Preliminary Report, Geology of Natashquan Area, Duplessis County P.R.- 582

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RP 582(A) PRELIMINARY REPORT, GEOLOGY OF NATASHQUAN AREA, DUPLESSIS COUNTY P.R.- 582

GOUVERNEMENT DU QUÉBEC

DEPARTMENT OF NATURAL RESOURCES

MINES BRANCH

GEOLOGICAL EXPLORATION SERVICE

GEOLOGY

of NATASHQUAN AREA

DUPLESSIS COUNTY

PRELIMINARY REPORT

Jean-Pierre Bassaget

QUEBEC 1970

P.R.- 582

GOUVERNEMENT DU QUÉBEC

DEPARTMENT OF NATURAL RESOURCES

MINES BRANCH

GEOLOGICAL EXPLORATION SERVICE

GEOLOGY

of NATASHQUAN AREA

DUPLESSIS COUNTY

PRELIMINARY REPORT

Jean-Pierre Bassaget

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QUEBEC 1970 P.R.-58Z Preliminary Report on

NATASHQUAN AREA

Jean-Pierre Bassaget

' INTRODUCTION

The Natashquan area, mapped during the summer of 1968, lies between longitudes 61°30' and 61055'. It is bounded on the north by the 50°30' parallel and on the south by the north shore of the Saint-Laurent, where the small port town of Natash- quan is located. Covering about 400 square miles of Duplessis county, the area includes all or parts of the following townships: Natashquan, Duval, Kegashka, 880, 980, 1080, 881, 981 and 1081. Travel within the area was by canoe and float plane, the latter from a base at Havre-Saint-Pierre, about 85 miles to the west of the center of the area studied. The coastal portion of the area between Romaine river and the present map-area, for a distance of about 18 miles inland, has been mapped by the following geologists for the Quebec Department of Natural Resources: J.A. Retty (1944), W. Longley (1948-50), J. Claveau (1949-50), R. Blais (1956), P.-E. Grenier (1957), G. Cooper (1957), D. McPhee (1959-60) , and J. Depatie (1967) . Topography The area is relatively flat, with a difference in elevation of only 700 feet. The southern part, covered by an old delta consisting of re=worked glacial deposits, has almost no local relief. To the north, the underlying gneissic structure ha' resulted in a ridge-and-valley topography. The ridges are barren, with vegetation being confined to intervening valleys. Because of this, the structures of the area can be easily discern- ed on the half-mile-to-the-inch aerial photographs. The quartzites and gabbros form hills masked by densely wooded areas. Sever- al of'the major valleys of the area follow apparent fault trends. Drainage The drainage pattern of the area reflects a reju- venation of the former river systems. Natashquan river, in par- titular, because of Holocene rebound, cuts through an ancient delta in the southern part of the area. GENERAL GEOLOGY The rocks of the area are all Precambrian in age, and are partly covered by Pleistocene glacial deposits. The rocks can be divided into two groups. One, representing the basement rock of the area, is made up of dense and strongly migmatizéd gneiss and granitic rocks. The several facies of this group are intermixed with one another, and their primary relationships are, in general, unknown. Pegmatites cut all these basement rocks. The other group comprises metasedimentary rocks and associated igneous rocks; some of the latter are metamorphosed and others are not. These younger rocks have been preserved within the synclinal structures of the area. The metasedimentary rocks include quartzites, arkose, and biotite-bearing and hornblende-bearing paragneiss. The associated gabbro intru- sives, which lie more or less parallel to the bedding of the metasedimentary rocks, have been transformed to amphibolites. The hornblende-bearing white gneiss of the area also appears to belong to this group of rocks. White muscovite-bearing pegmatites cut the metasedimentary rocks and their associated amphibolites and, locally, the granitic basement rocks. These unmetamorphosed pegmatites seem to bear a direct structural relationship: to the métasedimentary rocks and amphibolites, as they have not been observed as isolated bodies within the granitic. basement. •TABLE OF FORMATIONS

Pleistocene Sand, gravel, glacial boulders

Intrusive. Muscovite-bearing white pegmatite rocks Amphibolite (metagabbro) White hornblende orthogneis.s Wakeham Group Metasedi- Metamorphic quartzite mentary Metamorphic arkose rocks Hornblende paragneiss Biotite paragneiss

