33:
523:
862:
702:
175:
385:. Similar folds tend to display thinning of the limbs and thickening of the hinge zone. Concentric folds are caused by warping from active buckling of the layers, whereas similar folds usually form by some form of shear flow where the layers are not mechanically active. Ramsay has proposed a classification scheme for folds that often is used to describe folds in profile based upon the curvature of the inner and outer lines of a fold and the behavior of
983:
millions of years, this process is capable of gathering large quantities of trace minerals from large expanses of rock and depositing them at very concentrated sites. This may be a mechanism that is responsible for the veins. To summarize, when searching for veins of valuable minerals, it might be wise to look for highly folded rock, and this is the reason why the mining industry is very interested in the theory of geological folding.
278:
2679:
779:
661:
310:
225:
507:
366:
141:
975:
694:
149:
515:
686:
676:
When a sequence of layered rocks is shortened parallel to its layering, this deformation may be accommodated in a number of ways, homogeneous shortening, reverse faulting or folding. The response depends on the thickness of the mechanical layering and the contrast in properties between the layers. If
873:: a competent layer or bed of rock can withstand an applied load without collapsing and is relatively strong, while an incompetent layer is relatively weak. When rock behaves as a fluid, as in the case of very weak rock such as rock salt, or any rock that is buried deeply enough, it typically shows
681:
layers in a less competent matrix control the folding and typically generate classic rounded buckle folds accommodated by deformation in the matrix. In the case of regular alternations of layers of contrasting properties, such as sandstone-shale sequences, kink-bands, box-folds and chevron folds are
268:
Minor folds are quite frequently seen in outcrop; major folds seldom are except in the more arid countries. Minor folds can, however, often provide the key to the major folds they are related to. They reflect the same shape and style, the direction in which the closures of the major folds lie, and
982:
Layers of rock that fold into a hinge need to accommodate large deformations in the hinge zone. This results in voids between the layers. These voids, and especially the fact that the water pressure is lower in the voids than outside of them, act as triggers for the deposition of minerals. Over
722:
Fault-bend folds are caused by displacement along a non-planar fault. In non-vertical faults, the hanging-wall deforms to accommodate the mismatch across the fault as displacement progresses. Fault bend folds occur in both extensional and thrust faulting. In extension, listric faults form
960:
The rheology of the layers being folded determines characteristic features of the folds that are measured in the field. Rocks that deform more easily form many short-wavelength, high-amplitude folds. Rocks that do not deform as easily form long-wavelength, low-amplitude folds.
901:
Flexural slip allows folding by creating layer-parallel slip between the layers of the folded strata, which, altogether, result in deformation. A good analogy is bending a phone book, where volume preservation is accommodated by slip between the pages of the book.
881:, because little resistance is offered): the strata appear shifted undistorted, assuming any shape impressed upon them by surrounding more rigid rocks. The strata simply serve as markers of the folding. Such folding is also a feature of many igneous intrusions and
826:
form in poorly consolidated sediments, they commonly undergo folding, particularly at their leading edges, during their emplacement. The asymmetry of the slump folds can be used to determine paleoslope directions in sequences of sedimentary rocks.
1507:
Reicherter, K.; Froitzheim, N.; Jarosinki, M.; Badura, J.; Franzke, H.-J.; Hansen, M.; HĂĽbscher, C.; MĂĽller, R.; Poprawa, P.; Reinecker, J.; Stackebrandt, W.; Voigt, T.; von
Eynatten, H.; Zuchiewicz, W. (2008).
865:
Flow folding: depiction of the effect of an advancing ramp of rigid rock into compliant layers. Top: low drag by a ramp: layers are not altered in thickness; Bottom: high drag: lowest layers tend to crumple.
933:, a form of metamorphic process, in which rocks shorten by dissolving constituents in areas of high strain and redepositing them in areas of lower strain. Folds generated in this way include examples in
251:. A fold axis “is the closest approximation to a straight line that when moved parallel to itself, generates the form of the fold.” (Ramsay 1967). A fold that can be generated by a fold axis is called a
321:
of each limb), called the interlimb angle. Gentle folds have an interlimb angle of between 180° and 120°, open folds range from 120° to 70°, close folds from 70° to 30°, and tight folds from 30° to 0°.
36:
Folds of alternate layers of limestone and chert occur in Greece. The limestone and chert were originally deposited as flat layers on the floor of a deep sea basin. These folds were produced by
995:, oil accumulating in the crest of the fold. Most anticlinal traps are produced as a result of sideways pressure, folding the layers of rock, but can also occur from sediments being compacted.
743:
are caused when displacement occurs on an existing fault without further propagation. In both reverse and normal faults this leads to folding of the overlying sequence, often in the form of a
801:
typically contain minor asymmetric folds, with the direction of overturning consistent with the overall shear sense. Some of these folds have highly curved hinge-lines and are referred to as
929:
If the folding deformation cannot be accommodated by a flexural slip or volume-change shortening (buckling), the rocks are generally removed from the path of the stress. This is achieved by
849:. In the case of high-level intrusions, near the Earth's surface, this deformation is concentrated above the intrusion and often takes the form of folding, as with the upper surface of a
201:
portions; the limbs are the flanks of the fold, and the limbs converge at the hinge zone. Within the hinge zone lies the hinge point, which is the point of minimum radius of
815:
Recently deposited sediments are normally mechanically weak and prone to remobilization before they become lithified, leading to folding. To distinguish them from folds of
991:
Anticlinal traps are formed by folding of rock. For example, if a porous sandstone unit covered with low permeability shale is folded into an anticline, it may form a
1596:
1347:
2016:
714:
Many folds are directly related to faults, associated with their propagation, displacement and the accommodation of strains between neighboring faults.
