Lithologic Mapping of Mafic Intrusions in East Greenland Using 

Landsat Thematic Mapper Data. 

H. R. Naslund 

Department of Geological Sciences, State University of New York, 

Binghamton, NY 13901 

R. W. Birnie 

Department of Earth Sciences, Dartmouth College, Hanover, NH, 03755 

J. T. Parr 

The Analytical Sciences Corporation, Reading, MA, 01 867 

Final Report for Contract # NAS 5-28738 

April 24, 1989 
Table of Contents 

Introduction 

Field Research 

Laboratory Research 

Digital Processing of Th m tic Mapper Imagery 

Processing Environment and Objectives 

Imagery of the Skaergaard and Vicinity 

Merging Multi-Temporal TM Imagery 

Band Ratios Images 

Other Image Enhancement Techniques Employed 

Classification of Skaergaard Imagery 

Imagery of Other East Greenland lntrusives 

Mineral Resourse Evaluation 

Student Theses resulting from NAS 5-28738 

Publications resulting from NAS 5-28738 

Appendix 1 - Applications of Landsat Thematic Mapper and 

Ground Based Spectrometer Data to a Study of 

the Mafic Intrusions of East Greenland 

Calibration of Fibrefrax Standard and Effect 

of Different Illumination Angles 

TM Imagery of the Skaergaard intrusive center 

TM Imagery of the Kangerdlugssuaq, Kap Edvard 

Holm, Gardiner, Kruuse Fjord, Imilik, Lilloise, 

and Borgetinderne intrusive centers 

Appendix 2 - 

Appendix 3 - 

Appendix 4 - 

3 

5 

8 

9 

9 

10 

12 

13 

15 

16 

19 

20 

21 

22 

25 

42 

50 

57 I 

2 
Introduction 

The East Greenland Tertiary Igneous Province contains a variety of 

intrusive and extrusive rock types. Intrusive rock units include layered 

tholeiitic gabbro sills, macro-dikes, and plutons; alkaline gabbro, syenite, 

and granite plutons; and several episodes of tholeiitic and alkaline dike 

swarms. Extrusive rock units include alkaline and tholeiitic flows, tuffs, 

and agglomerates, which form an 8 km thick sequence of flat lying plateau 

lavas. The majority of the igneous activity occurred during the period from 

60 to 50 my. ago as Greenland was rifted from northern Europe during the 

opening of the north Atlantic Ocean. The intrusive rocks in the province 

form a series of plutonic centers exposed along an 800 km long segment of 

the East Greenland coast. The plateau lavas are exposed in the northern half 

of the province, but have been removed by erosion in the southern half. As a 

result, the host rocks for the plutonic centers in the northern half of the 

province are largely basaltic lavas, and the host rocks for the plutonic 

centers in the southern .half of the province are largely Archean 

quartz-feldspar gneisses and amphibolites. Additional volcanic rocks and 

plutonic centers may be present in the province offshore or under the inland 

ice field. Layered tholeiitic intrusions are the primary sources of Pt and Pd, 

, 

two strategic metals for which South Africa and the Soviet Union are the 

principal producers and the United States and Japan are the largest 

consumers. This study was initiated with the idea of using TM data to help 

locate potential Pt and Pd targets in the layered tholeiitic intrusions of the 

East Greenland Tertiary Igneous Province. 

The Skaergaard complex is the most well known of the intrusive 

centers. It contains a central layered tholeiitic pluton, several associated 

3 
layered tholeiitic macro-dykes and sills, and numerous quartz and 

felspar-rich granophyric bodies ranging from dikes only cms wide to sills 

up to 100 m thick. The central pluton, which is approximately 5 by 8 kms 

in plan view, has undergone an extensive differentiation history from an 

initial Mg-rich magma to a final Fe-rich magma. This differentiation 

history is recorded in the rocks which crystgllized on the floor (the 

Layered Series), the walls (the Marginal Border Series), and the roof (the 

Upper Border Series) of the magma chamber. A number of distinctive rock 

types were formed during this differentiation process, and include from 

the base of the intrusion upward (i.e. within the Layered Series): olivinepyroxene-plagioclase gabbro (Lower Zone 1 ); olivine-pyroxeneplagioclase-magnetite gabbro (Lower Zone 2); pyroxene-plagioclasemagnetite gabbro (Middle Zone): fayalite-pyroxene- plagioclase-magnetite 

gabbro (Upper Zone 1); and fayalite-pyroxene- plagioclase-magnetiteapatite gabbro (Upper Zone 2). In addition to mineralogical units within 

the pluton, additional units can be defined on the basis of grain-size and 

texture. In particular the units of the Upper Border Series are coarser 

grained than those of.the Layered Series, and the units of the Marginal 

Border Series are texturally distinct from those of the Layered or Upper 

border Series. The systematic variation in the chemical composition of 

the magma as it crystallized, resulted in recognizable gradational 

variations within many of the units (particularly with regard to iron 

content). TM data has been used to try to identify two types of changes in 

the intrusion: (1) abrupt changes in rock type caused by the presence or 

absence of particular mineral phases, and (2) gradational changes in rock 

type caused by systematic compositional variations. The host rocks for the 

4 
Skaergard intrusion, which is located in the middle of the province, include 

Archean gneiss and amphibolite on one side and Tertiary basaltic lavas on 

the other. The Skaergaard complex was chosen as the training site for this 

project because of the excellent exposures, the variety of rock types 

present, and because the geology of the complex is well known. It was hoped 

that information gained from TM analysis of the Skaergaard intrusion could 

be applied to other intrusive complexes in the province where the access is 

more difficult and the geology is not as well understood. 

Field Research 

A 1985 expedition to the field area consisted of five scientists: Dr. H. 

R. Naslund, P. A. Turner, D. W. Keith, J. Urquhart, and C. 6. Brinkema. Our 

field research was concentrated on the area in the vicinity of the 

Skaergaard intrusion. During the field season a number of representative 

areas were chosen for each of the rock types that we hoped to map with the 

TM data. We also noted areas with unusual surface conditions (gravel cover, 

scattered snow patches, mineral staining, etc.). Owing to technical 

problems with the satellite, we were only able to receive TM data from two 

1985 scenes: one collected on July 24a; and one collected on August 9B. 

Because of the heaviei snow and poorer weather conditions for the July 2@ 

scene, we have concentrated our data interpretation efforts on the August 

9a scene. In addition to identifying test sites for Landsat mapping we 

collected a number of rock samples in order to determine representative 

rock compositions and to evaluate PVPd resourse potential. These samples 

were used to complete three masters thesis projects, and one bachelors 

degree project. 

