# Geochemistry of the Neoarchaean Volcanic Rocks of the Kilimafedha Greenstone Belt, Northeastern Tanzania

Authors: Charles W. Messo; Shukrani Manya; Makenya A. H. Maboko
Journal: Journal of Geological Research
 (2012)

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## Abstract

The Neoarchaean volcanic rocks of the Kilimafedha greenstone belt consist of three petrological types that are closely associated in space and time: the predominant intermediate volcanic rocks with intermediate calc-alkaline to tholeiitic affinities, the volumetrically minor tholeiitic basalts, and rhyolites. The tholeiitic basalts are characterized by slightly depleted LREE to nearly flat REE patterns with no Eu anomalies but have negative anomalies of Nb. The intermediate volcanic rocks exhibit very coherent, fractionated REE patterns, slightly negative to absent Eu anomalies, depletion in Nb, Ta, and Ti in multielement spidergrams, and enrichment of HFSE relative to MORB. Compared to the other two suites, the rhyolites are characterized by low concentrations of TiO2 and overall low abundances of total REE, as well as large negative Ti, Sr, and Eu anomalies. The three suites have a εNd (2.7 Ga) values in the range of  −0.51 to +5.17. The geochemical features of the tholeiitic basalts are interpreted in terms of derivation from higher degrees of partial melting of a peridotite mantle wedge that has been variably metasomatized by aqueous fluids derived from dehydration of the subducting slab. The rocks showing intermediate affinities are interpreted to have been formed as differentiates of a primary magma formed later by lower degrees of partial melting of a garnet free mantle wedge that was strongly metasomatized by both fluid and melt derived from the subducting oceanic slab. The rhyolites are best interpreted as having been formed by shallow level fractional crystallization of the intermediate volcanic rocks involving plagioclase and Ti-rich phases like ilmenite and magnetite as well as REE-rich phases like apatite, zircon, monazite, and allanite. The close spatial association of the three petrological types in the Kilimafedha greenstone belt is interpreted as reflecting their formation in an evolving late Archaean island arc.


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## Body

## 1. Introduction

The Kilimafedha greenstone belt of northeast Tanzania is one of the six greenstone belts of the Tanzania Craton occurring in the northern part of the country in the area south and east of the Lake Victoria. Other greenstone belts include the Sukumaland, Shinyanga-Malita, Nzega, Musoma-Mara, and Iramba-Sekenke [1, Figure 1]. All of these greenstone belts are prospective for gold mineralization with several large-scale mines now in operation including the Bulyanhulu, Tulawaka, Geita, Buzwagi, North Mara, and Golden Pride (Figure 1). Because of their economic significance, the greenstone belts of the Tanzania Craton have recently been the focus of research on the processes that control gold mineralization (e.g., [2, 3]), lithostratigraphical relationships (e.g., [4, 5]), geochemistry, and geochronology (e.g., [6–12]). These studies have helped us to better understand, among other things, the timing of and the processes responsible for the formation of the earliest continental crust in Tanzania as well as the ancient tectonic settings in which the greenstone belts formed.Figure 1
Geological map of the northern part of the Tanzania Craton showing the greenstone belts in the area around Lake Victoria (modified after [13]). The inset frame indicates the area of study in Figure 2.Previous geological work in the Kilimafedha greenstone belt is limited to the geological mapping done by Macfarlane [14] and more recently to geochronological investigation by Wirth et al. [9] who reported zircon Pb-Pb ages from rhyolites and granitic intrusions in the area. In this paper, we present whole-rock major and trace element as well as the Nd-isotopic compositions for the volcanic rocks of the Kilimafedha greenstone belt around the Ikoma area with the aim of unraveling their petrogenesis and tectonic setting of eruption. The results of this study complement the information available from other greenstone belts of the Tanzania Craton on the processes that led to the growth of the continental crust during the late Archaean.


## 2. Geological Setting

The Tanzania Craton forms the central nucleus of Tanzania and extends northwards into southwestern Kenya and southeastern Uganda. The Craton is divided into two main lithological units: the Dodoman belt which is comprised of high-grade metamorphic rocks, granite, granitic gneisses, and migmatites of central Tanzania and the low-grade granite-greenstone terrane of northern Tanzania, southwestern Kenya, and southwestern Uganda [15]. The low-grade granite-greenstone terrane comprises mafic to felsic volcanic rocks and metasedimentary rocks including shales, sandstones, siltstones, chert, and banded iron formation (BIF) which are in turn intruded by granites.Robust geochronological data shows that the oldest greenstones in the Tanzania Craton are the mafic volcanic rocks of the Rwamagana area in the Sukumaland greenstone belt (Figure1). These yielded a Sm-Nd isochron age of 2823 ± 44 Ma reported by Manya and Maboko [7]. The youngest volcanism in the greenstone belts of the Tanzania Craton is from the Musoma-Mara greenstone belt reported by Manya et al. [10] as indicated by a zircon U-Pb age of 2667 ± 8 Ma obtained from dacites collected near Tarime (Figure 1). A more thorough review of the geochronology of the greenstones and intruding granites of the Tanzania Craton can be found in Borg and Krogh [6] and Manya et al. [10].The Kilimafedha greenstone belt forms an asymmetrical horseshoe-shaped exposure of metavolcanic and minor metasedimentary rocks in the area east and southeast of Lake Victoria (Figure2). Most of the greenstone exposures including the old Kilimafedha mining district lie within the Serengeti National park. The samples collected for this study, however, were sampled outside the National park boundary in the Ikoma area (Figure 2). According to Macfarlane [14], the greenstone sequences start with a poorly preserved mafic volcanic unit now converted into actinolite and hornblende schist (Figure 3) in the extreme southeastern and northern margins of the belt (within the Serengeti National Park boundary), and the rocks are thus metamorphosed into greenschist facies except for the hornblende schists that are proximal to granitic  intrusions. This unit has locally been found to be pillowed suggesting extrusion of the lavas under water.Figure 2
Geological map of the Kilimafedha greenstone belt showing sample locations (modified after [14]).Figure 3
Diagrammatic representation of the stratigraphic sequence of Kilimafedha greenstone belt, not to scale (modified after [14]).The mafic volcanic rocks are overlain by a more extensive and better preserved thick sequence of intermediate volcanic rocks with infrequent felsic volcanic rocks patched in the intermediate rocks (Figure3). This sequence locally contains thin horizons of tuff and metasediments including chert, jaspilite, and quartzite. The felsic volcanic rocks were dated by Wirth et al. [9] who reported 207Pb/206Pb zircon ages of 2712 ± 5 Ma (MSWD = 0.35) and 2720 ± 5 Ma (MSWD = 1.9).More fresh exposures of the greenstone sequence occur in the area near Fort Ikoma (Figure2) close to the northern boundary of the greenstone belt. In this area, the most common rock types include amygdaloidal andesite with streams of vesicles filled up with quartz, epidote, and chlorite (Figure 4). Other less vesicular types have large phenocrysts of albite-oligoclase. Sediments intercalated with metavolcanics are largely metamorphosed ferruginous quartzite, siltstones, mudstones, and felsic tuffs.Outcrop photographs showing Ikoma foliated metabasalts with an appearance of a schist (a) and amygdaloidal andesite with vesicles filled in with secondary quartz (b).
(a)
(b)The whole sequence has been deformed resulting into the development of a steeply dipping N to NW trending foliation. Folding is indicated by isoclinal contortions in the ferruginous quartzite [14]. Late orogenic granites outcrop along the eastern, northern, and southwestern margins of the greenstone belt. The granite-greenstone contact along the northern margin has been decorated with minor metagabbroic intrusions that have been correlated with the larger Nyamongo gabbros of the Musoma-Mara greenstone belt [16]. Neoproterozoic arenaceous to argillaceous sedimentary rocks of the Ikorongo Group [17] unconformably overlie all the Archaean rocks in the area.


## 3. Sampling and Analytical Methodology

Samples were obtained from surface outcrops, and sampling was dictated by the degree of accessibility, exposure, and freshness of the outcrops. Fifty volcanic rocks samples were collected in the field and were subsequently prepared for laboratory chemical analyses. All 50 samples were analyzed for major element compositions, but only 18 representative samples from distinguished suites were analyzed for trace element compositions (see Figure2 for sample locations). For chemical analyses, the samples were pulverized in an agate mill at the Southern and Eastern Africa Mineral Centre (SEAMIC) Laboratories, Dar es Salaam. Samples were first dried in an oven at 110°C, and 1 g of the powdered sample was mixed with 7 g of lithium metaborate and fused in a furnace at 1000°C for about 10 minutes to make glass beads. The glass beads were analyzed using an SRS 3000 Siemens X-ray Fluorescence Spectrometer at the same laboratories following procedures reported in Messo [18]. Loss on ignition (LOI) was determined by repeatedly heating the samples in a furnace at 1010°C and cooling until constant weight was achieved.The samples were also analyzed for trace elements at the Activation Laboratories of Ancaster, Ontario, Canada. 0.25 g of each sample was mixed with a flux of lithium metaborate and lithium tetraborate and fused in an induction furnace. The melt was immediately poured into a solution of 5% HNO3 containing an internal In standard and thoroughly mixed for ~30 minutes to achieve complete dissolution. An aliquot of the sample solution was spiked with internal In and Rh standards to cover the entire mass range and diluted 6000 times prior to introduction into a Perkin Elmer SCIEX ELAN 6000 ICP-MS for trace elements analysis. Precision and accuracy as deduced from replicate analyses of the BIR-1 and W2 standards are 5–10%. The analytical reproducibility deduced from replicate analyses of the samples is better than 8% for most trace elements.Nine samples were also analysed for Sm-Nd isotopic compositions as well as Sm and Nd concentrations using a Triton-MC Thermal Ionization Mass Spectrometer at the Activation Laboratories of Ontario, Canada. Aliquots of the powdered rock samples were spiked with a149Sm-146Nd mixed solution prior to decomposition using a mixture of HF, HNO3, and HClO4. The REEs were separated using conventional cation-exchange techniques. Sm and Nd were separated by extraction chromatography on HDEHP covered teflon powder. Total blanks are 0.1-0.2 ng for Sm and 0.1–0.5 ng for Nd and are negligible. The accuracy of the Sm and Nd analyses is ±0.5% corresponding to errors in the 147Sm/144Nd ratios of ±0.5% (2σ). The 143Nd/144Nd ratios are calculated relative to the value of 0.511860 for the La Jolla standard. During the period of analysis, the weighted average of 10 La Jolla Nd-standard runs yielded 0.511872 ± 15 (2σ) for 143Nd/144Nd, using a 146Nd/144Nd value of 0.7219 for normalization.


## 4. Geochemistry

### 4.1. Alteration and Element Mobility

Alteration of metavolcanic rocks is a common phenomenon, in particular for Archaean greenstones, and is typically characterized by high loss on ignition (LOI) values and increased scatter of major and large ion lithophile elements. In this regard, the volcanic rocks, collected for this study, are variably affected by greenschist metamorphism, so it is expected that major and LILE are also affected by alteration. However, numerous studies have demonstrated that rare earth elements (REEs) and high field strength elements (HFSEs) remain relatively undisturbed at greenschist facies and even higher grades of metamorphism [19, 20]. So in this study major and LILE are used with great care, and emphasize is placed on the REE and HFSE.


### 4.2. Classification and Petrography

The volcanic rocks of the Kilimafedha greenstone belt represent a mafic, intermediate to felsic compositional continuum as indicated by their wide range of SiO2 contents (48.48–76.02 wt%). Out of a total of 50 samples that were analyzed for major elements and as shown in Figure 4 and 7 samples are basaltic in composition (SiO2 = 48.48–51.57 wt%), 40 samples show intermediate compositions ranging from basaltic andesites to basaltic trachyandesites, which are predominant; andesites to dacites (SiO2 = 52.51–66.80 wt%); only 3 samples are rhyolites (SiO2 = 75.52–76.02 wt%, values quoted on water free basis), revealing the sporadic nature of the more felsic rocks. The predominance of the basaltic trachyandesitic rocks and the nature of these rocks are unique to the Kilimafedha greenstone belt (Figure 5).Figure 5
TAS classification diagram of Le Maitre et al. [21] for the Kilimafedha volcanic rocks. Also shown in the diagram are fields for volcanic rocks from other greenstone belts of the Tanzania Craton: ISGB: Iramba—Sekenke greenstone belt, SGB: Sukumaland greenstone belt, SMMGB: Southern Musoma—Mara greenstone belt, and NMMGB: Northern Musoma—Mara greenstone belt.  Numbers in the diagram indicate fields as follows: 1: basalt, 2: basaltic andesite, 3: andesite, 4: dacite, 5: rhyolite, 6: trachybasalt, 7: basaltic trachyandesite, 8: trachyandesite, and 9: trachydacite.Using the Winchester and Floyd [22]  classification scheme which is suitable for classifying metamorphosed rocks, of the 18 samples that were analyzed for both major and trace elements, four samples plot along the boundary between subalkaline basalt and andesite/basalt, eleven others plot in the fields of andesite/basalt and andesites, and three samples plot as rhyolites (Figure 6). The basalts to andesitic basalts exhibit tholeiitic affinity, the intermediate rocks intermediate geochemical characteristics between tholeiitic and calc-alkaline affinities, whereas the rhyolites are calc-alkaline. Accordingly, the rocks are henceforth subdivided into three suites: the tholeiitic basalts, the intermediate volcanic rocks, and the rhyolites.Figure 6
Classification of the Kilimafedha volcanic rocks using the Nb/Y-Zr/Ti diagram of Winchester and Floyd [22]. Symbols are filled triangles: tholeiitic basalts, open squares: intermediate volcanic rocks, and open cycles: rhyolites.The primary petrographic features of the tholeiitic basalts are strongly obliterated by alteration which has resulted in the formation of chlorite, epidote, and hornblendic amphibole which appear to form after olivines and pyroxenes. The predominant intermediate rocks are often amygdaloidal, with streams of vesicles filled up with quartz, epidote, and chlorite. Other less vesicular types have large phenocrysts of albite-oligoclase. Most felsic rocks have fine matrix of quartz and sericitized feldspars with sparse phenocrysts of quartz and altered feldspars. The presence of chlorite and epidote in the Kilimafedha volcanic rocks suggests that these rocks have mainly been metamorphosed into greenschist facies.


