HYDROTHERMAL ALTERATION ZONES DETECTION IN LIMNOS ISLAND, THROUGH THE APPLICATION OF REMOTE SENSING

Abstract

In this study we use Landsat 8 OLI satellite imagery in order to identify and map alteration zones in Limnos island (N. Aegean, Greece). Pre-processing included sea and vegetation masking. In order to enhance spatial resolution, data fusion to 15m is performed. A lineament map is extracted from the panchromatic image that gives the general tectonic view of the island. The detection and mapping of alteration minerals is performed using specific band ratios and consequent composite images. The colour composite using bands 10, 11, 7 (RGB) show the spectral signature and general distribution of silica. Band ratios 6/7, 4/2, 6/5, reveal alteration zones containing iron oxides, clay alteration and ferrous minerals correspondingly. The aforementioned analysis has shown that hydrothermally alteration areas in Limnos are located in the west part of the island and at the Fakos Peninsula, Sardes, Roussopouli and Paradeisi hill. These areas are compared and validated with the reported field work. We conclude that hydrothermal alteration zones can indeed be detected and mapped using medium resolution satellite multispectral data. However, for the identification and mapping of specific types of rocks and minerals, a sensor with high spectral resolution is required.

Full text

Bulletin of the Geological Society of Greece
Vol. 50, 2016
HYDROTHERMAL ALTERATION ZONES
DETECTION IN LIMNOS ISLAND, THROUGH THE
APPLICATION OF REMOTE SENSING
Anifadi A. Harokopeio University of
Athens, Department of
Geography
Parcharidis Is. Harokopeio University of
Athens, Department of
Geography
Sykioti O. Institute for Astronomy,
Astrophysics, Space
Applications & Remote
Sensing
http://dx.doi.org/10.12681/bgsg.11879
Copyright © 2016 A. Anifadi, Is. Parcharidis, O. Sykioti
To cite this article:
Anifadi, Parcharidis, & Sykioti (2016). HYDROTHERMAL ALTERATION ZONES DETECTION IN LIMNOS ISLAND,
THROUGH THE APPLICATION OF REMOTE SENSING. Bulletin of the Geological Society of Greece, 50, 1596-1604.
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Δελτίο της Ελληνικής Γεωλογικής Εταιρίας, τόμος L, σελ. 1595-1604
Πρακτικά 14ου Διεθνούς Συνεδρίου, Θεσσαλονίκη, Μάιος 2016
Bulletin of the Geological Society of Greece, vol. L, p. 1595-1604
Proceedings of the 14th International Congress, Thessaloniki, May 2016
HYDROTHERMAL ALTERATION ZONES DETECTION IN
LIMNOS ISLAND, THROUGH THE APPLICATION OF
REMOTE SENSING
Anifadi A.1, Parcharidis Is.1 and Sykioti O.2
1Harokopeio University of Athens, Department of Geography, Εl. Venizelou 70, 176 71, Athens,
Greece, parchar@hua.gr, alexandra.tragana@gmail.com
2Institute for Astronomy, Astrophysics, Space Applications & Remote Sensing Vas. Pavlou & I.
Metaxa, GR-15 236 Penteli, Greece, sykioti@noa.gr
Abstract
In this study we use Landsat 8 OLI satellite imagery in order to identify and map
alteration zones in Limnos island (N. Aegean, Greece). Pre-processing included sea
and vegetation masking. In order to enhance spatial resolution, data fusion to 15m is
performed. A lineament map is extracted from the panchromatic image that gives the
general tectonic view of the island. The detection and mapping of alteration minerals
is performed using specific band ratios and consequent composite images. The colour
composite using bands 10, 11, 7 (RGB) show the spectral signature and general
distribution of silica. Band ratios 6/7, 4/2, 6/5, reveal alteration zones containing iron
oxides, clay alteration and ferrous minerals correspondingly. The aforementioned
analysis has shown that hydrothermally alteration areas in Limnos are located in the
west part of the island and at the Fakos Peninsula, Sardes, Roussopouli and Paradeisi
hill. These areas are compared and validated with the reported field work. We
conclude that hydrothermal alteration zones can indeed be detected and mapped
using medium resolution satellite multispectral data. However, for the identification
and mapping of specific types of rocks and minerals, a sensor with high spectral
resolution is required.