921:. Folding under this mechanism is typical of a similar fold style, as thinned limbs are shortened horizontally and thickened hinges do so vertically.
807:. Folds in shear zones can be inherited, formed due to the orientation of pre-shearing layering or formed due to instability within the shear flow.
67:. Folds in rocks vary in size from microscopic crinkles to mountain-sized folds. They occur as single isolated folds or in periodic sets (known as
731:
form whenever a thrust fault cuts up section from one detachment level to another. Displacement over this higher-angle ramp generates the folding.
32:
1381:
1707:
1673:
1521:
1427:
1393:
1357:
1330:
1204:
913:
Typically, folding is thought to occur by simple buckling of a planar surface and its confining volume. The volume change is accommodated by
893:
Folding of rocks must balance the deformation of layers with the conservation of volume in a rock mass. This occurs by several mechanisms.
1451:
625:
Parasitic: short-wavelength folds formed within a larger wavelength fold structure - normally associated with differences in bed thickness
2259:
1661:
1545:
1961:
1938:
1821:
1799:
1772:
1300:
1266:
1237:
1179:
1150:
1087:
833:
Compaction: Folds can be generated in a younger sequence by differential compaction over older structures such as fault blocks and
2713:
2009:
317:
Fold tightness is defined by the size of the angle between the fold's limbs (as measured tangential to the folded surface at the
236:
is defined as a plane connecting all the hinge lines of stacked folded surfaces. If the axial surface is planar, it is called an
110:. Folds are commonly formed by shortening of existing layers, but may also be formed as a result of displacement on a non-planar
1509:
2708:
2044:
186:
is the line joining points of maximum curvature on a folded surface. This line may be either straight or curved. The term
1697:
615:
Slump: typically monoclinal, the result of differential compaction or dissolution during sedimentation and lithification.
1635:
830:
Dewatering: Rapid dewatering of sandy sediments, possibly triggered by seismic activity, can cause convolute bedding.
2703:
2682:
2002:
1731:
338:
Not all folds are equal on both sides of the axis of the fold. Those with limbs of relatively equal length are termed
255:. This term has been broadened to include near-cylindrical folds. Often, the fold axis is the same as the hinge line.
1320:
577:
Recumbent: linear, fold axial plane oriented at a low angle resulting in overturned strata in one limb of the fold.
522:
2344:
269:
their cleavage indicates the attitude of the axial planes of the major folds and their direction of overturning
64:
2349:
2125:
1732:"Productive Large Scale Folding Associated with Igneous Intrusions: El Trapial Field, Neuquen Basin, Argentina"
2049:
2115:
1417:
1117:
861:
846:
665:
346:. Asymmetrical folds generally have an axis at an angle to the original unfolded surface they formed on.
2626:
2430:
2319:
2189:
2169:
2069:
2039:
755:
When a thrust fault continues to displace above a planar detachment without further fault propagation,
701:
677:
the layering does begin to fold, the fold style is also dependent on these properties. Isolated thick
2603:
2487:
2204:
2159:
1846:
1611:
1557:
1466:
1105:
678:
123:
87:
759:
may form, typically of box-fold style. These generally occur above a good detachment such as in the
2636:
2512:
2497:
2474:
2470:
2249:
2174:
2074:
2059:
724:
163:
1837:
Hudleston, P. J. (1977). "Similar folds, recumbent folds and gravity tectonics in ice and rocks".
2613:
2585:
2482:
2364:
2269:
2184:
2149:
2079:
2025:
1870:
1862:
1627:
938:
803:
370:
354:
45:
1765:
Folding of viscous layers: mechanical analysis and interpretation of structures in deformed rock
1482:
2621:
2555:
2507:
2502:
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2314:
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1957:
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1703:
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1060:
1014:
1004:
930:
607:
286:
159:
95:
1760:
1284:
1167:
618:
Ptygmatic: Folds are chaotic, random and disconnected. Typical of sedimentary slump folding,
2425:
2420:
2354:
2329:
2324:
2299:
2239:
2199:
2054:
1989:
1930:
1921:
1902:
1854:
1619:
1573:
1565:
1474:
1221:
1113:
1052:
597:
527:
318:
214:
210:
91:
79:
53:
1984:
1888:
957:, or method of response to stress, of the rock at the time at which the stress is applied.
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2560:
2460:
2435:
2407:
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2229:
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206:
111:
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72:
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37:
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365:
174:
2697:
2455:
1874:
1631:
1222:
152:
99:
83:
1388:. Vol. Special Publications 253. Geological Society, London. pp. 285–305.
905:
The fold formed by the compression of competent rock beds is called "flexure fold".
636:
involves strata dipping in the same direction, though not necessarily any folding.)
330:, have an interlimb angle of between 10° and zero, with essentially parallel limbs.
2450:
2110:
2084:
1024:
974:
950:
798:
791:
778:
343:
1950:
193:
A fold surface seen perpendicular to its shortening direction can be divided into
819:
origin, such structures are called synsedimentary (formed during sedimentation).
17:
2631:
2517:
2492:
2445:
2440:
2415:
2304:
2224:
2194:
1195:
Barnes, J. W.; Lisle, Richard J. (2013). "5 Field
Measurements and Techniques".