5 
Ten scientists accompanied the 1986 expedition to East Greenland, 

August 2nd 1986 to September 2nd 1986. Expedition members included Dr. H. 

R. Naslund, Dr. R. W. Birnie, Dr. Robert Bindschadler, Daniel Barnett, Jennifer 

Nichols, Max Cobb, J. T. Parr, P. A. Turner, James Foster, and Mark Hirschman. 

During the 1986 field season we examined areas where our earlier TM data 

were not able to distinguish different rock types, in order to determine 

what surface features interfere with the TM mapping technique. We also 

examined areas where we obtained different TM signatures from what we 

had assumed were identical rock types. Field work was directed toward 

collecting TM spectra of representative rock and snow units using a 

tripod-mounted ratioing spectrometer (HHRR). The HHRR allows direct 

correlation of observations made in the field to the TM data collected by the 

satellite, and can be used to determine what surface features most strongly 

affect the TM signature recorded for the 30 x 30 meter pixels. The HHRR 

receives a signal from an approximately 100 cm2 area, so it can be used to 

compare the TM signatures for a variety of surface conditions (wet rock, dry 

rock, weathered rock, unweathered rock, stained rock, fresh rock, etc.). Test 

spectra of plant materials, mineral stains, and soil areas were also 

collected. Additional rock samples were collected from the Skaergaard 

intrusion and from the Kraemer Island Macrodyke intrusion. Field Results 

were used to complete one masters thesis and two bachelors theses. 

During the 1986 field season we provided logistical support for two 

scientists (R. Bindschadler and J. foster) from the Goddard Space Flight 

Center in Greenbelt, Maryland who collected field data on snow levels and 

snow moisture content on some of the alpine glaciers in the field area. They 

planned to try to correlate this data with TM data collected during the same 

6 
period. The long term objective of this project is to allow glacial snow 

budgets to be evaluated by TM data. This project is being carried out in 

cooperation with Dr. Dorothy Hall of the Goddard Space Flight Center in 

Greenbelt, Maryland. We also provided logistical support to Marc 

Hirschmann, a Masters degree candidate from the University of Oregon, 

who was studying granophyric dikes and sills in the Skaergaard 

intrusion. Mr. Hirschmann's thesis was indirectly supported by this 

project but is not included with the list of "Student Theses resulting 

from NAS 5-28738" (Hirschmann, Marc M., 1988, Petro logv 0 f the 

JrarlSgressive Granonhvres from the Skaerwrd Intrusion. E& 

Greenland, MS Thesis, The University of Oregon, Eugene, OR). 

Additional field observations were made during July and August of 

1988 by the PI with the goal of making on-site observations in areas 

where the TM images gave contradictory information, and obtaining 

more field data on the nature and distribution of surface stains and 

lichen cover in the field area. In addition, a number of oriented 

samples from the Skaergaard, Basistoppen, and Vandfaldsdalen 

intrusions were collected for petrofabric studies to determine the 

extent of preferred mineral alignments within these intrusions. Such 

preferred mineral orientations may result in increased specular 

reflection on some outcrop surfaces. The nature of mineral alignments 

in these rocks is also of interest because of its potential for providing 

insights into the crystallization processes responsible for the present 

distribution of chemical constituents. The 1988 expedition included Dr. 

H. Richard Naslund and Brian W. Stewart, a PhD candidate at The 

University of California at Los Angeles. Mr. Stewart's PhD Dissertation, 

7 
which will be completed'in the Fall of 1989, was indirectly supported by 

this project but is not included in the list of "Student Theses resulting from 

. Laboratory Research 

Laboratory research for this project included image processing of TM 

data under the direction of J. T. Parr at TASC, and processing of HHRR and 

topographic data under the direction of R. W. Birnie at Dartmouth College. 

The details of the image processing are presented in the following section 

of this report (Digital Processing of Thematic Mapper Imagery) and selected 

images are presented in appendices 3 (TM Imagery of the Skaergaard 

intrusive center) and 4 (TM Imagery of the Kangerdlugssuaq, Kap Edvard 

Holm, Gardiner, Kruuse Fjord, Imilik, Borgetinderne, and Lilloise intrusive 

centers). The results of the HHRR study are presented in appendices 1 

(Applications of Landsat Thematic Mapper and Ground Based Spectrometer 

Data to a Study of the Mafic Intrusions of East Greenland) and 2 (Calibration 

of Fibrefrax Standard and Effect of Different Illumination Angles). The 

correlation between topography and TM data in the Western part of the 

Skaergaard intrusion was investigated by M. K. Cobb and formed the basis for 

his Batchelors thesis at Dartmouth College (Analysis of the Topographic 

Effects on Landsat Spectral Brightness: Kraemer Island, Skaergaard 

Intrusion, East Greenland). 

8 
Digital Processing of Thematic Mapper Imagery 

Processing Environment and Objectives. 

All digital image processing for this study was accomplished by 

The Analytic Sciences Corporation (TASC) using the resources of its 

Computing Technology Center (CTC). At the initiation of the program, 

the image processing facilities were hosted on a DEC VAX 11-785. 

During the course of this effort that equipment was upgraded. All 

image processing results presented within this document were prepared 

- 

using the new configuration, comprising (in part) an Alliant FX/8 

mini-supercomputer and a Gould/DeAnza Model IP-8500 image processor. 

This sytem operates under Alliant Concentrix (a UNIX-like operating 

system). The image processing software used is part of the TASC 

. 

Interactive Image Processing System (TIIPS), a C language based 

package of algorithms developed by TASC. Fortran subroutines are used 

within the more 

of the Alliant's parallel architecture. 

computationally intensive programs to take advantage 

TASC's role in this study was to utilize its imaging expertise and 

computer resources in the processing and enhancement of the Landsat 

Thematic Mapper (TM) imagery. Initially, the TM data was processed 

to provide base maps for use in the field portion of the study. 

Preliminary enhancements and attempts at lithologic classification 

were also made for use during the second field season (1986). This 

report discusses the final image processing results. These include 

various efforts aimed at lithologic discrimination and classificaticn 

of units in the vicinity of the Skaergaard test area, and a 

9 
preliminary effort at discrimination of units around seven other 

Tertiary intrusions in East Greenland. 