### 4.3. Major and Trace Element Geochemistry

#### 4.3.1. Tholeiitic Basalts

Major and trace element composition of the tholeiitic basalts of the Kilimafedha greenstone belt are presented in Table1. The rocks have SiO2 compositions that are in the range of 48.48–51.57 wt%, TiO2 = 0.61–1.80 wt%, Fe2O3 = 6.32–13.92 wt%, MgO = 5.56–8.49 wt%, and Mg numbers, calculated as 100×Mg2+/(Mg2++Fetotal2+),  range from 47 to 73 (the major elements presented on a water free basis). Cr and Ni contents are 160–240 ppm and 90–190 ppm, respectively. La contents vary considerably (1.7–9.2 ppm), whereas Yb contents range from 1.7 to 3.1 ppm resulting in La/Yb ratios of 1.00–4.00 (Table 1). On major and trace element bivariate plots (Figure 7), Fe2O3, MgO, CaO, and Ni correlate negatively with SiO2 pointing to fractionation signature or cogenetic relationship. The tholeiitic basalts alone do not show any major trends most likely due to the small number of samples and their restricted range in SiO2 content.Table 1
Major (wt%) and trace (ppm) element composition for the Kilimafedha greenstone belt volcanic rocks.
Tholeiitic basalts
Transitional intermediate volcanic rocks
MU 14
MU 15
MU 19
MU 20
MU 43
MU 69
MU 109
MU 12
MU 13
MU 21
MU 27
MU 33
MU 35
MU 36
MU 37
MU 38
MU 39
MU 49
MU 54
MU 57
MU 60
MU 64
MU 65
MU 66
MU 68
SiO2
50.3
47.4
50.4
50.3
47.8
48.2
49.2
55.2
52.9
52.8
65.3
60.6
53.7
55.1
54.3
54.1
53.5
53.7
53.5
54.1
54.9
56.0
54.9
55.3
62.4
TiO2
1.36
0.92
0.60
0.66
1.73
1.75
0.62
1.53
1.44
0.84
0.58
0.67
1.45
1.46
1.36
1.54
1.60
1.46
1.26
1.35
1.38
0.91
1.24
1.41
0.84
Al2O3
14.7
16.0
14.4
13.5
14.6
14.1
17.3
13.1
15.1
15.0
15.5
16.5
14.0
13.4
14.1
14.3
14.9
14.2
13.7
13.2
13.5
14.7
14.3
13.6
14.2
Fe2O3
12.3
12.4
11.9
12.9
13.3
13.5
6.2
9.3
10.8
11.2
4.2
6.7
11.3
12.0
11.2
11.9
12.1
12.1
11.8
11.3
11.7
9.1
10.8
12.0
6.6
MnO
0.27
0.17
0.17
0.18
0.19
0.18
0.08
0.25
0.24
0.16
0.06
0.10
0.11
0.14
0.11
0.14
0.14
0.15
0.12
0.12
0.12
0.19
0.13
0.13
0.09
MgO
5.45
8.09
7.53
7.32
6.62
6.76
8.30
6.00
4.66
5.58
2.68
3.57
3.42
3.71
3.43
3.46
3.62
3.85
4.24
3.53
3.77
5.27
3.80
3.50
2.60
CaO
10.9
10.9
10.7
10.7
10.3
10.5
12.3
7.54
10.94
8.54
3.65
2.73
9.62
6.25
9.49
6.41
5.30
5.69
8.30
6.40
6.94
6.28
7.16
7.43
4.53
Na2O
2.29
1.84
1.92
1.79
1.96
1.91
2.99
5.14
2.49
1.74
4.91
6.15
3.12
4.96
2.70
4.02
5.00
5.34
2.67
4.69
3.10
3.85
3.01
3.94
4.20
K2O
0.52
0.17
0.15
0.11
0.03
0.10
0.81
0.79
0.27
1.45
0.83
0.31
1.44
1.09
1.43
1.88
1.77
1.34
2.09
1.44
2.75
0.37
2.20
0.73
1.50
P2O5
0.04
0.01
0.01
0.01
0.19
0.09
0.01
0.07
0.06
0.01
0.06
0.08
0.12
0.12
0.12
0.15
0.15
0.13
0.12
0.13
0.03
0.01
0.11
0.13
0.16
LOI
1.46
2.14
2.17
2.45
3.19
2.55
2.15
0.92
1.03
2.29
2.19
2.53
1.39
1.34
1.72
1.81
1.83
1.75
1.97
3.30
1.66
2.93
2.00
1.69
2.80
Total
99.5
100
99.9
100
99.9
99.8
99.9
99.9
99.9
99.6
100
100
99.7
99.6
99.9
99.7
99.9
99.6
99.8
99.5
99.8
99.7
99.6
99.8
100
Mg#
46.8
56.5
55.6
52.8
49.6
49.7
72.7
56.1
46.1
49.8
56.0
51.2
37.4
38.0
37.7
36.5
37.3
38.7
41.5
38.2
39.1
53.3
41.0
36.7
43.9
Ba
204
27
66
140
1230
418
329
97
763
755
Rb
26
9
5
5
16
35
40
2
97
18
Sr
147
106
101
214
428
236
239
293
320
423
Ni
100
190
90
120
30
80
90
60
90
30
Cr
160
200
240
170
30
40
70
40
90
20
V
342
228
232
249
76
171
154
162
153
108
Th
0.5
0.3
0.2
1
3.9
8
8.7
7
8.9
5.8
Pb
5
5
5
5
7
5
9
42
6
10
U
0.2
0.1
0.1
0.4
1.3
2.1
2.9
1.9
2.5
1.4
Nb
3
2
1
4
4
8
8
7
8
7
Ta
0.3
0.2
0.1
0.3
0.4
0.6
0.8
0.6
0.7
0.5
Zr
80
53
31
88
126
163
177
147
184
176
Hf
2.2
1.4
1
2.4
3.2
4.3
4.9
3.9
4.7
4.6
Y
29
20
16
23
15
23
24
21
24
24
La
4.60
3.00
1.70
9.20
22.1
26.2
28.1
23.8
28.2
33.7
Ce
12.4
8.2
4.6
21.6
42.2
53.5
60
49.4
59.9
69.3
Pr
1.96
1.27
0.75
3.05
4.99
6.46
7.74
6.21
7.49
9
Nd
6.58
6.70
4.10
17.82
17.9
24.4
28.1
22.9
28.5
31.6
Sm
1.63
2.1
1.3
6.1
3.5
5.7
6.4
5.4
6.2
6.5
Eu
1.11
0.84
0.57
1.36
1.06
1.37
1.66
1.68
1.65
1.62
Gd
4.3
3.0
2.0
4.1
3.3
5.7
5.8
4.8
6.1
5.3
Tb
0.8
0.5
0.4
0.7
0.5
0.8
0.9
0.8
0.9
0.8
Dy
5.0
3.4
2.5
4.0
2.6
4.7
4.7
4.0
4.8
4.2
Ho
1.1
0.7
0.6
0.8
0.5
0.9
0.9
0.8
0.9
0.8
Er
3.3
2.1
1.7
2.4
1.5
2.4
2.5
2.1
2.5
2.5
Tm
0.48
0.32
0.26
0.36
0.22
0.34
0.35
0.29
0.34
0.37
Yb
3.10
2.10
1.70
2.30
1.40
2.10
2.20
1.80
2.10
2.30
Lu
0.46
0.31
0.26
0.35
0.22
0.31
0.31
0.26
0.3
0.34
La/Yb
1.5
1.4
1.0
4.0
15.8
12.5
12.8
13.2
13.4
14.7
La/Nb
1.53
1.5
1.7
2.3
5.53
3.28
3.51
3.40
3.53
4.81
Eu/Eu*
0.90
1.02
1.08
1.10
0.95
0.74
0.83
1.01
0.82
0.84
La/SmCN
0.90
0.92
0.84
1.70
4.08
2.97
2.83
2.85
2.94
3.35
La/YbCN
1.06
1.02
0.72
2.87
11.3
8.95
9.16
9.48
9.63
10.5
Nb/Lapm
0.63
0.64
0.57
0.42
0.17
0.29
0.27
0.28
0.27
0.20
Transitional intermediate volcanic rocks
Rhyolites
MU 76
MU 77
MU 78
MU 79
MU 80
MU 81
MU 82
MU 83
MU 84
MU 85
MU 86
MU 87
MU 89
MU 90
MU 91
MU 92
MU 93
MU 94
MU 95
MU 96
MU 97
MU 100
MU 16
MU 17
MU 18
SiO2
51.9
51.9
53.2
52.4
53.1
53.3
54.3
53.5
52.2
54.3
55.1
54.3
55.6
55.8
52.8
51.3
52.6
54.9
54.2
53.7
55.4
52.3
74.9
75.5
75.3
TiO2
1.42
1.38
1.34
1.37
1.49
1.49
0.70
1.51
1.62
1.25
1.35
1.41
1.41
1.43
1.52
0.84
1.20
1.37
1.41
1.09
1.07
1.42
0.03
0.03
0.03
Al2O3
14.7
14.2
14.1
14.4
14.2
13.9
15.1
14.0
14.7
13.5
14.4
13.8
13.6
13.4
14.4
14.1
14.2
14.6
14.2
15.1
14.2
15.6
14.28
14.38
14.46
Fe2O3
12.4
12.6
12.2
12.4
12.5
12.6
8.2
12.4
13.0
11.3
11.3
12.2
11.8
11.4
13.5
11.6
12.5
11.4
11.6
12.5
11.3
12.9
0.34
0.28
0.34
MnO
0.14
0.14
0.14
0.14
0.14
0.14
0.13
0.14
0.14
0.13
0.14
0.13
0.13
0.12
0.16
0.15
0.19
0.13
0.14
0.15
0.17
0.15
0.02
0.01
0.01
MgO
4.40
4.20
4.04
4.10
3.88
3.92
6.47
3.86
3.89
4.44
3.60
3.68
3.72
3.55
3.82
7.08
4.89
3.66
4.10
4.56
4.26
3.64
0.23
0.22
0.25
CaO
7.36
7.97
8.36
8.38
6.74
7.00
8.87
6.82
6.01
7.40
6.36
7.03
6.39
7.13
6.32
9.37
5.66
5.84
5.56
5.28
5.40
5.97
0.26
0.10
0.15
Na2O
3.66
2.83
2.88
2.87
4.32
3.92
3.14
4.20
4.63
2.91
5.57
3.79
3.73
3.62
4.63
2.41
4.53
4.55
4.00
4.91
5.04
4.75
5.14
5.17
5.32
K2O
1.25
1.91
1.48
1.67
1.60
1.52
0.57
1.57
1.79
2.89
1.27
1.47
1.91
0.15
0.95
0.88
2.06
1.66
2.57
1.77
1.62
1.16
3.98
3.61
3.41
P2O5
0.11
0.02
0.11
0.11
0.12
0.13
0.11
0.13
0.14
0.11
0.12
0.13
0.14
0.13
0.13
0.03
0.09
0.10
0.13
0.10
0.09
0.12
0.01
0.01
0.01
LOI
2.48
2.35
1.78
1.79
1.59
1.57
2.46
1.52
1.49
1.70
1.40
1.97
1.65
2.94
1.70
2.27
1.87
1.40
1.63
0.94
1.50
1.99
0.75
0.69
0.69
Total
99.8
99.5
99.6
99.7
99.7
99.6
100
99.6
99.6
99.9
101
99.9
100
99.6
100
100
99.8
99.6
99.5
100
100
100
100
100
100
Mg#
41.3
39.7
39.6
39.5
38.1
38.1
60.9
38.2
37.2
43.9
38.8
37.4
38.4
38.3
35.9
54.8
43.6
38.9
41.2
42.0
42.8
35.8
57.3
60.9
59.3
Ba
504
415
643
626
485
301
220
217
Rb
56
48
61
54
40
91
83
77
Sr
349
398
395
296
312
37
32
31
Ni
160
90
80
80
43
20
20
20
Cr
40
70
70
30
40
20
20
20
V
180
155
149
163
175
5
5
5
Th
7.8
8.9
8.8
7.2
7.5
3.1
2.9
2.7
Pb
5
14
18
5
5
9
5
5
U
2.2
2.5
3.1
2
2.2
2.5
2.1
2
Nb
7
9
8
6
7
5
5
4
Ta
0.6
0.7
0.8
0.6
0.6
0.6
0.6
0.6
Zr
158
179
173
137
155
34
36
33
Hf
4.3
4.6
4.9
3.7
4.1
1.9
2
1.9
Y
25
24
24
23
25
12
9
10
La
23.6
27.4
28.0
22.8
20.1
6.60
3.90
3.70
Ce
50.7
58.3
59.5
47.4
46.6
13.2
9.3
12.3
Pr
6.35
7.2
7.68
5.82
6.24
1.90
1.31
1.12
Nd
24.4
27.3
27.9
22.7
23.6
7.80
5.40
4.60
Sm
5.8
6.2
6.6
5.2
5.7
2.1
1.4
1.4
Eu
1.78
1.6
1.81
1.63
1.62
0.12
0.09
0.1
Gd
6.0
6.2
5.7
5.3
5.5
2.1
1.4
1.5
Tb
0.9
0.9
0.9
0.8
0.9
0.4
0.3
0.3
Dy
4.9
4.7
4.7
4.4
4.7
2.0
1.5
1.5
Ho
0.9
0.9
0.9
0.8
0.9
0.4
0.3
0.3
Er
2.6
2.4
2.5
2.3
2.6
1
0.8
0.9
Tm
0.36
0.34
0.36
0.32
0.36
0.15
0.13
0.14
Yb
2.20
2.00
2.20
2.00
2.20
0.90
0.80
0.90
Lu
0.32
0.3
0.31
0.3
0.33
0.13
0.12
0.12
La/Yb
10.7
13.7
12.7
11.4
9.1
7.3
4.9
4.1
La/Nb
3.37
3.04
3.50
3.80
2.87
1.32
0.78
0.925
Eu/Eu*
0.92
0.79
0.90
0.95
0.89
0.17
0.20
0.21
La/SmCN
2.63
2.85
2.74
2.83
2.28
2.03
1.80
1.71
La/YbCN
7.69
9.83
9.13
8.18
6.55
5.26
3.50
2.95
Nb/Lapm
0.29
0.32
0.28
0.25
0.34
0.73
1.24
1.04
Mg# (Magnesium number) = 100 ×Mg2+/(Mg2+ + Fetotal2+) as in Section 4.3.1, and Eu/Eu* = Eu/((SmN × GdN)1/2).Major and trace elements variation diagram for the Kilimafedha volcanic rocks. Symbols as in Figure6.
(a)
(b)
(c)
(d)
(e)
(f)
(g)
(h)
(i)The rocks display slightly depleted LREE to nearly flat REE patterns (Figure8(a)) that are characterized by La/SmCN and La/YbCN ratios of 0.8-0.9 and 0.72–1.06, respectively, except for sample MU 69 which is relatively enriched in LREE (La/SmCN = 1.7 and La/YbCN = 2.89) compared to the other three samples (where CN refers to chondrite normalized values). The La/SmCN and La/YbCN values of the three samples (MU 69 excluded) are slightly higher than those of NMORB (La/SmCN = 0.6, La/YbCN = 0.59; [23]) indicating relative enrichment of the LREE in the Kilimafedha tholeiites. The samples do not show any Eu anomalies (Eu/Eu* = 0.90–1.10). The samples were also plotted on primitive mantle spidergrams (Figure 9(a)), where they display enrichment in Rb, Ba,Th, K, and Pb relative to the more compatible elements with flatter  multielement  patterns characterized by negative Nb anomalies (Nb/Lapm = 0.42–0.64) and minor negative Ti anomalies (where pm refers to primitive mantle normalized values).Chondrite normalized REE diagrams for the Kilimafedha volcanic rocks normalizing values from Sun and McDonough [23]. (a) Tholeiitic basalts superimposed with NMORB, (b) intermediate volcanic rocks superimposed with adakites, and (c) rhyolites.
(a)
(b)
(c)Primitive mantle normalized diagrams for the Kilimafedha volcanic, normalizing values from Sun and McDonough [23]. (a) Tholeiitic basalts, (b) intermediate volcanic rocks, and (c) rhyolites.
(a)
(b)
(c)