669:
660:
309:
2659:
2646:
2264:
2154:
1699:
Nontechnical guide to petroleum geology, exploration, drilling, and production
1569:
1478:
787:
298:
224:
1125:
1064:
574:: linear, strata dip in one direction between horizontal layers on each side.
389:. that is, lines connecting points of equal dip on adjacent folded surfaces:
2595:
2575:
2570:
2550:
2532:
2522:
2334:
2279:
2141:
1419:
Structural analysis and synthesis: a laboratory course in structural geology
934:
850:
767:
744:
645:
633:
619:
571:
539:
202:
140:
134:
130:
1139:
Ghosh, Subir Kumar; Naha, Kshitindramohan (1997). Sengupta, Sudipta (ed.).
693:
628:
Disharmonic: Folds in adjacent layers with different wavelengths and shapes
148:
562:: linear, strata dip away from the axial center, age unknown, or inverted.
218:
2654:
2580:
1255:"Figure 10.14: Classification of fold profiles using dip isogon patterns"
954:
816:
783:
764:
559:
549:
339:
209:
of the fold represents the highest point of the fold surface whereas the
155:
1866:
1452:"Style and sequence of deformation during extensional fault-propagation"
2387:
2339:
2284:
1009:
882:
845:
The emplacement of igneous intrusions tends to deform the surrounding
568:: linear, strata dip toward the axial center, age unknown, or inverted.
565:
127:
107:
56:
514:
2254:
2219:
1994:
294:
1597:"Paleoslope Analysis of Slump Folds in the Devonian Flysch of Maine"
685:
1858:
1623:
1382:"Geometric and experimental models of extensional fault-bend folds"
2274:
973:
860:
777:
700:
692:
684:
659:
364:
308:
276:
223:
173:
147:
139:
31:
1416:
Rowland, S. M.; Duebendorfer, E. M.; Schieflebein, I. M. (2007).
2309:
834:
1998:
102:. A set of folds distributed on a regional scale constitutes a
221:
reverses; on regular folds, this is the midpoint of the limb.
1974:: McGraw-Hill Book Company, New York, 560pp., ISBN 193066589X
357:
is calculated in a direction perpendicular to the fold axis.
1142:
Evolution of geological structures in micro- to macro-scales
590:: nonlinear, strata dip away from center in all directions,
1386:
Analogue and numerical modelling of crustal-scale processes
377:
Folds that maintain uniform layer thickness are classed as
1450:
Jackson, C. A. L.; Gawthorpe, R. L.; Sharp, I. R. (2006).
1285:"Figure 3.12: Fold classification based upon dip diagrams"
1096:
Donath, F. A.; Parker, R. B. (1964). "Folds and
Folding".
542:: linear, strata normally dip away from the axial center,
1352:. Vol. 2 (3 ed.). Academic Press. p. 392.
600:: nonlinear, strata dip toward center in all directions,
1078:
Davis, George H.; Reynolds, Stephen J. (1996). "Folds".
1662:"17. Sediments into rocks: post-depositional processes"
552:: linear, strata normally dip toward the axial center,
391:
75:
folds are those formed during sedimentary deposition.
1118:
10.1130/0016-7606(1964)75[45:FAF]2.0.CO;2
1082:. New York: John Wiley & Sons. pp. 372–424.
455:
Orthogonal thickness at limbs narrower than at hinge
435:
Orthogonal thickness at hinge narrower than at limbs
2645:
2612:
2594:
2541:
2469:
2406:
2363:
2139:
2098:
2032:
610:: angular fold with straight limbs and small hinges
289:, with planar limbs meeting at an angular axis, as
1949:
1929:. Upper Saddle River, NJ: Prentice Hall. pp.
1920:
1516:. Geological Society, London. pp. 1233–1285.
1043:Fleury, M. J. (1964). "The description of folds".
297:with a curved axis, or as elliptical with unequal
52:is a stack of originally planar surfaces, such as
1889:"Geological Folding and the Presence of Minerals"
144:Kink band folds in the Permian of New Mexico, USA
1948:Pollard, David D.; Fletcher, Raymond C. (2005).
1759:Johnson, Arvid M.; Fletcher, Raymond C. (1994).
1314:
1312:
869:The compliance of rock layers is referred to as
1730:Orchuela, I.; Lara, M. E.; Suarez, M. (2003).
1544:Carreras, J.; Druguet, E.; Griera, A. (2005).
217:of a fold is the point on a limb at which the
98:, and even as primary flow structures in some
2010:
1816:(2nd ed.). Macmillan. pp. 241–242.
1253:Price, Neville J.; Cosgrove, John W. (1990).
556:strata in center irrespective of orientation.
546:strata in center irrespective of orientation.
8:
1927:Physical Geography: A Landscape Appreciation
1422:(3 ed.). Wiley-Blackwell. p. 301.
1384:. In Buiter, S. J. H.; Schreurs, G. (eds.).
1349:The techniques of modern structural geology
1261:. Cambridge University Press. p. 246.
1224:Geological Structures and Maps: 3rd Edition
2017:
2003:
1995:
1380:Withjack, M. O.; Schlische, R. W. (2006).
1045:Proceedings of the Geologists' Association
342:, and those with highly unequal limbs are
1767:. Columbia University Press. p. 87.
518:A monocline at Colorado National Monument
90:, as evidenced by their presence in soft
1794:(3rd ed.). Routledge. p. 109.
