 
720 
560 
300 
350 
190 
300 
190 
300 
190 
390 
300 
400 
400 
160 
82 

290 
143 
170 

74 
100 
82 
56 
74 
94 
82 
27 
32 
26 
54 
36 
64 
60 
70 
54 
25 
1 5  
26 
74 
72 

580 
360 
230 
530 
250 
200 
200 

, 72 
400 
63 

100 
96 

210 
170 
95 

100 
600 
160 
120 
27 
46 

18 
26 
18 
19 
19 
20 
20 

5 
12 
12 
12 
8 

14 
14 
14 
14 
5 

<5 
8 

12 
13 

280 
250 
66 

100 
100 
74 
80 
13 
34 
38 
40 
22 
68 
70 
34 
60 
24 

120 
50 
9 

17 

9 19 
31 15 
27 16 
19 15 
20 24 
22 17 
18 16 

<5 14 
5 9  

23 12 
10 10 
4 14 
<5 20 
12 22 
18 15 
19 14 
18 9 
8 11 

14 19 
11 16 
12 17 



Newtontoppen granitoid rocks, their geology, chemistry and Rb-Sr age 73 

granites, while it occurs as much as 2 modal % in 
the granosyenites. The phenocrystic K-feldspar 
contains inclusions of prismatic plagioclase grains, 
often showing granulated texture with overgrowth 
of sericite, biotite and hornblende. This suggests 
that a large part of the K-feldspar was formed 
after the inclusion minerals and the granulation 
of plagioclase. Albite usually rims the K-feldspar 
phenocrysts. 

Green hornblende shows prismatic and 
idiomorphic shapes, 0.5-2.5 mm in length, and 
rarely includes small grains of prismatic cli- 
nopyroxene. The clinopyroxene has optical par- 
ameters of the diopside-hedenbergite series. 
Brown biotite flakes, 0.5-1.5 mm in length, con- 
tain zircon and orthite. Conversion of the biotite 
into chlorite is not common. Accessories are 
idiomorphic sphene, often up to 1.5 mm in length, 
bipyramidal orthite with zonal structures and 
twins, zircon, monazite, apatite and opaques. 
Orthopyroxene, anatase and fluorite have been 
identified by the X-ray powder diffraction method 
in the heavy mineral fractions separated from 
twelve samples. Opaques are magnetite, hemat- 
ite, ilmenite, sphalerite and molybdenite. 

Granosyenite with aligned K-feldspar phenocrysts 

This granosyenite (sample no. 18 in Tables 1, 2 
and Figs. 2 - 4 )  exposes in the southeastern corner 
of the Newtontoppen granitoid body and cuts the 
pink-grey granosyenite at LOC. 28 (Fig. 1). The 
cross-cutting rock is characterised by subparallel 
alignment of long prismatic feldspars, 3-5 cm 
long. Total feldspars comprise ca. 80-90% of the 
rock. Phenocrystic K-feldspar is microperthitic, 
occupying ca. 50% of the rock. K-feldspar grains 
in the matrix are usually prismatic, 2-5 mm in 
length. Plagioclase grains are also prismatic, 0.5- 
1.0 mm long in the matrix, with compositions 
ranging from oligoclase to andesine, showing nor- 
mal zoning. Quartz and biotite occupy 5-10 and 
1-5 modal %, respectively, of the rock in the 
matrix. 

Aplitic veins 

Aplitic veins (sample nos. 19 and 20, in Tables 1, 
2 and Figs. 2-4), 40-50cm wide and as much 
as 1001-11 long cutting all previously described 
rocks, occur near the margins of the body. Most 
of them strike subparallel t o  the margins with 
various dips. 

The aplites are fine-grained, biotite-bearing 
rocks, having K-feldspar, plagioclase and quartz 
in roughly equal amounts in a hypidiomorphic 
texture. Biotite flakes comprise ca. 1-2 modal % 
and have a dark green colour. 

Pegmatites 

Pegmatite veins are rare, they are less than 50 cm 
in width and cut all previously described rocks. 
The pegmatites have muscovite-K-feldspar-bear- 
ing assemblages and some veins show zonal struc- 
tures constituting one or more of the following 
zones; muscovite-quartz-K-feldspar, rnuscovite- 
K-feldspar, quartz-K-feldspar and quartz mon- 
omineralic zones, from the margin to the core. 

