Surface-Rupturing Historical Earthquakes in Australia and Their Environmental Effects: New Insights from Re-Analyses of Observational Data

King, Tamarah R.; Quigley, Mark; Clark, Dan

doi:10.3390/geosciences9100408

Open AccessEditor’s ChoiceReview

Surface-Rupturing Historical Earthquakes in Australia and Their Environmental Effects: New Insights from Re-Analyses of Observational Data

by

Tamarah R. King

^1,*

,

Mark Quigley

¹ and

Dan Clark

²

¹

School of Earth Sciences, University of Melbourne, Melbourne 3010, Australia

²

Geoscience Australia, Canberra 2609, Australia

^*

Author to whom correspondence should be addressed.

Geosciences 2019, 9(10), 408; https://doi.org/10.3390/geosciences9100408

Submission received: 2 August 2019 / Revised: 14 September 2019 / Accepted: 16 September 2019 / Published: 20 September 2019 / Corrected: 10 February 2022

(This article belongs to the Special Issue New Perspectives in the Definition/Evaluation of Seismic Hazard through Analysis of the Environmental Effects Induced by Earthquakes)

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Abstract

:

We digitize surface rupture maps and compile observational data from 67 publications on ten of eleven historical, surface-rupturing earthquakes in Australia in order to analyze the prevailing characteristics of surface ruptures and other environmental effects in this crystalline basement-dominated intraplate environment. The studied earthquakes occurred between 1968 and 2018, and range in moment magnitude (Mw) from 4.7 to 6.6. All earthquakes involved co-seismic reverse faulting (with varying amounts of strike-slip) on single or multiple (1–6) discrete faults of ≥ 1 km length that are distinguished by orientation and kinematic criteria. Nine of ten earthquakes have surface-rupturing fault orientations that align with prevailing linear anomalies in geophysical (gravity and magnetic) data and bedrock structure (foliations and/or quartz veins and/or intrusive boundaries and/or pre-existing faults), indicating strong control of inherited crustal structure on contemporary faulting. Rupture kinematics are consistent with horizontal shortening driven by regional trajectories of horizontal compressive stress. The lack of precision in seismological data prohibits the assessment of whether surface ruptures project to hypocentral locations via contiguous, planar principal slip zones or whether rupture segmentation occurs between seismogenic depths and the surface. Rupture centroids of 1–4 km in depth indicate predominantly shallow seismic moment release. No studied earthquakes have unambiguous geological evidence for preceding surface-rupturing earthquakes on the same faults and five earthquakes contain evidence of absence of preceding ruptures since the late Pleistocene, collectively highlighting the challenge of using mapped active faults to predict future seismic hazards. Estimated maximum fault slip rates are 0.2–9.1 m Myr⁻¹ with at least one order of uncertainty. New estimates for rupture length, fault dip, and coseismic net slip can be used to improve future iterations of earthquake magnitude—source size—displacement scaling equations. Observed environmental effects include primary surface rupture, secondary fracture/cracks, fissures, rock falls, ground-water anomalies, vegetation damage, sand-blows/liquefaction, displaced rock fragments, and holes from collapsible soil failure, at maximum estimated epicentral distances ranging from 0 to ~250 km. ESI-07 intensity-scale estimates range by ± 3 classes in each earthquake, depending on the effect considered. Comparing Mw-ESI relationships across geologically diverse environments is a fruitful avenue for future research.

Keywords:

Intraplate earthquake; surface rupture; Australian earthquakes; earthquake environmental effects; reverse earthquake; ESI 2007 scale; historical and recent earthquakes

1. Introduction

In the 50 years between 1968 and 2018 Australia experienced eleven known surface rupturing earthquakes (Table 1, Figure 1). Studies of Australian surface rupturing earthquakes have contributed to improvements in our collective understanding of intraplate earthquake behavior, including rupture recurrence, in stable continental regions (SCR) [1,2,3,4,5] and empirically-derived scaling relationships for reverse earthquakes [6,7,8,9]. This paper reviews available published literature on historic surface ruptures (Table 1 and Table 2) and collates geological data (Table 3 and Table 4, Figure 1 and Figure 2), seismological data and analyses (Table 5), surface rupture measurements (Table 6), environmental damage (Table 7), and paleoseismic data (Table 8) (Figure 3, Figure 4, Figure 5, Figure 6, Figure 7, Figure 8, Figure 9 and Figure 10). We re-evaluate and reconsider rupture and fault characteristics in light of new data (e.g., geophysical and geological) using modern analysis techniques (e.g., environmental seismic intensity scale (ESI-07) [10]) and new or updated concepts in earthquake science since the time of publication (e.g., paleoseismology, SCR earthquake recurrence).

Table 1. Summary of known historic Australian surface rupturing earthquakes and relevant references.

Name	Fig. 1	Magnitude (Mw) [11]	Date (UTC)	This Paper:			Published		Relevant References
Name	Fig. 1	Magnitude (Mw) [11]	Date (UTC)	Length (km)	Dip	Avg. Net-Slip (m)	Length (km)	Max. Vert. Disp. (m)	Relevant References
Meckering, WA	1	6.59	14/10/1968	40 ± 5	35° ± 10	1.78	37	2.5	[12,13,14,15,16,17,18,19,20,21,22,23,24,25,26,27,28,29,30,31,32,33,34,35,36,37]
Calingiri, WA	8	5.03	10/03/1970	3.3 ± 0.2	20° ± 10	0.46	3.3	0.4	[23,24,25,38,39]
Cadoux, WA	4	6.1	02/06/1979	20 ± 5	60° ± 30	0.45	14	1.4	[28,40,41,42,43,44,45]
Marryat Creek, SA	5	5.7	30/03/1986	13 ± 1	40° ± 10	0.31	13	0.9	[1,28,46,47,48,49]
Tennant Creek 1 (Kunayungku) NT	7	6.27	22/01/1988	9 ± 1	40° ± 5	0.55	10.2	0.9	[1,49,50,51,52,53,54,55,56,57,58,59,60,61,62,63,64,65,66,67,68,69]
Tennant Creek 2 (Lake Surprise west)	6	6.44	22/01/1988	9 ± 2	60° ± 10	0.84	6.7	1.1	[1,49,50,51,52,53,54,55,56,57,58,59,60,61,62,63,64,65,66,67,68,69]
Tennant Creek 3 (Lake Surprise east)	3	6.58	22/01/1988	16 ± 0.5	35 ° ± 5	1.23	16	1.8	[1,49,50,51,52,53,54,55,56,57,58,59,60,61,62,63,64,65,66,67,68,69]
Katanning, WA	10	4.7	10/10/2007	0.5 ± 0.5	40° ± 5	0.2	1.26	0.1	[70,71]
Pukatja, SA	9	5.18	23/03/2012	1.3 ± 0.3	30° ± 10	0.25	1.6	0.5	[9,72]
Petermann, NT	2	6.1	20/05/2016	21 ± 0.5	30° ± 5	0.42	20	1.0	[73,74,75,76,77,78]
Lake Muir, WA		5.3	16/09/2018				3	0.5	[79]

Other literature with relevant analysis or data regarding historic ruptures: [80,81,82,83,84,85,86,87,88,89,90,91,92,93,94,95,96,97,98].

Australia is regarded as a stable continental region [104] surrounded by passive margins with an intraplate stress field controlled by plate boundary forces [100,105] (Figure 1). This stress field has been extant throughout much of Australia since the late Miocene, broadly concurrent with a rearrangement of tectonic boundaries in India, New Zealand, New Guinea, and Timor [101]. More than 360 potentially neotectonic features (those showing displacements associated with, or since initiation of, the current stress-field conditions) [5,95] have been recognized in the landscape through field mapping, subsurface geophysical imaging, digital elevation modelling, and palaeoseismic investigation [2,3,5,34,95,106,107,108,109,110,111,112,113] (Figure 1).

Southeast Australia and the Flinders Ranges (Figure 1) have the highest rates of seismicity [101,102] and estimated neotectonic fault slip rates [3,109,111] yet all of the largest onshore historic Australian earthquakes have occurred in Archean to Proterozoic cratonic crust across the central and western parts of the country (Figure 1) [11]. Of four defined zones of high seismicity (Figure 1) [101,102], the South West Seismic Zone (SWSZ) is the only to coincide with historic surface ruptures (Meckering, Calingiri, Cadoux, Katanning, Lake Muir). Other ruptures (Marryat Creek, Tennant Creek, Pukatja, Petermann) have occurred in historically aseismic regions of the cratonic crust (Figure 1, Table 5, Section 3.2).

Table 2. Summary of data sources used in reviewing Australian historic surface ruptures.

