European Metallogeny, Lima_2013!1!2

7/28/2019 European Metallogeny, Lima_2013!1!2

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Geologa, metalogena y aspectoshistricos de la minera en Europa

Krister Leon SundbladUniversidad de Turku, Finlandia

Universidad Nacional Mayor de San Marcos,Lima, Peru

Junio 17-19, 2013


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Partes 1 y 2


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Que es Turku y que es Finlandia?

Finlandia es ubicada en el norte de Europa.Turku es una ciudad en el suroueste de Finlandia.


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Krister Leon Sundblad

1952 Born in Stockholm, Sweden.

1970-1974 Basic university studies in Stockholm, Sweden.

1981 PhD thesis at the University of Stockholm, Sweden

1974-1982 Geologist at the Geological Survey of Sweden.

1983 Exploration geologist in Nicaragua.

1984-1986 State Geologist at the Geological Survey of Sweden.

1987-1997 Associate Professor at the University of Stockholm.

1997-2001 Professor at the Technical University of Trondheim, Norway.

2001- Professor at the University of Turku, Finland


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Geologa, metalogena y aspectos

histricos de la minera en Europa Contenido

Parte 1. Perspectivos histricos. Junio 17

Parte 2. Metalogena Precambrico Junio 17El Escudo de Fennoscandia

Parte 3. Metalogena Palaeozoico Junio 18

Parte 4. Metalogena del Mar Tethys y de los Alpes Junio 18


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Parte 1, Junio 17, 20135:30 - 6:30 p.m.

Perspectivos histricos

Krister Leon

Sundblad


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In a historical perspective, nothing can beat Cyprus, Greece and Cornwall,when comes to earliest mining in Europe.


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Cyprus, Laurion and Cornwall served the Roman empire (and many previouscultures) with necessary metals for peaceful and hostile purposes


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Cyprusserved pre-Roman cultures and the Roman empire with Cu.

Cornwall(Sn), provided the tin for the bronze cultures for 1000s of years,whileLaurion(Ag) was essential for the Greek culture.


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Later, Belgium and Germany were the centersfor mining and developing mining techniques.


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Vielle Montagnein the Ardennes (Belgium) served the Roman empire with Pb-Zn.

Kupferschiefer (Cu) andErzgebirge(Sn and Ag), both Germany,were main European metal producers for 1000 years.


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German knowledge and technology on ores and mining were world-leading.Agricola formulated the first scientific principles on ores and how to find them.

Georgius Agricola (1494-1555) De Re Metallica (1555)


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But in amodernperspective, nothing can beat Finland and Sweden,when comes to present mining in Europe.

1. It is the biggest complex of Precambrian crust in Europe.2. It isvery rich in mineral resources (and metals).


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a. history of mining activities in northern Europe

The Falun mined produced copper before Sweden existedand was for a time the biggest copper mine in the world.


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The Sala mine was the biggest silver producer in the world before the Spanish conquistadors came to Latin America


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b. discoveries of metals (and other elements)many tens of elements have been discovered in northern Europe)


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c. the metal production (from ancient to present)


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d. present mining

More metals than ever are produced from ores in the Fennoscandian Shield.


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Present mines in EuropeKiruna Sweden FeAitik Sweden CuSkellefte District Sweden Cu, Zn and AuSvartliden Sweden AuGarpenberg Sweden Cu, Zn, AgZinkgruvan Sweden Zn, PbDannemora Sweden FePyhsalmi Finland Cu, Zn

Laiva Finland AuSuurikuusiskko Finland AuKemi Finland Cr Hitura Finland NiTalvivaara Finland NiKevitsa Finland NiOrivesi Finland Au

Pampalo Finland AuSydvaranger Norway FeKupferschiefer Poland Cu


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Parte 2, Junio 17, 20136:30 - 8:00 p.m.

Metalogena del Precambrio El Escudo de Fennoscandia

Krister LeonSundblad


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Northern Europe is strongly dominated by the Fennoscandian Shield

The Fennoscandian Shield is the largest Precambrian crustal complex in Europe.


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The amount of ore deposits in northern Europe is larger than in most other parts of the world.Some of these ores are significant in size and many hundreds of these have been mined, some in

very large operations.

As a consequence, mining has played a major role for the Nordic countries to evolve frominsignificant and peripheral areas in northern Europe to leading centers with respect to mining,metal production and high-technology industries.

Mining started already during the iron age, became significant in the 9th century whenunderground mining started in Falun, and is still important in several regions, particularly inSweden, Finland and westernmost Russia.

The ore deposits are hosted by rocks of a large variety of types, ages and origin and themetallogeny of northern Europe is a result of a long and complex history that started more than3000 millions of years ago.