#### 4.3.2. Intermediate Volcanic Rocks

The intermediate volcanic rocks have a wide range of SiO2 contents (52.51–66.80 wt%) spanning from basaltic andesites through basaltic trachyandesites and andesites to dacites. The compositions, however, are skewed to the basaltic andesitic compositions as indicated by the averages (SiO2 = 52.51–66.80 wt%, average = 55.67 wt%, n=40, Table 1, Figures 5 and 6), and only 5 samples have SiO2 > 57 wt%. TiO2 contents are 0.59–1.65 wt%, Fe2O3 = 4.26–13.78 wt%, MgO = 2.68–7.25 wt%, and Mg numbers range from 36 to 61. Cr and Ni contents are 20–90 ppm and 30–160 ppm, respectively. La varies from 20.1–33.7 ppm and Yb from 1.4–2.3 ppm which results in La/Yb ratios of 9.14–15.8.The intermediate volcanic rocks display fractionated REE patterns (Figure8(b)) and in comparison with the tholeiitic basalts are characterized by an enrichment of the LREE relative to the MREE and HREE (La/SmCN = 2.3–4.1, La/YbCN = 6.5–11.3).  The degree of REE fractionation, however, is less than that of adakites which have La/SmCN = 5.8, La/YbCN = 43.5 [25, Figure 8(b)]. The rocks show slightly negative to nonexistent Eu anomalies (Eu/Eu* = 0.74–1.01). On the primitive mantle-normalized diagram (Figure 9(b)), the samples display fractionated patterns with enrichment of the incompatible elements (Rb, Ba, Th, K, and Pb) relative to the compatibles ones and are associated with negative anomalies of Nb, Ta, and Ti relative to adjacent elements (Nb/Lapm = 0.17–0.34).


#### 4.3.3. Rhyolites

The rhyolite samples have a restricted range in SiO2 contents (75.52–76.02 wt%, n=3). TiO2 contents are 0.03 wt% for all the 3 samples, whereas Fe2O3 and MgO vary from 0.28 to 0.34 wt% and from 0.22 to 0.25 wt%, respectively. The samples are depleted in Cr and Ni (≤20 ppm) as well as in Zr (33–36 ppm). Compared with the tholeiitic basalts and the intermediate volcanic rocks, the rhyolites have lower total REE contents. La varies from 3.7 to 6.6 ppm, whereas Yb is restricted in the range of 0.8-0.9 ppm resulting into La/Yb ratios of 4.11–7.13.The rhyolites are characterized by slight enrichment of the LREE relative to MREE and HREE (La/SmCN = 1.7–2.0, La/YbCN = 2.95–5.26) with characteristic strong negative Eu anomalies (Eu/Eu* = 0.17–0.21, Figure 8(c)). On primitive mantle-normalized plots (Figure 9(c)), the samples show enrichment in incompatible elements (Rb, Ba, Th, K, and Pb),  negative anomalies of Nb, Ta, Eu, Sr, and Ti anomalies relative to adjacent elements.


### 4.4. Sm-Nd Isotopic Composition

Sm-Nd isotopic compositions for the Kilimafedha greenstone belt rhyolites are reported in Table2. Also shown in the Table are the εNd values calculated assuming a crystallization age of 2712 ± 5 Ma reported by Wirth et al. [9]. The εNd (2.7 Ga) values range from +1.87 to +2.18 for the tholeiitic basalts, +1.57 to +2.46 for the intermediate volcanic rocks, and −0.51 to +5.16 for the rhyolites (Figure 10), and these values are comparable with those from the volcanic rocks from the northern Musoma-Mara greenstone belt reported by Manya et al. [11, 12], some few hundreds of km north of the Kilimafedha greenstone belt. Their respective depleted mantle (TDM) ages are 2980–3763 Ma, 2846–2970 Ma, and 2557–3914 Ma (Table 2).Table 2
Sm-Nd isotopic data for the Kilimafedha greenstone belt volcanic rocks.
Sample
Rock suite
Sm (ppm)
Nd (ppm)
147Sm/144Nd
143Nd/144Nd
εNd (at 2.7 Ga)
TDM (Ma)
MU 14
Tholeiite basalts
1.68
6.57
0.1545
0.511995
2.18
2980
MU 69
6.12
18.82
0.1965
0.512731
1.87
3763
MU 49
Transitional intermediate volcanic rocks
6.09
29.4
0.1252
0.511451
1.82
2923
MU 57
5.06
24.2
0.1263
0.511481
1.99
2910
MU 68
6.08
33.3
0.1103
0.511218
2.46
2846
MU 89
6.02
28.7
0.1267
0.51148
1.83
2926
MU 100
5.45
24.6
0.1339
0.511594
1.57
2970
MU 16
Rhyolites
1.94
6.81
0.1721
0.512459
5.10
2557
MU 17
1.37
4.51
0.1835
0.512378
−0.51
3914
Calculations are based on a decay constant of 6.54 × 10−12 per year for 147Sm and DM values for Nd are (143Nd/144Nd)today = 0.51316, (147Sm/144Nd)today = 0.2137.Figure 10
Plot ofεNd versus t (Ma) for the Kilimafedha  greenstone belt volcanic rocks. The depleted mantle model is from DePaolo [24] and the northern Musoma-Mara greenstone belt high-Mg andesites and dacites data is from Manya et al. [11].


## 4.1. Alteration and Element Mobility

Alteration of metavolcanic rocks is a common phenomenon, in particular for Archaean greenstones, and is typically characterized by high loss on ignition (LOI) values and increased scatter of major and large ion lithophile elements. In this regard, the volcanic rocks, collected for this study, are variably affected by greenschist metamorphism, so it is expected that major and LILE are also affected by alteration. However, numerous studies have demonstrated that rare earth elements (REEs) and high field strength elements (HFSEs) remain relatively undisturbed at greenschist facies and even higher grades of metamorphism [19, 20]. So in this study major and LILE are used with great care, and emphasize is placed on the REE and HFSE.


## 4.2. Classification and Petrography

The volcanic rocks of the Kilimafedha greenstone belt represent a mafic, intermediate to felsic compositional continuum as indicated by their wide range of SiO2 contents (48.48–76.02 wt%). Out of a total of 50 samples that were analyzed for major elements and as shown in Figure 4 and 7 samples are basaltic in composition (SiO2 = 48.48–51.57 wt%), 40 samples show intermediate compositions ranging from basaltic andesites to basaltic trachyandesites, which are predominant; andesites to dacites (SiO2 = 52.51–66.80 wt%); only 3 samples are rhyolites (SiO2 = 75.52–76.02 wt%, values quoted on water free basis), revealing the sporadic nature of the more felsic rocks. The predominance of the basaltic trachyandesitic rocks and the nature of these rocks are unique to the Kilimafedha greenstone belt (Figure 5).Figure 5
TAS classification diagram of Le Maitre et al. [21] for the Kilimafedha volcanic rocks. Also shown in the diagram are fields for volcanic rocks from other greenstone belts of the Tanzania Craton: ISGB: Iramba—Sekenke greenstone belt, SGB: Sukumaland greenstone belt, SMMGB: Southern Musoma—Mara greenstone belt, and NMMGB: Northern Musoma—Mara greenstone belt.  Numbers in the diagram indicate fields as follows: 1: basalt, 2: basaltic andesite, 3: andesite, 4: dacite, 5: rhyolite, 6: trachybasalt, 7: basaltic trachyandesite, 8: trachyandesite, and 9: trachydacite.Using the Winchester and Floyd [22]  classification scheme which is suitable for classifying metamorphosed rocks, of the 18 samples that were analyzed for both major and trace elements, four samples plot along the boundary between subalkaline basalt and andesite/basalt, eleven others plot in the fields of andesite/basalt and andesites, and three samples plot as rhyolites (Figure 6). The basalts to andesitic basalts exhibit tholeiitic affinity, the intermediate rocks intermediate geochemical characteristics between tholeiitic and calc-alkaline affinities, whereas the rhyolites are calc-alkaline. Accordingly, the rocks are henceforth subdivided into three suites: the tholeiitic basalts, the intermediate volcanic rocks, and the rhyolites.Figure 6
Classification of the Kilimafedha volcanic rocks using the Nb/Y-Zr/Ti diagram of Winchester and Floyd [22]. Symbols are filled triangles: tholeiitic basalts, open squares: intermediate volcanic rocks, and open cycles: rhyolites.The primary petrographic features of the tholeiitic basalts are strongly obliterated by alteration which has resulted in the formation of chlorite, epidote, and hornblendic amphibole which appear to form after olivines and pyroxenes. The predominant intermediate rocks are often amygdaloidal, with streams of vesicles filled up with quartz, epidote, and chlorite. Other less vesicular types have large phenocrysts of albite-oligoclase. Most felsic rocks have fine matrix of quartz and sericitized feldspars with sparse phenocrysts of quartz and altered feldspars. The presence of chlorite and epidote in the Kilimafedha volcanic rocks suggests that these rocks have mainly been metamorphosed into greenschist facies.