Seismological Catalogues
Primary literature	[9,12,46,47,57,60,61,63,70,73,74,75,15,88,18,24,25,38,40,41,43]
Geoscience Australia (GA) online catalogue	https://earthquakes.ga.gov.au/
National Seismic Hazard Assessment 2018 (NSHA18)	http://pid.geoscience.gov.au/dataset/ga/123139; [11]
Focal Mechanisms
Primary literature	[9,23,70,73,74,26,28,41,43,46,55,57,60]
GA compilation	[90]
Global centroid moment tensor catalogue	https://www.globalcmt.org/CMTsearch.html
Surface Rupture Trace
Primary literature	[9,25,41,48,63,70,73,78]
GA Neotectonic Features Database	[95]; http://pid.geoscience.gov.au/dataset/ga/74056
Google satellite imagery	https://www.google.com/earth/
Bing satellite imagery	https://www.bing.com/maps/aerial
National SRTM DEM	SRTM 1-Sec DEM: http://pid.geoscience.gov.au/dataset/ga/72759
Geological Maps
Primary literature	[9,16,25,41,65,114,115,116,117]
Geological Survey of Western Australia	http://www.dmp.wa.gov.au/Geological-Survey/Geological-Survey-262.aspx
Northern Territory Geological Survey	https://geoscience.nt.gov.au/
Geological Survey of South Australia	http://www.energymining.sa.gov.au/minerals/geoscience/geological_survey
Geoscience Australia	https://ecat.ga.gov.au/geonetwork/srv/eng/catalog.search
Borehole Data
Northern Territory Government	http://nrmaps.nt.gov.au/nrmaps.html
South Australia Government	https://www.waterconnect.sa.gov.au/Systems/GD/Pages/Default.aspx
Geophysical Maps
Primary literature	[33,50,51]
Bouguer gravity anomaly	http://pid.geoscience.gov.au/dataset/ga/101104
Total magnetic intensity	http://pid.geoscience.gov.au/dataset/ga/89596
Rupture Offset Data
Primary literature	[9,25,41,48,62,63,70,73,77]
Historic Photos of Ruptures
Primary literature	[1,9,47,48,59,63,64,72,73,87,118,12,14,15,25,35,37,40,41]
Websites	https://aees.org.au/; http://fortennantcreekers.com/events/earthquake-friday-22-january-1988/
News articles	https://trove.nla.gov.au/; https://www.abc.net.au/news/

2. Review Data, Methods and Terminology

Publications reviewed for ten of the eleven historic ruptures are provided in Table 1. At the time of writing, no publications are available for the most recent (eleventh) earthquake (8 November 2018 Mw 5.3 Lake Muir earthquake), although one is currently in review [79] and some imagery and data are available online (https://riskfrontiers.com/the-2018-lake-muir-earthquakes/, https://www.abc.net.au/news/2018-11-09/earthquake-hits-lake-muir-western-australia/10480694 (accessed on 21 June 2019)). Available details for this event are included in Table 1, Table 3 and Table 7 but it is otherwise not investigated in this paper. The Tennant Creek event comprises three mainshocks in a 12-hr period on the 22 January 1988, with three separate scarps recognized at the surface. Analysis of available seismological and surface data supports a direct association between each mainshock and an individual rupture (TC1: Kunayungku; TC2: Lake Surprise west; TC3: Lake Surprise east) [57,59,62,69] and they are treated as separate events in this paper.

Relevant papers were identified by reading through either (a) reference lists of recent (2010–2018) publications or (b) the citation history of older publications using Google Scholar. In total N = 67 articles were identified as containing relevant primary data and interpretations for individual or multiple surface rupturing events (Table 1). A further 16 publications were identified containing relevant information on Australian seismicity (drawing on data from the primary publications) or compilations of previously published material (Table 1). Other sources of data used to complement analysis of primary published data are summarized in Table 2.

Epicenter locations and focal mechanisms were collated from primary literature and online databases (Table 2). Geoscience Australia (GA) maintain an online earthquake catalogue that is continuously updated and recently published a national earthquake catalogue (NSHA18) from 1840 to 2017 [11]. The NSHA18 catalogue contains revised magnitude values (Mw) for all surface rupturing events based on a comprehensive reanalysis [11,119], which are used in this study. Epicenters for surface rupturing events are generally located closer to the surface ruptures in the online database than the NSHA18 catalogue.

Published surface rupture maps were previously digitized into GA’s publicly available Neotectonic Features Database [95]. In this paper, we sourced the original maps, georeferenced them, and digitized secondary fracturing that was left out of the GA database (Figure 3, Figure 4, Figure 5, Figure 6, Figure 7, Figure 8, Figure 9 and Figure 10). Some ruptures were relocated up to 200 m from the locations in the Neotectonic Features Database based on infrastructure and visible surface rupture matched on high resolution satellite imagery (Table 2) and primary maps, to correct for datum transformation errors.

For the purposes of this paper we use the terms “surface rupture” and “scarp” to describe the primary zone along which hanging-wall and foot-wall offset is visible at the surface. Fracturing relates to secondary surface features which do not host significant displacement, associated with the primary rupture (e.g., cracking). “Fissures” describe significant extensional cracks often with non-seismic edge collapse extending their width. “Fault” is used to describe the seismologically defined plane of rupture, of which the surface rupture is the observable expression.

3. Results

Detailed summaries of the geology, seismology, surface rupture and palaeoseismology for the eleven considered historical surface ruptures from 1968 to 2016 are available as seven EarthArXiv reports ([120,121,122,123,124,125,126]). Figures and data in these reports include available geological maps, geophysical maps, borehole data, surface rupture maps, displacement data, and available palaeoseismic trench logs. In the process of reviewing available literature, a number of inconsistencies in data usage or reproduction were identified. These are summarized in Section 4.1 of this paper, with more detail available in the EarthArXiv reports. Below is a concise summary of the seven reports (the three Tennant Creek ruptures are contained within a single report) with key data presented in Table 3, Table 4, Table 5, Table 6, Table 7, Table 8 and Table 9 and Figure 3, Figure 4, Figure 5, Figure 6, Figure 7, Figure 8, Figure 9 and Figure 10, and provided as Supplementary Data.

3.1. Geology

The Meckering, Calingiri, Cadoux, and Katanning events occurred in the Archean Yilgarn Craton within ~25 km of significant terrane boundaries (Figure 1). The Lake Muir event occurred in the Albany-Fraser Orogen, <15 km south of the south dipping terrane boundary with the Yilgarn Craton (Figure 1). The Marryat Creek, Pukatja and Petermann events occurred within the Mesoproterozoic Musgrave Block (Figure 1) within 0–10 km of major terrane boundaries. The Tennant Creek ruptures extend across the boundary of the Proterozoic Warramunga Province and Neoproterozoic–Cambrian Wiso Basin (Figure 1) (summary of all regional geology in Table 3, comprehensive details in EarthArXiv reports [120,121,122,123,124,125,126]).

Table 3. Summary of regional geology for each historic surface rupture.

Rupture	Refs.	Geological Province			Nearby Regional Structure
Rupture	Refs.	Name	Age	Sub-Division	Name	Age	Geometry	Dist. from Rupture	Approx. Aligned?
Meckering	[33,91,108,127]	Yilgarn Craton	Archean	Jimperding Metamorphic Belt, Lake Grace Terrane	Boundary Lake Grace and Boddington Terranes	Archean	NW-SE, shallow E dipping suture	~25 km on HW	Yes
Calingiri	[91,108,127]	Yilgarn Craton	Archean	Jimperding Metamorphic Belt, Lake Grace Terrane	Boundary Lake Grace and Boddington Terranes	Precambrian	NW-SE, shallow E dipping suture	~10 km on HW	Yes
Cadoux	[91,108,127]	Yilgarn Craton	Archean	Archean greenstone	Boundary Murchison Terrane and Southern Cross Province	Archean	N-S	~10 km?	Yes
Marryat Creek	[128,129,130,131]	Musgrave Block	Mesoproterozoic	Fregon Domain	Mann Fault	Neoproterozoic	ENE-WSW, ~1km wide suture	<0.5 km	Yes (part)
Kunayungku ^	[66,68]	Wiso Basin	Neoproterozoic – Cambrian	–	–	–	–	–	–
Lake Surprise west ^	[66,68]	Tennant Creek Region	Paleoproterozoic	Warramunga Province	–	–	–	–	–
Lake Surprise east ^	[66,68]	Tennant Creek Region	Paleoproterozoic	Warramunga Province	–	–	–	–	–
Katanning,	[91,108,127]	Yilgarn Craton	Archean	Boddington Terrane	–	–	–	–	–
Pukatja	[128,129,130,131]	Musgrave Block	Mesoproterozoic	Fregon Domain	Woodroffe Thrust	Neoproterozoic	NE-SW, ~30° S, ~3 km wide suture	~10 km on HW	No
Petermann	[116,128,129,130,131]	Musgrave Block	Mesoproterozoic	Fregon Domain	Woodroffe Thrust	Neoproterozoic	NW-SE, ~30° S, ~3 km wide suture	~ 10 km on HW	Yes
Lake Muir		Albany Fraser Orogen	Proterozoic	Biranup Zone	Boundary Yilgarn and Albany Fraser Orogen	Mesoproterozoic	E–W, S dipping, ~10–20 km wide shear zone	~ 5–15 km on HW	No

^ Tennant Creek scarp.

Granitic gneiss, migmatite, mylonite, granulite, and/or amphibolite basement rock is observed in trenches or outcrop at <1 m depth at multiple locations along the Petermann (Figure 2), Pukatja, Marryat Creek (Figure 2), Cadoux and Meckering ruptures. Proterozoic basement in the vicinity of the Tennant Creek ruptures is variably overlain by 10 s to 100 s of meters of Phanerozoic basin bedrock. Structural measurements (foliations, intrusive boundaries) for bedrock outcrops within 5 km of surface ruptures are qualitatively well-aligned to surface ruptures in eight of ten events, though dip measurements are only qualitatively well aligned in three cases. This may relate to dip measurement difficulties for heavily weathered bedrock. (Summary of basement/bedrock in Table 4, comprehensive details in EarthArXiv reports [120,121,122,123,124,125,126]).

