GSA Data Repository 2016208
Meteoric fluid infiltration in crustal-scale normal fault systems as indicated by
18O and 2H geochemistry and 40Ar/39Ar dating of neoformed clays in brittle fault
rocks
S. Haines et al.
2016208.zip
Supplementary DR 1
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016,
Meteoric fluid infiltration in crustal-scale normal fault systems as indicated by 18O
and 2H geochemistry and 40Ar/39Ar dating of neoformed clays in brittle fault rocks:
Lithosphere, v. 8, doi:10.1130/L483.1.
Detachments sampled
1 Ruby Mountains
The Ruby Mountains are a metamorphic core complex in northeastern Nevada
(Howard, 1980, Snoke, 1980). The complex was exhumed by a large WNW-dipping, 1-2
km thick shear zone that strikes along the NW side of the range. The detachment was
active from the late Cretaceous to the Miocene (McGrew & Snee, 1994 Colgan &
Metcalf, 2006). The fault system evolved from a well-defined mid-crustal mylonite zone
found in the footwall of the brittle detachment. The detachment fault system is well
exposed in 3 closely spaced road cuts along Nevada Rt. 229, west of Secret Pass. The
main detachment (samples SEC 4-2 and SEC 4-3), an overlying brittle detachment in the
hanging wall (not analyzed for this study), and a high-angle normal fault (SEC 1-2 illite) that soles into the main detachment all have well-developed clay-rich illitic and
smectitic gouges (Haines and van der Pluijm, 2010; Figure 1E). XRD analysis indicates
that both the SEC 1-2 and SEC 4-2 gouges are predominantly the low-temperature 1Md
polytype of illite, formed by the alteration of cataclasticaly-derived micas from hanging
wall shales (Figure 3A and 3B, Haines and van der Pluijm, 2010). Where hanging wall
lithologies are tuffs, gouges are smectite-dominated (SEC 4-3, Haines and van der
Pluijm, 2010, 2012, Figure 1E).
40
Ar/39Ar dating of the illitic gouge shows the clays
formed at 11-13 Ma, marking the final period of activity on the detachment fault system
(Haines and van der Pluijm, 2010). The stable isotopic analysis for both O and H was
performed on splits of the fine fraction of SEC 1-2 and SEC 4-2 as reported in Haines
and van der Pluijm, (2010, 2012).
2 Death Valley area detachments – Badwater, Mormon Point, and Amargosa
Detachments
The Black Mountains on the east side of Death Valley have several spectacularly
exposed LANFs. The faults record considerable extension in the Death Valley area from
the Miocene to Recent, although the exact timing and magnitude of extension remains the
subject of controversy (see Miller & Pavlis, 2005, for discussion). Three low-angle
normal faults, known colloquially as ‘turtlebacks’ (from north to south, the Badwater,
Copper Canyon, and Mormon Point turtlebacks) are exposed along the east side of Death
Valley (Curry, 1938, Miller & Pavlis, 2005; Hayman et al., 2006). Each turtleback
(detachment) has a distinctive turtleshell-like form with an anticlinal carapace of
mylonitic mid-crustal rocks separated from a hanging wall of unmetamorphosed Miocene
to Recent sediments by a ductile to brittle LANF.. Gouges from one exposure of the
Badwater Detachment and two exposures of the Mormon Point Detachment were
analyzed. Two older, possibly kinematically-linked brittle detachments, the Gregory Peak
detachment and the Amargosa Detachment, are exposed further to the south (Figure 1).
One gouge sample from the Amargosa Detachment was analyzed for this study.
2.1 – Badwater Detachment
The Badwater Detachment was sampled at 2 localities, in an unnamed wash near
the southern edge of the detachment, (Badwater-1, Table 1, geospatial data 1) and at the
Natural Bridge trail (Badwater-2). At both localities the fault juxtaposes epidote +
chlorite-altered mylonitic granite and schist in the footwall against Pleistocene gravels
and fanglomerates. Both the illite-dominated clay gouge and chloritally-altered footwall
were sampled, samples BAD-1 (F) and BAD-1 (G) respectively. See Figures 2A, 3A and
3C. Although not brecciated, the chloritic footwall at Badwater-1 (BAD-1 (G)) was
fractured sufficiently that it disaggregated readily in water, permitting chlorite to be
easily separated out by suspension in water and subsequent centrifugation.
2.2 – Mormon Point Detchment
Two exposures of the Mormon Point Detachment were sampled for material for
stable isotopic analysis (Mormon-2, Mormon-3, both on the western edge of the northern
flank of the detachment) and one for geochronology (Mormon-1, on the western flank of
the detachment). At both Mormon-2 and Mormon-3, accessed by walking up Mormon
Point Canyon, the hanging wall consists of Plio-Pleistocene gravels, while the footwall
lithology varies. At Mormon-2, accessed by walking up a wash to the east (samples
MOR-2 (M) and MOR-2 (F),) the footwall consists of chlorite-altered diorite. The gouge
consists entirely of fragmental footwall chlorite/epidote-altered diorite without
discernable alteration (Haines and van der Pluijm, 2012). Two size fractions of the
fragmental gouge sample were analyzed (0.2 – 0.05 m (“M”) and <0.05 m (“F”)
Figure 3).
At Mormon-3, accessed by walking up an unnamed wash from the Badwater
Road on the west side of Mormon Point (sample MOR-3 (M), Figure 1D)) the footwall
consists of chlorite-altered dioritic gneiss and interlayered dolomite. At Mormon-3, the
gouge consists of two distinct layers, a fragmental chlorite-dominated footwall gouge,
consisting of chlorite structurally and compositionally indistinguishable from that found
in the footwall (Haines and van der Pluijm, 2012), which was sampled (Figure 3), and a
low-temperature, Mg-rich silicate assemblage consisting of smectite, sepiolite, talc, and
lizardite (Haines and van der Pluijm, 2012), which was not analyzed for this study.
Insufficient <0.05 m fraction material was recovered from centrifugation to analyze,
consistent with a cataclastic origin (Haines and van der Pluijm, 2012).