Pink pegmatite Intrusive Massive or gneissic biotite- muscovite granite rocks Massive or slightly foliated Granitic biotite granite basement rocks Granitic Gneiss, with or without hornblende Migmatites Banded gneiss Augen gneiss, with or without hornblende

Granitic Basement Rocks The rocks of the basement complex include migma- tized gneiss, usually of the augen variety, although banded gneiss occurs in some places, as well as granitic gneiss and massive granite with, in places, a vague local orientation. All of these rocks have a similar mineralogical composition. Augen Gneiss The augen gneiss for the most part occurs in the form of concordant, but discontinuous, bands. Its relation to the other granitic rocks has not been clearly established in the field. It grades into the granitic gneiss, which may lie above or below it, through a difficult-to-map transitional facies that has characteristics of both rock-types. The augen gneiss 4 is pink on both fresh and weathered surfaces, and has fairly well developed "eyes". It contains about 10-20% quartz, 50-70% potash feldspar and plagioclase, 5-10% biotite and hornblende, and minor opaque and accessory minerals. The augen, which are porphyroblasts of feldspar and quartz, are outlined by thin wavy bands of ferromagnesian minerals. Hornblende, in variable percentages, is confined to the southwest part of the area, between Le Gal lake and the second falls on Natashquan river. Elsewhere, the ferromagnesian minerals are represented only by biotite. Banded Gneiss Banded gneiss is rare, being confined mainly to the southwest, near the western boundary. It has the same general composition as the augen gneiss, but mineral percentages vary from band to band. Some bands are entirely quartzo- feldspathic; others are rich in ferromagnesian minerals. The bands range from 2 inch to about 1 foot thick. Granitic Gneiss The granitic gneiss is characterized by a distinct and regular foliation resulting from the orientation of the ferromagnesian minerals. In the field, it may be difficult to separate this rock type from the massive or slightly foliated granite, although, on a large scale, areas of exposure of the two rock types are readily distinguished. The granite intrusive contact is exposed in places. The transition from granitic gneiss to augen gneiss, on the other hand, appears to be grada- tional. The mineralogical composition is similar to that of the augen gneiss, although relative percentages differ slightly. Hornblende, as in the augen gneiss, is present only in the south and southwestern parts of the area. The granitic gneiss is pink on the fresh surface, with a pink or pinkish white weathered surface. The gneiss near Natashquan represents a distinctive facies, it is red on both fresh and weathered surfaces, and the hornblende, which is abundant, forms discontinuous streaks a few millimeters wide. Massive or Slightly Foliated Granite On a large scale, granite forms sinuous bands which more or less follow the regional structure, as represented by the foliation of the gneiss. The intrusive contact of the 5 granite with the augen gneiss can be seen in places. The granite is intercalated within thé granitic gneiss and augen gneiss, and displays the stratiform appearance that is charac- teristic of syngenetic granites. The granite contains quartz, potash feldspar, plagioclase, biotite, and opaque and accessory minerals. The percentages are variable, particularly that of quartz (2-30%); some syenitic facies are virtually devoid of quartz. The content of biotite may be as low as 1%. The rock is fine to medium grained and pink on both fresh and weathered surface. Close jointing is everywhere in evidence on the outcrop, but is not seen in hand specimens. The biotite is roughly oriented in places. Biotite-muscovite Gneiss and Granite These rocks can be distinguished from the granitic gneiss and the ordinary granites by the presence of appreciable quantities of muscovite and by their whitish color. Most of the biotite-muscovite gneiss exhobits a lineation, due to the elongation of the minerals. These rocks outcrop in the north- east corner of the area, east of Paimpont lake. Pegmatites All of the granitic basement rocks have been injected by pegmatite. These pegmatites, mainly feldspathic and pink in color, may lie parallel to the foliation of the enclosing rocks, but they usually display a haphazard injection pattern and, in places, even appear to grade into the enclosing rocks. The Wakeham Group and Associated Intrusive Rocks The Wakeham Group is made up of biotite paragneiss, hornblende paragneiss, and metamorphic quartzites and arkoses. This facies lies in large-scale unconformity on the granitic basement. Where seen in individual exposures, how.ever,,the Wakeham Group contact appears to be a metamorphic one, and,'in detail, it would be difficult to define the primary relationships between the two assemblages. Biotite Paragneiss The biotite paragneiss is made up of dark and light bands, about 1 centimeter thick, containing variable percentages of quartz, feldspar and biotite; some are quartzitic. 6

