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Article

The Medicine Hat Block and the Early Paleoproterozoic Assembly of Western Laurentia

by
Jennifer N. Gifford
1,*,
Shawn J. Malone
2 and
Paul A. Mueller
3
1
Department of Geology and Geologic Engineering, University of Mississippi, Oxford, MS 38677, USA
2
Department of Environment, Geology, and Natural Resources, Ball State University, Muncie, IN 47304, USA
3
Department of Geological Sciences, University of Florida, Gainesville, FL 32611, USA
*
Author to whom correspondence should be addressed.
Geosciences 2020, 10(7), 271; https://0-doi-org.brum.beds.ac.uk/10.3390/geosciences10070271
Submission received: 12 June 2020 / Revised: 3 July 2020 / Accepted: 8 July 2020 / Published: 15 July 2020
(This article belongs to the Special Issue 2020: A 10 Years Journey-Advances in Geosciences)
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Abstract

:
The accretion of the Wyoming, Hearne, and Superior Provinces to form the Archean core of western Laurentia occurred rapidly in the Paleoproterozoic. Missing from Hoffman’s (1988) original rapid aggregation model was the Medicine Hat block (MHB). The MHB is a structurally distinct, complex block of Precambrian crystalline crust located between the Archean Wyoming Craton and the Archean Hearne Province and overlain by an extensive Phanerozoic cover. It is distinguished on the basis of geophysical evidence and limited geochemical data from crustal xenoliths and drill core. New U-Pb ages and Lu-Hf data from zircons reveal protolith crystallization ages from 2.50 to 3.28 Ga, magmatism/metamorphism at 1.76 to 1.81 Ga, and εHfT values from −23.3 to 8.5 in the Archean and Proterozoic rocks of the MHB. These data suggest that the MHB played a pivotal role in the complex assembly of western Laurentia in the Paleoproterozoic as a conjugate or extension to the Montana Metasedimentary Terrane (MMT) of the northwestern Wyoming Province. This MMT–MHB connection likely existed in the Mesoarchean, but it was broken sometime during the earliest Paleoproterozoic with the formation and closure of a small ocean basin. Closure of the ocean led to formation of the Little Belt arc along the southern margin of the MHB beginning at approximately 1.9 Ga. The MHB and MMT re-joined at this time as they amalgamated into the supercontinent Laurentia during the Great Falls orogeny (1.7–1.9 Ga), which formed the Great Falls tectonic zone (GFTZ). The GFTZ developed in the same timeframe as the better-known Trans-Hudson orogen to the east that marks the merger of the Wyoming, Hearne, and Superior Provinces, which along with the MHB, formed the Archean core of western Laurentia.

1. Introduction

The Precambrian Medicine Hat Block (MHB) lies south of the Archean Hearne Province (Figure 1), and it was originally defined by structural features in overlying Paleozoic sedimentary rocks [1] and subsequently by potential field and seismic surveys [2,3]. Although its history is poorly constrained due to extensive Phanerozoic sedimentary cover (Figure 1), an Archean age for the MHB was first proposed on the basis of multi-grain U-Pb zircon ages acquired by ID-TIMS (isotope dilution-thermal ionization mass spectrometry) from five samples of drill core recovered from oil and gas exploration wells [4]. U-Pb ages of these samples range from approximately 2.6 to 3.3 Ga [4]. With its long history, the MHB clearly occupied an important position between the Wyoming Craton and the Hearne Province during the formation of the supercontinent Laurentia.
In this paper, we focus on refining the evolution of the northwestern crystalline basement of the MHB and western Canada sedimentary basin and relate that history to that of other terranes that accreted to Laurentia prior to 1.7 Ga. We report results of 484 new single zircon U-Pb ages obtained by laser ablation multi-collector ICP-MS from drill core and xenoliths previously described and analyzed by Villeneuve et al. [4] and Davis et al. [5] in order to extract the maximum information from these unique samples, including all new in situ Lu-Hf analyses by the same method. The xenoliths are from Eocene minettes of the Sweetgrass Hills area of the Montana alkali province (MAP) located within southern Alberta and northern Montana (Figure 1; [6]). These alkaline volcanic-entrained xenoliths provide a unique opportunity to study the age and history of the enigmatic continental crust of the northwestern MHB (e.g., [5,7]) and the buried southern (Alberta) part of the western Canada sedimentary basin [8,9,10,11,12,13]. Constraining the relationships of the Medicine Hat block to the adjacent Paleoproterozoic belts (e.g., Great Falls Tectonic Zone (GFTZ), Trans-Hudson orogen (THO), and Vulcan low) is important for understanding the geodynamics of the rapid, Paleoproterozoic assembly of Laurentia proposed by Hoffman [14].