Nine of ten ruptures align with linear magnetic anomalies (Figure 2) and six align with linear gravity anomalies/gradients. The Katanning rupture does not align with either gravity or magnetics at the scale of available geophysical data (Figure 2, Table 2), and the Lake Muir rupture was not studied in this paper (paper in review: [79]). In cases where surface rupture traces are highly curved, arcuate, and/or segmented (Meckering, Marryat Creek, Tennant Creek, Pukatja), the distinctly-oriented rupture traces all align with distinct orientations of linear geophysical anomalies interpreted as faults, dikes, and lithological contacts (e.g., [33]).

Figure 2. Examples of the relationship between geophysical data and surface outcrop to historic ruptures (a) national total magnetic intensity map with ruptures overlaid, and dashed lines indicating linear anomalies (b) interpreted basement geology around the three Tennant Creek scarps (no basement outcrops at the surface) demonstrating strong correlation between intrusive/lithological boundaries, basement faults, and historic surface rupture (legend heavily simplified to show lithologies around the ruptures, more details in EarthArXiv report [126] legend and original map. Map used under creative commons NT Gov) (c) examples of surface outcrop structures visible in basement around the Marryat Creek rupture including three sets of dike/foliation/fault orientations coincident with the three major orientations of the historic rupture, uninterpreted satellite imagery insets (i) and (ii) available in Marryat Creek EarthArXiv report [123] (d) example of mylonite foliation orientation along a section of the Petermann rupture where outcrop occurs within the primary rupture zone.

Table 4. Degree of alignment between rupture, basement structures, and geophysical anomalies.

Rupture	Refs.	Mapped Basement							Geophysics				Evidence of Basement Control on Rupture
Rupture	Refs.	Description	Depth (m)	Method *	Dominant Strikes	Alignment	Dips	Alignment	Mag.	Alignment	Gravity	Alignment	Y/N	Type ^#
Meckering	[16,25,33,114]	Granites, gneiss, mafic dikes	0–20	Geol.	NW, SW	Mod.	55°–90°	Low	Yes	Very high	Part	Mod.	Y ¹	FL_GS, V_S, D_G, FD_GS
Calingiri	[25,114]	Migmatite, gneiss	0–20	Geol.	NE	High	60°–90°	Low	Yes	High	Yes	High	Y	FL/FD_G
Cadoux	[41,115]	Granite, gneiss, mafic dikes	0–20	Geol. + BH	N, NW, NE, W	High	50°–90°	Mod.–High	Yes	Very high	Yes	Mod.	Y ²	FL_GS, V_S, D_G
Marryat Creek	[47,48,117]	Mylonite, gneiss, granite, mafic dikes	0–5	Geol. + BH	W, NNE, NE	Very high	–	–	Yes	Very high	Part	High	Y ³	FL_GS, FT_GS, D_GS
Kunayungku ^	[50,51,52,66,68,132]	Schist, granite	50+	BH + Geo.Int.	NE	Very high	–	–	Yes	High	Yes	Very high	Y ⁴	FT_G
Lake Surprise west ^	[50,51,66,68,132]	Metavolc., metased., granite	?20+	BH + Geo.Int.	NW	Very high	–	–	Yes	Very high	No		Y ⁵	FT_G, L_G
Lake Surprise east ^	[50,51,66,68,132]	Metavolc., metased., granite	50+	BH + Geo.Int.	NE	Very high	–	–	Yes	Very high	Yes	High	Y	FT_G, L_G
Katanning,	[133]	Granite, gneiss	–	Geol.	NW	Very low	–	–	No	–	No	–	N
Pukatja	[9]	Granite, gneiss	0–10	Geol.	NE	High	30°	Very high	Yes	Very high	No	–	Y ⁶	L_GS, FL_GS
Petermann	[73,128,134]	Mylonite	0–10	Geol. + BH	NW	Very high	20°–50°	Very high	Yes	Very high	Yes	Very high	Y ⁷	FL_GS

^ Tennant Creek scarp. * 1:250,000 surface geology map (Geol.), ground-water borehole records (BH), geophysical interpretation (Geo.Int.). ^# Evidence for basement control: foliation (FL); fault (FT); fold (FD); vein (V); dike (D); lithological/batholith (L); geophysical (_G)/surface (_S) with specific examples detailed below: ¹ Rupture along brecciated quartz in cutting / trench [25]. ² Tank scarp ruptures through surface granite, and along a quartz vein in a hand-dug trench; bedrock within 10 m of the Kalajzic scarp aligned with rupture [41]. ³ Two trenches confirm rupture occurred along a pre-existing Proterozoic fault [118]. ⁴ Normal fault interpreted below Kunayungku scarp from ground-water boreholes and geophysical data prior to rupture (1981) [52,59]. ⁵ Lake Surprise west scarp runs along a 1–2 m high quartz ridge, associated with fluid movement along a bedrock fault [59,63,64]. Bedrock does not outcrop at the surface. ⁶ Rupture aligns with the projected boundary between a granite batholith and granulite facies gneiss; rupture curves around outcrop of granite batholith [9]. ⁷ Rupture abuts mylonite outcrop with the same strike and dip; mylonite with the same strike and dip outcrops within 1 m of the scarp in multiple locations [73].

3.2. Seismology

The sparse nature of the Australian National Seismograph Network (https://www.fdsn.org/networks/detail/AU/) results in large (i.e., ≥5–10 km) uncertainties in earthquake epicenter and hypocenter location estimates that are difficult to quantify, including those for the earthquakes studied here [102]. Epicentral determinations (Figure 3, Figure 4, Figure 5, Figure 6, Figure 7, Figure 8, Figure 9 and Figure 10) are typically not sufficiently accurate to unambiguously associate with surface ruptures. Six of ten ruptures have favored epicenter locations that are located on the rupture hanging-wall, within approximated positional uncertainty bounds.

Many publications do not state statistical uncertainties for their epicenter locations. Uncertainties listed in Table 5 include published uncertainties or an assigned value of ± 10 km where no uncertainties are available [102]. Epicenters with lower uncertainties are derived using a variety of relocation methods including extra analysis (e.g., InSAR slip distributions, joint hypocenter determination) or extra data (e.g., surface rupture location, aftershocks from temporary seismometer arrays) (comprehensive details in EarthArXiv reports [120,121,122,123,124,125,126]). The epistemic uncertainty relating to the quality of velocity models used to locate epicenters is unconstrainted but appears to be one of the major sources of inaccurate locations where instrumentation is particularly sparse. For instance, epicenters for Pukatja and Marryat Creek are located up to 17 and 30 km from the identified surface rupture respectively, showing large uncertainties still affecting remote earthquake locations between 1986–2012.

Hypocenters derived from mainshock instrumental data do not project onto rupture planes as defined by surface rupture for any of the studied events. Hypocentral depth estimates based on aftershock data and relocated epicenter locations suggest depths of <5 km (for Tennant Creek [59], Petermann [73] and Meckering [37]). Centroid moment tensor depths are <6 km depth, with the authors’ preferred best-fits all <4 km depth (Meckering [26,27,28]; Cadoux [28]; Marryat Creek [28]; Tennant Creek [55]; Katanning [70]; Petermann [74]).

Epicentral location uncertainties limit the study of rupture propagation directions(s) for most events. Model scenarios for the Meckering earthquake support a bilateral rupture [37]. Unilateral upwards propagation has been proposed for the first Tennant Creek mainshock, complex propagation in the second mainshock, and unilateral upwards propagation to the Southeast in the third mainshock (all on separate faults) [57].

Seven of ten events show foreshock activity within six months and 50 km of the mainshock epicenter and six of ten show instrumentally recorded prior seismicity (more than five events within 10 years and 50 km). Precise locations are difficult to obtain due to epistemic and statistical uncertainties, particularly for assessing seismicity prior to 1980 due to sparse instrumentation [102]. Aftershock data are inherently incomplete for most events due to sparse instrumentation. However, temporary seismometers were deployed following most events and magnitude completeness from the national network is >3.0 Mw for all events [102] (though, the locations of these events are generally highly uncertain compared to the temporary arrays, as discussed above). The Musgrave block events (Marryat Creek, Pukatja, Petermann, Figure 1, Table 3) show less aftershock activity in comparison to the Tennant Creek and Western Australia earthquakes (Meckering, Calingiri, Cadoux) which had extended aftershock sequences [5,34].

Table 5. Summary of seismological data and interpretations for each rupture.