## 4.3. Major and Trace Element Geochemistry

### 4.3.1. Tholeiitic Basalts

Major and trace element composition of the tholeiitic basalts of the Kilimafedha greenstone belt are presented in Table1. The rocks have SiO2 compositions that are in the range of 48.48–51.57 wt%, TiO2 = 0.61–1.80 wt%, Fe2O3 = 6.32–13.92 wt%, MgO = 5.56–8.49 wt%, and Mg numbers, calculated as 100×Mg2+/(Mg2++Fetotal2+),  range from 47 to 73 (the major elements presented on a water free basis). Cr and Ni contents are 160–240 ppm and 90–190 ppm, respectively. La contents vary considerably (1.7–9.2 ppm), whereas Yb contents range from 1.7 to 3.1 ppm resulting in La/Yb ratios of 1.00–4.00 (Table 1). On major and trace element bivariate plots (Figure 7), Fe2O3, MgO, CaO, and Ni correlate negatively with SiO2 pointing to fractionation signature or cogenetic relationship. The tholeiitic basalts alone do not show any major trends most likely due to the small number of samples and their restricted range in SiO2 content.Table 1
Major (wt%) and trace (ppm) element composition for the Kilimafedha greenstone belt volcanic rocks.
Tholeiitic basalts
Transitional intermediate volcanic rocks
MU 14
MU 15
MU 19
MU 20
MU 43
MU 69
MU 109
MU 12
MU 13
MU 21
MU 27
MU 33
MU 35
MU 36
MU 37
MU 38
MU 39
MU 49
MU 54
MU 57
MU 60
MU 64
MU 65
MU 66
MU 68
SiO2
50.3
47.4
50.4
50.3
47.8
48.2
49.2
55.2
52.9
52.8
65.3
60.6
53.7
55.1
54.3
54.1
53.5
53.7
53.5
54.1
54.9
56.0
54.9
55.3
62.4
TiO2
1.36
0.92
0.60
0.66
1.73
1.75
0.62
1.53
1.44
0.84
0.58
0.67
1.45
1.46
1.36
1.54
1.60
1.46
1.26
1.35
1.38
0.91
1.24
1.41
0.84
Al2O3
14.7
16.0
14.4
13.5
14.6
14.1
17.3
13.1
15.1
15.0
15.5
16.5
14.0
13.4
14.1
14.3
14.9
14.2
13.7
13.2
13.5
14.7
14.3
13.6
14.2
Fe2O3
12.3
12.4
11.9
12.9
13.3
13.5
6.2
9.3
10.8
11.2
4.2
6.7
11.3
12.0
11.2
11.9
12.1
12.1
11.8
11.3
11.7
9.1
10.8
12.0
6.6
MnO
0.27
0.17
0.17
0.18
0.19
0.18
0.08
0.25
0.24
0.16
0.06
0.10
0.11
0.14
0.11
0.14
0.14
0.15
0.12
0.12
0.12
0.19
0.13
0.13
0.09
MgO
5.45
8.09
7.53
7.32
6.62
6.76
8.30
6.00
4.66
5.58
2.68
3.57
3.42
3.71
3.43
3.46
3.62
3.85
4.24
3.53
3.77
5.27
3.80
3.50
2.60
CaO
10.9
10.9
10.7
10.7
10.3
10.5
12.3
7.54
10.94
8.54
3.65
2.73
9.62
6.25
9.49
6.41
5.30
5.69
8.30
6.40
6.94
6.28
7.16
7.43
4.53
Na2O
2.29
1.84
1.92
1.79
1.96
1.91
2.99
5.14
2.49
1.74
4.91
6.15
3.12
4.96
2.70
4.02
5.00
5.34
2.67
4.69
3.10
3.85
3.01
3.94
4.20
K2O
0.52
0.17
0.15
0.11
0.03
0.10
0.81
0.79
0.27
1.45
0.83
0.31
1.44
1.09
1.43
1.88
1.77
1.34
2.09
1.44
2.75
0.37
2.20
0.73
1.50
P2O5
0.04
0.01
0.01
0.01
0.19
0.09
0.01
0.07
0.06
0.01
0.06
0.08
0.12
0.12
0.12
0.15
0.15
0.13
0.12
0.13
0.03
0.01
0.11
0.13
0.16
LOI
1.46
2.14
2.17
2.45
3.19
2.55
2.15
0.92
1.03
2.29
2.19
2.53
1.39
1.34
1.72
1.81
1.83
1.75
1.97
3.30
1.66
2.93
2.00
1.69
2.80
Total
99.5
100
99.9
100
99.9
99.8
99.9
99.9
99.9
99.6
100
100
99.7
99.6
99.9
99.7
99.9
99.6
99.8
99.5
99.8
99.7
99.6
99.8
100
Mg#
46.8
56.5
55.6
52.8
49.6
49.7
72.7
56.1
46.1
49.8
56.0
51.2
37.4
38.0
37.7
36.5
37.3
38.7
41.5
38.2
39.1
53.3
41.0
36.7
43.9
Ba
204
27
66
140
1230
418
329
97
763
755
Rb
26
9
5
5
16
35
40
2
97
18
Sr
147
106
101
214
428
236
239
293
320
423
Ni
100
190
90
120
30
80
90
60
90
30
Cr
160
200
240
170
30
40
70
40
90
20
V
342
228
232
249
76
171
154
162
153
108
Th
0.5
0.3
0.2
1
3.9
8
8.7
7
8.9
5.8
Pb
5
5
5
5
7
5
9
42
6
10
U
0.2
0.1
0.1
0.4
1.3
2.1
2.9
1.9
2.5
1.4
Nb
3
2
1
4
4
8
8
7
8
7
Ta
0.3
0.2
0.1
0.3
0.4
0.6
0.8
0.6
0.7
0.5
Zr
80
53
31
88
126
163
177
147
184
176
Hf
2.2
1.4
1
2.4
3.2
4.3
4.9
3.9
4.7
4.6
Y
29
20
16
23
15
23
24
21
24
24
La
4.60
3.00
1.70
9.20
22.1
26.2
28.1
23.8
28.2
33.7
Ce
12.4
8.2
4.6
21.6
42.2
53.5
60
49.4
59.9
69.3
Pr
1.96
1.27
0.75
3.05
4.99
6.46
7.74
6.21
7.49
9
Nd
6.58
6.70
4.10
17.82
17.9
24.4
28.1
22.9
28.5
31.6
Sm
1.63
2.1
1.3
6.1
3.5
5.7
6.4
5.4
6.2
6.5
Eu
1.11
0.84
0.57
1.36
1.06
1.37
1.66
1.68
1.65
1.62
Gd
4.3
3.0
2.0
4.1
3.3
5.7
5.8
4.8
6.1
5.3
Tb
0.8
0.5
0.4
0.7
0.5
0.8
0.9
0.8
0.9
0.8
Dy
5.0
3.4
2.5
4.0
2.6
4.7
4.7
4.0
4.8
4.2
Ho
1.1
0.7
0.6
0.8
0.5
0.9
0.9
0.8
0.9
0.8
Er
3.3
2.1
1.7
2.4
1.5
2.4
2.5
2.1
2.5
2.5
Tm
0.48
0.32
0.26
0.36
0.22
0.34
0.35
0.29
0.34
0.37
Yb
3.10
2.10
1.70
2.30
1.40
2.10
2.20
1.80
2.10
2.30
Lu
0.46
0.31
0.26
0.35
0.22
0.31
0.31
0.26
0.3
0.34
La/Yb
1.5
1.4
1.0
4.0
15.8
12.5
12.8
13.2
13.4
14.7
La/Nb
1.53
1.5
1.7
2.3
5.53
3.28
3.51
3.40
3.53
4.81
Eu/Eu*
0.90
1.02
1.08
1.10
0.95
0.74
0.83
1.01
0.82
0.84
La/SmCN
0.90
0.92
0.84
1.70
4.08
2.97
2.83
2.85
2.94
3.35
La/YbCN
1.06
1.02
0.72
2.87
11.3
8.95
9.16
9.48
9.63
10.5
Nb/Lapm
0.63
0.64
0.57
0.42
0.17
0.29
0.27
0.28
0.27
0.20
Transitional intermediate volcanic rocks
Rhyolites
MU 76
MU 77
MU 78
MU 79
MU 80
MU 81
MU 82
MU 83
MU 84
MU 85
MU 86
MU 87
MU 89
MU 90
MU 91
MU 92
MU 93
MU 94
MU 95
MU 96
MU 97
MU 100
MU 16
MU 17
MU 18
SiO2
51.9
51.9
53.2
52.4
53.1
53.3
54.3
53.5
52.2
54.3
55.1
54.3
55.6
55.8
52.8
51.3
52.6
54.9
54.2
53.7
55.4
52.3
74.9
75.5
75.3
TiO2
1.42
1.38
1.34
1.37
1.49
1.49
0.70
1.51
1.62
1.25
1.35
1.41
1.41
1.43
1.52
0.84
1.20
1.37
1.41
1.09
1.07
1.42
0.03
0.03
0.03
Al2O3
14.7
14.2
14.1
14.4
14.2
13.9
15.1
14.0
14.7
13.5
14.4
13.8
13.6
13.4
14.4
14.1
14.2
14.6
14.2
15.1
14.2
15.6
14.28
14.38
14.46
Fe2O3
12.4
12.6
12.2
12.4
12.5
12.6
8.2
12.4
13.0
11.3
11.3
12.2
11.8
11.4
13.5
11.6
12.5
11.4
11.6
12.5
11.3
12.9
0.34
0.28
0.34
MnO
0.14
0.14
0.14
0.14
0.14
0.14
0.13
0.14
0.14
0.13
0.14
0.13
0.13
0.12
0.16
0.15
0.19
0.13
0.14
0.15
0.17
0.15
0.02
0.01
0.01
MgO
4.40
4.20
4.04
4.10
3.88
3.92
6.47
3.86
3.89
4.44
3.60
3.68
3.72
3.55
3.82
7.08
4.89
3.66
4.10
4.56
4.26
3.64
0.23
0.22
0.25
CaO
7.36
7.97
8.36
8.38
6.74
7.00
8.87
6.82
6.01
7.40
6.36
7.03
6.39
7.13
6.32
9.37
5.66
5.84
5.56
5.28
5.40
5.97
0.26
0.10
0.15
Na2O
3.66
2.83
2.88
2.87
4.32
3.92
3.14
4.20
4.63
2.91
5.57
3.79
3.73
3.62
4.63
2.41
4.53
4.55
4.00
4.91
5.04
4.75
5.14
5.17
5.32
K2O
1.25
1.91
1.48
1.67
1.60
1.52
0.57
1.57
1.79
2.89
1.27
1.47
1.91
0.15
0.95
0.88
2.06
1.66
2.57
1.77
1.62
1.16
3.98
3.61
3.41
P2O5
0.11
0.02
0.11
0.11
0.12
0.13
0.11
0.13
0.14
0.11
0.12
0.13
0.14
0.13
0.13
0.03
0.09
0.10
0.13
0.10
0.09
0.12
0.01
0.01
0.01
LOI
2.48
2.35
1.78
1.79
1.59
1.57
2.46
1.52
1.49
1.70
1.40
1.97
1.65
2.94
1.70
2.27
1.87
1.40
1.63
0.94
1.50
1.99
0.75
0.69
0.69
Total
99.8
99.5
99.6
99.7
99.7
99.6
100
99.6
99.6
99.9
101
99.9
100
99.6
100
100
99.8
99.6
99.5
100
100
100
100
100
100
Mg#
41.3
39.7
39.6
39.5
38.1
38.1
60.9
38.2
37.2
43.9
38.8
37.4
38.4
38.3
35.9
54.8
43.6
38.9
41.2
42.0
42.8
35.8
57.3
60.9
59.3
Ba
504
415
643
626
485
301
220
217
Rb
56
48
61
54
40
91
83
77
Sr
349
398
395
296
312
37
32
31
Ni
160
90
80
80
43
20
20
20
Cr
40
70
70
30
40
20
20
20
V
180
155
149
163
175
5
5
5
Th
7.8
8.9
8.8
7.2
7.5
3.1
2.9
2.7
Pb
5
14
18
5
5
9
5
5
U
2.2
2.5
3.1
2
2.2
2.5
2.1
2
Nb
7
9
8
6
7
5
5
4
Ta
0.6
0.7
0.8
0.6
0.6
0.6
0.6
0.6
Zr
158
179
173
137
155
34
36
33
Hf
4.3
4.6
4.9
3.7
4.1
1.9
2
1.9
Y
25
24
24
23
25
12
9
10
La
23.6
27.4
28.0
22.8
20.1
6.60
3.90
3.70
Ce
50.7
58.3
59.5
47.4
46.6
13.2
9.3
12.3
Pr
6.35
7.2
7.68
5.82
6.24
1.90
1.31
1.12
Nd
24.4
27.3
27.9
22.7
23.6
7.80
5.40
4.60
Sm
5.8
6.2
6.6
5.2
5.7
2.1
1.4
1.4
Eu
1.78
1.6
1.81
1.63
1.62
0.12
0.09
0.1
Gd
6.0
6.2
5.7
5.3
5.5
2.1
1.4
1.5
Tb
0.9
0.9
0.9
0.8
0.9
0.4
0.3
0.3
Dy
4.9
4.7
4.7
4.4
4.7
2.0
1.5
1.5
Ho
0.9
0.9
0.9
0.8
0.9
0.4
0.3
0.3
Er
2.6
2.4
2.5
2.3
2.6
1
0.8
0.9
Tm
0.36
0.34
0.36
0.32
0.36
0.15
0.13
0.14
Yb
2.20
2.00
2.20
2.00
2.20
0.90
0.80
0.90
Lu
0.32
0.3
0.31
0.3
0.33
0.13
0.12
0.12
La/Yb
10.7
13.7
12.7
11.4
9.1
7.3
4.9
4.1
La/Nb
3.37
3.04
3.50
3.80
2.87
1.32
0.78
0.925
Eu/Eu*
0.92
0.79
0.90
0.95
0.89
0.17
0.20
0.21
La/SmCN
2.63
2.85
2.74
2.83
2.28
2.03
1.80
1.71
La/YbCN
7.69
9.83
9.13
8.18
6.55
5.26
3.50
2.95
Nb/Lapm
0.29
0.32
0.28
0.25
0.34
0.73
1.24
1.04
Mg# (Magnesium number) = 100 ×Mg2+/(Mg2+ + Fetotal2+) as in Section 4.3.1, and Eu/Eu* = Eu/((SmN × GdN)1/2).Major and trace elements variation diagram for the Kilimafedha volcanic rocks. Symbols as in Figure6.
(a)
(b)
(c)
(d)
(e)
(f)
(g)
(h)
(i)The rocks display slightly depleted LREE to nearly flat REE patterns (Figure8(a)) that are characterized by La/SmCN and La/YbCN ratios of 0.8-0.9 and 0.72–1.06, respectively, except for sample MU 69 which is relatively enriched in LREE (La/SmCN = 1.7 and La/YbCN = 2.89) compared to the other three samples (where CN refers to chondrite normalized values). The La/SmCN and La/YbCN values of the three samples (MU 69 excluded) are slightly higher than those of NMORB (La/SmCN = 0.6, La/YbCN = 0.59; [23]) indicating relative enrichment of the LREE in the Kilimafedha tholeiites. The samples do not show any Eu anomalies (Eu/Eu* = 0.90–1.10). The samples were also plotted on primitive mantle spidergrams (Figure 9(a)), where they display enrichment in Rb, Ba,Th, K, and Pb relative to the more compatible elements with flatter  multielement  patterns characterized by negative Nb anomalies (Nb/Lapm = 0.42–0.64) and minor negative Ti anomalies (where pm refers to primitive mantle normalized values).Chondrite normalized REE diagrams for the Kilimafedha volcanic rocks normalizing values from Sun and McDonough [23]. (a) Tholeiitic basalts superimposed with NMORB, (b) intermediate volcanic rocks superimposed with adakites, and (c) rhyolites.
(a)
(b)
(c)Primitive mantle normalized diagrams for the Kilimafedha volcanic, normalizing values from Sun and McDonough [23]. (a) Tholeiitic basalts, (b) intermediate volcanic rocks, and (c) rhyolites.
(a)
(b)
(c)