1510:"19. Alpine Tectonics north of the Alps"
763:, where the detachment occurs on middle
521:
513:
505:
1919:McKnight, Tom L.; Hess, Darrel (2000).
1174:(3rd ed.). Routledge. p. 26.
1080:Structural Geology of Rocks and Regions
1035:
953:in which the rocks are located and the
949:Folds in the rock are formed about the
652:. They arise from a variety of causes.
393:Ramsay classification scheme for folds
1903:"Oil and gas traps - Energy Education"
1291:(3rd ed.). Routledge. p. 31
1098:Geological Society of America Bulletin
727:in their hanging walls. In thrusting,
126:or due to the effects of a high-level
118:), at the tip of a propagating fault (
78:Folds form under varied conditions of
1325:(3 ed.). Routledge. p. 33.
1220:Lisle, Richard J. (2004). "Folding".
1199:. John Wiley & Sons. p. 79.
1197:Basic geological mapping: 4th Edition
937:and areas with a strong axial planar
205:(maximum curvature) of the fold. The
190:has also been used for this feature.
7:
1810:"Figure 12.8: Passive shear folding"
1808:Twiss, R. J.; Moores, E. M. (1992).
1346:Ramsay, J. G.; Huber, M. I. (1987).
381:folds. Those that do not are called
2260:List of tectonic plate interactions
644:Folds appear on all scales, in all
27:Stack of originally planar surfaces
1952:Fundamentals of Structural Geology
369:Ramsay classification of folds by
25:
1922:"The Internal Processes: Folding"
1791:Foundations of structural geology
1289:Foundations of structural geology
1259:Analysis of geological structures
1172:Foundations of structural geology
622:and decollement detachment zones.
240:and can be described in terms of
2678:
2677:
1668:. Wiley-Blackwell. p. 355.
1595:Bradley, D.; Hanson, L. (1998).
1322:Foundation of Structural Geology
797:Shear zones that approximate to
1972:Folding and fracturing of rocks
1966:– via Archive Foundation.
1943:– via Archive Foundation.
1702:. PennWell Books. p. 598.
1956:. Cambridge University Press.
1666:Sedimentology and stratigraphy
1:
1550:Journal of Structural Geology
1514:The Geology of Central Europe
1459:Journal of Structural Geology
1057:10.1016/S0016-7878(64)80023-7
782:Dextral sense shear folds in
494:
484:
481:
472:
462:
459:
454:
452:
449:
444:
442:
439:
434:
432:
429:
424:
414:
411:
406:
400:
373:of dip isogons (red lines).
285:A fold can be shaped like a
1168:"Fold axis and axial plane"
917:the volume, which grows in
739:Fault propagation folds or
59:, that are bent or curved (
2730:
1546:"Shear zone-related folds"
510:An anticline in New Jersey
473:Dip isogons are parallel:
2673:
2345:Thick-skinned deformation
1570:10.1016/j.jsg.2004.08.004
1479:10.1016/j.jsg.2005.11.009
1145:. Springer. p. 222.
915:layer parallel shortening
735:Fault propagation folding
656:Layer-parallel shortening
450: 1C
440: 1B
430: 1A
361:Deformation style classes
213:is the lowest point. The
2350:Thin-skinned deformation
2126:Stereographic projection
2714:Deformation (mechanics)
2116:Orthographic projection
2099:Measurement conventions
2045:Lamé's stress ellipsoid
1512:. In McCann, T. (ed.).
648:, at all levels in the
94:, the full spectrum of
979:
866:
794:
774:Folding in shear zones
706:
705:Fault-propagation fold
698:
690:
673:
666:La Herradura Formation
530:
519:
511:
374:
314:
293:with curved limbs, as
282:
281:Chevron folds, Ireland
229:
179:
166:
145:
120:fault propagation fold
106:, a common feature of
41:
2627:Paleostress inversion
2320:Strike-slip tectonics
2190:Extensional tectonics
2170:Continental collision
2040:Deformation mechanism
1228:. Elsevier. pp.
977:
965:Economic implications
864:
781:
710:Fault-related folding
704:
696:
688:
663:
525:
517:
509:
425:Dip isogons converge
368:
312:
280:
227:
177:
151:
143:
35:
2709:Geological processes
2205:Fold and thrust belt
1970:Ramsay, J.G., 1967,
1788:Park, R. G. (1997).
1696:Hyne, N. J. (2001).
1660:Nichols, G. (1999).
1319:Park, R. G. (2004).
1283:Park, R. G. (2004).
1166:Park, R. G. (2004).
945:Mechanics of folding
931:pressure dissolution
822:Slump folding: When
811:Folding in sediments
495:Dip isogons diverge
259:Descriptive features
178:Fold sketch 3D model
88:temperature gradient
2637:Section restoration
2513:Rock microstructure
2175:Convergent boundary
2075:Strain partitioning
2060:Overburden pressure
2050:Mohr–Coulomb theory
1851:1977JG.....85..113H
1616:1998JG....106..305B
1562:2005JSG....27.1229C
1471:2006JSG....28..519J
1110:1964GSAB...75...45D
725:rollover anticlines
682:normally produced.