Keywords: Satellite data, Landsat 8 OLI, Miocene Volcanism.
Περίληψη
Στην παρούσα εργασία αναλύθηκαν τα δεδομένα του θεματικού χαρτογράφου Landsat
8, με σκοπό την διάκριση και αναγνώριση ζωνών υδροθερμικής εξαλλοίωσης στην
ευρύτερη περιοχή της νήσου Λήμνου. Η προ-επεξεργασία των δορυφορικών δεδομένων
αφορούσε την δημιουργία μάσκας της βλάστησης και της θάλασσας. Για να βελτιωθεί η
χωρική διακριτική ικανότητα στα 15 m έγινε συγχώνευση δεδομένων. Ένας χάρτης
γραμμώσεων παρήχθη από την πανγχρωματική εικόνα προσδίδοντας τη γενική
τεκτονική άποψη του νησιού. Η ανίχνευση και η χαρτογράφηση των εξαλλοιωμένων
πετρωμάτων πραγματοποιήθηκε χρησιμοποιώντας λόγους καναλιών και ακολούθως
σύνθετων ψευδέγχρωμων εικόνων. Η ψευδέγχρωμη εικόνa 10, 11, 7 (RGB) δείχνει την
φασματική υπογραφή και την κατανομή των πυριτικών ορυκτών. Οι λόγοι καναλιών 6/7,
4/2, 6/5, αποκαλύπτουν ζώνες εξαλλοίωσης που περιέχουν οξείδια του σιδήρου,
αργιλική εξαλλοίωση, και σιδρούχα (Fe 2+) ορυκτά. Η ανάλυση έδειξε ότι οι
υδροθερμικά εξαλλοιωμένες περιοχές στη νήσο Λήμνο τοποθετούνται στα δυτικά της
Λήμνου, στη χερσόνησο του Φακού, στις Σάρδες, στο Ρουσσοπούλι και περιμετρικά στο
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λόφο Παραδείσι. Αυτές οι περιοχές συγκρίθηκαν και τεκμηριώθηκαν με εργασίες πεδίου
που πραγματοποιήθηκαν από προηγούμενους ερευνητές. Συνοψίζοντας, οι
υδροθερμικές ζώνες εξαλλοίωσης μπορούν να εντοπιστούν και να χαρτογραφηθούν
χρησιμοποιώντας μέτριας ανάλυσης δορυφορικά πολυφασματικά δεδομένα. Ωστόσο, για
την αναγνώριση και χαρτογράφηση συγκεκριμένων τύπων ορυκτών και πετρωμάτων,
απαιτείται ένας αισθητήρας υψηλής φασματικής ανάλυσης.
Λέξεις κλειδιά: Δορυφορικά δεδομένα, Landsat 8 OLI, Μειοκαινική ηφαιστειότητα.
1. Introduction
The goal of the present paper is to detect the hydrothermal alteration zones in Limnos Island, N. Aegean,
through the application of Landsat 8 OLI band ratios. The key elements in mineral exploration are to
gain understanding of geologic area through lithological mapping and to assist in defining target areas
of potential mineral interest. Remote sensing can assist and provide valuable information in bedrock
mapping, detection, identification and estimating affluence of specific minerals at a specific scale
(Ahmed and Beiranvand Pour, 2014; Sabins, 1999; Parcharidis et al., 1998; Hunt, 1977). In Limnos
Island, field geological studies have referred the detection of hydrothermal alteration zones in several
sites like Sardes, Roussopouli and Fakos peninsula (Papoulis et al., 2014; Fornadel, 2010; Papoulis et
al., 2009; Skarpelis and Voudouris, 1998). Positive results can be obtained using band rationing and
false colour using these ratios. Limnos island is located at the North Aegean sea in Greece. The island
occupies 476 Κm2 with a coastal line of 260 Km.To sum up the hydrothermal alteration zones can
indeed be detected and mapped using medium resolution satellite multispectral data but it is not
possible to identify and map specific types of rocks and minerals.
