THE TECTONICS AND GEOMORPHOLOGY OF THE MOMA RANGE, NE RUSSIA
By
Benjamin G. Johnson

A THESIS
Submitted to
Michigan State University
in partial fulfillment of the requirements
for the degree of
Geological Sciences – Master of Science

2013

ABSTRACT
TECTONICS AND GEOMORPHOLOGY OF THE MOMA RANGE, NE RUSSIA
By
Benjamin G. Johnson
The Moma Range is a Late Cretaceous to Cenozoic, northeast verging fold-and-thrust
belt situated along the western boundary of the North American plate in northeast Asia. The
slow convergence between North America, Eurasia, and Okhotsk results in a zone of diffuse
continental deformation. While the Moma Range is >150 km northeast of main plate boundary
zone, the geomorphic character of major rivers along its northeast slope and the recent largemagnitude (up to 6.6 Mww) teleseismic earthquakes indicate that the Moma Range is actively
undergoing crustal shortening and accommodating regional convergence.
Changes in channel morphology, river knickpoints, and steepened channels suggest the
existence of a break in uplift rates along a previously mapped thrust-sense shear zone. In the
central portions of the fold-and-thrust, the deformation is focused along a structure ~30 km
inboard of the deformation front. However, the large-magnitude earthquakes are focused in the
western portions of the Moma Range, along thrust faults closer to outer edge of the fold-andthrust belt. These contrasting styles of deformation along-strike are potentially linked to
variations in decollement strength, syntectonic sedimentation, and the middle Cenozoic rifting
event that shut down convergence in region. This brief rifting event may have caused significant
thinning of the orogenic wedge of the fold-an-thrust belt by means of erosion and possibly
crustal thinning. By the Pliocene, the North American-–Eurasian rotation pole shifted north of
The Moma Range, reestablishing convergence in the region, and resulting in the continued
growth and internal deformation of the fold-and-thrust belt.

ACKNOWLEDGEMENTS

Foremost, I would to like to acknowledge the endless help and intellectual guidance of
my advisor, Kaz Fujita, without him this project would have never gotten off the ground, nor
reached its completion. He introduced me to plate tectonics and showed me what it takes to be
scientist. Most importantly, Kaz believed in me, often at times when not many did, and for that I
will always be indebted to him
I would also like to extend my gratitude to my other committee members, Kevin Mackey
and Brian Hampton: Kevin for his wealth of knowledge on all things Russian; and Brian for
helping me develop as a geologist, and for showing me the bigger picture.
Michigan State was a wonderful place for a geology graduate student. Professors like
Tyrone Rooney, Grahame Larsen, and Alan Arbogast, got me outside, away from the computer,
where geology is truly learned. Andrew Cyr (a guest lecturer) introduced me to the stream
profiler and ArcGIS methods. Renate Snider helped with the early stages writing, and Dan Burke
helped get things polished near the end. And I’m pretty sure I learned a great deal more from all
the students I TAed then they ever learned from me.
Without the companionship of my closest friends and family, my motivation to finish
would have long expired. Patricia was endless with her patients during the late nights and
weekends of writing. Blaze Budd, Matt Malkowski, Carl Fraser, and Brian Sparks were always
there when I needed beer. My siblings, Sam, Ashley and Kyle, let me forget about the stresses
graduate life over holiday breaks and vacations to Colorado. Lastly, I need to thank my parents,
Jim and Barb Johnson, whose selfless love and support kept me a-float when times were hard.

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TABLE OF CONTENTS

LIST OF FIGURES .........................................................................................................................v
1. INTRODUCTION......................................................................................................................1
2. TECTONIC EVOLUTION AND MODERN GEODYNAMICS ...............................................4
2.1 Mesozoic geology ..........................................................................................................4
2.2 Cenozoic geology ..........................................................................................................6
2.3 Geodynamics..................................................................................................................7
3. STUDY AREA ..........................................................................................................................10
3.1 High Moma Range .......................................................................................................10
3.2 Zyryanka Basin ............................................................................................................14
3.3 Alazeya Uplift ..............................................................................................................18
4. METHODS ...............................................................................................................................19
4.1 Channel morphology....................................................................................................20
4.2 Knickpoints in stream profiles .....................................................................................22
4.3 Normalized steepness index (ksn) ................................................................................24
5. RESULTS .................................................................................................................................31
5.1 Channel morphology ...................................................................................................31
5.2 Knickpoints in stream profiles .....................................................................................35
5.3 Normalized steepness index (ksn) ................................................................................43
6. DISCUSSION ...........................................................................................................................48
6.1 Interpretation of geomorphic data ................................................................................48
6.2 Earthquakes in the Moma Range .................................................................................51
6.3 Mechanisms for out-of-sequence deformation ............................................................54
6.4 Limitations of the analysis ...........................................................................................58
6.5 Future research .............................................................................................................60
7. CONCLUSIONS ......................................................................................................................62
REFERENCES .............................................................................................................................65

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LIST OF FIGURES

Figure 1:

Generalized tectonic and geographic index map of the Verkhoyansk—Kolyma
orogen (VKO) showing major tectonic plates (North America (NA), Eurasia
(EU), Okhotsk (OK), Pacific (PA), Amur (AM) and Bering (BE)). Star denotes
Cook et al. (1986) NA–EU pole of rotation .............................................................2

Figure 2:

Tectonic evolution of the Verkhoyansk—Kolyma orogen (VKO). Modified form
Parfenov (1991) and Layer et al. (2001). ...............................................................5

Figure 3:

Structural province map (outlined in Figure 1) of the Zyryanka foreland fold-andthrust belt (modified from Gaiduk et al., 1993). ITT, Ilin’-Tas thrust fault; MTF,
Myatis thrust fault. Thrust faults are represented by teeth on the hanging wall. ..11

Figure 4:

Geologic cross-sections of the Moma Range fold-and-thrust belt (modified from
Gaiduk et al., 1990; and Gaiduk and Prokopiev, 1999). Top two sections illustrate
a simplified and schematic restoration of the entire region, while the lower section
shows the architecture of the foreland fold-and-thrust belt. Lower cross-section
begins in the high Moma Range and transverses across the alluvial plain (see Fig.
3). For interpretation of the references to color in this and all other figures, the
reader is referred to the electronic version of this thesis .......................................12

Figure 5:

Generalized stratigraphic succession and lithology of Mesozoic and Cenozoic
deposits in the Zyryanka Basin (Modified from Ivanov, 1985).............................13

Figure 6:

Detailed geologic map (outlined in figure 3) of the Zyryanka thrust zone in the
region of the Myatis River. Major thrust faults, Ilin’-Tas (ITT) and Myatis (MTF),
are represented by teeth on the hanging wall, while minor thrust are represented
with hatch marks on the hanging wall. Geologic units: Bs, Bastakh Group; Og,
Ozhogina Formation; Si, Silyap Formation; Br, Buorkemyus Formation; Dr,
Darkylakh Formation; Kl, Kyllakh Formation (see figure 5 for stratigraphic
succession; modified from Gaiduk and Prokopiev, 1999). ...................................16

Figure 7:

Landsat image of the of the Zyryanka thrust zone in the region of the Myatis
River. The MTF is traceable by escarpments in the foothills of the Moma Range,
and the ITT marks a distinct transition in the topography. Area is appoximently
the same as figure 6................................................................................................17

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Figure 8:

Channel sinuosity plotted as function of channel slope (modified after Schumm
and Khan, 1972). B. The schematic response of a mixed-load meandering river to
the growth of an anticline. The localized uplift causes an increase in channel slope
on the downstream segment of the fold limb. This triggers an increase in channel
sinuosity and is coupled with incision across the fold limb, while the upstream
segment drops its sediment load. As time progresses the locus of incision migrates
upstream, smoothing the channel profile and eventually establishing the original
channel pattern (modified after Ouchi, 1985). .......................................................21

Figure 9:

Schematic models of knickpoint migration and morphology for various resistant
and nonresistant channel bed material (modified after Gardner, 1983). ...............23

Figure 10:

Schematics of equilibrium longitudinal profiles and their derived parameters
(modified from Whipple and Tucker, 1999). A. Longitudinal stream profile
concavity is set by q (concavity index). Graph shows how q values influence
profile shape, inset shows how q values are represented in slope-area space. B.
Two profiles with varying steepness indices (ksn). Note that although stream B is
twice as steep as stream A, they have the same concavity. ...................................25

Figure 11:

Sample distribution of slope-area data (black crosses) with the classification of
stream properties (modified from Sklar and Dietrich, 1998). Note that transitions
between classes are gradual and the extent of each class are dependent on the
specific grain size and sediment supply rate for any given stream ........................28

Figure 12:

Landsat image showing the abrupt change in thalweg sinuosity of the Indigirka
River as it cuts through the the western region of the Moma Range (see figure 3).
Inset shows a close up of the eastern terrace sequence and the meander scars
along the floodplain. Centroid moment tensor (Mww) from the February 14, 2013
earthquake in the Andrei-Tas Mountains shown in the upper left. ........................32

Figure 13:

Exposures of the Late Jurassic Bastakh Group along the Indigirka River. A. An
exposure along the west bank of the sinuous segment of the Indigirka River (see
Fig. 12). B. Upstream from the sinuous segment, showing a bed rock terrace on
the east bank of the river. Note steeply dipping and isoclinally folded strata
(pictures taken by Yuri Klaver) .............................................................................33

Figure 14:

Landsat image of narrowed channel segments along the Kyllakh and Myatis
Rivers just south of the Physiographic transition. Note the occurrence of icings
upstream of the narrowed channel segments .........................................................34