Illite-dominated gouge was sampled at a third locality to the south of Mormon
Point on the western flank of the detachment (Mormon-1). The finest size fraction of the
material contained too much carbonate for stable isotopic analysis, but was suitable for
Ar-Ar dating, with an age of 2.8 +/- 0.5 Ma. The chloritic material at Mormon-2 and -3
ilikely formed at greater depths than the illitic material, and is likely older.
2.3 – Amargosa Detachment
The Amargosa detachment lacks mylonites in the footwalls and apparently was
active entirely in the brittle regime (Hamilton, 1988, Castonguay, 2013). The detachment
was sampled at a klippe north of Ashford Canyon, accessed by walking northwest along
the range front from the Ashford Canyon Trail head road, where the fault juxtaposes
weakly lithified conglomerates in the hanging wall against chloritcally-altered and
brecciated granite in the footwall (Figure 1C). The clay fraction of the gouge consists of
the low-temperature 1Md polytype of illite, formed from the breakdown of fragmental
2M1 polytype (the high-temperature polytype) illite/mica, likely derived from the
footwall (Figure 3, Haines and van der Pluijm, 2012).
We dated clays in gouges from the Badwater, Mormon Point and Amargosa
detachment using Illite Age Analysis (IAA), which are 2.8-3.3 Ma in age.
3 Panamint Mountains
The Panamint Mountains are partially bounded on their west flank by a series of
west-dipping low-angle normal faults that formed during the latter stages of the
exhumation (Hodges et al., 1989). A separate low-angle fault outcrops further south
along the east side of Panamint Valley, the Panamint Valley low-angle fault (Cichanski,
2000).
3.1 – Panamint Range Front Detachment
The Panamint Valley low-angle normal fault was sampled in South Park Canyon,
where the fault dips 20° west and juxtaposes Pliocene and older Pleistocene
conglomerates against a footwall of Proterozoic schists. The Panamint Valley low-angle
normal fault lacks a mylonitic footwall and was apparently active entirely in the brittle
regime. The gouge consists of the 1Md polytype of illite, derived from the dissolution of
K-feldspar (Haines and van der Pluijm, 2012, Figure 3). The Panamint Valley gouge was
dated with IAA, resulting in an age of 3.6 Ma (see below).
3.2 – Mosaic Canyon Detachment
The Mosaic Canyon fault (also known as the Harrisburg Fault, Hodges et al.,
1990) bisects the northern portion of the Panamint Mountains. The fault dips moderately
to the east and has been argued to be an overturned west-dipping normal fault that may be
contiguous with the Emigrant fault on the west side of the range. The Mosaic Canyon
fault was sampled at Mosaic Canyon, where the fault juxtaposes Neoproterozoic
metasediments (Johnnie Quartzite in the hanging wall and Noonday Dolomite in the
footwall). The Mosaic Canyon Detachment was sampled in Mosaic Canyon on the trail
into Mosaic Canyon. Gouge was suitable for dating, but owing to the presence of
carbonate in the fine fraction, and uncertainty about the effect of acid treatments on H
isotopes in clays, the sample was not used for isotopic analysis.
4 Chemehuevi Detachment
The Chemehuevi detachment is a Miocene-age NE-dipping detachment fault in
southeastern California, part of the suite of metamorphic core complexes with LANFs
known as the Colorado River Extensional Corridor (Spencer and Reynolds, 1991). The
detachment fault was sampled on the northwest side of Lobeck Pass where the fault
juxtaposes a post 18.5 Ma monomict megabreccia (Miller & John, 1999) against a
chloritized but unmylonized 19.1 Ma granite (Foster et al, 1996). The gouge zone
consists of 3 mineralogically distinct layers on the basis of XRD characterization (Haines
and van der Pluijm, 2012). The upper and middle layers are dominated by authigenic trioctahedral phyllosilicates saponite in the middle layer, and palygorskite in the upper
layer, both formed from low-temperature alteration of chlorite-dominated fragmental
gouge. Only the lower fragmental chlorite-dominated gouge (LOBECK-3 (M), Figure
1B) was analyzed for this study.
5 Buckskin-Rawhide Mountains Detachment
The Buckskin-Rawhide detachment is a Miocene NE-dipping LANF located in
central-western Arizona, and is also part of the Colorado River Extensional Corridor
(Spencer and Reynolds, 1991, Singleton et al., 2014). The detachment was sampled at
“A-Bomb Canyon”, (Spencer & Reynolds, 1986) where the fault juxtaposes a granite in
the upper plate over a chlorite tectonic breccia in the footwall. The gouge consists of two
layers: cataclastically-reworked footwall epidote-chlorite microbreccia, and an upper
layer dominated by tri-octahedral smectite, formed by low-temperature alteration of the
lower fragmental gouge (Haines and van der Pluijm, 2012). Only the 0.2 – 0.05 m size
fraction of the fragmental gouge (A-BOMB-3 (M)) was analyzed for this study.
6 Central Mojave Detachment (Waterman Hills detachment)
The Central Mojave metamorphic core complex is exposed in the Waterman
Hills, Mitchell Range and Newberry Mountains of southeastern California, The
detachment is exposed in a cliff face 150 m WNW of the KDUC radio transmitter 10 km
N of Barstow (Figure 1F). The detachment accommodated 40-50 km of NE-directed
extension during the early Miocene (Walker et al., 1990). The detachment fault trace
trends roughly northwest-southeast and dips gently to the east. The detachment fault was
sampled in the northern Waterman Hills where it juxtaposes Tertiary rhyolites in the
hanging wall and mylonitic granodiorite in the footwall. The temporal and kinematic
relationship of the brittle fault to the mylonitic detachment is complex in that kinematic
indicators associated with the brittle fault records north-south extension as opposed to the
northeast-southwest extension recorded by the mylonites (Anderson, 2007). Gouge
material was visibly segregated at outcrop; grayish material is illitic, formed from the
dissolution of K-feldspar, while yellowish material is smectitic, formed from dissolution
and reprecipitation of hanging wall acid volcanic lithologies.
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Supplementary DR 2
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016,
Meteoric fluid infiltration in crustal-scale normal fault systems as indicated by δ18O
and δ2H geochemistry and 40Ar/39Ar dating of neoformed clays in brittle fault rocks:
Lithosphere, v. 8, doi:10.1130/L483.1.
