# Provenance and erosional impact of Quaternary megafloods through the Yarlung-Tsangpo Gorge from zircon U-Pb geochronology of flood deposits, eastern Himalaya

Michael Turzewski, Katharine Huntington, Alexis Licht, Karl Lang

► To cite this version:

Michael Turzewski, Katharine Huntington, Alexis Licht, Karl Lang. Provenance and erosional impact of Quaternary megafloods through the Yarlung-Tsangpo Gorge from zircon U-Pb geochronology of flood deposits, eastern Himalaya. Earth and Planetary Science Letters, 2020, 535, pp.116113. 10.1016/j.epsl.2020.116113. hal-03657017

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1 Provenance and erosional impact of Quaternary megafloods through the Yarlung-Tsangpo

2 Gorge from zircon U-Pb geochronology of flood deposits, Eastern Himalaya

3

4 Michael D. Turzewski¹*, Katharine W. Huntington¹*, Alexis Licht¹, Karl A. Lang²,³

5

6 ¹Department of Earth and Space Sciences and Quaternary Research Center, University of

7 Washington, Seattle, WA, USA

8 ²School of Earth and Environmental Sciences, Queens College, Queens, NY, USA

9 ³Graduate Center, City University of New York, New York, NY, USA

10 *correspondence to: zewski@uw.edu, kate1@uw.edu

11

12 **Key words:**

13 Megaflood

14 Himalaya

15 Zircon

16 Geochronology

17 Erosion

18

19 **Abstract:**

20 Holocene and Upper Pleistocene sediments in the eastern Himalayan syntaxis represent

21 an extraordinary record of glacial outburst megafloods in one of the most tectonically active

22 landscapes on Earth. Glacial damming and outburst floods in the syntaxis may have focused

23 erosion in the steep Tsangpo Gorge and inhibited river incision into the margin of the Tibetan
Plateau. However, few flood slackwater deposits have been studied, and it is unknown which of the hundreds of known glacial impoundments in Tibet may have sourced the floods. Here we report n=1438 new detrital zircon U-Pb data from individual ancient megaflood and historical outburst flood slackwater deposits to examine the provenance and erosive potential of these events. Detrital zircon U-Pb geochronology of megaflood deposits show that megaflood provenance is more consistent with impoundment of the Yarlung River drainage at or west of the Namche Barwa massif, than impoundment of eastern drainages along the Yigong and Parlung Rivers. Compared to active bedload in the Siang River, and historical floods within the same drainage area, megaflood samples overall contain a disproportionately large amount of zircons eroded from the Tsangpo Gorge. We interpret this preferential derivation to reflect preferential erosion during large discharge events—supporting the hypothesis that Quaternary megafloods are a primary contributor to rapid exhumation of the Eastern Himalayan syntaxis.

36

37

# 1. Introduction

The contribution of extreme events such as earthquakes, landslides, and outburst floods to the long-term erosion and landscape evolution on Earth and on Mars is debated (e.g., Lamb et al., 2008; Lamb and Fonstad, 2010; Lang et al., 2013; Perron and Venditti, 2016; Larsen and Lamb, 2016). Bedrock rivers respond to perturbations in climate and tectonics to drive landscape evolution (Whipple et al., 2013), and recent work has highlighted important connections between outburst floods of different magnitudes, bedrock incision, lateral erosion, and hillslope processes (Turowski et al., 2008; Larsen and Montgomery, 2012; Turzewski et al., 2019). However, we lack direct observations of the largest magnitude flood events on Earth and must rely on

38

39

40

41

42

43

44

45
46 numerical simulations and information about these events stored in sedimentary and geomorphic
47 archives.

48 The eastern Himalaya contains a rich geomorphic and sedimentary record of outburst
49 floods in its rugged landscape (Figure 1). Widespread geomorphic evidence records glacial
50 damming (e.g., Montgomery et al., 2004; Liu et al., 2006, 2015, 2018; Korup and Montgomery,
51 2008; Kaiser et al., 2010; Guangxiang and Qingli, 2012; Zhu et al., 2013, 2014; Huang et al.,
52 2014; Chen et al., 2016; Hu et al., 2018), and outburst megafloods with discharges >10⁶ m³/s
53 sourced from such impoundments in Tibet (Montgomery et al., 2004; O’Conner et al., 2013;
54 Srivastava et al., 2017). In addition to experiencing high peak annual flows (10⁴ m³/s; Goswami,
55 1985), rivers in the region also experience century-scale landslide-dam outburst floods (10⁵ m³/s;
56 Delaney and Evans, 2015), resulting in a high capacity for erosion throughout the Holocene and
57 Upper Pleistocene (e.g., Larsen and Montgomery, 2012; Lang et al., 2013; Turzewski et al.,
58 2019). Sediment eroded from the Himalaya during megafloods includes biospheric particulate
59 organic carbon that is deposited and buried in the Bay of Bengal, making these events relevant to
60 the global carbon budget in one of the largest river deltas in the world (Galy and Eglinton, 2015).

61 Previous workers have used detrital zircon geochronology and thermochronology as a
62 tracer for erosion in the Tsangpo Gorge (Stewart et al., 2008; Enkelmann et al., 2011; Lang et al.,
63 2013). Detrital zircon U-Pb core crystallization ages from four slackwater deposits (n=450)
64 presented in Lang et al. (2013) suggest that megafloods have a different signature of erosion on
65 the landscape than sediment traveling in the modern river bedload and sediment derived from a
66 historical landslide-dam outburst flood on the Yigong River (Shang et al., 2003; Delaney and
67 Evans, 2015), consistent with disproportionate derivation from the Tsangpo Gorge.
This intriguing result highlights the important role of megafloods in the evolution of this landscape, and demonstrates the utility of detrital zircon U-Pb geochronology as an erosional tracer for comparing the erosional impact of variable discharges within the same drainage area.

Here we expand on this work to investigate megaflood sources and variability among individual event deposits with 1438 new zircon U-Pb age data from modern/historical outburst flood and megaflood slackwater deposits. We combine these data with previously reported zircon ages for flood and fluvial deposits and source regions within the Siang-Brahmaputra drainage to examine the role of impoundment location and sediment recycling on detrital zircon U-Pb age distributions in megaflood deposits; constrain potential flood source regions in Tibet; and evaluate the hypothesis that Quaternary megafloods reflect greater preferential erosion of Tsangpo Gorge compared to what is observed in modern river flows.

## 2. Background

### 2.1 Potential source regions of megafloods through the Eastern Himalaya

Megafloods through the Tsangpo Gorge could have been sourced from any of hundreds of paleo-lake impoundments that have been mapped within the upstream drainage area in Tibet (Figure 1; Korup and Montgomery, 2008; Korup et al., 2010). The rugged pathways of the Yarlung and Po Rivers meet in between the peaks of Gyala Peri (7294 m.a.s.l.) and Namche Barwa (7782 m.a.s.l.) in the Tsangpo Gorge (Figure 1). The Yigong and Parlung Rivers are upstream of this confluence to the northeast; upstream of this confluence to the west, the Yarlung River drainage contains an extensive network of tributaries including the Nyingoh and Lhasa Rivers (Figure 1). In this paper, we refer to glacial-lake impoundments to the northeast of the Namche Barwa massif on the Yigong and Parlung Rivers as eastern Tibetan sources, and
90 impoundments at and to the west of Namche Barwa on the Yarlung River as western Tibetan
91 sources.