Figure 15:

Longitudinal profiles of the Indigirka River and its tributaries. Inset shows the
geographical distribution of the large rivers. White dots represent the major
knickpoints .............................................................................................................36

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Figure 16:

Channel data of the Kyllakh River. A. Slope-area distribution collected from the
60 m DEM. B. Longitudinal profile showing the major thrust faults crossed by the
river, the Ilin’-Tas (ITT) and the Myatis (MTF). In both plots blue lines are fits to
data with reference concavity (θref) of 0.45; red lines are fits to data with
concavity as a free parameter .................................................................................38

Figure 17:

Channel data of the Myatis River. A. Slope-area distribution collected from the 60
m DEM. B. Longitudinal profile showing the major thrust faults crossed by the
river, the Ilin’-Tas (ITT) and the Myatis (MTF). In both plots blue lines are fits to
data with reference concavity (θref) of 0.45; red lines are fits to data with
concavity as a free parameter. ...............................................................................39

Figure 18:

Channel data from a western tributary of the Ozhogina River. A. Slope-area
distribution collected from the 60 m DEM. B. Longitudinal profile showing he
major thrust faults crossed by the river, the Ilin’-Tas (ITT) and the Myatis (MTF).
In both plots blue lines are fits to data with reference concavity (θref) of 0.45; red
lines are fits to data with concavity as a free parameter. White dot indicates
knickpoint in the river. ..........................................................................................40

Figure 19:

Channel data from a left a tributary of the Zyryanka River (Sibik River, Figure
22). A. Slope-area distribution collected from the 60 m DEM. B. Longitudinal
profile showing the major thrust faults crossed by the river, the Myatis (MTF). In
both plots blue lines are fits to data with reference concavity (θref) of 0.45; red
lines are fits to data with concavity as a free parameter. White dot indicates
knickpoint in the river. ..........................................................................................41

Figure 20:

Channel data of the Susukmyakh River. A. Slope-area distribution collected from
the 60 m DEM. B. Longitudinal profile showing. In both plots blue lines are fits
to data with In both plots blue lines are fits to data with reference concavity (θref)
of 0.45; red lines are fits to data with concavity as a free parameter. White dot
indicates knickpoint in the river. Note the laqrge knickpoint (white dot) just above
the Ilin’-Tas thrust (ITT). Other knickpoints shown in profile (stair-step pattern)
are artifacts of processing (see text).......................................................................42

Figure 21:

Map of calculated normalized steepness values (ksn) for channels draining the
north slope of the Moma Range, in the region of the Myatis River. Values of ksn
are color coded to magnitude and plotted over hillshaded topography (provided by
www.viewfinderpanoramas.org). Narrowed channel segments are highlighted in
dark gray. Major thrust faults, Ilin’-Tas (ITT) and Myatis (MTF) are shown in
black with teeth on the hanging wall side. .............................................................45

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Figure 22:

Map of calculated normalized steepness values (ksn) for channels draining the
north slope of the Moma Range, in the region of the Ozhogina and Zyryanka
Rivers (Arga-Tas sub-province). Narrowed channel segments are highlighted in
dark gray. Dashed fault line is an inferred structure along the Taskan Ridge
(previously un-mapped) .........................................................................................46

Figure 23:

Map of calculated normalized steepness values (ksn) for channels draining the
north slope of the Moma Range, in the region of the Andrei-Tas sub-province.
Narrowed channel segments are highlighted in dark gray, and the knickpoint in
the Susukmyakh River is indicated with a white dot .............................................47

Figure 24:

Seismicity map of the Moma Range fold-and-thrust belt. Focal mechanisms are
shown with their corresponding magnitudes. Mww 6.6 is the February 14, 2013
event. .....................................................................................................................52

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1. INTRODUCTION
The original plate tectonic paradigm divides the Earth’s lithosphere into rigid plates, and
requires that all motion between the rigid plates occur at their boundaries (e.g., Morgan, 1968).
However, within continent-continent collisional and accretionary orogens, plate boundaries are
commonly characterized by zones of diffuse deformation (e.g., England and Jackson, 1989;
Gordon, 1995, 1998; Bird, 2003; Cawood et al., 2009). Among these complex intracontinental
settings is the Verkhoyansk—Kolyma orogen (VKO), a broad mountain belt of diffuse
deformation presently situated within the boundary region of the North American, Eurasian, and
Okhotsk plates in northeast Asia (Fig. 1).
The VKO extends from the Lena River in the west to the Kolyma River in the east (Fig.
1), covering an area of nearly 2 million km2. The region is sparsely populated, generally
inaccessible, and home to the coldest temperatures in the northern hemisphere. Adding to these
logistical issues; Soviet control for much of the 20th century kept western scientists from
entering the region until the late 1980’s, and very little of the original Soviet geologic literature
has been readily available, let alone translated into English. These issues have confined western
study of the region mostly to seismological studies (e.g., Chapman and Solomon, 1976; Cook et
al., 1986; Riegel et al., 1993; Mackey et al., 1998; Fujita et al., 2009), a few geodetic
investigations (Calais et al., 2003; DeMets et al., 1990; Gaina et al., 2002; Merkouriev and
DeMets, 2008), and one geochronology study (Layer et al., 2001); all of which are primarily
focused on delineating the main tectonic boundaries within the VKO. These tectonic boundaries
are traditionally drawn along the major, seismically active, strike-slip faults that traverse the
VKO’s interior (Fig. 1); however, the entire region is enclosed by the two, outward verging,
fold-and-thrust belts, the Verkhoyansk and the Moma Range (Fig. 1).

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Research on the present-day geodynamics in northeast Russia has concluded that Eurasia
and North America are currently converging (e.g., Cook et al., 1986; Parfenov et al., 1988; Fujita
et al., 2009), but few (Gaiduk et al., 1990; Imaev, 1991) have suggested that either of the foldand-thrust belts are currently active. This is likely because both fold-and-thrust belts are at
significant distance (> 150 km) from where the plate boundaries have been drawn (Fig. 1), and
up until recently, the fold-and-thrust belts for the most part have been characterized only by
microseismicity. However, there are a select number of moderate and larger-magnitude (> 5
Mw) events located in the western Moma Range and in the Nel’kan-Kyllakh thrust system of the
southern Verkhoyansk (Fujita et al., 2009). The complex tectonic history of the VKO traces back
to the mid-Mesozoic (e.g., Parfenov, 1991), and includes the collision of several crustal blocks
whose boundaries remain as zones of weakness, partitioning modern strain across a broad area.
The objective of this research is to combined geomorphology with remote sensing to
examine stream profiles and channel morphologies in the Moma Range fold-and-thrust belt to
help delineate the surface expressions of active deformation. Additionally, I explore the ability
and limitations of obtaining meaningful information on the tectonics of an inaccessible region,
where uplift rates and active structures are largely unknown, without going in the field.

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2. TECTONIC EVOLUTION AND MODERN GEODYNAMICS
2.1 Mesozoic geology
The VKO has developed since ~160 Ma in response to the closure of the Oimyakon
Ocean and subsequent collision of the Kolyma-Omolon superterrane with the Siberian craton
(e.g., Fujita and Newberry, 1982; Zonenshain et al., 1990; Parfenov, 1991; Oxman et al., 1995;
Prokopiev, 2000; Layer et al., 2001). Layer et al. (2001) constrained the tectonic evolution by
40Ar/39Ar geochronology and trace element geochemistry obtained from plutonic belts and
individual intrusions sampled within the VKO’s interior. It begins with the subduction of
oceanic crust beneath the Kolyma-Omolon superterrane in the Middle Jurassic (~160-140 Ma),
and the emplacement of subduction related granitoids (Layer et al., 2001) and the devlopment of
the Uyandina–Yasachnaya volcanic arc along with its backarc basin, the Ilin’-Tas (Fig. 2)
(Parfenov, 1991).
By the Early Cretaceous, the Kolyma-Omolon superterrane collided with the Siberian
craton, emplacing the 140-138 Ma collisional granites (Layer et al., 2001). The overlying
sedimentary cover detached from the basement in the form of large, outward-vergent fold-andthrust belts in both east and west directions. In the west, late Paleozoic and early Mesozoic
passive margin strata, back-thrust onto the Siberian Craton resulting in the formation of the
Verkhoyanask fold-and-thrust belt and Priverkhoyanask foredeep (Parfenov, 1991). The
westward propagation of thrusting in the Verkhoyansk Mountains, presumably ended in the Late
Cretaceous (Prokopiev, 2000). The eastward propagation lead to the inversion of the Ilin’-Tas
basin and the uplift and development of the Moma Range fold-and-thrust belt (Fig. 2) (Gaiduk et
al., 1990; Gaiduk et al., 1993; Gaiduk and Prokopiev, 1999). The timing and evolution of this