Geologic Background and Previous Work

The boundary separating the MHB and the Hearne Province to the north is the Vulcan structure, which is a prominent, linear feature characterized by both gravity and magnetic lows (Figure 1; [9]). The northern limit of the MHB in southern Alberta and northern Montana, including the Vulcan structure, is entirely buried beneath the sediments filling the Western Canada sedimentary basin, which is a Cordilleran foreland basin. On its eastern margin, the MHB is bounded by Paleoproterozoic rocks of the Trans-Hudson orogen (Figure 1; [20,21,22]). To the south, at least parts of the MHB lie within the Great Falls tectonic zone (GFTZ) that formed during the Great Falls orogeny (1.7–1.9 Ga; [23]). The GFTZ also marks the northern limit of the Archean Beartooth-Bighorn magmatic zone of the Wyoming Province [24,25]. Proposals for the origin of the GFTZ have ranged from Archean and Paleoproterozoic suture zones to an intra-continental shear zone [2,26,27,28].
South and west of the MHB, the Montana Metasedimentary terrane (MMT; Figure 1) of the Wyoming Province is dominated by >3.0 Ga quartzofeldspathic gneisses in which belts of distinct Archean metasupracrustal rocks are preserved [29,30,31,32,33,34]. Exposures in the MMT are predominantly in Laramide uplifts, e.g., the Tobacco Root Mountains, Highland Mountains, Madison Range, and Ruby Range [24,25,30,31,32,33,34,35,36,37,38,39,40,41,42,43,44,45,46,47,48,49,50,51,52,53,54,55]. The ages reported from the MMT include: (1) rare Eoarchean ca. 3.93 Ga detrital zircons from Archean quartzites [33,40]; (2) Paleoarchean tonalitic to tronhjemitic gneisses (ca. 3.3 Ga) [32,37]; (3) Neoarchean quartzofeldspathic gneisses and amphibolite-grade metamorphism at ca. 2.7 Ga to 2.8 Ga [31,32,33,34,37,41,42,43,44,45,46]; and (4) Paleoproterozoic metamorphism at 2.45 and 1.7–1.9 Ga [24,30,37,38,39,45,47,48,49,50,51,52,53,54,55]. Throughout the MMT, ages representing prograde, peak, and retrograde intervals of metamorphism have been reported from zircon, monazite, micas, and amphibole in the U-Pb, Sm-Nd, and K-Ar systems. This clearly defined approximately 1.7–1.9 Ga event [24,30,37,39,45,47,48,49,50,51,52,53,54,55] is broadly recorded across western Laurentia, particularly in the K-Ar (40Ar/39Ar) system. In addition to the MMT, terranes bordering the MHB and recording this interval of dominantly metamorphic cooling ages include the Vulcan aeromagnetic low [9], GFTZ [28,56,57,58,59], and THO [60,61,62,63,64,65,66,67]. The broad geographic range of this event(s) leads to the conclusion that these parts of western Laurentia were fully assembled prior to approximately 1.7 Ga and one or more widespread thermal event(s) likely affected the amalgamated terranes in the interval from approximately 1.7 to 1.8 Ga. Knowing that all of the cratonic sections were unified by approximately 1.7 Ga leads to the question of how and when these various terranes evolved prior to their amalgamation into Laurentia.

2. Materials and Methods

2.1. Location and Description of Samples

Zircon concentrates from seven samples were obtained from the Geological Survey of Canada. These include drill cores from the “PCA Home Pacific Knappen” (PCAPK), “Imperial Calstan Lake Newel” (ICLN), “PCA Calstan Parkland” (PCACP), and “PCP Medicine Hat Block” (PCPMB) wells [4]. Samples DRA-93-26, DRA-93-01, and DRA-93-20 are xenoliths from two localities in the Sweetgrass Hills, Coulee 29 minette [7,68] in the Milk River area of southern Alberta [69] and Sill 39 in northern Montana (Figure 1). Published U-Pb ages from Villeneuve et al. [4] and Davis et al. [5], analysis type, as well as sample descriptions are in Table 1.

2.2. U-Pb Geochronology of Zircon

Zircon grains provided by the Geological Survey of Canada were prepared using traditional methods of crushing and grinding, followed by density separation by panning, high-density liquids, and by magnetic susceptibility using a Frantz magnetic separator. Hand-picked zircon grains were embedded in a 25 mm epoxy disk, together with fragments of a natural zircon standard FC-1 [70,71,72]. The mounts were polished to approximately half thickness of the individual zircon grains, and imaged using cathodoluminescence (CL). In addition to the 484 U-Pb analyses, 106 Lu-Hf analyses were obtained from selected zircon domains identified in the CL images for each zircon. The zircon mounts were first analyzed for U-Pb, followed by Lu-Hf analysis in the same CL domain as the U-Pb analysis, but conducted in a separate session.
The U-Pb ages were determined using the Nu Plasma laser ablation-multi-collector-inductively coupled plasma mass spectrometry (LA-MC-ICP-MS) at the University of Florida (Gainesville, FL, USA) following methods in Mueller et al. [73]. The analyses utilized a New Wave 213 nm laser and a 20 μm spot diameter. Each individual U-Pb analysis consisted of 30 s of measurement during ablation in order to minimize ablation pit depth and elemental fractionation. Isotopic data were acquired using the Nu-Instruments Time Resolved Analysis software, which allowed isotopic ratios to be calculated from data collected simultaneously in individual faraday and ion-counting channels during the 30 s ablation. Fractionation and drift corrections were calibrated against multiple ablations of the FC-1 natural zircon standard (Duluth Gabbro; 1098 Ma; [70,71,72]); each batch of 10 unknowns was bracketed between two pairs of FC-1 analyses. The zircon isotopic data were reduced with the in-house program hosted in Microsoft Excel (CALAMARI, © P.A. Mueller), with ages and concordia diagrams calculated using Isoplot v. 4.0 [74,75]. Representative age errors based on the long-term reproducibility of FC-1 are 2% for 206Pb/238Pb (standard error of the mean (s.e.m.)) and 1% for 207Pb/206Pb (s.e.m.). U-Pb data, including for FC-1, are provided in the Supplementary Data (Tables S1 and S3).