### 4.3.2. Intermediate Volcanic Rocks

The intermediate volcanic rocks have a wide range of SiO2 contents (52.51–66.80 wt%) spanning from basaltic andesites through basaltic trachyandesites and andesites to dacites. The compositions, however, are skewed to the basaltic andesitic compositions as indicated by the averages (SiO2 = 52.51–66.80 wt%, average = 55.67 wt%, n=40, Table 1, Figures 5 and 6), and only 5 samples have SiO2 > 57 wt%. TiO2 contents are 0.59–1.65 wt%, Fe2O3 = 4.26–13.78 wt%, MgO = 2.68–7.25 wt%, and Mg numbers range from 36 to 61. Cr and Ni contents are 20–90 ppm and 30–160 ppm, respectively. La varies from 20.1–33.7 ppm and Yb from 1.4–2.3 ppm which results in La/Yb ratios of 9.14–15.8.The intermediate volcanic rocks display fractionated REE patterns (Figure8(b)) and in comparison with the tholeiitic basalts are characterized by an enrichment of the LREE relative to the MREE and HREE (La/SmCN = 2.3–4.1, La/YbCN = 6.5–11.3).  The degree of REE fractionation, however, is less than that of adakites which have La/SmCN = 5.8, La/YbCN = 43.5 [25, Figure 8(b)]. The rocks show slightly negative to nonexistent Eu anomalies (Eu/Eu* = 0.74–1.01). On the primitive mantle-normalized diagram (Figure 9(b)), the samples display fractionated patterns with enrichment of the incompatible elements (Rb, Ba, Th, K, and Pb) relative to the compatibles ones and are associated with negative anomalies of Nb, Ta, and Ti relative to adjacent elements (Nb/Lapm = 0.17–0.34).


### 4.3.3. Rhyolites

The rhyolite samples have a restricted range in SiO2 contents (75.52–76.02 wt%, n=3). TiO2 contents are 0.03 wt% for all the 3 samples, whereas Fe2O3 and MgO vary from 0.28 to 0.34 wt% and from 0.22 to 0.25 wt%, respectively. The samples are depleted in Cr and Ni (≤20 ppm) as well as in Zr (33–36 ppm). Compared with the tholeiitic basalts and the intermediate volcanic rocks, the rhyolites have lower total REE contents. La varies from 3.7 to 6.6 ppm, whereas Yb is restricted in the range of 0.8-0.9 ppm resulting into La/Yb ratios of 4.11–7.13.The rhyolites are characterized by slight enrichment of the LREE relative to MREE and HREE (La/SmCN = 1.7–2.0, La/YbCN = 2.95–5.26) with characteristic strong negative Eu anomalies (Eu/Eu* = 0.17–0.21, Figure 8(c)). On primitive mantle-normalized plots (Figure 9(c)), the samples show enrichment in incompatible elements (Rb, Ba, Th, K, and Pb),  negative anomalies of Nb, Ta, Eu, Sr, and Ti anomalies relative to adjacent elements.