Quartz-feldspar porphyry 

A dyke of this rock (sample no. 21 in Tables 1, 2 
and Figs. 2 4 ) ,  1-1.5 m thick and ca. 50 m long, 
occurs along a joint in the pink-grey granosyenite, 
with a NW-SE strike and a subvertical dip in the 
southeastern part of the body (LOC. 1, Fig. 1). 
The dyke is considered to be the latest intrusion. 
The rock is massive and has a fine-grained mic- 
rofelsic matrix of quartz and feldspars. Large 
flakes of biotite and phenocrysts of feldspars and 
quartz are characteristic. The biotite shows a dark 
green to almost black pleochroism. Quartz pheno- 
crysts show corroded outlines and rarely have an 
idiomorphic shape. K-feldspar is short prismatic 
in shape and albite forms small prismatic pheno- 
crysts aligned in a subparallel texture. 

Lamprophyre 

A lamprophyre dyke cuts the pink-grey grano- 
syenite at LOC. 27 (Fig. 1) in the southeastern part 
of the body. The rock has dark green to black 
colour and a fine-grained texture with ca. 20 
modal % of large flaky biotite. The matrix consists 
of talc and carbonate aggregates (some are prob- 
ably after olivine), zeolitized glass and small flakes 
of biotite. The mafic minerals occupy ca. 3C-40 
modal % of the rock and the rest is mainly dusty 
feldspars. Accessories are apatite and quartz. The 
modal and chemical compositions of the rock are 
that of a felsic monchiquite. This rock is similar 
to the Late Paleozoic lamprophyres from other 
parts of Svalbard, such as the monchiquite and 
comptonite from Krosspynten, on the western 
side of Austfjorden, a comptonite from inner 



74 A .  M .  Teben’kou et al. 

Wahlenbergfjorden, central Nordaustlandet 
(Lauritzen & Ohta 1984; Kovalyova & Teben’kov 
1986), and a lamprophyre on the southern side of 
Ragnarbreen, N E  Petuniabukta, recently found 
by the present authors. These rocks do not seem 
t o  be genetically related to the late Caledonian 
granitoid rocks, but are the members of the Late 
Paleozoic platform magmatic. activity. 

Sequence of emplacement 

The following successive emplacement stages 
have been deduced from the occurrence of the 
melanozomes and intrusive relationships among 
various types of rocks in the Newtontoppen grani- 
toid body: 

1. Incorporation of the melanozomes at depth, 
as inclusions in the dark grey granosyenites, 

2. Emplacement of the dark grey granos- 
yenites, 

3. Emplacement of the pink-grey granosy- 
enites, pink quartz monzonites and grey granites 
to form main part of the body, 

4. A small intrusion of the granosyenite with 
aligned K-feldspar phenocrysts in the south- 
eastern part of the body, 

5. Intrusion of aplites, pegmatites and quartz 
feldspar porphyry. 

Petrochemistry 
Major and trace element compositions of the 
Newtontoppen granitoid rocks are given in Tables 
1 and 2. 

Porphyritic and hypidiomorphic textures of the 
constituent minerals in all rocks indicate a mag- 
matic crystallisation process. The normative Q- 
Ab-Or diagram (Fig. 2) shows that the aplites, 
the grey granites and the quartz-feldspar porphyry 
plot near the eutectic valley of relatively high H 2 0  
pressure, while the melanozomes and dark-grey 
granosyenites have the highest O r  ratios, but with 
larger amounts of mafic minerals than of common 
granites. All other rocks plot between these two 
groups of rock types. 

The ACF ratios (not shown in this article) show 
that two aplites and a quartz-feldspar porphyry 
plot in the muscovite-biotite plagioclase field, 
while all other rocks are in the biotite-hornblende- 
plagioclase field, conformable with the observed 
assemblages. 

The present rocks are projected in a field of 
slightly lower total iron than common calc-alka- 
line rocks (Ringwood 1974) on the AFM diagram 
(Fig. 3). The alkali-lime index is difficult to esti- 
mate, due to a flat trend of the total alkalis, but 
it is estimated t o  be between 56 and 47, which is 
in the alkali-calcic to alkalic rock series (Fig. 4). 
The roughly constant amount of total alkalis in 
the whole range of SiOz is remarkable, unlike a 
positive trend normal for magmatic rocks. Four 
grey granosyenites, three melanozome-dark grey 
granosyenites and the granosyenite with aligned 
K-feldspar are just in the alkalic rock field (Irvine 
& Baragar 1971), while the rest are in the sub- 
alkalic field (Fig. 4). 