394:
350:Facing and vergence
164:Barstow, California
122:), by differential
63:) during permanent
2704:Structural geology
2614:Kinematic analysis
2270:Mountain formation
2185:Divergent boundary
2150:Accretionary wedge
2026:Structural geology
1839:Journal of Geology
1814:Structural geology
1604:Journal of Geology
1281:See, for example,
980:
978:anticline oil trap
889:Folding mechanisms
867:
795:
751:Detachment folding
718:Fault bend folding
707:
699:
691:
689:Rollover anticline
674:
531:
520:
512:
392:
375:
315:
283:
230:
180:
167:
146:
46:structural geology
42:
38:Alpine deformation
2691:
2690:
2622:3D fold evolution
2508:Pressure solution
2503:Oblique foliation
2383:Exfoliation joint
2373:Columnar jointing
2033:Underlying theory
1990:Oil and gas traps
1709:978-0-87814-823-3
1675:978-0-632-03578-6
1576:on 17 August 2012
1523:978-1-86239-264-9
1429:978-1-4051-1652-7
1395:978-1-86239-191-8
1359:978-0-12-576922-8
1332:978-0-7487-5802-9
1206:978-1-118-68542-6
1015:Mountain building
1005:3D fold evolution
993:hydrocarbons trap
925:Mass displacement
841:Igneous intrusion
640:Causes of folding
604:strata in center.
594:strata in center.
499:
498:
247:Folds can have a
228:Flank & hinge
160:Barstow Formation
96:metamorphic rocks
18:Folding (geology)
16:(Redirected from
2721:
2681:
2680:
2426:Detachment fault
2421:Cataclastic rock
2355:Thrust tectonics
2325:Structural basin
2300:Pull-apart basin
2240:Horst and graben
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1651:
1650:
1648:
1646:
1640:
1634:. Archived from
1601:
1592:
1586:
1585:
1583:
1581:
1572:. Archived from
1556:(7): 1229–1251.
1541:
1535:
1534:
1532:
1530:
1504:
1498:
1497:
1495:
1493:
1487:
1481:. Archived from
1456:
1447:
1441:
1440:
1438:
1436:
1413:
1407:
1406:
1404:
1402:
1377:
1371:
1370:
1368:
1366:
1343:
1337:
1336:
1316:
1307:
1306:
1279:
1273:
1272:
1250:
1244:
1243:
1227:
1217:
1211:
1210:
1192:
1186:
1185:
1163:
1157:
1156:
1136:
1130:
1129:
1093:
1075:
1069:
1068:
1040:
757:detachment folds
528:King Oscar Fjord
526:Recumbent fold,
395:
313:Interlimb angles
253:cylindrical fold
215:inflection point
170:Fold terminology
21:
2729:
2728:
2724:
2723:
2722:
2720:
2719:
2718:
2694:
2693:
2692:
2687:
2669:
2641:
2608:
2590:
2561:Detachment fold
2537:
2465:
2461:Transform fault
2436:Fault mechanics
2402:
2359:
2295:Plate tectonics
2245:Intra-arc basin
2135:
2106:Brunton compass
2094:
2028:
2023:
1981:
1964:
1947:
1941:
1918:
1915:
1913:Further reading
1910:
1901:
1900:
1896:
1887:
1886:
1882:
1836:
1835:
1831:
1824:
1807:
1802:
1787:
1786:
1782:
1775:
1758:
1757:
1753:
1743:
1741:
1734:
1729:
1728:
1724:
1714:
1712:
1710:
1695:
1694:
1690:
1680:
1678:
1676:
1659:
1658:
1654:
1644:
1642:
1641:on 17 July 2011
1638:
1599:
1594:
1593:
1589:
1579:
1577:
1543:
1542:
1538:
1528:
1526:
1524:
1506:
1505:
1501:
1491:
1489:
1488:on 16 June 2011
1485:
1454:
1449:
1448:
1444:
1434:
1432:
1430:
1415:
1414:
1410:
1400:
1398:
1396:
1379:
1378:
1374:
1364:
1362:
1360:
1345:
1344:
1340:
1333:
1318:
1317:
1310:
1303:
1282:
1280:
1276:
1269:
1252:
1251:
1247:
1240:
1219:
1218:
1214:
1207:
1194:
1193:
1189:
1182:
1165:
1164:
1160:
1153:
1138:
1137:
1133:
1095:
1090:
1077:
1076:
1072:
1042:
1041:
1037:
1033:
1001:
989:
972:
970:Mining industry
967:
947:
927:
911:
899:
891:
879:passive folding
859:
843:
813:
776:
753:
737:
729:ramp anticlines
720:
712:
658:
642:
584:
536:
504:
492:
488:
470:
466:
445:Parallel folds
422:
418:
363:
352:
336:
328:isoclinal folds
319:inflection line
307:
275:
266:
261:
172:
116:fault bend fold
28:
23:
22:
15:
12:
11:
5:
2727:
2725:
2717:
2716:
2711:
2706:
2696:
2695:
2689:
2688:
2686:
2685:
2674:
2671:
2670:
2668:
2667:
2662:
2657:
2651:
2649:
2643:
2642:
2640:
2639:
2634:
2629:
2624:
2618:
2616:
2610:
2609:
2607:
2606:
2600:
2598:
2592:
2591:
2589:
2588:
2583:
2578:
2573:
2568:
2563:
2558:
2553:
2547:
2545:
2539:
2538:
2536:
2535:
2530:
2528:Tectonic phase
2525:
2520:
2515:
2510:
2505:
2500:
2495:
2490:
2485:
2479:
2477:
2467:
2466:
2464:
2463:
2458:
2453:
2448:
2443:
2438:
2433:
2428:
2423:
2418:
2412:
2410:
2404:
2403:
2401:
2400:
2395:
2390:
2385:
2380:
2375:
2369:
2367:
2361:
2360:
2358:
2357:
2352:
2347:
2342:
2337:
2332:
2327:
2322:
2317:
2312:
2307:
2302:
2297:
2292:
2290:Passive margin
2287:
2282:
2277:
2272:
2267:
2262:
2257:
2252:
2247:
2242:
2237:
2232:
2227:
2222:
2217:
2215:Foreland basin
2212:
2210:Fold mountains
2207:
2202:
2197:
2192:
2187:
2182:
2177:
2172:
2167:
2165:Back-arc basin
2162:
2157:
2152:
2146:
2144:
2137:
2136:
2134:
2133:
2131:Strike and dip
2128:
2123:
2118:
2113:
2108:
2102:
2100:
2096:
2095:
2093:
2092:
2087:
2082:
2077:
2072:
2067:
2065:Rock mechanics
2062:
2057:
2052:
2047:
2042:
2036:
2034:
2030:
2029:
2024:
2022:
2021:
2014:
2007:
1999:
1993:
1992:
1987:
1980:
1979:External links
1977:
1976:
1975:
1968:
1962:
1945:
1939:
1914:
1911:
1909:
1908:
1894:
1880:
1859:10.1086/628272
1845:(1): 113–122.
