Duluth Complex

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Shaded-relief image showing Duluth Complex arcing from Duluth to Pigeon Point, interrupting and splitting Mesabi and Gunflint Ranges
Shaded-relief image showing Duluth Complex arcing from Duluth to Pigeon Point, interrupting and splitting Mesabi and Gunflint Ranges

The Duluth Complex, the related Beaver Bay Complex (often treated as part of the Duluth Complex),[1] and the associated North Shore Volcanic Group are rock formations which comprise much of the basement bedrock of the northeastern part of the U.S. state of Minnesota.[2] The Duluth and Beaver Bay complexes are intrusive rocks formed during the Midcontinent Rift; they adjoin and are interspersed with the extrusive rocks of the North Shore Volcanic Group produced during the same geologic event. These formations are part of the Superior Upland physiographic region of the United States, which is associated with the Laurentian Upland of the Canadian Shield,[3] the core of the North American Craton.

Contents

[edit] Location

The Duluth Complex includes much of Minnesota's Arrowhead Region north of Lake Superior. From the west near Duluth, Minnesota, it arcs north and northeast to about 48° north latitude south of Knife Lake, proceeds east at that latitude some five to twenty kilometers distant from and south of the Canadian border to about 90° west longitude where it joins the border at the Pigeon River, and thence runs east near and along the border to Lake Superior.[4] The Duluth and Beaver Bay complexes lie south of this line.

Near Lake Superior these intrusive formations intermingle in a complex mosaic with the rocks of the associated North Shore Volcanics, which also are relics of the Midcontinent rifting event.[5] The Duluth and Beaver Bay Complexes extend a short distance under Lake Superior south of the present lakeshore, but in most places along and near that shore their southern reaches are overlain by the North Shore Volcanic Group.[6]

[edit] Formation

Some 1,100 million years ago (mya) the North American craton began to split apart in the Midcontinent Rift.[7] Over a period of some 15-22 million years, magma rose through the earth’s crust, separating the older formations and creating new rock in the area of the rift.[8] The rock sequences thereby created are known as the Keweenawan Supergroup.[9] Rocks of this group north of Lake Superior are the layers of the North Shore Volcanic Group and the adjoining formations of the Duluth and Beaver Bay Complexes.

The Sawtooth Mountains rising from Lake Superior
The Sawtooth Mountains rising from Lake Superior
Palisade Head, a rhyolitic extrusion of the Midcontinent Rift, on Lake Superior
Palisade Head, a rhyolitic extrusion of the Midcontinent Rift, on Lake Superior

The North Shore Volcanics originated c. 1109-1096 mya[10] from hundreds of individual lava flows, forming six distinct tilted and partially-stacked plateaus which total more than 8,000 meters in thickness. These tilt toward the syncline under Lake Superior, as shown in the adjacent picture of the Sawtooth Mountains, whose slopes mirror the shoreline rocks. While principally basaltic, these flows also include rhyolites and other types.[11] As part of of the Middle Proterozoic Keweenawan sequence, these volcanic layers are part of one of the oldest, largest, and best-preserved plateau lava provinces in the world.[12]

These volcanics created the "roof rocks" into which were emplaced the mafic formations of the Duluth Complex. Primarily formed after 1102 mya,[13] the oldest formations are near Duluth, and the youngest to the northeast near Tofte.[14] Insulated by the overlying roof rock, upwelling magma cooled slowly, and the mafic rock into which it cooled therefore is coarse-grained. These intrusions formed a sill some 16 km thick,[15] primarily of gabbro, but with significant amounts of anorthosite and other related granitic rocks.[16] The Duluth Complex is one of the largest intrusions of gabbro on earth,[17] and one of the largest layered mafic intrusions known. It covers an area of 4715 km2.[18] The lower portion of the intrusion along the northwestern margin consists of ultramafic cumulates with associated segregations of nickel, copper and platinum group elements. The upper differentiated portions include ilmenite bearing labradorite anorthosites.[18]

Along its northern margin, the Duluth Complex adjoins older structures, the Archaen Ely Greenstones (once thought to be the oldest exposed rock on earth),[19] and the ore-bearing Mesabi and Gunflint iron ranges from the Penokean orogeny, a mountain-building event from Paleoproterozoic times.[20] Those two Middle Precambrian ranges are thought to have once been joined, but intruding magma of the Duluth Complex baked and engulfed the center of the mountain chain, separating it into the two ranges present today.[21]