L483_DR2.kml Supplementary DR 3
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016,
Meteoric fluid infiltration in crustal-scale normal fault systems as indicated
by 18O and 2H geochemistry and 40Ar/39Ar dating of neoformed clays in
brittle fault rocks: Lithosphere, v. 8, doi:10.1130/L483.1.
Methods
Oxygen isotope measurements
Mineral separates and whole rock powders were analyzed in the University of Wisconsin
Stable Isotope Laboratory by laser fluorination. Isotope ratios were measured on a dualinlet gas-source Finnigan/MAT 251 mass spectrometer. Refractory minerals such as
quartz were loaded in a sample holder and pre-exposed to BrF5 reagent at room
temperature overnight to remove water and traces of other contaminants that react readily
at room temperature. For these minerals there is no mineral reaction at room T, and
accuracy and precision of this technique are better than ±0.1‰. Because our samples
contain fine-grained clay minerals that will react with BrF5 at room temperature, samples
were introduced to the reaction chamber from an adjoining ”air lock'' vacuum chamber,
which was not exposed to BrF5 at any time (Spicuzza et al. 1998). This step serves to
avoid pre-reaction and contamination of the sample from the otherwise excessive blank
produced by room temperature reaction with BrF5 during pre-treatment. Before analysis,
a blank was measured with reagent but no heating. Comparisons of whole rock analyses
with conventional analyses in externally heated Ni reaction vessels show excellent
agreement. Oxygen was liberated from ~2mg powdered samples with BrF5 using a 30W
CO2 laser (λ = 10.6µm), then purified cryogenically, passed through hot Hg to remove
any residual F2, and finally converted to CO2 with a hot carbon rod. All analyses were
standardized daily by four or more analyses of UWG-2, Gore Mountain garnet standard,
and sample δ18O values were corrected to the accepted value of 5.80‰ VSMOW for
UWG-2 (31 Valley et al. 1995).
Hydrogen isotope measurements were made at the Stable Isotope Laboratory at Leibniz
Universität Hannover except for sample WH68-1 (F), which was analyzed at the USGS
lab in Denver. Isotope ratios were measured by continuous flow mass spectrometry with
a ThermoElectron TC-EA coupled on-line to a ThermoElectron deltaV advantage mass
spectrometer. Clay mineral separates (0.8 to 1.0 mg) were wrapped in Ag-foil, loaded
into an Al sample holder, and dried at 150-200°C over night. To minimize the effects of
potential rehydration of swelling clays with atmospheric moisture, samples were rapidly
(<120 s) transferred into a sealed autosampler assembly and immediately exposed to dry
He. Hydrogen was liberated at 1450°C in the TC-EA. Three internationally referenced
standard materials and two in-house quality control standards were run with the samples,
and the raw isotope data were corrected for mass bias, daily drift of the reactor, and offset
from the certified reference values. After correction, standards NBS30 (biotite), CH-7
(polyethylene foil), and NBS22 (oil) yielded D values within 3% of the certified
reference values. All isotopic ratios are reported relative to standard mean ocean water
(SMOW).
Supplementary DR 4
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016,
Meteoric fluid infiltration in crustal-scale normal fault systems as indicated
by 18O and 2H geochemistry and 40Ar/39Ar dating of neoformed clays in
brittle fault rocks: Lithosphere, v. 8, doi:10.1130/L483.1.
L483_DR4.xls Supplementary DR 5
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016, Meteoric fluid infiltration in crustal-scale normal fault
systems as indicated by d18O and d2H geochemistry and 40Ar/39Ar dating of neoformed clays in brittle fault rocks:
Lithosphere, v. 8, doi:10.1130/L483.1.
mc24-14 Ashland-1(C) Illite
0.5
Ca/K
0.4
0.3
0.2
0.1
0.0
0.025
Cl/K
0.020
0.015
0.010
0.005
0.000
Age in Ma
300
250
200
150
100
Total gas age = 139.7 0.2 Ma
Retention age = 164.6 0.3 Ma
frecoil = 0.157
50
0
0.0
0.1
0.2
0.3
0.4
Fraction of
0.5
39
0.6
0.7
Ar Released
0.8
0.9
1.0
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016, Meteoric fluid infiltration in crustal-scale normal fault
systems as indicated by d18O and d2H geochemistry and 40Ar/39Ar dating of neoformed clays in brittle fault rocks:
Lithosphere, v. 8, doi:10.1130/L483.1.
mc24-1 Ashland 1(M) Illite
0.5
Ca/K
0.4
0.3
0.2
0.1
0.0
Cl/K
0.004
0.003
0.002
0.001
0.000
180
Age in Ma
160
140
120
Total gas age = 49.52 0.17 Ma
Retention age = 63.94 0.22 Ma
frecoil = 0.230
100
80
60
40
20
0
0.0
0.1
0.2
0.3
0.4
Fraction of
0.5
39
0.6
0.7
Ar Released
0.8
0.9
1.0
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016, Meteoric fluid infiltration in crustal-scale normal fault
systems as indicated by d18O and d2H geochemistry and 40Ar/39Ar dating of neoformed clays in brittle fault rocks:
Lithosphere, v. 8, doi:10.1130/L483.1.
mc24-7 Ashland-1(F) Illite
0.5
Ca/K
0.4
0.3
0.2
0.1
0.0
0.025
Cl/K
0.020
0.015
0.010
0.005
0.000
70
Age in Ma
60
50
40
Total gas age = 11.54 0.18 Ma
Retention age = 15.95 0.25 Ma
frecoil = 0.283
30
20
10
0
0.0
0.1
0.2
0.3
0.4
Fraction of
0.5
39
0.6
0.7
Ar Released
0.8
0.9
1.0
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016, Meteoric fluid infiltration in crustal-scale normal fault
systems as indicated by d18O and d2H geochemistry and 40Ar/39Ar dating of neoformed clays in brittle fault rocks:
Lithosphere, v. 8, doi:10.1130/L483.1.