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event is unclear. Most authors recognize a Late Cretaceous folding event (e.g., Parfenov, 1991,
Prokopiev, 2000; Peach, 2009).
Subsequent to, and possibly concurrent with, the Late Cretaceous outward propagation of
the fold-and-thrust development, Layer et al. (2001) suggest a late-stage, east-west extensional
event that emplaced several granites and a series of north-south oriented dikes. They speculate
that the extension is related to the far-field back-arc effect of Okhotsk–Chukotka volcanic belt or
the more intermediate-field effect of the north-south closure of the South Anyui suture. A third
explanation for the Late Cretaceous extension is a hinterland collapse model, where the
sufficiently thickened crust of the VKO collapses under its own weight, laterally spreading out
and adding to the outward propagation of fold-and-thrust development (Fig. 2).
2.2 Cenozoic geology
The history of Cenozoic deformation in the VKO is poorly constrained, and several
models regarding its tectonic evolution exist. One model argues that collisional tectonics,
initiated in the Mesozoic, persisted until Quaternary time (Gaiduk et al., 1993; Gaiduk and
Prokopiev 1999; Fridovsky and Prokopiev, 2000; Paech, 2009). The evidence for prolonged
Cenozoic compression is minimal, but thrust structures in the northern foothills of the Moma
Range displace Late Cretaceous strata onto Oligocene-Miocene strata, lending to a late Cenozoic
shortening event (e.g., Gaiduk et al., 1990; Gaiduk and Prokopiev, 1999).
A second model includes a relatively short-lived period of middle Cenozoic riffing,
possibly associated with the protrusion of the Gakkel Ridge into the Asian continent (Cook et al.,
1986; Parfenov et al., 1988; Fujita et al., 1990; Calais et al., 2003, Teschegg et al., 2011). This is
supported by series of large topographical depressions within the eastern VKO (e.g., Moma–
Selennyakh, Uyandina, Ust-Nera, Seimchan–Buyunda). These depressions are intermontane and

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filled with Neogene to Paleogene strata (Grinenko et al., 1999). The largest of these is Moma–
Selennyakh depression (~16,000 km2, Fig. 3), and it is situated geographically between the
Chersky and Moma ranges.
In addition to topographical depressions, seafloor magnetic lineations along the MidAtlantic and Gakkel ridges reveal that the North America and Eurasia pole of rotation was
situated in the southern VKO during the middle Cenozoic (Savostin et al., 1984; Gaina et al.,
2002; Merkouriev and DeMets, 2008). It is likely that this southern sift of the pole of rotation
triggered the middle Cenozoic rifting event associated with the topographical depressions and
rift-related volcanism.
2.3 Geodynamics
Much of the attention by western scientists has focused on the modern geodynamics of
the VKO, in particular, deciphering the present-day tectonic boundary between the North
American and Eurasian plates in the region. Nearly 90% of the boundary between North
America and Eurasia is well defined; it begins in the North Atlantic Ocean along the MidAtlantic Ridge. It traces north into the Gakkel Ridge, the ultra-slow spreading center that bisects
the Arctic Ocean (e.g., Snow and Edmond, 2007). From there, the plate boundary penetrates into
the VKO, passing near or through its pole of rotation (Cook et al., 1986; Kogan et al., 2000;
Calais et al., 2003), where extension in the Arctic transitions to a seismically active, diffuse zone
of compression, known as the Chersky Seismic Belt (Parfenov et al., 1988; Fujita et al., 2009).
The Chersky Seismic Belt encompasses much of the VKO, but likely extends eastward to
northern Kamchatka and southward to Sakhalin Island (Fujita et al., 2009).
Contemporary thought surrounding the tectonic configuration involves three plates:
North America, Eurasia, and Okhotsk (e.g., Cook et al., 1986). The major boundaries between

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these plates are presumed to occur along a network of large strike-slip faults that occupy the
internal regions of the VKO (Kozmin, 1984; Imaev, 1991; Imaev et al., 1994, 1995; Fujita et al.,
2009). The most notable of these faults is the Ulakhan, a NW-SE sinistral strike-slip fault that
stretches for more than 700 km though the central Chersky Range to the Sea of Okhotsk, which
has been proposed to delineate the North American–Okhotsk tectonic boundary (e.g., Cook et al.,
1986; Parfenov et al., 1988; Riegel et al., 1993; Seno et al., 1996; Fujita et al., 2009). In the
southwestern portion of the VKO a series of north-south striking faults, known as Ketanda fault
system (Imaev et al., 1990; Riegel et al., 1993; Fujita et al., 2009), possibly delineates the
Eurasia–Okhotsk boundary. In the northern VKO no single fault has been proposed to be the
plate boundary; however, all the published tectonic maps draw the North American–Eurasian
plate boundary through this region (e.g., Bird, 2003; Fujita et al., 2009).
The present-day geodynamics in northeast Russia are unique in that the pole of rotation
between NA and EU, calculated using geophysical data, lie within the plate boundary zone (Fig
1., Cook et al. 1986; DeMets et al., 1990; Kogan et al., 2000; Sella et al., 2002; Calais et al.,
2003). The consensus among authors is that North America is converging with Eurasia, with
Okhotsk wedged in between. A number of models exist to explain how this “nutcracker” style of
motion is accommodated in the VKO. Riegel et al. (1993) and Hindle et al. (2009) hypothesized
that Okhotsk is undergoing lateral escape to the southeast along the seismogenic strike-slip faults
(e.g., Fujita et al., 2009) that dissect the internals of the VKO. This situation is similar to the
westward extrusion of Turkey along the North Anatolian fault zone (e.g., Mckenzie, 1972; Barka
1992), where Turkey is wedged between the converging Arabian and Eurasian plates. In both
situations, the convergence between the three plates is accommodated by localized transpression
along the internal strike-slip faults.

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In this research, I propose that the convergence between North America and Eurasia is
not exclusively accommodated by transpression along the strike-slip faults of the VKO. Active
shortening in the Moma Range fold-and-thrust belt, generally disregarded by past geodynamic
research (with the exception of Imaev’s limited work) because of its weak seismicity and
significant distance from the plate boundary zone, aids in the accommodation of strain within the
VKO. The structures of the Moma Range formed during the collision of the Kolyma–Omolon
superterrane with the Siberian Craton in the Mesozoic, and have possibly remained active
throughout the Cenozoic or were recently reactivated. Active structures can be identified using
geomorphic indicators, derived from remote sensing data, and then integrated into a mechanical
model based on Coulomb wedge of Davis et al. (1983).

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3. STUDY AREA
Soviet structural field expeditions and oil and gas surveys in the mid 1980's provided
much of what is currently known about the fold-and-thrust structures in the eastern VKO (e.g.,
Gaiduk et al., 1989, 1990, 1993; Imaev, 1991). The region is divided into five main structural
provinces, each characterized by a distinctive structure, stratigraphy, and physiography. From
south to north, I refer to these as the Chersky Range, the Moma-Selennyakh depression, the High
Moma Range, the Zyryanka basin, and the Alazeya Uplift (Fig. 3). The three most northern
provinces show elements of a foreland basin system, as defined by DeCelles and Giles (1996),
that comprises a fold belt (High Moma Range), thrust zone and foredeep (Zyryanka Basin), and
forebulge (Alazeya Uplift) (Fig. 4).
3.1 High Moma Range
The High Moma Range has three sub-provinces: Andrei-Tas, Ilin’-Tas, and Arga-Tas
mountains (Fig. 3). Together they cover an area nearly 30,000 km2 and reach elevations greater
than 2,000 m. Transverse drainage is a common feature along both the southern and northern
flanks of the range, with v-shaped river valleys that cut into and across the structural grain of the
mountain belt. In the High Moma Range the geology consists primarily of two formations, the
Ilin'-Tas and Bastakh formations. The Ilin'-Tas formation represents the bottom of the MomaZyryanka stratigraphic section (Fig. 5), and consists of Middle Jurassic (Callovian) tuffaceous
and basaltic volcaniclastic rocks (up to 850 m thick) (Ivanov, 1985). Outcrops of the Ilin’-Tas
are rare, and have only been mapped in the Andrei-Tas and Arga-Tas mountains (Surmilova,
1986). The Bastakh Formation (up to 6 km thick) consists of thin, rhythmically interbedded
sandstone and mudstone, and is locally tuffaceous. This is the main unit found in the central
portions of the High Moma Range (Ilin’-Tas Mountains).

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Cross sections published in Gaiduk et al. (1993) and Gaiduk and Prokopiev (1999) bound
the High Moma Range by two oppositely-directed overthrusts that penetrate the basement. The
fault along the northern boundary is the Ilin'-Tas thrust (ITT), which marks the boundary
between the High Moma Range and the northern foothills of the Zyryanka Basin. The southdirected thrust fault, on the back end of the fold-and-thrust belt, lacks conclusive evidence, as
some authors favor this as a normal fault associated with the Moma Rift (e.g., Fujita et al., 1990).
In the interior of the High Moma Range, the Bastakh Formation is isoclinally folded with steep
northeast verging folds. The folding is potentially driven by the reactivation of basement fabrics,
such as inverted grabens (Fig. 4) (Gaiduk et al., 1993). However, little is known about the deep
crustal structure of the region, and the cross-sections shown here and published in other works
are a speculative representation of the region’s structure.
3.2 Zyryanka Basin
The Zyryanka Basin is divided into two segments, a thrust zone and a foredeep. The
thrust zone segment, commonly referred to as the foothills zone (e.g., Gaiduk et al., 1993),
consist of an imbrication of northeast verging thrust sheets that expose early Cretaceous and
Cenozoic strata in the northern foothills of the Moma Range. In some localities, the Jurassic
Bastakh Formation is included in the thrust sheets. The majority of exposed geology in the thrust
zone is the Early Cretaceous strata of the Zyryanka Series (Fig. 5), where three formations are
recognized: Ozhogina, Silyap, and Buorkemyus (Ivanov, 1985). The series is several thousand
meters thick and consists of sandstone, siltstone, argillite, and coal. Exposed at the very northern
edge of the fold-and-thrust belt is the Eocene-Pliocene Myatis Series, where three formations are
recognized: El'gandya, Darkylakh, and Kyllakh (Grinenko et al., 1989). The series is