Imagery of Skaergaard and Vicinity 

For ease of interpretation by field personnel, some of whom had 

minimal backgrounds in remote-sensing, a basic false color band 

composite image was used as the standard reference for imagery . 

developed for use as base maps in the field. For this purpose, 

composites were generated using TM band 2 (blue), band 3 (green), and 

band 4 (red). The bands were each interactively enhanced using an 

interactive, non-linear (piecewise linear) contrast stretch to 

optimize discrimination of the regi'onal geology. band 1 was used 

minimally in this study due to the frequent saturation of the detector 

on the abundant snowcover, and the time dependent biases resulting 

therefrom. While this band combination is sufficient to distinguish 

the gabbro at Skaergaard from the adjacent Precambrian gneiss, it 

enables little other lithologic discrimination. 

In an effort to distinguish variations within the gabbro and other 

units, a variety of band enhancements and band composites were 

evaluated. As noted above, band 1 tended to be rather noisy in this 

environment, and bands 1 and 2 were very highly correlated. 

Additionally, bands 5 and 7 were also highly correlated. A band 5/7 

ratio had esentially no variance for areas of geologic interest. The 

best band composites for the Skaergaard area were generated using 

band 3 (blue), 

discrimination 

band 4 (green), and band 5 

of the gabbro, gneiss, and 

(red). These enabled both 

basalt, as well as the 

10 
definition of some stucture with each of these units. The success 'of 

this band combination was, however, highly dependent on the use of the 

interactive contrast stretch. Because of the low reflectance of the 

gabbro and basalt, variations within these units are expressed as only 

a few gray levels. The sensitivity of a good interactive tool is 

essential to the analysis of this data. 

While preliminary evaluation was performed using imagery acquired 

during the summer of 1985, the results were not particularly 

satisfying. Snowcover that season was unusually high, and a failure 

in the Landsat data downlink precluded image collection after 

13 August. Maximal snowmelt generally occurs in September. A 

tradeoff must be made between mimimizing the snowcover and acceptance 

of greater shadowing, since the sun elevation is steadily decreasing 

after the summer solstace. The latitude at Skaergaard is 

approximately 68 degrees north. In mid-August the apparent sun 

elevation is about 35 degrees, but by mid-September it is down to 25 

degrees. Since local terrain relief is slighly in excess of 1000 

meters, a serious compromise.between shadowing and snowmelt must be 

made. Unfortunately, the snowcover during the 1986 season was again 

greater than normal for the region, so lower sun elevations became a 

fact in the TM acquisitions actually used for this study. The final 

evaluations of the Skaergaard locality were made using imagery from 

both 8 August 1985 and 13 September 1986. 

11 
Merging of Multi-Temporal TM Imagery 

Since extensive snowcovel was such a serious problem in the 

evaluation of the Skaergaard imagery, approaches enploying 

multi-temporal coverage were investigated. The most significant 

problem presented by the snow was the partial coverage prevalent in so 

many of the TM pixels. This, of course, has the impact of 

contaminating the apparent spectral reflectance of such pixels. Since 

many of these contaminated pixels are not contiguous with pixels 

obviously containing snow, the real problem is simply one of 

recognition. 

To mitigate this problem, the best images from each of the 1985 

and 1986 seasons were co-registered using a standard polynomial 

warping algorithm. Then, using data from areas known (from field 

photography) to be snow free, a transform (lookup table) was designed 

to'effect a radiometric balancing of the 1986 inage to the 1985 scene. 

This was done independently for each of the spectral bands, using 

control areas with a broad diversity in spectral characteristics. Once 

this transformation was accomplished the two scenes were compared on a 

pixel by pixel basis, again for each TM band. For bands 1-4, the 

assumption was made that as subpixel snowcover was reduced, the 

apparent brightness would decrease: therefore, a nerged image was 

created using the lesser of the reflectances from the 1985 and the 

radiometrically balanced and co-registered 1986 data. Since snow is 

non-reflective in the short wave infrared, the brightening was 

assumed to imply reduced snowcover and the greater of the two 

12 
reflectances was used in the construction of the merged images for 

bands 5 and 7. Because of wind, terrain relief, and running watw 

over many surfaces, the thermal infrared data were not found to be 

useful to this study, and no further processing of band 6 data was 

undertaken. 

It is recognized that the assumed associations of pixel 

reflectance with snowcover are not exclusively true. The changes in 

solar azimuth and elevation also produce changes in shadowing. The 

impact of direct shadows is obvious and can be accounted for during 

analysis of the imagery. More suble darkening of a surface due to 

surface roughness where the local solar grazing angle (relative to the 

actual terrain surface) is small is more problematic. In large 

measure this can be accounted for since the majority of areas impacted 

will be contiguous with regions in direct shadow. Any pixel can, 

however, be affected if the local roughness is sufficient. This will 

necessarily result in erroneous results from the merge process 

described above. Nevertheless, when viewed from a contextural 

perspective, the merged results appear to improve significantly the 

spatial coherency of the images and thus facilitate the geologic 

interpretation. These images were used for all subsequent studies of 

the immediate Skaergaard area. 

Band Ratios Images 

The calculation of band ratio images was motivated by two 

considerations. Perhaps most significant was the need to mitigate the 

lighting effects produced by the substantial terrain relief ar.d 

13 
subsequent variations in solar illumination of the surface. Of nearly 

equal interest, however, was the desire to enhance the effects of iron 

oxide and any hydroxyl absorption, and to test the band 5/1 ratio as 

an indicator of nagnetite abundance. In addition, as the Hand Held 

Ratioing Radiometer (HHRR) data became available after the 1986 field 

season, the importance of both lichen coatings and surface mineral 

staining were better defined. Both of these surface coatings tended 

to overwelm the subtle spectal differences among the various units 

within the Skaergaard gabbro. As suggested by the HHRF. data, band 

5/3, 4/3, and 3/1 ratios were also calculated. 

All band ratio images were derived from the raw TM data and 

subsequently scaled (linear clip and stretch) so as to maximize the 

discrimination of lithologic units. Presentation of that data with 

this report is in two basic formats. The first is a pseudocolor 

version of the stretched ratio images, where a low ratio appears blue 

in the iaage and a high ratio red: intermediate values change hue 

continuously through the visible spectrum. The second format is the 

band ratio composite, where each band ratio being used is assigned one 

of the three primary colors (red, green, or blue). In this format 

high ratio values contribute a larger fraction (intensity) of that hue 

to the composite image: hence, if the ratio represented by green has a 

very low value, green will' be absent in the composite, resulting in a 

blue-magenta-red hue. In order to improve lithologic discrimination, 

a11 ratio composite images have been contrast stretched by individual 

band ratio, using the non-linear interactive tool previously noted. 