To the south near Lake Superior, rock strata of the Duluth and Beaver Bay complexes are interspersed with and underlie the extrusive rock of the North Shore Volcanic Group.[22] The Beaver Bay Complex occupies the center of the North Shore Volcanics, and is slightly younger in age than the other mafic rocks of the Duluth Complex, dating from c. 1096 mya.[23] The volcanics and more recent sedimentary rocks were once thought to be underlain by the Duluth Complex all the way across Lake Superior to Wisconsin, where gabbro formations also exist.[24] The Duluth Complex was considered to be a giant lopolith, a lens-shaped structure depressed in the middle, connecting gabbro exposures on opposite sides of the lake,[25] but now is recognized to extend only a few kilometers south of Superior's North Shore.[26]

[edit] Contemporary landforms

Duluth's Enger Tower, constructed of local Keweenawan rocks, atop a gabbro knob (foreground)
Duluth's Enger Tower, constructed of local Keweenawan rocks, atop a gabbro knob (foreground)[27]
The rugged Misquah Hills
The rugged Misquah Hills

The Precambrian bedrock of the Duluth Complex and the North Shore Volcanics are not buried beneath layers of later sedimentary rock, as is common further south. And much of this bedrock is close to or at the surface. Glaciers scoured away earlier soils, and as is typical of the Canadian Shield, the new topsoils are thin and poor, being derived from the rock beneath or nearby rather than from deep layers of glacial till, which is intermittent and relatively shallow over most of the region.[28] Consequently much of the bedrock is exposed, except for the sediments and glacial till in the watershed of the Saint Louis and Cloquet Rivers inland on the west.[29]

Gabbro outcroppings anchor both ends of the complex. They dominate the city which gave the Duluth complex its name,[30] and also form part of Pigeon Point, the easternmost point of Minnesota. In between, Superior's shoreline from Duluth to the international border has been likened to one long volcanic outcrop,[31] albeit interrupted by parts of the Beaver Bay Complex, such as the anorthosite cliffs at Split Rock Lighthouse adjacent to basalt flows.[32] Prominent relics of volcanism include rhyolitic cliffs at Palisade Head, basaltic lava flows at Gooseberry Falls, and the Sawtooth Mountains further east. Along the lakeshore can be found quartz-banded thomsonite and agate gemstones created by mineral infilling of gas cavities created when the lava flows cooled.[33]

Interior highlands include Eagle Mountain and the other Misquah Hills.[34] Most of the eastern part of the Superior National Forest and its Boundary Waters Canoe Area Wilderness (BWCA) is located on the Duluth Complex, and its exposed Late Precambrian bedrock created many of the characteristic features of the region. The inland lakes on the gabbro intrusions lie in hollows formed by differential erosion of various formations of the bedded rock. These depressions were given their final form by glacial scouring during recent ice ages and then were dammed by glacial drift, creating the irregularly-shaped and rocky-shored lakes which are hallmarks of the wilderness.[35]