92 Several Holocene and Upper Pleistocene impounded paleolakes have been documented
93 on the Yarlung River, representing potential western Tibetan sources for megafloods that would
94 have traveled through the Tsangpo Gorge and into the Siang River valley in India (Montgomery
95 et al., 2004; Liu et al., 2006; Korup and Montgomery, 2008; Kaiser et al., 2010; Zhu et al., 2013;
96 Zhu et al., 2014; Huang et al., 2014; Liu et al., 2015; Chen et al., 2016; Hu et al., 2018; Liu et al.,
97 2018). Impoundment of the Yarlung River immediately upstream of Namche Barwa produced at
98 least two lakes during the last 13 ka (Figure 1). Holocene lake terraces dated at 1160-1574 cal yr
99 B.P. correlate to glacial-moraine dams near the entrance of the Tsangpo Gorge at Namche
100 Barwa, recording a ~81 km³ paleolake, the failure of which produced a flood with an estimated
101 peak discharge of 1x10⁶ m³/s (Montgomery et al., 2004). A second set of terraces dating to
102 9,997-11,285 cal. yr B.P. may correspond to a larger, 835 km³ reconstructed lake thought to have
103 produced an estimated peak discharge of 5x10⁶ m³/s in a catastrophic flood (Montgomery et al.,
104 2004). However, other terraces in the area show that this larger lake may have existed in several
105 stages at different maximum elevations (Montgomery et al., 2004; Liu et al., 2006; Zhu et al.,
106 2013; Huang et al., 2014), and various dated lacustrine sediments up to 75 ka B.P. are difficult to
107 correlate to one another (Montgomery et al., 2004; Liu et al., 2006, 2015; Huang et al., 2014).

108 Further upstream and to the west in the middle reaches of the Yarlung River there is
109 evidence of a prolonged glacial-impoundment (32.3 to 13.2 cal. ka B.P.) and resulting flood
110 above the Dazhuka-Yueju Gorge (Kaiser et al., 2010; Zhu et al., 2013; Hu et al., 2018; Figure
111 1). The catastrophic failure of this lake is supported by field evidence of coarse gravels and
112 boulders near the Dazhuka-Yueju Gorge (Hu et al., 2018); estimates of the timing of a flood
include constraints from luminescence (12.8 to 13.5 ka; Kaiser et al., 2010; Zhu et al., 2013; Hu et al., 2018) and radiocarbon dating (13.2 ka B.P.; Hu et al., 2018) of the topmost lacustrine sediments, and may be related to warming in the region during the due to the Bølling-Allerød period (Hu et al., 2018).

In addition to impoundment of the main stem Yarlung River, dams may have temporarily blocked northward flowing Yarlung tributaries upstream of the gorge (Burrard and Hayden, 1907). Zhang et al. (2016) proposed that ice dams blocking the Siqunama River may have led to localized lake spillover into the Subansiri River valley. Lake spillover into the Subansiri River valley would have been contained within a separate drainage basin southwest of our study area, and cannot explain deposition of the Siang River valley deposits samples in this study.

Hundreds of potential glacial-moraine dams have been mapped on eastern Tibetan tributaries of the Yigong and Parlung Rivers upstream of the Po-Tsangpo Gorge (Figure 1; Korup and Montgomery, 2008; Korup et al., 2010). However, exposures of paleo-lake sediments in this region are sparse and is limited to a few lacustrine terraces identified on the Parlung River, which date from 16.1 to 22.5 ka B.P. (Guangxiang and Qingli, 2012).

It is unknown whether ancient slackwater flood deposits downstream of the Tsangpo Gorge along the Siang River valley (Figure 2) record megaflood events sourced from eastern Tibetan impoundments and/or western Tibetan impoundments in the Yarlung River drainage at or upstream of the Namche Barwa massif. Here we use variations in detrital zircon U-Pb crystallization ages to discriminate between potential source regions in Tibet.

## 2.2 Constraints on source-region zircon U-Pb ages

Tectonic terrains resulting from the collision of the Indian and Eurasian plates have produced distinct patterns of zircon crystallization ages in bedrock eroded by the Yarlung-Siang-
Brahmaputra River system (Booth et al., 2004; Booth et al., 2009; Cina et al., 2009; Gehrels et al., 2011; Lang et al. 2014; Hu et al., 2018). Of the detrital zircon ages that characterize the bedrock of this region, the less than ~1000 Ma ages (Figure 3, Table 1) include contributions from Himalayan zircons (~300-750 Ma, with a peak probability density at ~490 Ma; Stewart et al., 2008; Cina et al., 2009; Amidon et al., 2005); Tibetan zircons (<300 Ma; Cina et al., 2009; Zhang et al., 2012); and anatectic zircons from Himalayan rock of the Namche Barwa massif/Tsangpo Gorge specifically that are distinguished by their young crystallization ages (<30 Ma; Booth et al., 2009) and high U/Th ratios (>10; see Lang et al., 2013).

Previously published detrital zircon data from the source region (n=2299) are summarized in **Figures 1-4**, and **Tables 1 and 2**. Western Tibetan sources are characterized by detrital zircon ages from the main trunk of the Yarlung River and its tributaries (Figure 3). Main trunk Yarlung River samples west of the Tsangpo Gorge are generally dominated by a narrow ~50 Ma age peak representing Paleogene igneous rocks; a few 100-220 Ma zircons sourced from Cretaceous to upper Triassic volcanic and sedimentary rocks; and a minor component of 400-750 Ma zircons from Paleozoic to late Proterozoic rock of the Greater Himalayan Sequence south of the Indus-Tsangpo suture, sourced from tributaries that flow north into the Yarlung River (Stewart et al., 2008; Cina et al., 2009; Zhang et al., 2012). We note that while ~50 Ma zircons are generally diagnostic of western Tibetan sources due to their abundance in Yarlung River samples, zircons in this age range may also be sourced from transhimalayan plutonic units northeast of the gorge (Zhang et al., 2012; Lang and Huntington, 2014). Age distributions of tributaries to the Yarlung River farther upstream in the middle reaches of the drainage are more variable, and generally contain age peaks <250 Ma as well as contributions of ~500-750 Ma zircons plus or minus other age components. Zircon ages from the Tsangpo Gorge and Namche
Barwa massif have two peaks at 27 Ma and 490 Ma (Booth et al., 2004, 2009; Zhang et al., 2012). Cenozoic ages reflect anatectic zircons with U/Th ratios >10 (Lang et al., 2013) whereas 490 Ma ages reflect recycled ages derived from Indian crust. Zircons from tributaries entering the Gorge through the Po River from eastern Tibetan sources are mostly ~100-220 Ma in age, with some ~45-75 Ma and few >220 Ma zircons.

## 2.3 Detrital zircon U-Pb geochronology of modern Siang River sediments and historical outburst flood deposits

Detrital samples from the Siang River integrate the Tibetan and Himalayan source age distributions described above (Figure 2, 4). Most zircons from samples representative of the modern Siang River are distributed between 50 Ma and 350-550 Ma (Stewart et al., 2008; Lang et al., 2013). These authors argued that the large proportion of 350-550 Ma zircons (~47%) from just 2% of the total upstream drainage reflects localized, extreme erosion of the Tsangpo Gorge area.