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1. The Fennoscandian Shield

The Fennoscandian Shield is the largest of all Precambrian terrains in Europe and includesseveral orogenic complexes ranging in age from Archaean to Proterozoic. The metallogenetichistory of the Fennoscandian Shield is complex but follows closely the crustal evolution.

Several important segments are recognized in the Fenno-scandian Shield.

1. The Archaean Domain

2. The Karelian Schist Belt (+ Lapland Greenstone Belt)

3. The Svecofennian Domain

4. Transscandinavian Igneous Belt

5. Gothian Domain

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3

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The Fennoscandian Shield, includes bothArchaean and Proterozoic orogenies, inRussia, Finland, Sweden and Norway.


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More details on the crustal evolution in the Fennoscandian Shield

1. The Archaean Domain

The Archaean Domain is dominated by granodiorites, tonalites and komatiitic greenstone belts,emplaced at 2700-3100 Ma.

Slightly older crustal components (up to 3500 Ma) have been found locally.

The Archaean rocks were deformed and metamorphosed by theSaamian and Lopian orogenies,which led to cratonization of the Archaean crust. In this way, one of the first continents inEurope had been formed. A similar process had simultaneously also created a continent in theUkraine, but that continent was at that time located far away from Fennoscandia).


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2. The Karelian Schist Belt (+ Lapland Greenstone Belt)

Weathering and erosion of the Archaean continent started immediately after the continent had been formed. No vegetation existed at this time and the erosion products were quickly trans- ported by landslides and rivers to the surrounding oceanic waters.

We can see many pieces of evidence for this along the southwestern margin of the ArchaeanDomain; conglomerates, quartzites, marbles and turbiditic sediments indicate silent shallow-marine deposition while the deeper marine products further off shore indicate more rapidaccumulation.

Igneous activity started already at 2400 Ma, when large gabbroic layered intrusions wereemplaced at various sites within the Archaean craton.

These intrusions were followed by dolerites and komatiitic volcanic rocks that were intercalatedwith the epiclastic sediments. Most of this igneous activity took place at 2200-2100 Ma, inconjunction with rifting along the south-western margin of the Archaean continent.

At 1960 Ma, this rifting became successful and a proper ocean (with development of oceaniccrust) was created. The best evidence for this is the Jormua ophiolite in eastern Finland.


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3. The Svecofennian Domain

The oceanic conditions remained during the Svecofennian (1920-1890 Ma) when a huge amountof juvenile crust was formed.

Some of this activity took place along, and within, the south-western margin of the Archaeancontinent, which now was an active continental margin related to subduction. This can bestudied in the Kiruna and Aitik regions in northern Sweden.

Most Svecofennian rocks were, however, formed under marine conditions and gave rise toisland arcs (in the Skellefte and Pyhsalmi regions) and turbidite-dominated areas.

The southwesternmost Svecofennian region is located in Bergslagen, Sweden, where the deposi-tional conditions indicate shallow-marine sedimentary and volcano-plutonic environments near an Archaean continent. This continent must have been located southwest of the Svecofennianenvironments and been lost since then.

The Svecofennian crust was subject to orogenic activities at repeated times, including 1870,1845, 1830 and 1800 Ma, all referred to as theSvecokarelian orogeny. As a result, the continenthad increased in size and consisted now of Archaean and Svecofennian crustal components.


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4. Transscandinavian Igneous Belt (and rapakivi granites)

The south-western margin of the Archaean and Svecofennian continent turned immediately intoan active continental margin, resulting in extensive granitoid and rhyolitic subaerial volcanicrocks. The first expressions of this subduction-related activity took place already at 1845 Ma, but the main igneous phases were formed at 1800 and 1770 Ma respectively.

A very different igneous phase lasted from 1700 to 1670 Ma and in an extensional environmentwith generation of A-type granitic and rhyolitic subaerial volcanic rocks.

Both above-mentioned igneous complexes are referred to as the Transscandinavian Igneous Belt(TIB) and is always located along the western margin of the metamorphosed Svecofennian crust.It is very well exposed in south-eastern Sweden but also occur under the Caledonian rocks alongthe border between Sweden and Norway.

The extensional environment that had created the 1700 to 1670 Ma TIB rocks continued atcertain spots in southern Finland and in the Ladoga region. The first spot was the 1645 MaWiborg rapakivi granite Batholith and was followed by similar rapakivi batholiths at 1545 Ma atSalmi, land and (under the Phanerozoic cover) in the Riga region.


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5. Gothian Domain

The Gothian Domain has got its name from the oldest crustal components in south-westernScandinavia, 1600 Ma old meta-sedimentary rocks and metamorphosed granitoids.