mc24-2 Mormon-1(F) Illite
5
Ca/K
4
3
2
1
0
Cl/K
4
3
2
1
0
Age in Ma
25
20
15
Total gas age = 2.76 0.45 Ma
Retention age = 4.74 1.00 Ma
frecoil = 0.556
10
5
0
0.0
0.1
0.2
0.3
0.4
Fraction of
0.5
39
0.6
0.7
Ar Released
0.8
0.9
1.0
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016, Meteoric fluid infiltration in crustal-scale normal fault
systems as indicated by d18O and d2H geochemistry and 40Ar/39Ar dating of neoformed clays in brittle fault rocks:
Lithosphere, v. 8, doi:10.1130/L483.1.
mc47-10 BW2C <2 Illite
0.2
Ca/K
0.2
0.1
0.0
0.0
Cl/K
0.04
0.03
0.02
0.01
0.00
Age in Ma
12
10
8
Total Gas age = 6.99 0.21 Ma
Retention age = 8.31 0.23 Ma
frecoil = 0.1491
6
4
2
0
0.0
0.1
0.2
0.3
0.4
Fraction of
0.5
39
0.6
0.7
Ar Released
0.8
0.9
1.0
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016, Meteoric fluid infiltration in crustal-scale normal fault
systems as indicated by d18O and d2H geochemistry and 40Ar/39Ar dating of neoformed clays in brittle fault rocks:
Lithosphere, v. 8, doi:10.1130/L483.1.
mc47-11 BW2C <1 Illite
0.2
Ca/K
0.2
0.1
0.0
0.0
Cl/K
0.04
0.03
0.02
0.01
0.00
Total Gas age = 5.64 0.20 Ma
Retention age = 7.09 0.26 Ma
frecoil = 0.2099
Age in Ma
12
10
8
6
4
2
0
0.0
0.1
0.2
0.3
0.4
Fraction of
0.5
39
0.6
0.7
Ar Released
0.8
0.9
1.0
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016, Meteoric fluid infiltration in crustal-scale normal fault
systems as indicated by d18O and d2H geochemistry and 40Ar/39Ar dating of neoformed clays in brittle fault rocks:
Lithosphere, v. 8, doi:10.1130/L483.1.
mc47-12 BW2C <0.2 Illite
0.2
Ca/K
0.2
0.1
0.0
0.0
Cl/K
0.015
0.010
0.005
0.000
Age in Ma
12
Total Gas age = 4.87 0.17 Ma
Retention age = 8.04 0.26 Ma
frecoil = 0.3917
10
8
6
4
2
0
0.0
0.1
0.2
0.3
0.4
Fraction of
0.5
39
0.6
0.7
Ar Released
0.8
0.9
1.0
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016, Meteoric fluid infiltration in crustal-scale normal fault
systems as indicated by d18O and d2H geochemistry and 40Ar/39Ar dating of neoformed clays in brittle fault rocks:
Lithosphere, v. 8, doi:10.1130/L483.1.
mc47-13 BW2C <0.05 Illite
0.5
Ca/K
0.4
0.3
0.2
0.1
0.0
Cl/K
0.15
0.10
0.05
0.00
18
Age in Ma
16
14
12
10
Total Gas age = 3.25 0.55 Ma
Retention age = 6.18 1.01 Ma
frecoil = 0.4848
8
6
4
2
0
0.0
0.1
0.2
0.3
0.4
Fraction of
0.5
39
0.6
0.7
Ar Released
0.8
0.9
1.0
Supplementary DR 5
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016,
Meteoric fluid infiltration in crustal-scale normal fault systems as indicated
by 18O and 2H geochemistry and 40Ar/39Ar dating of neoformed clays in
brittle fault rocks: Lithosphere, v. 8, doi:10.1130/L483.1.
References reporting paired 18O and 2H measurements of illite (I), smectite (S), and/or
chlorite (C)
Abdioglu, E., Arslan, M., (2005). Mineralogy, geochemistry and genesis of bentonites of
the Ordu area, NE Turkey. Clay Minerals 40, pp. 131-151. (S)
Addy, S., Ypma,, P., (1977). Origin of massive sulfide deposits at Ducktown, Tennessee:
an oxygen, carbon and hydrogen isotope study. Economic Geology 72, pp. 12451268. (C)
Alderton, D., Fallick, A., (2000). The nature and genesis of gold-silver-tellurium
mineralization in the Metaliferi Mountains, of western Romania. Economic
Geology 95, pp. 495-516. (I)
Alexandre, P., Kyser, K., Polito, P., Thomas, D., (2005). Alteration mineralogy and
stable isotope geochemistry of paleoproterozoic basement-hosted unconformitytype unranium deposits in the Athabasca Basin, Canada. Economic Geology 100,
pp. 1547-1563. (I,C)
Bechtel, A., Shieh, Y-N., Elliott, W., Oszczepalski, S., Hoernes, S., (2000). Mineralogy,
crystallinity and stable isotopic composition of illitic clays within the Polish
Zechstein basin: implications for the genesis of Kupferschiefer mineralization.
Chemical Geology 163, pp. 189-205. (I)
Benavides, J., Kyser, T., Clark, A., Oates, C., Zamora, R., Tarnovschi, R., Castillo, B.,
(2007). The Mantoverde Iron Oxide-Copper-Gold District, III Región, Chile: The
Role of Regionally Derived, Nonmagmatic Fluids in Chalcopyrite Mineralization
Economic Geology 102, pp. 415-440. (C)
Benthke, P. Rye, R., (1979). Environment of ore deposition in the Creede mining district,
San Juan Mountains, Colorado; Part IV, Source of fluids, from oxygen, hydrogen,
and carbon isotope studies. Economic Geology 74, pp. 1832-1851. (I,C)
Boulvais, P., de Parseval, P., D’Hulst, A., Paris, P., (2006). Carbonate alteration
associated with talc-chlorite mineralization in the eastern Pyrenees, with emphasis
on the St. Barthelemy Massif. Mineralogy and Petrology 88, pp. 499-592. (C)
Cadrin, A., Kyser, T., Caldwell, W., Longstaffe, F., (1995). Isotopic and chemical
compositions of bentonites as paleoenvironmental indicators of the Cretaceous
western interior seaway. Paleogeography, Paleoclimatology, Paleoecology 119,
pp. 301-320. (S)
Clark, C., Hand, M., Faure, K., Schmidt Mumm, A., (2006). Up-temperature flow of
surface-derived fluids in the mid-crust: the role of pre-orogenic burial of hydrated
fault rocks. J. Metamorphic Geology 24, pp. 367-387. (C)
Clauer, N., Honty, M., Fallick, A., Sucha, V., Aubert, A., (2014). Regional illitization in
bentonite beds from the East Slovak Basin based on isotopic characteristics (KAr, 18O and D) of illite-type nanoparticles. Clay Minerals 49, pp. 247-275. (I)
Compton, J., Conrad, M., Vennemann, T., (1999). Stable isotopic evolution of volcanic
ash layers during diagenesis of the Miocene Monterey Formation, California.