Zircon age distributions of slackwater deposits from the 2000 Yigong River landslide-dam outburst flood sampled up to 30 m above the Siang River channel by Lang et al. (2013) differ slightly from those of modern Siang River sediments (Figure 4). The youngest age peak in these Yigong flood deposits is ~66 Ma, older than the ~50 Ma peak that characterizes Yarlung River source samples and modern Siang River detritus. The Yigong flood deposits also contain 350-550 Ma Himalayan-age zircons like the modern Siang River samples, and ~100-220 Ma zircons representing the Yigong River age signature (Figure 3).

Detritus from four ancient megaflood slackwater deposits sampled up to 150 m above the modern Siang River channel by Lang et al. (2013) (n=450) contains more ~350-550 Ma zircons
that are characteristic of the Tsangpo Gorge compared to the modern Siang River and Yigong flood samples (Figure 4). Based on forward mixture modeling of these and previously published source-region zircon, Lang et al. (2013) argued that megafloods disproportionately focused erosion in the Tsangpo Gorge compared to these smaller magnitude flows. Building on this previous work, we sampled and analyzed additional flood deposits in the Siang River valley to explore the potential influence of flood provenance, erosion, and sediment recycling on detrital age signals.

## 3. Methods

### 3.1 Slackwater flood deposit identification and sample collection

The n=1438 new detrital zircon U-Pb data reported here come from two historical landslide-dam outburst flood samples, one reported here for the first time and one described by Turzewski et al. (2019), and seven new ancient megaflood samples described here for the first time (Figure 2; Table 2). All samples were collected in northeast India during fieldwork performed in 2013. Sample locations for these deposits, as well as previously published samples of Lang et al. (2013) are shown in Figure 2 and Table 2.

Flood deposits were distinguished from fluvial and landslide deposits based on their sedimentary features and position, following Lang et al. (2013) and Turzewski et al. (2019). Ancient flood deposits are exposed in roadcuts above the Siang River and near major tributaries that inundate during floods. One slackwater deposit from the 2000 Yigong flood that was identified in a previous field season was observed in 2013 to have been covered by a small landslide, illustrating a mechanism by which ancient flood deposits may be preserved in this
rapidly eroding landscape. In several locations, deposits from multiple megaflood events were located in stratigraphic succession, in some cases separated by landslide deposits.

We analyzed zircons from two slackwater flood deposits interpreted to represent deposition from historical landslide-dam-break outburst floods on the Yigong River (e.g., Delaney and Evans, 2015). The 2000 Yigong flood sample (13SI18) was mapped by Turzewski et al. (2019) 48 m above the modern river at low flow. This deposit is composed of laminated fine to medium grain sand, shows no signs of soil development, and has small <0.5 m vegetation growth on top. Sample 13SI17 is from a laminated deposit with similar grain size, that is located on a surface 1-2 m lower in elevation than the 2000 flood deposit and is capped by thick vegetation including a ~40 cm diameter jackfruit tree at least 50-70 years old. The age of this tree and the characteristics of this deposit suggest deposition by the 1900 Yigong River outburst flood (Figure S2).

The seven new megaflood deposits (Figure 2) are located 72-381 m above the modern Siang River level at low-flow. The highest deposit (13SI02) exposure is approximately 90 m long and 6 m thick, making it the largest deposit identified in the field (Figure S3). Samples 13SI21 and 13SI40 are from deposits on terraces >70 m above the river level exposed in roadcuts and are 1-2 m thick (Figure S4; S5). The remaining samples are from vertical sequences of slackwater megaflood deposits separated by landslide colluvium (Figure S6). Three of the deposits (13SI28, 13SI32, 13SI34) are 96-163 m above the river on a series of terraces near Nubo Bridge, which was destroyed during the 2000 Yigong flood (Figure S7; S8). For reference, at this location, deposits from the 2000 Yigong flood are located at 35 m above the river level.

## 3.2 Detrital zircon sample preparation and U-Pb geochronology
For each sample, approximately 1-2 kg of fine-medium sand was processed with standard mineral separation techniques. Samples were sieved to isolate the 80-250 µm size fraction, which is a size-range that is typical of the sand observed in deposits (Table 2). Zircons were separated with a Wilfley table, lithium polytungstatye and diiodomethane heavy liquids, and a Frantz magnetic separator. Although the Wilfley table and magnetic separator are a standard method to extract zircons, we note that they may introduce bias (Sircombe and Stern, 2002; Vermeesch et al., 2017). Zircons were mounted, polished, and imaged with backscattered electron imaging (Hitachi 3400N SEM) at the University of Arizona. Zircon cores were analyzed for U-Th-Pb geochronology with laser ablation multi-collector inductively coupled mass spectrometry (LA-MC-ICPMS) using a 30 µm spot diameter at the Arizona LaserChron Center (Gehrels et al., 2011). U-Pb age data were reduced using NUPMagecalc and ISOPLOT using standard age filters. Additional information about preparation, analysis, and reduction of data is available in Pullen et al. (2014).

## 3.3 Statistical analysis of detrital provenance

We compared zircon U-Pb age distributions from the new and previously published samples using a variety of statistical methods. Zircon age distributions are presented as kernel density estimates (KDE) fitted with automatic selection of bandwidth (Botev et al., 2010). We also used multidimensional scaling (MDS) to quantify similarity among the age distributions of different samples (Vermeesch, 2013); this method has shown to be a useful tool for examining similarity in detrital datasets in a variety of geological applications (e.g., Vermeesch, 2013, 2015, 2017; Licht et al., 2016; Makuluni et al., 2018). Detrital provenance was further investigated via Bayesian inversion of zircon age distributions, which uses the information in the downstream detrital sample to search for age components and their characteristics.
250 Inversions were performed with BayesMix software (Jasra et al., 2006; Gallagher et al.
251 2009), which has been used by previous workers to distinguish tectonic terrains and analyze the
252 provenance of loess and paleosol deposits (e.g. Licht et al., 2016; Perrot et al., 2017). BayesMix
253 uses a reversible jump Markov chain Monto-Carlo (RJ-MCMC) sampling strategy to select the
254 age, width, and number of individual components, and the proportion of each component present
255 in sample age distributions. We ran BayesMix with 20,000 iterations assuming heavy skew-t
256 distributions for priors and compared the age, error, and proportion of all components from each
257 sample. The inversion was performed on compilations of detrital zircon data from geologically
258 equivalent deposits recording the same event/processes including five 2000 Yigong outburst
259 flood deposits (n=387), and four modern Siang river samples (n=356). We performed inversions
260 on a compilation of all 11 megaflood deposits (n=1608) and on sub-groups of similar megaflood
261 samples.
262

262

263 **4. Results**

264 **4.1 Detrital zircon U-Pb geochronology results**

265 Zircon U-Pb data from the n=1438 new analyses presented here are available in **Table S1**
266 of the supplementary information. **Figure 4** presents zircon age distribution KDEs for seven new
267 and four previously reported megaflood samples (Lang et al., 2013); one new 1900 Yigong flood
268 sample; the 2000 Yigong flood sample compilation (data from Lang et al. (2013) and sample
269 13SI18 from this study); and the compilation of modern Siang River sample data (Stewart et al.,
270 2008; Lang et al., 2013).