Later rocks include 1400 and 1200 Ma granitoids as well as sedimentary formations andassociated mafic volcanic rocks.

This Gothian Domain evolved far away from the rocks in the Archaean-Svecofennian-TIBcontinent, but finally, at 1000-950 Ma, the Gothian Domain collided with the Archaean-Svecofennian-TIB continent.

This collisional event is referred to as theSveconorwegian orogenyand was followed byextensive post-orogenic (900 Ma) granitic intrusions, mainly in southern Norway.


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The Metallogeny of the Fennoscandian Shield follows closely the crustalevolution and is thus very complex.

The following basic mineralizing events can be recognized:

A. ARCHAEAN MINERALIZATION

B. PROTEROZOIC MINERALIZATION

I. Mineralization in the earliest Palaeoproterozoic

II. 1.9 Ga mineralization within the Svecofennian Domain

III. Stitching plutons within the Svecofennian (and Archaean) Domains

IV. Proterozoic gold within the Svecofennian (and Archaean) Domains

V. Mid to Late Proterozoic mineralization in Southwestern Scandinavia


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A. ARCHAEAN MINERALIZATION

Archaean crust occur in eastern Finland and westernmost Russia (as well as smaller areas innorthern Sweden and Norway).

A number of ore types, tied to Archaean crust have been recognized in Finnish and RussianKarelia as well as in the Kola Peninsula region.

The most important of these are the ore bodies tied to 2700-3100 Ma old greenstone belts andassociated tonalitic intrusions, both in the Finnish and Russian parts of Karelia.


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B. PROTEROZOIC MINERALIZATION


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I. Mineralization in the earliest Palaeoproterozoic;

a. failed rift systems

After a craton had been formed in the Late Archaean, several (failed) attempts to rift this cratontook place in the earliest Palaeoproterozoic, which resulted in a variety of ore-bearing environ-ments in the Nordkalott province:

a) 2.4 Ga layered intrusions with Cr, Pt, and PdPenikat in the Kemi regionMonchegorsk in the Kola Peninsula regionBurakovski east of lake Onega

b) 2.1 Ga layered intrusions with Ni-CuPetsamo (Pechenga) in the Kola Peninsula regionKevitsa and Sakattilampi, NE Finland

c) 2.1 Ga stratiform Cu in greenstone beltsViscaria, Kiruna region, N Sweden


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2400 Ma layered intrusions with Cr, Pt & PdMonchegorsk and Burakovski, Russia

Penikat (Kemi region), Finland

2100-2200 Ma Ni-Cu deposits in greenstone belts Petsamo (Rus), Kevitsa and Sakattilampi (Fin)

2100-2200 Ma stratiform Cu in greenstone beltsViscaria, Sweden


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b. Sediment-hosted Cu-mineralization

Nussir and Voronov Bortwo examples of early Proterozoic sediment-hosted chalcocine-bornite-chalcopyrite mineralization


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c. Successful ocean opening at 1960 Ma

At 1960 Ma the efforts to rift the Archaean continent finally became sucessful. An ocean openedup southwest of the Archaean continent and led to the production of oceanic crust. A piece of Archaean crust was probably now removed from Fennoscandia and if this was the case, we havenever seen it again. A small piece of the 1960 Ma oceanic crust is, however, preserved inFinland; the Jormua ophiolite.

This ophiolite was thrust on top of the Archaean continent (probably during the Svecokarelianorogeny) and rests with a tectonic contact on top of the Archaean crust. The Jormua ophiolitecan be followed towards the south (although overprinted with deformation and metamorphism)into the Outokumpu region.

With such an association, an ophiolite and a large-scale massive sulphide deposit, it is easy toimagine that Outokumpu is a Cyprus type deposit.


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d. Ore deposits in the 1950-2200 Ma Kalevian meta-sedimentary successions

The sedimentary rock units associated with the Jormua ophiolite have also attracted attentionrecently:

Talvivaara is a big industrial operation that recently has started for extracting Ni and U out of black schists in the Kajaaai region.

Hammaslahti was mined for Cu and Zn during the 1980:ies from a volcanogenic massivesulphide deposit in turbiditic host rocks. It can be compared with the Escanaba model.


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Talvivaara (Ni, U)

Outokumpu (Cu, Zn, Co)

Hammaslahti (Cu, Zn)


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II. 1920-1890 Ma mineralization within the Svecofennian Domain

After the accretion of the Jormua ophiolite, emplaced on top of the Archaean continent, a newocean opened at the same site at about 1890-1920 Ma, i.e. to the southwest of the presentArchaean crust (and its obducted fragments of ophiolites and Kalevian schists.

The SW border was then located slightly more to thesouthwest, coinciding with the Raahe-Ladoga line.