Clays and Clay Minerals 47, pp. 84-95 (S)
Eslinger, E., Yeh, H., (1986). Oxygen and hydrogen isotope geochemistry of Cretaceous
bentonites and shales from the Disturbed Belt, Montana. Geochimical et
Cosmochimica Acta 50, pp. 59-68. (I,S)
Fallick, A., Macualay, C., Haszeldine, R., (1993). Implications of linearly correlated
oxygen and hydrogen isotopic compositions for kaolinite and illite in the Magnus
Sanstone, North Sea. Clays and Clay Minerals 41, pp. 184-190. (I)
Faure, K., Matsushisa, Y., Metsugi, H., Mizota, C., Hayashi, S., (2002). The Hishikari
Au-Ag epithermal deposit, Japan: Oxygen and hydrogen isotope evidence in
determining the source of paleohydrothermal fluids. Economic Geology 97, pp.
481-498. (S)
Gilg, H., Weber, B., Kasbohm, J., Frei, R., (2003). Isotope geochemistry and origin of
illite-smectite and kaolinite from the Seilitz and Kemmlitz kaolin deposits,
Saxony Germany. Clay Minerals 38, pp. 95-112. (I)
Girard, J-P., Munz, I., Johansen, H., Lacharpagne, J-C., Sommer, F., (2002). Diagenesis
of the Hild Brent sandstones, northern North Sea: Isotopic evidence for the
prevailing influence of deep basinal water. J. Sedimentary Research 72, pp. 746759. (I)
Glasmann, J., Lundergard, P., Clark, R., Penny, B., Collins, I., (1989). Geochemical
evidence for the history of diagenesis and fluid migration: Brent Sandstone,
Heather Field, North Sea. Clay Minerals 24, pp. 255-284 (I)
Heaton, T., Sheppard, S., (1977). Hydrogen and oxygen isotope evidence for sea-waterhydrothermal alteration and ore deposition, Troodos Complex, Cyprus. In:
Volcanic processes in ore genesis, Inst. Mining Metallurg., London, pp. 42-57.
(C)
Hillier, S., Fallick, A., Matter, A., (1996). Origin of pore-lining chlorite in the Aeolian
Rotliegand of northern Germany. Clay Minerals 31, 153-171. (C)
Hogg, A., Pearson, M., Fallick, A., Hamilton, P., (1995). An integrated thermal and
isotopic study of the diagenesis of the Brent Group, Alwyn South, UK North Sea.
Applied Geochemistry 10, pp. 531-546. (I)
Horton, T., Sojstrom, D., Abruzzese, M., Poage, M., Waldbauer, J., Hren, M., Wooden,
J., Chamberlin, C. (2004). Spatial and temporal variation of Cenozoic surface
elevation in the Great Basin and Sierra Nevada. American Journal of Science 304,
pp. 862-888. (S)
Horton, T., Chamberlin, C., (2006). Stable isotopic evidence for Neogene surface
downdrop in the Central Basin and Range Province. Geological Society of
America Bulletin 118, pp. 475-490. (S)
Isik, V., Tonguc Uysal, I., Caglayan, A., Seyitoglu, G., (2014). The evolution of
intraplate fault systems in central Turkey: Structural evidence and Ar-Ar and RbSr age constraints for the Savcili Fault Zone. Tectonics 33, pp. 1875-1899. doi:
10.1002/2014TC003565. (I)
Klein, E., Ribeiro, J., Harris, C., Moura, C., Giret, A., (2008). Geology and fluid
characteristics of the Mina Velha and Mandiocal orebodies and implications for
the genesis of the orogenic Chega Tudo gold deposit, Gurupi Belt, Brazil.
Economic Geology 103, pp. 957-980. (C)
Klein, E., Harris, C., Giret, A., Moura, C., (2007). The Cipoeiro gold deposit, Gurupi
belt, Brazil: Geology, chlorite geochemistry and stable isotope study. J. South
American Earth Sciences 23, pp. 242-255. (C)
Kerrich, R., Rehrig, W., 1987. Fluid motion associated with Tertiary mylonitization and
detachment faulting: 18O/16O evidence from the Picacho metamorphic core
complex, Arizona. Geology 15, p. 58-62. (C)
Lacroix, B., Charpintier, D., Buatier, M., Vennemann, T., Labaume, P., Adatte, T., Trave,
A., Dubois, M., (2012). Formation of chlorite during thrust fault reactivation.
Record of fluid origin and P-T conditions in the Monte Perdido thrust fault
(southern Pyrenees). Contrib. Min. Petrol. 163, pp. 1083-1102. (C)
Leclere, H., Lacroix, B., Fabbri, O., (2014). Fault mechanics at the base of the continental
seismogenic zone: Insights from geomechanical and mechanical analyses of a
crustal-scale transpressional fault from the Argentera crystalline massif, FrenchItalian Alps. J. Structural Geology 66, pp. 115-128. (C)
Longstaffe, F., Ayalon, A., (1987). Hydrogen-isotope geochemistry of diagenetic clay
minerals from Cretaceous sandstones, Alberta, Canada: evidence for exchange.
Applied Geochemistry 5, pp. 657-668. (I)
Masuda, H., Kusakabe, M., Sakai, H., (1992). Hydrogen and oxygen isotope ratios of
shales and characteristics of formation Geochimical et Cosmochimica Acta 56, pp.
3505-3511. (I)
Marumo, K., Longstaffe, F., Matsubaya, O., (1995). Stable isotope geochemistry of clay
minerals from fossil and active hydrothermal systems, southwestern Hokkaido,
Japan. Geochimical et Cosmochimica Acta 59, pp. 2545-2559. (I,S,C)
Menzies, C., Teagle, D., Craw, D., Cox, S., Boyce, A., Barrie, C., Roberts, S., (2014).