These rocks are well foliated ;and, where biotite is abundant, a schistosity can be seen. They appear to include bands of amphibolite, which may be derived either from an earlier gabbro or from an earlier paragneiss. Although their.stratigraphic position is not too well known, the biotite paragneisses have been placed at the base of the Wakeham Group. They have been observed mainly at the contact of the granitic basement bordering the metasedimentary formations and at the bottom of eroded synclines. The thickness of the gneiss appears to be quite variable. In some places, this rock type is well represented between the basement complex and the quartzites; in other places, it is absent. This may be due to tectonic action. Some exposures of biotite gneiss occupy an uncertain position within the metasedimentary synclines, particularly east of Paimpont lake, and - possibly reprësent intercalations within the quartzite. Hornblende Paragneiss ' The hornblende paragneiss occurs in the same areas of exposure as the biotite paragneiss, in places in alternating bands. These rocks are strongly foliated, in places even schistose, with acidular amphibole crystals irregularly oriented along the foliation planes. They appear to be bedded in places, the hornblende content varying from bed to bed. Quartz, feldspar, biotite and hornblende are the essential minerals. Metamorphic Quartzite and Arkose Most of the metasedimentary rocks of the area fall into this class. The quartzites are quite variable in appearance; their color is grayish white, greenish gray or dark green, and their texture varies from massive and granoblastic to bedded, with micaceous interbeds. The quartz may be either glassy or granular. The beds of quartzite, about a centimeter thick, in places alternate with beds of recrystallized pink arkose. In addition to quartz, these rocks contain feldspar, biotite, muscovite, and opaque and accessory minerals; muscovite is ubiquitous in its occurrence. The micas, in variable percentages, are either disseminated through the rock or form thin scaly interbeds. With an increase in feldspar content, these rocks become mainly pink in color and can be classified as arkose. Primary bedding could nowhere be clearly distinguished, and the rocks show none of the sedimentary features noted farther to the west. This is probably due to the greater degree of recrystallization of the rocks of the present map-area as com- pared; for example, to the rocks of the Beetz Lake area (Grenier, 7

