shortening rates at the mountain front of the andean ... · brooks et al. (2003) (salomon et al.,...
TRANSCRIPT
Eric Salomon 1,2, Silke Schmidt-Mechernich 1,3, Ralf Hetzel 1, Francisco Mingorance 4, Victor A. Ramos 5
1 Institut für Geologie und Paläontologie, Westfälische Wilhelms-Universität Münster, Germany.2 Institut für Geowissenschaften, Johannes Gutenberg-Universität Mainz, Germany.3 Institut du Physique du Globe, CNRS Strasbourg, France. 4 Instituto de Mecánica Estructural y Riesgo Sísmico, Universidad Nacional de Cuyo, Mendoza, Argentina.5 Laboratorio de Tectónica Andina, Universidad de Buenos Aires, Argentina.
References
5. Conclusions
Acknowledgements
(1) The Peñas and Cal thrusts appear to have ruptured in characteristic Mw ~7 earthquakes that produced vertical offsets of ~1.0 m.
(2) The Holocene horizontal shortening rates of both thrusts are 1-2 mm/a.
(3) The geological shortening rates (3-6 mm/a) and the GPS rates (2-5 mm/a) are only slightly higher indicating (i) that the two range-bounding thrust faults account for a large amount of the deformation at the Andean mountain front, and (ii) that the shortening rates at the eastern Andean mountain front are similar since ~10 Ma.
Brooks, B.A. et al. (2003). Crustal motion in the Southern Andes (26°-36°S): Do the Andes behave like a microplate? G3 4, 1085, doi: 10.1029/2003GC000505.
Hilley, G.E., Strecker, M.R., Ramos, V.A. (2004). Growth and erosion of fold-and-thrust belts with an application to the Aconcagua fold-and-thrust belt, Argentina. J. Geophys. Res. 109, B01410, doi: 10.1029/2002jb002282.
Kendrick, E. et al. (2006). Active orogeny of the south-central Andes studied with GPS geodesy. Rev. Asoc. Geol. Arg. 61, 555-566. Ramos, V.A. et al. (2004). The Andean thrust system- Latitudinal variations in structural styles and orogenic shortening, in Thrust tectonics and hydrocarbon systems: AAPG Memoir, edited by K.R. McClay, pp. 30-50. Salomon, E. et al. (in press). Repeated folding during late Holocene earthquakes on the La Cal thrust fault near Mendoza city (Argentina). Bull. Seismol. Soc. Am. 103, doi: 10.1785/0120110335.
The financial support of the German Research Foundation (DFG, HE 1704/6-1) is gratefully acknowledged.
AGU2012: T43A-2639
Schmidt, S. et al. (2011). A note of caution on the use of boulders for exposure dating of depositional surfaces. EPSL 302, 60-70. Schmidt, S. et al. (2011). Coseismic displacements and Holocene slip rates for two active thrust faults at the mountain front of the Andean Precordillera (~33°S). Tectonics 30, TC5011, doi:10.1029/2011TC002932. Schmidt, S. et al. (2012). Optical dating of alluvial deposits at the orogenic front of the Andean Precordillera (Mendoza, Argentina). Geochronometria 39, 62-75. Walcek, A.A. & Hoke, G.D. (2012). Surface uplift and erosion of the Southernmost Argentine Precordillera. Geomorphology 153-154, 156-168.
Shortening rates at the mountain front of the Andean Precordillera (Argentina) on timescales of millions, thousands and a few years
contact: [email protected]
Slip rates of active reverse faults remain largely unknown at the eastern Andean mountain front, although large historical earthqua-kes illustrate the serious threat - e.g. a magnitude 7 earthquake deva-stated Mendoza in 1861 (Fig. 1).
According to GPS measure-ments, the present day E-W shortening rate in the Andean back-arc region (29.3 - 33.5°S) is 2-5 mm/a (Brooks et al., 2003; Kendrick et al., 2006; Fig. 2).In the extension of the Cal fault a local shortening rate of 2.8 ± 1.3 mm/a was calcu-lated using GPS data of Brooks et al. (2003) (Salomon et al., in press).