Rupture	Refs.	Published Epicenters		Located on Hanging-Wall		Hypocenter Depth ¹ (km)		Focal Mechanisms				Rup. Propagation	Foreshocks ⁴	Prior Seismicity ⁵
Rupture	Refs.	N=	Uncert. ² (km)	Initial	Relocated	Range	Uncert.	N=	CMT Depth ³ (km)	Dip Range	Strike Corr. with Rupture?	Rup. Propagation	Foreshocks ⁴	Prior Seismicity ⁵
Meckering	[11,12,15,18,23,24,25,26,28,90]	8	~10	1	2	2.5–13	1–10 km	4	1.5–3	29°–45°	Yes	Bilateral	Yes	Yes
Calingiri	[11,23,25,38]	2	~10	0	1	1–15	>5	1		50°	Yes	Unknown	Yes	Yes
Cadoux	[11,28,40,41,43]	6	~10	N/A ⁶	N/A ⁶	3–15	>5	4	4–6	N/A ⁶	Part ⁶	Unknown	Yes	Yes
Marryat Creek	[11,28,46,47,88]	7	>10	0	1	5–19	>5	3	0–3	35°–67°	Part	Unknown	No	No
Kunayungku ^	[11,55,57,60,61,63]	4	2–10	?	0	5–6.5	1–4	4	2.7	35°–55°	Yes	Unilateral	Yes	Yes
Lake Surprise west ^	[11,55,57,60,61,63]	4	2–10	?	2	3–4	0.5–3	4	3.0	38°–70°	Part ⁷	Unknown	Yes	Yes
Lake Surprise east ^	[11,55,57,60,61,63]	4	2–10	?	4	4.5–5	0.5–3	4	4.2	36°–45°	Yes	Unilateral	Yes	Yes
Katanning,	[70]	3	0.04–5	0	2	<1		1		43°	Yes	Unknown	No	No
Pukatja	[9,11]	6	>10	0	1	4–12	5?	3		45°–72°	Yes	Unknown	No	No
Petermann	[73,74,75]	6	2.5–8	4	2	1–10	> 5	4	1–2	26°–52°	Yes	Unknown	yes	No

^ Tennant Creek scarp. ¹ Includes both initial hypocentral depth estimates, and revised depths based on aftershock depths and locations, uncertainties from source literature. ² Epicenter uncertainty based on published uncertainties and/or estimate based on published uncertainties for similar events. ³ Centroid moment tensor depth, preferred value from publication. ⁴ Earthquake within 6 months and 50 km of epicenter (affected by catalogue completeness for very remote events, see EarthArXiv reports ([120,121,122,123,124,125,126]) for details). ⁵ Earthquakes (n > 5) within 10 years and 50 km of the epicenter (affected by catalogue completeness for very remote events, see EarthArXiv reports for details). ⁶ Geometry of the seismogenic fault is unclear as scarps in the Cadoux rupture dip both east and west. ⁷ Waveform analysis of the second Tennant Creek mainshock show complicated rupture, potentially related to complex fault interaction

3.3. Surface Ruptures

Methods for the original mapping of individual ruptures are summarized in Table 6 and give some indication of data quality (explored in more detail in EarthArXiv reports [120,121,122,123,124,125,126]). Some readjustment of terminology and classification is required when considering the earlier ruptures (e.g., ‘fault’ may refer to both primary rupture and secondary fractures) and considerable detail of rupture morphology was lost between fine-scale (i.e., 1:500) and whole rupture (1:25,000–1:50,000) for pre-digital maps (Meckering to Tennant Creek). Six of ten ruptures are concave relative to the hanging-wall, three are straight and one is slightly convex (Petermann) (Table 6). All ruptures are reverse, and only two events have surface measurements consistent with secondary lateral movement (Meckering: dextral; Calingiri: sinistral; Table 6, explored in individual EarthArXiv reports [120,121,122,123,124,125,126]).

Nine of ten ruptures studied (Katanning was excluded due to lack of field mapping) show a relationship between surface sediments/bedrock depth to rupture morphology. Discrete rupture and duplexing rupture are more common where bedrock is close to the surface or surface sediments are predominately calcrete/ferricrete/silcrete. Where sands dominate in the surface sediments, rupture tends to present as warping and folding, or correspond with breaks in visible surface rupture (e.g., Petermann: morphology explored in individual EarthArXiv report [125])).

Figure 3, Figure 4, Figure 5, Figure 6, Figure 7, Figure 8, Figure 9 and Figure 10 show digitized versions of published primary ruptures, secondary fracturing, and dip values measured at the surface. Primary sources inconsistently derive published length values to describe their mapped rupture (Table 1 and Table 6; explored in detail in EarthArXiv reports [120,121,122,123,124,125,126]) which are then used in secondary sources including scaling relationships. This includes simplifying scarps to straight lengths (Calingiri, Cadoux, Marryat Creek), capturing along-rupture complexity to varying degrees (Pukatja, Tennant Creek), excluding segments that have length, offset and morphology characteristics of primary rupture (Meckering, Tennant Creek, Cadoux), and reporting InSAR derived lengths rather than visible rupture (Katanning). (Explored in more detail in individual EarthArXiv reports [120,121,122,123,124,125,126]).

Measurements of rupture length in the past have been inconsistent in their approach. Here, we re-classify mapped primary ruptures from original primary sources in order to generate a consistent rupture length dataset (Table 6). We simplify ruptures to straight lines and define new faults where mapped primary rupture has gaps/steps > 1 km and/or where strike changes by > 20° for distances > 1km [135]. The Splinter and Burges scarps (Meckering), Lake Surprise west foot-wall scarp (Tennant Creek), and individual Cadoux scarps were not included in original published lengths. These features show offsets, lengths, and locations consistent with primary slip along basement structures proximal to the main scarps, and therefore we include them in our length values.

Where InSAR is available (Katanning and Petermann) we present fault lengths described by both visible rupture and InSAR (Table 6). Visible rupture in the Petermann event was highly segmented due to ineffective rupture propagation through sand dunes up to six metres high [73]. Due to this we apply a slightly altered set of criteria to this event, faults are defined where strike of visible rupture and InSAR changes by > 20° and/or where steps in InSAR and visible rupture are > 1 km (Figure 10) [75,78].

Under these criteria seven of ten ruptures have more than one source fault defined (i.e., a multi-fault rupture). The total length of faulting is the same as published values for two events, increases by 2%–51% for four events relative to published length, and decreases by 4%–60% for three events (Table 1 and Table 6). These lengths describe primary surface ruptures in a consistent way, accounting for all segments of rupture which show evidence of slip along basement structures. Our preferred length for each rupture, including uncertainties, is presented in Table 1 and Table 6.

Table 6. Summary of surface measurements for each rupture.

Rupture	Refs.	Method ³	Shape ⁴	Published			Simplified Faults ¹			Preferred:		Displacement ² (m)						Disp. Profile Shape ⁶
Rupture	Refs.	Method ³	Shape ⁴	Length (km)	Kin.	Dip Range	N=	Sum Length (km)	% Diff. Publ.	Length (km)	Dip	Max Vert. Disp.	Avg. Vert. Disp. ⁵	% Diff.	Max Net Slip	Avg. Net Slip ⁵	% Diff	Disp. Profile Shape ⁶
Meckering	[25]	FW; A; S_B	CC	37	R(D)	15–54°	4	44.4	+20%	40 ± 5	35° ± 10	1.98	0.97	51%	3.7	1.78	52%	S. Tg.
(Splinter)	[25]			9	R	24–42°	3	44.4	+20%	40 ± 5	35° ± 10	0.67	0.22	67%	1.34	0.44	67%	AS. Tg.
Calingiri	[25]	FW	S	3.3	R(S)	12–31°	1	3.3	0%	3.3 ± 0.2	20° ± 10	0.38	0.15	61%	1.26	0.46	63%	AS. Tg.
Cadoux	[41]	FW; A; S_B	CC/S	14	R	20–80°	6	20.6	+47%	20 ± 5	60° ± 30	1.4	0.35	75%	1.79	0.45	75%	AS. Tg.
Marryat Creek	[48]	FW; A; S_C	CC	13	R	36–60°	3	13.6	+4%	13 ± 1	40° ± 10	0.9	0.21	77%	1.07	0.31	71%	Avg.
Kunayungku	[63]	FW; A; S_C	S	10.2	R	58°	1	8.6	−15%	9 ± 1	40° ± 5	0.9	0.36	60%	1.41	0.55	61%	S. Tg
Lake Surprise west	[63]	FW; A; S_C	CC	6.7	R	65–84°	1	10.1	+51%	9 ± 2	60° ± 10	1.13	0.45	60%	2.26	0.84	63%	AS. Sine
(LS west foot-wall)	[63]			3.1	R		1	10.1	+51%	9 ± 2	60° ± 10	0.74	0.43	42%	1.16	0.9	22%	Avg.
Lake Surprise east	[63]	FW; A; S_C	CC	16	R	28–30°	2	15.3	−4%	16 ± 0.5	35° ± 5	1.8	0.61	66%	3.6	1.23	66%	Avg
Katanning (visible) ⁷	[70,71]		S	0.3	R		1	0.3	0 %	0.5 ± 0.5	40° ± 5	0.1
Katanning (InSAR)	[70]	In.		2.5 ⁸			1	2.2	−12%	0.5 ± 0.5	40° ± 5	0.2⁸	0.1	50%	0.32 *	0.2 *	38%	AS. Tg.
Pukatja	[9]	FW	CC	1.6	R	22–28°	1	1.0	−60%	1.3 ± 0.3	30° ± 10	0.48	0.12	75%	0.96	0.25	74%	AS. Sine
Petermann (visible)	[73,77]	FW; S_C; In; D; SI	CV	20	R	25–36°	3	21	+5%	21 ± 0.5	30° ± 5	0.96	0.2		1.92	0.42	78%	Avg.
Petermann (InSAR)	[73]	In.		21			2	21.5	+2%	21 ± 0.5	30° ± 5

¹ Where mapped primary rupture has a gap/step > 1 km and/or change in strike > 20° across a length > 1 km (except where InSAR is available to validate rupture continuing along strike across gaps > 1 km). Lengths of individual faults available in EarthArXiv reports [120,121,122,123,124,125,126]. ² Vertical and lateral displacements digitized from original publications. Net slip calculated for this study. ³ Original mapping method: Field work (FW); aerial photographs (A); surveying (levelling, cadastral or GPS) basic (S_B), comprehensive (S_C); InSAR (In); Drone (D); Satellite (SI). ⁴ Concave (CC) relative to hanging-wall, convex (CV) relative to hanging-wall, straight (minor deviations but overall straight shape). ⁵ Length weighted average across 0.5 km increments (where rupture length > 5 km) or 0.1 km increments (where rupture length < 5 km). ⁶ Profile shape based on Wesnousky (2008) [7] from visual fit (e.g., not best-fit regression curves): symmetrical (S); asymmetrical (AS); triangle (Tg); sine; average line (Avg). ⁷ Katanning visible surface rupture was observed, but no field mapping was conducted [70,71]. Original and subsequent publications describe Katanning length based on best-fit InSAR-derived source parameters (1.26 km) [70], rather than length of InSAR trace (2.5 km). Offset comes from field estimates (0.1 m) and fault modelling from InSAR data [70].