O n  the cation oxides vs. S i 0 2  diagrams, FeO* 
(= total FeO), MgO and N a 2 0  (Fig. 5) and CaO 
(Fig. 4) show smooth curves in the range of SiOz 
more than 63 wt 70 and these indicate a series of 
magmatic crystallisation. The same oxides show 
consistent trend, but have some deviations in the 
rocks with SiOz less than 63 wt %; these rocks 
are melanozomes, dark-grey granosyenites and 
grey granosyenites. These deviations are due to 
mafic components and seem t o  reflect initial dif- 
ferences of protolith compositions or different 
temperatures of anatectic melting at depth. These 
rocks plot away from the eutectic valley in Fig. 2. 
Very large deviations of A1203 and K 2 0  in the 
low SiO, range reflect modal differences of K- 
feldspar and biotite. The K 2 0  contents are anom- 
alously high in the rocks with SiOz less than 65% 
and this can be explained by later K-feldspar 
addition t o  the rocks formed in an earlier stage, 
as mentioned in the petrography. Conversion of 
the mafic minerals into chlorite is rare, indicating 
a less hydrous condition during the later stages of 
the consolidation. According t o  Hjelle (1966), 
the K-feldspar phenocrysts from these granitoids 
have 20-26 mole % of A b  contents, including 
exsolved perthites, but excluding inclusions. This 
indicates that the K-feldspar crystallisation 
occurred at not as low a temperature as the hydro- 
thermal stage. 

The Newtontoppen granitoid rocks are not the 
M-type on the K 2 0 - N a 2 0 - C a 0  diagram (not 
shown in this article, White 1979; Pitcher 1979, 
1983a, 1983b; Whalen 1985), and not the A-type 
on the CaO + MgO/total FeO vs. SiOz and the 
G a  vs. A1203 diagrams (not shown, Whalen et al. 
1982; Collins et al. 1982). Then, the rocks were 
examined on the NazO vs. K 2 0  diagram (Fig. 
6) which shows that all melanozomes, dark-grey 



Newtontoppen grunitoid rocks, their geology, chemistry and Rb-Sr age 75 

1 6 .  

1 4 .  

13' 

12 

'19 
7 %16 

j 5 - 2  06 ' p 1 7  A1203 
15 13 10 
8 + 4. 0 2 0  

11+ + 
2 i 3  12 

218 + 
14 A 

A5 
, 

FeO* 

2 

L ,  El 

*A 0 i 
Aol 

Na2O 
0 3 .  0 

Fig. 5. Cation oxides vs. S i 0 2  diagrams, in weight percent 

granosyenites and grey granosyenites are of the 
S-type, while the other rocks plot around the 
boundary between the S- and I-type (Chappel & 
White 1974; White & Chappel 1977, 1983). The 

R 
Y 

6 .  

51 

oj+ + 
I 
I 

I 
1 . .  . i .  . . 
1 2 3 4 

Nan0 
Fig. 6. K 2 0 - N a 2 0  diagram, in weight percent. The S -  and I- 
type division: White & Chappel (1977). 

majority of the grey granites plot in the I-type 
field. Normative corundum values are higher than 
1 in the aplites and the quartz-feldspar porphyry, 
while four granites and pink granosyenites have 
normative corundum less than 1 and fourteen 
others have 0. This also shows that the majority 
of the rocks are around the boundary composition 
between the two granite types (White & Chappel 
1983). The S-type nature of the melanozomes, 
dark grey granosyenites and grey granosyenites 
suggests an anatectic origin. Their higher modal 
mafic constituents and occurrence of clino- 
pyroxene in these rocks infer contamination from 
residual materials of the partial melting. The 
other rocks are the products of fractional crys- 
tallisation of the anatectic magma, the process of 
which was terminated around the eutectic valley 
to form the granites, aplites, and quartz-feldspar 
porphyry, thus they show I-type chemical natures. 
The existence of hornblende and the lack of mus- 
covite, except for secondary sericite and those in 
the aplites and pegmatites, suggest that most of 
the rocks belong to the magnetite series of Ishi- 
hara (1977). 