## 4.3.1. Tholeiitic Basalts

Major and trace element composition of the tholeiitic basalts of the Kilimafedha greenstone belt are presented in Table1. The rocks have SiO2 compositions that are in the range of 48.48–51.57 wt%, TiO2 = 0.61–1.80 wt%, Fe2O3 = 6.32–13.92 wt%, MgO = 5.56–8.49 wt%, and Mg numbers, calculated as 100×Mg2+/(Mg2++Fetotal2+),  range from 47 to 73 (the major elements presented on a water free basis). Cr and Ni contents are 160–240 ppm and 90–190 ppm, respectively. La contents vary considerably (1.7–9.2 ppm), whereas Yb contents range from 1.7 to 3.1 ppm resulting in La/Yb ratios of 1.00–4.00 (Table 1). On major and trace element bivariate plots (Figure 7), Fe2O3, MgO, CaO, and Ni correlate negatively with SiO2 pointing to fractionation signature or cogenetic relationship. The tholeiitic basalts alone do not show any major trends most likely due to the small number of samples and their restricted range in SiO2 content.Table 1
Major (wt%) and trace (ppm) element composition for the Kilimafedha greenstone belt volcanic rocks.
Tholeiitic basalts
Transitional intermediate volcanic rocks
MU 14
MU 15
MU 19
MU 20
MU 43
MU 69
MU 109
MU 12
MU 13
MU 21
MU 27
MU 33
MU 35
MU 36
MU 37
MU 38
MU 39
MU 49
MU 54
MU 57
MU 60
MU 64
MU 65
MU 66
MU 68
SiO2
50.3
47.4
50.4
50.3
47.8
48.2
49.2
55.2
52.9
52.8
65.3
60.6
53.7
55.1
54.3
54.1
53.5
53.7
53.5
54.1
54.9
56.0
54.9
55.3
62.4
TiO2
1.36
0.92
0.60
0.66
1.73
1.75
0.62
1.53
1.44
0.84
0.58
0.67
1.45
1.46
1.36
1.54
1.60
1.46
1.26
1.35
1.38
0.91
1.24
1.41
0.84
Al2O3
14.7
16.0
14.4
13.5
14.6
14.1
17.3
13.1
15.1
15.0
15.5
16.5
14.0
13.4
14.1
14.3
14.9
14.2
13.7
13.2
13.5
14.7
14.3
13.6
14.2
Fe2O3
12.3
12.4
11.9
12.9
13.3
13.5
6.2
9.3
10.8
11.2
4.2
6.7
11.3
12.0
11.2
11.9
12.1
12.1
11.8
11.3
11.7
9.1
10.8
12.0
6.6
MnO
0.27
0.17
0.17
0.18
0.19
0.18
0.08
0.25
0.24
0.16
0.06
0.10
0.11
0.14
0.11
0.14
0.14
0.15
0.12
0.12
0.12
0.19
0.13
0.13
0.09
MgO
5.45
8.09
7.53
7.32
6.62
6.76
8.30
6.00
4.66
5.58
2.68
3.57
3.42
3.71
3.43
3.46
3.62
3.85
4.24
3.53
3.77
5.27
3.80
3.50
2.60
CaO
10.9
10.9
10.7
10.7
10.3
10.5
12.3
7.54
10.94
8.54
3.65
2.73
9.62
6.25
9.49
6.41
5.30
5.69
8.30
6.40
6.94
6.28
7.16
7.43
4.53
Na2O
2.29
1.84
1.92
1.79
1.96
1.91
2.99
5.14
2.49
1.74
4.91
6.15
3.12
4.96
2.70
4.02
5.00
5.34
2.67
4.69
3.10
3.85
3.01
3.94
4.20
K2O
0.52
0.17
0.15
0.11
0.03
0.10
0.81
0.79
0.27
1.45
0.83
0.31
1.44
1.09
1.43
1.88
1.77
1.34
2.09
1.44
2.75
0.37
2.20
0.73
1.50
P2O5
0.04
0.01
0.01
0.01
0.19
0.09
0.01
0.07
0.06
0.01
0.06
0.08
0.12
0.12
0.12
0.15
0.15
0.13
0.12
0.13
0.03
0.01
0.11
0.13
0.16
LOI
1.46
2.14
2.17
2.45
3.19
2.55
2.15
0.92
1.03
2.29
2.19
2.53
1.39
1.34
1.72
1.81
1.83
1.75
1.97
3.30
1.66
2.93
2.00
1.69
2.80
Total
99.5
100
99.9
100
99.9
99.8
99.9
99.9
99.9
99.6
100
100
99.7
99.6
99.9
99.7
99.9
99.6
99.8
99.5
99.8
99.7
99.6
99.8
100
Mg#
46.8
56.5
55.6
52.8
49.6
49.7
72.7
56.1
46.1
49.8
56.0
51.2
37.4
38.0
37.7
36.5
37.3
38.7
41.5
38.2
39.1
53.3
41.0
36.7
43.9
Ba
204
27
66
140
1230
418
329
97
763
755
Rb
26
9
5
5
16
35
40
2
97
18
Sr
147
106
101
214
428
236
239
293
320
423
Ni
100
190
90
120
30
80
90
60
90
30
Cr
160
200
240
170
30
40
70
40
90
20
V
342
228
232
249
76
171
154
162
153
108
Th
0.5
0.3
0.2
1
3.9
8
8.7
7
8.9
5.8
Pb
5
5
5
5
7
5
9
42
6
10
U
0.2
0.1
0.1
0.4
1.3
2.1
2.9
1.9
2.5
1.4
Nb
3
2
1
4
4
8
8
7
8
7
Ta
0.3
0.2
0.1
0.3
0.4
0.6
0.8
0.6
0.7
0.5
Zr
80
53
31
88
126
163
177
147
184
176
Hf
2.2
1.4
1
2.4
3.2
4.3
4.9
3.9
4.7
4.6
Y
29
20
16
23
15
23
24
21
24
24
La
4.60
3.00
1.70
9.20
22.1
26.2
28.1
23.8
28.2
33.7
Ce
12.4
8.2
4.6
21.6
42.2
53.5
60
49.4
59.9
69.3
Pr
1.96
1.27
0.75
3.05
4.99
6.46
7.74
6.21
7.49
9
Nd
6.58
6.70
4.10
17.82
17.9
24.4
28.1
22.9
28.5
31.6
Sm
1.63
2.1
1.3
6.1
3.5
5.7
6.4
5.4
6.2
6.5
Eu
1.11
0.84
0.57
1.36
1.06
1.37
1.66
1.68
1.65
1.62
Gd
4.3
3.0
2.0
4.1
3.3
5.7
5.8
4.8
6.1
5.3
Tb
0.8
0.5
0.4
0.7
0.5
0.8
0.9
0.8
0.9
0.8
Dy
5.0
3.4
2.5
4.0
2.6
4.7
4.7
4.0
4.8
4.2
Ho
1.1
0.7
0.6
0.8
0.5
0.9
0.9
0.8
0.9
0.8
Er
3.3
2.1
1.7
2.4
1.5
2.4
2.5
2.1
2.5
2.5
Tm
0.48
0.32
0.26
0.36
0.22
0.34
0.35
0.29
0.34
0.37
Yb
3.10
2.10
1.70
2.30
1.40
2.10
2.20
1.80
2.10
2.30
Lu
0.46
0.31
0.26
0.35
0.22
0.31
0.31
0.26
0.3
0.34
La/Yb
1.5
1.4
1.0
4.0
15.8
12.5
12.8
13.2
13.4
14.7
La/Nb
1.53
1.5
1.7
2.3
5.53
3.28
3.51
3.40
3.53
4.81
Eu/Eu*
0.90
1.02
1.08
1.10
0.95
0.74
0.83
1.01
0.82
0.84
La/SmCN
0.90
0.92
0.84
1.70
4.08
2.97
2.83
2.85
2.94
3.35
La/YbCN
1.06
1.02
0.72
2.87
11.3
8.95
9.16
9.48
9.63
10.5
Nb/Lapm
0.63
0.64
0.57
0.42
0.17
0.29
0.27
0.28
0.27
0.20
Transitional intermediate volcanic rocks
Rhyolites
MU 76
MU 77
MU 78
MU 79
MU 80
MU 81
MU 82
MU 83
MU 84
MU 85
MU 86
MU 87
MU 89
MU 90
MU 91
MU 92
MU 93
MU 94
MU 95
MU 96
MU 97
MU 100
MU 16
MU 17
MU 18
SiO2
51.9
51.9
53.2
52.4
53.1
53.3
54.3
53.5
52.2
54.3
55.1
54.3
55.6
55.8
52.8
51.3
52.6
54.9
54.2
53.7
55.4
52.3
74.9
75.5
75.3
TiO2
1.42
1.38
1.34
1.37
1.49
1.49
0.70
1.51
1.62
1.25
1.35
1.41
1.41
1.43
1.52
0.84
1.20
1.37
1.41
1.09
1.07
1.42
0.03
0.03
0.03
Al2O3
14.7
14.2
14.1
14.4
14.2
13.9
15.1
14.0
14.7
13.5
14.4
13.8
13.6
13.4
14.4
14.1
14.2
14.6
14.2
15.1
14.2
15.6
14.28
14.38
14.46
Fe2O3
12.4
12.6
12.2
12.4
12.5
12.6
8.2
12.4
13.0
11.3
11.3
12.2
11.8
11.4
13.5
11.6
12.5
11.4
11.6
12.5
11.3
12.9
0.34
0.28
0.34
MnO
0.14
0.14
0.14
0.14
0.14
0.14
0.13
0.14
0.14
0.13
0.14
0.13
0.13
0.12
0.16
0.15
0.19
0.13
0.14
0.15
0.17
0.15
0.02
0.01
0.01
MgO
4.40
4.20
4.04
4.10
3.88
3.92
6.47
3.86
3.89
4.44
3.60
3.68
3.72
3.55
3.82
7.08
4.89
3.66
4.10
4.56
4.26
3.64
0.23
0.22
0.25
CaO
7.36
7.97
8.36
8.38
6.74
7.00
8.87
6.82
6.01
7.40
6.36
7.03
6.39
7.13
6.32
9.37
5.66
5.84
5.56
5.28
5.40
5.97
0.26
0.10
0.15
Na2O
3.66
2.83
2.88
2.87
4.32
3.92
3.14
4.20
4.63
2.91
5.57
3.79
3.73
3.62
4.63
2.41
4.53
4.55
4.00
4.91
5.04
4.75
5.14
5.17
5.32
K2O
1.25
1.91
1.48
1.67
1.60
1.52
0.57
1.57
1.79
2.89
1.27
1.47
1.91
0.15
0.95
0.88
2.06
1.66
2.57
1.77
1.62
1.16
3.98
3.61
3.41
P2O5
0.11
0.02
0.11
0.11
0.12
0.13
0.11
0.13
0.14
0.11
0.12
0.13
0.14
0.13
0.13
0.03
0.09
0.10
0.13
0.10
0.09
0.12
0.01
0.01
0.01
LOI
2.48
2.35
1.78
1.79
1.59
1.57
2.46
1.52
1.49
1.70
1.40
1.97
1.65
2.94
1.70
2.27
1.87
1.40
1.63
0.94
1.50
1.99
0.75
0.69
0.69
Total
99.8
99.5
99.6
99.7
99.7
99.6
100
99.6
99.6
99.9
101
99.9
100
99.6
100
100
99.8
99.6
99.5
100
100
100
100
100
100
Mg#
41.3
39.7
39.6
39.5
38.1
38.1
60.9
38.2
37.2
43.9
38.8
37.4
38.4
38.3
35.9
54.8
43.6
38.9
41.2
42.0
42.8
35.8
57.3
60.9
59.3
Ba
504
415
643
626
485
301
220
217
Rb
56
48
61
54
40
91
83
77
Sr
349
398
395
296
312
37
32
31
Ni
160
90
80
80
43
20
20
20
Cr
40
70
70
30
40
20
20
20
V
180
155
149
163
175
5
5
5
Th
7.8
8.9
8.8
7.2
7.5
3.1
2.9
2.7
Pb
5
14
18
5
5
9
5
5
U
2.2
2.5
3.1
2
2.2
2.5
2.1
2
Nb
7
9
8
6
7
5
5
4
Ta
0.6
0.7
0.8
0.6
0.6
0.6
0.6
0.6
Zr
158
179
173
137
155
34
36
33
Hf
4.3
4.6
4.9
3.7
4.1
1.9
2
1.9
Y
25
24
24
23
25
12
9
10
La
23.6
27.4
28.0
22.8
20.1
6.60
3.90
3.70
Ce
50.7
58.3
59.5
47.4
46.6
13.2
9.3
12.3
Pr
6.35
7.2
7.68
5.82
6.24
1.90
1.31
1.12
Nd
24.4
27.3
27.9
22.7
23.6
7.80
5.40
4.60
Sm
5.8
6.2
6.6
5.2
5.7
2.1
1.4
1.4
Eu
1.78
1.6
1.81
1.63
1.62
0.12
0.09
0.1
Gd
6.0
6.2
5.7
5.3
5.5
2.1
1.4
1.5
Tb
0.9
0.9
0.9
0.8
0.9
0.4
0.3
0.3
Dy
4.9
4.7
4.7
4.4
4.7
2.0
1.5
1.5
Ho
0.9
0.9
0.9
0.8
0.9
0.4
0.3
0.3
Er
2.6
2.4
2.5
2.3
2.6
1
0.8
0.9
Tm
0.36
0.34
0.36
0.32
0.36
0.15
0.13
0.14
Yb
2.20
2.00
2.20
2.00
2.20
0.90
0.80
0.90
Lu
0.32
0.3
0.31
0.3
0.33
0.13
0.12
0.12
La/Yb
10.7
13.7
12.7
11.4
9.1
7.3
4.9
4.1
La/Nb
3.37
3.04
3.50
3.80
2.87
1.32
0.78
0.925
Eu/Eu*
0.92
0.79
0.90
0.95
0.89
0.17
0.20
0.21
La/SmCN
2.63
2.85
2.74
2.83
2.28
2.03
1.80
1.71
La/YbCN
7.69
9.83
9.13
8.18
6.55
5.26
3.50
2.95
Nb/Lapm
0.29
0.32
0.28
0.25
0.34
0.73
1.24
1.04
Mg# (Magnesium number) = 100 ×Mg2+/(Mg2+ + Fetotal2+) as in Section 4.3.1, and Eu/Eu* = Eu/((SmN × GdN)1/2).Major and trace elements variation diagram for the Kilimafedha volcanic rocks. Symbols as in Figure6.
(a)
(b)
(c)
(d)
(e)
(f)
(g)
(h)
(i)The rocks display slightly depleted LREE to nearly flat REE patterns (Figure8(a)) that are characterized by La/SmCN and La/YbCN ratios of 0.8-0.9 and 0.72–1.06, respectively, except for sample MU 69 which is relatively enriched in LREE (La/SmCN = 1.7 and La/YbCN = 2.89) compared to the other three samples (where CN refers to chondrite normalized values). The La/SmCN and La/YbCN values of the three samples (MU 69 excluded) are slightly higher than those of NMORB (La/SmCN = 0.6, La/YbCN = 0.59; [23]) indicating relative enrichment of the LREE in the Kilimafedha tholeiites. The samples do not show any Eu anomalies (Eu/Eu* = 0.90–1.10). The samples were also plotted on primitive mantle spidergrams (Figure 9(a)), where they display enrichment in Rb, Ba,Th, K, and Pb relative to the more compatible elements with flatter  multielement  patterns characterized by negative Nb anomalies (Nb/Lapm = 0.42–0.64) and minor negative Ti anomalies (where pm refers to primitive mantle normalized values).Chondrite normalized REE diagrams for the Kilimafedha volcanic rocks normalizing values from Sun and McDonough [23]. (a) Tholeiitic basalts superimposed with NMORB, (b) intermediate volcanic rocks superimposed with adakites, and (c) rhyolites.
(a)
(b)
(c)Primitive mantle normalized diagrams for the Kilimafedha volcanic, normalizing values from Sun and McDonough [23]. (a) Tholeiitic basalts, (b) intermediate volcanic rocks, and (c) rhyolites.
(a)
(b)
(c)


## 4.3.2. Intermediate Volcanic Rocks

The intermediate volcanic rocks have a wide range of SiO2 contents (52.51–66.80 wt%) spanning from basaltic andesites through basaltic trachyandesites and andesites to dacites. The compositions, however, are skewed to the basaltic andesitic compositions as indicated by the averages (SiO2 = 52.51–66.80 wt%, average = 55.67 wt%, n=40, Table 1, Figures 5 and 6), and only 5 samples have SiO2 > 57 wt%. TiO2 contents are 0.59–1.65 wt%, Fe2O3 = 4.26–13.78 wt%, MgO = 2.68–7.25 wt%, and Mg numbers range from 36 to 61. Cr and Ni contents are 20–90 ppm and 30–160 ppm, respectively. La varies from 20.1–33.7 ppm and Yb from 1.4–2.3 ppm which results in La/Yb ratios of 9.14–15.8.The intermediate volcanic rocks display fractionated REE patterns (Figure8(b)) and in comparison with the tholeiitic basalts are characterized by an enrichment of the LREE relative to the MREE and HREE (La/SmCN = 2.3–4.1, La/YbCN = 6.5–11.3).  The degree of REE fractionation, however, is less than that of adakites which have La/SmCN = 5.8, La/YbCN = 43.5 [25, Figure 8(b)]. The rocks show slightly negative to nonexistent Eu anomalies (Eu/Eu* = 0.74–1.01). On the primitive mantle-normalized diagram (Figure 9(b)), the samples display fractionated patterns with enrichment of the incompatible elements (Rb, Ba, Th, K, and Pb) relative to the compatibles ones and are associated with negative anomalies of Nb, Ta, and Ti relative to adjacent elements (Nb/Lapm = 0.17–0.34).


## 4.3.3. Rhyolites

The rhyolite samples have a restricted range in SiO2 contents (75.52–76.02 wt%, n=3). TiO2 contents are 0.03 wt% for all the 3 samples, whereas Fe2O3 and MgO vary from 0.28 to 0.34 wt% and from 0.22 to 0.25 wt%, respectively. The samples are depleted in Cr and Ni (≤20 ppm) as well as in Zr (33–36 ppm). Compared with the tholeiitic basalts and the intermediate volcanic rocks, the rhyolites have lower total REE contents. La varies from 3.7 to 6.6 ppm, whereas Yb is restricted in the range of 0.8-0.9 ppm resulting into La/Yb ratios of 4.11–7.13.The rhyolites are characterized by slight enrichment of the LREE relative to MREE and HREE (La/SmCN = 1.7–2.0, La/YbCN = 2.95–5.26) with characteristic strong negative Eu anomalies (Eu/Eu* = 0.17–0.21, Figure 8(c)). On primitive mantle-normalized plots (Figure 9(c)), the samples show enrichment in incompatible elements (Rb, Ba, Th, K, and Pb),  negative anomalies of Nb, Ta, Eu, Sr, and Ti anomalies relative to adjacent elements.