14

predominately an arenaceous sequence, consisting of sandstone and sand conglomerate, but is
locally interbedded with mudstone and lignite in the Darkylakh Formation.
Prokopiev and Gaiduk (1999) provide a detailed geologic map of the eastern half of the
thrust zone (Fig. 6), showing several northwest striking, sub-parallel thrust sheets, and two
northeast striking tear faults. The outermost thrust sheets are marked by a series of large
escarpments that form a salient around the region of the Myatis River, visible in the satellite
imagery (Fig. 7). Here the upper member of the Zyryanka Series, the Buorkemyus Formation, is
thrust into contact with the lower member of the Myatis Series, the El'gandya Formation, at the
southern side of the frontal escarpment (Fig. 4). I refer to this thrust as the Myatis Thrust Fault
(MTF), and it likely represents the frontal thrust of the Moma Range fold-and-thrust belt (Fig. 3).
Exposed along the northern escarpment near the Myatis River are the El'gandya and
Darkylakh Formations. Here bedding is nearly vertical at the contact with the MTF, and dip
angles gradually decrease to the northeast into the foredeep (Paech, 2009; Imaev, 1991). This
forms a leading edge monocline at the structural front (Fig. 4) that formed during thrusting along
the MTF.
The lateral extent of the thrust zone is not well studied, particularly along the eastern half
of the foothills between the Ozhogina and Zyryanka Rivers. Here the thrust zone is presumably
much thicker, extending out some 50 km from the topographic front of the hinterland. To the
west, the thrust zone extends across the foothills of Andrei-Tas Mountains to the Selennyakh
River. Outcrops examined along Bolchuk and Nikandya rivers, correlate with the observed
stratigraphy along the Myatis River in the central portions of the thrust zone (Grinenko et al.,
1989). The thrust zone widens along this stretch as well, but like the eastern portions of the thrust
zone, the structures are not mapped in any detail.

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16

17

The Zyryanka foredeep covers an area greater than 60,000 km2, and the strata exposed in
the thrust zone is flat lying and buried beneath a thick Quaternary cover. The depth down to the
Upper Jurassic basement is the thickest on the southwest side where it presumably thickens to 4
km (Gaiduk et al., 1989). A series of basement normal faults at the foredeep’s northern edge, dip
towards the basin's interior (Fig. 4).
At the surface, the foredeep resembles an alluvial plain. In the regions closest to the
thrust front, a series of broad fans with radiating drainage patterns extend more the 20 km out
from the thrust front. Their slopes do not exceed 0.4. The Badyarikha River makes the largest
of the fans, covering an area of ~650 km2 with a slope of 0.3 (Fig. 7). The fans appear to
decrease in size away from this central region and lose their distinctive fan shape. At the base of
the alluvial fans, the surface of the foredeep is characterized by a marshy swampland that covers
a large area (>40,000 km2) and consist of many large lakes.
3.3 Alazeya Uplift
The Alazeya Uplift is a topographically, isolated highland that bounds the northern end of
the Zyryanka Basin (Fig. 3). It covers an area greater than 17,000 km2, and reaches elevations of
600 m. Forebulge uplift has exposed pre-Upper Jurassic basement, presumably of island arc
affinity (Parfenov, 1991). Additionally, rocks exposed in the Alazeya Uplift include a series of
middle Cretaceous, plutonic, volcanic, and volcaniclastic rocks. Many faults, of various
orientations have been mapped in the region, but most of them presumably relate to preCretaceous/Cenozoic deformation. The rivers flow south with dendritic drainage patterns,
flowing into the larger rivers (Ozhogina and Badyarikha) in the alluvial plain of the Zyryanka
Basin before emptying into the Kolyma and Indigirka rivers.
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4. METHODS
Embedded in the Earth’s topography is information related to the external and internal
forces that shape the Earth’s lithosphere. At convergent plate boundaries, shortening of the
lithosphere generally produces broad, uplifted mountain belts of steep topography, where
surficial processes continually work to level them down. By this observation, it could be
hypothesized that mean topographic gradient correlates positively with uplift rates; however,
because hillslopes often reach limits in their gradients (Burbank et al., 1996) and uplift in many
mountain belts is distributed differentially, the fluvial network is frequently exploited to
examine, in more detail, the relationship between topography and tectonic forcing (e.g., Jackson
et al., 1996, Kirby and Whipple 2001, Kirby et al., 2003, Lesh and Ridgway 2007, Ponza et al.,
2010). Here, I provide an analysis of the rivers that drain the north slope of the Moma Range
with a primary focuses on channel morphology, steepness index of individual rivers (ksn), and
disturbances in stream profiles (knickpoints). Due to the inaccessibility of the region, digital and
analog topography and satellite imagery constitute the major datasets for this tectonic
geomorphic analysis.
In northeast Russia, the best resolution of topographic data publically available are the
1:200,000-scale Soviet military topographic maps, which recently have been converted into a 68
m digital elevation model (DEM) that spans all of Russia (www.viewfinderpanoramas.org).
Other elevation datasets, such as NASA’s Shuttle Radar Topography Mission (SRTM) and the
Advanced Spaceborne Thermal Emission and Reflection Radiometer (ASTER), are inadequate
for topographic analysis in northeast Russian because of the lack of coverage (north 60 latitude
for SRTM) and excessive data holes caused by cloud cover and abrupt changes in topographic
relief.

19

The best available satellite imagery of the Moma Range is the EarthSat NaturalVue 15 m
resolution color imagery that nearly covers the entire land area of the Earth. The imagery is
derived from images taken by NASA's Landsat 7 satellite, and is constructed by merging a 15 m
high-resolution panchromatic band, a 60 m thermal infrared band, and six 30 m multispectral
bands to create a single high-resolution color image. The images are orthorectified, mosaicked,
and color balanced to create a digital image that is seamless, accurate, and can be used in various
mapping software like ArcGIS (available at:
http://raster.arcgisonline.com/arcgis/rest/services/MDA_NaturalVue_Imagery/ImageServer).
4.1 Channel morphology
Abrupt changes in channel morphology are often associated with active tectonics,
particularly if morphologic changes correspond to areas of increased stream gradient or areas
where tectonic structures have been mapped. Numerous stream table experiments have indicated
that channel shape is a product of several competing controls, including sediment load, flow
velocity, and stream power (e.g., Shumm, 1986). In a particular stream table experiment, a
propagating fold was induced across the midsection of an established channel (Ouchi, 1985). It
was noticed that in the section immediately downstream from the fold axis, the channel increased
its sinuosity, drastically changing its shape (Fig. 8). The increased sinuosity becomes coupled
with incision, leaving behind a sequence of terraces (Fig. 8, Ouchi, 1985).
Changes in channel morphology have been identified in tectonically active landscapes
from around the globe (e.g., Bullard and Lettis, 1993; Lesh and Ridgeway, 2001; Amos and
Burbank, 2007), and they have illustrated a diverse fluvial response to active tectonic forcing.
Amos and Burbank (2007) noted that streams undergoing low uplift rates or streams with large
drainage areas tend to adjust to differential uplift by narrowing their channel widths, and tend to

20

21

be more incised. Streams undergoing high rates of differential uplift or streams with small
drainage areas adjust by steepening their channel bed.
As is discussed throughout this research, there are numerous competing controls on ways
in which fluvial systems adjust their channel morphologies apart from differential uplift or
tectonic forcing, including sediment load, stream bed lithology, and climatic factors. Using the
EarthSat NaturalVue satellite imagery I have identified several examples of changes in both
sinuosity and channel widths of some of the large rivers that drain the northern slope of the
Moma Range. I use these in combination with the best geological (Surmilova et al., 1986) and
geomorphic (Kolpakov, 1986) maps available to constrain possible external factors outside of
tectonic forcing.
4.2 Knickpoints in stream profiles
A knickpoint in a stream’s profile is an oversteepened reach or segment that occurs along
the course of a smooth profile (Fig. 9). Such a steepened reach could develop in the absence of
tectonic forcing simply because of differences in the erodability of the streambed lithology: more
resistant rocks will tend to underlie steeper reaches of a stream. Tectonically generated
knickpoints can be formed through differential folding or faulting at a localized segment along a
stream’s profile. Thrust faulting that differentially uplifts an upstream segment with respect to
the downstream segment will create a knickpoint in the stream’s profile by lowering the base
level of erosion for the stream below the fault. Across the steepened knickpoint, stream power
(the energy expended on the streambed) will increase due to the increased slope, and erosion of
the streambed will be enhanced. The effect of this erosion is to cause the knickpoint to migrate or
propagate upstream (Fig. 9; Gardner, 1983).