14 
Other image Enhancement Techniques Employed 

Intensity-hue-saturation (IHS) transforms were also used in an 

effort to improve discrimination of the subtle lithologic differences 

among the Skaergaard units. The IHS technique was chosen to enhance 

the minor variations in hue which were manifested within the gabbroic 

units using both band and band ratio composites. This was 

accomplished primarily by an interactive contrast stretch in hue 

space. Additional benefits were derived by compressing intensity 

space so as to mitigate the distracting effects of dark shadow and 

very bright snow and ice surfaces. Improvement was also achieved by 

stretching in saturation space; the band ratio data associated with 

shadow, snow, ice, and water were decolored, while the saturation 

levels associated with the lithologic units were increased. The 

combined effect of these changes, when the image was inverse 

transformed back into red-green-blue space, was to improve the 

interpretability of the imagery. 

A final enhancement technique employed with the Skaergaard imagery 

involved the use of a principal component transformation. Since the 

image variance associated with snow, ice, water, and shadow is of 

little interest to the geologist, a multi-band synthetic image was 

first created by aggregating small patches of imagery, each of which 

was essentially free of the undesired factors. The patches were 

chosen from various sites around the Skaergaard area so as to obtain a 

reasonable distribution of lithologies. A covariance matrix was then 

computed from this TM image subset and applied to the full Skaergaard 

subscene. The resulting principal conponent iinases were then 

15 
evaluated, principal components 1, 2, and 4 appearing to contain the 

greatest lithologic information. A band composite imaqe was created 

with these, along with an alternative presentation using highly 

non-linear, negative stretches of these same principal component 

inages. 

Classification of Skaergaard Imagery 

Early in the study a supervised maximum likelihood classification 

of the August 1935 ixlagery of Skaergaard was attempted. Training 

cells for all major lithologic units as well as the various subunits 

within the Skaergaard intrusion were defined along with cells used to 

define snow, ice, seawater, turbid water, ponds, and shadow. No 

significant vegetation (except lichen and moss cover) exists in this 

region. The classification was highly confused, with even the major 

lithologic units being poorly defined. As previously reported, field 

work at Skaergaard has now identified several factors responsible for 

this inability to discrizinate successfully. Perhaps most significant 

was th2 abundance on subpixel scale snowcover. Also inportant is the 

extensive lichen and nineral coating found, especially with the 

gabbroic units: thus far there has been no totally consistent pattern 

discerned which associates these coatings with any particular rock 

chemistry or lithology. Another factor of significance is specular 

reflectance. The combination of low sun elevations and the preferred 

dip slope orientation of the layered series in the gabbro yields a 

bias toward the specular conponent being detected by Landsat. The 

abundact magnetite alteration, glacial polish, and thin sheets of 

16 
water from snowmelt all vere found to result in specular returns six 

to ten times brighter than the diffuse component. The color shift 

associated with these specular returns, though not quantified, was 

readily discernable in the field by eye. 

Given the minor differences in the composition and the measured 

HHRR spectra for the gabbroic subunits, confusion within the intrusion 

was not surprising. Subsequent classification efforts were aimed 

primarily at an improved discrimination of the basic lithologies - the 

gneiss, gabbro, and basalt. To mitigate the snowcover issue, further 

evaluations were based upon the multi-temporal merged data set. New . 

training cells were chosen, based upon field observations and 

photography, so as to better define representative, snow-free pixels. 

A maximum likelihood classification was run, using training 

classes for the full set of non-lithologic categories along with 

classes for the gabbro (as a whole), the Basistoppen sill, the gneiss, 

and the basalt. The result was improved relative to the initial, 

preliminary study; but the large number of classes still resulted in a 

significant degree of confusion, manifested as a lack of spatial 

coherency. Identification of the Basistoppen was particularly poor, 

often being confused with the gneiss. 

In an effort to improve these results, the non-lithologic classes 

were aggregated into a unifed sncw-ice, (all) water, and 

shadow-morraine categories. The Basistoppen was eliminated, but the 

Skaergaard was divided into five subunits (Lower Zone 1, Lower Zone 2, 

Middle Zone, Upper Zone 1, and Upper Zone 2). Divergence statistics 

(based upon training cell covariance) predicted reasonable success in 

17 
discriminating the basic lithologic units, but little success in 

separating any of the gabbroic units (except minor success with the 

Middle Zone). The actual classification upheld these expectations. 

The gabbro and gneiss were reasonably well discrin5nated (in 

conparison with field napping). The basalt to the southeast was 

identified along with an anomalous area on Kraeners Island (known 

asphibolites). Within the Skaergaard no discrinination was perceived 

except for perhaps 10-20 pixels of Middle Zone which were correctly 

identified. To eliminate sone of the statistical noise prevalent in 

this classification, a 3 by 3 pixel median filter was then used to 

produce an image with somewhat higher spatial coherency. This image 

represents the most successful effort to date in using Landsat TM 

imagery to discriminate the lithologic units in the vicinity of 

Skaergaard. 

A clustering algorithm was used in a final attempt to discriminate 

gabbroic subunits. Using the training cells previously identified, 

statistics werc coc2iled using the band 3/1, band 5/3, and 5/1 ratios. 

The algorithm was run in an attempt to further split the gabbroic 

unit. Convergence was nsver achieved by the algorithn, again 

indicating the spectral similarity of the subunits. Though the rnatter 

has not Seen thoroughly malyzed, it is suspected that sensor 

quantization error ray be a liiniting factor in th+ discrimination of 

these very dark nafic and ultrarr,afic units. 

18 
Imagery of Other East Greenland lntrusives 

. The original objective was to extend the classification results 

from Skaergaard to other known intrusive bodies in the East Greer,land 

region. 

imagery came through the merging of multi-temporal data, 

classification of the other intrusions was precluded (no appropriate 

1985 data had been obtained due to the Landsat downlink failure). 

was subsequently decided to examine the September 1986 data. Both 

band 2, 3, 4 (blue, green, and red) and band 3, 4, 5 (blue, green, 

red) color composites were generated for each of the seven intrusives 

of interest. 

Since the only success in classification of the Skaergaard 

It 

The plutons examined were (from southwest to northeast) Imilik, 

Kruse Fjord, Kap Edvard Holm, Kangerdlugssuaq, Gardiner, Lilloise, and 

Borgtinderne. 

meters per pixel according to the dimension of the individual pluton. 

Full resolution (30 meter per pixel) subscenes were also created for 

selected portions of each of these bodies. The band 3, 4, 5 color 

composites were generally the most effective for discrimination of 

The scales used for these images varied from 40-120 

basic lithologies. Differences were, however, often subtle, requiring 

careful application of the interactive contrast stretching tool. With 

this particular band combination, the intrusives generally appear more 

tan to brownish than the brighter orange of the surrounding gneisses. 