2.3. Lu-Hf Isotopic Analysis of Zircon

Lu-Hf analyses were also conducted by laser ablation with the MC-ICP-MS in static mode following the methods in Mueller et al. [73]. Faraday collectors were used for the simultaneous measurement of 180Hf, 178Hf, 177Hf, 176Hf, 175Lu, 174Hf, and 172Yb [73]. The analyses were performed with online Lu and Yb isobaric interference corrections, using 176Lu/175Lu = 0.02653 and 176Yb/172Yb = 0.5870, both of which are within the range of published values [76,77]. The non-radiogenic isotopic ratio of 180Hf/177Hf was measured to monitor mass bias corrections determined using 177Hf/179Hf and determined to be within the error of the true value (1.88710) for all unknowns and standards. Analyses that did not meet this criterion were discarded. Corrections for Lu and Yb interferences (peak stripping) were done on-line and based on mass bias-corrected ratios using the mass bias factors derived from Hf isotopes. This method was chosen because of the low reproducibility of Yb isotope ratios. Although mass bias for Yb, Lu, and Hf may have an elemental component to them, we do not utilize 176Hf/177Hf data that have combined Yb + Lu corrections in excess of 25%. Analyses with Yb + Lu corrections exceeding 20% are not used to define the limits of model ages or initial εHf for any suite of zircons. All Hf, Lu, and Yb isotopic ratios were corrected for mass bias using 178Hf/177Hf = 1.46718. Each analysis consisted of a 40 μm spot size and 20-s background measurement, up to one minute of measurement during ablation, and a 30-s purging period between analyses. Multiple analyses of FC-1 (Duluth Gabbro zircon standard; [71,78]) yielded 176Hf/177Hf = 0.28217 (± 0.00002, 2σ, n = 9), which was within the error of solution analyses of this standard (176Hf/177Hf = 0.282174 ± 0.000013, 2σ; [73]) as well as data published by Woodhead and Hergt (2005; 176Hf/177Hf = 0.282172 ± 0.000042, 2σ). The reproducibility of 176Hf/177Hf for FC-1 analyses in epsilon notation without age correction was −21.8 +/−1.1 εHf (2σ), which is within the error of reported values and the Florida lab’s measurements of FC-1 by wet plasma [73,78]. The standard data were obtained during the same session as the unknown samples (1 standard, 15 unknowns, 1 standard). Measured and on-line mass-bias-corrected present-day 176Lu/177Hf ratios were utilized to calculate initial 176Hf/177Hf ratios using the decay constant of Lu (λ = 1.867e−11; [79,80]) and the 207Pb/206Pb age of the analytical spot, following established procedures [81,82]. Overall, because of the very low Lu/Hf ratios (FC-1: 176Lu/177Hf = 0.001329 ± 0.000091, 2σ, n = 9), the difference between the present-day measured and calculated initial 176Hf/177Hf ratios in most cases is < 1 ε unit (e.g., [73]).
Zircons were selected for Lu-Hf analysis on the basis of low discordance (<10% 206Pb/238U versus 207Pb/206Pb), zonation patterns, and grain size in order for the Lu-Hf analyses (40 μm spot) to be in the same domain as the U-Pb analysis (20 μm spot). Measuring Hf isotopes on the same zircons that are dated has the advantage of estimating the likelihood of open system behavior: Zircons that have experienced no, or only very little, Pb loss (i.e., concordant or nearly concordant) are the least likely to have suffered open system behavior of either Lu or Hf. The 176Hf/177Hf ratio is commonly represented as εHf, which is the 176Hf/177Hf in the unknown sample minus the 176Hf/177Hf in chondritic uniform reservoir, and then that value divided by 176Hf/177Hf in the chondritic uniform reservoir times 10,000 [83]. The chondritic uniform reservoir (CHUR) values are those of Bouvier et al. [84]: 176Lu/177Hf = 0.0336 and 176Hf/177Hf = 0.282785. Initial ratios are given as 176Hf/177Hf(T) and εHf(T) for all analyzed samples and were calculated using the 207Pb/206Pb crystallization age of the zircon or its host rock and the measured Lu/Hf ratio, (e.g., initial Hf at 2.4 Ga = εHf(2.4 Ga)); propagated net uncertainties for initial ratios are approximately 1.5 ε-units (2σ) on average. On the basis of limited U-Pb age discordance, the initial Hf compositions likely reflect the composition of the magmas from which the zircons crystallized. Decay corrections are typically <1ε unit/b.y. in the case of Precambrian zircons. Depleted mantle (DM) model ages for FC-1 averaged 1.5 +/− 0.1 Ga (2σ) using the linear depleted mantle model from Mueller et al. [73]: 176Hf/177Hf = 0.0387, εHf = 0.0 at 4.567 and 16 today) with propagated analytical errors only. The value of + 16 today for DM is within the range of values for modern Mid-Ocean Ridge Basalt (MORB) as summarized in Jones et al. [85] and Sanfilippo et al. [86]. The mean values for 176Hf/177Hf(T) and εHf(T) (and related errors (± 2σ)) are summarized in Table 1; details of the specific grain analyses are available in Supplementary Table S2. FC-1 standard Lu-Hf isotopic data are available in Supplementary Data Table S4. Note that some grains were too small for both U-Pb and Lu- Hf analyses; only age data are reported for these grains.
In addition to providing insight into the role of mantle and crustal reservoirs in the development of the magmas from which the zircons crystallized, the range of initial εHf values can also be used to identify zircons that may not have crystallized from that magma, i.e., xenocrysts. Although there is no fixed range of initial εHf that can be used to constrain a felsic magma generated in a terrane with very old crust, the viability of the age can be enhanced if those ages lead to initial εHf values that cover a limited range and that range of values is comparable to the εHf values measured in the zircons today. The limits are unavoidably ad hoc to some degree, but comparisons with the ranges of initial εHf values determined for rocks of similar age in the region provide useful benchmarks. For example, the approximately 2.8 Ga Long Lake magmatic complex of the Beartooth Mountains has a range of initial εHf of 15 epsilon units [39,87], and the Paleoproterozoic igneous rocks of the Little Belt Mountains range over 23 epsilon units [88]. Measurement errors (i.e., ± 2σ) are inconsequential compared to the ranges of initial ratios.

3. Results

3.1. U-Pb Zircon Geochronology

Figure 2 shows representative CL images in which some grains show concentric, oscillatory zonation, which is characteristic of igneous zircon (HPK, #4 and DRA-93-26, #23) and unzoned or featureless outer domains (DRA-93-01, #35 and #39), which are interpreted as metamorphic overgrowths, while other grains appear to be completely featureless in CL (PCP-MHB).
Grains analyzed by ICP-MS for this study were selected from the zircon concentrates provided by the Geological Survey of Canada and previously described as part of earlier multi-grain ID-TIMS studies [4,5]. Here, individual analyses were first evaluated as acceptable if they met two criteria: (1) The 207Pb/206Pb age was < 5% discordant compared to the 206Pb/238U age, and (2) common Pb (i.e., mass 204(Pb + Hg)) cps were less than the measured cps at mass 204 for the FC-1 standard. The values for 204Pb cps and 204Pb/206Pb for the analyses and standards are available in the Supplementary Data. CA-TIMS analyses [72] showed that typical FC-1 zircons have 204Pb/206Pb < 0.001. All analyses were plotted on a Tera-Wasserburg (TW) concordia diagram using the Isoplot program of Ludwig [74,75] to examine trends in discordance (Figure 3, Figure 4 and Figure 5). The probability distribution function in Isoplot was used to identify age populations. Plots of 207Pb/206Pb ages versus percent discordance provided further insight into the behavior of age populations (Supplementary Table S1). These plots assisted in selecting grains for weighted average 207Pb/206Pb age calculations by clarifying relationships between age populations and discordance. Grains were selected based on their near concordance and limited range of 207Pb/206Pb ages as demonstrated within the plot. The calculation of a useful concordia intercept age was hindered in some samples by multi-stage Pb-loss. In these cases, we conducted a second evaluation (described with each sample) and used error-weighted mean calculations (Isoplot v. 4.3, [74,75]) of low-discordance 207Pb/206Pb ages as the best minimum age estimate for the crystallization of the protolith. The external reproducibility of each individual zircon analysis (207Pb/206Pb age) is approximately 1% (2σ) on the basis of reproducibility of the standard (FC-1; See Supplementary Data). Error error-weighted mean calculations [74,75] U-Pb age estimates (where applicable) are reported in Table 2.