Incursion of meteoric waters into the ductile regime in an active orogen. Earth and
Planetary Science Letters 399, pp. 1-13. (C)
Montiero, L., Xavier, R., de Carvalho, E., Hitzman, M., Johnson C., de Souza Filho C.,
Torresi, I., (2008). Spatial and temporal zoning of hydrothermal alteration and
mineralization in the Sossego iron oxide–copper–gold deposit, Carajás Mineral
Province, Brazil: paragenesis and stable isotope constraints. Mineralium Deposita
43, pp. 129-159. (C)
Murzin, V., Shanina, S., (2007). Fluid Regime and Origin of Gold-Bearing Rodingites
from the Karabash Alpine-Type Ultrabasic Massif, Southern Ural. Geochemistry
International 45, pp. 998-1011. (C)
Primmer, T., Shaw, H., (1991). Variations in the D and 18O compositions of illitesmectites in a partially overpressured Tertiary sequence from an offshore well,
Texas Gulf Coast, USA. Marine and Petroleum Geology 8, pp. 225-231. (I,S)
Raimondo, T., Clark, C., Hand, M., Faure, K., (2011). Assessing the geochemical and
tectonic impacts of fluid-rock interaction in mid-crustal shear zones: a case study
from the intracontinental Alice Springs Orogen, central Australia. J. Metamorphic
Geology 29, pp. 821-850. (C)
Relvas, J., Barriga, F., Longstaffe, F., (2006). Hydrothermal alteration and mineralization
in the Neves-Corvo volcanic-hosted massive sulfide deposit, Portugal. II Oxygen,
hydrogen and carbon isotopes. Economic Geology 101, pp. 791-804. (C)
Rossi, M., Rolland, Y., (2014). Stable isotope and Ar/Ar evidence of prolonged
multiscale fluid flow during exhumation of orogenic crust: Example from the
Mont Blanc and Aar Massifs (NW Alps). Tectonics 33, pp. 1681-1709. Doi:
10.1002/2013TC003438. (C)
Sheppard, S., Nielson, R., Taylor, H., (1969). Oxygen and hydrogen isotope ratios of clay
minerals from porphyry copper deposits. Economic Geology 64, pp. 755-777. (S)
Sheppard, S., Taylor, H., (1974). Hydrogen and Oxygen Isotope Evidence for the Origins
of Water in the Boulder Batholith and the Butte Ore Deposits, Montana.
Economic Geology 69, pp. 926-946. (S)
Sjostrom, D., Hren, M., Horton, T., Waldbauer, J., Chamberlin, C., (2006). Stable
isotopic evidence for a pre—late Miocene elevation gradiant in the Great PlainsRocky Mountains region, USA. Geological Society of America Special Paper
398, pp. 309-319. (S)
Tonguç Uysal, I., Golding, S., Baublys, K., (2000) Stable isotope geochemistry of
authigenic clay minerals from Late Permian coal measures, Queensland,
Australia: implications for the evolution of the Bowen Basin. Earth and Planetary
Sciences Letters 180, pp. 149-162. (I,S)
Tonguç Uysal, I., Mutlu, H., Altunel, E., Karabacak, V., (2006). Clay mineralogical and
isotopic (K-Ar, 18O, D) constraints on the evolution of the North Anatolian
Fault Zone, Turkey. Earth and Planetary Science Letters 243, p. 181-194. (I)
Whitney, G., Northrop, H., (1987). Diagenesis and fluid flow in the San Juan Basin, New
Mexico – Regional zonation in the mineralogy and stable isotope composition of
clay minerals in sandstone. American Journal of Science 287, pp 353-382. (I,S,C)
Wilkinson, M., Fallick, A., Keaney, G., Hazeldine, R., McHardy, W., (1994). Stable
isotopes in illite: The case for meteoric water flushing within the upper Jurassic
Fulmar Formation sandstones, UK, North Sea. Clay Minerals 29, pp. 567-574. (I)
Yeh, H., Savin, S., (1977). Mechanism of burial metamorphism of argillaceous
sediments, III. O-isotope evidence. Geological Society of America Bulletin 88, pp.
1321-1330. (I,S)
Yeh, H., (1980). D/H ratios and late-stage dehydration of shales during burial.
Geochimical et Cosmochimica Acta 44, pp. 341-352. (I,S)
Ziegler, K., Longstaffe, F., (2000). Multiple episodes of clay alteration at the
Precambbriand/Paleozoic unconformity, Appalachian Basin: Isotopic evidence for
long-distance and local fluid migrations. Clays and Clay Minerals 48, pp. 474493. (I,C)
Ziegler, K., Longstaffe, F., (2000). Clay mineral authigenesis along a mid-continental
fluid conduit in Paleozoic sedimentary rocks from southern Ontario, Canada. Clay
Minerals 35, pp. 239-260. (I,C)
Supplementary DR 6
Haines, S., Lynch, E., Mulch, A., Valley, J.W., and van der Pluijm, B., 2016,
Meteoric fluid infiltration in crustal-scale normal fault systems as indicated
by 18O and 2H geochemistry and 40Ar/39Ar dating of neoformed clays in
brittle fault rocks: Lithosphere, v. 8, doi:10.1130/L483.1.
References reporting paired 18O and 2H measurements of illite (I), smectite (S), and/or
chlorite (C)
Abdioglu, E., Arslan, M., (2005). Mineralogy, geochemistry and genesis of bentonites of
the Ordu area, NE Turkey. Clay Minerals 40, pp. 131-151. (S)
Addy, S., Ypma,, P., (1977). Origin of massive sulfide deposits at Ducktown, Tennessee:
an oxygen, carbon and hydrogen isotope study. Economic Geology 72, pp. 12451268. (C)
Alderton, D., Fallick, A., (2000). The nature and genesis of gold-silver-tellurium
mineralization in the Metaliferi Mountains, of western Romania. Economic
Geology 95, pp. 495-516. (I)
Alexandre, P., Kyser, K., Polito, P., Thomas, D., (2005). Alteration mineralogy and
stable isotope geochemistry of paleoproterozoic basement-hosted unconformitytype unranium deposits in the Athabasca Basin, Canada. Economic Geology 100,
pp. 1547-1563. (I,C)
Bechtel, A., Shieh, Y-N., Elliott, W., Oszczepalski, S., Hoernes, S., (2000). Mineralogy,
crystallinity and stable isotopic composition of illitic clays within the Polish
Zechstein basin: implications for the genesis of Kupferschiefer mineralization.