The basalts take on a somewhat greener hue, while syenites appear 

redder if a little less bright than the gneisses. It should be noted 

that, as is so often the case, these differences, while apparent on a 

digital display, are difficult to preserve in second generation 

photography. 19 
Mineral Resourse Evaluation 

In addition to developing a set of criteria for using TM data to 

recognize the various rock types associated with mafic intrusions in East 

Greenland, a major goal of this project is to evaluate the resource potential 

of mafic intrusions in East Greenland, and in continental rifting 

environments in general. Our field mapping of the distribution of sulfides in 

the Skaergaard intrusion has resulted in the location of a potential 

Pd/Pt/Au ore horizon. Layered tholeiitic intrusions are the primary sources 

of Pt and Pd, two strategic metals for which South Africa and the Soviet 

Union are the principal producers and the United States and Japan are the 

largest consumers. The initial Skaergaard magma, as sampled at the chilled 

contacts of the intrusion, contained approximately 20 ppb Pt, 15-26 ppb Pd, 

and 4-1 0 ppb Au. During crystallization of the lower part of the intrusion 

the magma was not saturated in S, and as a result the early formed rocks 

contain only minor amounts of Pt, Pd, and Au sulfides. During 

crystallization of the Middle Zone, the magma became saturated in S and 

precipitated an immiscible sulfide liquid. As a result of the extremely high 

partitioning of precious metals into sulfide liquids, the initial sulfide 

precipitation scavanged the magma of precious metals and formed a horizon 

with total Pt, Pd, and Au in excess of 4 gms per ton, and average ratios of 

Pt-Pd-Au approximately 1 -4-3. Rocks overlying the economic horizon 

contain negligable precious metal values, evidence of the effective removal 

of these components from the magma by the initial sulfide precipitation. 

Volume estimated for the Skaergaard intrusion (1 50 km3) suggest a total 

original Pt content of 9x1 O6 kgs, a total Pd content of 9x1 O6 Kgs, and a 

total gold content of 3x1 O6 kgs. Approximately half of the original mass of 

20 
the intrusion has been removed by erosion. Estimates of the extent of the 

enriched horizon in the Middle Zone of the intrusion (1 m x 30 km2) suggest 

that 5x1 O4 kgs Pt, 2x1 O5 kgs Pd, and 13x1 O5 kgs Au may be concentrated in 

an ore horizon. Platinova Resources Ltd. of Toronto, Canada, which has the 

exploration license for East Greenland (issued by the Danish Government) is 

currently evaluating the economic potential of this deposit. 

Other intrusions in the East Greenland Tertiary Igneous Province which 

contain rocks types similar to those in the Skaergaard intrusion include the 

Kap Edvard Holm, Kruuse Fjord, and lmilik plutons, the Basistoppen sill, and 

the Kraemers Island, Vandfalsdalen, and Miki's Fjord Macrodykes. The initial 

Pt, Pd, and Au contents of the magmas which formed these intrusions are 

likely to be similar to that of the Skaergaard, but it is not known if these 

intrusions reached saturation in a sulfide liquid to produce horizons with 

concentrations of precious metals. The areal extent of the Kap Edvard Holm 

intrusion is approximately 5x that of the Skaergaard and the areal extent of 

the Kruuse Fjord is.more than lox that of the Skaergaard. The presently 

exposed extent of the lmilik intrusion is approximately half that of the 

Skaergaard but the lmilik extends for an unknown distance below sea level. 

The areal extents of the Basistoppen sill and the associated macrodykes are 

significantly less than that of the Skaergaard intrusion. 

Student Theses resulting from NAS 5-28738: 

Brinkema, C. B., 1986, The Hamersdal S ill. Kanw I suaa Reaion. Ea3 

Greenland, BS thesis, Dartmouth College, Hanover NH. 

Turner, P. A., 1986, The Su lfide Miner-v and the Rehavior of S and Cem 

Transition Elements in the Skae rwd Intrusion. bt Green[&, MS .. 

21 
thesis, Dartmouth College, Hanover, NH. 

Urquhart, J., 1986, Depth of Emdacement and Cool ina Historv of tk 

.. Skaerwntrusion. East Green land as Revea led bv Fission Track Dates, 

MS thesis, Dartmouth College, Hanover, NH. 

Barnett, D. E., 1987, A Petroloaic Studv of the Krawer island Macrodike, 

&st Green, MS thesis, Dartmouth College, Hanover, NH. 

Nichols, J. D., 1987, A Ground Based and I andsat Sgectral Swv of tha 

Skaer- awd Intrusion. East Greenland, BS thesis, Dartmouth College, 

Hanover NH. 

Cobb, M. K., 1987, Analvsis of the Top oaraDhlc Effects on mectrd 

Briahwss: Kraerner Isl- Skmrd Intrusion. Fast Greem, BS 

thesis, Dartmouth College, Hanover NH. 

Keith, D. W., 1988, Qbservations on Lave rina - in the LoDer I Border Series of 

lhe Skaeraaa rd Intrusion. Fast G reenland , MS thesis, Dartmouth College, 

Hanover, NH. 

Publications resulting from NAS 5-28738: 

Naslund, H.R., Conrad, M.E., Urquhart, J. and Turner, P.A., 1986. Computer 

simulation of apparent grain sizes in thin sections - applications to 

grain size variation in the Skaergaard intrusion, EOS Trans. Amer, 

Geophvs. Union 67,384. 

Turner, P.A., and Naslund, H.R., 1986, The mineralogy and distribution of 

sulfides in the Skaergaard intrusion, East Greenland, Geo I. SOC. Amer, 

Pbst. with Pros la, n6-777. 

layering in the middle zone of the Skaergaard intrusion, East Greenland, 

Turner, P.A., Naslund, H.R., and Keith, D.W., 1986, Observations on rhythmic 

22 
Geol. SOC. Amer. Abst. with Pro& 18, 777. 

Naslund, H.R., 1987, Lamellae of baddeleyite and Fe-Cr-spinel in ilmenite 

from the Basistoppen sill, East Greenland, Canadian MineraL 25, 91-96. 

Naslund, HA., Parr, J.T., and Birnie, R.W., 1987, Lithologic mapping of mafic 

intrusions in East Greenland using Landsat thematic mapper data, 

Proceedus of the Third Annual Landsat WorkshWoratorv for 

Jerrestr ial Phvs ics. NASA, 157-1 62. 

Barnett, DE, and Naslund, H.R. , 1987, A petrologic study of the Kraemer 

. Island Macrodyke, East Greenland, Geol. SOC. Amer. Abst. with Pros 191 

580. 