The analysed trace elements (Table 2) are nor- 
malised to the average I-type granite (Taylor & 
McLennan 1985) in spider diagrams (Figs. 7A, 
7B and 7C). These diagrams show that the present 
granitoid rocks are evidently different from I-type 
granites and have similar patterns to the average 
S-type granite (Taylor & McLennan 1985), with 
more pronounced characteristics of high Zr, Cr 
and Ni, and low Y ,  Ti and V. Large deviations of 
alkali and alkali-earth trace elements reflect the 
modal difference of feldspars. High concen- 



76 A .  M .  Teben'kov et al. 

800 

k 500 
n 

cij 300 

200 

trations of Cr and Ni infer that their protoliths 
may have some basic components and that the 
supposed anatectic melting occurred at a rela- 
tively high temperature. This is conformable with 
relatively high MgO contents in the melanozomes 
and dark grey granosyenites (Fig. S ) ,  which may 
contain some residuals of inferred partial melting, 
e.g. clinopyroxene. Blank tests of the Cr and 
Ni analyses to check the contamination during 
preparation of samples have not been performed; 
however, the same laboratory procedures have 
been applied for many samples from various 
localities without any recognisable contami- 
nation. 

Two groups are recognisable on the Y-MgO 

A 
0 

c 
+ x+ Ycx. f 

+ +  + 
- 

0 A 

+ x  
a 

+ 
X 

Ae A A  
A 

A 

1 2 3 4 5 6 7  
MgO w t  % 1 

Fig. 7. Spider diagrams of the trace elements, normalised to the 
average I-type granite (Taylor & McLennan 1985). Average S -  
type granite (Taylor & McLennan 1985) is shown by the dotted 
line in all three diagrams. 
A. Between solid lines: melanozomes and dark grey grano- 
syenites (5 samples); broken lines: pink-grey granosyenites (2 
samples). 
B. Between solid lines: grey granites (4 samples); broken lines: 
aplites (2 samples). 
C. Between solid lines: pink quartz monzonites (4 samples); 
broken line: granosyenite with aligned K-feldspar; chained line: 
quartz-feldspar porphyry. 

3000 

2000' A 'AA 

1000 - 

B 

X 

+ +  + +A + k 500 A 
d 300 0 0  

~ 

P 

2ool 

A 
1 2 3 4 100 " . @ ' 

CaO wt % 

Fig. 8. Some trace and major element ratios. Symbols are the 
same as Fig. 2. A .  Y-MgO diagram. B. Ba-CaO diagram. C. 
Sr-CaO diagram. 



Newtontoppen granitoid rocks, their geology, chemistry and Rb-Sr age 77 

diagram (Fig. 8A). One is a very weak positive 
relation of Y with MgO in the high MgO range, 
which corresponds to the low SiO? range of Fig. 
5. The other group is in the low MgO range and 
shows large deviations without any recognisable 
trend. As these elements are mostly in the mafic 
constituents, this reflects the difference of modal 
mafic minerals which, in turn, depends on the 
amount of K-feldspar. In the present samples, 
rocks with large amounts of feldspar have small 
amounts of mafic. Y-Ti02, Cr and Ni vs MgO 
(not shown) show similar groups as the Y-MgO 
diagram. 

Two similar trends can be seen in the Ba and 
Sr vs. CaO diagrams (Figs. 8B and 8C). Negative 
relations in the high CaO range are shown by the 
melanozomes, dark-grey granosyenites, while the 
pink-grey granosyenites in these diagrams and the 
other rocks show positive trends. The positive 
trends are caused by a decrease of plagioclase 
during crystallisation fractionation, while the 
negative trends in the high CaO range show no 
relation with the magmatic process. 

O n  the Zr-MgO and Sc-Ti02 diagrams (not 
shown in this article), the two groups are also 
recognised; the melanozomes, dark-grey grano- 
syenites and the pink-grey granosyenites in the 
high MgO and high T i 0 2  fields, and the rest of 
the rocks in the low fields. Both groups have 
positive relations in these diagrams, but with dif- 
ferent ratios. 