3.1.1. Home Pacific Knappen

Cathodoluminescence (CL) imaging revealed oscillatory zoned zircon grains typical of magmatic crystallization, with some grains exhibiting core-and-rim structures and fractures (Figure 2). Grains range in size from approximately 30 μm to 400 μm (long axis). Of the 90 analyses, discordance ranged to 90% (Supplementary Table S1). Seven low discordance grains (<5%) yielded an error-weighted mean age of 3.28 ± 0.01 Ga (MSWD = 2.3), which is interpreted as the age of protolith crystallization (Figure 3, Table 2).

3.1.2. Imperial Calstan Lake Newell

Zircon grains in this sample were mostly fragmented and dark in CL images, with limited observable zonation. Grains range in size from approximately 40 μm to 110 μm (long axis). The probability distribution function revealed two age populations in the total of 69 analyses: An older population of 31 grains at ca. 2.74 Ga, and a population of grains ≤ 2.7 Ga. The youngest two grains yielded ages of 1.76 ± 0.01 Ga and 1.91 ± 0.01 Ga, which may reflect zircon growth during later tectonothermal events [56]. The ca. 2.74 Ga analyses were further evaluated using the plots comparing percent discordance versus apparent 207Pb/206Pb ages grains, revealing a near concordant cluster of grains with discordance values between −2.1% and +2.2%, and 207Pb/206Pb ages from 2735 to 2755 Ma. This population of 20 grains yields an error-weighted mean age of 2.74 ± 0.03 (MSWD = 1.7; Figure 3, Table 2), which was interpreted as a crystallization age.

3.1.3. PCA Calstan Parkland

Most zircon grains in this sample are fragmented, but singly and doubly terminated grains are present as well. Grains range in size from approximately 60 to 200 μm (long axis). CL images reveal many grains with oscillatory growth zoning, in some cases also showing thin overgrowths or dark cores (Figure 2). Data were omitted based on the filtering criteria and occurrence along a Pb-loss trajectory observed on the concordia plot (Figure 3). The data were further evaluated in age versus percent discordance space, which revealed a population of grains with percent discordance values from −1.2 to + 0.9, and 207Pb/206Pb ages from 2634 to 2656 Ma. This population of 16 grains yield an error-weighted mean age of 2.64 ± 0.02 (MSWD = 0.88; Figure 3, Table 2). This age is interpreted as the minimum crystallization age, with the < 2.624 Ma ages possibly reflecting ancient Pb loss or total to partial metamorphic recrystallization.

3.1.4. PCP Medicine Hat

Zircon grains in this sample are often fragmented, but some elongate, rounded grains are present, ranging in size from approximately 50 to 170 μm (long axis). All grains were dark in CL images, with limited observable zonation (Figure 2). Out of the 70 individual zircon grains analyzed, only 11 pass the filtering criteria (Figure 4), and they range in age from approximately 2.70 to 2.78 Ga. This age distribution is interpreted to represent xenocrystic zircon in the protolith described as a granodiorite gneiss, with possible later overgrowths too small to be analyzed.

3.1.5. DRA-93-26

Zircon grains from this xenolith include stubby, rounded morphologies and some blockier grain fragments, ranging in size from approximately 70 to 160 μm (long axis). CL images reveal apparent oscillatory zoned cores and unzoned dark CL overgrowths in some grains (Figure 2). Other grains display simpler oscillatory growth zoning (Figure 2). Many analyses that pass the filtering criteria lie on a discordia with intercepts at approximately 1.79 Ga and 2.86 Ga; however, no grains with 207Pb/206Pb ages older than 2.84 Ga are observed (Figure 5). The TW plot of this sample reveals an older age cluster at ca. 2.83 Ga, with a young tail (discordance >5%) trending down to approximately 2.45 Ga (Figure 5; Supplementary Table S1). We further evaluated analyses for an error-weighted mean age, favoring grains yielding percent discordance values between −1.6 and +2.5, and apparent 207Pb/206Pb ages ca. 2.82–2.84 Ga. The 22 grains passing these criteria yielded a 207Pb/206Pb age of 2.84 ± 0.02 Ga (MSWD = 1.2; Figure 5, Table 2). Younger, concordant ages from both cores and rims likely reflect Pb loss due to Paleoproterozoic tectonothermal event(s). The error-weighted mean age of 2.84 Ga is interpreted to be the best estimate of the minimum crystallization age of the protolith.

3.1.6. DRA-93-01

Zircon grains from this xenolith are stubby to elongate, often with missing or rounded tips, ranging in size from approximately 50 to 180 μm (long axis). CL images reveal oscillatory growth zoning that, in some cases, is overgrown by more homogenous rims (Figure 2). Thirteen of 59 analyses were rejected based on the initial filtering criteria. The three oldest concordant analyses from zircon cores yielding ages of ca. 2.69 Ga are interpreted as xenocrystic. The Paleoproterozoic aged analyses were further evaluated using plots comparing percent discordance versus apparent 207Pb/206Pb ages. We favored analyses yielding percent discordance values between −0.6 and +2.5. Sixteen analyses from zircon cores passed these secondary criteria, and 15 grains yielded an error-weighted mean age of 1.81 ± 0.05 Ga (MSWD = 2.1; Figure 5, Table 2). Petrographic analysis indicates a high-grade mineral assemblage (i.e., garnet–clinopyroxene–pigeonite–rutile +/− hornblende +/− quartz assemblage; [5,7,89]), suggesting that the original magma was emplaced into the lower crust (i.e., a charnockite).