Keith, D.W., and Naslund, H.R., 1987, Petrographic and chemical 

characteristics of a layered sequence in the Upper Border Zone of the 

Skaergaard intrusion, East Greenland, Geol. SOC. Amer. Abst. with Proa, 

19,723. 

Turner, P.A., and Naslund, H.R., 1987, PGE abundance in the Skaergaard 

intrusion, East Greenland, Geol. SOC. Amer. Abst. with Prog, 19, 872. 

Urquhart, J., and Naslund, H.R., 1988, Depth of emplacement for the 

Skaergaard intrusion, East Greenland as revealed by fission track dates, 

SOC. Amer. Abst. w ith Pro& 20,77. 

Parr, J.T., Birnie, R.W., Naslund, H.R., and Nichols, J.D., 1988, Lithologic 

mapping in East Greenland with Landsat thematic mapper imagery, 

Proceed inas of the S i~ Themic Conference on Remote Sensa for 

Exoloration Geology. ER Ib&,Houston. Texa, 203-21 2. 

Naslund, H.R., 1989, Petrology of the Basistoppen sill, East Greenland: A 

calculated magma differentiation trend, J, Petrol. 3Q, 301 -321. 

Birnie, R. W., Parr, J. T., Naslund, H. R., Nichols, J. D., and Turner, P. A., 1989, 

23 
Applications of Landsat Thematic Mapper and Ground Based Spectrometer 

Data to a Study of the Skaergaard and Other Mafic Intrusions of East 

Greenland, accepted for publicationin Pemote Sensing of tb 

bvironment. 

Naslund, H.R., ( );Grain size variations in plutonic igneous rocks part 1 : 

Theory, submitted to J. PetroL 

Naslund, H.R., Turner, P.A., and Keith, D.W., ( ), Crystallization and Layer 

- Formation in the Middle Zone of the Skaergaard intrusion, submitted to 

Turner, P. A., and Naslund, H. R., ( ), Distribution of sulfides in the 

Skaergaard intrusion, East Greenland, IN PREPARATION. 

Naslund, H. R., Birnie, R. W., and Parr, J. T., ( ), Geologic mapping in East 

Greenland using Landsat TM imagery, IN PREPARATION. 

24 
Appendix 1 

Applications of Landsat Thematic Mapper and Ground Based Spectrometer Data . to a Study of the Skaergaard and Other Mafic Intrusions of East Greenland 

Richard W. Birnie (l), J. Thomas Parr (2), H. Richard Naslund (3), 

Jennifer D. Nichols (4), and Patricia A. Turner (5) 

(1) Dartmouth College, Hanover, MI 

(2) The Analytic Sciences Corporation, Reading, MA 

(3) Dartmouth College, now at SUNY - Binghamton, Binghamton, NY 

(4) Dartmouth College, now at Harvard University, Cambridge, MA 

(5) Dartmouth College, now at Platinova Resources Ltd., Toronto, Canada 

Submitted: 

Remote Sensing of Environment 

August 1988 

(revised Xovember 1988) 
Landsat TM data have been used in conjunction with field spectrometer data to map the 

lithologic units associated with a series of gabbroic intrusions in the East Greenland Tertiary 

Igneous Province. The general lack and vegetation combined with the difficulty of accm to 

these intrusions make them ideal candidates for lithologic mapping using remote sensing 

techniques. In addition, these bodies are of interest as possible precious metal ore deposits. The 

intrusions are spectrally distinct from the sunounding Precambrian gneisses; however, subpixel 

contamination by snow, oxide surface coatings, lichen cover ad severe! topography limit the 

discrimination of lithologic units within the gabbro. The spectral nature of the surface 

contaminants was evaluated with a Barringer Hand Held Ratioing Radiometer (HHRR). These 

HMiR data indicate that bare rock exposures have distinct TM signatures for each lithologic unit 

but that even small amounts of subpixel contar@ation are enough to mask these differences 

because of the large differences between the TM signatures of the rocks aod the contaminants. 

I 

26 
I 

27 
28 
29 

. 
.a 

YI 

33 
31 
B 

06 t 

u 

f 

s 

n. 

32 
FIGURE CAPTIONS 

Figure 1: Sketch map of the East Grmland coast between Angmagssalik and Scoresby Sund 

showing the approximate locations of the major intrusions (after Deer, 1976). The 

dark patches show the limit of exposed rock. 

Figure 2: Geologic map of the Skaergaard Intrusion showing the distribution of the major 

subdivisions of the intrusion. Qgm = glacial moraine; Bs = post Skaergaard 

Basistoppen sill; UBS = Upper Border Series; MBS = marginal Border Series; LS = Layered Series; Tb = Tertiary basalts; Ks = Cretaceous sediments; PC = 

Precambrian gneiss (from Naslund, 1984). 

Figure 3: Generalized east-west cross section of the Skaergaard intrusion. 

Figure 4: Principal Components Image of Skaergaard Intrusion (Scene ID ## 509261301 1, 13 

Sept. 1986). The image is approximately 10 km on a side. See text for discussion. 

Figure 5: Air photo with north approximately up showing approximate N-S contact of 

Precambrian gneiss (light colored) and Skaergaard intrusion (dark colored) on 

Kraemer Island. Forbindelsesgletscher enters from the east on the right side of the 

photo. Uttental Sund separates Kraemer Island on the left from the mainland on the 

right. See Figure 2 for the geology. 

Figure 6: View from Kraemer Island looking north across Uttental Sund showing contact of 

Precambrian gneiss (light colored) and Skaergaard intrusion (dark colored) on the 

Uttental Plateau. 

Figure 7: Ternary diagrams of "RR field data (7-1 is TM5-TM3-TMI and 7-2 is 

TM4-TM3-TMl). Solid points are surface alteration (MI-moderate mineral stain, 

M2-heavy mineral stain, P1-moderate lichen cover, P2- heavy lichen cover, and 

S-snow). Open symbols are bare rock surfaces (1-gneiss, 2-LZa+LZb, 3-LZc, 

4-MZ, 5-UZa, and 6-basalt). In Figure 7-2, points 1 and 6 are to the lower left, 

points 3 and 4 are to the top, and points 2 and 5 are to the lower right. 