## 4.4. Sm-Nd Isotopic Composition

Sm-Nd isotopic compositions for the Kilimafedha greenstone belt rhyolites are reported in Table2. Also shown in the Table are the εNd values calculated assuming a crystallization age of 2712 ± 5 Ma reported by Wirth et al. [9]. The εNd (2.7 Ga) values range from +1.87 to +2.18 for the tholeiitic basalts, +1.57 to +2.46 for the intermediate volcanic rocks, and −0.51 to +5.16 for the rhyolites (Figure 10), and these values are comparable with those from the volcanic rocks from the northern Musoma-Mara greenstone belt reported by Manya et al. [11, 12], some few hundreds of km north of the Kilimafedha greenstone belt. Their respective depleted mantle (TDM) ages are 2980–3763 Ma, 2846–2970 Ma, and 2557–3914 Ma (Table 2).Table 2
Sm-Nd isotopic data for the Kilimafedha greenstone belt volcanic rocks.
Sample
Rock suite
Sm (ppm)
Nd (ppm)
147Sm/144Nd
143Nd/144Nd
εNd (at 2.7 Ga)
TDM (Ma)
MU 14
Tholeiite basalts
1.68
6.57
0.1545
0.511995
2.18
2980
MU 69
6.12
18.82
0.1965
0.512731
1.87
3763
MU 49
Transitional intermediate volcanic rocks
6.09
29.4
0.1252
0.511451
1.82
2923
MU 57
5.06
24.2
0.1263
0.511481
1.99
2910
MU 68
6.08
33.3
0.1103
0.511218
2.46
2846
MU 89
6.02
28.7
0.1267
0.51148
1.83
2926
MU 100
5.45
24.6
0.1339
0.511594
1.57
2970
MU 16
Rhyolites
1.94
6.81
0.1721
0.512459
5.10
2557
MU 17
1.37
4.51
0.1835
0.512378
−0.51
3914
Calculations are based on a decay constant of 6.54 × 10−12 per year for 147Sm and DM values for Nd are (143Nd/144Nd)today = 0.51316, (147Sm/144Nd)today = 0.2137.Figure 10
Plot ofεNd versus t (Ma) for the Kilimafedha  greenstone belt volcanic rocks. The depleted mantle model is from DePaolo [24] and the northern Musoma-Mara greenstone belt high-Mg andesites and dacites data is from Manya et al. [11].


## 5. Discussion

### 5.1. Petrogenesis

#### 5.1.1. Tholeiitic Basalts

The slight depletion in LREE to nearly flat REE patterns shown by the tholeiitic basalts coupled with their close compositional similarity to N-MORB suggests that these rocks were generated in a source similar to that generating modern N-MORB. Unlike NMORB, however, these patterns display negative anomalies in Nb and Ti, features which together with tectonic setting discrimination diagrams (see next section) are suggestive of derivation in a subduction setting. The nature of the mantle source rocks can further be constrained by the trace element ratios Nb/Yb, Zr/Yb, and Th/Yb [26]. When plotted on the Nb/Yb versus Zr/Yb diagram (Figure 11), the tholeiitic basalts plot around NMORB with a general trend towards increasing mantle enrichment to E-MORB within the MORB array. This suggests that the enrichment observed in the Kilimafedha tholeiites can be explained by their derivation from an initially homogeneous MORB-like source that was differentially metasomatized by an aqueous fluid derived from the subducting slab [26]. Fluxing of the source by the metasomatizing fluid most likely enhanced melting of the mantle wedge at a relatively low pressure. Melting of the mantle wedge which was not affected significantly by the metasomatism yielded the La-depleted basalts, whereas the La-enriched basalts were produced by melting of a mantle wedge that has been slightly metasomatized. The compositional similarity to NMORB is also reflected in similar εNd (2.7 Ga) of the samples (+2.18 for sample MU 14) to the depleted mantle value of 2.2 [24] at the same time. The slightly lower εNd (2.7Ga) values of 1.87 for sample MU 69 would indicate minimal contamination of the magmas by older continental crust.Figure 11
Nb/Yb-Zr/Yb diagram (after Pearce and Peate, [26]) for the Kilimafedha tholeiitic basalts (filled triangles) and intermediate volcanic rocks (open squares). The tholeiitic basalt samples plot around the NMORB field tending towards the mantle enrichment direction within the MORB array suggestive of metasomatism by aqueous fluid.  The intermediate rocks plot just above the EMORB tending to higher Zr values illustrating input of the HFSE from the subducted slab. NMORB, EMORB, and OIB data are from Sun and McDonough [23].


#### 5.1.2. Intermediate Volcanic Rocks

Unlike the flat REE patterns that characterize the tholeiitic basalts, the intermediate rocks show fractionated patterns characterized by La/Yb ratios of 9.14–15.8. These ratios are, however, lower than those reported in adakites (La/Yb = 40; [23]). In adakites, such high ratios are indicative of the presence of garnet ± amphibole in the source during partial melting. Thus, the lower La/Yb ratios of the rocks preclude the involvement of garnet ± amphibole in their magma genesis. In Figure 11, the intermediate volcanic rocks cluster just above E-MORB out of the MORB array towards increasing Zr content, which according to Pearce and Peate [26] signifies the involvement of both slab melt and hydrous fluid in metasomatising the source rocks. The metasomatism resulted in the enrichment of the source mantle wedge in the HFSE that has been scavenged from the subducting oceanic slab thereby explaining the observed enrichment in the HFSE relative to MORB (Figure 11). The involvement of slab partial melts in the petrogenesis of the intermediate volcanic rocks suggests that temperatures in the subduction zone were sufficiently high to initiate partial melting of the slab. According to Pearce and Peate [26], the onset of melting of the subducting slab in the Phanerozoic occurs at relatively greater depth (>100 km) beneath the subduction zone. This suggests that, unlike the tholeiitic basalts that were formed at relatively shallow depths, the primary magmas for the intermediate volcanic rocks originated at greater depth, but outside the garnet stability field. The intermediate volcanic rocks have εNd (2.7 Ga) values of +1.57 to +2.46 similar to those of the tholeiitic basalts and are indicative of the juvenile nature of the magmas accompanied by minimal crustal contamination. Such a conclusion was also reached for the northern MMGB high-Mg andesites and dacites [11] which share similar εNd values with the Kilimafedha greenstobe belt volcanic rocks.


#### 5.1.3. Rhyolites

Rhyolites differ from the other two suites in having lower contents of TiO2, P2O5, Zr, and overall lower abundances of the REE (Table 1). In chondrite normalized REE diagrams (Figure 8) and extended trace element diagram (Figure 9), the rhyolites are characterized by large negative Eu (Eu/Eu* = 0.17–0.21, Table 1) accompanied by negative Sr anomalies as well as Nb and Ti anomalies. The close spatial association of the rhyolites and other suites of the Kilimafedha greenstone belt coupled with their trends towards lower Fe2O3, MgO, CaO, TiO2, Cr, and Ni with increasing SiO2 (Figure 7) may suggest that the rhyolites may be products of extensive fractional crystallization of the same magmas that generated the more basic members. Such a model is also supported by experimental studies which showed that low-pressure fractional crystallization of olivine, pyroxene, plagioclase, and Fe-Ti oxides can produce rhyolites [27] with relatively flat HREE patterns. Thus, the generally lower REE abundances, TiO2, P2O5, and Zr contents can be explained by shallow level fractionation of Ti-rich phases (e.g., titanomagnetite) and REE-rich phases such as apatite, monazite, zircon, and allanites, whereas the large negative Eu and Sr anomalies could be due to plagioclase fractionation. Compared to the other two suites, the rhyolites show variable εNd (2.7 Ga) values of −0.51 to +5.17 and suggest that older crustal involvement in the genesis of the rhyolites either by partial melting of older crust or  contamination of evolving magmatic liquid cannot be ruled out as an important process in the genesis of these rocks. The wide variation in εNd towards more depleted signatures demands reexamination of the rocks.


### 5.2. Tectonic Setting

Trace element discrimination diagrams developed for Phanerozoic rocks have been used together with their ratios to infer the tectonic setting for Archaean rocks (e.g., [19]). Using this approach, the Kilimafedha tholeiitic basalts and basaltic andesites were plotted on the Th-Hf-Nb triangular diagram of Wood [28] which is suitable for mafic as well as intermediate volcanic rocks. On this diagram, three of the four tholeiitic basalt samples plot along the boundary between the N-MORB and E-MORB fields, while the other samples together with all intermediate volcanic samples plot in the field of volcanic arc basalts (Figure 12). The similarity of the three tholeiitic basalt samples with N-MORB on the Th-Hf-Nb diagram is also reflected in Figure 8(a).  The La/Nb ratio of basaltic samples is particularly important in discriminating basalts that erupted in ocean ridges and ocean plateaus from those that erupted in arcs [29, 30]. According to Rudnick [29] and Condie [30], ocean ridge and ocean plateau basalts have La/Nb < 1.4, whereas arc basalts have La/Nb > 1.4. Both the tholeiitic basalts and intermediate rocks of the Kilimafedha greenstone belt show La/Nb > 1.4 (1.5–2.30 and 2.87–5.53, resp.) suggestive of arc affinities. Thus, the results obtained from the discrimination diagrams combined with trace element ratios data are suggestive of an arc tectonic setting for the Kilimafedha greenstone belts rocks. This conclusion is supported by the fact that the rocks exhibit negative anomalies of Nb, Ti, and/or Ta anomalies in extended trace element spidergrams (Figure 9), features attributed to magmas generated at subduction zones [26].Figure 12
Ta-Hf-Th tectonic setting discrimination diagram [28] for the tholeiitic basalts (filled triangles) and intermediate volcanic rocks (open squares) for the Kilimafedha greenstone belts.


## 5.1. Petrogenesis

### 5.1.1. Tholeiitic Basalts

The slight depletion in LREE to nearly flat REE patterns shown by the tholeiitic basalts coupled with their close compositional similarity to N-MORB suggests that these rocks were generated in a source similar to that generating modern N-MORB. Unlike NMORB, however, these patterns display negative anomalies in Nb and Ti, features which together with tectonic setting discrimination diagrams (see next section) are suggestive of derivation in a subduction setting. The nature of the mantle source rocks can further be constrained by the trace element ratios Nb/Yb, Zr/Yb, and Th/Yb [26]. When plotted on the Nb/Yb versus Zr/Yb diagram (Figure 11), the tholeiitic basalts plot around NMORB with a general trend towards increasing mantle enrichment to E-MORB within the MORB array. This suggests that the enrichment observed in the Kilimafedha tholeiites can be explained by their derivation from an initially homogeneous MORB-like source that was differentially metasomatized by an aqueous fluid derived from the subducting slab [26]. Fluxing of the source by the metasomatizing fluid most likely enhanced melting of the mantle wedge at a relatively low pressure. Melting of the mantle wedge which was not affected significantly by the metasomatism yielded the La-depleted basalts, whereas the La-enriched basalts were produced by melting of a mantle wedge that has been slightly metasomatized. The compositional similarity to NMORB is also reflected in similar εNd (2.7 Ga) of the samples (+2.18 for sample MU 14) to the depleted mantle value of 2.2 [24] at the same time. The slightly lower εNd (2.7Ga) values of 1.87 for sample MU 69 would indicate minimal contamination of the magmas by older continental crust.Figure 11
Nb/Yb-Zr/Yb diagram (after Pearce and Peate, [26]) for the Kilimafedha tholeiitic basalts (filled triangles) and intermediate volcanic rocks (open squares). The tholeiitic basalt samples plot around the NMORB field tending towards the mantle enrichment direction within the MORB array suggestive of metasomatism by aqueous fluid.  The intermediate rocks plot just above the EMORB tending to higher Zr values illustrating input of the HFSE from the subducted slab. NMORB, EMORB, and OIB data are from Sun and McDonough [23].