2. Geologic Settings
Figure 1 - Digitized geologic map of Limnos island (after IGME scale 1:50000).
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2.1 Stratigraphy
Limnos is an island of Greece in the northern part of the Aegean Sea. The principal town of the island
and seat of the municipality is Myrina. The island is mostly flat (hence its more than 30 sand beaches),
but the west, and especially the northwest part, is rough and mountainous. The main gulfs are
Moundros and Pournia, but the rock weathering creates many coves. The areas with high frequency, a
dense hydrographical system and big slope use to be faults with direction NW-SE, NE-SW. Generally,
at the center and east of the island the rocks are permeable (Quaternary) so the hydrographical system
is poor. On the other hand, at the rest of the island the hydrographical system is dense (volcano rocks).
2.2 Geology
The geology of Limnos Island is characterized by a sedimentary background which is a basin-fill
succession. Hydrothermal alteration in the island is linked to early Miocene volcanism that occurred
in the broader north-eastern Aegean Sea and Western Turkey. The remnants of large stratovolcanoes
are present in specific areas in the islands of Lesvos, Limnos and Samothraki and in western Turkey.
The sedimentary rocks are flysch and molasse. They were deposited in NE-SW trending
postorogenic basin that formed as a result of normal faulting and extension during postorogenic
collapse of the Rhodope-Sakarya zone and were slightly folded prior to igneous activity. The
Tertiary sedimentary basement rocks can be delineated into two discrete units, the Upper Unit and
the Lower Unit. The Upper Eocene to lower Oligocene Lower Unit covers the majority of the island
and is composed of siliclastic continental slope deposits including conglomerates, sandstones,
mudstones, claystones and turbidites. The lower Oligocene Upper Unit has been deposited in a
shallower environment than the Lower Unit. Lower in its section, the Upper Unit is composed of
marine and brackish fluviodeltaic sediments including interbedded claystones and sandstones,
sandstones and sandy limestones. Towards the top of its exposure, the Upper Unit is composed of
terrestrial fluvial sediments including conglomerates and sandstones. The volcanic centers are
located in the western and southwestern portions of the island where volcanic rocks overlie the
sedimentary basement. The presence of the volcanic centers is delineated by domes and lava flows
that are accompanied by lesser agglomerate. The sedimentary basement is exposed at the surface in
the east and northeast of the island, distal to the volcanic centers. The volcanic rocks are divided
into three units: Katakolon, Romanou and Myrina. These rocks are early Miocene (21-18 Ma) and
demonstrate a calc-alkaline to shoshonitic affinity. The lower-most Katakolon unit consists of NW-
SE trending K-rich andesitic to dacitic lavas. In places, it is interbedded with or is crosscut by
andesitic lava flows monomineralic breccias, sills and E-W trending dikes. Andesite and dacite in
the Katakolon unit yielded a K-Ar age of 20-21 Ma. The Katakolon unit is overlain by the Romanou
unit that is composed of K-rich dacites and latites. At its base, the Romanou unit is dominated by
ligh- colored lithic and pumice-rich pyroclastic flows that are up to 160m thick. To the west and
upsection, the pyroclastic flows of the Romanou unit are intercalated with volcanic breccias,
banakitic lavas, airfall tuffs and terrigenous sediments. Ignimbrites and andesites from the Romanou
unit yielded K-Ar ages of 19.8 Ma. The uppermost Myrina unit, overlies Romanou unit and is
composed of K-rich dacite with lesser amounts of andesite and trachyte, which are associates with
monomineralic breccias, lava lows, and lahars. Lavas, dackites and andesites of the Myrina unit
yielded K-Ar ages of 19.3 to 18.2 Ma. Both volcanic and sedimentary basements of Limnos Island
are overlain by a Pliocene to recent alluvial sedimentary unit that is composed of conglomerates,
calc-arenites and sandstones. Faults and joints cut-cross both sedimentary and igneous rocks. The
axes trend E-W and WSW-ENE to the WSW. Folding does not affect the Miocene volcanic rocks.