3.1.7. DRA-93-20

Zircon grains from this xenolith are generally small and round to oval in shape, ranging in size from approximately 40 to 140 μm (long axis). CL images reveal small, oscillatory zoned cores in some grains, with thicker and rounder overgrowths. Other grains tend to show patchy zonation or little visible zonation. Four analyses were omitted based on the basic filtering criteria (Figure 5). Analyses were further evaluated using plots comparing percent discordance versus age (Supplementary Table S1). We favored analyses yielding percent discordance values between −1.2 and +2.5, and apparent 207Pb/206Pb ages ca. 1.75–1.78 Ga. The youngest coherent population of eight analyses passing these criteria were used to determine an error-weighted mean age of 1.76 ± 0.06 Ga (MSWD = 2.1; Figure 5, Table 2). This age is interpreted as the crystallization age for this sample.

3.2. Lu-Hf Zircon Isotope Geochemistry

Error-weighted mean εHf(0) (modern) and εHf(T) (ancient) values are available in Table 2. Individual grain εHf(0) and εHf(T) values are available in the Supplementary Data (Table S2). All εHf(T) data are plotted on Figure 6 versus the estimated crystallization age (207Pb/206Pb) of their host rock.

3.2.1. Home Pacific Knappen (HPK)

HPK yielded an error-weighted mean εHf(0) value of −78.2 ± 0.95 and a range of 4.9 ε-units, from −76.6 to −81.5 (n = 11). εHf(3.3 Ga) values for the grains range from −3.1 to −8.7 (5.6 ε-units), with an error-weighted mean value of −4.6 ± 1.1 (Figure 6, Table 2).

3.2.2. Imperial Calstan Lake Newell (ICLN)

The error-weighted mean εHf(0) value for the data is −58.3±0.62, and the data range is a total of 6.9 ε-units, from −53.1 to −60.0 (n = 16). εHf(2.7 Ga) defines a range from 8.1 to 1.6 (6.5 ε-units), with an error-weighted mean of 3.1 ± 0.61 (Figure 6, Table 2).

3.2.3. PCA Calstan Parkland (PCACP)

PCACP yielded an error-weighted mean εHf(0) value of −56.8 ± 0.83 and a range of 7.5 ε-units, from −51.0 to −58.5 (n = 13). εHf(2.6 Ga) for the grains range from 8.5 to 1.1 (7.4 ε-units), with an error-weighted mean value of 2.5 ± 0.76 (Figure 6, Table 2).

3.2.4. PCP Medicine Hat (PCPMH)

The sample yielded εHf(0) values ranging from −54.6 to −60.9 (n = 15; 6.3 ε-unit range) (Table 2). Due to the lack of a coherent crystallization age for this sample, εHf(T) values are calculated to the individual zircon age. These values range from −2.9 to 5.3 (8.2 ε-unit range).

3.2.5. DRA-93-26

The zircons yielded an error-weighted mean εHf(0) value of −61.4 ± 0.67, ranging from −55.9 to −63.2 (n = 22; 7.3 ε-units) and εHf(2.8 Ga) define a range from 7.9 to 0.1 (7.8 ε-units), with an error-weighted mean of 1.6 ± 0.64 (Figure 6, Table 2).

3.2.6. DRA-93-01

The sample showed an error-weighted mean εHf(0) value of −59.5 ± 1.0 ranging from −50.8 to −63.9 (n = 16; 13.1 ε-unit range). When εHf(1.8 Ga) was calculated, the εHf(1.8 Ga) values range from −15.7 to −23.2 (7.5 ε-units), with an error-weighted mean value of −17.0 ± 2.3 (Figure 6, Table 2).

3.2.7. DRA-93-20

εHf(0) values yielded an error-weighted mean of −53.6 ± 1.6 ranging from −49.8 to −58.6 (n = 13; 8.8 ε-units), and εHf(1.8 Ga) define a range from −10.1 to −20.1 (10 ε-units), with an error-weighted mean of −14.4 ± 1.8 (Figure 6, Table 2).