271 All megaflood deposits have a ~490 Ma age peak corresponding to the prominent age
272 peak in the Namche Barwa/Tsangpo Gorge source sample (Figure 3, 4). The relative magnitude
of the ~490 Ma peak, as well as the position, width, and relative magnitude of the youngest age peak varies among deposits. Four of the megaflood deposits (group 1) have a youngest age peak at ~50 Ma (Figure 4a, b), corresponding to the youngest age peak observed in western Tibetan source samples along the main trunk of the Yarlung River (line 1 in Figure 3); a fifth sample (08KH24; Figure 4b) has a similar youngest age peak that is broader and relatively smaller than those of the other samples in group 1. Three of the deposits (group 2) have a youngest age peak (Figure 4c) that matches the ~27 Ma youngest age peak in the Namche Barwa source sample that represents anatectic zircons (Figure 3, 6). Three deposits (group 3) have youngest age peaks in the ~25 to 65 Ma range and also contain prominent age peaks from ~100-220 Ma (Figure 4d) that may correspond to eastern Tibetan sources of the Yigong and Parlung Rivers or tributaries of the middle-reaches of the Yarlung River to the west (Figure 3).

The new 1900 Yigong flood sample and updated 2000 Yigong flood sample compilation share an age peak at ~490 Ma similar to the megaflood samples, but have a youngest age peak around ~66 Ma with positive skew toward older ages (Figure 4e). When the new megaflood sample data are combined with the previously published megaflood zircon data of Lang et al. (2013), the compiled dataset support the previous hypothesis that megaflood sediments contain more zircons from the Tsangpo Gorge (bar 3) compared to the modern Siang River and 2000 Yigong flood sample compilations (Figure S9).

## 4.2 MDS similarity results

The MDS map (Figure 5) plots dissimilarity among detrital samples representing source areas in Tibet and the Tsangpo Gorge, modern Siang River sediment and Yigong flood deposit data compilations, and individual megaflood deposits. The overall stress value of the map is 0.10283, between a fair and good fit to the data (Vermeesch, 2013). Consistent with the sample
296 KDEs, the MDS map shows more overlap between the Yarlung, Yigong, and Parlung zircon distributions compared to the distribution from the Namche Barwa cirque sample—and supports 297 that the Tsangpo Gorge detrital zircon signal is distinct from other sedimentary sources in the 298 drainage. The modern Siang River and 2000 Yigong flood deposit compilations plot close 299 together, reflecting the similarity of their KDEs. The 1900 Yigong flood sample is close to but 300 not directly linked to the 2000 flood compilation, highlighting the potential for significant 301 variability among detrital age distributions for very similar outburst flood events sourced from 302 the same location. 303

304 Further insight from MDS analysis is limited. The MDS map is relatively insensitive to 305 the positions of small age peaks observed in the different sample distributions. For example, 306 samples 13SI32 and 13SI28 have prominent zircon age peaks from ~100-220 Ma, yet they plot 307 nearest to the Namche Barwa source sample, which lacks these defined age peaks. In addition, 308 comparing large and small *n* samples on an MDS map can be problematic (Vermeesch, 2015), so 309 we evaluated the effects of sample size using a bootstrap approach. When we randomly remove 310 20% of the grains and re-compute the MDS map, we find in many iterations that the positions 311 and connections among the samples vary. For example, a connection between PFS-1 and 13SI32 312 appears in several iterations (**Figure S10**) that is not present in the original map (**Figure 5**), yet 313 we group these two samples based on the similarity of their KDEs (**Figure 4**). Together, these 314 observations suggest the large difference in sample size between megaflood deposits and some 315 source samples makes the MDS map of limited use for interpreting zircon provenance. 316

## 4.3 BayesMix age component results

317 BayesMix inversion (**Figure 6, Table 3**) identifies age components consistent with a ~50 318 Ma peak representing Tibetan source sediment in all sample compilations, but in varying
319 proportions. The youngest age component in the modern Siang River and 2000 Yigong Flood
320 sample compilations, respectively, represents 30-32% of the zircons, whereas the youngest
321 component in the megaflood compilation represents 22% of the zircons. The next largest age
322 components by proportion are consistent with ~350-550 Ma Himalayan ages from the Tsangpo
323 Gorge area. Components in the 350-550 Ma range are identified in smaller proportions in the
324 modern Siang River and 2000 Yigong flood compilations (23-24 %) compared to the megaflood
325 compilation (37 %). The two age components in this range that are resolved in the megaflood
326 compilation have means at 391 Ma and 475 Ma, corresponding to peaks in the Namche Barwa
327 source sample. The BayesMix model identifies age components in the 50 to 350 Ma age range
328 for the megaflood sample compilation that are not observed in the modern Siang River and
329 Yigong flood deposit compilations.

330 BayesMix inversion of the zircon data for sample groups 1, 2 and 3 show differences in
331 the position and magnitude of the age components in each group (Table 3, Figure 6). Prominent
332 age components at ~41 Ma and ~45 Ma in group 1 and group 3 samples represent 40 % and 17
333 % of the zircons in each group, respectively; these age components overlap the diagnostic ~50
334 Ma peak from the Yarlung River source samples, although the positions of peaks in some
335 individual samples varies and may be consistent with other sources. In contrast, the youngest age
336 component in the group 2 samples comprising 11 % of zircons with a mode at 27 Ma is
337 consistent with the ≤30 Ma ages seen in the Namche Barwa source sample. The relative
338 contribution from 350-550 Ma Himalayan rock from the Tsangpo Gorge area varies among
339 individual samples, but on average these components make up 22-24% of zircons in groups 1
340 and 3, and 49 % of group 2 zircons. Taken together, the BayesMix results highlight prominent
341 Himalayan and Tibetan age components in the sample data, which we relate to zircon source areas below.
342

343 **5. Discussion**

344 Here we interpret zircon data from 11 megaflood deposits in the context of the zircon age distributions from potential source areas in Tibet, modern Siang River sediments, and historical outburst flood deposits. Floodwaters may entrain impounded lake sediment, material eroded from the hillslopes and channel during a flood event, and reworked sediment from previous lake/flood/fluvial deposits along the flood pathway—recording contributions from each of these sources in the zircon age distributions they deposit. Most of the megaflood deposit age distributions indicate zircon provenance from areas at or to the west of Namche Barwa in the Yarlung River drainage, or from Himalayan rocks of the Tsangpo Gorge. These data (1) suggest most of the megafloods that produced the sampled deposits were sourced from impoundments at or to the west of Namche Barwa in the Yarlung River drainage, and (2) suggest preferential erosion of the Tsangpo Gorge area during most of the recorded megaflood events in comparison to the modern river monsoonal and century-flood discharges, supporting the hypothesis that megafloods may have had a disproportionately large impact on Gorge exhumation.