1829:
1822:
1800:
1780:
1773:
1751:
1739:AAPG Abstracts
1722:
1708:
1688:
1674:
1652:
1624:10.1086/516024
1610:(3): 305–318.
1587:
1536:
1522:
1499:
1465:(3): 519–535.
1442:
1428:
1408:
1394:
1372:
1358:
1338:
1331:
1308:
1301:
1274:
1267:
1245:
1238:
1212:
1205:
1187:
1180:
1158:
1151:
1131:
1088:
1070:
1051:(4): 461–492.
1034:
1032:
1029:
1028:
1027:
1022:
1020:Rock mechanics
1017:
1012:
1007:
1000:
997:
988:
985:
971:
968:
966:
963:
946:
943:
926:
923:
910:
907:
898:
895:
890:
887:
858:
855:
842:
839:
812:
809:
775:
772:
761:Jura Mountains
752:
749:
741:tip-line folds
736:
733:
719:
716:
711:
708:
697:Ramp anticline
657:
654:
641:
638:
630:
629:
626:
623:
616:
613:
611:
605:
595:
583:
580:
579:
578:
575:
569:
563:
557:
547:
535:
532:
503:
500:
497:
496:
493:
490:
486:
483:
479:
478:
471:
468:
464:
461:
457:
456:
453:
451:
447:
446:
443:
441:
437:
436:
433:
431:
427:
426:
423:
420:
416:
413:
409:
408:
405:
399:
362:
359:
351:
348:
335:
332:
306:
305:Fold tightness
303:
274:
271:
265:
262:
260:
257:
242:strike and dip
171:
168:
108:orogenic zones
73:Synsedimentary
26:
24:
14:
13:
10:
9:
6:
4:
3:
2:
2726:
2715:
2712:
2710:
2707:
2705:
2702:
2701:
2699:
2684:
2676:
2675:
2672:
2666:
2663:
2661:
2658:
2656:
2653:
2652:
2650:
2648:
2644:
2638:
2635:
2633:
2630:
2628:
2625:
2623:
2620:
2619:
2617:
2615:
2611:
2605:
2602:
2601:
2599:
2597:
2593:
2587:
2584:
2582:
2579:
2577:
2574:
2572:
2569:
2567:
2564:
2562:
2559:
2557:
2554:
2552:
2549:
2548:
2546:
2544:
2540:
2534:
2531:
2529:
2526:
2524:
2521:
2519:
2516:
2514:
2511:
2509:
2506:
2504:
2501:
2499:
2496:
2494:
2491:
2489:
2486:
2484:
2481:
2480:
2478:
2476:
2472:
2468:
2462:
2459:
2457:
2456:Transfer zone
2454:
2452:
2449:
2447:
2444:
2442:
2439:
2437:
2434:
2432:
2429:
2427:
2424:
2422:
2419:
2417:
2414:
2413:
2411:
2409:
2405:
2399:
2396:
2394:
2391:
2389:
2386:
2384:
2381:
2379:
2376:
2374:
2371:
2370:
2368:
2366:
2362:
2356:
2353:
2351:
2348:
2346:
2343:
2341:
2338:
2336:
2333:
2331:
2328:
2326:
2323:
2321:
2318:
2316:
2313:
2311:
2308:
2306:
2303:
2301:
2298:
2296:
2293:
2291:
2288:
2286:
2283:
2281:
2278:
2276:
2273:
2271:
2268:
2266:
2263:
2261:
2258:
2256:
2253:
2251:
2248:
2246:
2243:
2241:
2238:
2236:
2233:
2231:
2228:
2226:
2223:
2221:
2218:
2216:
2213:
2211:
2208:
2206:
2203:
2201:
2198:
2196:
2193:
2191:
2188:
2186:
2183:
2181:
2178:
2176:
2173:
2171:
2168:
2166:
2163:
2161:
2158:
2156:
2153:
2151:
2148:
2147:
2145:
2143:
2138:
2132:
2129:
2127:
2124:
2122:
2119:
2117:
2114:
2112:
2109:
2107:
2104:
2103:
2101:
2097:
2091:
2088:
2086:
2083:
2081:
2078:
2076:
2073:
2071:
2068:
2066:
2063:
2061:
2058:
2056:
2055:Mohr's circle
2053:
2051:
2048:
2046:
2043:
2041:
2038:
2037:
2035:
2031:
2027:
2020:
2015:
2013:
2008:
2006:
2001:
2000:
1997:
1991:
1988:
1986:
1985:Mark Peletier
1983:
1982:
1978:
1973:
1969:
1965:
1963:0-521-83927-0
1959:
1954:
1953:
1946:
1942:
1940:0-13-020263-0
1936:
1932:
1928:
1923:
1917:
1916:
1912:
1904:
1898:
1895:
1890:
1884:
1881:
1876:
1872:
1868:
1864:
1860:
1856:
1852:
1848:
1844:
1840:
1833:
1830:
1825:
1823:0-7167-2252-6
1819:
1815:
1811:
1803:
1801:0-7487-5802-X
1797:
1793:
1792:
1784:
1781:
1776:
1774:0-231-08484-6
1770:
1766:
1762:
1755:
1752:
1740:
1733:
1726:
1723:
1711:
1705:
1701:
1700:
1692:
1689:
1677:
1671:
1667:
1663:
1656:
1653:
1637:
1633:
1629:
1625:
1621:
1617:
1613:
1609:
1605:
1598:
1591:
1588:
1575:
1571:
1567:
1563:
1559:
1555:
1551:
1547:
1540:
1537:
1525:
1519:
1515:
1511:
1503:
1500:
1484:
1480:
1476:
1472:
1468:
1464:
1460:
1453:
1446:
1443:
1431:
1425:
1421:
1420:
1412:
1409:
1397:
1391:
1387:
1383:
1376:
1373:
1361:
1355:
1351:
1350:
1342:
1339:
1334:
1328:
1324:
1323:
1315:
1313:
1309:
1304:
1302:0-7487-5802-X
1298:
1294:
1290:
1286:
1278:
1275:
1270:
1268:0-521-31958-7
1264:
1260:
1256:
1249:
1246:
1241:
1239:0-7506-5780-4
1235:
1231:
1226:
1225:
1216:
1213:
1208:
1202:
1198:
1191:
1188:
1183:
1181:0-7487-5802-X
1177:
1173:
1169:
1162:
1159:
1154:
1152:0-412-75030-9
1148:
1144:
1143:
1135:
1132:
1127:
1123:
1119:
1115:
1111:
1107:
1103:
1099:
1091:
1089:0-471-52621-5
1085:
1081:
1074:
1071:
1066:
1062:
1058:
1054:
1050:
1046:
1039:
1036:
1030:
1026:
1023:
1021:
1018:
1016:
1013:
1011:
1008:
1006:
1003:
1002:
998:
996:
994:
986:
984:
976:
969:
964:
962:
958:
956:
952:
944:
942:
940:
936:
932:
924:
922:
920:
916:
908:
906:
903:
897:Flexural slip
896:
894:
888:
886:
884:
880:
877:(also called
876:
872:
863:
856:
854:
852:
848:
840:
838:
836:
831:
828:
825:
820:
818:
810:
808:
806:
805:
800:
793:
789:
785:
780:
773:
771:
769:
766:
762:
758:
750:
748:
746:
742:
734:
732:
730:
726:
717:
715:
709:
703:
695:
687:
683:
680:
671:
667:
662:
655:
653:
651:
647:
639:
637:
635:
627:
624:
621:
617:
614:
612:
609:
606:
603:
599:
596:
593:
589:
586:
585:
581:
576:
573:
570:
567:
564:
561:
558:
555:
551:
548:
545:
541:
538:
537:
533:
529:
524:
516:
508:
502:Types of fold
501:
480:
476:
458:
448:
438:
428:
410:
404:
397:
396:
390:
388:
384:
383:similar folds
380:
372:
367:
360:
358:
356:
349:
347:
345:
341:
334:Fold symmetry
333:
331:
329:
325:
320:
311:
304:
302:
300:
296:
292:
288:
279:
272:
270:
263:
258:
256:
254:
250:
245:
243:
239:
235:
234:axial surface
226:
222:
220:
216:
212:
208:
204:
200:
196:
191:
189:
185:
176:
169:
165:
161:
157:
154:
153:Rainbow Basin
150:
142:
138:
136:
133:e.g. above a
132:
129:
125:
121:
117:
113:
109:
105:
101:
100:igneous rocks
97:
93:
89:
85:
84:pore pressure
81:
76:
74:
70:
66:
62:
58:
55:
51:
47:
39:
34:
30:
19:
2542:
2451:Thrust fault
2140:Large-scale
2111:Inclinometer
2085:Stress field
1971:
1951:
1926:
1897:
1883:
1842:
1838:
1832:
1813:
1790:
1783:
1764:
1761:"Figure 2.6"
1754:
1742:. Retrieved
1738:
1725:
1713:. Retrieved
1698:
1691:
1679:. Retrieved
1665:
1655:
1643:. Retrieved
1636:the original
1607:
1603:
1590:
1578:. Retrieved
1574:the original
1553:
1549:
1539:
1527:. Retrieved
1513:
1502:
1490:. Retrieved
1483:the original
1462:
1458:
1445:
1433:. Retrieved
1418:
1411:
1399:. Retrieved
1385:
1375:
1363:. Retrieved
1348:
1341:
1321:
1292:
1288:
1277:
1258:
1248:
1223:
1215:
1196:
1190:
1171:
1161:
1141:
1134:
1104:(1): 45–62.