4. Discussion

The new, single grain U–Pb zircon ages presented here largely support previous multi-grain analyses, mostly concordia upper intercept ages, reported by Villeneuve et al. [4] and Davis et al. [5] for the same zircon concentrates. The Home Pacific Knappen core yields zircons with reliable ages of approximately 3.28 Ga, while the remainder of the samples yielded slightly older ages than previously cited (Table 1 and Table 2), with the exception of DRA-93-20, which yielded a slightly younger age than previously published (Table 1 and Table 2; [4,5]). Collectively, the Archean crystallization ages presented here and by Davis et al. [5] and in other samples analyzed by Villeneuve et al. [4] confirm the widespread presence of Mesoarchean crust in the MHB and southern Hearne Province.
Whole-rock Sm-Nd isotopes of two samples discussed in Villeneuve et al. [4] yielded initial εNd values of + 0.6 and −0.1 (PCP Travers and HPK respectively), crustal residence, or mantle extraction ages of 2.86 and 3.48 Ga, respectively, and 147Sm/144Nd ratios not typical of continental crust (147Sm/144Nd = 0.1532; [90]). The Sm–Nd isotopic data of Villeneuve et al. [4] are similar to the data of Frost and Burwash [91] for the MHB and southern Hearne Province with crustal residence ages ranging from approximately 2.6 Ga to 3.2 Ga [91] and a range (−4.04 to −12.8; [91]) of εNd1.8 Ga values.
In terms of Hf isotopes, Archean samples show a mixture of initial Hf isotopic values ranging from positive depleted mantle values to CHUR/BSE values (Figure 6; εHf(T) = 8.5 to 0.1). These values indicate that mantle-derived melts invariably interacted with older, more heterogeneous crust to yield the range of observed Hf(T) values. The age estimates for this older crust (approximately 2.8 Ga to 3.6 Ga) are based on the lower crustal Lu–Hf ratio (176Lu/177Hf = 0.0187) shown in Figure 6; current ratios, as well as depleted mantle model ages, are shown in Table 2. There is evidence in the Lu/Hf ratios of the Mesoarchean zircons, albeit limited, of Archean crust with components >3.2 Ga within the MHB (Figure 6; this study; [4,5,56,57]), which indicates that there might be parts of the MHB not yet discovered that record an older history. These possible exceptions aside, the data summarized here strongly suggest that the MHB is similar to other Archean provinces around the world in containing a large amount of crust created between approximately 2.8 and 2.5 Ga [4,5,66]. This conclusion is compatible with interpretations of extant whole rock Sm-Nd isotopic data that yield Archean crustal residence ages for all of the xenoliths and basement cores discussed here and elsewhere [4,5,91]. Similarly, εHf values of zircons for the drill cores and xenoliths range from DM to more negative epsilon values, indicating the mixing and reworking of older crustal materials. The Lu-Hf TDM of approximately 3.6 Ga for zircons from the HPK core (Table 2) indicates that older material equivalent to the MMT [32,92,93,94] was likely present in the MHB during development of the Neoarchean and Paleoproterozoic crust. This buried Meso- to Paleoarchean crust is a good candidate for the older contaminating component that contributed to lowering the εHf values of the Neoarchean samples (e.g., Figure 6 lower crustal evolution path). Similarly, the Sm-Nd isotopic values for the Mesoarchean MMT crust also involve the mixing of juvenile and older crustal material, although showing a larger range in ε-units (approximately 8.5 Nd ε-units; + 4.9 εNd to −4.3 εNdT values [49,95]).
Although the extent of the Wyoming province, Medicine Hat block, and Hearne provinces and their temporal relationships to the Superior Province across the Trans-Hudson orogen are still debated, the similarity of ages and isotopic compositions between the MHB and the northern Wyoming Province, particularly the MMT, suggests that these two terranes may have shared at least a partial history (Figure 7A). If so, the MMT–MHB connection likely existed as far back as the Mesoarchean, strengthening proposals for a connection between the MHB and Wyoming Province [6]. The connection was likely broken sometime during the earliest Paleoproterozoic with the formation of a small ocean basin (Medicine Hat ocean) that separated the MMT and other parts of the northern Wyoming Province from the MHB and possibly related terranes such as the Clearwater and Priest River (e.g., [96,97,98,99]). Closure of this ocean by north dipping subduction [28] led to the formation of the Little Belt continental arc on MHB crust beginning at approximately 1.9 Ga [58]. The MHB and MMT re-joined at this time as they amalgamated into the supercontinent Laurentia during the Great Falls orogeny (1.7–1.9 Ga), which formed the GFTZ [1,28,56,57,58,59]. The GFTZ developed in the same timeframe as the better known Trans-Hudson orogen [60,61,62,63,64,65,66,67] to the east that marks the merger of the Wyoming, Hearne, and Superior Provinces, which along with the MHB formed the Archean core of western Laurentia. The impetus for closure of the Medicine Hat ocean, formation of the GFTZ, and amalgamation of the Superior, Hearne, and Wyoming Provinces remains unclear, but the presence of the approximately 1.8 Ga Rimbey arc immediately northwest of the MHB/Vulcan zone and its proposed relation to the collision of Australia and Laurentia (e.g., [100,101]) coincides with ages presented here and high-grade 1.75–1.85 metamorphism of the western Hearne Province [102]. This collisional scenario is complex and associated with the formation of Nuna-Columbia. Although there are several extant proposals for the sequence of events that led to the formation of a combined Nuna-Columbia-Laurentia scale supercontinent in the Paleoproterozoic, many authors have proposed that a firm connection was established between Laurentia and Australia in the interval 1.8–1.6 Ga (e.g., [103,104,105]). Establishing this connection involved at least one continent–continent or craton–craton collision, which would be of the appropriate scale to induce a wide area of modern northwestern North America characterized by 1.7–1.8 Ga magmatic crystallization ages and metamorphic cooling ages.

5. Conclusions

The data presented here help expand our understanding of the age and tectonic evolution of the largely concealed Medicine Hat block. The new U-Pb ages presented generally agree with previous Archean and Paleoproterozoic age determinations for the region [4,5]; however, they help resolve complexities caused by discordance only hinted at by previous analyses of these samples. The ages generated in this study tend to be slightly older than the earlier multi-grain analyses, which may have been more affected by Pb loss or the incorporation of later metamorphic zircon growth in multi-grain dissolutions. Lu-Hf isotopic analyses paired with single-grain U-Pb data help further constrain the crustal evolution of the MHB, reinforcing that it contains a large amount of crust created between approximately 2.8 and 2.5 Ga. The initial εHf values for the majority of the samples from this study range from DM, indicating juvenile materials, mixed with reworked older Meso- to Paleoarchean crustal materials. The samples reveal similarities to the ages and isotopic compositions of the MMT, suggesting a connection between the MHB and the MMT in their history. This connection was likely broken sometime in the earliest Paleoproterozoic, leading to the formation of a small ocean basin that later closed, resulting in the Little Belt continental arc at approximately 1.9 Ga. The prevalence of Paleoproterozoic ages across the MHB, GFTZ, and MMT (approximately 1.9 Ga to 1.7 Ga) record the entire Great Falls Orogeny, and time that the combined MHB-WY-Hearne crust was amalgamated with the Superior Province to form the Archean core of Laurentia.

Supplementary Materials

The following are available online at https://0-www-mdpi-com.brum.beds.ac.uk/2076-3263/10/7/271/s1, Table S1: U-Pb zircon geochronologic analyses. Table S2: Lu-Hf zircon isotope geochemical analyses. Table S3: FC-1 standard U-Pb zircon analyses. Table S4: FC-1 standard Lu-Hf isotope geochemical analyses.

Author Contributions

Conceptualization, J.N.G.; Formal analysis, J.N.G. and S.J.M.; Funding acquisition, J.N.G.; Investigation, J.N.G.; Methodology, J.N.G.; Project administration, J.N.G.; Resources, J.N.G.; Validation, J.N.G., S.J.M. and P.A.M.; Visualization, J.N.G. and S.J.M.; Writing—original draft, J.N.G. and S.J.M.; Writing—review and editing, J.N.G., S.J.M. and P.A.M. All authors have read and agreed to the published version of the manuscript.

Funding

This research was funded by The University of Mississippi Department of Geology and Geological Engineering.