These two groups roughly coincide with those 
showing different degrees of deviation in the 
A1203 and KzO variation diagrams (Fig. 5) and 
represent the different formation processes; an 
anatectic partial melting containing some pro- 
tolith residuals in the early stage, e.g. with less 
than 63% S i 0 2 ,  and an eutectic crystallisation in 
the later stage. 

Isotopic age determination 
Previous dating 

All three granitoid bodies of the Chydeniusbreen 
granitoid suite intrude within the Lomfjorden 
Supergroup producing thermal aureoles, and the 
Raudberget granitoid is covered unconformably 
by Carboniferous strata. The rocks have not suf- 
fered any orogenic deformation; they are there- 
fore later than the major Caledonian orogenic 
events which probably ended in the late Silurian 

(Gee & Page 1994). The K-Ar whole rock and 
Rb-Sr biotite ages, ca. 400 Ma, (Hamilton et al. 
1962) suggest cooling in Early Devonian time. 

A new Rb-Sr whole rock-apatite isochron 
dating, using 15 samples and an U-Pb zircon 
dating with four samples has been attempted. 

Rb-Sr dating 

Analytical procedure. - Thirteen whole rocks and 
two apatites were analysed for their Rb and Sr 
contents and Sr isotope compositions. The 
samples were dissolved in H F  and HC104 and the 
residue was dissolved in HCI and put in a column 
with resin Dowex 50 x 3 (200-400 mesh). Rb and 
Sr contents were determined by isotope dilution 
and mass-spectrometry. All isotope compositions 
were measured with the MI 1201-T mass-spec- 
trometer at the Geochemical Laboratory of the 
Kola Science Centre at Apatity, Russia. The Rb 
and Sr blanks are 2 ng and 8 ng, respectively. The 
uncertainty of the 87Rb/s6Sr ratio is assumed to 
be 1.5% and that of the s7Sr/86Sr to be 0.04%. 
The age calculation has been carried out after the 
program of Ludwig (1991). 

Results and interpretation. -The results of R b  and 
Sr isotope analyses are given in Table 3 and shown 
in Fig. 9. The best-fit line includes seven samples: 
one apatite (28-2-ap, which has a smaller "Rb/ 
s6Sr ratio than 13-8-ap), two aplites, two grano- 
syenites with aligned K-feldspar phenocrysts, one 
quartz monzonite and one melanozome. These 
make a seven-point isochron (MSDW = 2.59) 
which yields 432 2 lOMa, with a high 87Sr/86Sr 
initial ratio, 0.715 4 3, indicating a crustal origin 
of the rocks. Seven other samples (two quartz 
monzonites, a melanozome, a pink-grey grano- 
syenite, a granosyenite with aligned K-feldspar, 
a quartz porphyry and an apatite; 13-8-ap) are 
scattered above and one quartz monzonite below 
the isochron. No special reason for the deviation 
has been found, but it may be due to the het- 
erogeneity of these rocks. The obtained age is 
considered as the crystallisation age of the grani- 
toid rocks. This age is ca. 30 Ma older than the 
previously reported K-Ar whole rock and Rb-Sr 
biotite ages (Hamilton et al. 1962) which show 
the cooling time. 

The T(DM) calculated after the model-1 of Bal- 
aSov et al. (1992), with the parameters of present 
day s7Rb/86Sr = 0.062576 and 87Sr/86Sr = 0.7032 
of the E(enriched)-type, using the average of the 



78 A .  M. Teben'kou et al. 

0.058- 

n 
n 
In 

0.062 

0.054 

Table 3. Rb and Sr isotope analyses. The first numbers in the 
first column are the locality nos. in Fig. 1. Rb and Sr of the 
apatites were not measured. 

Loc. N o .  Kb ppm Sr ppm 87Rb/86Sr 87Sr/a6Sr 

360 

1-1 141.3 
1-2 318.4 
1-5 299.8 
5-1 342.8 
8-1 310.9 
9-1 276.3 

13-8 249.7 
15-1 312.0 
19-1 261.6 
20- 1 323.4 
23-3 306.0 
28-2 257.3 
34-1 253.9 
13-8-ap 
28-2-ap 