Limnos Island is located in the area of Aegean Sea that is characterized by a moderate positive heat
flow anomaly. This anomaly, in conjunction with active hot springs found on the island, indicate
that a steepened thermal gradient has persisted even after the end of observable igneous activity on
the island (Skarpelis and Voudouris, 1998; Fornadel, 2010). The presence of hot springs on the
island implies that brittle structures on the island play a role in conducting fluids (Fornadel, 2010).
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2.3 Metal bearing
The area of Fakos peninsula is dominated by two large hills, the western Tourlida Hill and the
Petrospitos Hill both of which are 300 m in elevation. Their prominence is controlled by subvolcanic
intrusions that were emplaced into the sedimentary host rocks. The sedimentary basement on Fakos
peninsula is composed largely of medium-grained quartz - rich sandstones that were subjected to, and
cemented by a hydrothermal silicification event. Finely disseminated sulfides are pervasive in these
sandstones. The extrusive rocks on Fakos Peninsula range from shoshonitic andesites (latites) to
trachyandesites and trachytes. Towards the central portion of Fakos peninsula, the extrusive
sedimentary basement rocks were intruded by subvolcanic microporphyritic quartz monzonite. Much
of the southwestern portion of Limnos Island was subject to hydrothermal alteration along fault zones.
Four discrete zones of hydrothermal alteration based on clay mineralogy were defined as smectite,
illite, hallousite and kaolinite-dickite zones. The Fakos Peninsula like the rest of Limnos island is
crosscut by many major NE-SW and ENE-WSW-trending faults. These structures controlled the
emplacement of the subvolcanic bodies and facilitated the flow of hydrothermal –magmatic fluids that
were responsible for metallic mineralization. Fakos quartz monzonite and adjacent host rocks were
locally subjected to intense hydrothermal alteration. In silica zones there is a metal bearing, to the south
of the area and especially to the quartz veins within the sandstones and to the quartz monzonite. At the
western metal bearing zone in the quartz veins with direction N55ο W και N70οE. The east metal
bearing zone, large 1 Km and wide 10m, is located about 600 m SE of the central zone and it is
characterized by the major concentration of gold of the Fakos Peninsula. In the Sardes area, a system
of quartz is developed inside the subvolcanic and sandstones and is connected with faults systems of
direction Ν55ο W, Ν70ο Α (like in Fakos area). In the Roussopouli area: three zones of black silification
are observed in the volcanic breccias. The silification is opaline and is connected with sericitic
alteration of the adjacent rock. The zone of alunite is developed up from the silicification zone. The
metal-bearing includes pyrite, marcasite and veinlets of silica (Voudouris and Skarpelis, 1998).
3. Materials and Methods
3.1. Remote sensing data
Landsat 8 is the new product from NASA under Landsat open source series which has been launched
in February 2013. Landsat 8 data consist of 11 bands; 5 in the visible and Near-Infrared (VNIR), 2
in the Thermal Infrared (TIR) region of the electromagnetic spectrum, 2 in the Shortwave Infrared
(SWIR) region, and 1 panchromatic band (band 8). The spatial resolution is 15 m for the
panchromatic band, 30 m for VNIR and SWIR bands, and 100 m for the TIR bands. Two additional
bands represent the difference between Landsat8 and the previous product (Landsat ETM+), a deep
blue coastal / aerosol band and a shortwave-infrared cirrus band (table 1).
Table 1 - Bands of Landsat 8.