22

23

Knickpoints are identified within north slope rivers of the Moma Range using
longitudinal profiles extracted from the View-Pathfinder 68 m DEM. The method of data
extraction is that of Whipple et al. (2007), where it is clearly described. It provides a dual
interfaced and user-interactive environment between ArcGIS and Matlab to automate the
generation of stream profiles and to retrieve the corresponding slope-area data for individually
selected streams. Rivers with very large drainage areas (e.g., the Indigirka and Kolyma rivers)
require powerful computers to generate profiles, so some profiles were generated using analog
methods (i.e., using the 1:200,000 topographic maps and Google Earth) . The knickpoints are
handpicked by observing individual profiles streams and by looking at abrupt changes to trends
in the slope–area plots (see following section and Fig. 10).
4.3 Normalized steepness index (ksn)
Channel morphologies and knickpoints in stream profiles have relatively short residence
times in the geologic record (<10 kyr), and are therefore useful in identifying potential locations
of active displacement on faults or growth of folds. However, tectonic processes in northeast
Russia, like many other tectonic regions, are slow, and to more accurately understand how the
landscape responds to mountain building-scale tectonics, geomorphic processes that operate at
more intermediate time scales (>10 kyr) need to be examined. The components pertaining to the
shape of a stream profile, the steepness and concavity, are know to reflect the external variables
(rock uplift, climate, and streambed lithology) acting on the fluvial system (e.g., Whipple and
Tucker, 1999). The profile shapes reflect the long-term landscape processes. Multiple
knickpoints may propagate up a given streams profile within the span of 10 kyr. For this reason,
stream profiles are widely exploited to gain understanding about the external factors that shape
mountain belts (e.g., Kirby and Whipple 2001, Roe et al., 2002; Duvall et al., 2004)

24

25

Within the past two decades, drastic improvements have been made to the theoretical and
practical methods of stream profile analysis (e.g., Howard et al., 1994; Whipple and Tucker,
1999; Snyder et al., 2000; Whipple, 2001; Wobus et al., 2006). The evolution of a stream’s
profile is frequently modeled using the detachment-limited concept developed by Howard,
(1994), where material eroded from the channel bed is removed entirely from the fluvial system,
and bed load transport is not considered. This assumes a fluvial system consisting of bedrock
channel beds with little to no alluvium mantle. However, most alpine fluvial systems are
characterized by a range channel bed material and sediment transport processes. In the case of
the Moma Range, several channel bed properties must be considered when modeling channel
steepness, most of which can be dealt with using stream profile concavity (discussed in the
proceeding)
Using the detachment-limited concept, it can be assumed that the only controls on a
profile’s shape are uplift (or base level fall) and erosion.
𝑑𝑧
𝑑𝑡

=𝑈−𝐸

(1)

In equation (1) dz/dt represents the change of the stream’s elevation, across the entire profile
through time, U is the uplift rate, and E is the erosion rate or vertical incision rate. E can be
expressed using the vertical incision model proposed by Howard (1994):

𝐸 = 𝐾𝐴𝑚 𝑆 𝑚

(2)

where A is the drainage area in km2, S the stream’s gradient, K the erodibility coefficient of the
channel bed, and m and n are constants related to hydraulic geometry and basin hydrology. At
steady state (dz/dt = 0, i.e., when vertical incision and uplift are in equilibrium), equations (1)
and (2) can be combined and solved for S.

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1

𝑈 𝑛 (−𝑚)
( ) 𝐴 𝑛
𝐾

=𝑆

(3)

Under steady state, U, K, n, and m are constant, and so additional constants are commonly
defined:
1

𝑈 𝑛
( )
𝐾

= 𝑘𝑠

(4)

and
𝑚
𝑛

= 𝜃

(5)

substituting equations (4) and (5) into (3) to yields,

𝑆 = 𝑘𝑠 𝐴−𝜃

(6)

Equation (6), first proposed by Hack (1957), expresses a stream’s slope as a power-law function
of the contributing drainage area. The constants ks and  represent the steepness and concavity
indexes of the profile respectively. By plotting individual slope and drainage area values (black
crosses on Fig. 11) for a given interval, ks and  can be determined by measuring regressions of
distributed slope–area data in logarithmic space (y-intercept for ks and the slope for , see Fig.
10) (Snyder et al., 2000; Wobus et al., 2006). Equation (6) holds conditionally only for critical
slopes, generally less than 0.2, which represents the transition from debris-flow dominated to
stream-flow processes (Fig. 11) (Sklar and Dietrich, 1998).
In streams where the uplift and vertical incision are uniform across the entirety of the
stream's profile, one regression line (one value each for ks and ) can fit the accompanying
slope–area data below a critical slope (~0.2). Streams perturbed by external variables like

27

tectonic forcing, climate, or changes in streambed lithology, will inherently be characterized by
different values of ks and  in different segments. In this study, it is these variations that I exploit
to obtain tectonic information from the topography of the Moma Range. Using equation (6) as
the regression model, where ks and  are free parameters, regressions are fit below the critical
slope (0.2) to appropriate segments of the individual stream profiles. Those that contain multiple
regressions reflect variations in rock uplift rate, climate, and/or streambed lithology. To compare
channel steepness (ks) from profiles across different catchments, a second regression is
performed where  is fixed to a reference concavity (ref = .45), thus producing normalized
steepness values (ksn) that can be plotted geographically and compared with the values of
neighboring streams and can be used as proxy for uplift rates operating at intermediate time
scales (Wobus et al., 2006).
In equation (4) there is a direct power-law relationship between uplift (U) and channel
steepness (ks), assuming the coefficient of erosion (K) is uniform across the entirety of the stream
(Whipple and Tucker, 1999; Snyder et al., 2000; Kirby and Whipple, 2001). Profile concavity ()
is generally thought to be independent of rock uplift when spatially uniform (Tucker and
Whipple, 2002; Duvall et al., 2004); however, Kirby and Whipple (2001) used profile concavity
to mark transition zones from high to low uplift regimes across a fault-bend fold in the Siwalki
Hills of central Nepal.
Using the above technique, I modeled channel profile steepness for channels that drain
transversely across the north slope of the Moma Range in an attempt to map out the distribution
of uplift across the range. I have created three maps that focus on the Ilin’-Tas, Arga-Tas and the

28

Andrei-Tas mountains. The raw elevation data are smoothed with a 1 km long window. The
slope-area data are sampled at an interval of 40 m (the contour interval the DEM was created
from). To automate the process, normalized steepness values (ksn) were calculated using a 20 km
long moving window parallel to the entire length of the profile.
As stated earlier, the upper bounding limit of the regression analysis is the critical slope
(~0.2), while the lower limit is where streambeds are no longer over bedrock (i.e., alluvialbedded or transport-limited systems), generally when the slopes are very low and/or when
drainage area is large (Fig. 11). Commonly associated with the transition from bedrock to
alluvial channels is a negative steeping of the slope-area regressions (increase in channel
concavity), and generally a theoretically predicted range of concavity indices ( = 0.3-0.6) is
implemented to enforce the detachment-limited model (Snyder et al., 2000).

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5. RESULTS
5.1 Channel morphology
Along the Indigirka River, where it cuts through the western region of the Moma Range
(between the Andrei-Tas and Ilin'-Tas mountains; Fig. 3), the largest and most pronounced
change in channel morphology occurs. There, the river undergoes an abrupt change in thalweg
sinuosity (actual path length/shortest path length), and forms a wide meandering and channelized
geometry. The sinuosity changes from ~1.2 in the upstream segment, to ~2.82 in the channelized
segment, back to ~1.5 in the downstream segment (Fig. 12). In the channelized segment, the
Indigirka River is deeply incised along both of its banks, exposing large outcrops of the Bastakh
Group (Fig. 13).
Upstream from the sinuous segment, a series of bedrock capped terraces, over 30 km
long, are mapped along the eastern floodplain of the Indigirka (Kolpakov, 1986). Between the
eastern terraces and the river, within the floodplain, are a series of noticeable meander scars. On
the western bank of this segment, the river is banked up against the Andrei-Tas Mountains, and
no terraces are mapped along this side. Near the confluence of the Moma and Indigirka rivers
and along the lower reaches of the Ilin-Eselyach River, the major right tributary to the Indigirka,
large terraces with broad flat tops sit 200 m above the adjacent floodplains.
On the northeastern slope of the Moma Range, the changes in channel morphology are
subtle, and manifest as narrowed channel widths. Channel narrowing can be observed using the
satellite imagery along rivers of higher order (e.g., Kyllakh, Myatis, Badyarikha, and Ozhogina;
Fig. 14). The best example occurs along the Myatis River, at the border of the High Moma
Range and Zyryanka Basin (i.e., at the ITT). Here, the Myatis transitions from what a appears to
be a wide,

31

32

33

34

almost dammed-up reach into a narrow and incised 5 km long segment, and then back into a
more braided morphology as it crosses the thrust zone segment of the Zyryanka Basin (Fig. 14).
5.2 Knickpoints in stream and river profiles
The entire Indigirka watershed (~360,000 km2) contains a number of large knickpoints
located upstream from the Zyryanka foredeep. Figure 15 shows the profile of Indigirka River
together with the profiles from two of its large tributaries, the Moma and Selennyakh rivers
(constructed using the topographic maps for the elevation and Google Earth for the length
measurements), and a map showing the location of the major knickpoints. Along the Indigirka
there are three places where there is an apparent break in the slope of the profile (120 m, 400 m,
and 600 m elevation, Fig. 15). The knickpoint at the 400 m elevation on the Indigirka is possibly
linked with changes in lithology, as this is the location where the river crosses over the batholiths
of the Unyandina-Yasachnaya volcanic belt. Along the Selennyakh River, two obvious
knickpoints occur in the lower reaches, one at 240 m and another at 350 m elevation.
The Moma River contains the most pronounced knickpoint in the entire Indigirka
watershed, and it occurs at an elevation around 500 m. Upstream of this knickpoint, the Moma is
a slow, meandering channel, but as it crosses knickpoint it enters a large braided segment (~25
km long and up to 2 km wide), known as the Ulakhan Taryn. Here the channel becomes very
shallow, and during the winter months the channel freezes to its bottom and thick sheets of ice
can accumulate, leaving portions of the channel covered in ice all year. This phenomena is
referred to as a river icing, which are common in Arctic and sub-Arctic watersheds (e.g., Hu and
Pollard, 1997), particularly along wide channel segments.
It remains unclear as to what causes these knickpoints. The rivers shown in figure 15 are
all large rivers, and they have multiple ways to adjust their channels (e.g., channel narrowing or