Figure 3. 1968 Mw 6.6 Meckering earthquake (a) rupture and fracture map of Meckering and Splinter scarps [25] with faults labelled as per displacement graphs, trench location from [37] (b) published epicenter locations, open stars show approximate locations of epicenters without published coordinates (c) selected dip measurements of scarp and displacement of resurveyed road bench marks [25] (d) graphs of along-rupture vertical and lateral displacement measurements and net slip calculations [25] and net slip calculated from available data averaged over 0.5 km increments (this study) (e) focal mechanisms (red line shows preferred plane from original publication) from (i) Fitch et al., 1973, (ii) Fitch et al., 1993 & Leonard et al., 2002, (iii) Fredrich et al., 1988, and (iv) Vogfjord and Langston 1987.

Figure 4. 1970 Mw 5.0 Calingiri earthquake (a) rupture and fracture map of Calingiri [25] showing published epicenter locations and dip measurements of scarp [25], focal mechanism (red line shows preferred plane from original publication) from Fitch et al., 1973 (b) graph of along-rupture vertical and lateral displacement measurements [25] and net slip calculated from available data averaged over 0.1 km increments (this study).

Figure 5. 1979 Mw 6.1 Cadoux earthquake (a) rupture scarps and fracturing involved in the Cadoux rupture with named faults [41], focal mechanisms from (i) Denham et al., 1987 (ii) Fredrich et al., 1988 (iii) Everingham and Smith (unpublished, Lewis et al., 1981) (iv) CMT (b) available dip measurements, black where directly measured and grey were calculated based on available displacement measurements [41] (c) published epicenter locations (d) graph along-rupture of vertical and lateral displacement measurements and calculated net slip [41] and net slip calculated from available data averaged over 0.5 km increments (this study).

Figure 6. 1986 Mw 5.7 Marryat Creek earthquake (a) rupture and fracture map of Marryat Creek scarp and available dip measurements [48,118] with faults labelled as per displacement graphs, focal mechanisms (red line shows preferred plane from original publication) from (i) Fredrich et al., 1968, (ii) Barlow et al., 1986, (iii) CMT, trench location from [118], (b) published epicenter locations, and (c) graph of along-rupture vertical and lateral displacement measurements [48] and net slip calculated from available data averaged over 0.5 km increments (this study).

Figure 7. 1988 Mw 6.3 (TC1), 6.4 (TC2) and 6.6 (TC3) Tennant Creek earthquakes (a) rupture and cracking map of Kunayungku and Lake Surprise scarps with available dip measurements also the locations of trenches from [63] with faults labelled as per displacement graphs, focal mechanisms (red line shows preferred plane from original publication) from (i) McCaffrey 1989, (ii) Choy and Bowman 1990, (iii) Jones et al., 1991, (iv) CMT, (b) published epicenter locations of all three mainshocks (c) resurveyed benchmark offsets [63] uncertainties as discussed in text, and (d) graphs of along-rupture vertical and lateral displacement measurements [63] and net slip calculated from available data averaged over 0.5 km increments (this study).

Figure 8. 2008 Mw 4.7 Katanning earthquake (a) approximate visible rupture and InSAR trace (digitized from [70]), published epicenter locations and focal mechanism [70] (b) graph of along-rupture vertical and displacement taken from InSAR data [70] and net slip calculated from InSAR data (this study).

Figure 9. 2012 Mw 5.2 Pukatja/Ernabella earthquake (a) rupture and fracture map of Pukatja scarp and available dip measurements also the location of hand-dug trench [9], focal mechanisms as described in [9] from (i) Clark et al., 2014, (ii) GCMT, (iii) St Louis University; (b) graph of along-rupture vertical displacement measurements [9] and net slip calculated from available data averaged over 0.1 km increments (this study).

Figure 10. 2016 Mw 6.1 Petermann earthquake (a) rupture and fracture map of Petermann scarp [73] showing published epicenter locations and dip measurements of rupture (also the location of hand-dug trenches), focal mechanisms (i–iii) as described in [73], (i) USGS, (ii) GCMT, (iii) Geofon, and (iv) from Hejrani and Tkalcic 2018; (b) graph of along-rupture vertical displacement measurements and net slip calculated from available data averaged over 0.5 km increments.

Vertical and lateral offsets for all ruptures were digitized from primary literature (see EarthArXiv reports [120,121,122,123,124,125,126] for methods and uncertainties). New net-slip values were calculated for all ruptures from measured offsets, with dips assigned to each field offset measurement based on measured surface dips and/or focal mechanisms (dip measurements from primary literature shown on Figure 3, Figure 4, Figure 5, Figure 6, Figure 7, Figure 8, Figure 9 and Figure 10 and in Table 6—preferred dip from this paper in Table 1 and Table 6). Offset and net-slip data are presented in Figure 3, Figure 4, Figure 5, Figure 6, Figure 7, Figure 8, Figure 9 and Figure 10 along with length weighted averages to reduce bias towards sections of scarp where high number of measurements were taken (generally where offset is higher). Average offset is between 42%–77% lower than the maximum offset for each rupture (Table 6). Displacement data are visually assigned a displacement profile shape [7] with six of ten ruptures best described by triangle profiles (2= symmetrical, 4= asymmetrical), two assigned an asymmetrical sine profile, and three best represented by a straight average profile (Table 6).

Offset data from resurveyed benchmarks (Tennant Creek [62]) and relevelling along infrastructure (Meckering [25]) were digitized from original publications to visualize distributed deformation across the rupture zone (Figure 1 and Figure 7). No uncertainties are reported for the Meckering data [25], though they are likely in the order of Tennant Creek where original authors report uncertainties of ± 9.3–25 cm [62,136]. Despite large uncertainties, the authors of both datasets believe offsets constrain fault geometries and show distributed hanging-wall uplifts (and to a lesser extent, foot-wall depression).

3.4. Environmental Damage

Environmental damage as described in primary literature or visible in published photos for each event were classified under the ESI-07 Scale [10] and summarized in Table 7 (comprehensive details in EarthArXiv reports [120,121,122,123,124,125,126]). Seven of eleven historic ruptures (excluding Katanning) can be described as an ESI IX – X despite having a wide range of lengths, magnitudes, and displacements.

Fracturing/cracking is reported for all historic surface ruptures, but generally only in the immediate vicinity of the surface rupture, captured by the rupture ESI value. This may relate to a lack of far-field mapping but is considered to be fairly representative of the true spatial distribution based on described mapping campaigns. The Meckering and Petermann events have the most aerially extensive fracturing, with areas of 580 and 210 km² respectively. Of the total area covered by Meckering and Petermann fracturing, approximately 70% and 77% respectively is on the hanging-wall.

Where events occurred close to population centers (Meckering, Cadoux, Calingiri) ground water bores showed evidence of seismic fluctuation (no anomalies were identified in Tennant Creek bore data). The only observed liquefaction for any historic rupture comes from Meckering, where multiple sand blows were observed on the hanging-wall along the Mortlock River. Rockfalls are reported for three ruptures. Concentric or polygonal cracking was reported in the Meckering, Calingiri, Cadoux and Petermann events [25,41,73], and holes (possibly related to collapsible soils e.g., [137]) were reported along the rupture on the hanging-wall for Calingiri and Petermann [41,73]. It is possible that tree damage, hydrological effects, rock falls, polygonal cracking, or holes occurred for other ruptures than those listed but were not observed or described. Until the 2012 Pukatja event, field investigations immediately following the event were conducted by hard-rock geologists or seismologists not necessarily familiar with earthquake mapping techniques.

3.5. Paleoseismology and Slip Rate

In total, 14 trenches are described across the Meckering, Calingiri, Cadoux, Marryat Creek, Tennant Creek, Pukatja and Petermann ruptures (Table 8). Tennant Creek, Marryat Creek and Meckering are the only ruptures where detailed palaeoseismic work is published, including multiple trenches, luminescence dating, and soil descriptions and chemistry [37,63].

Table 7. Summary of environmental effects described for each rupture, assigned ESI level, and approximate area around, or distance from, rupture.