1101:
1097:
1079:
1073:
1048:
1044:
1038:
1025:Thrust fault
990:
987:Oil industry
981:
959:
951:stress field
948:
928:
918:
914:
912:
904:
900:
892:
878:
875:flow folding
874:
870:
868:
857:Flow folding
847:country rock
844:
832:
829:
821:
814:
804:sheath folds
802:
799:simple shear
796:
792:Cap de Creus
754:
740:
738:
728:
721:
713:
675:
664:Box fold in
643:
631:
601:
591:
553:
543:
474:
402:
386:
382:
378:
376:
353:
344:asymmetrical
337:
327:
323:
316:
290:
284:
267:
252:
248:
246:
237:
233:
231:
198:
194:
192:
187:
183:
181:
119:
115:
103:
77:
68:
60:
49:
43:
29:
2632:Paleostress
2518:Slickenside
2493:Crenulation
2446:Fault trace
2441:Fault scarp
2431:Disturbance
2416:Cataclasite
2305:Rift valley
2225:Half-graben
2195:Fault block
2180:DĂ©collement
670:Morro Solar
387:dip isogons
371:convergence
340:symmetrical
238:axial plane
69:fold trains
65:deformation
54:sedimentary
2698:Categories
2660:Pure shear
2647:Shear zone
2604:Competence
2488:Compaction
2365:Fracturing
2160:Autochthon
2155:Allochthon
1744:31 October
1715:1 November
1681:31 October
1645:31 October
1580:31 October
1529:31 October
1492:1 November
1435:1 November
1401:31 October
1365:1 November
935:migmatites
871:competence
788:shear zone
768:evaporites
646:rock types
620:migmatites
401:Curvature
379:concentric
299:wavelength
273:Fold shape
188:hinge line
184:fold hinge
124:compaction
2596:Boudinage
2576:Monocline
2571:Homocline
2551:Anticline
2533:Tectonite
2523:Stylolite
2498:Fissility
2475:lineation
2471:Foliation
2335:Syneclise
2280:Obduction
2250:Inversion
2142:tectonics
1875:129424734
1632:129086677
1126:0016-7606
1065:0016-7878
919:thickness
851:laccolith
786:within a
784:mylonites
745:monocline
679:competent
634:homocline
572:Monocline
540:Anticline
482: 3
460: 2
412: 1
324:Isoclines
264:Fold size
249:fold axis
219:concavity
203:curvature
135:laccolith
131:intrusion
104:fold belt
92:sediments
2683:Category
2655:Mylonite
2586:Vergence
2581:Syncline
2483:Cleavage
2408:Faulting
1867:30068680
999:See also
955:rheology
939:cleavage
909:Buckling
817:tectonic
765:Triassic
602:youngest
560:Antiform
554:youngest
550:Syncline
407:Comment
355:Vergence
295:circular
156:syncline
61:"folded"
2556:Chevron
2543:Folding
2388:Fissure
2340:Terrane
2285:Orogeny
2265:MĂ©lange
2200:Fenster
2090:Tension
1847:Bibcode
1612:Bibcode
1558:Bibcode
1467:Bibcode
1106:Bibcode
1010:Orogeny
883:glacier
608:Chevron
566:Synform
475:similar
291:cuspate
287:chevron
158:in the
128:igneous
2330:Suture
2315:Saddle
2255:Klippe
2220:Graben
2080:Stress
2070:Strain
1960:
1937:
1931:409–14
1873:
1865:
1820:
1798:
1771:
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1672:
1630:
1520:
1426:
1392:
1356:
1329:
1299:
1265:
1236:
1203:
1178:
1149:
1124:
1094:after
1086:
1063:
824:slumps
672:, Peru
592:oldest
544:oldest
534:Linear
489:< C
477:folds
419:> C
211:trough
86:, and
80:stress
57:strata
2665:Shear
2393:Joint
2275:Nappe
2235:Horst
2230:Horse
1871:S2CID
1863:JSTOR
1735:(PDF)
1639:(PDF)
1628:S2CID
1600:(PDF)
1486:(PDF)
1455:(PDF)
1031:Notes
885:ice.
835:reefs
650:crust
598:Basin
582:Other
491:outer
487:inner
469:outer
465:inner
421:outer
417:inner
398:Class
326:, or
207:crest
195:hinge
162:near
112:fault
2566:Dome
2473:and
2398:Vein
2378:Dike
2310:Rift
2121:Rake
1958:ISBN
1935:ISBN
1818:ISBN
1796:ISBN
1769:ISBN
1746:2009
1717:2009
1704:ISBN
1683:2009
1670:ISBN
1647:2009
1582:2009
1531:2009
1518:ISBN
1494:2009
1437:2009
1424:ISBN
1403:2009
1390:ISBN
1367:2009
1354:ISBN
1327:ISBN
1297:ISBN
1263:ISBN
1234:ISBN
1201:ISBN
1176:ISBN
1147:ISBN
1122:ISSN
1084:ISBN
1061:ISSN
588:Dome
232:The
199:limb
197:and
182:The
50:fold
48:, a
1855:doi
1620:doi
1608:106
1566:doi
1475:doi
1114:doi
1053:doi
632:(A
467:= C
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