Chemical Geology 163, pp. 189-205. (I)
Benavides, J., Kyser, T., Clark, A., Oates, C., Zamora, R., Tarnovschi, R., Castillo, B.,
(2007). The Mantoverde Iron Oxide-Copper-Gold District, III Región, Chile: The
Role of Regionally Derived, Nonmagmatic Fluids in Chalcopyrite Mineralization
Economic Geology 102, pp. 415-440. (C)
Benthke, P. Rye, R., (1979). Environment of ore deposition in the Creede mining district,
San Juan Mountains, Colorado; Part IV, Source of fluids, from oxygen, hydrogen,
and carbon isotope studies. Economic Geology 74, pp. 1832-1851. (I,C)
Boulvais, P., de Parseval, P., D’Hulst, A., Paris, P., (2006). Carbonate alteration
associated with talc-chlorite mineralization in the eastern Pyrenees, with emphasis
on the St. Barthelemy Massif. Mineralogy and Petrology 88, pp. 499-592. (C)
Cadrin, A., Kyser, T., Caldwell, W., Longstaffe, F., (1995). Isotopic and chemical
compositions of bentonites as paleoenvironmental indicators of the Cretaceous
western interior seaway. Paleogeography, Paleoclimatology, Paleoecology 119,
pp. 301-320. (S)
Clark, C., Hand, M., Faure, K., Schmidt Mumm, A., (2006). Up-temperature flow of
surface-derived fluids in the mid-crust: the role of pre-orogenic burial of hydrated
fault rocks. J. Metamorphic Geology 24, pp. 367-387. (C)
Clauer, N., Honty, M., Fallick, A., Sucha, V., Aubert, A., (2014). Regional illitization in
bentonite beds from the East Slovak Basin based on isotopic characteristics (KAr, 18O and D) of illite-type nanoparticles. Clay Minerals 49, pp. 247-275. (I)
Compton, J., Conrad, M., Vennemann, T., (1999). Stable isotopic evolution of volcanic
ash layers during diagenesis of the Miocene Monterey Formation, California.
Clays and Clay Minerals 47, pp. 84-95 (S)
Eslinger, E., Yeh, H., (1986). Oxygen and hydrogen isotope geochemistry of Cretaceous
bentonites and shales from the Disturbed Belt, Montana. Geochimical et
Cosmochimica Acta 50, pp. 59-68. (I,S)
Fallick, A., Macualay, C., Haszeldine, R., (1993). Implications of linearly correlated
oxygen and hydrogen isotopic compositions for kaolinite and illite in the Magnus
Sanstone, North Sea. Clays and Clay Minerals 41, pp. 184-190. (I)
Faure, K., Matsushisa, Y., Metsugi, H., Mizota, C., Hayashi, S., (2002). The Hishikari
Au-Ag epithermal deposit, Japan: Oxygen and hydrogen isotope evidence in
determining the source of paleohydrothermal fluids. Economic Geology 97, pp.
481-498. (S)
Gilg, H., Weber, B., Kasbohm, J., Frei, R., (2003). Isotope geochemistry and origin of
illite-smectite and kaolinite from the Seilitz and Kemmlitz kaolin deposits,
Saxony Germany. Clay Minerals 38, pp. 95-112. (I)
Girard, J-P., Munz, I., Johansen, H., Lacharpagne, J-C., Sommer, F., (2002). Diagenesis
of the Hild Brent sandstones, northern North Sea: Isotopic evidence for the
prevailing influence of deep basinal water. J. Sedimentary Research 72, pp. 746759. (I)
Glasmann, J., Lundergard, P., Clark, R., Penny, B., Collins, I., (1989). Geochemical
evidence for the history of diagenesis and fluid migration: Brent Sandstone,
Heather Field, North Sea. Clay Minerals 24, pp. 255-284 (I)
Heaton, T., Sheppard, S., (1977). Hydrogen and oxygen isotope evidence for sea-waterhydrothermal alteration and ore deposition, Troodos Complex, Cyprus. In:
Volcanic processes in ore genesis, Inst. Mining Metallurg., London, pp. 42-57.
(C)
Hillier, S., Fallick, A., Matter, A., (1996). Origin of pore-lining chlorite in the Aeolian
Rotliegand of northern Germany. Clay Minerals 31, 153-171. (C)
Hogg, A., Pearson, M., Fallick, A., Hamilton, P., (1995). An integrated thermal and
isotopic study of the diagenesis of the Brent Group, Alwyn South, UK North Sea.
Applied Geochemistry 10, pp. 531-546. (I)
Horton, T., Sojstrom, D., Abruzzese, M., Poage, M., Waldbauer, J., Hren, M., Wooden,
J., Chamberlin, C. (2004). Spatial and temporal variation of Cenozoic surface
elevation in the Great Basin and Sierra Nevada. American Journal of Science 304,
pp. 862-888. (S)
Horton, T., Chamberlin, C., (2006). Stable isotopic evidence for Neogene surface
downdrop in the Central Basin and Range Province. Geological Society of
America Bulletin 118, pp. 475-490. (S)
Isik, V., Tonguc Uysal, I., Caglayan, A., Seyitoglu, G., (2014). The evolution of
intraplate fault systems in central Turkey: Structural evidence and Ar-Ar and RbSr age constraints for the Savcili Fault Zone. Tectonics 33, pp. 1875-1899. doi:
10.1002/2014TC003565. (I)
Klein, E., Ribeiro, J., Harris, C., Moura, C., Giret, A., (2008). Geology and fluid
characteristics of the Mina Velha and Mandiocal orebodies and implications for
the genesis of the orogenic Chega Tudo gold deposit, Gurupi Belt, Brazil.
