WEST HAWK IMPACT CRATER
by: Charles O’Dale
- Type: Simple
- Age (ma): 100 (geological analysis)a
- Diameter: 2.44 km
- Location: Manitoba, Canada. N 49° 46′ W 95° 11′
- Shock Metamorphism: PDF in quartz grains, a large amount of glassy and melted fragments, isotropization of tectosilicates, and shock-induced twinning in target carbonate rocks grains.
a Dating Method: The presence of a breccia lens, which is usually eroded or not present in very old craters implies a Mesozoic age of 250 to 65 MA. (see the Presqu’ile Impact Structure for an illustration of a crater with the breccia lens fully eroded away). The impact crater is devoid of rocks whose presence would be detected if the crater existed 180 million years ago. The sediments that have accumulated in the crater do not contain fossil remains but resemble 60 million year old Manitoba sediments. No reliable age has been determined by isotopic age dating (Ogilvie et al., 1984). The best estimate for the West Hawk impact event is 100 million years ago.
General Area: Subdued relief near the southwestern edge of the Canadian Shield. The area is heavily forested and has been glaciated. The target rocks are crystalline.
Specific Features: Structure lies within the polygonal 3.6 km diameter West Hawk Lake. The shape of the lake contrasts with others in the immediate area. There is a partial ring of hills rising -40 m around the lake. The crater is clearly superimposed upon the structural fabric of the rocks in the area. A major fold can be seen northwest of the crater.
The West Hawk Lake Impact Crater, a simple crater, was excavated in metavolcanic and metasedimentary rocks of the Precambrian Superior Province. It lies within Whiteshell Provincial Park in eastern Manitoba, about 100 km east of Winnipeg.
Severe erosion of the crater’s original fractured rim has expanded the shoreline to a roughly circular lake with an average diameter of 3.6 km. The present erosion plane is approximately 66 m below the original surface leaving some inconspicuous hills around the circumference of the lake that may be the remains of part of the rim. Numerous cliffs showing fractured rock are found around the shoreline. The southern boundary of the lake is underlain by volcanic greenstones of Archean age while the northern area consists of Keewatin meta-clastics sediments and tuffs underlain by granite and gneiss. (Halliday and Griffin, 1963)
In the fall of 2001 by a team of researchers led by Drs. J. Teller and M. Boyd studied the unique characteristics of the sediments in the basin of West Hawk Lake.
Four cores were extracted from the deepest part of the lake and analyzed to relate changes in the sediments to:
- The hydrologic changes within the basin, and;
- A fire history of the region.
Moisture content, bulk mineralogy, clay mineralogy, and particle size distributions were determined from regularly spaced samples in the sequence as well as from specifically targeted samples. Microscopic charcoal analysis was done at regularly spaced intervals to construct a regional fire record. The charcoal record indicates that the occurrence of fires in the region surrounding West Hawk Lake may be related to climate.
(M. Boyd, PhD, Lakehead University, personal correspondence with the author) We believe the upper ~2 m [of the sediment in the lake] represents the last 7000-8000 years of the lake’s history, and represents a time when the lake (as today) was small and isolated. On the other hand, the varved (seasonally laminated) sediment in the lower 9 m of the core was deposited during the late Pleistocene, when the waters of glacial Lake Agassiz covered the basin.
Boyd, M., Kling, H., McMillan, K. and Teller, J.T. 2003. “A varved paleoecological record from West Hawk Lake meteorite impact crater, southeastern Manitoba, Canada”. Abstracts, 2003 CANQUA meeting, Halifax, Nova Scotia, (CONCLUSION).
Preliminary analysis of the upper 10.8 m of sediment in West Hawk Lake indicates that major changes have occurred in this basin since deglaciation. Although radiocarbon dates do not provide a clear chronology, pollen stratigraphy (specifically, the shift from Picea to Pinus-dominated vegetation) indicates that the base of the core dates to ca. 9000 – 10,000 BP. Likewise, the rise of Pinus strobes in the upper 2m of the core indicates that unit B was deposited after 7000 BP. Roughly 3 m of varved sediment lies between these two chronological markers, and the accompanying paleoecological record provides initial evidence of 200-yr. (min) drought cycles. Similar cycles have been identified on the Northern Great Plains throughout the middle to late Holocene (Clark et al., 2002), and may be due to solar forcing (Yu and Ito. 1999). Our results suggest that these cycles also significantly impacted biota on the southwestern edge of the boreal forest.
Four trophic periods are reconstructed from algal microfossil content. At the base of the core, absence of algae suggests cold, turbid, and/or nutrient-poor conditions. This is consistent with deposition in glacial Lake Agassiz, and the basal age estimate of ~9000-10,000 BP determined from pollen correlation broadly supports this hypothesis (Leverington et al., 2002). Between this phase and the establishment of modern conditions, West Hawk Lake was part of a more productive system which likely declined in a real extent through time. This ‘transitional’ period may represent a time when West Hawk Lake was part of an expanded Lake of the Woods, or it may represent a more productive, terminal, phase of glacial Lake Agassiz. Varve counts indicate that this transitional period lasted <900 yrs.
- The target rock type is Precambrian crystalline and metasedimentary;
- The impact crater is completely enclosed in the 3.6 km diameter 110 m deep West Hawk Lake;
- A 94 m thick accumulation of unconsolidated sediments resting on top of bedrock covers the crater (Boyd 2008);
- The bedrock below the lake and the unconsolidated sediments consist of a badly broken up and disturbed zone of 330 m thick fall back breccia lens. The impact crater was discovered when a drill core taken from West Hawk Lake was studied and found to possess impact breccias. Further examination of these breccias has revealed numerous signs of shock metamorphism. These include secondary minerals such as zeolite, zoisite, calcite, chlorite, montmorillonite and biotite. These minerals are common in impact melt and indicate that hydrothermal alteration was widespread after the impact event. Hot springs on earth resulting from hydrothermal vents are a source of exotic forms of life, and;
- Beneath the breccias is a 200 m thick zone of fractured bedrock of metamorphosed sedimentary and volcanic rocks. The broken bedrock is characterized by a number of mineralogic, crystallographic and textural changes that are produced by instantaneous application of high stress. These are called shock metamorphic features and are characteristic of known meteorite impact craters.