BAND
WAVELENGHT
(micrometers)
RESOLUTION
(meters)
Band 1 - Coastal aerosol
0.43 - 0.45
30
Band 2 - Blue
0.45 - 0.51
30
Band 3 - Green
0.53 - 0.59
30
Band 4 - Red
0.64 - 0.67
30
Band 5 - Near Infrared (NIR)
0.85 - 0.88
30
Band 6 - SWIR 1
1.57 - 1.65
30
Band 7 - SWIR 2
2.11 - 2.29
30
Band 8 - Panchromatic
0.50 - 0.68
15
Band 9 - Cirrus
1.36 - 1.38
30
Band 10 - Thermal Infrared (TIRS) 1
10.60 - 11.19
100
Band 11 - Thermal Infrared (TIRS) 2
11.50 - 12.51
100
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The Landsat 8 Oli image which has been used in this study cloud free acquired on August 16 2014.
The sun azimuth is about Β139ο and the sun elevation about 57ο.
3.2. Image processing
The initial DN values were converted to reflectance through atmospheric correction of the initial
image. In Fig. 1 a flowchart showing with the processing steps is presented. The following four
images were then produced. A colour composite image with the spectral bands 7, 5, 3 (RGB) in
order to distinguish the lithological units from the vegetation (Fig. 2).
Figure - Flow chart: processing steps.
The Normalized Difference Vegetation Index (NDVI) in order to discern the vegetation distribution
and consequently mask of vegetated areas. A colour composite image using the thermal bands tir1-
tir2-swir2 (10-11-7) (RGB) for silicate mapping (Fig.3).
The colour composite ratio image 6/7, 4/2, 6/5 (RGB). The ratio 6/7 reveals clays, the 4/2 iron oxides
and the 6/5 the ferrous (Fe2+) minerals. This colour composite was produced after data fusion data
(15m) (Fig. 4) and without data fusion data (30m) (Fig. 5).
Image Landsat 8 Oli
L1
pre-processing of the image: converting the digital numbers of the image to
reflectance through atmospheric correction of the initial image.
Lineaments
(faults)
Data fusion (Panchromatic and
multispectral bands)
Detect silica and no silica
False composite color image
(FCC) 10,11,7 (RGB)
γραμμώσεων
Color Composite image of
Band Rationing (CCR)
6/7, 4/2, 6/5 (RGB)
γραμμώσεων
Analyse the landscape
γραμμώσεων
False composite color image
(FCC) 5,7,3 (RGB)
Sea mask
Mask NDVI
Band Ratio Spectral Bands
6/7, 4/2, 6/5
Detection of hydrothermally altered zones
γραμμώσεων
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Figure 2 - colour composite image 7, 5, 3 (RGB).
Figure 3 - Silica distribution. Silica rocks yellow colour and no silica purple (10-11-7) (RGB).
Figure 4 - composite ratio image 6/7 (clays) 4/2 (FeO) 6/5 (Ferrous) (RGB). After data fusion (15m).
The lineaments that were extracted from the panchromatic image (band 8) provided the general
tectonic view of the island.
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Figure 5 - composite ratio image 6/7 (clays) 4/2 (FeO) 6/5 (Ferrous) (RGB). Without data
fusion. (30 m) the black area is the vegetation mask and the sea mask.
Figure 6 - Left: the main hydrothermal alteration zone in Fakos Peninsula. Right: Limits of
hydrothermally alteration zones in Fakos Penisnula by Fornadel, 2010.
Figure 7 - Left: Lineaments issued from the panchromatic image of Landsat 8 OLI. Right:
The lineament directions are shown in the rose diagram (by demo surfer 11 golden).
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4. Results and Discussion
The colour composite image 7, 5, 3 (RGB) can give an analysis of the landcover. The red and
brownish areas correspond to vegetation, while the white colour corresponds to rocks and soil.
Generally, the vegetation in the island is very low, and as it is shown in fig. 2 the vegetation extends
mainly in drainage systems and hills. The colour composite image 10,11,7 (RGB) shows the spectral
signature and distribution of silicate. Yellowish and yellow colours correspond to areas with silica
presence and purple to areas of absence of silica as it is shown in Fig. 2. The Figures 4, 5 and 6 show
the areas with hydrothermal alteration zones.