Name	Rupture		Fractures		Displaced Rocks		Sand Blows		Tree Shaking		Slope/Rock fall		Hydrology ¹		Holes [41,73]	Concentric Fracturing [25,41,73]	Vegetation Death/Root Tear along Rupture [9,25,47,48,63,73]
Name	ESI	Area (km²)	ESI	Area (km²)	ESI	Area (km²)	ESI	Area (km²)	ESI	Area (km²)	ESI	Dist. (km)	ESI	Dist. (km)	Holes [41,73]	Concentric Fracturing [25,41,73]	Vegetation Death/Root Tear along Rupture [9,25,47,48,63,73]
Meckering	X	190	VIII	580	–		V	100	●		IV	200	IV	200	–	□	□
Calingiri	IX	2	VII	3	*		–		–		–		–		□	□	□
Cadoux	IX	50	VI	55	–		–		●		–		IV	250	–	□	–
Marryat Creek	X	20	VII	20	–		–		–		–		–		–	–	□
Tennant Creek ^	X	160	VIII	160	–		–		–		–		●		–	–	□
Katanning,	VIII	0.2	–		–		–		–		–		–		–	–	–
Pukatja	IX	1	VII	1	–		–		*		VII	15	–		–	–	□
Petermann	X	12.5	VII	210	IX	290	●		VI	20	VII	20	–		□	□	□
Lake Muir	IX		*		–		–		*		–		*		–	–	–

^ Treating the three Tennant Creek scarps as individual or combined results in the same ESI values. Area given is for a combined scarp. Magnitude is for largest mainshock. ¹ Anomalous ground-water levels recorded following earthquake. – No data or observations published. □ Observations of damage outside of ESI-07 descriptions. ● Damage noted as explicitly not present. * Evidence of damage but no detailed description.

Table 8. Summary of available paleoseismic trenching.

Rupture	Ref.	Location	Bedrock			Sediments		Pre-Existing:		Possible Rup. Since 100 ka
Rupture	Ref.	Location	Desc.	Age	Depth (m) (HW/FW)	Desc.	Age *	Cenozoic Offset	Bedrock Offset	Possible Rup. Since 100 ka
Meckering 1	[34,36,37]	Tributary of river	Not exposed		>3	Fluvial sands	Late Pleistocene	No	No	N
Meckering 2	[34,36,37]	Farmland	Altered granite	Archean	<1.5	Ferricrete / sand	T?/Holocene	No	Maybe ¹	N
Calingiri	[25]							No	Maybe ¹
Cadoux/Carter scarp	[41]	Farmland	Altered granite	Archean	<0.5	Sand/soil	Q?	No	No
Cadoux/Tank scarp	[41]	Farmland	Granite	Archean	0?			No	No
Marryat Creek west	[118]	10m N of dry creek	Altered gneiss	Proterozoic	<0.3	Ferricrete / eolian sand	T?/<130 ka	No	No	N
Marryat Creek south	[118]	‘Near’ dry creek	Altered greenstone	Proterozoic	<1.25	Ferricrete/gravel, eolian sand	T?/<130 ka	No	No	N
Kunayungku	[63]	Max vert. disp.	Altered sedimentary rock	Cambrian?	<2	Ferricrete/eolian sand	T?/<30 ka	No	No	N
Lake Surprise east	[63]	Max vert. disp.	Not exposed		>2	Ferricrete/eolian sand	T?/<46 ka	No	No	N
Lake Surprise west 1	[63]	Monoclinal rupture (near quartz ridge)	Altered “iron-rich quartzite”	Cambrian?	<0.5/>2	Gravel/eolian sand	Q/<50 ka	No	Yes ³	Y
Lake Surprise west 2	[63]	Discrete rupture (375m E LSW-1)	Altered “hematitic quartzite”	Cambrian?	<0.5/>0.7	Ferricrete/gravel/eolian sand	T?/Q/<50 ka	Maybe ²	Yes ³	Y
Pukatja	[9]	Max. vert. disp.	Not exposed		>1.5	Sand	~10⁴–10⁵	No	No	Y
Petermann 1	Unpub.	Paleovalley	Not exposed		>1.5	Calcrete/eolian sand	T?/Q	No	No	N
Petermann 2	Unpub.	Inter-dune region	Not exposed		>1.5	Calcrete/eolian sand	T?/Q	No	No	N

* ages in bold from direct dating in literature, italics inferred based on nearby dating, underline from estimate in literature, “T?” or “Q?” estimated Tertiary or Quaternary. ¹ Thicker soil horizons described on foot-wall relative to hanging-wall [25]. ² Fissure of potentially seismic origin filled with gravel, overlain by eolian sand; fracture through ferricrete overlain by gravel and eolian sand [63]. ³ Authors propose three possible origins: earthquake rupture bedrock offset; paleochannel along pre-existing bedrock structure; or combination of both; paleotopography greater than twice the height of historic slip [63].

Of seven ruptures with detailed trench data (Table 8), five show evidence of no rupture since the lake Pleistocene (Meckering, Marryat Creek, Kunayungku, Lake Surprise east, Petermann). The only evidence of a pre-existing bedrock scarp exposed in any trench occurs in the second Lake Surprise west trench, and no clear evidence was found to support a seismic-offset origin for this topography (see EarthArXiv report [126] for more detail). Penultimate ruptures since 100 ka are possible for two of seven of these earthquake events, where sediments are estimated to be <100 ka in age, and where either no ferricrete/bedrock is exposed (Pukatja), or a bedrock scarp exists prior to overlying sedimentation (Lake Surprise west) (Table 8).

Maximum slip rates are calculated by applying minimum and maximum erosion rates for bedrock to determine the amount of slip (from average observed historic slip (Table 6)) that could have accumulated and been removed in the past million years. Minimum (0.3 m Myr⁻¹) and maximum (5.7 m Myr⁻¹) cosmogenic nuclide erosion rates from crystalline bedrock inselbergs across the Precambrian crust of central Australia (Figure 1) [138] are applied for ruptures where crystalline basement is exposed in trenches or observed at the surface within two meters of rupture (implying shallow bedrock). Where trenching exposed ferricrete or quartzite, cosmogenic nuclide erosion rates for quartzite exposed on flat bedrock summits in the Flinders Ranges are applied (5–10 m Myr⁻¹) [109].

Applying erosion rates from inselbergs and quartzite bedrock summits to surface bedrock across the different cratonic and erosional environments in which ruptures occurred (e.g., Figure 1) introduces uncertainties that are unavoidable due to a lack of more appropriate erosion data. Based on a lack of evidence of any preceding ruptures for any of the historic events, including topographic or geomorphic, we prefer the minimum erosional estimates, giving maximum slip rates of 0.2–9.1 m Myr⁻¹.

Table 9. Maximum slip rates based on minimum and maximum bedrock erosion rates [109,138] and length-weighted average net-slip values (Table 6).

Name	Rate Applied *	Mw	Pref. Length (km)	Avg. Net-Slip (m)	Maximum Slip Rate (m/Myr)
Name	Rate Applied *	Mw	Pref. Length (km)	Avg. Net-Slip (m)	Min.	Max.	Mean
Meckering	CB	6.59	40 ± 5	1.78	0.2	3.2	1.7
Calingiri	CB	5.03	3.3 ± 0.2	0.46	0.7	12.4	6.6
Cadoux	CB	6.1	20 ± 5	0.45	0.7	12.7	6.7
Marryat Creek	CB	5.7	13 ± 1	0.31	1	18.4	9.7
Kunayungku	Q	6.27	9 ± 1	0.55	9.1	18.2	13.7
Lake Surprise west	Q	6.44	9 ± 2	0.84	6	11.9	8.9
Lake Surprise east *	Q	6.58	16 ± 0.5	1.23	4.1	8.1	6.1
Katanning (InSAR)	CB	4.7	0.5 ± 0.5	0.2	1.5	28.5	15
Pukatja	CB	5.18	1.3 ± 0.3	0.25	1.2	22.8	12
Petermann	CB	6.1	21 ± 0.5	0.42	0.7	13.6	7.2

* Erosion rate for crystalline basement (CB) [138]; erosion rate for quartzite (Q) [109].

4. Discussion-Lessons from the Last 50 Years of Australian Surface Ruptures

4.1. Inconsistancies in Data Use

A number of inconsistent uses of data were found while reviewing papers that reference primary sources, as summarized below:

Some of the original Marryat Creek vertical offset measurements are reproduced incorrectly in subsequent publications [7,118]. We recommend referring to the original source [48] or the data tables from this paper.
Limbs of the Marryat Creek rupture show sinistral (west limb) and dextral (south limb) components due to SW over NE directed uplift along an arcuate rupture (best described as three faults, Figure 2 and Figure 6). Data tables used in subsequent scaling relationships [6] describe the event as left-lateral based on one of three published focal mechanisms. We recommend a dominantly reverse mechanism for this event based on all available data.
We recommend referring to the original source of the Calingiri focal mechanism [23] when describing kinematics and preferred rupture plane geometry, as subsequent authors [25] appear to misread the mechanism [121].
The Tennant Creek rupture has been treated by multiple authors as a single rupture length for fault scaling relationships [7,8,104,139,140] and hazard mapping [119,141,142] as opposed to three separate earthquakes and associated ruptures [6,143,144,145], a decision which significantly changes the length to magnitude ratio and slip distribution relative to an averaged epicentre location and magnitude.
An instance of the above decision is seen where a 6 km step over between Tennant Creek scarps is identified as an outlier for reverse fault data [7]. The rupture length and complexity for this event is not anomalous if treated as three separate events.
Some scaling relationships (e.g., [7]) define only a portion of the Cadoux scarp (the 10km long Robb Scarp), due to “insufficient mapping” of the northern ~6 km. The full rupture includes one step-over that fits the publication analysis criteria (>1 km) but is not represented in the original paper’s database [7] and subsequent work [8,139,146]. Mapping of the Cadoux rupture was thorough, but uncertainty regarding which of the mapped scarps (if any) represent the Cadoux mainshock fault complicates the use of this event in scaling relationships.
A slip rate of 0.005 mm/yr is used to describe the Marryat Creek scarp [147]. This value is likely derived from ~0.5 m measured historic slip in a trench with no evidence of prior rupture between deposition of Quaternary sediments (estimated age from primary source < 130 ka [63]) and formation of the structure along which the modern event ruptured (Proterozoic) [118]. While evidence of prior Quaternary–Tertiary rupture may have been removed by erosion, a slip rate of 0.5 m per 100,000 years is unsupported by available evidence.
The recently published NSHA18 applies slip rates of 4–8 m/Myr for the historic ruptures discussed in this paper [119,141]. No historic surface ruptures provide convincing evidence of rupture between deposition of Quaternary sediments (50 ka to late Pleistocene) and formation of the host structure (Archean–Cambrian). At least for cratonic areas of Australia (Figure 1), questions arise as to whether historically seismogenic faults are recurrent at all, or if long-term seismic release may be hosted across unique basement structures (e.g., [4]), as well as on recurrent structures (e.g., Lort River, Hyden, Dumbleyung [2,34,108]). We recommend caution in applying these rates in future work.

4.2. Surface rupture Bedrock Controls, Updated Datasets and Environmental Intensity

Analysis of geology and reanalysis of mapped ruptures presented in this paper suggest that in four of the ten events studied (Meckering, Marryat Creek, Cadoux and Peterman) rupture propagated across 2–6 bedrock-controlled faults (e.g., pre-existing fractures and/or foliation planes and/or lithological boundaries and/or intrusive boundaries), and nine of ten events show strong basement controls on rupture location and orientation. Simplistic projection of surface defined faults using our preferred dips results in faults intersecting at depths that are consistent with published centroid depths (e.g., <4 km) in three of the four events with more than one fault defined (Petermann excluded). In all four cases, fault intersections project up-dip to the area of maximum vertical offset (in the case of Petermann, maximum dip occurs where the two faults overlap). It is uncertain with available seismic data whether hypocenters align with these projected fault intersections, and more data would be required to show that surface defined faults can be extended to depth along planar slip zones. However, linear geophysical anomalies in many cases show ruptures associated with basement conjugate fracture/dike orientations underlying rupture, suggesting strong control of the crustal architecture on intraplate earthquake nucleation and/or propagation.

New length, dip, and net-slip data presented for historic ruptures are derived by applying consistent framework and methodology. Past scaling relationships have included and excluded Australian surface rupturing events inconsistently, generally without clear explanation. They have also relied on vertical offset measurements as most of the original publications do not calculate net-slip. Length-weighted averages of net-slip values calculated in this paper are 32%–67% larger than those for vertical offset data, and maximum net-slip is 68%–89% higher than maximum vertical offset. This suggests that Australian events may be systematically misrepresented in past scaling relationships. Our new data, compiled by thorough analysis of available seismological and field data, and coupled with the recent revision of magnitude values [11], will facilitate more consistent integration of Australian events into earthquake catalogues and displacement-length scaling relationships.

In Table 10 we compare the calculated M_w, area and average displacement from SCR dip-slip scaling relationships of [148] using the surface rupture length used in developing the scaling relationships with the length from this paper. Table 10 then compares the difference between calculated average displacement and magnitude as derived using length of this paper and SCR dip-slip scaling relationship [148] with the average net slip derived from this paper, and update M_w values [11]. Results show differences of over 600% between scaling relationship average displacement and calculated average net slip values of this paper, and up to 18.7% difference in calculated M_w and updated values [11]. This highlights the need to investigate length, magnitude, and net-slip inputs of previous scaling relationships.

Most vertical displacement data for historic surface ruptures are collected as spot-height measurements of foot-wall elevation relative to hanging-wall elevation proximal to the surface trace. Less frequently, scarp perpendicular profiles are captured 5–50 m either side of the rupture. Satellite-based imaging of recent scarps (Petermann [75,77,78], Katanning [70], Lake Muir ([79])) shows permanent distributed displacement of the hanging-wall, and to a lesser degree of the foot-wall that is not captured by these spot-heights and short traverses. Specifically, InSAR imaging shows distributed deformation extending hundreds of metres to kilometres perpendicular to surface scarps [78], and extending along-strike for kilometres beyond the surface rupture detectable in the field [70,78,79]. This is particularly the case for smaller earthquakes (Katanning [70] (Figure 8) and Lake Muir (in review [79])), where the rupture ellipse only partially intersects the surface. Without these satellite derived deformation imaging techniques, the degree to which field observations and spot-height measurements along the visible surface rupture underestimate the length, height and width of surface deformation along a fault cannot be quantified.

Digitized offset data from resurveyed benchmarks across the Tennant Creek (Figure 7), Meckering (Figure 3) and Cadoux (EarthArXiv report [122]) ruptures provide evidence of distributed hanging-wall offset, though published uncertainties are on the order of measured offsets and data should be interpreted with caution. This data cannot be improved upon within the resolution of pre-deformation height data but suggests that the deformation envelope extends beyond the discrete surface rupture, and offset measurements as presented in Figure 3, Figure 4, Figure 5, Figure 6, Figure 7, Figure 8, Figure 9 and Figure 10 may underestimate the true total vertical displacement values for each event. The ratio of distributed deformation to discrete deformation at a rupture tip might be expected to be larger for surface rupture segments that are more modest in vertical displacement, or cut through relatively more weathered regolith or thicker sedimentary deposits, as much of the initial deformation will be taken up as folding prior to the emergence of the fault tip [149].

This paper reviews primary literature to identify environmental earthquake effects (EEEs) for the purposes of applying the ESI-07 Scale [10,150] to Australian surface rupturing earthquakes. We find that the majority of environmental damage is observed in the immediate rupture zone, with the exception of rare rockfalls in prone-areas (e.g., road cuttings) at distances of ~200 km, and rare ground-water fluctuations up to 250 km away for some but not all events where ground water data was investigated. While this dataset likely does not capture the full range of potential ESI values and affected area due to sparse reporting of EEEs in the literature, it does provide a basis for comparing the maximum ESI and magnitude of reverse earthquakes in intraplate, low-topography, near-surface crystalline bedrock (in most cases), and generally arid settings against events in tectonically and geomorphically diverse regions (e.g., [151,152,153,154,155,156,157,158,159]).

Table 10. Comparisons between calculated magnitude, area and displacement from previous length scaling relationship [148] using surface rupture length from [148] and length from this paper.

Name	Leonard 2014 [148]		Calculated [148]			This Paper	Calculated (This Paper)			Percent Difference Calculated			Avg. Net Slip ⁵	% Diff ⁶	M_w [11]	% Diff ⁶
Name	SRL ¹ (km)	Source	Mw ²	A ³ (km²)	D ⁴ (m)	L (km)	Mw ²	A ³ (km²)	D ⁴ (m)	Mw	A (km²)	D (m)	Avg. Net Slip ⁵	% Diff ⁶	M_w [11]	% Diff ⁶
Meckering	37	[160]	6.93	5546	5.44	40	6.99	6316	5.8	0.9%	12.2%	6.3%	1.78	−225.8%	6.59	−6.1%
Calingiri	3.3	[160]	5.18	99	0.73	3.3	5.18	99	0.73	0.0%	0.0%	0.5%	0.46	−58.7%	5.03	−3.0%
Cadoux	14	[160]	6.23	1098	2.42	20	6.49	1989	3.26	4.0%	44.8%	25.8%	0.45	−624.4%	6.1	−6.4%
Marryat Creek	13	[160]	6.18	970	2.27	13	6.18	970	2.27	0.0%	0.0%	−0.2%	0.31	−632.3%	5.7	−8.4%
Kunayungku	10.2	[160]	6	648	1.86	9	5.91	526	1.67	−1.5%	−23.2%	−11.3%	0.55	−203.6%	6.27	5.7%
Lake Surprise west	6.7	[160]	5.7	321	1.31	9	5.91	526	1.67	3.6%	39.0%	21.7%	0.84	−98.8%	6.44	8.2%
Lake Surprise east *	16	[160]	6.33	1372	2.70	16	6.33	1372	2.7	0.0%	0.0%	−0.1%	1.23	−119.5%	6.58	3.8%
Katanning (InSAR)	1.26	[70]	4.49	20	0.33	0.5	3.82	4	0.15	−17.5%	−400.0%	−117.6%	0.2	25.0%	4.7	18.7%
Pukatja	1.6	[9]	4.66	30	0.40	1.3	4.51	21	0.33	−3.3%	−42.9%	−21.2%	0.25	−32.0%	5.18	12.9%

¹ Surface rupture length. ² [148]: M_w = a + b*log(L). ³ [148]: A = C₁L^1+β. ⁴ [148]: D = C₂A^1/2. ⁵ Average net slip calculated in this paper (Table 6). ⁶ Percent difference between calculated average displacement and M_w using length of this paper [148], and average net slip calculated in Table 6, and M_w of [11].