In this 1900 Ma ocean, several Svecofennianterranes developed, which amalgamated to theArchaean continent in the Svecokarelian orogeny.

These terranes include the following mining districtsor deposits:

a. Kiruna/Aitik b. Vihanti/Pyhsalmi

c. Skellefte Districtd. Bergslagen District

b

a

c

d


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a) Terrestrial 1910 Ma volcanism, along the south-western margin of the Archaean continent(comparable to present-day Chile), was associated with the Kiruna magnetite-apatite Fe ores andthe Aitik Cu-Au deposit.


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b) Continental-margin, shallow-marine1910 Ma volcanism along the southwestern

margin of the Archaean continent.This zone extends from Tjmotis (T) innorth Sweden to Varkaus (V) in southeastFinland.

It was associated with formation of VMSdeposits (of which the largest are located atVihanti and Pyhsalmi).

Although similar in style compared to theisland arc environment of the Skelleftedistrict, these groups arenot the same.

T

V


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c) Island arc 1890 Ma magmatism in the Skellefte district (S),

with a number of Kuroko type Cu-Zn deposits (Kristineberg, Nsliden, Udden, etc.)

Comagmatic plutonic complexes to the island arc system include granitoids within the CentralFinnish Batholith and its associated Cu-Mo-W deposits (Kopsa, Yljrvi and Ktaberget).

The region can be further traced into theTampere region (T).

T

S


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The island arc environment of the Skellefte district is spatially surrounded by discontinuous pods of ultramafics with significant Ni ores (Lappvattnet, Kotalahti, Kylmkoski and Vammala),revealing deep and regionally significant sutures, which probably represent terrane boundaries.


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FalunDannemora

Garpenberg NorbergGrngesberg

Zinkgruvan


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III. Stiching plutons within the Svecofennian (and Archaean) Domains

After metamorphism and amalgamation of Svecofennian terranes to the Archaean craton, theSvecofennian and (Archaean) Domains were intruded by granitoids in several generations:

1. 1800 Ma granites

a) Late collisional uplift granitesintragranitic Mo deposits(Bispberg,

Allebuoda and Tepasto)exoskarn-W deposits(Yxsjberg) U deposits(Pleutajokk)

b) Subduction-related TIB batholithsepithermal Pb-Zn deposits(latorp)


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2. 1700-1500 Ma anorogenic granites and volcanic rocks in extensional tectonics

a) 1700-1670 Ma batholiths in the northern part of the Transscandinavian Igneous Belt polymetallic (Cu-Zn-Pb-Sn-In) intragranitic greisen deposits (Van and Gillerdrgen)


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b) 1650-1500 Ma rapakivi granites

i. polymetallic (Cu-Zn-Pb-Sn-In) intragranitic greisen deposits (Eurajoki, Pahasaari, Korsvik and Jungfrubergen)

ii. polymetallic (Cu-Zn-Pb-Sn-In) exoskarn deposits (Pitkranta).


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Post-Svecofennian granitoid-related deposits

1800 Ma Pleutajokk U deposit

1800 Ma Bispberg Mo deposit andYxsjberg W skarn deposit.

1800 Ma TIB and epithermal latorpPb-Zn-Ag deposit.

1650-1500 Ma anorogenic Cu-Zn-Pb-Sn-In skarn deposit (Pitkranta).

1650-1500 Ma anorogenic Cu-Sn-Ingreisen deposits (Jungfrubergen,Korsvik and Eurajoki).


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IV. Proterozoic gold within the Lapland Greenstone Belts, the Svecofennian(and Archaean) Domains

Mesothermal gold deposits are found in several geological environments within theLapland Greenstone Belts and the Svecofennian Domain, formed from a number of orogenic processes:


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a) Svecokarelian (1800-1850 Ma) shear zones in the greenstone belts of the Nordkalott province

This group includes Bidjovagge, Pahto-havare, Saattopora, Suurikuusikko andmany others.

The mesothermal gold at Ringvassyaalso belong here, although Archaeanzircons have been recorded in these

greenstone successions.


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b) Svecokarelian shear zones c) Even later (


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V. Mid to Late Proterozoic mineralization in Southwestern Scandinavia

Southwestern Scandinavia records a different geological and metallogenetic evolution comparedto the Archaean-Svecofennian domains. The following ore types are among the most important:

a) Stratiform Zambia-type Cu deposits in1100 Ma continental sedimentary basinsrelated to failed rift (Stora Strand)

b) Mesothermal Au deposits, associatedwith the 900-1000 Ga Sveconorwegianorogeny (Eidsvoll and Harns)

c) Stitching 900 Ma granites with Mo(Knaben) and Ti deposits in anorthosites(Tellnes), all in SW Norway

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