33 
Figure 1 

34 
Figure 2 

i 35 
Figure 3 

36 
Figure 4 

Figure 5 

37 
Figure 6 

38 
39 
Table 1 

TM SIGNATURES OF SKAERGAARD UNITS 

(in Digital Numbers) 

Lithologic 1 2 3 4 5 7 

Unit 

Lower Zone a+b 

Lower Zone c 

Middle Zone 

Upper Zone a 

Upper Zone b+c 

Basistoppen 

Granophyre 

pC Gneiss 

11 7.2 

119.0 

109.9 

105.2 

104.9 

119.7 

11 3.4 

130.4 

48.5 + 

48.1 

45.7 

45.0 

44.5 

49.3 

49.1 

55.6 

59.9 

59.3 

56.2 

58.4 

55.8 

62.5 

64.9 

70.3 

43.9 

42.1 

42.7 

43.2 

43.2 

46.6 

50.9 

53.1 

67.8 40.9 

60.0 35.7 

71.2 42.1 

66.7 41.4 

72.0 42.7 

87.8 53.3 

105.2 62.6 

101.4. 61.4 
, 

TabIe 2 

ESTIMATED CLASSIFICATION ACCURACY 

(“YO BASED UPON TRAINING CELL STATISTICS) 

(see text for unit abbreviations) 

LZa+b LZc MZ UZa UZb+c Bs Gs PCG 

LZ a+b 

LZC 

Mz 

UZ a 

UZ b+c 

Bs 

Gs 

ffi 

- 

0 

0 

76 

0 

64 

99 

93 

0 0 

- 0 

0 - 

70 55 

0 5 

100 100 

100 94 

100 94 

76 0 

70 0 

55 5 

0 

0 - 

- 

100 98 

100 54 

100 88 

64 99 93 

100 100 too 

100 94 94 

100 100 100 

98 54 a8 

- 66 0 

66 - 99 

0 99 
Appendix 2 

Calibration of Fibrefrax Standard and Effect of Different Illumination Angles 

Because the ground based spectral measurements undertaken in the field with the 

Barringer Hand Held Rationing Radiometer (HHRR) were done at a generally low but also 

highly variable sun elevation angles (between at least 18 and 35" ), we undertook an 

experiment to evaluate whether there is any specular component to the reflectance from 

fiberfrax standard. Thatk, does the color of the fiberfrax change with illumination angle. 

An experiment was undertaken to examine the spectral reflectance properties of 

fiberfmc at illumination angles between 10" and 80" (Figure 1) A 90" (nadir) illumination 

angle was not possible because the illumination source interfern with the spectroradiometer 

at that position (Figure 1). Data were collected in this experimental set up with both the 

high spectral resolution SE590 spectroradiometer ('Table la) and the HHRR (Table Ib). 

Since only the HHRR was used in the field in Greenland, this analysis focuses on the 

HHRR data. The values in Table 1 b are fiberfrax target signatures at various illumination 

angles ( 1Oo-7O0) referenced against a fiberfrax standard at 80" illumination angle. 

Therefore, the illumination of the standard is held constant while the illumination of the 

target varies. 

The results are plotted in Figures 2 and 3. Figure 2 shows that there is a steady 

decrease in reflectance with illumination angle. These would be predicted because as 

illumination angle gets lower, the cone of dispersion of the incident beam gets broader and, 

therefore, the intensity of illumination per unit of surface area drops. The drop off is 

predicted to be related to the sin of the illumination angle and that prediction is clearly 

supported in Figure 2 which includes a plot of the sin of the illumination angle with the 

spectral data. The reflectance values in Figure 2 converge to a value of 1.00 at 80" where 

the target and standard are both viewed at the same illumination angle. In Figure 2, the 

spectral characteristics of the standard are shown by plotting the six bands signatures at the 

different illumination angles. It can be seen clearly that there are now systematic changes in 

the color of the standard with illumination angle. There is some small random variability of 

the reflectance values, but no systematic change. 

We next undertook an experiment to evaluate whether the reflectance properties of a 

rock might change under different illumination conditions. This experiment was 

undertaken with the exposed fresh surface of a large sample of gabbro from Greenland. 

42 
In this case, the data are measured and presented as standard field observations; that is, 

both target and standard are measured under the same illumination conditions. 

The results listed in Table 2 and plotted in Figures 4 and 5. The TM band 1 values 

are not considered reliable because the incident illumination is low at those wavelengths and 

small percentage changes in instrument response will produce large changes in reflectance. 

BGth Figures show that there is an increase in the reflectance values as the illurnhation 

angle gets lower. There appears to be little change in the relationship between bands at a 

given illumination angle, i.e. little difference in color; but there is a change in overall 

intensity. The systematic increase in reflectance with decreasing illumination angle is 

highlighted in Figure 6 with one band from the visible (Th4 3) and one band from the near 

infrared (TM 5) plotted. 

While the change in reflectance with illumination angle is systematic, the actual 

diMerences measured on both the target and standard are small. These values are plotted 

for both the gabbro and the fiberfrax for TM bands 3 and 5 in Figures 7 and 8 respectively. 

The general drop in reflectance signal with lowering illumination angle for the target and 

standad are shown clearly in these figures; the fibrefrax has already been shown to follow 

the sin cume (Figure 2). However, it is also clear from these figures (particularly Figure 8) 

that the gabbro does not fall off as rapidly. as the fibre&. Therefore, when the 

reflectances are calculated by rationing gabbro to fibrefrax, the relative reflectances 

increase. 

The reason for the increase at lower angles is not known, but it may be related to 

preferential orientation of feldspar cleavage faces. Since field measurements were taken 

under a variety of incident solar illumination angles varying between at least 18' and 35", 

some variation in the overall brightness of our "RR spectra are expected. 

This change in reflectance is small relative to the differences seen in "RR spectral 

signatures (Parr et id., 1988 and Birnie et al. in press) and would not effect the 

interpretations based on band ratios. However, this relationship may be critical in 

understanding reflected radiance differences seen in the satellite data. The step topograph 

and extreme illumination conditions in this artk environment provide a tremendous 

variation in surface plane to solar illumination direction. 

43 
40 0.643 0.243 0.290 0.275 0.348 - - 

50 0.766 0.337 0.403 0.381 0.476 - - 

60 0.866 0.395 0.468 0.440 0.546 - - 

70 0.940 0.433 0.511 0.478 0.588 - - i 

Table la. Simulated TM signatures of bands 1 , 2, 3 and 4 for Fiberfrax reference standart 

calculated from E590 spectra collected at different angles of illumination. 

Table 1 b. Simulated TM signatures of bands 1, 2, 3, 4, 5 and 7 for Fiberfrax reference 

standard collected with HHRR at different angles of illumination. 

Table 2. Laboratory reflectance spectra of gabbro under differing illumination conditions. 
SE590 or HHRR . ’ Spectroradiometer 

a J macII 

Angle of Illumination 

Artificial light prwided by two 75 watt incandescent flood lamps 

Figure 1. Laboratory set-up used for the analysis of Fiberfrax reflectance prop,,qies unczr 

differing illumination conditions. Measurements made with both the SE590 and HHRR 

spectroradiorneters. 