Acknowledgments

We wish to thank William (Bill) Davis from the Geological Survey of Canada for allowing us to work on the samples. George Kamenov is gratefully acknowledged for all of his help with attaining the U–Pb and Lu–Hf analyses for this project.

Conflicts of Interest

The authors declare no conflict of interest. The funders had no role in the design of the study; in the collection, analyses, or interpretation of data; in the writing of the manuscript, or in the decision to publish the results.

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Figure 1. Generalized map of Precambrian basement provinces of southwestern Laurentia with the Montana alkali province (MAP) shown without a solid boundary, as the extent of the MAP is not well known (after [2,15,16,17,18,19]). MMT: Montana Metasedimentary Terrane; BBMZ: Bighorn-Beartooth Magmatic Zone. TRM: Tobacco Root Mountains; HM: Highland Mountains; RR: Ruby Range; MR: Madison Range; LRM: Little Rocky Mountains; LBM: Little Belt Mountains. Drill core locations: (1) Home Pacific Knappen; (2) Imperial Calstan Lake Newell; (3) PCA Calstan Parkland; (4) PCP Medicine Hat. Xenolith localities: (5) Coulee 29; (6) Sill 39.
Figure 1. Generalized map of Precambrian basement provinces of southwestern Laurentia with the Montana alkali province (MAP) shown without a solid boundary, as the extent of the MAP is not well known (after [2,15,16,17,18,19]). MMT: Montana Metasedimentary Terrane; BBMZ: Bighorn-Beartooth Magmatic Zone. TRM: Tobacco Root Mountains; HM: Highland Mountains; RR: Ruby Range; MR: Madison Range; LRM: Little Rocky Mountains; LBM: Little Belt Mountains. Drill core locations: (1) Home Pacific Knappen; (2) Imperial Calstan Lake Newell; (3) PCA Calstan Parkland; (4) PCP Medicine Hat. Xenolith localities: (5) Coulee 29; (6) Sill 39.
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Figure 2. Representative CL images of analyzed zircon. Red smaller circles represent 20 μm U-Pb analysis spots. Green larger circles represent 40 μm Lu–Hf analysis spots.
Figure 2. Representative CL images of analyzed zircon. Red smaller circles represent 20 μm U-Pb analysis spots. Green larger circles represent 40 μm Lu–Hf analysis spots.
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Figure 3. Unfiltered concordia plots of 207Pb/206Pb versus 238U/206Pb and corresponding ages showing the spread of zircons for samples analyzed in this study, and error-weighed mean 207Pb/206Pb ages Home Pacific Knapppen, PCA Castalan Parkland, and Imperial Castalan Lake Newel samples. The analyses used for the error-weighted mean calculations are highlighted in blue. Plots, ages, and age statistics are from Isoplot 3.7. See text for full discussion.
Figure 3. Unfiltered concordia plots of 207Pb/206Pb versus 238U/206Pb and corresponding ages showing the spread of zircons for samples analyzed in this study, and error-weighed mean 207Pb/206Pb ages Home Pacific Knapppen, PCA Castalan Parkland, and Imperial Castalan Lake Newel samples. The analyses used for the error-weighted mean calculations are highlighted in blue. Plots, ages, and age statistics are from Isoplot 3.7. See text for full discussion.
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Figure 4. Unfiltered concordia plot and a probability distribution plot of filtered 207Pb/206Pb ages for sample PCP-Medicine Hat, showing the wide range of concordant analyses. See text for discussion.
Figure 4. Unfiltered concordia plot and a probability distribution plot of filtered 207Pb/206Pb ages for sample PCP-Medicine Hat, showing the wide range of concordant analyses. See text for discussion.
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Figure 5. Unfiltered concordia plots of 207Pb/206Pb versus 238U/206Pb and corresponding ages showing the spread of zircon ages for samples analyzed in this study, and error-weighed mean 207Pb/206Pb ages for DRA-93-26, DRA-93-20, and DRA-93-01 samples. The analyses used for the error-weighted mean calculations are highlighted in blue. Plots, ages, and age statistics are from Isoplot 3.7. See text for full discussion.
Figure 5. Unfiltered concordia plots of 207Pb/206Pb versus 238U/206Pb and corresponding ages showing the spread of zircon ages for samples analyzed in this study, and error-weighed mean 207Pb/206Pb ages for DRA-93-26, DRA-93-20, and DRA-93-01 samples. The analyses used for the error-weighted mean calculations are highlighted in blue. Plots, ages, and age statistics are from Isoplot 3.7. See text for full discussion.
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Figure 6. Lu-Hf evolution diagram showing the range for the drill core and xenolith samples. Lu-Hf data from xenoliths from the Medicine Hat block (MHB) are shown for comparison (thick gray bars; [56]). Lu-Hf data from the Little Rocky Mountains are shown for comparison (open bars; [57]). Evolution path based on lower crustal Lu/Hf ratios from Rudnick and Gao [90] (dotted lines). Symbols represent error-weighted means. CHUR: Chondritic Uniform Reservoir; BSE: Bulk Silicate Earth.
Figure 6. Lu-Hf evolution diagram showing the range for the drill core and xenolith samples. Lu-Hf data from xenoliths from the Medicine Hat block (MHB) are shown for comparison (thick gray bars; [56]). Lu-Hf data from the Little Rocky Mountains are shown for comparison (open bars; [57]). Evolution path based on lower crustal Lu/Hf ratios from Rudnick and Gao [90] (dotted lines). Symbols represent error-weighted means. CHUR: Chondritic Uniform Reservoir; BSE: Bulk Silicate Earth.