4.3. Recurrence of Historic Surface Ruptures and Implications for Hazard Modelling

In the fifty years between 1968 and 2018, eleven moderate magnitude reverse earthquakes caused surface ruptures in cratonic Australian. Nine of the ten events analyzed show evidence of rupture along pre-existing structures with little to no evidence of prior Neotectonic movement. While this does not preclude the possibility that evidence of prior rupture was removed prior to the late Pleistocene, the lack of topographic or geomorphic evidence supporting repeated rupture suggests historic surface ruptures may have occurred on faults that could be considered previously inactive in the Neotectonic period (e.g., [4]).

It is unclear whether the historic surface rupturing faults have entered a period of activity and will host future Neotectonic earthquakes, have occurred as isolated events, or have such long recurrence intervals as to obscure all evidence of prior rupture. Paleoseismic work across the Precambrian SCR crust (Figure 1) has shown that faults in similar settings as the historic ruptures have hosted multiple Neotectonic earthquakes [2,34,108], with available dating indicating long recurrence (>30–70 ka [2]), and low topography indicating erosion may outpace seismic slip-rate. In contrast, paleoseismic investigations in the Phanerozoic non-extended crust of eastern Australia identify multiple faults with recurrence frequent enough to maintain topography [3,5,34,101,107,109], despite no historic surface rupturing or large earthquakes in this part of the continent.

Historic surface rupture kinematics are all consistent with S_Hmax (as measured from bore-hole breakouts, drilling induce fractures, and focal mechanisms [100]) either directly (e.g., a straight fault perpendicular to S_Hmax) or indirectly (e.g., rupture occurred along multiple faults, some of which are aligned oblique to S_Hmax, but uplift of the hanging-wall block is perpendicular to S_Hmax). The past fifty years of historic surface rupturing events show that in the Precambrian non-extended crust, basement with at least one set of linear structures aligned with S_Hmax, or multiple conjugate basement structures, could host a shallow moderate magnitude surface rupturing earthquake along one or multiple (in these cases, previously unrecognized and typically unrecognizable) faults. Eight of eleven surface rupturing earthquakes have occurred in areas of (or proximal to) preceding seismicity, while three (Petermann, Pukatja and Marryat Creek) occurred in areas with low historic seismicity, though instrument density limits the magnitude of completeness and location accuracy and precision of the historic earthquake catalogue in these locations. This suggests that spatially smoothed (distributed) seismicity models may provide the best utility for seismic hazard analyses in the central and western parts of Australia (e.g., [161]). This is also relevant for assessments of earthquake hazard in Precambrian intraplate crust elsewhere (e.g., Canada [162,163,164]). Further work is required to understand tentative correlations between seismogenic potential and large geophysical anomalies and/or Moho discontinuities (e.g., [165,166]), and whether transient local stress perturbations increase the potential for shallow seismicity (e.g., changes in pore-fluid pressure [76] or surface load variations [4]).

The historic earthquake catalogue for Australia is complete for M_L > 5.5 since 1910, and M_L > 5.0 since 1960 [102]. The magnitude values of historic earthquakes were recently revised [11]. This new catalogue contains seven M_W > 5.5 on-shore earthquakes within the Precambrian non-extended crust that are not related to the historic surface rupturing events, and only one onshore event in the eastern Phanerozoic crust (Figure 1). The Precambrian crustal events include: four events (1941 M_w 5.6, 5.9, 6.5, and 1972 M_w 5.6) in the Simpson Desert NT [80,83,167], one event (1970 M_w 5.9) within the Lake Mackay WA sequence (20 events M_w 4.5–5.5 between 1970–1992) [23,81,83,167], one event 200 km south of Warburton WA (1975 M_w 5.6), and the 1941 M_w 6.8 Meeberrie WA event—Australia’s largest recorded onshore earthquake (Figure 1). No surface ruptures have been identified for these events. While depths are poorly constrained due to poor instrumental density, estimates range from 7–33 km [11,83], deeper than the best estimates of depth for surface rupturing events (1–4 km for centroids, <6 km for hypocentral/base of fault depth). This suggests that moderate magnitude and potentially damaging earthquakes (e.g., M_w > 5.5) can be generated at depths of up to 33 km within the Precambrian non-extended crust, providing another source of hazard that cannot be effectively captured by active-fault catalogues in seismic hazard analysis.

5. Conclusions

We provide new length, dip, and net-slip data derived using a consistent framework and methodology in order to facilitate more consistent integration of Australian events into earthquake catalogues and displacement-length scaling relationships. Our reanalysis of primary data from 67 publications on ten of eleven historical surface rupturing earthquakes in Australia shows:

Surface rupture fault orientations aligned with basement structures identified in proximal surface outcrops (foliations ± quartz veins ± intrusive boundaries ± pre-existing faults) and linear geophysical anomalies;
Rupture involve 1–6 discrete faults based on reanalysis of surface rupture lengths using consistent criteria, with evidence that intersecting basement structures may control rupture initiation and/or propagation;
Large aleatoric and epistemic uncertainties in seismological data, related to a sparse seismic network, limit determination of hypocenter and fault interaction, rupture propagation, and assessment of whether surface ruptures project to seismogenic depths along planar principle slip zones or whether rupture propagates to multiple basement structures in the near-surface;
Available analyses of rupture centroids (seven of ten events) show depths of 1–4 km indicating predominately shallow seismic moment release;
None of the historic surfacing rupturing events have unambiguous geological or geomorphic evidence for preceding earthquakes on the same faults, with five events showing an absence of rupture since at least the late Pleistocene;
Within the constraints of available basement erosion rates, preferred maximum slip rates are 0.2–9.1 m Myr⁻¹ with an estimated minimum epistemic uncertainty of at least one order of magnitude lower. These are considered applicable only within the non-extended Precambrian crust in which all historic surface ruptures have occurred;
ESI-07 estimates range by ±3 classes in each earthquake and provide new maximum ESI vs. magnitude data for comparison between different tectonic and geomorphic settings;

Supplementary Materials

The following are available online at https://www.mdpi.com/2076-3263/9/10/408/s1.

Author Contributions

Conceptualization, M.Q. and T.R.K.; methodology, T.R.K.; validation T.R.K. and D.C.; formal analysis, T.R.K.; investigation, T.R.K.; data curation T.R.K.; writing—original draft preparation, T.R.K.; writing—review and editing, T.R.K., M.Q. and D.C.; visualization, T.R.K. and M.Q.; supervision, M.Q.; project administration, T.R.K. and M.Q.; funding acquisition, M.Q.

Funding

This research was funded by the Australian Research Council through Discovery Grant #DP170103350. T. King received funding through the Australian Government Research Training Program Scholarship.

Acknowledgments

The authors thank the editors and three reviewers for comments that improved this work. We would like to acknowledge the Noongar people of south-west Western Australia, the Warumungu people of Tennant Creek, and the Antakirinja, Yankunytjatjara, and Pitjantjatjara people of the Western Desert and APY lands in South Australia/Northern Territory, as the traditional custodians of the land on which all historic surface ruptures occurred, and where the data described in this paper were collected. D. Clark publishes with the permission of the Chief Executive Officer of Geoscience Australia.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Map of Australia showing locations of historic surface rupturing events, continental scale crustal divisions [99], onshore historic seismology >4.0 (1840–2017) [11], simplified crustal stress trajectory map [100], GA neotectonic features database [95], recognized seismic zones [101,102] and specific crustal provinces relevant for surface rupture events (Table 3) [103]. Small maps show individual surface ruptures at the same scale and ordered by rupture length (excluding 2018 Lake Muir).

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King, T.R.; Quigley, M.; Clark, D. Surface-Rupturing Historical Earthquakes in Australia and Their Environmental Effects: New Insights from Re-Analyses of Observational Data. Geosciences 2019, 9, 408. https://doi.org/10.3390/geosciences9100408

AMA Style

King TR, Quigley M, Clark D. Surface-Rupturing Historical Earthquakes in Australia and Their Environmental Effects: New Insights from Re-Analyses of Observational Data. Geosciences. 2019; 9(10):408. https://doi.org/10.3390/geosciences9100408

Chicago/Turabian Style

King, Tamarah R., Mark Quigley, and Dan Clark. 2019. "Surface-Rupturing Historical Earthquakes in Australia and Their Environmental Effects: New Insights from Re-Analyses of Observational Data" Geosciences 9, no. 10: 408. https://doi.org/10.3390/geosciences9100408

APA Style

King, T. R., Quigley, M., & Clark, D. (2019). Surface-Rupturing Historical Earthquakes in Australia and Their Environmental Effects: New Insights from Re-Analyses of Observational Data. Geosciences, 9(10), 408. https://doi.org/10.3390/geosciences9100408

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Surface-Rupturing Historical Earthquakes in Australia and Their Environmental Effects: New Insights from Re-Analyses of Observational Data

Abstract

1. Introduction

2. Review Data, Methods and Terminology

3. Results

3.1. Geology

3.2. Seismology

3.3. Surface Ruptures

3.4. Environmental Damage

3.5. Paleoseismology and Slip Rate

4. Discussion-Lessons from the Last 50 Years of Australian Surface Ruptures

4.1. Inconsistancies in Data Use

4.2. Surface rupture Bedrock Controls, Updated Datasets and Environmental Intensity

4.3. Recurrence of Historic Surface Ruptures and Implications for Hazard Modelling

5. Conclusions

Supplementary Materials

Author Contributions

Funding

Acknowledgments

Conflicts of Interest

References

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