Peñas thrust
32.788°S
32.790°S
68.836°W
N
50 m
suburb of Mendozasuburb of Mendoza
Calthrust
Calthrust
0.77±0.15 ka0.77±0.15 ka
CT1CT1
CT2CT2
T4T4
T3T3
T2T2T3T3
T2T2
T0T0
T2T2T3T3
T1T1
T2T2
T4T4
T0T0
trenchtrench
c
CT3
CT4
CT3
CT4
23.2±1.0 ka23.2±1.0 ka
12.1±0.6 ka12.1±0.6 ka13.7±0.6 ka13.7±0.6 ka
21.9±1.0 ka21.9±1.0 ka
27.2±1.3 ka27.2±1.3 ka16.4±1.0 ka16.4±1.0 ka
fan surface
fan surface
active surfaceactive surface
roadroad
200 m
T4T4
T4T4
T4T4
T3T3
T3T3
T2T2
T2T2
T2T2T1T1
T3T3
N
3.84±0.14 ka
68.85°W68.86° W
32.755°S
32.76°S
active Cal thrustscarp profiles10Be age (ka) of boulders12.112.114C age (ka) of wood3.83.8
CT1CT1
fluvial terraces
T1 - T4
OSL age (ka) of quartz
0.770.77
b
Fig. 3: (a) Google Earth image showing northern Mendoza, the trace of the Cal thrust, and the study sites. (b,c) Terraces at the Cal thrust with the location of fault scarp profiles. 10Be ages from sandstone boulders are maximum ages (Schmidt et al., 2011 EPSL), hence terrace T4 has an age of ≤ 12.1 ka. (d) Profiles on terraces T1, T2, T3 and T4 indicate vertical displacements of ~0.9, ~2.6, ~3.6 and ~7 m, respectively (Schmidt et al., 2011 Tectonics).
Fig. 4: (a) Trench across the 2.5-m-high fault scarp of the Cal thrust (Salomon et al., in press). OSL ages after Schmidt et al. (2012). (b) Photograph of fold F1. (c) Retrodefor-mation of the folds using the area-balancing method (here example for F1).
2.6°
2.0°0.9 m
T1
T1
CT1
3.1°
4.6°
3.6 m
T3
T3
CT3
CT4
3.2°
3.7°
6.9 m
T4
T4
20 m5m
VE=3
T3: 3.84 ± 0.14 ka
T4: ≤12.1 ka
W E
T2: 0.77 ± 0.15 ka trench in Fig. 4
d
1.9°
2.8°
2.5 m
T2
T2
CT2
2. Cal thrust (millennial timescale)
Cal thrustCal thrust
MendozaMendoza5 km
68°58'W 68°50'W
32°46'S
32°46'S
a
Pre
cord
ill e
ra
NLa Cal
mountain1065 m
a
b
Fig. 5: Sequential restoration of the trench section (Salomon et al., in press).
PT3
E
50 m10 m
VE=3
T3 (12.6 ± 0.2 ka)vertical offset: 11.0 ± 1.0 m
1.9°
2.2°
10.6 mT3
PT1
T1vertical offset:0.9 ± 0.1 m
W
50 m10 m
VE=32.6°
2.6° 1.9 mT2 T2
T2 (3.3 ± 0.6 ka)vertical offset:1.9 ± 0.2 m
2.9°
0.9 m2.7°
T1
T15 m
1 m
VE=3
PT2
PT3PT3
WSW ENE3. Peñas thrust (millennial timescale)
active Peñas thrustterraces
view of Fig. 7
scarp profiles
14C age (cal) of wood
10Be age of sand
13.010Be age of pebbles
12.4 12.6
PT1T1 - T3
T2
20
Escondida creek
PT2
PT3
PT1
3.2 ± 0.6 ka
5.4 ± 1.0 ka
68.79°W
32.52°S
12.4 ± 1.5 ka 13.0 ± 1.9 ka
12.6 ± 0.2 ka
100 m
T3T3
T3T3
T2T2
T2T2
T1T1T1T1
N
b
11.1 ± 1.4 ka
3.3 ± 0.6 ka 3.3 ± 0.6 ka
500 m
68.78°W68.79°W
32.52°S
Peñas thrust
Escondida creek
a
bN
Fig. 7: Terraces T1, T2 and T3 have been dis-placed vertically by ~0.9, ~2 and ~11 m, respectively (Schmidt et al., 2011 Tec-tonics).
Fig. 6: (a) QuickBird image of an alluvial fan cut by the Peñas thrust. (b) Dated terraces at the Peñas thrust with the lo-cation of fault scarp profiles. In case ofthe 10Be depth profiles we calculated two ages: a minimum age by neglecting erosion and an age using a constant erosion rate of 20 mm/ka.