357 **5.1 Zircon provenance and constraints on megaflood sources**

358 There is widespread evidence of glacial-moraine dams in the eastern Himalaya, but it is unclear which potential sources of zircons are represented in the Siang River valley megaflood deposits. Lang et al. (2013) suggested that the megafloods that produced these deposits were sourced from glacially-impounded lakes in western Tibet because of the extensive record of lacustrine deposits on the Yarlung River adjacent to and upstream of Namche Barwa (Montgomery et al., 2004; Liu et al., 2006, 2015, 2018; Kaiser et al., 2010; Zhu et al., 2013,
2014; Huang et al., 2014; Chen et al., 2016). Recent observations of coarse sediments and bed forms in the middle-reaches of the Yarlung River provide evidence of megafloods sourced from impoundments even further to the west (Hu et al., 2018). Limited evidence also exists for paleo-lake deposits on the Yigong and Parlung Rivers in eastern Tibet (Guangxiang and Qingli, 2012), raising the question of whether megafloods were sourced from glacial impoundments in this area.

Outburst floods may be highly erosive at and immediately downstream of the dam breach (O'Connor and Beebee, 2009; Table, et al., 2018; Turzewski et al., 2019), entraining impounded lake sediment and/or dam, hillslope, and fluvial material near the source. Zircons from the dammed area may therefore be well represented in flood deposits downstream, as is observed for slackwater deposits of the 1900 and 2000 Yigong River floods (Lang et al., 2013; this study).

Distinctive age peaks <250 Ma from potential megaflood source areas to the east and west of Namche Barwa in Tibet appear in varying proportions in the megaflood slackwater deposits, and have the potential to constrain the source areas of megafloods that produced the Siang River valley slackwater deposits.

Most of the megaflood deposits contain a strong western Tibetan source signature. The four megaflood deposits in group 1 (Figure 4a) and sample 08KH24 (Figure 4b) contain a prominent ~50 Ma peak characteristic of a Yarlung River source and generally lack other significant <600 Ma zircon peaks, except for the ~490 Ma Himalayan age component present in all flood deposits in this study. The three megaflood deposits in group 2 (Figure 4c) contain a significant proportion of zircons that appear to have been sourced from the Namche Barwa massif/Tsangpo Gorge specifically, with a peak at ~27 Ma and a very large contribution of zircons at 350-550 Ma (Figure 3e). Two of the group 3 deposits (08KH28, 13SI28; Figure 4d)
also have prominent ≤ 50 Ma age peaks indicative of Yarlung catchment/Namche Barwa

provenance. These clear Yarlung River and Namche Barwa zircon provenance signals provide

strong evidence that all eight group 1 and 2 deposits, and two of the group 3 deposits, record

megafloods sourced from impoundments at or to the west of Namche Barwa that would have

traversed the Yarlung River pathway through the Tsangpo Gorge.

Only one of the megaflood deposits (13SI02) may be compatible with an eastern Tibetan

flood source (Figure 4d). The youngest age peak at ~66 Ma and significant contribution of

~100-220 Ma zircons in deposit 13SI02 are similar to the zircon signals found in the Yigong and

Parlung River source and the 1900 and 2000 Yigong flood samples and may be compatible with

an impounded lake source to the east of Namche Barwa, although the age distribution of sample

13SI02 is poorly resolved. The other two group 3 deposits that show a significant contribution of

≤ 50 Ma zircons indicative of Yarlung catchment/Namche Barwa provenance (08KH28, 13SI28)

also contain zircons in the ~100-220 Ma age range, which may be consistent with eastern

Tibetan sources and/or flood-transported or reworked sediment that originated in the middle

reaches of the Yarlung River. However, given that the youngest zircon age peak in these samples

is significantly younger than 66 Ma, the impoundments that sourced the depositing floods were

likely located west of Namche Barwa in the Yarlung drainage.

Diagnostic age peaks from multiple flood source areas are present in most of the flood

deposits, showing the extent to which outburst floods rework previous flood and/or fluvial

deposits. The 2000 Yigong flood deposit data show that a flood sourced from this eastern

Tibetan tributary impoundment contains ~100-220 Ma zircons that characterize the eastern

tributary source regions as well as ~50 Ma zircons characteristic of western Tibetan sources,

similar to modern Siang River sediment (Figure 4e,f). Several of the group 1 and group 2
410 megaflood deposits from western Tibetan sources contain age peaks that are diagnostic of source areas in the middle reaches of the Yarlung drainage. It is not possible to tell whether zircons with 411 these diagnostic ages were entrained from their source area directly during the flood that 412 produced the sampled deposit, or reworked from the deposits of a previous flood event. 413
414 Nevertheless, the zircon ages may be consistent with provenance from impoundments on the 415 middle Yarlung River (e.g., the Dazhuka-Yueju Gorge; **Figure 1**) or tributaries to the Yarlung. 416
417 Despite contributions to the zircon age signals of sediment reworking, our data show that the 418 sediment preserved in megaflood slackwater deposits mostly comes from the western Tibetan 419 sources within the Yarlung River drainage and from Namche Barwa/the Tsangpo Gorge— 420 suggesting that these areas were where impounded lakes that sourced the megafloods were 421 located. 422

421 Our data link most slackwater megaflood deposits to glacially impounded lake sources to 422 the west of Namche Barwa, which is not surprising given the difference in valley morphology of 423 the eastern and western drainages. Widespread glacial advances are dated throughout the region 424 from 11-30 ka (Owen and Benn, 2005; Korup and Montgomery, 2008; Hu et al., 2017), 425 including eastern Tibetan tributaries of the Yigong and Parlung River (Guangxiang & Qingli, 426 2012) that could result in glacial-moraine damming and lake impoundment. Glacial-moraine 427 damming might produce smaller lakes in the eastern catchments compared to the Yarlung River 428 catchment to the west of Namche Barwa because there is limited accommodation space for large 429 (>10 km³) lakes in these high-relief, narrow eastern tributaries. Indeed, the only mapped 430 evidence of lacustrine sediments from glacial-impounded lakes exists in the Songzong sub-basin 431 of the Parlung River catchment, which has a total area of only 16 km² (Guangxiang and Qingli, 432 2012). The area of the Songzong sub-basin is dwarfed by the areas of the Yarlung River sub-
basins to the west of Namche Barwa (Figure 1, 3). If the morphology of the Parlung and Yigong basins did not facilitate the formation of large glacially impounded lakes, this might explain why there is little evidence of megafloods from these tributaries in slackwater megaflood deposits along the Siang River.

## 5.2 Preferential erosion and sediment evacuation from the Tsangpo Gorge during megafloods

Our findings bear on the use of zircon age distributions as tracers of sediment sources and proxies for spatial patterns of erosion in the Eastern Himalaya. Variation in source rock zircon fertility may bias comparisons of erosion rate or sediment flux estimates and is important to account for in studies comparing erosion rates across different drainage areas (Vezzoli et al., 2016; Braun et al., 2018). Like Lang et al. (2013), we avoid this bias by comparing deposits within the same drainage area, with the same potential source rocks. We assume that source rock zircon fertility did not change significantly over the Quaternary, and that the best explanation for changes in the zircon age distributions is changes in the relative contribution of zircons from different locations within the source area.

Lang et al. (2013) found a disproportionate amount of zircons from the Tsangpo Gorge in megaflood slackwater deposits compared to Yigong flood deposits and modern Siang River sediments, and used this result to argue that megafloods preferentially focus erosion in the Gorge. Our analyses of 1438 zircons from seven additional megaflood deposits brings the total observations to 11 deposits and n=1608 zircon data, which confirm that on average the megaflood samples do have a higher proportion of zircons derived from the Gorge compared to the modern Siang River and Yigong flood samples. However, our large dataset also shows significant variation among the zircon age distributions of individual megaflood deposits.
456

Section 5.1 discussed the potential contributions to zircon provenance and age distributions of flood impoundment location and sediment reworking; here we explore the degree to which the age distributions reflect the spatial pattern of erosion during a flood event.