Economic Geology 103, pp. 957-980. (C)
Klein, E., Harris, C., Giret, A., Moura, C., (2007). The Cipoeiro gold deposit, Gurupi
belt, Brazil: Geology, chlorite geochemistry and stable isotope study. J. South
American Earth Sciences 23, pp. 242-255. (C)
Kerrich, R., Rehrig, W., 1987. Fluid motion associated with Tertiary mylonitization and
detachment faulting: 18O/16O evidence from the Picacho metamorphic core
complex, Arizona. Geology 15, p. 58-62. (C)
Lacroix, B., Charpintier, D., Buatier, M., Vennemann, T., Labaume, P., Adatte, T., Trave,
A., Dubois, M., (2012). Formation of chlorite during thrust fault reactivation.
Record of fluid origin and P-T conditions in the Monte Perdido thrust fault
(southern Pyrenees). Contrib. Min. Petrol. 163, pp. 1083-1102. (C)
Leclere, H., Lacroix, B., Fabbri, O., (2014). Fault mechanics at the base of the continental
seismogenic zone: Insights from geomechanical and mechanical analyses of a
crustal-scale transpressional fault from the Argentera crystalline massif, FrenchItalian Alps. J. Structural Geology 66, pp. 115-128. (C)
Longstaffe, F., Ayalon, A., (1987). Hydrogen-isotope geochemistry of diagenetic clay
minerals from Cretaceous sandstones, Alberta, Canada: evidence for exchange.
Applied Geochemistry 5, pp. 657-668. (I)
Masuda, H., Kusakabe, M., Sakai, H., (1992). Hydrogen and oxygen isotope ratios of
shales and characteristics of formation Geochimical et Cosmochimica Acta 56, pp.
3505-3511. (I)
Marumo, K., Longstaffe, F., Matsubaya, O., (1995). Stable isotope geochemistry of clay
minerals from fossil and active hydrothermal systems, southwestern Hokkaido,
Japan. Geochimical et Cosmochimica Acta 59, pp. 2545-2559. (I,S,C)
Menzies, C., Teagle, D., Craw, D., Cox, S., Boyce, A., Barrie, C., Roberts, S., (2014).
Incursion of meteoric waters into the ductile regime in an active orogen. Earth and
Planetary Science Letters 399, pp. 1-13. (C)
Montiero, L., Xavier, R., de Carvalho, E., Hitzman, M., Johnson C., de Souza Filho C.,
Torresi, I., (2008). Spatial and temporal zoning of hydrothermal alteration and
mineralization in the Sossego iron oxide–copper–gold deposit, Carajás Mineral
Province, Brazil: paragenesis and stable isotope constraints. Mineralium Deposita
43, pp. 129-159. (C)
Murzin, V., Shanina, S., (2007). Fluid Regime and Origin of Gold-Bearing Rodingites
from the Karabash Alpine-Type Ultrabasic Massif, Southern Ural. Geochemistry
International 45, pp. 998-1011. (C)
Primmer, T., Shaw, H., (1991). Variations in the D and 18O compositions of illitesmectites in a partially overpressured Tertiary sequence from an offshore well,
Texas Gulf Coast, USA. Marine and Petroleum Geology 8, pp. 225-231. (I,S)
Raimondo, T., Clark, C., Hand, M., Faure, K., (2011). Assessing the geochemical and
tectonic impacts of fluid-rock interaction in mid-crustal shear zones: a case study
from the intracontinental Alice Springs Orogen, central Australia. J. Metamorphic
Geology 29, pp. 821-850. (C)
Relvas, J., Barriga, F., Longstaffe, F., (2006). Hydrothermal alteration and mineralization
in the Neves-Corvo volcanic-hosted massive sulfide deposit, Portugal. II Oxygen,
hydrogen and carbon isotopes. Economic Geology 101, pp. 791-804. (C)
Rossi, M., Rolland, Y., (2014). Stable isotope and Ar/Ar evidence of prolonged
multiscale fluid flow during exhumation of orogenic crust: Example from the
Mont Blanc and Aar Massifs (NW Alps). Tectonics 33, pp. 1681-1709. Doi:
10.1002/2013TC003438. (C)
Sheppard, S., Nielson, R., Taylor, H., (1969). Oxygen and hydrogen isotope ratios of clay
minerals from porphyry copper deposits. Economic Geology 64, pp. 755-777. (S)
Sheppard, S., Taylor, H., (1974). Hydrogen and Oxygen Isotope Evidence for the Origins
of Water in the Boulder Batholith and the Butte Ore Deposits, Montana.
Economic Geology 69, pp. 926-946. (S)
Sjostrom, D., Hren, M., Horton, T., Waldbauer, J., Chamberlin, C., (2006). Stable
isotopic evidence for a pre—late Miocene elevation gradiant in the Great PlainsRocky Mountains region, USA. Geological Society of America Special Paper
398, pp. 309-319. (S)
Tonguç Uysal, I., Golding, S., Baublys, K., (2000) Stable isotope geochemistry of
authigenic clay minerals from Late Permian coal measures, Queensland,
Australia: implications for the evolution of the Bowen Basin. Earth and Planetary
Sciences Letters 180, pp. 149-162. (I,S)
Tonguç Uysal, I., Mutlu, H., Altunel, E., Karabacak, V., (2006). Clay mineralogical and
isotopic (K-Ar, 18O, D) constraints on the evolution of the North Anatolian
Fault Zone, Turkey. Earth and Planetary Science Letters 243, p. 181-194. (I)
Whitney, G., Northrop, H., (1987). Diagenesis and fluid flow in the San Juan Basin, New
Mexico – Regional zonation in the mineralogy and stable isotope composition of
clay minerals in sandstone. American Journal of Science 287, pp 353-382. (I,S,C)
Wilkinson, M., Fallick, A., Keaney, G., Hazeldine, R., McHardy, W., (1994). Stable
isotopes in illite: The case for meteoric water flushing within the upper Jurassic
Fulmar Formation sandstones, UK, North Sea. Clay Minerals 29, pp. 567-574. (I)
Yeh, H., Savin, S., (1977). Mechanism of burial metamorphism of argillaceous
sediments, III. O-isotope evidence. Geological Society of America Bulletin 88, pp.
1321-1330. (I,S)
Yeh, H., (1980). D/H ratios and late-stage dehydration of shales during burial.
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