1957), where all of the characteristics of. detrital sedimentary rocks have been preserved in some of the quartzites. Granitization of the Wakeham Group Granitization within the Wakeham Group, particularly the quartzites, is evident near the contact with the granitic basement. This granitization takes several forms, not necessar- ily related. It may affect the entire rock mass, in which case the rock has the appearance of a quartz-rich granite; this type of granitization is confined to the zone immediately above the basement contact. It may also take the form of aplitic or pegmatitic sills or a network of pegmatitic injections, in places quite dense. The injected material is pink and made up essen- tially of potash feldspar. This type of granitization is not directly related to the contact with the basement rocks, but is never very far away from it. Nodular Gneiss - Near the contact with the Wakeham Group, some rocks (biotite gneiss, quartzites and granitic gneiss) have a distinctive appearance, owing to the presence of nodules of sillimanite outlined by muscovite. This facies no doubt resulted from pneumatolytic emanations contemporaneous with the muscovite- bearing white pegmatites. Metagabbros - The metagabbros are dark green to black on the fresh surface, and black to rusty where weathered. They are intercalated within the metasedimentary gneisses, either in the biotite or hornblende paragneiss or in the quartzitic rocks. Their occurrence within the paragneiss is hard to define, as the various contact facies contain biotite and hornblende and are difficult to separate in the field. However, the contacts of a metamorphic gabbro dike were seen in quartzites not far from the east side of Paimpont lake. This metagabbro dike is enclosed, above, by a massive greenish quartzite and, below, by a coarse- and transludent-grained quartzite. The contacts are sharp, the enclosing quartzites not having been metamorphosed by the dike. The metagabbro, which is coarse grained and mainly ophitic tex- tured, becomes fine grained near both the top and bottom contacts. This indicates that the quartzites were in place at the time of intrusion of the gabbro. A border of biotite, 2 to 3 inches thick, has been noted at the lower contact. The enclosing quartzites are massive, and it is not known whether the gabbro cuts across or is parallel to the primary bedding. However, the dip of the contact surface is roughly parallel to the local structure, as represented by the nearby foliation. In addition to hornblende, the metagabbros contain feldspar, biotite, secondary quartz, a high percentage of opaque minerals (which represent altered pyroxene), and accessory minerals. Locally, where_th_d'ophitic texture: remains, the pyroxene may have been preserved. The rock is usually quite well foliated, in places almost schistose, and has the appearance of a typical amphibolite. Hornblende Orthogneiss - A somewhat unusual, white, hornblende- bearing gneissic facies, locally resembling the metagabbro, has been noted in a few places within the basement complex. Feldspars are predominant and give the gneiss its white color. These rocks alternate with amphibolites which are similar to the metagabbros, as well as with biotite-bearing granitic gneiss and a very quartz- rich granitic facies (granitized quartzite?). This facies may be affiliated with the intrusive metagabbros of the Wakeham Group, for Many of its exposures are found in extensions of synclines in the metasedimentary rocks. A more detailed study of this facies may lead to a more accurate determination of its origin. Muscovite-bearing white Pegmatite - The Wakeham formations occur in two complexly folded synclinoria: one at Aliecte and Barbé lakes and the other to the east of Paimpont lake. Cutting the metasedimentary rocks and metagabbros in both of these structures is a band of pegmatite, â mile wide and a few miles long, elon- gated parallel to the synclinal axes. These pegmatites are char- acteristically white and are made up of 90% feldspar, with quartz, muscovite and traces of biotite; magnetite occurs locally. In a few places, the pegmatites appear to cut the granitic basement rocks, but no contacts have been observed nor have any isolated bodies of these pegmatites been noted within the rocks of the basement complex. They seem to be related either to the Wakeham Group or to tye metagabbros. PLEISTOCENE The southern part of the area is covered by sand, and deltaic features are clearly visible on the aerial photographs. The presence of a few widely scattered erratic boulders in the sand provides evidence of the glacial origin of these deposits, which were later re-worked by water. Glacial erratics are numerous in the northern part of the area, but there is virtually no sand here. The rock exposures along Natashquan river display glacial striae trending north-south to NNE.-SSW. STRUCTURE The foliation of the rocks provides the only clue to the structure of the area. Primary bedding in the sedimentary rocks is ; nowhere clearly evident, although it does not seem that, in places, thé foliation corresponds to the 'sedimentary bedding in the quartzites. 9

Folding Two major directions of folding are apparent within the area: one trending N.-S. to NW.-SE., the other trending E.-W. to SW.-NE. In the field; these- fold trends are expressed by two directions of foliation, in many cases superimposed on one another. Indications are that the north-south to NW.-SE. folds have been deformed by the later east-west to SW.-NE. folds. The north-south to NW.-SE. folds are of quite broad extent, and form the two large synclines which contain the Wakeham formations at Aliecte lake and at Paimpont lake. The secondary east- west to SW.-NE folds are more limited in extent, and are closely folded, with dips either to the south or north. They may be very tightly folded, as to the west and southwest of Aliecte lake, where the Wakeham formations and gabbros have been sqeezed out and laminated within narrow synclines. Faults and Jointing - Four faults were mapped, all trending SW.- NE. One follows a tributary of Aguanus river in the northwest corner of the area. It brings the granitic basement rocks into contact with The Wakeham formations comprised in the lowest ' faulted block, west of the area. Another fault, 5 miles south- east of Aliecte lake,bends to the north at its eastern end and is lost in Natashquan river. The other two faults follow straight valleys about 6 miles south of Paimpont lake. The southernmost one involves considerable lateral displacement and vertical throw. The pegmatites which intrudes the Wakeham formations have been fractured by four small breaks, also trending SW.-NE., to the south of Aliecte lake. These fractures are apparently confined to the pegmatite. The main joint systems, as seen on the aerial photographs, trend SW.-NE. (the same direction as the above- mentioned faults), SE.-NW., E.-W., and N.-S. ECONOMIC GEOLOGY A scintillometer was carried during the traverses to take measurments of radioactivity. In only one place, an area of a few square feet in the muscovite-bearing white pegmatite south of Aliecte lake, was any radioactivity noted (about twice the background count). Here, the pegmatite contains black iso- metric crystals of magnetite a few millimeters across. No radioactive minerals were seen. Some zones of granite and granitic gneiss contain above-normal, but still minor, percentages of magnetite --enough to give the rock a rusty-weathering surface. - 10 -