35

36

changing sinuosity) to accommodate external forces like tectonic uplift. However, the Moma and
Selennyakh rivers make up the major drainages of the Moma-Selennyakh depression, and the
knickpoints along these streams are at similar elevations and distances from their confluence
with the Indigirka River. This suggest a possible transient link between knickpoints in these
tributaries and base-level changes occurring at the lower reaches if the Indigirka River as it
crosses the Zyryanka foredeep.
Knickpoints in rivers draining the northern slope of the Moma Range are more subtle
than in the large tributaries of the Indigirka. The profile of the Kyllakh appears smooth and
unperturbed when plotted along and at the same scale with the larger rivers (Fig. 15), but upon
closer examination the profile of the Kyllakh exhibits a large, concave shaped knickpoint just
before the Kyllakh enters the Zyryanka Basin. This is one of the largest knickpoints within the
north slope streams. The knickpoint is clear in the plotted profile (Fig. 16), and the there is also a
significant jump in the trends in the slope–area plots that correlate with the position of the
knickpoint. Other rivers that are similar in order or drainage area (e.g. the Myatis River Fig. 17)
do not exhibit large knickpoints, and the knickpoints found along these streams appear subdued.
Knickpoints are more common in streams with smaller order, but remain difficult to identify
(Fig. 18).
Many of the streams in the eastern regions of the Moma Range, in the Arga-Tas
Mountains, display knickpoint clusters that are significantly upstream from border between the
High Moma Range and the thrust zone of the Zyryanka Basin (e.g., Sibik River, Fig. 19). A
northwest-southeast linear trend in the knickpoint locations exists along the upper reaches of a
group of streams that originate along Taskan Ridge (north of the Dalekaya River, Fig. 22). The
only major knickpoint found in the streams of the western regions, the Andrei-Tas Mountains,

37

38

39

40

41

42

occurs along the Susukmyakh River. The knickpoint is at an elevation of ~500 m (Fig. 20), right
at the topographic front and the westward continuation of the ITT. Behind this knickpoint is what
appears to be a subsequent series of smaller knickpoints; however, these are artifacts of
processing from when the elevation data were extracted to construct the profile. Stair-step
artifacts like these are common in profiles extracted from DEMs that were built from
topographic maps. By going back and referring to the topographic maps, I was able to
distinguish between the major real knickpoints, like the one in the Susukmyakh River, and stairstep artifacts.
5.3 Normalized steepness indices (ksn)
The magnitudes of the normalized steepness indices for the channel reaches analyzed
using the automated approach are plotted as a color-coded maps in figures 21, 22, and 23. These
three maps also show the geographical locations of the major knickpoints indentified in this
study. The major faults in the thrust zone of Zyryanka Basin, including the ITT and MTF, are
shown as a series of black lines that trace along the northern foothills of the Moma Range. The
ksn data are classified into five groups, with values >80 and <20 representing the high and low
ends of the spectrum respectively. The stream segment with the highest individual ksn value is
the upper reach of a right tributary to the Zyryanka River in the Arga-Tas sub-province (126.3).
The second highest ksn value (116) occurs along the Kyllakh River, in the segment that includes
the major knickpoint (Fig. 16).
In general, channels with larger drainage basins, that have headwaters in the highest
regions of the Moma Range have higher ksn values in comparison to the small streams that are

43

sourced in the foothills. There is also a concentration of high ksn values in the Ilin'-Tas
mountains; centered around the region near the Myatis River (Fig. 21).

44

45

46

47

6. DISCUSSION
The Moma Range is a Cenozoic fold-and-thrust belt, with vergence to the northeast (e.g.,
Gaiduk et al., 1990). Many questions remain regarding its architecture and its deformation
history, but here I focus on how the fold-and-thrust belt is currently deforming based on the
geomorphic indicators. The traditional view of fold-and-thrust belt development consists of a
break-forward sequence model, where thrust faults form in-sequence, one after another, initiating
in the hinterland and progressing towards the foreland (Davis et al., 1983). If the Moma Range is
an actively deforming fold-and-thrust belt, it may be expected that all the current tectonic strain
on the Moma Range is accommodated by shear along the frontal thrust, the Myatis thrust fault
(MTF); however the data from this study suggest that the portions of the Moma Range are
deforming out of sequence, and that thrusting is or recently has been focused along the Ilin’-Tas
thrust (ITT).
6.1 Interpretation of geomorphic data
The big jump in thalweg sinuosity of the Indigirka River and its abrupt change in channel
morphology as cuts across the interior of the Moma Range, is a clear indication that the Moma
Range, in that location, is undergoing uplift. In this case, uplift is triggering an increase in valley
slope along Indigirka's channel, and as a consequence the river adjusts its sinuosity to
compensate for the change in slope. The change in uplift also causes the channel to incise itself
into the landscape, forcing the river into a single channel with steep terraces on both sides. Based
on geologic maps (Surmilova et al., 1986), there is no major change in stream bed lithology, and
no major tributaries confluence here; leaving a zone of active uplift as the likely candidate for the
abrupt change in channel morphology. Bullard and Lettis (1993) drew similar conclusions by
observing sinuosity changes in rivers that perpendicularly cross axes of actively growing

48

anticlines associated with blind-thrust in the Los Angeles basin in southern California. The
sinuosity changes measured by Bullard and Lettis (1993) are much smaller in magnitude (~1.06
to 1.24) than the changes measured here (~1.2 to 2.82).
The upstream segment of the Indigirka is characterized by a long sequence of terraces
along the eastern floodplain (Fig. 12). I propose that these were formed at an earlier time, when
the sinuous portion of the Indigirka was perhaps further upstream (southward). The active zone
of uplift may have initiated further back, and the progression of Moma Range deformation and
uplift has recently propagated northward. Alternatively, the uplift could be recent and initiating
in its current locality with the terraces forming as pre-uplift features; however, timing of such
phenomena are currently unconstrained. The meander scars that favor only the right bank of the
Indigirka is an indication of an additional westward tilting of the valley floor. Alexander et al.
(1994) used similar patterns of meander scars along the Madison River in southwestern Montana
to document the direction of tilting of an extensional fault block triggered by the 1959 Hebgen
Lake earthquake.
Channel morphology changes for the rivers that transversely drain the north slope of the
Moma Range are more difficult to identify. These rivers have much lower stream power
therefore making it difficult to cut and erode the landscape, and in turn change their channel
morphology. However, several of the higher order streams appear to narrow their channels for
short segments (~5 km) near the vicinity of the ITT (Figs. 14 and 21), the bounding fault
between the High Moma Range and the Zyryanka thrust zone. These larger rivers are likely
gravel bedded in many locations, and when crossing growing folds or zones of differential uplift,
alluvial rivers tend to narrow their channels before steepening of the channel occurs (Amos and
Burbank, 2007). I suggest that the narrowing of channels is triggered by the active or very recent

49

differential uplift at the ITT, caused by active thrusting of High Moma Range over the Zyryanka
thrust zone.
Knickpoints at these narrowed channel segments are not observed; except for along the
narrowed segment of the Kyllakh River, where a large, convex shaped knickpoint is present (Fig.
16). Most of the knickpoints identified in this study occur along low-order channels, and many of
them are upstream of the ITT (Figs. 20 and 21), suggesting that vertical displacement along the
ITT has at least very recently perturbed the streams that cross it. The knickpoints observed in the
large-scale Indigirka profile plot (Fig. 15) may represent the oldest record of base-level fall,
caused by the initial subsidence in the Zyryanka foredeep.
In the Arga-Tas Mountains of the Moma Range (Fig. 3), a distinct trend of knickpoints
occurs along the northeastern slope of the Taskan Ridge (Fig. 22), and the Yugyun River
narrows its channel as it crosses the ridge. These results suggest that there is a significant amount
of deformation ongoing within the High Moma Range, several tens of kilometers inward from
the deformational front, the MTF. The Taskan Ridge is ~20 km south of the topographic front of
the eastern Moma Range, where Gaiduk et al. (1993) have extended the ITT. Many of the
structures mapped in the Arga-Tas mountains are poorly constrained by field observation, so my
interpretations of the geomorphic indicators should be treated as a preliminary conjecture.
The spatial distribution of ksn values in the Moma Range is not totally clear, but higher
values appear concentrated the central portions of the Moma Range, centered around the vicinity
of the Myatis River and the Ilin’-Tas Mountains (Fig. 21). I interpret this as a result of long-term
(10 kyr to 300 kyr) sustained uplift rates in this location. In addition, streams sourced from the
High Moma Range, south of ITT, have higher ksn values assigned to their profiles; while streams
sourced north of the fault, in the northern foothills, have lower ksn values. These changes from
50

high to low channel steepness could be an implication that uplift rates from south to north are
broken by a distinct structural boundary. An alternative interpretation is that uplift rates are
gradational from high to low elevations. The geomorphic indicators, particularly the narrowed
channel segments on the Myatis and Kyllakh rivers (Fig. 14), corroborate the notion that ITT
represents a boundary between high and low uplift regimes across the Moma Range, in turn
suggesting that portions of the fold-and-thrust belt are subject to out-of-sequence deformation.
6.2 Earthquakes in the Moma Range
Seismological studies in northeast Russia (e.g., Parfenov et al., 1988; Cook et al., 1986;
Fujita et al., 2009) and in many other tectonic plate boundary regions, use earthquakes as a major
strain indicator along plate boundaries or plate boundary zones. Over fifty events have been
recorded in the Moma Range fold-and-thrust belt, but most of the events are smaller than mb 3.0
(Fujita et al., 2009; Mackey et al., 2010). Only a few events have exceed mb 4.0: one mb 5.0 in
Ilin’-Tas Mountains (144, 67; Figs. 21 and 24), two mb 4.0 events in eastern foothills of the
Arga-Tas Mountains, and three large events distributed within western foothills of the AndreiTas Mountains, with moment magnitudes (Mw) 6.6, 6.1 and 5.3 (Figs. 23 and 24). The
geomorphic indicators that coincide with the active out-of-sequence thrust structures (i.e. the
ITT), are loosely coupled with any sort of seismicity. But epicenters and depth estimates of
individual events are limited by the seismic network currently in place in northeast Russia, and
thus are poorly constrained. In addition to this, many of these events likely occur along thrust
ramps in the shallow (< 15 km) sedimentary cover, hindering the use of teleseismic data to
obtain reliable epicenters and magnitudes (Jackson, 1980).