457

458

459

Megafloods that we interpret to have come from failed glacial moraine impoundments on the flanks of Namche Barwa just upstream of the Tsangpo Gorge (group 2) have the greatest contribution (~49%) of ~490 Ma zircons and anatectic zircons characteristic of Himalayan rock from the Tsangpo Gorge area in their deposits. We do not know how many of these zircons were eroded from the Gorge area during vs. prior to the megafloods that produced the sampled deposits. However, these megaflood deposits contain about twice as many ~490 Ma zircons as is observed in 2000 Yigong flood and modern Siang River deposits, and significantly more ~490 Ma zircons than are found in all but one of the other flood deposits (08KH24), indicating that sediment reworking cannot explain the bulk of this signal. Outburst floods sourced from impoundments at Namche Barwa would be expected to focus erosion near the breach, eroding and entraining a disproportionate amount of material in the Gorge area. We suggest the simplest interpretation is that the great abundance of Himalayan and anatectic zircons in these deposits does reflect preferential erosion in the Tsangpo Gorge.

460

461

462

463

464

465

466

467

468

469

470

471

472

473

474

475

476

477

478

Varying proportions of Gorge-sourced zircons in the other megaflood samples are more difficult to interpret, but nevertheless support the idea that megafloods preferentially eroded and entrained material from the Tsangpo Gorge area compared to modern river flows. Individual megaflood sample age distributions vary due to factors like impoundment location and sediment recycling, making it impossible to quantify the specific percent contribution to the Gorge-sourced zircon signal due to erosion from the depositing megaflood. It is also possible that some of the ~490 Ma zircons may have been derived from Himalayan rocks that crop out in
northward-draining tributaries to the Yarlung upstream of the Gorge. Fission-track double dating of these zircons to further refine their provenance (Lang et al., 2016) is beyond the scope of this study. However, the megaflood samples also contain a higher proportion of <30 Ma anatectic zircons eroded directly from the Gorge compared to the modern Siang River samples (Figure 6), providing independent provenance constraints. Thus despite these complications, the data indicate 9 of the 11 megaflood deposits contain significantly more zircons sourced from the Tsangpo Gorge compared to modern Siang River sediments (Figure 4), providing strong evidence that megafloods are capable of focusing erosion in the Gorge. This finding combined with evidence indicating that most of these megafloods were probably sourced from impoundments in the Yarlung River drainage at or to the west of Namche Barwa, highlight the potential for repeated megafloods to influence the morphology of the Yarlung-Po River pathway through the Tsangpo Gorge—and support the hypothesis that preferential erosion of the Tsangpo Gorge during megafloods may have been an important mechanism for keeping pace with rapid rock uplift during the Quaternary.

493

## 494 Conclusions

We presented new detrital zircon U-Pb geochronology data for outburst flood slackwater deposits preserved downstream of the Tsangpo Gorge, that combined with previous zircon data for Tibetan source regions and downstream fluvial and outburst flood deposits shed light on the sources and erosional impact of Quaternary megafloods in the eastern Himalayan syntaxis.

Despite complications due to the entrainment of previously deposited sediment along the flood pathway, the flood slackwater deposits contain clear zircon provenance signals that we interpret to reflect impounded lake sources and spatial patterns of erosion during floods:

495

496

497

498

499

500

501
502 • Diagnostic ≤250 Ma age components in the studied deposits indicate that most megaflood
503 events were sourced from impoundments in the Yarlung River drainage at or to the west
504 of Namche Barwa, with some sample ages suggesting provenance potentially as far
505 upstream as the middle Yarlung.

506 • Only one of the eleven studied megaflood deposits may be compatible with an eastern
507 Tibetan source on the Yigong and Parlung Rivers. It is possible that limited
508 accommodation space for large (>10 km³) lakes in the high-relief, narrow valleys of the
509 Parlung and Yigong drainages may explain the paucity of evidence for megafloods from
510 eastern Tibetan sources in our dataset.

511 • Our analyses of n=1139 zircons from 7 new megaflood deposits add significantly to the
512 available data documenting floods through the Tsangpo Gorge, and show that megaflood
513 deposits contain a disproportionate amount of zircons from the Gorge compared to the
514 modern Siang River and historical Yigong flood deposits. The overabundance of Gorge-
515 sourced zircons is unlikely to be explained by sediment reworking alone, and provides
516 evidence that megafloods preferentially focused erosion in the Gorge.

517 • The highest proportions of Gorge-sourced zircons are found in deposits from megafloods
518 that we interpret to have been sourced from glacial-moraine dam impoundments on the
519 flanks of Namche Barwa, immediately upstream of the Tsangpo Gorge. This finding
520 highlights the potential for outburst flood source location to control erosion patterns by
521 focusing erosion at and immediately downstream of the dam breach.

522 Taken together, our findings place new constraints on megaflood source locations and processes
523 of sediment reworking that influence downstream zircon age distributions, and show that
524 megafloods had the potential to preferentially erode the Tsangpo Gorge and contribute
525 substantially to rapid exhumation of the Eastern Himalayan syntaxaxis.

526

527 Tables

528 Table 1. Previously published zircon U-Pb samples characterizing Tibetan source areas.

<table><thead><tr><th>Sample name</th><th>Location Lat [DD]</th><th>Location Lon [DD]</th><th>Size (n)</th><th>Reference</th></tr></thead><tbody><tr><td>Quxu</td><td>29.3193</td><td>90.6864</td><td>77</td><td>Zhang et al., 2012</td></tr><tr><td>Gonggar</td><td>29.3228</td><td>91.0921</td><td>340</td><td>Cina et al., 2009</td></tr><tr><td>Gyacca</td><td>29.0747</td><td>92.7748</td><td>78</td><td>Zhang et al., 2012</td></tr><tr><td>Yarlung R.</td><td>29.3228</td><td>91.0921</td><td>163</td><td>Stewart et al., 2008</td></tr><tr><td>Renbu Qu</td><td>29.2959</td><td>89.7952</td><td>95</td><td>Zhang et al., 2012</td></tr><tr><td>Lhasa</td><td>29.4426</td><td>90.9315</td><td>86</td><td>Zhang et al., 2012</td></tr><tr><td>Zedong</td><td>29.2837</td><td>91.8158</td><td>84</td><td>Zhang et al., 2012</td></tr><tr><td>Siqunama</td><td>29.219</td><td>92.0144</td><td>103</td><td>Zhang et al., 2012</td></tr><tr><td>Langxian</td><td>29.141</td><td>93.135</td><td>84</td><td>Zhang et al., 2012</td></tr><tr><td>Nyingoh</td><td>29.4333</td><td>94.4543</td><td>91</td><td>Zhang et al., 2012</td></tr><tr><td>Namche Barwa Cirque</td><td>29.60642</td><td>94.93687</td><td>129</td><td>Booth et al., 2004</td></tr><tr><td>Layue Qu</td><td>29.9888</td><td>94.875</td><td>89</td><td>Zhang et al., 2012</td></tr><tr><td>Yigong R.</td><td>30.0967</td><td>95.0647</td><td>116</td><td>Zhang et al., 2012</td></tr><tr><td>Parlung R.</td><td>29.9084</td><td>95.4606</td><td>94</td><td>Zhang et al., 2012</td></tr></tbody></table>