 Alteration in Fakos Cape: A zone about 16 km at the south of Fakos cape which separates the tints of
red-yellow from tints of blue-cyan. Inside the alteration zone the tints of yellow shows the high
reflectance at bands 6 and 4 and low reflectance at other bands 2, 7, 5. The different tints of yellow
indicates the predominance one of the two kind of rock (iron oxides-clay minerals) (Parcharidis et al.,
1998). The tints of blue-cyan perimetricaly external of the alteration zone are referring to ferrous-iron
oxide (high reflectance to band 4). The geological bedrock is characterized by ploutonian rocks that
have intruded in the sediments age Upper Eocene-Oligocene and present strong alteration (granites,
syenites, diorites, biotite). The alteration products of trachiandesites are clays and iron oxides (serikite,
chlorite, calcite, iron oxides). Also, a smaller alteration zone (~3 km) exists at NE of Fakos cape and
the geological bedrock consists of trachiandesites. Unfortunately because of the low spectral analysis
of Landsat 8 OLI it is impossible to detect and map specific rocks. Furthermore, the mask of vegetation
does not allow the possibility of vegetation existence where there is a high reflectance in 5 and 6 bands.
Also in that area the rocks have impregnated with iron oxides (geological map of IGME) which means
high reflectance at band 4. Fornadel, 2010 has mentioned the existence of metallic minerals in the
western ore zone that have been oxidized, as denoted by the abundance of iron oxides (i.e. limonite,
goethite) in the vein material, and largely disseminated in the vein matrix, although locally it forms ≥1
cm wide aggregates or infillings. The metallic minerals include pyrite, chalcopyrite, sphalerite, galena,
arsenopyrite, tetrahedrite, bournonite, hessite, altaite, and native gold. These minerals can be detected
with hyperspectral data. At the NE in Fakos cape there is cyan colour (width ~ 300m and length ~ 2
km) due to the fact that there are iron oxides according to the geological map of IGME. The geological
bedrock consists of silificated volcanic rocks whose initial composition has change from the influence
of hydrothermal fluid which are rich to SiO2 through faults. There are reddish lavas because of the
abidance of iron oxides. Fornadel, 2010 mentioned about a veins system which penetrates the silica
alteration zone and the adjacent rocks. The veins consist of small quantities of tourmaline, barite and
sericite. Ore minerals in the eastern ore zone include galena, sphalerite, arsenopyrite, and bournonite.
The silica distinguishment can be confirmed at the map in fig. 3. The alunitic alteration zone, as well as
the topographically higher silicic alteration zone, is crosscut by hydrothermal breccias in which
alunitized rock fragments are surrounded and cemented by iron oxides. Alunite also occurs in veins,
which consist of alunite, sulfur, and tridymite/cristobalite that crosscut sericitized rock in the northern
part of the study area.
 Other alteration in the island: At the NW of the island near Sardes and at the west coast there are
small areas with hydrothermal alteration, as well as, at the east of the island in Roussopouli near
to the contact with the tuffs. Finally, parametrically of Paradeisi hill, is seemed to be an alteration
zone around the vegetation (black color) and at the west Fig.5. At the geological map of IGME
this area is characterized of sediments (Up. Heocene-Oligocene) and at the west there is a contact
with trachiandesites. At Paradeisi hill, geological map shows impregnation of iron oxides and
sulfides.
5. Conclusion
The aim of this study was to conduct an investigation using Landsat 8 data and remote sensing
techniques to map the alteration zones in Limnos Island. The outcome of the remote sensing techniques
such as colour composite and band ratios are promising in mapping lithological and altered rocks. Band
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ratio technique showed the distribution of the alteration zones. The results showed that Landsat 8 data
have the potential to detect and map hydrothermal alteration zones at a regional scale.
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