, 

45 
W 

0 

z 

Io 

W 

-I 

L 

W 

U 

a 

0.7 

0.6 - 

0.5 - 

0.4 - 

1 .o 1 

1 .o 

0.9 - 

0.8 - 

0 A 

w w v w 0 

I 

- I 

- I 

I 

sin of experimental 

'I V.V I I 1 1 I 1 I I I 

0 10 20 30 40 50 . 60 70 80 

ILLUMINATION ANGLE (0) 

Figure 2 

w 0.7 

0 5 0.61 

Io 

W 

-I 0.5 

L wi 

0.0 ' I I I I I I 

TM 1 TM 2 TM 3 TM 4 TM 5 TM 7 

TM BAND 

Figure 3 

Illumination Angle 

70° 

60° 

SO" 

40° 

30° 

200 

100 

46 

I 
1 

Y 

a 

0 

c 

0 

a 

c = a 301 20 

TM band 1 

TMband2 

TM band 3 

TM band 4 

TM band 5 

TM band 7 

' 

- 

- 

- 

10 - 

0- I I 1 I I 

0 10 20 30 40 50 En 

60 

50 

n 

40 v 

a 

0 

c 

m c 30 

0 

Q, = 

Q) 

U 

20 

10 

0 

illumination conditions (low light). 

Illumination Angle (degrees) 

Figure 4. 

-- 

I I I I I I 1 

TM band 1 data are suspect due to 

poor detector response under laboratory 

illumination conditions (low light). 

- - 10" 

- 20" 

- 30" 

- 40" 50" 

I I I 

TM band 2 

I I I I 

TM band 3 TM band 4 TM band 5 TM band 7 TM band 1 

Band 

Figure 5. 

47 
5c 

40 

30 

20 

10 

_f_ * TMband3 

TMband5 

I I I I 1 I 

0 30 40 50 60 10 20 

Illumination Angle 

Figure 6. 

48 
1 O( 

8C 

60 

40 

20 

0 

1 00 

80 

60 

40 

20 

0 

I I I 

I I 

20 40 

I 

60 80 0 

Illumination Angle (degrees) 

Figure 7. 

I I I 

I I I 

0 20 40 60 80 

Illumination Angle (degrees) 

Figure 8. 

49 
Appendix 3 

TM lmagery of the Skaergaard intrusive center. 

Image 1 - Bands 2, 3, and 4 false color image (504 x 504 pixels). 

Image 2 - Bands 3,4, and 5 false color image (504 x 504 pixels). 

Image 3 - Band ratio 511 image with blue>green>yellow>red denoting 

increasing values (504 x 504 pixels). 

Image 4 - Band ratio 513 image with blue>green>yellow>red denoting 

increasing values (504 x 504 pixels). 

Image 5 - Band ratio 413 image with blue~green~yellow~red denoting 

increasing values (504 x 504 pixels). 

Image 6 - Bands-Band Ratio 1 , 311 , and 5 false color image (504 x 504 

pixels). 

Image 7 - Band Ratios 413, 511, and 513 false color image (504 x 504 

pix el s) . 

lmzge 8 - Band Ratios 311, 413, and 513 false color image (504 x 504 

pixels). 

Image 9 - Band Ratios 311,413, and 513 transformed and enhanced image 

Image 10 - ld, 2@ and 4 principal components false color image 

(504 x 504 pixels). 

(504 x 504 pixels). 

Image 11 - Supervised maximum likelihood classification image based on 

selected test sites (504 x 504 pixels). 

Image 12 - Supervised maximum likelihood classification image based on 

selected test sites (504 x 504 pixels). 

50 

52 

.- 0 

c. 

f! 

2 

a 

m 

5 .- 

3 

a 

aJ 

.- E 

d 

0 ln 

X 

d 

0 

v 

m 

d 

0 In 

X 

w 

0 

v 

v) 

v) 

W 

- 3 
ORIGINAL PAGE 

COLOR PHOTOGRAPH 
54 

OKIGiNAL PAGE 

COLOR PHOTOGRAPH 
A 

v) 

0 

X 

Q 

w 

0 

In 

x 

d 

0 

In 

- 

.- 

Y 

Lbj?ic.:GlNkL PAGE 

COLOR PHOTOGRAPH 

Appendix 4 

TM Imagery of the Kangerdlugssuaq, Kap Edvard Holm, Gardiner, Kruuse 

Fjord, Imilik, Borgetinderne, and Lilloise intrusive centers 

Image 13 - Bands 3,4, and 5 false color image of the Kap Edvard Holm 

intrusive complex (1 008 x 1008 pixels). 

Image 14 - Bands 3,4, and 5 false color image of the Kangerdlugssuaq 

intrusive complex (1 008 x 1008 pixels). 

Image 15 - Bands 3,4, and 5 false color image of the southern half of the 

Kap Edvard Holm intrusive complex (504 x 504 pixels). 

Image 16 - Bands 3,4, and 5 false color image of the northern half of the 

Kap Edvard Holm intrusive complex (504 x 504 pixels). 

Image 17 - Bands 3,4, and 5 false color image of the north central part of 

the Kangerdlugssuaq intrusive complex (504 x 504 pixels). 

Image 18 - Bands 3,4, and 5 false color image of the northeastern part of 

. the Kangerdlugssuaq intrusive complex (504 x 504 pixels). 

Image 19 - Bands 3,4, and 5 false color image of the Borgtinderne and 

Lilloise intrusions (2016 x 1344 pixels). 

Image 20 - Bands 3,4, and 5 false color image of the Lilloise intrusion 

(672 x 672 pixels). 

Image 21 - Bands 3, 4, and 5 false color image of the Kruuse Fjord 

intrusive complex (1 008 x 1008 pixels). 

Image 22 - Bands 3,4, and 5 false color image of the lmilik intrusive 

complex (1 51 2 x 151 2 pixels). 

Image 23 - Bands 3,4, and 5 false color image of the Gardiner intrusive 

complex (504 x 504 pixels). 

57 
58 

ORIGINAL PAGE 

COLOR PHOTOGRAPH 
I ORIGINAL PAGE 

COLOR PHOTOGRAPH 

d 

0 

In 

X 

d 

0 

Y 

In 
60 

ORIGINAL PAGE 

COLOR PHOTOGRAPH 
c 

0 

In 

.- 

.- $ 

ORfGINAL PAGE 

.&&OR PHOTOGRAPH 

0RIGir.IEaL PAGE 

COLOR PHOTOGRAPH 

63 

'c 

0