A few specks of chalcopyrite were seen here and there in the gabbros. Iron-bearing 'sands of Natashquan The Pleistocene sands along the north shore of the St. Lawrence river, between Natashquan and Kegashka bay, contain concentrations of iron-bearing minerals. These iron- rich concentrations form lenses, a few hundreds of feet long, which can be seen in small scarps bordering the St. Lawrence and thé outlet of the Natashquan river. History Due to their prominent location, these iron-bearing sands have been known since the early days of mineral exploration in Quebec, and they have been subject to analysis by the Geol- ogical Survey of Canada since 1866. The federal Department of Mines and Technical Surveys carried out a drilling program in the area from 1911 to 1913. In 1950, J. Claveau, of the Quebec Department of Mines, mentioned the deposits in his geological study of the North Shore of the St. Lawrence and in 1951, J. Dugas, also of the Department, experimented with magnetic methods in an attempt to discover other such deposits. Development work began in 1955 when Aconic Mining Corporation obtained a long-term working permit covering 31,650 acres in Duval and Natashquan townships. The company erected a pilot plan: Which was operative in 1957. In 1962, Mines Metal- lurgies Kebec took over the property, as well as the existing equipment, with a view to developing the deposits. This project, to our knowledge; was never put into operation, and the mining rights reverted to the public domain in July of 1969. The Deposit The iron-bearing sands are on the southern edge of the sàndy-terrace which covers the area north of Natashquan. this terrace is made up mainly of post-glacial deltaic material, but the mineralized portion has been reworked by the sea, as evidenced by ripple marks, marine fossils and recent sedimentary deposits. Facies variations are numerous, and the magnetite-rich concentrations are thus quite irregular, forming lenses with a lateral extent of only a few hundred feet. The magnetite content is also irregular, ranging from 3 to 35%. The most common minerals in the iron-bearing sands, in addition to magnetite, are ilmenite, quartz, biotite and garnet. Accessory minerals include feldspar, calcite, horn- blehde altered augite, tourmaline (rare), amethyst quartz, zir- con, rutile and monazite. Reserves - The irregularity of the mineralized zones and variations in grade make reserve estimates difficult. Following the work of MacKenzie and Parsons from 1911 to 1913, the reserves in Duval township were estimated at 27,384,890 tons containing 6.54% magnetite and capable of pro- ducing 1,776,195 tons of. concentrate grading 68% iron. Later, the drilling carried out by Aconic Mining Corporation greatly increased these figures. Estimates vary considerably, ranging to more than 15 billion-tons. One of the latest statements by Aconic, based on drilling done in 1958, places the reserves at 1.5 billion tons grading 3.7% iron. GEOCHEMISTRY Stream sediment samples were taken at forty locations in the area. They were analysed, at the laboratories of the Quebec Department of Natural Resources, for the elements Cu, Zn, Pb, Mo, U, Sb, Ag, Au, Sn, W, Ni, Co and Mn. The results are given on the accompanying map and in the following table.

BIBLIOGRAPHY Atkins, W.R. - 1958 - Report on Exploration of Natashquan Beach Sands, Aconic Mining Corporation. Confidential report in the files of the Quebec Dept. of Natural Resources; GM-7801 Biais, Roger A.,- 1956 - Pashashibou Area, Drucourt and Costebelle townships, Saguenay County; Quebec Dept. of Mines, P.R. 316. Bray, A.C. - 1954 - The Iron Sands Property of Aconic Mining Corporation in Natashquan Township. Confidential report in the files of the Quebec Dept. of Natural Resources; GM-3197. Bray, A.C., - 1965 - Report on Certain Properties Belonging to Mines Metallurgies Kebec. Confidential report in the files of the Quebec Dept. of Natural Resources; GM-16113. Claveau, J., - 1949 - Upper Romaine River Area, Saguenay County; Quebec Dept. of Mines, G.R. 38. Claveau, J., - 1950 - The North Shore of the St. Lawrence from Aguanish to Washicoutai Bay, Saguenay County; Quebec Dept. of Mines, G.R. 43. - 12 -