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Figure 7. (A) Published Archean to Paleoproterozoic U-Pb ages of zircons from the Montana Metasedimentary terrane (MMT: Ruby Range, Tobacco Root Mountains, Madison Range, Highland Mountains: [32,49,94,95,106,107,108]). Published ages for the Medicine Hat block and Great Falls tectonic zone (MHB/GFTZ: drill cores, Sweetgrass Hills xenoliths, Priest River Complex, Clearwater Complex, Little Belt Mountains, Little Rocky Mountains, Grassrange Diatreme xenoliths, this study; [4,5,56,57,58,59,95,98,99], all of which is being reported here. For reference, ages are plotted compared to U-Pb ages from this study. Ages interpreted as times of igneous crystallization are represented as squares, and potential metamorphic ages are represented as circles. Ages from this study are solid symbols, and ages from the literature are open symbols. (B) The approximate locations and relative positions of the Wyoming Province, MHB, Hearne Province, GFTZ (tightly dashed lines), Trans-Hudson, and Vulcan low (represented by the widely spaced waved lines) [14,24,25,91,109] with corresponding ages cited above.
Figure 7. (A) Published Archean to Paleoproterozoic U-Pb ages of zircons from the Montana Metasedimentary terrane (MMT: Ruby Range, Tobacco Root Mountains, Madison Range, Highland Mountains: [32,49,94,95,106,107,108]). Published ages for the Medicine Hat block and Great Falls tectonic zone (MHB/GFTZ: drill cores, Sweetgrass Hills xenoliths, Priest River Complex, Clearwater Complex, Little Belt Mountains, Little Rocky Mountains, Grassrange Diatreme xenoliths, this study; [4,5,56,57,58,59,95,98,99], all of which is being reported here. For reference, ages are plotted compared to U-Pb ages from this study. Ages interpreted as times of igneous crystallization are represented as squares, and potential metamorphic ages are represented as circles. Ages from this study are solid symbols, and ages from the literature are open symbols. (B) The approximate locations and relative positions of the Wyoming Province, MHB, Hearne Province, GFTZ (tightly dashed lines), Trans-Hudson, and Vulcan low (represented by the widely spaced waved lines) [14,24,25,91,109] with corresponding ages cited above.
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Table
Table 1. Published zircon U-Pb ages, analysis type, and sample descriptions of drill cores from Villeneuve et al. [4]. Published zircon U-Pb ages, analysis type, and sample descriptions of xenoliths are from Davis et al. [5].
Table 1. Published zircon U-Pb ages, analysis type, and sample descriptions of drill cores from Villeneuve et al. [4]. Published zircon U-Pb ages, analysis type, and sample descriptions of xenoliths are from Davis et al. [5].
207Pb/206PbAnalysis TypeDescriptions
Age (Ga)
Drill Core Samples [4]
Home Pacific Knappen3.278single zircon core analysisBanded greenish colored gneiss composed of quartz and feldspar with 20% biotite
Imperial Calstan Lake Newell2.714single zircon core analysisModerately fresh pegmatitic granodioritic gneiss composed of quartz, alkali feldspar, plagioclase, and hornblende with subordinate epidote and biotite
PCA Calstan Parkland2.627single zircon core analysisHomogenous fresh medium- to fine-grained metabasite gneiss composed of biotite and plagioclase with subordinate hornblende
PCP Medicine Hat2.7–2.8single zircon core analysisMassive, weakly foliated granitic gneiss that ranges in texture from medium-grained equigranular to pegmatitic and is cross-cut by chlorite-covered fractures
Xenolith Samples [5]
DRA-93-262.65not specifiedHornblende-biotite tonalite
DRA-93-011.72multi-grain zircon U-PbMafic granulite with a high-pressure assemblage (garnet–clinopyroxene–pigeonite–rutile +/− hornblende +/− quartz)
DRA-93-201.81single zircon core analysesQuartzo-feldspathic mesoperthite-rich granulite
Table
Table 2. LA-ICP-MS data. 207Pb/206Pb ages and Lu–Hf-isotope data summarized.
Table 2. LA-ICP-MS data. 207Pb/206Pb ages and Lu–Hf-isotope data summarized.
207Pb/206PbErrorz/d/c a176Hf/177HfεHf(0)εHf(0)εHf(T) cεHf(T) cHf Model Age
Age (Ga)2σ (T) bRangeMeanRangeMean(Ga) (DM) d
Drill Core Samples
Home Pacific Knappen3.280.0190/7/110.28054−76.6 to −81.5−78.2 ± 0.95−3.1 to −8.7−4.6 ± 1.13.62
Imperial Calstan Lake Newell2.740.0368/20/160.28112−53.1 to −60.0−58.3 ± 0.628.1 to 1.63.1 ± 0.612.86
PCA Calstan Parkland2.640.0260/16/130.28117−51.0 to −58.5−56.8 ± 0.838.5 to 1.12.5 ± 0.762.79
PCP Medicine HatN/AN/A70/NA/150.28103−54.6 to −60.9N/A5.3 to −2.9 eN/A2.84 to 3.22
Xenolith Samples
DRA-93-262.840.0270/22/220.28101−55.9 to −63.2−61.4 ± 0.677.9 to 0.11.6 ± 0.643.01
DRA-93-011.810.0559/16/160.28114−56.5 to −63.9−59.5 ± 1.0−15.7 to −23.3−17.0 ± 2.32.89
DRA-93-201.760.0631/8/130.28125−49.8 to −58.6−53.6 ± 1.6−10.1 to −20.1−14.4 ± 1.82.69
a z/d; z, number of zircons analyzed for U–Pb per sample; d, number of zircon analyses used for age calculation; n, number of zircons analyzed for Lu–Hf per sample. b Error-weighted mean 176Hf/177Hfint calculated by applying the ages given in 207Pb/206Pb Age (Ga) column. c εHfT calculated by applying the ages given in 207Pb/206Pb Age (Ga) column, ± the standard deviation of the mean. d Depleted Mantle model ages were calculated using the model of Mueller et al. [73]. e εHf values were calculated using the individual U-Pb age for each grain.

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Gifford, J.N.; Malone, S.J.; Mueller, P.A. The Medicine Hat Block and the Early Paleoproterozoic Assembly of Western Laurentia. Geosciences 2020, 10, 271. https://0-doi-org.brum.beds.ac.uk/10.3390/geosciences10070271

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Gifford JN, Malone SJ, Mueller PA. The Medicine Hat Block and the Early Paleoproterozoic Assembly of Western Laurentia. Geosciences. 2020; 10(7):271. https://0-doi-org.brum.beds.ac.uk/10.3390/geosciences10070271

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Gifford, Jennifer N., Shawn J. Malone, and Paul A. Mueller. 2020. "The Medicine Hat Block and the Early Paleoproterozoic Assembly of Western Laurentia" Geosciences 10, no. 7: 271. https://0-doi-org.brum.beds.ac.uk/10.3390/geosciences10070271

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