529
530
531
532
533
534
535
536
537
538
539
540
541
542
543
544
545

<table><caption>Table 2. Samples from slackwater flood deposits</caption><thead><tr><th>Sample Name</th><th>Deposit type</th><th>Grain size (D50) [mm]</th><th>Lat [DD]</th><th>Lon [DD]</th><th>Elevation [m]</th><th>Number of analyses n</th></tr></thead></table>
<table><tr><td>13SI02</td><td>Megaflood</td><td>0.512</td><td>28.1533</td><td>95.19072</td><td>555</td><td>92</td></tr><tr><td>13SI11</td><td>Megaflood</td><td></td><td>28.23355</td><td>94.98277</td><td>271</td><td>215</td></tr><tr><td>13SI40</td><td>Megaflood</td><td></td><td>28.41904</td><td>95.08376</td><td>309</td><td>135</td></tr><tr><td>13SI28</td><td>Megaflood</td><td>0.164</td><td>28.5763</td><td>95.06302</td><td>427</td><td>164</td></tr><tr><td>13SI32</td><td>Megaflood</td><td>0.240</td><td>28.57915</td><td>95.06281</td><td>400</td><td>133</td></tr><tr><td>13SI34</td><td>Megaflood</td><td>0.253</td><td>28.57959</td><td>95.06693</td><td>360</td><td>200</td></tr><tr><td>13SI21</td><td>Megaflood</td><td></td><td>28.63944</td><td>95.02667</td><td>394</td><td>200</td></tr><tr><td>08KH10<sup>1</sup></td><td>Megaflood</td><td></td><td>29.051366</td><td>94.906178</td><td>502</td><td>161</td></tr><tr><td>08KH24<sup>1</sup></td><td>Megaflood</td><td></td><td>28.965522</td><td>94.847082</td><td>553</td><td>89</td></tr><tr><td>08KH28<sup>1</sup></td><td>Megaflood</td><td></td><td>28.317589</td><td>94.95328</td><td>353</td><td>115</td></tr><tr><td>PFS-1<sup>1</sup></td><td>Megaflood</td><td></td><td>28.233917</td><td>94.983443</td><td>270</td><td>85</td></tr><tr><td>13SI17</td><td>1900 Yigong flood</td><td></td><td>28.40177</td><td>95.07956</td><td>278</td><td>149</td></tr><tr><td>13SI18</td><td>2000 Yigong flood</td><td></td><td>28.40177</td><td>95.07956</td><td>279</td><td>131</td></tr><tr><td>08KH34<sup>1</sup></td><td>2000 Yigong flood</td><td>0.140</td><td>28.173515</td><td>95.030536</td><td>199</td><td>42</td></tr><tr><td>08KH31<sup>1</sup></td><td>2000 Yigong flood</td><td></td><td>28.235035</td><td>94.996516</td><td>230</td><td>113</td></tr><tr><td>08KH05<sup>1</sup></td><td>2000 Yigong flood</td><td>0.355</td><td>28.960825</td><td>94.865067</td><td>466</td><td>44</td></tr><tr><td>08KH15<sup>1</sup></td><td>2000 Yigong flood</td><td>0.167</td><td>29.048683</td><td>94.910801</td><td>475</td><td>57</td></tr><tr><td>SC03-26-08-(6)<sup>2</sup></td><td>Modern Siang River</td><td></td><td>28.0768</td><td>95.3356</td><td>156</td><td>137</td></tr><tr><td>S032508-16<sup>1</sup></td><td>Modern Siang River</td><td></td><td>28.576655</td><td>95.070195</td><td>264</td><td>88</td></tr><tr><td>TUTING<sup>1</sup></td><td>Modern Siang River</td><td></td><td>28.996279</td><td>94.903436</td><td>425</td><td>58</td></tr><tr><td>S032808-36<sup>1</sup></td><td>Modern Siang River</td><td></td><td>29.048474</td><td>94.910787</td><td>449</td><td>73</td></tr></table>

Superscripts indicate previous detrital samples of Lang et al. (2013)¹ and Stewart et al. (2013)²