51

52

The magnitude of shallow seismic events in thrust ramps from fold-and-thrust belts can
range between moderate to large (5.0 < Mw < 7.5) (Namson and Davis, 1990), and their
distribution and magnitude are thought to be strongly controlled by basal friction along a
decollement (Koyi et al., 2000). Only three events of moderate to large magnitude have been
recorded teleseismicly in the Moma Range, the three large events in the Andrei-Tas Mountains,
all have compressional moment tensor solutions (Figs. 23 and 24). This could indicate that this
portion of the fold-and-thrust belt is accommodating more of the convergence, that it is the most
currently active portion, or that it could be related to lateral differences in decollement strength.
Koyi et al. (2000) demonstrated that fold-and-thrust belts shortened above a frictional
decollement tend to have larger magnitude earthquakes that take place along short-lived thrust
ramps within narrow seismic zones. A frictional decollement is realistic for the Moma Range, as
rocks that constitute weak decollements, rock salt and mudstone, are absent from the regional
stratigraphy. Slip along thrust ramps connected to a frictional decollement might explain why the
large earthquakes occur in a focused area (Andrei-Tas Mountains). The structures in the central
and eastern portions of the fold-and-thrust belt may have been short lived, during a time before
instrumental seismology, but active in the very recent geologic past (<10 kyr). This could explain
why the ITT in the central and eastern portions of the Moma Range has a strong geomorphic
signal, but is absent of large-magnitude earthquakes. This would suggest that the earthquake
recurrence rate is slow and that the eastern portions of the Moma Range have not ruptured within
instrumental seismology timeframe.
Alternatively, the differences in epicenter distribution across the fold-and-thrust belt are
possibly related to the lateral changes in decollement strength. In this case, the western portion
has the larger-magnitude earthquakes because it is deforming above a frictional decollement.

53

Conversely, the central and eastern portions of the fold-and-thrust belt lack large-magnitude
earthquakes and appear to be deforming out-of-sequence/internally. Out-of-sequence thrusting is
known to be maintained in fold-and-thrust belts deforming above weak decollements (Koyi et
al., 2000). In this scenario, active displacement along both the major bounding faults of the trust
zone, ITT and MTF, would be expected and possibly taking place aseismically. More detailed
stratigraphic and geophysical studies that target the nature and characteristics of the decollement
below the thrust ramps of Moma Range are needed to test these models.
6.3 Mechanisms for out-of-sequence deformation
No mechanistic model currently exists to explain the occurrence of active thrusting in the
Moma Range fold-and-thrust belt, so the material discussed here is preliminary and speculative. I
apply the critical taper theory proposed by Davis et al. (1983) where the deformation of the
Moma Range is comparable to that of a Coulomb wedge (e.g., a sand wedge) pushed by a
backstop. In the early stages of development, during collision between the Siberian Craton and
the Kolyma–Omolon superterrane, the wedge (i.e., the sedimentary cover referred to as the Ilin’Tas assemblage) deforms internally by forming a complex series of folds, the Ilin’-Tas
Anticlinorium (Parfenov, 1991). As a consequence of folding, the wedge increases its surface
slope until it reaches a certain critical taper (the surface slope angle plus the dip of the
decollement). Internal friction builds up in the wedge and it overcomes the coefficient of friction
along the decollement, and the wedge slides forward as a whole forming frontal thrust at the
outer edge. This is probably what happened during Cretaceous to early Cenozoic deformation of
the Moma Range (Prokopiev, 2000; Fridovsky and Prokopiev, 2002). What occurs after this
stage in the Moma Range remains unknown.

54

Gaiduk et al. (1993) showed that the frontal thrust, the MTF, displaces the Early
Cretaceous Zyryanka Series on top of the Eocene to Miocene Myatis Series (Fig. 5). Many of the
Russian authors (e.g., Ivanov, 1985; Grinenko et al., 1999) cap the thrusting under a Late
Miocene and Pliocene unconformity that is found at the base of the Kyllakh formation (Fig. 5),
but convincing field evidence that shows truncation of the thrust by the unconformity is missing.
One interpretation is the sediments of the Kyllakh formation were deposited in the form
syntectonic strata in front and on top of the growing Zyryanka thrust zone.
Results from this study show that the central and eastern portions of the fold-and-thrust
belt are currently (or very recently) deforming out-of-sequence. Davis et al. (1983) demonstrated
that out-of-sequence deformation occurs as a consequence of decreasing the surface slope of the
Coulomb wedge, typically by means of erosion. However, out-of-sequence deformation is now
common in many fold-and-thrust belts, and is not exclusively linked to erosion. Conditions such
as weak decollements (Koyi et al., 2000; Nieuwland et al., 2000), syntectonic sedimentation
(Storti and McClay, 1995), and extensional collapse (Willett, 1992) can all decrease the surface
slope the deforming wedge, in turn causing out-of-sequence thrusting.
In the case of the Moma Range, the surface slope of the wedge was possibly lowered
below its critical taper during the Late Eocene to early Pliocene. At this time, convergence
between the North American, Eurasian, and Okhotsk plates reached a standstill, potentially
caused by the southward migration of the NA–EU pole of rotation as proposed by several
authors (e.g., Cook et al., 1986; Parfenov, 1988; Fujita et al., 1990; Merkouriev and DeMets,
2008). This would have been coupled with removal of wedge material by erosion, decreasing the
surface slope angle. The repositioning of the rotation pole to its current northern location, has

55

reinitiated convergence in the region, triggering crustal shortening that is accommodated in the
wedge’s interior (the High Moma Range) by out-of-sequence deformation.
Out-of-sequence deformation in the north slope of Moma Range has not previously been
suggested, but the results of my geomorphologic analysis are similar to those recently reported in
studies of out-of-sequence thrusting in the Himalayan fold-and-thrust belt. Contrary to the
traditional model of deformation in the Himalaya, Wobus et al., (2003, 2005, 2006) invoke a
locus of active deformation well north (~100 km) of the traditional deformation front, the Main
Frontal Thrust. Their findings are based on knickpoints observed in stream profiles (Wobus et
al., 2003, 2006), field mapping of deformational and geomorphic features (Hodges et al., 2004),
discontinuities in thermochronologic data (Wobus et al., 2003), and elevated erosion rates
(Wobus et al., 2005). The zone of deformation proposed by these authors coincides with a strong
precipitation gradient, presumably triggering a narrow zone of enhanced erosion, and thus a
dynamic feedback relationship between climate and tectonics (Wobus et al., 2003, 2005; Hodges
et al., 2004).
An alternative analog for the out-of-sequence thrusting in the Moma Range is the Zagros
fold-and-thrust belt in Iran. There, the out-of-sequence thrusting is controlled by lateral
differences in decollement strength that separate the northwestern and southeastern portions of
the fold-and-thrust belt (Koyi et al., 2000 and references therein). In the northwest part of the
Zagros (strong decollement) the epicenters of moderate to large-magnitude earthquakes occur
within a narrow zone, along thrust ramps at the outer edge of the fold-and-thrust belt (Koyi et al.,
2000). In the southeast (weak decollement), the earthquakes are spread out over a broad zone,
and the large-magnitude earthquakes are restricted to displacements along the deep-seated
basement faults (Ni and Barazangi, 1986; Jackson and McKenzie, 1984).