1. GPS and geological slip rates
Fig. 1: Map of the central Andes showing M ≥ 7 earthquake epicen-ters at the eastern mountain front.
AT35
AT37
AT39AT40
AT32
AT31
Jocoli
Mendoza
UspallataUspallata
32.5°
33°S
68.5°W69°69.5°69.5°
N
20 km
Pr e
c or d
i ll e
r a
Pr e
c or d
i ll e
r a
Peñas thrust
Cal thrust
Elevation5940 m
500 m
2.8 ± 1.3 mm/a
1920Ms 6.3
AT32
road
study sites of millennial rates
GPS station of Brooks et al. (2003) with velocity
earthquake epi- center, year, and magnitude
10 mm/a
Borbollón anticline
Capdeville anticline
1782Ms 7
1920Ms 6.3
2006Ms 5.6
1929Ms 5.7
Ms 7.01861
1917Ms 6.5
1985Ms 6.0
1967Ms 5.7
2001Ms 5.6
Fig. 6Fig. 6
Fig. 3Fig. 3
Pacific Ocean
125 Depth contours of Benioff zone (km)
SanJuanPr
ecor
dille
raPr
ecor
dille
ra
26°S
30°
34°
70°W 65°
N
100 km
Mendoza
1000 km
1861Ms 7.0
1944Ms 7.4
1977Ms 7.4
1782
Ms 7
1984Ms 7.5
Normal sub-
duction
Flat-slab sub-
duction
Normal sub-
duction
5075 100 150
200
64 mm/a
Santiago
Mendoza
Fig. 2: Tectonic map of the study area near Mendoza. GPS station velocities are taken from Brooks et al. (2003).
GPS shortening rates
Geological shortening ratesFor geolgical timescales, the rate of deformation is estimated by balanced crus-tal cross sections and different dating methods (mainly Ar-Ar of tuff). In the Precordillera the shortening rate illustrates 3-6 mm/a at 33°S (<30 km shorten-ing in ~10-5 Ma; compilation from Hilley et al., 2004; Ramos et al., 2004; Walcek and Hoke, 2012).
4. Millennial shortening rates4. Millennial shortening rates
Fig. 8: Horizonral shortening rates of the Cal and Peñas thrust faults in the Holocene.
Peñas thrust fault
T2
T3
00 2 4 6 8 10 12
age (ka)
5
10
15
20
25
horiz
onta
l offs
et (m
)
2.0 mm/a
2.2 mm/a
constant shortening rate
18611-2 EQs
1 EQ
Cal thrust fault
00 2 4 6 8 10 12
horiz
onta
l offs
et (m
)
age (ka)
2
4
6
8
10
12
T2
T3
T4
0.5 mm/a
maximum age
maximum age
variable shortening rate
≥0.9 mm/a
5.3 m
m/a
1.5 m
m/aunit (a)
deposition of unit (a): 770 ± 150 years ago(a)
(b)
axial plane of future fold F1
vertical displacement: 1.47 m
formation of folds F2 and F3 during the penultimate event
future wedge II
fold F2shortening:2.39 m
shortening: 1.71 m
vertical displacement: 1.08 m
formation of fold F1 during the last event
futurewedge I
fold F1
(c)
present-day
wedge Iwedge II
fold F3
fold F2
fold F1
C2
C1
(d)
W E
1 m
1 m
Fold F3
Fold F2
Terrace T2
1m
1m
W E
unit a
unit b
unit a
wedge I
wedge II
Fold F1
Terrace T2
1861 Ms~7.0 earthquake
1-2 M6.5-7.0 earthquakes between 861 AD and 770 BP
C2
C1OSL:12.3±2.4 ka
OSL:12.3 ± 2.3 ka
OSL: 11.7 ± 2.2 ka
OSL:770 ± 150 a
ba
Fold F1
WE
W ERetrodeformation of fold F1:
Fold F2: V=1.05 m, H=2.10 m, T=2.35 mFold F3: V=0.42 m, H=0.29 m, T=0.51 m
0.47 m
3.46 m
3.38 m2.049 m2
H = 1.71 mV = 1.08 m
T = 2.02 m
3.26 m
3.58 m
2.049 m2
0.76 m
cb