[edit] References

  1. ^ Green, Volcanic and Sedimentary Rocks (2004), p. 47.
  2. ^ Jira, Mineral Potential (2000).
  3. ^ Tapestry of Time and Terrain (2003).
  4. ^ Jira, Mineral Potential (2000); Heinselman (1996), plate 1.
  5. ^ Miller, Green, Severson, Chandler, & Peterson, Geologic Map of the Duluth Complex, (2001).
  6. ^ Ojakangas & Matsch (1982), pp. 52, 55–56.
  7. ^ Ojakangas & Matsch (1982), pp. 49–50, 55–57; Tapestry of Time and Terrain (2003).
  8. ^ Schneider, Holm & Chandler, Superior Swath (2006); Ojakangas, Morey & Green, Mesoproterozoic Midcontinent Rift System (2001), Abstract.
  9. ^ Ojakangas and Dickas, 1.1-Ga Midcontinent Rift System, central North America (2002), Abstract.
  10. ^ Naldrett (2004), p. 244 (Fig. 4.49).
  11. ^ Ojakangas & Matsch (1982), pp. 50–54.
  12. ^ Schmidt, Regional and local patterns of low-grade metamorphism (2008), Abstract; Green Volcanic and Sedimentary Rocks (2004), p. 52.
  13. ^ Green Volcanic and Sedimentary Rocks (2004), p. 52; Naldrett (2004), pp. 244 (Fig. 4.49), 246.
  14. ^ Frey & Robinson (1999), pp. 157–58.
  15. ^ Ojakangas & Matsch (1982), pp. 55–57.
  16. ^ Jira, Mineral Potential (2000); Topinka, America's Volcanic Past (2003); Miller, Green, Severson, Chandler, & Peterson, Geologic Map of the Duluth Complex (2001).
  17. ^ Schwartz & Thiel (1963), p. 114.
  18. ^ a b Guilbert, John M. and Charles F. Park, Jr., The Geology of Ore Deposits, Freeman, 1986, pp. 314-346, ISBN 0-7167-1456-6.
  19. ^ Chandler (2005), Geophysical Investigation of the Ely Greenstone Belt, pp. 4-5. Older rocks have since been found in Minnesota (the Morton gneiss of Southwest Minnesota) and Greenland and Labrador. Ojakangas & Matsch (1982), p. 24.
  20. ^ LaBerge (1994), p. 157; Ojakangas & Matsch (1982), pp. 56–57.
  21. ^ Ojakangas & Matsch (1982), pp. 56–57.
  22. ^ Ojakangas & Matsch (1982), pp. 52, 56.
  23. ^ Miller, Green, Severson, Chandler, & Peterson, Geologic Map of the Duluth Complex (2001).
  24. ^ LaBerge (1994), pp. 159–160.
  25. ^ Schwartz & Thiel (1963), pp. 114–15.
  26. ^ Ojakangas & Matsch (1982), pp. 55–56.
  27. ^ Sansome (1983), pp. 20–23.
  28. ^ Heinselman (1996), pp. 13–14.
  29. ^ Generalized Density of Bedrock Outcrops (map) (2001).
  30. ^ Sansome (1983), pp. 24–25; Ojakangas & Matsch (1982), pp. 167–68.
  31. ^ Ojakangas & Matsch (1982), p. 50.
  32. ^ Split Rock Lighthouse State Park Info (2008).
  33. ^ Ojakangas & Matsch (1982), pp. 53–54.
  34. ^ Miller, Green, Severson, Chandler, & Peterson, Geologic Map of the Duluth Complex (2001).
  35. ^ Ojakangas & Matsch (1982), p. 162; Heinselman (1996), pp. 12–13, 200.

[edit] Sources

  • Frey, Martin; Robinson, Doug (1999). Low-Grade Metamorphism. Oxford: Blackwell Science. ISBN 978-0632047567. 
  • Green, John (2004): Volcanic and Sedimentary Rocks of the Southwestern Sequence of the North Shore Volcanic Group, Field Trip Guidebook, Proceedings 50, Vol. 2. Institute on Lake Superior Geology, 2004. Retrieved 2008-04-27.
  • Guilbert, John M. and Charles F. Park, Jr., The Geology of Ore Deposits, Freeman, 1986, ISBN 0-7167-1456-6.
  • Heinselman, Miron (1996). The Boundary Waters Canoe Area Wilderness Ecosystem. Minneapolis: University of Minnesota Press. ISBN 0-8166-2804-1. 
  • LaBerge, Gene L. (1994). Geology of the Lake Superior Region. Tucson, AZ: Geoscience Press. ISBN 0-945005-15-6. 
  • Ojakangas, Richard W.; Matsch, Charles L. (1982). Minnesota's Geology. Minneapolis: University of Minnesota Press. ISBN 0-8166-0953-5. 
  • Sansome, Constance Jefferson (1983). Minnesota Underfoot: A Field Guide to Minnesota's Geology. Stillwater, MN: Voyageur Press. ISBN 0-8965-8036-9. 
  • Schwartz, George M.; Thiel, George A. (1963). Minnesota's Rocks and Waters. Minneapolis: University of Minnesota Press. LOC 54-6370. 

[edit] External links