### 5.1.2. Intermediate Volcanic Rocks

Unlike the flat REE patterns that characterize the tholeiitic basalts, the intermediate rocks show fractionated patterns characterized by La/Yb ratios of 9.14–15.8. These ratios are, however, lower than those reported in adakites (La/Yb = 40; [23]). In adakites, such high ratios are indicative of the presence of garnet ± amphibole in the source during partial melting. Thus, the lower La/Yb ratios of the rocks preclude the involvement of garnet ± amphibole in their magma genesis. In Figure 11, the intermediate volcanic rocks cluster just above E-MORB out of the MORB array towards increasing Zr content, which according to Pearce and Peate [26] signifies the involvement of both slab melt and hydrous fluid in metasomatising the source rocks. The metasomatism resulted in the enrichment of the source mantle wedge in the HFSE that has been scavenged from the subducting oceanic slab thereby explaining the observed enrichment in the HFSE relative to MORB (Figure 11). The involvement of slab partial melts in the petrogenesis of the intermediate volcanic rocks suggests that temperatures in the subduction zone were sufficiently high to initiate partial melting of the slab. According to Pearce and Peate [26], the onset of melting of the subducting slab in the Phanerozoic occurs at relatively greater depth (>100 km) beneath the subduction zone. This suggests that, unlike the tholeiitic basalts that were formed at relatively shallow depths, the primary magmas for the intermediate volcanic rocks originated at greater depth, but outside the garnet stability field. The intermediate volcanic rocks have εNd (2.7 Ga) values of +1.57 to +2.46 similar to those of the tholeiitic basalts and are indicative of the juvenile nature of the magmas accompanied by minimal crustal contamination. Such a conclusion was also reached for the northern MMGB high-Mg andesites and dacites [11] which share similar εNd values with the Kilimafedha greenstobe belt volcanic rocks.


### 5.1.3. Rhyolites

Rhyolites differ from the other two suites in having lower contents of TiO2, P2O5, Zr, and overall lower abundances of the REE (Table 1). In chondrite normalized REE diagrams (Figure 8) and extended trace element diagram (Figure 9), the rhyolites are characterized by large negative Eu (Eu/Eu* = 0.17–0.21, Table 1) accompanied by negative Sr anomalies as well as Nb and Ti anomalies. The close spatial association of the rhyolites and other suites of the Kilimafedha greenstone belt coupled with their trends towards lower Fe2O3, MgO, CaO, TiO2, Cr, and Ni with increasing SiO2 (Figure 7) may suggest that the rhyolites may be products of extensive fractional crystallization of the same magmas that generated the more basic members. Such a model is also supported by experimental studies which showed that low-pressure fractional crystallization of olivine, pyroxene, plagioclase, and Fe-Ti oxides can produce rhyolites [27] with relatively flat HREE patterns. Thus, the generally lower REE abundances, TiO2, P2O5, and Zr contents can be explained by shallow level fractionation of Ti-rich phases (e.g., titanomagnetite) and REE-rich phases such as apatite, monazite, zircon, and allanites, whereas the large negative Eu and Sr anomalies could be due to plagioclase fractionation. Compared to the other two suites, the rhyolites show variable εNd (2.7 Ga) values of −0.51 to +5.17 and suggest that older crustal involvement in the genesis of the rhyolites either by partial melting of older crust or  contamination of evolving magmatic liquid cannot be ruled out as an important process in the genesis of these rocks. The wide variation in εNd towards more depleted signatures demands reexamination of the rocks.


## 5.1.1. Tholeiitic Basalts

The slight depletion in LREE to nearly flat REE patterns shown by the tholeiitic basalts coupled with their close compositional similarity to N-MORB suggests that these rocks were generated in a source similar to that generating modern N-MORB. Unlike NMORB, however, these patterns display negative anomalies in Nb and Ti, features which together with tectonic setting discrimination diagrams (see next section) are suggestive of derivation in a subduction setting. The nature of the mantle source rocks can further be constrained by the trace element ratios Nb/Yb, Zr/Yb, and Th/Yb [26]. When plotted on the Nb/Yb versus Zr/Yb diagram (Figure 11), the tholeiitic basalts plot around NMORB with a general trend towards increasing mantle enrichment to E-MORB within the MORB array. This suggests that the enrichment observed in the Kilimafedha tholeiites can be explained by their derivation from an initially homogeneous MORB-like source that was differentially metasomatized by an aqueous fluid derived from the subducting slab [26]. Fluxing of the source by the metasomatizing fluid most likely enhanced melting of the mantle wedge at a relatively low pressure. Melting of the mantle wedge which was not affected significantly by the metasomatism yielded the La-depleted basalts, whereas the La-enriched basalts were produced by melting of a mantle wedge that has been slightly metasomatized. The compositional similarity to NMORB is also reflected in similar εNd (2.7 Ga) of the samples (+2.18 for sample MU 14) to the depleted mantle value of 2.2 [24] at the same time. The slightly lower εNd (2.7Ga) values of 1.87 for sample MU 69 would indicate minimal contamination of the magmas by older continental crust.Figure 11
Nb/Yb-Zr/Yb diagram (after Pearce and Peate, [26]) for the Kilimafedha tholeiitic basalts (filled triangles) and intermediate volcanic rocks (open squares). The tholeiitic basalt samples plot around the NMORB field tending towards the mantle enrichment direction within the MORB array suggestive of metasomatism by aqueous fluid.  The intermediate rocks plot just above the EMORB tending to higher Zr values illustrating input of the HFSE from the subducted slab. NMORB, EMORB, and OIB data are from Sun and McDonough [23].


## 5.1.2. Intermediate Volcanic Rocks

Unlike the flat REE patterns that characterize the tholeiitic basalts, the intermediate rocks show fractionated patterns characterized by La/Yb ratios of 9.14–15.8. These ratios are, however, lower than those reported in adakites (La/Yb = 40; [23]). In adakites, such high ratios are indicative of the presence of garnet ± amphibole in the source during partial melting. Thus, the lower La/Yb ratios of the rocks preclude the involvement of garnet ± amphibole in their magma genesis. In Figure 11, the intermediate volcanic rocks cluster just above E-MORB out of the MORB array towards increasing Zr content, which according to Pearce and Peate [26] signifies the involvement of both slab melt and hydrous fluid in metasomatising the source rocks. The metasomatism resulted in the enrichment of the source mantle wedge in the HFSE that has been scavenged from the subducting oceanic slab thereby explaining the observed enrichment in the HFSE relative to MORB (Figure 11). The involvement of slab partial melts in the petrogenesis of the intermediate volcanic rocks suggests that temperatures in the subduction zone were sufficiently high to initiate partial melting of the slab. According to Pearce and Peate [26], the onset of melting of the subducting slab in the Phanerozoic occurs at relatively greater depth (>100 km) beneath the subduction zone. This suggests that, unlike the tholeiitic basalts that were formed at relatively shallow depths, the primary magmas for the intermediate volcanic rocks originated at greater depth, but outside the garnet stability field. The intermediate volcanic rocks have εNd (2.7 Ga) values of +1.57 to +2.46 similar to those of the tholeiitic basalts and are indicative of the juvenile nature of the magmas accompanied by minimal crustal contamination. Such a conclusion was also reached for the northern MMGB high-Mg andesites and dacites [11] which share similar εNd values with the Kilimafedha greenstobe belt volcanic rocks.


## 5.1.3. Rhyolites

Rhyolites differ from the other two suites in having lower contents of TiO2, P2O5, Zr, and overall lower abundances of the REE (Table 1). In chondrite normalized REE diagrams (Figure 8) and extended trace element diagram (Figure 9), the rhyolites are characterized by large negative Eu (Eu/Eu* = 0.17–0.21, Table 1) accompanied by negative Sr anomalies as well as Nb and Ti anomalies. The close spatial association of the rhyolites and other suites of the Kilimafedha greenstone belt coupled with their trends towards lower Fe2O3, MgO, CaO, TiO2, Cr, and Ni with increasing SiO2 (Figure 7) may suggest that the rhyolites may be products of extensive fractional crystallization of the same magmas that generated the more basic members. Such a model is also supported by experimental studies which showed that low-pressure fractional crystallization of olivine, pyroxene, plagioclase, and Fe-Ti oxides can produce rhyolites [27] with relatively flat HREE patterns. Thus, the generally lower REE abundances, TiO2, P2O5, and Zr contents can be explained by shallow level fractionation of Ti-rich phases (e.g., titanomagnetite) and REE-rich phases such as apatite, monazite, zircon, and allanites, whereas the large negative Eu and Sr anomalies could be due to plagioclase fractionation. Compared to the other two suites, the rhyolites show variable εNd (2.7 Ga) values of −0.51 to +5.17 and suggest that older crustal involvement in the genesis of the rhyolites either by partial melting of older crust or  contamination of evolving magmatic liquid cannot be ruled out as an important process in the genesis of these rocks. The wide variation in εNd towards more depleted signatures demands reexamination of the rocks.


## 5.2. Tectonic Setting

Trace element discrimination diagrams developed for Phanerozoic rocks have been used together with their ratios to infer the tectonic setting for Archaean rocks (e.g., [19]). Using this approach, the Kilimafedha tholeiitic basalts and basaltic andesites were plotted on the Th-Hf-Nb triangular diagram of Wood [28] which is suitable for mafic as well as intermediate volcanic rocks. On this diagram, three of the four tholeiitic basalt samples plot along the boundary between the N-MORB and E-MORB fields, while the other samples together with all intermediate volcanic samples plot in the field of volcanic arc basalts (Figure 12). The similarity of the three tholeiitic basalt samples with N-MORB on the Th-Hf-Nb diagram is also reflected in Figure 8(a).  The La/Nb ratio of basaltic samples is particularly important in discriminating basalts that erupted in ocean ridges and ocean plateaus from those that erupted in arcs [29, 30]. According to Rudnick [29] and Condie [30], ocean ridge and ocean plateau basalts have La/Nb < 1.4, whereas arc basalts have La/Nb > 1.4. Both the tholeiitic basalts and intermediate rocks of the Kilimafedha greenstone belt show La/Nb > 1.4 (1.5–2.30 and 2.87–5.53, resp.) suggestive of arc affinities. Thus, the results obtained from the discrimination diagrams combined with trace element ratios data are suggestive of an arc tectonic setting for the Kilimafedha greenstone belts rocks. This conclusion is supported by the fact that the rocks exhibit negative anomalies of Nb, Ti, and/or Ta anomalies in extended trace element spidergrams (Figure 9), features attributed to magmas generated at subduction zones [26].Figure 12
Ta-Hf-Th tectonic setting discrimination diagram [28] for the tholeiitic basalts (filled triangles) and intermediate volcanic rocks (open squares) for the Kilimafedha greenstone belts.


## 6. Comparison with Other Greenstone Belts of the Tanzania Craton

A closer review of geochemistry and geochronology by Manya et al. [10] and Manya and Maboko [8] showed that the individual greenstone belts of the Tanzania Craton exhibit different formation ages, and their formation occurred in different tectonic settings. This suggestion is also evident in different volcanic rock packages found in these belts. Kilimafedha greenstone belt (KGB) differs from the Sukumaland (SGB) to the west and Iramba-Sekenke (ISGB) to the far south in having predominantly intermediate volcanic rocks with tholeiitic to calc-alkaline intermediate affinities, rare mafic, and felsic volcanic package, which are in contrast to the later that are dominated by tholeiitic basalts and rare intermediate volcanic rocks. The volcanic package in KGB also differs from those of the southern Musoma-Mara greenstone belt (MMGB) to the near north as the later is comprised of bimodal volcanic assemblage [31]. Although the northern part of the MMGB is predominantly comprised of intermediate rocks similar to KGB, the former lacks mafic members.The foregoing discussion corroborates the findings by Manya et al. [10] that the individual greenstone belts evolved as separate entities at different time intervals having different volcanic rocks assemblages. Although volcanism in greenstone belts of the Tanzania Craton seems to have erupted at different time intervals (2823–2780 Ma for SGB, 2755–2712 Ma for MMGB, ISGB, and KGB, 2676–2667 Ma for northern MMGB, [8] and references therein); one thing is common to all of them: they formed exclusively at convergent margins. This signifies the importance of formation and growth of late Archaean continental crust at convergent margins.


## 7. Conclusion

The Neoarchaean Kilimafedha greenstone belt of northeastern Tanzania consists of three closely associated suites of volcanic rocks: the predominant intermediate basaltic andesite and dacites, and the volumetrically minor tholeiitic basalts and rhyolites.  The tholeiitic basalts have nearly flat REE patterns and show close compositional similarity to NMORB. Trace element systematics of the tholeiites suggest that they were formed by shallow partial melting of a mantle wedge that has been variably metasomatized by an aqueous fluid in a convergent tectonic setting. The intermediate rocks are characterized by fractionated REE patterns, enrichment of the HFSE relative to NMORB, and negative anomalies of Nb and Ta. Such geochemical features are consistent with derivation of these rocks by partial melting of a mantle wedge that has been metasomatized by both fluid and slab melt at a greater depth than the tholeiitic basalts source but outside the garnet stability field. The geochemical features defining the Kilimafedha greenstone belt rhyolites include low TiO2, P2O5, Zr, and overall lower abundance of total REE compared with the other two suites and large negative Eu, Sr, and Ti anomalies in extended trace element spidergrams. These features can be explained by shallow level fractional crystallization of the parent magma of the intermediate volcanic rocks involving plagioclase, Ti-rich phases like ilmenite and magnetite as well as REE-rich phases like apatite, zircon, monazite, and allanite. The close spatial association of the three petrological types in the Kilimafedha greenstone belt is interpreted as reflecting their formation in an evolving late Achaean island arc.



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*Source: 603971-2012-10-24.xml*