405.5 
449.4 
312.6 
678.8 
532.9 
752.0 
546.1 
476.1 
346.6 
520.8 
76.4 

696.5 
637.9 

1.154 
1.850 
2.482 
1.232 
1.590 
1.060 
1.386 
1.977 
2.236 
1.839 

11.590 
1.067 
1.042 
0.015 
0.005 

0.7309 
0.7278 
0.7320 
0.7256 
0.7255 
0.7232 
0.7238 
0.7278 
0.7277 
0.7266 
0.7867 
0.7216 
0.7223 
0.7165 
0.7155 

seven data points of the isochron, yielded a late 
Mesoproterozoic source age of ca. 1050 Ma. T(uR) 
calculation after McCulloch & Chappell (1982), 
using the parameters of present day 87Rb/86Sr = 
0.0827 and 87Sr/86Sr = 0.7045, gave an age of 
ca. 730 Ma. These may suggest a Grenvillian pro- 
tolith, derived from a mantle source, which would 
be the first indication of the Grenvillian event in 
Ny Friesland. However, these model ages could 
also be the results of mixing of older crustal rocks 
and juvenile mantle materials. 

U-Pb Zircon dating 

U-Pb isotopic data of zircon were obtained from 
four samples by conventional dissolution method 
(Table 4). The analytical method is the same as 
that described in Barashov et al. (1993). The 
isotopic results are strongly scattered and do not 
fit any single discordia. However, sample 13-8 
plots near the concordia at around 420 Ma (Fig. 
10 and Table 4), which is conformable with the 
Rb-Sr age. 

Conclusions 
New names for the Chydeniusbreen granitoid 
suite and its three separate bodies are introduced, 
based on recent mapping. The granitoid rocks 
intruded into the metasediments of the Lomfjor- 
den Supergroup, causing thermal effects, and are 
covered unconformably by Carboniferous sedi- 

I '  I '  I 

432 + I-1 0 Ma 
MSWD = 2.59 
ISr87186 = 0.71 5 + 1-3 
T(DM) = 1,056 Ma 

0 2 4 6 8 1 0 1 2  
87RbI86Sr 

0.70 

R g .  9. Rb-Sr isotope ratios. The first numbers: locality numbers 
shown in Fig. 1. -ap = apatite; open square = included in the 
best-fit line; cross = excluded. 

1 0.074 
0.070 

2 
R 0.066 . 

207pb / 235u 

Fig. 10. U-Pb isotope ratios. The first numbers are locality 
numbers shown in Fig. 1. 

ments. The shape of the Newtontoppen granitoid 
body is suggested to be an asymmetric lopolith or 
a harpolith-like body. The three bodies are 
located near the boundaries of different litho- 
logies in the surrounding metasediment 
successions, suggesting some structural control on 
their emplacement positions. 

The rocks of the Newtontoppen granitoids are 
mainly granite and granosyenite in composition 
and have the chemical characteristics of the alkali- 
calcic t o  alkalic series. They have transitional 
chemical characteristics between S- and I-type. 
Magmatic crystallisation is clear from their 



Newtontoppen granitoid rocks, their geology, chemistry und Rb-Sr age 79 

textures, and the granites and aplitic dyke rocks 
have near eutectic compositions. The variation of 
SiOz-rich lithologies resulted from the magmatic 
differentiation of anatectic melts. Later K-feld- 
spar introduction modified the rocks formed in 
earlier stages. The rocks with SiOz less than 63 
wt % ; the melanozomes, dark-grey granosyenites 
and grey granosyenites, have relatively large vari- 
ations in major cation oxides and trace element 
contents and are considered t o  be anatectic prod- 
ucts from various protoliths under relatively high 
temperature conditions. 

A new age determination by the Rb-Sr whole 
rock-apatite isochron method gives an Early Sil- 
urian (Tucker & McKerrow 1995) age of 
432 2 lOMa, ca. 30Ma older than the previous 
K-Ar whole rock and Rb-Sr biotite ages. The 
difference of these two ages may be considered 
as the cooling period of the body. This age is 
within the error range of that of the Hor- 
nemantoppen granite, the largest Caledonian 
granite body in northwestern Spitsbergen, 
414 2 10 Ma Rb-Sr whole rock (Hjelle 1979). The 
high s7Sr/86Sr initial ratio, 0.715, supports a cru- 
stal anatectic origin of the granitoid rocks. One 
of the U-Pb analyses suggest a similar age to the 
Rb-Sr age. 

Acknowledgements. - The authors are grateful t o  A. McCann 
for improvement of the language. Many constructive comments 
by two anonymous referees are very much appreciated. 

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