Cooper, G., - 1957 - Johan'Beetz Area, Saguenay Electoral 'District; Quebec Dept. of Mines, G.R.74. Dépatie, J., 1967 - Geology of Ours Lake Area, Duplessis County; Quebec Dept. of Natural Resources, P.R. 559. Dugas, J., 1951 - Magnetic survey on the iron-bearing sands of Natashquan. Confidential report. Que. Dept. Nat. Resources. Grenier, P.-E., - 1957 - Beetz Lake Area, Saguenay Electoral District;'Quebec Dept. of Mines, G.R.73. Longley, W.W., - 1948 - Forget Lake Area, Saguenay County; Quebec Dept. of Mines, G.R. 36. Longley, W.W., - 1950 - North Shore of the St. Lawrence from Mingan to Aguanish, Saguenay County; Quebec Dept. of Mines, G.R. 42, Part 1. MacKenzie, G.C:,- 1915 - Summary Report, 1914, Mines Branch, Dept. of Mines and Technical Surveys, Ottawa.

McPhee, D.S. - 1958 -Eric Lake Area, Saguenay; Quebec repar:tmènt of.Natural Resources, R.P. 369 McPhee; D.S. 1959 - Aguanish Area,,. Saguenay, Quebec Department of Natural Resources, R.P. 403

Retty, J.A.,- 1944 - Lower Romaine River Area, Saguenay County; Quebec Dept. of Mines, G.R. 19. 20.4.13A - 13 -

Sample Code No. No. on a! sample RESULTS OF ANALYSES IN P.P.M. the ma, DDept. pl'e" ` Cu Zn Pb Mo Ni U Co W Mn Sn Au Ag 1 3212 4 20 16 0 8 4 3 - - - - - 2 3711 2 15 10 0 5 2 5 0 13 0 0 0 3 1111 4 15 10 0 10 1 8 0 22 0 0 0 4 3711 2 15 16 0 8 4 8 0 13 0 0 0 5 7311 2 5 16 0 5 1 8 0 13 0 0 0 6 2317 7 15 6 0 8 2 8 0 53 0 0 0 7 2 5 16 0 3 1 8 0 30 0 0 0 8 10 10 30 - 16 - 10 0 - - - - 9 311 2 10 20 0 5 3 8 0 30 0 0 0.4 10 213 2 5 10 1 8 28 10 0 53 0 0 0 11 212 4 10 16 0 5 1 8 0 33 0 0 0 12 211 2 10 16 0 5 6 10 0 28 0 0 0 11 2922 2 ._1.5 10 0 8 0.5 5 0 13 0 0 0 ._14_ 2721 6 25 8 0 - 4 ------15 2912 2 15 40 ------16 2921 4 5 16 0 5 1 8 0 28 0 0 0 17 2911 4 15 20 , 0 20 2 33 - , - - - - 1R 2211 4 5 10 0 3 1 8 0 13 0 0 0 19 1211 2 15 16 0 8 1 8 0 62 0 0 0 70 ..1112 2 10 16 0 8 2 8 0 - - - - 21 1111 7 10 16 0 8 0.5 8 0 53 - 0 0 27 1421 4 5 10 0.5 , 8 1 8 0 78 0 0 0 23 1471 7 5 10 0 5 4 B 0 37 0 0 0 24 1571 4 5 16 2 5 12 8 0 20 0 0 0 75 1427 4, 10 16 0 8 2 3 0 30 0 0 0 76 7571 6 25 10 0 ------77 7811 4 25 20 0 5 2 10 0 38 0 0 0 7R 1911 7 . 10 16 0 5 0.5 8 0 38 0 0 0 29 1323 6 10 10 0 5 0.5 5 0 28 0 0 0 30 1221 4 10 10 0 5 0.5 5, 0 20 0 0 0 31 1321 2 10 16 0 8 0.5 8 0 130 0 0 0 32 2611 4 10 10 0 3 0.5 5 0 20 0 0 0 33 1322 6 50 16 15 0 3 8 0 230 0 0 0.3 34 611 30 15 20 0 10 14 8 0 78 - 0 0 35 8154 10 5 20 0 8 2 8 0 62 0 0 0 36 812 4 15 16 0 13 1 10 0 145 0 0 0 37 511 20 60 16 0 18 5 13 0 340 0 0 0.6 38 813 4 15 10 0 10 2 8 0 105 0 0 0' 39 514 2 20 16 0 10 2 20 0 - - - - 40 512 4 40 10 0 13 3 8 0 185 - 0 0.9

A dash indicates absence of determination =

A zero indicates'- that- the - element- was- not detected =