546

547

548

549

550

551

552

553

554
<table><caption>Table 3. Results from BayesMix inversions</caption><thead><tr><th>Compilation</th><th colspan="3">Modern Siang River samples (n=356)</th><th colspan="3">2000 Yigong flood samples (n=387)</th><th colspan="3">Megafloods (n=1608)</th><th colspan="3">Group 1 (n=721)</th><th colspan="3">Group 2 (n=418)</th><th colspan="3">Group 3 (n=380)</th></tr><tr><th>Sample names</th><th colspan="3">S32808-36,TUTING, S032508-16,PASIGHAT</th><th colspan="3">08KH15,08KH05,08KH31, 08KH34,13SI17</th><th colspan="3">08KH10,13SI34,13SI11,13SI40, 13SI02,13SI28,08KH28 13SI32,13SI21,08KH24,PFS-1</th><th colspan="3">08KH10, 13SI34, 13SI11, 13SI40</th><th colspan="3">13SI21, PFS-1, 13SI32</th><th colspan="3">13SI28, 08KH28, 13SI02</th></tr><tr><th>Component</th><th>Mean (Ma)</th><th>Error (Ma)</th><th>(%)</th><th>Mean (Ma)</th><th>Error (Ma)</th><th>(%)</th><th>Mean (Ma)</th><th>Error (Ma)</th><th>(%)</th><th>Mean (Ma)</th><th>Error (Ma)</th><th>(%)</th><th>Mean (Ma)</th><th>Error (Ma)</th><th>(%)</th><th>Mean (Ma)</th><th>Error (Ma)</th><th>(%)</th></tr></thead><tbody><tr><td>1</td><td>53</td><td>12.6</td><td>30.0</td><td>66</td><td>15.7</td><td>31.8</td><td>54.8</td><td>9.5</td><td>22.4</td><td>41.6</td><td>8.6</td><td>40.0</td><td>17.9</td><td>22.6</td><td>11.7</td><td>28.2</td><td>3.4</td><td>5.2</td></tr><tr><td>2</td><td>112.1</td><td>2.4</td><td>3.4</td><td>196.5</td><td>8.6</td><td>6.3</td><td>90</td><td>4.6</td><td>0.7</td><td>238.6</td><td>95.4</td><td>8.7</td><td>128.0</td><td>6.7</td><td>0.7</td><td>45.2</td><td>11.9</td><td>17.1</td></tr><tr><td>3</td><td>199.4</td><td>27.2</td><td>3.6</td><td>477.1</td><td>21.3</td><td>23.1</td><td>129.6</td><td>8.4</td><td>2.1</td><td>469.1</td><td>5.1</td><td>24.7</td><td>206.4</td><td>7.9</td><td>3.0</td><td>114.1</td><td>7.5</td><td>1.3</td></tr><tr><td>4</td><td>482.2</td><td>19.6</td><td>24.0</td><td>766.2</td><td>7.8</td><td>1.9</td><td>220.1</td><td>3.2</td><td>3.5</td><td>978.9</td><td>10.0</td><td>4.2</td><td>437.0</td><td>22.3</td><td>15.7</td><td>142.2</td><td>13.4</td><td>1.2</td></tr><tr><td>5</td><td>817.1</td><td>7</td><td>6.8</td><td>1094.7</td><td>114.2</td><td>13.0</td><td>275</td><td>8.9</td><td>1.5</td><td>1214.1</td><td>9.6</td><td>8.8</td><td>471.9</td><td>4.5</td><td>34.8</td><td>213.9</td><td>4.7</td><td>10.2</td></tr><tr><td>6</td><td>1008.7</td><td>13.2</td><td>3.1</td><td>1151.3</td><td>31.9</td><td>8.8</td><td>443.1</td><td>65.3</td><td>14.8</td><td>1855.8</td><td>53.7</td><td>8.5</td><td>835.3</td><td>61.2</td><td>6.5</td><td>414.8</td><td>5.5</td><td>1.7</td></tr><tr><td>7</td><td>1155</td><td>6.9</td><td>12.6</td><td>1563.4</td><td>111.2</td><td>15.1</td><td>478.1</td><td>3.7</td><td>22.7</td><td>1619.7</td><td>5.1</td><td>3.6</td><td>991.4</td><td>4.7</td><td>6.9</td><td>482.1</td><td>2.4</td><td>20.3</td></tr><tr><td>8</td><td>1597.4</td><td>45.4</td><td>10.6</td><td>-</td><td>-</td><td>-</td><td>697.8</td><td>5.1</td><td>0.8</td><td>2494.9</td><td>64.9</td><td>1.1</td><td>1202.1</td><td>17.4</td><td>7.5</td><td>692.7</td><td>204.0</td><td>15.7</td></tr><tr><td>9</td><td>2900.9</td><td>12.2</td><td>4.1</td><td>-</td><td>-</td><td>-</td><td>834.1</td><td>4.3</td><td>3.6</td><td>2865.3</td><td>9.6</td><td>0.5</td><td>1305.4</td><td>7.0</td><td>0.1</td><td>1006.7</td><td>11.4</td><td>5.6</td></tr><tr><td>10</td><td>3227.1</td><td>8.1</td><td>0.6</td><td>-</td><td>-</td><td>-</td><td>1007.9</td><td>7.3</td><td>4.7</td><td>-</td><td>-</td><td>-</td><td>1726.2</td><td>57.0</td><td>13.2</td><td>1186.2</td><td>4.3</td><td>9.4</td></tr><tr><td>11</td><td>3529.2</td><td>24.4</td><td>1.2</td><td>-</td><td>-</td><td>-</td><td>1133.2</td><td>171.4</td><td>9.0</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>1349.6</td><td>43.4</td><td>5.5</td></tr><tr><td>12</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>1176</td><td>4.7</td><td>6.4</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>1608.8</td><td>33.7</td><td>5.2</td></tr><tr><td>13</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>1615.6</td><td>45.3</td><td>7.5</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>2849.5</td><td>15.7</td><td>0.1</td></tr><tr><td>14</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>2861.6</td><td>24.2</td><td>0.5</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td><td>-</td></tr></tbody></table>
<figure><img src="image_2.png" /><figcaption>Figures</figcaption></figure>

**Figure 1.** Location map of study area as a hillshade over topography (SRTM3 digital elevation model). The Yarlung River flows into the Tsangpo Gorge (red) from the west, and the Yigong and Parlung Rivers flow into the Gorge through the Po River from the north. Zircon age distributions in the study area are characterized by detrital samples from the main trunk Yarlung River, tributaries to the Yarlung, and the Yigong and Parlung Rivers; and from bedrock data from Namche Barwa. Drainage areas for the detrital zircon samples are outlined in white. Locations of dated ancient megaflood deposits (Lang et al., 2013; this study), reconstructed glacially-impounded lakes (Montgomery et al., 2004; Hu et al., 2018; see text), and glacial dams mapped between 92 and 96°E by Korup and Montgomery (2008) are also shown.
<figure><img src="image_3.png" /><figcaption>**Figure 2.** Sample locations along the Siang River, northeast India, showing previously dated flood slackwater samples (Lang et al., 2013) and modern river detritus (Stewart et al., 2008; Lang et al., 2013), and new samples collected in this study.</figcaption></figure>
<figure><img src="image_4.png" /></figure>
**Figure 3.** Zircon age distributions of previously published samples that characterize some potential source regions in this study (sample locations and references shown in Figure 1). Kernel density estimate (KDE) plots show data for (a) Yarlung River main trunk detrital samples; (b-d) detrital samples from western tributaries to the Yarlung; (e) bedrock samples from Namche Barwa; and (f) detrital samples from northern and eastern Tibetan sources of sediment. Line (1) represents the age peak at ~50 Ma that is characteristic of the Yarlung River source samples (a), and line (2) represents the age peak at ~490 Ma that is characteristic of Namche Barwa bedrock. Sources for detrital samples include: Zhang et al. (2012)¹, Cina et al., (2009)², Stewart et al., (2008)³. The bedrock data are from Booth et al. (2004)⁴.
<figure><img src="image_5.png" /></figure>
**Figure 4.** Detrital zircon age distributions from Siang River valley samples, including (a-d) ancient megaflood deposits from this and previously work (* indicates previously published data of Lang et al., 2013); (e) slackwater deposits from historical landslide-dam outburst floods including a new 1900 Yigong flood sample (this study) and the updated 2000 Yigong flood data compilation (Lang et al., 2013; this study); and (f) published modern Siang River sample compilation (Stewart et al., 2008; Lang et al., 2013).

<figure><img src="image_6.png" /></figure>

**Figure 5.** MDS map displaying similarity between four source samples used in previous studies shown in Figure 3 (Yarlung River, Namche Barwa Cirque, Yigong River, and Parlung River), modern Siang River and 2000 Yigong flood compilations, the 1900 Yigong flood sample, and all individual megaflood deposits (Stress value = 0.10283). Solid lines between samples represent the most similar neighbor, whereas a dotted line is the second most similar. The distance in the x and y direction on this plot is in the unit of a KS statistic, so more dissimilar samples plot further apart on the 2D map.
<figure><img src="image_7.png" /><figcaption>**Figure 6.** Age components <600 Ma identified with BayesMix inversion of (a) modern Siang River sample, (b) 2000 Yigong flood sample compilation, (c) megaflood compilation, and (d-f) megaflood subgroups 1-3.</figcaption></figure>

33

34

35

36
37

38 Acknowledgements

39 We thank Oken Tayeng, Tapir Tayeng and Abor Travels for field support. We
40 acknowledge David Montgomery, Alison Duvall, and Megan Mueller for commenting on earlier
41 drafts. Thank you to Paul O'Sullivan at GeoSep Services who aided with mineral separations,
42 and Mariah Danner for assistance in the laboratory and with zircon analyses. We also thank the
43 Arizona LaserChron Center for performing zircon analyses and assistance with data reduction.
44 Funding was provided by the Quaternary Research Center at the University of Washington and
45 U.S. National Science Foundation (EAR-1349279 and EAR-0955309 to KWH).

46

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