56

The out-of-sequence deformation in the Moma Range fold-and-thrust belt differs from
that of the Himalaya and the Zagros because it is possibly linked to a complex middle Cenozoic
history, where the regional convergence has been switched on and off. There appears to be no
dynamic feedback between climate and tectonics, and variations in decollement strength are
speculative at this time, although neither scenario should be ruled out. The Cenozic evolution of
the Moma Range fold-and-thrust belt, is complicated by the potential existence of a continental
rifting event, the Moma Rift (e.g., Grachev, 1982; Fujita et al., 1990; Franke et al., 2000;
Tschegg et al., 2011). The evidence supporting the Moma Rift is the series of topographical and
structural depressions (e.g., the Moma-Selennyakh depression, Fig. 3) that trend northwestsoutheast behind the Moma Range. In addition to the surface expression of the rift, is the
presence of the hot springs (Grachev, 1982), Cenozoic volcanism (Tschegg et al., 2011), elevated
heat flow measurements (Duschkov and Sokolova, 1985), and regionally lower crustal thickness
(Parfenov, 1988; Mackey et al., 1998). While Russian authors originally argued for a modern
continuation of the Gakkel Ridge from the Arctic into and actively rifting Asian continent, many
authors have confirmed that rifting was aborted in the Pliocene, when extensional forces changed
to compression (e.g., Cook et al., 1986; Parfenov et al., 1988; Fujita et al., 1990; Franke et al.,
2000). Tschegg et al. (2011) obtained six 40Ar/39Ar plateau ages from the Rudich basanites
(volcanic rocks commonly associated with continental rifting) that yield ages ranging from
36.0 ± 0.8 to 38.3 ± 0.6 Ma (middle Eocene). They conclude that the extrusion of the Rudich
basanites possibly represents the onset of continental rifting and the continuation of Gakkel
Ridge extension into the Asian continent. However, there is a discrepancy between onset of
volcanism (middle Eocene, Tschegg et al., 2011) and the presumed southward migration of the
NA-EU rotation pole (middle Miocene, e.g., Merkouriev and DeMets, 2008). Regardless of this

57

discrepancy, continental extension, via rifting, likely had a profound effect on the thickness of
the wedge (i.e., the Moma Range fold-and-thrust belt).
With the slow convergence rates (<10 mm/yr) between North America and Eurasia in the
region, it might take millions of years for the fold-and-thrust belt to build up enough internal
deformation to regain its critical taper, and resume the break-forward sequence, where slip
displacement is focused on thrust ramps at the outer edge of the of the fold-and-thrust belt (i.e.,
along the MTF or faults further out in the foreland). This is not to say that all portions of the
Moma Range are currently deforming internally, but that there might be lateral variations in
where the deformation takes place. In the foothills of the Andrei-Tas Mountains, the largemagnitude earthquakes are probably occurring because of displacement along a frontal thrust
ramp equivalent to the MTF. The epicenters of those earthquakes do coincide with a topographic
front and possible westward continuation of the ITT (Fig. 24); however, with the depth of these
events (~10 km) factored in, they are likely associated with structures that meet the surface far
out in the foreland. But the results presented in this study should not be ignored. There is clearly
a connection between the geomorphic indicators and the very recent displacements in the central
portions of the fold-and-thrust belt along ITT, an out-of-sequence thrust fault. These contrasting
styles of deformation along-strike could be attributed to number of limiting factors (e.g., original
wedge thickness, variations in decollement strength, erosion patterns, syntectonic
sedimentation), but without further geological and geophysical data, many of these questions will
remain unanswered.
6.4 Limitations of the analysis
There are two primary issues that limit the reliability of this study: the resolution of the
raw data (topography and satellite imagery), and the shortage of ground-truthing geological and

58

geophysical data. The resolution of the topographic and the satellite data limits how much detail
can be retained in the geomorphic analysis. Knickpoints and changes in channel morphology
might go totally unnoticed. The largest deficiency in the raw data is the low resolution of the
topographic maps that the DEM was constructed from. They are currently mapped at 1:200,000
with a 40 m contour interval. This means that there is roughly 130 ft. between contour lines, a
vertical distance represented by thirteen contours on the 1:24,000 topographic maps of the
contiguous US. Higher resolution elevation data with global coverage has become more readily
available to the public in past couple of years, in particular, the ASTER Global Digital Elevation
Model (http://www.jspacesystems.or.jp/ersdac/GDEM/E/index.html). It provides a 30 m
resolution for nearly the entire globe, but using this data requires additional processing to fix the
anomalies and artifacts within the raw data. Increasing the spatial resolution of the elevation data
will greatly enhance future remote sensing research in northeast Russia.
There are still a few unknowns associated with the channel steepness index (ksn). The
largest assumption made is that K, the erosion coefficient from equation 2, is uniform throughout
the Moma Range, and that ksn is a direct consequence of rock uplift rates. However, Duvall et al.
(2004) noticed from their field site in coastal California, that rock uplift rates vary between ~.75
and ~5 mm yr-1, a six- to seven-fold difference, but only a twofold differences in ksn values were
observed (~13.8 to ~26.1). They suggest this ambiguity is the result of a channel’s tendency to
narrow its width with increased rock uplift, and thus changing the K with respect to rock uplift.
For this reason, I looked for narrowed channel segments as the rivers crossed the major faults,
and with a better satellite image resolution (or access to aerial photographs) more narrowed
channel segments might be visible.

59

The biggest challenge in using remote sensing in a poorly studied, tectonically active
region like northeast Russia, is the difficulty in ground-truthing the observations derived from
the remotely sensed data with geological and geophysical data. For example, the erosion
coefficients, K, discussed in the last paragraph are poorly constrained because no data exist on
the strength of channel bed lithology. With no fieldwork to the region, I cannot confirm whether
the changes stream behavior (e.g., channel steepness, knickpoints, or channel morphology) are
truly a function of rock uplift or channel bed lithology. Furthermore, detailed the geological data
are only available for a very small area within the fold-and-thrust belt, primarily in the Myatis
River region (Gaiduk and Prokopiev, 1999). Having the opportunity to go in the field and map
faults and potential shear zones within the fold-and-thrust belt would constrain some of the
uncertainties associated with the geomorphic indicators and improve the mechanistic model
presented in this research.
The last of the major limitations are uncertainties in the subsurface of the Zyryanka
foredeep. Very few wells have been drilled there and even fewer seismic lines cross it.
Regardless, none of the subsurface data is yet available to western scientists. Much of what is
known about the foredeep is derived from gravity surveys (Parfenov, 1988), but these data are
out of date and of poor resolution. A geomorphic approach to finding active structures only
records processes that occur on the surface. There may be active structures that are buried
beneath the alluvial plane of the foreland, but without the ability to image such structures and
their exclusion from the geomorphic analysis, forces them to remain unaccounted for.
6.5 Future Research
Future research needs to be field focused. One approach to resolve some of the problems
presented in this research would be to conduct a low-temperature thermochronology transect

60

across the fold-and-thrust belt. By sampling within the individual thrust sheets and applying
40

Ar/39Ar, fission track and (U-Th)/He techniques to the minerals found within the sedimentary

rocks, the timing and rates of uplift associated with the growth of the Moma Range could be
established, thus verifying or repudiating the results from this preliminary study. Fieldwork
would also afford the opportunity to map out the major thrust structures and help establish a
better structural framework for the Moma Range fold-and-thrust belt.

61

7. CONCLUSIONS
The results from this research suggest that the Moma Range is an actively growing foldand-thrust belt that accommodates some convergence between North America, Eurasia, and
Okhotsk. Uplift of the fold-and-thrust began in the Late Cretaceous, after the closure of the
Oimyakon Ocean and the onset of the Verkhoyansk-Kolyma Orogen (VKO) (Parfenov, 1991).
Uncertainties remain about the fold-and-thrust belt’s Cenozoic history, but convergence
presumably paused during a middle Cenozoic continental rifting episode, the Moma Rift (e.g.,
Tschegg et al., 2011). The northward migration of the North American—Eurasian pole of
rotation (Cook et al., 1986), reestablished thrusting in the Moma Range during the Pliocene
(Gaiduk et al., 1993).
In an analysis of DEM and satellite data, I studied the geomorphic expression of the
rivers that drain the northeast slope of the Moma Range in an attempt to identify active thrust
faults to establish a structural framework for the fold-and-thrust belt. There are three main take
home points from this research:

1. Portions of the fold-and-thrust belt are deforming internally or out-of-sequence. The
Indigirka’s abrupt change in channel sinuosity, as it cuts across the Moma Range, suggests broad
internal folding and uplift. This out-sequence deformation extends over to the central portions of
the fold-and-thrust belt, in the Ilin’-Tas Mountains (Fig. 3), where thrusting is maintained at the
topographic front of the High Moma Range, along Ilin’-Tas thrust fault (ITT). High-order
streams that cross the ITT here experience significant channel narrowing, and streams that are
sourced above the ITT tend to have steepened profiles. In the eastern portions of the fold-andthrust belt, near the Arga-Tas Mountains, deformation is possibly focused along the Taskan

62

Ridge, a structure situated within the hinterland of the fold-and-thrust belt (~20 km south of
ITT). The ITT has a strong geomorphic expression in the Andrei-Tas Mountains, but the recent
earthquakes in the region suggest that thrusting is probably maintained out in front of the foldand-thrust belt there.

2. Styles of deformation vary along strike of fold-and-thrust belt. Uplift rates, inferred from the
normalized steepness values (ksn), appear to not be spatial uniform along the fold-and-thrust belt,
but concentrated in certain localities. The heightened ksn values in the Ilin’-Tas Mountains
suggests sustained uplift rates over longer timescales (10 kyr to 300 kyr). Additionally, the
recorded seismicity varies along strike of the fold-and-thrust belt. All of the large-magnitude
thrust events have epicenters in the Andei-Tas Mountains, and this corresponds with a general
west to east decrease in seismicity along the fold-and-thrust belt.

3. Remote sensing can be used to obtaining meaningful information on the tectonics of an
inaccessible region like northeast Russia, but it needs complementary data. Without earthquakes
or previously mapped faults, the components of this research would remain largely inconclusive.
The tools used in analyzing stream profiles are still in their early stages of development, and
without higher resolution of elevation and satellite data in the Moma Range, the analysis is
limited to first-order observations; however, the results from this research provide a useful
reconnaissance for future field investigation.

A unified, mechanistic model that explains the out-of-sequence thrusting and the alongstrike variation in the fold-and-thrust belt remains incomplete. Complexities in these models are

63

probably associated with the rather rapid changes in the tectonic environment the region
underwent during the middle Cenozoic, but are also likely influenced by additional factors (such
as decollement strength or syntectonic sedimentation). These models await further field study,
additional seismic monitoring, and expanded geophysical surveys to more precisely map out the
active structures and to construct a more complete structural framework for the Moma Range
fold-and-thrust belt.

64

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